PhD Thesis SJB Dec_04

Platinum-Group Element Mineralization in Nipissing Gabbro

Intrusions and the River Valley Intrusion, Sudbury Region, Ontario

VOLUME I

(Spine title: PGE in Nipissing Gabbro and River Valley Intrusions - Vol I)

(Thesis format: Monograph)

by

Laurence Scott Jobin-Bevans

Graduate Program in Geology Department of Earth Sciences

A thesis submitted in partial fulfillment of the requirements for the degree of

Doctor of Philosophy

Faculty of Graduate Studies The University of Western Ontario

London, Ontario, Canada

© Laurence Scott Jobin-Bevans 2004

ABSTRACT

The ~2.5 Ga River Valley intrusion is one of several Early Proterozoic layered mafic

intrusions that, along with the ~2.2 Ga Nipissing Gabbro suite of intrusions, form the

dominant mafic intrusive bodies within the Huronian Magmatic Belt, in the Sudbury

Region, Ontario. These intrusive suites present excellent exploration targets for PGE-Cu-

Ni sulphide mineralization.

In the River Valley intrusion, the Marginal Series rocks are host to magmatic, low-

sulphide, Cu-PGE-rich mineralization that is associated with heterogeneous fragment-

bearing rocks (Breccia Unit). The Breccia Unit is up to 100 m wide and occurs within a

few metres of the intrusive contact. It is characterized by pyroxenitic fragments hosted

by a gabbroic matrix. The geochemistry of the fragments indicates that they are

xenoliths, entrained in the magmas that now constitute the matrix and PGE-rich sulphide

mineralization. PGE-rich sulphide, which is predominant in the matrix but also occurs in

the fragments, was introduced to the intrusion as suspended droplets in a second-stage

magma.

The Nipissing Gabbro represents the intrusive portion of an eroded Continental

Flood Basalt. Low-sulphide, Cu-PGE-rich mineralization is best represented by

stratabound sulphides that occur in the lowermost orthopyroxene gabbro unit.

Chalcophile element variations through mineralized and poorly differentiated intrusions

indicate in-situ sulphide fractionation from the base upwards, whereas other intrusions

exhibit simultaneous inward-directed sulphide precipitation from the base and top of the

sill.

Evidence for significant crustal contamination of the mantle-derived parental

magmas (high (Th/Nb)N), the high PGE tenor of the sulphides, and the lack of PGE-

depletion in the rock units that overly the Breccia Unit at River Valley, suggests that the

sulphides formed in a deep seated “staging chamber”. Here, primitive mantle-derived

magma assimilated crustal rocks and became crustally contaminated which induced S-

saturation and co-precipitation of PGE-rich sulphides and olivine-orthopyroxene

cumulates. When new primitive magma flowed into the staging chamber it displaced the

initial magma and the early-formed cumulates (fragments) and PGE-rich sulphides were

carried upwards in pregnant magmas and emplaced into the River Valley chamber.

iii

Adiabatic decompression in the ascending magma permitted some of the S in the

sulphide melts to dissolve into the magma; PGE would have also remained in the residual

sulphides leading to an increase in the PGE tenor. Evidence for PGE depletion in rocks

overlying PGE-rich mineralized zones in Nipissing Gabbro suggests that the sulphides

went into solution rather than being entrained as droplets in the ascending magmas.

Keywords: Platinum-group elements, Nipissing Gabbro, Nipissing Diabase, River Valley

Intrusion, East Bull Lake Suite, Contact-type, Marginal Series, Chalcophile element,

Southern Province, Continental Flood Basalt, Staging Chamber, Boninite.

iv

ACKNOWLEDGEMENTS

This research project represents a contribution to ongoing investigations into the

characterization of the Huronian Magmatic Province in Ontario, including research at

Laurentian University and the Ontario Geological Survey. This project benefited in part

from funding through an NSERC grant to Dr. Reid Keays and logistical support and

funding in-kind was provided by the Ontario Geological Survey (Dr. Andy Fyon). I am

especially indebted to Anglo American Platinum Corporation Ltd. (Gordon Chunnett and

Ron Hieber), Goldwright Explorations Inc. (Sudbury), and Pacific North West Capital

Corp. for their contributions to field support and sample analysis, and for the use of their

geological database. The author thanks prospectors J. Rauhala, M. Kosovsky, B. Wright,

M. Turcott, F. Racicot, D. Brunne, J. Morgan, R. Huggins, C. Johnson, T. Loney, M.

Loney, G. Salo, and H. Tracanelli, along with Mustang Minerals Corp. (Ken Lapierre)

and Ursa Major Minerals Inc. (Richard Sutcliffe) for their co-operation in accessing

many of the sulphide occurrences. Invaluable field assistance was rendered by

Christopher Jobin-Bevans, Bill Jobin-Bevans, Teslin d’Canine, Grant Mourre, Chris

Gauld, Trevor Richardson, David Lyon, Cecil Johnson, Richard Rintala, Joerg

Kleinboeck, and Steve Wetherup.

I gratefully acknowledge the support from the Department of Earth Sciences,

Laurentian University and in particular Dr. Richard James, who has been researching

East Bull Lake suite intrusions for nearly 20 years, and Dr. Andy MacDonald and Nicole

Tardif for the use of a petrographic microscope. A special thanks to Dr. Michael Lesher

for his constant encouragement, to Troy Richardson and Merilla Clement at the

Geoscience Laboratories for their cooperation, Dr. Michael Easton for his feedback and

discussion on the topic, and Alliance Pacific Resources Inc. for their patience.

Most importantly, I thank my wife Marnie and my son Christopher for their immense

support, patience and understanding over the past seven years. I also thank my parents

(Bill and Onalee), my brothers (Dean and Sandy), and my in-laws (June and Doug) who

have always been there, offering their support and encouragement. I am also grateful to

Dr. David Peck for suggesting the project area, stimulating my interest in PGE and

introducing me to Dr. Reid Keays; and to Dr. Reid Keays and Dr. Neil MacRae for their

support throughout this process and who’s guidance and input has been invaluable.

v

TABLE OF CONTENTS

CERTIFICATE OF EXAMINATION ii

ABSTRACT iii

ACKNOWLEDGEMENTS v

TABLE OF CONTENTS vi

LIST OF TABLES xii

LIST OF FIGURES xv

LIST OF PHOTOS xxiv

VOLUME I

CHAPTER 1: INTRODUCTION 1

1.1 General Statement of Objectives 1

1.2 Location and Access 6

1.3 Previous Geological Work 7

1.4 Terminology 9

1.4.1 Abbreviations 10

CHAPTER 2: COURSE OF INVESTIGATION 12

2.1 Field Work 12

2.2 Geochemical and Petrographic Analysis 13

2.3 Presentation and Interpretation of Geochemical Data 15

2.3.1 Presentation and Interpretation 15

2.3.2 Element Mobility 18

2.3.3 Archaean Tectonics and Mantle Chemistry 18

2.3.4 Partition Coefficients 19

2.3.5 Mass Balance (R Factor) Calculations 19

CHAPTER 3: REGIONAL GEOLOGY 21

3.1 General Geology 21

3.2 Huronian Supergroup 24

3.2.1 Elliot Lake Group 24

3.2.2 Hough Lake, Quirke Lake and Cobalt Groups 26

vi

3.2.3 Development of the Huronian Supergroup 26

3.2.4 Regional Correlation of the Huronian Supergroup 30

3.3 East Bull Lake Suite and Associated Rocks 32

3.3.1 Emplacement Models and Depth 36

3.3.2 Geochemistry and Magma Composition 39

3.3.3 Sulphide Mineralization 42

3.3.4 Platinum-Group Minerals 43

3.3.5 Sulphide and PGE Formation 44

3.4 Nipissing Gabbro Suite and Associated Rocks 46

3.5 Matachewan and Hearst Dike Swarms 49

3.6 Sudbury Dike Swarm and Grenville Dike Swarm 49

3.7 Sudbury Igneous Complex 50

3.8 Regional Metamorphism and Structure 50

3.8.1 Regional Albitization 51

3.8.2 Murray Fault System 52

CHAPTER 4: NIPISSING GABBRO INTRUSIONS 54

4.1 General Geology and Regional Morphology 54

4.1.1 Local Morphology 54

4.2 General Stratigraphy 58

4.2.1 Lower & Upper Quartz Diabase-Gabbro Units 64

4.2.2 Orthopyroxene Gabbro (Gabbronorite) Unit 66

4.2.3 Gabbro Unit 67

4.2.4 Gabbro-Leucogabbro Unit 71

4.2.5 Vari-Textured Gabbro Unit 71

4.2.6 Granophyric Gabbro Unit 73

4.3 Petrography and Mineralogy 77

4.3.1 Lower & Upper Quartz Diabase-Gabbro Units 78

4.3.2 Orthopyroxene Gabbro (Gabbronorite) Unit 78

4.3.3 Gabbro Unit 82

4.3.4 Gabbro-Leucogabbro Unit 82

4.3.5 Vari-Textured Gabbro Unit 82

vii

4.3.6 Granophyric Gabbro Unit 82

4.4 Mineral Chemistry 83

4.4.1 Olivine 83

4.4.2 Plagioclase 84

4.4.3 Pyroxene 84

4.4.4 Sulphides 85

4.4.5 Platinum-Group Minerals 85

4.5 General Geochemistry 88

4.5.1 Emplacement Model for Nipissing Gabbro 89

4.6 Mineralization 93

CHAPTER 5: CONSIDERED NIPISSING GABBRO INTRUSIONS 98

5.1 Introduction and Overview 98


5.2.1 Major Element Variations 106

5.2.2 Trace Element Variations 108

5.2.3 Chalcophile (PGE, Cu, Ni) Element Variations 123

5.2.4 Modelling of Sulphide Compositions 141

5.3 Basswood Lake Intrusion – Traverse 143

5.3.1 Geology and Mineralization 144


5.3.3 Trace and Rare-Earth Element Variations 150


5.4 Appleby Lake Intrusion – Traverse 158





5.5 Charlton Lake Intrusion – Traverse 169




viii


5.6 AN3 Occurrence and Traverse 184





5.7 Bell Lake Intrusion – Traverse 195





5.8 Makada Lake Intrusion – Traverse 210





5.9 Makada Lake Intrusion – Drill Hole A1-97 232

5.9.1 Chalcophile (PGE, Cu, Ni) and Trace Element Variations 232

5.10 Kukagami Lake Intrusion – Traverse 239





5.11 Manitou Lake Intrusion – Traverse 263





5.12 Chiniguchi River Intrusion – Detail 268



ix



5.13 Rastall Occurrence – Drill Holes JR99-01 and 06 295



5.14 Summary 315

VOLUME II

CHAPTER 6: RIVER VALLEY INTRUSION 318

6.1 Introduction 318

6.2 General Geology of the River Valley Intrusion 318

6.2.1 External Contacts 320

6.2.2 Country Rocks 321

6.2.3 Structure, Deformation and Metamorphism 323

6.3 Stratigraphy, Mineral Chemistry and Petrography 324


6.5 Marginal Series Stratigraphy, Mineralization and Geochemistry 329

6.5.1 General Geochemistry 340

6.6 Petrology and Geochemistry of Drill Hole RV00-22 342





6.7 Petrology and Geochemistry of the Breccia Unit 385





6.8 Modelling of Sulphide Compositions 421

6.9 Summary 424

CHAPTER 7: DISCUSSION AND PETROGENESIS 429

x

7.1 Summary and Implications 429

7.2 Parental Magmas and Contamination 430

7.3 Pregnant Magmas 436

7.4 Genetic Model 437

7.5 Implications to Mineral Exploration 445

REFERENCES 448

APPENDIX I: Specimen Descriptions, Whole-rock and CIPW Data 473

APPENDIX II: Petrographic Descriptions 538

APPENDIX III: Diamond Drill Hole Data Listing and Drill Core Logs 558

VITA 572

xi

LIST OF TABLES

Table 3-1. Tectono-metamorphic history of the Southern Province. 22

Table 3-2. Summary of geochronology for East Bull Lake intrusive suite 34

Table 3-3. Summary of platinum-group minerals in River Valley intrusion 45

Table 3-4. Summary of geochronology for Nipissing Gabbro intrusions 47

Table 5-1. Summary of sample locations in Nipissing Gabbro intrusions 101

Table 5-2. Summary of geochemical characteristics, Nipissing Gabbro rocks 103

Table 5-3. Summary of CIPW normative calculations, Nipissing gabbro rocks 105

Table 5-4. Summary of rare-earth elements features for Nipissing Gabbro rocks 110

Table 5-5. Summary of average chalcophile metals and ratios for all Nipissing

Gabbro samples 124

Table 5-6. Summary of average chalcophile metals and ratios from 59

unmineralized (<0.05 wt% S) Nipissing Gabbro samples 125

Table 5-7. Summary of average chalcophile metals and ratios from 24

mineralized (>0.05 wt% S) Nipissing Gabbro samples 125

Table 5-8. Summary of whole-rock geochemical characteristics for samples from

the Basswood Lake intrusion 146


the Appleby Lake intrusion 160


the Charlton Lake intrusion 171


the AN3 sample section, Casson Lake 188

Table 5-12. Summary of the highest concentrations of PGE-Au-Cu-Ni from

historical sampling of the Charlton Lake sill 189


the Bell Lake intrusion 197


the Makada Lake intrusion 213

Table 5-15. Summary of chalcophile element concentrations and ratios for

xii

core samples, drill hole A1-97, Rauhala property 237


the Kukagami Lake intrusion 243

Table 5-17. Summary of diamond drill core assay results from the

Washagami Lake occurrence 248


the Manitou Lake intrusion 265


the Chiniguchi River intrusion 270

Table 5-20. Summary of drill core assay results from the Rastall occurrence

in the Chiniguchi River intrusion 277

Table 5-21. Summary of surface channel sample assay results from the

Rastall occurrence in the Chiniguchi River intrusion 278

Table 5-22. Summary of drill core assay results from the Sargesson Lake

occurrence in the Sargesson Lake intrusion 279

Table 5-23. Summary of drill hole data for the composite drill hole, comprising

drill holes JR99-01 and JR99-06, Rastall occurrence 297

Table 6-1. Average and median values and ratios for whole-rock PGE and base

metal concentrations, Marginal Series rocks, River Valley Intrusion 331

Table 6-2ab. Summary of drill core log for drill hole RV00-22, Dana North

Deposit, River Valley intrusion 343

Table 6-3. Average whole-rock chalcophile element concentrations for core

samples from drill hole RV00-22, River Valley intrusion 344

Table 6-4. Geochemical data from drill hole RV00-22, Dana North Deposit

River Valley intrusion. 351

Table 6-5. CIPW normative calculations for samples from drill hole RV00-22 352

Table 6-6. Principal features of trace and REE abundances and ratios for each

of the units intersected in drill hole RV00-22 357

Table 6-7. Summary of average chalcophile metals and Au, and important metal

ratios for core from drill hole RV00-22 367

Table 6-8. Summary of matrix and fragment samples, River Valley intrusion. 391

xiii

Table 6-9. Summary of whole-rock geochemistry for matrix and fragment

samples, River Valley, intrusion. 394

Table 6-10. CIPW normative calculations for matrix and fragment samples from

the Central and South zones, River Valley intrusion 395

Table 6-11. Principal features of trace and REE abundances and ratios for matrix

and fragment samples from River Valley intrusion 402

Table 6-12. Absolute and average chalcophile abundances and important ratios

for matrix and fragment samples, River Valley intrusion 408

Table 6-13. Chalcophile abundances and ratios for matrix and fragment samples

from the River Valley intrusion 409

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LIST OF FIGURES

Figure 1-1. Regional Geology and location of the study area 2

Figure 1-2. Geology and location of specific intrusions in the study 3

Figure 3-1. Distribution of Early Proterozoic supracrustal rocks in the Great

Lakes Region and correlations with rocks in the study area 23

Figure 3-2. Generalized stratigraphic section through the Huronian Supergroup 22

Figure 3-3. Schematic diagrams showing the successive stages in the palaeotectonic

model for the development of the Huronian Supergroup 28

Figure 3-4. Geological map of the eastern Canadian Shield showing locations of

major anorthosite massifs and the River Valley intrusion 33

Figure 3-5. Correlation between Archaean-Palaeoproterozoic rocks in the study area

and those of the northern Fennoscandian shield, Finland 37

Figure 3-6. Schematic representation of the exposed crustal section in the River

Valley area. east of Sudbury 38

Figure 3-7. Primitive mantle-normalized rare earth element diagrams for samples

from the East Bull Lake suite of intrusions 40

Figure 4-1. Schematic cross-section through a typical undulating Nipissing Gabbro

sill, showing the distribution of lithologies 57

Figure 4-2. Type-section showing the typical sequence of lithologies and features

through a well-differentiated Nipissing Gabbro intrusion 60

Figure 4-3. Model for the evolution of a Nipissing Gabbro sill through the process

of assimilation-fractional crystallization (AFC) 90

Figure 4-4. Model for the development of undulatory Nipissing Gabbro intrusions 91

Figure 4-5. Regional distribution of mineralization in Nipissing Gabbro intrusions

between Lake Temagami and Sault Ste. Marie 95

Figure 5-1. Regional geology in the area east of Sudbury 100

Figure 5-2. AFM diagram for samples from the Nipissing Gabbro rocks 107

Figure 5-3. Variation in Mg-number versus TiO2. 109

Figure 5-4. Primitive mantle-normalized multi-element diagrams for Group-1 data 111

Figure 5-5. Primitive mantle-normalized multi-element diagrams for Group-2 data 112

xv

Figure 5-6. Primitive mantle-normalized multi-element diagrams for chilled

margin gabbro samples 113

Figure 5-7. Mixing curves for primitive mantle-normalized values of (Th/Yb)N

and (Nb/Th)N using 150 unmineralized and mineralized samples 115

Figure 5-8. Chondrite-normalized REE diagrams for Group-1 data 117

Figure 5-9. Chondrite-normalized REE diagrams for Group-2 data 118

Figure 5-10. Chondrite-normalized REE diagrams for chilled gabbro samples 119

Figure 5-11. Plot of Zr/Sm versus Nb/Ta ratios for 50 Nipissing Gabbro rocks 121

Figure 5-12a. Bivariate plots of whole-rock Pd-Pt and Cu-Pd 126

Figure 5-12b. Bivariate plots of whole-rock Cu-Pt and Ni-Pt 127

Figure 5-13a. Bivariate plots of whole-rock S/Se versus Pd 129

Figure 5-13bc. Bivariate plots of whole-rock (La/Sm)N-Pd. and (Th/Nb)N-Pd 130

Figure 5-14. Bivariate scatter diagram of MgO versus Ir 132

Figure 5-15a. Discrimination diagram of Ni/Cu versus Pd/Ir 134

Figure 5-15b. Discrimination diagram of Cu/Ir versus Ni/Pd 135

Figure 5-16. Discrimination diagram of Se versus Pd 137

Figure 5-17a. Primitive mantle-normalized PGE-chalcophile element diagram for

average unmineralized Nipissing Gabbro samples 138

Figure 5-17b. Primitive mantle-normalized PGE-chalcophile element diagram for

chilled margin gabbro 139

Figure 5-18. Primitive mantle-normalized PGE-chalcophile element diagrams for

average mineralized Nipissing Gabbro samples 140

Figure 5-19. Discrimination plot of Pd versus Cu/Pd showing mixing lines between

sulphide and silicate melts at various R factors 142

Figure 5-20. General geology and sample locations, Basswood Lake intrusion 145

Figure 5-21. Schematic diagram of interpreted structure of the Basswood Lake and

Appleby Lake intrusions 147

Figure 5-22. Bivariate scatter plot of Mg-number and wt% TiO2 for samples

from the Basswood Lake intrusion 151

Figure 5-23. Profiles of Mg# and SiO2 through the Basswood Lake intrusion 152

Figure 5-24. Primitive mantle-normalized multi-element diagrams for rock samples

xvi

from the Basswood Lake intrusion 153

Figure 5-25a. Profile of S/Se through the Basswood Lake intrusion 155

Figure 5-25b. Profile of Cu/Ni through the Basswood Lake intrusion 156


sulphides from Basswood Lake intrusion 157

Figure 5-27. General geology and sample locations, Appleby Lake intrusion 159

Figure 5-28. Bivariate scatter plot of Mg-number and wt% TiO2 for samples from

the Appleby Lake intrusion 162

Figure 5-29. Profiles of Mg-number and SiO2 through the Appleby Lake intrusion 163


from the Appleby Lake intrusion 165

Figure 5-31a. Profile of S/Se through the Appleby Lake intrusion 166

Figure 5-31b. Profile of Cu/Ni through the Appleby Lake intrusion 167


sulphides from the Appleby Lake intrusion 168

Figure 5-33. General geology and sample locations, Charlton Lake intrusion 170

Figure 5-34. Bivariate scatter plot of Mg-number and wt% TiO2 for samples from the

Charlton Lake intrusion 173

Figure 5-35a. Profile of Mg-number and SiO2 through the Charlton Lake intrusion 174

Figure 5-35b. Profile of TiO2. through the Charlton Lake intrusion 175

Figure 5-36. Profile of Zr and ∑REE through the Charlton Lake intrusion 177


from the Charlton Lake intrusion 178

Figure 5-38a. Profiles of S, S/Se and Cu/Pd through the Charlton Lake intrusion 180

Figure 5-38b. Profiles of Cu/Ni, Pd/Pt, Pt+Pd, Pt/S and Pd/S through the Charlton

Lake intrusion 181


sulphides from the Charlton Lake intrusion 183

Figure 5-40. General geology, locations of sulphide and gold showings, and outlined

location of the AN3 traverse near Casson Lake 186

Figure 5-41. AN3 sample section with general geology and sample locations 187

xvii


from the AN3 sample section 191

Figure 5-43. Profiles of Pt/Se, Pd/Se, Pt, Pd, Cu, Ni, S, S/Se and Cu/Pd through the

AN3 sample section 193


sulphides from the AN3 section 194

Figure 5-45. General geology and sample locations, Bell Lake intrusion 196


the Bell Lake intrusion 201


from the Bell Lake intrusion 203

Figure 5-48a. Profiles of Pt+Pd, Cu, Ni, S/Se, Cu/Pd, S through the Bell Lake

intrusion sample section 205

Figure 5-48b. Profiles of Pd/Se, Pt/Se, Cu/Ni, Pd/Pt through the Bell Lake


Figure 5-49a. Primitive mantle-normalized PGE-chalcophile element diagrams for

Group-1 andGroup-2 sulphides from the Bell Lake intrusion 208

Figure 5-49b. Primitive mantle-normalized PGE-chalcophile element diagrams for

Group-3 sulphides from the Bell Lake intrusion 209

Figure 5-50. General geology and location of sample area, Makada Lake intrusion 211

Figure 5-51. General geology and locations of samples, Rauhala property 212

Figure 5-52. Schematic diagram showing the interpreted structure of the Makada

Lake intrusion 216


the Makada Lake intrusion 221

Figure 5-54a. Profiles of Mg-number and SiO2 through the Makada Lake intrusion 222

Figure 5-54b. Profile of TiO2 through the Makada Lake intrusion 223


from the Makada Lake intrusion 225

Figure 5-56a. Profiles of Pt+Pd, Cu, Ni, S/Se, Cu/Pd, S through the Makada Lake


xviii

Figure 5-56b. Profiles of Pd/Se, Pt/Se, Cu/Ni, Pd/Pt through the Makada Lake



Group-1 sulphides from Makada Lake intrusion 229


Group-2 sulphides from Makada Lake intrusion 230

Figure 5-57c. Primitive mantle-normalized PGE-chalcophile element diagrams for

high mineralized samples from Makada Lake intrusion 231

Figure 5-58a. Profiles of Au, Pd, Pt, Se, Ni, Cu and S through drill hole A1-97 from

the Rauhala property (Makada Lake intrusion) 233

Figure 5-58b. Profiles of S/Se through drill hole A1-97 from the Rauhala property 234

Figure 5-59a. Profiles of Co and Cr through drill hole A1-97 from the Rauhala

property (Makada Lake intrusion) 235

Figure 5-59b. Profiles of Pt/Se and Pd/Se through drill hole A1-97 from the Rauhala

property (Makada Lake intrusion) 236

Figure 5-60. General geology and study areas in the Kukagami Lake intrusion 240

Figure 5-61. General geology and location of samples, western portion of the

Kukagami Lake intrusion 241

Figure 5-62. General geology and location of samples, eastern portion of the

Kukagami Lake intrusion 242


the Kukagami Lake intrusion 249

Figure 5-64a. Profiles of Mg-number and SiO2 through the Kukagami Lake

intrusion 251

Figure 5-64b. Profiles of TiO2 through the Kukagami Lake intrusion 252


from the Kukagami Lake intrusion 253


from the Kukagami Lake intrusion 255

Figure 5-67a. Profiles of Pd, Pt, Ni, Cu, S/Se, Cu/Pd and S through the Kukagami

Lake intrusion 257

xix

Figure 5-67b. Profiles of Pt/Se, Pd/Se, Cu/Ni, Pd/Pt in Kukagami Lake intrusion 258


sulphides from the Kukagami Lake intrusion 259


sulphides from the Kukagami Lake intrusion 260


sulphides from Kukagami Lake intrusion 261


sulphides from Kukagami Lake intrusion 262

Figure 5-70. General geology and location of the sample section for the Manitou

Lake intrusion 264


from the Manitou Lake intrusion 267

Figure 5-72. General geology and location of rock samples from the Chiniguchi

River and Sargesson Lake intrusions 269

Figure 5-73. Schematic map of the Rastall property (Janes Township) showing the

locations of drill holes, trenches and general geology 275

Figure 5-74. Schematic drill hole cross-section from the Rastall occurrence 276

Figure 5-75. Bivariate scatter plot of MgO versus TiO2 for rock samples from the

Chiniguchi River and Sargesson Lake intrusions 282


from the Chiniguchi River and Sargesson Lake intrusions 283

Figure 5-77. Bivariate scatter plots of whole-rock Cu-Pt and Cu-Pd concentrations

from the Chiniguchi River and Sargesson Lake intrusions 285

Figure 5-78a. Discrimination diagram of S/Se versus Pd 286

Figure 5-78b. Discrimination diagram of Se versus Pd 287

Figure 5-79. Discrimination diagram of Ni/Cu versus Pd/Ir 289


sulphides from the Chiniguchi River & Sargesson Lake intrusions 291



xx





Figure 5-82. Bivariate scatter plots of Mg-number and TiO2.and MgO and TiO2

for core samples from the composite drill hole, Rastall occurrence 299

Figure 5-83a. Profile of SiO2 through the composite drill hole, Rastall occurrence 300

Figure 5-83b. Profile of TiO2 through the composite drill hole, Rastall occurrence 301

Figure 5-84a. Profile of Mg# through the composite drill hole, Rastall occurrence 302

Figure 5-84b. Profile of MgO through the composite drill hole, Rastall occurrence 303

Figure 5-85. Bivariate scatter plots Pt-Cu and Pd-Cu for core samples from the

Rastall occurrence 305

Figure 5-86a. Discrimination diagram of S/Se versus Pd 306

Figure 5-86b. Discrimination diagram of Se versus Pd 307

Figure 5-87a. Profiles of Pt/Se, Pd/Se, Pt, Pd, Cu, Ni, S and Cu/Pd through the

composite drill hole, Rastall occurrence 308

Figure 5-87b. Profiles of Cu/Ni, Pd/Pt, Se and S/Se through the composite drill hole,

Rastall occurrence 309


sulphides from core samples, Rastall occurrence 312



Figure 5-88c. Primitive mantle-normalized PGE-chalcophile element diagrams for


Figure 6-1. General geological map of the River Valley intrusion 319

Figure 6-2. Generalized geology of the northwest portion, River Valley intrusion 328

Figure 6-3. Schematic of typical stratigraphy through the Marginal Series rocks 330

Figure 6-4. Schematic geological section through the Dana South Deposit 335

Figure 6-5. Chondrite-normalized diagram for sulphides in East Bull Lake and

River Valley intrusions 341

Figure 6-6a. Variation in wt% TiO2 in drill hole RV00-22 353

xxi

Figure 6-6b. Variation in wt% MgO in drill hole RV00-22 354

Figure 6-7a. Variation in Zr in drill hole RV00-22 358

Figure 6-7b. Variation in (Th/Nb)N in drill hole RV00-22 359

Figure 6-8. Chondrite-normalized REE plots for average samples from drill hole

RV00-22, Dana North Deposit 362

Figure 6-9. Primitive mantle-normalized multi-element diagrams for samples from

drill hole RV00-22, Dana North Deposit 364

Figure 6-10. Bivariate scatter plots for Cu-Pd and Cu-Pt 368

Figure 6-11. Bivariate scatter plots Pd-Ir and Pd-Pd/Ir 369

Figure 6-12. Discriminant plot of Se versus Pd 371

Figure 6-13. Discriminant plots of whole-rock S/Se versus Pt+Pd 372

Figure 6-14a. Variation in whole-rock S/Se through drill hole RV00-22 373

Figure 6-14b. Variation in whole-rock Pd through drill hole RV00-22 374

Figure 6-15a. Variation in whole-rock Cu through drill hole RV00-22 375

Figure 6-15b. Variation in whole-rock Pd/Pt ratios through drill hole RV00-22 376

Figure 6-16. Variations in the whole-rock Cu/Pd ratio in drill hole RV00-22 379

Figure 6-17ab. Discrimination plots of Ni/Cu versus Pd/Ir and Cu/Ir versus Ni/Pd 381

Figure 6-17c. Bivariate scatter plot of MgO versus Pd/Ir 382

Figure 6-18. Primitive mantle-normalized chalcophile metal abundances for sulphides

in core samples from diamond drill hole RV00-22 384

Figure 6-19ab. Bivariate scatter plots of MgO versus SiO2 and Ir versus MgO 396

Figure 6-19cd. Bivariate scatter plots of MgO versus Al2O3 and Fe2O3 397

Figure 6-19ef. Bivariate scatter plots of MgO vs TiO2 and Al2O3/TiO2 vs V 398

Figure 6-20. Bivariate scatter plots of Zr vs Y and Zr vs (La/Sm)N for fragment and

matrix samples from the River Valley intrusion 399

Figure 6-21. Mixing curves for primitive mantle-normalized values of (Th/Yb)N and

(Nb/Th)N using drill hole RV00-22, fragment, and matrix data 401

Figure 6-22. Chondrite-normalized REE plots for matrix and fragment samples 403

Figure 6-23. Primitive mantle-normalized multi-element diagrams for matrix and

fragment samples from the River Valley intrusion 406

Figure 6-24. Plot of Zr/Sm versus Nb/Ta ratios from whole-rock analyses of 44

xxii

unmineralized and mineralized River Valley intrusion samples 407

Figure 6-25. Discriminant plots of whole-rock S/Se versus Pt+Pd and

concentrations of Pt+Pd recalculated to metals in 100% sulphide 411

Figure 6-26. Discriminant plot of Se versus Pd and Cu/Pt versus Ni/Pd for fragment

and matrix samples from the River Valley intrusion 413

Figure 6-27ab. Primitive mantle-normalized chalcophile metal abundances for

sulphides from the matrix and fragment samples 415

Figure 6-27cd. Primitive mantle-normalized chalcophile metal abundances for


Figure 6-27ef. Primitive mantle-normalized chalcophile metal abundances for


Figure 6-27gh. Primitive mantle-normalized chalcophile metal abundances for


Figure 6-27i. Primitive mantle-normalized chalcophile metal abundances for


Figure 6-28. Discrimination plot of Pd versus Cu/Pd showing the sulphide

compositions of River Valley samples and mixing lines between

sulphide and silicate melt at various R factors 422

Figure 7-1a. Primitive mantle-normalized multi-element diagram comparing

estimates of parental magma compositions for the River Valley

intrusion and Nipissing Gabbro intrusions with heavily

contaminated and uncontaminated Siberian Trap CFB, boninite,

N-MORB and E-MORB 432

Figure 7-1b. Primitive mantle-normalized multi-element diagram comparing

estimates of parental magma compositions for the River Valley

intrusion and Nipissing Gabbro intrusions with heavily

contaminated Siberian Trap CFB 433

Figure 7-2a. Magmatic Model Stage 1 - Staging Chamber 440

Figure 7-2b. Magmatic Model Stage 2 – Displacement 442

Figure 7-2c. Magmatic Model Stage 3 – Ascent 443

Figure 7-2d. Magmatic Model Stage 4 – Emplacement 444

xxiii

LIST OF PHOTOS

Photo 4-1. Kukagami Lake sill “Kukagami Cliff Section”. 56

Photo 4-2.(A) Looking north toward a conformable, sill-like contact and

(B) Irregular contact of Nipissing Gabbro sill 49

Photo 4-3. (A) and (B) Modal and textural layering in Nipissing Gabbro 62

Photo 4-4. Conspicuous textural variations which are possible examples

of textural layering in outcrop at the Rauhala property 63

Photo 4-5. (A) and (B) Gabbro-sediment breccia occurring along the contact

of a Nipissing Gabbro intrusion in Porter Township 65

Photo 4-6. Sulphide-bearing basal breccia in drill core, Rastall occurrence 66

Photo 4-7. (A) and (B) Typical orthopyroxene-gabbro unit 68

Photo 4-8. (A) Typical disseminated and blebby sulphide mineralization and (B)

atypical sulphide textures in orthopyroxene gabbro 69

Photo 4-9. (A) Typical unmineralized, medium-grained orthopyroxene gabbro

and (B) Mafic fragment in medium-grained orthopyroxene gabbro 70

Photo 4-10. (A) typical vari-textured gabbro and (B) coarser-grained gabbro

patches from vari-textured gabbro 72

Photo 4-11. (A) Gabbro pegmatite, termed “snowball” gabbro and(B) close up

of the “snowballs” 74

Photo 4-12. (A) Granophyric pod (or dike?) from the upper portion of the

Basswood Lake Intrusion and (B) Close up of photo (A) 75

Photo 4-13. (A) Miarolitic cavity lined with carbonate and quartz and

(B) patchy sulphide mineralization 76

Photo 4-14. Photomicrographs of Lower & Upper quartz Diabase-Gabbro Units 79

Photo 4-15. Photomicrographs of rocks from the Orthopyroxene Gabbro Unit 80

Photo 4-16. Photomicrographs of altered rocks in the Orthopyroxene

Gabbro (Gabbronorite) Unit 81

Photo 4-17. Photomicrographs of magmatic disseminated and blebby

sulphide mineralization 86

Photo 4-18. BSE images of discrete platinum-group minerals in sulphide-bearing

xxiv

rocks from the Chiniguchi River Intrusion 87

Photo 4-19. (A) and (B) Orthopyroxene gabbro with disseminated and coarse

blebby sulphide from the Bassoon Lake Intrusion 96

Photo 5-1. (A) Aplite dike and (B) Sediment fragment in gabbro from the

Basswood Lake Intrusion 149

Photo 5-2. (A) Medium-grained massive gabbro-orthopyroxene gabbro hosting

distinct “pipe-like” unit of sulphide (PGE) bearing vari-textured gabbro

and (B) Close up of sulphide-bearing vari-textured gabbro; Charlton

Lake Intrusion, Casson Lake AN3 occurrence 190

Photo 5-3. Heavily gossaned Nipissing Gabbro from the northern part of the

traverse across the Bell Lake Intrusion near sample JB98-151 199

Photo 5-4. (A) Fragments of Huronian Supergroup sedimentary rocks in fine- to

medium-grained gabbro and (B) Extensively altered gabbro with

fine-grained blue quartz and finely disseminated sulphide; from the

Makada Lake Intrusion 218

Photo 5-5. (A) Sharp contact between Huronian Supergroup sedimentary rocks

fine-grained gabbro and (B) Medium-grained orthopyroxene gabbro from

the Whalen showing (sample JB98-103A), Kukagami Lake Intrusion 246

Photo 5-6. (A) Fragments of Huronian sedimentary rocks in very-fine-grained to

chilled margin gabbro and (B) Exposed sulphide mineralization at the

Rastall occurrence, Chiniguchi River Intrusion 274

Photo 5-7. (A) Gossan from semi-massive to massive sulphide mineralization

proximal to the intrusive contact and (B) Malachite-stained sulphide

mineralization at the contact, Rastall occurrence 281

Photo 6-1. (A) Tectonized igneous contact along the western margin of the River

Valley intrusion; (B) Chaotic Zone, correlative with the Marginal

and/or Inclusion/Autolith-bearing zones 322

Photo 6-2. (A) Typical footwall (hangingwall) paragneiss to the River Valley

intrusion; (B) Boundary Unit of the River Valley 336

Photo 6-3. (A) Breccia Unit with fragments and mafic matrix; (B) Breccia Unit

with felsic matrix, River Valley intrusion 337

xxv

Photo 6-4. (A) Inclusion-bearing Unit; (B) Fine-grained (diabase) mafic dike

cutting through the Breccia and Inclusion-bearing units 338

Photo 6-5. Layered Units: (A) Modal and textural layering in olivine gabbronorite;

(B) Flat-lying layering in olivine gabbronorite 339

Photo 6-6. Core from drill hole RV00-22. (A) Footwall; (B) Boundary Unit 346

Photo 6-7. Core from drill hole RV00-22. (A) Breccia Unit; (B) Breccia Unit 347

Photo 6-8. Core from drill hole RV00-22. (A) Breccia Unit; (B) Breccia Unit 348

Photo 6-9. Core from drill hole RV00-22. (A) Inclusion-bearing Unit and

(B) Layered Unit 349

Photo 6-10. Central Zone (Dana North Deposit) fragment and matrix sampling from

the Breccia Unit. (A) Fragment sample CZF01, matrix sample CZM01;

(B) Fragment sample CZF02 and matrix sample CZM02 386

Photo 6-11. South Zone (Dana South Deposit) fragment and matrix sampling from

the Breccia Unit. (A) Fragment sample SZF01 and matrix sample

SZM01; (B) Fragment sample SZF05 and matrix sample SZM05 387

Photo 6-12. Fragments in the South Zone (Dana South Deposit). (A) Medium-

grained gabbroic matrix hosting a fine-grained fragment cut by

fine-grained diabase dike; (B) Fragment of layered gabbroic rocks

in massive medium-grained gabbro 388

Photo 6-13. (A) and (B) Photomicrographs typical of the matrix in the Breccia

Unit, Dana South Deposit showing relict igneous textures 389

Photo 6-14. (A) and (B) Photomicrographs typical of extensively altered fragments

in the Breccia Unit, Dana South Deposit 390

xxvi

1

CHAPTER 1: INTRODUCTION

This thesis deals with platinum-group elements (PGE), copper (Cu), nickel (Ni)

sulphide mineralization that occurs in both the Nipissing Gabbro and the East Bull Lake

suite of mafic intrusive rocks within the southeastern portion of the Canadian Shield,

close to the juncture of the Superior, Southern, and Grenville Geological Provinces (Fig.

1-1). These two suites of mafic rocks are the dominant intrusive bodies within the 600

km long Huronian Magmatic Belt as described by Peck et al. (1993a); the Huronian

Magmatic Belt is alternatively known as the Huronian Metallogenic Province.

In approximate chronological order, the Huronian Magmatic Belt includes: basal,

mafic to felsic volcanic rocks of the Elliot Lake Group; north-trending Matachewan dikes

and northwest-trending Hearst dikes (2.45 Ga; Heaman, 1989); East Bull Lake Suite

(James et al., 2002a) intrusions (2.49 Ga; Krogh et al., 1984) that include the East Bull

Lake, Agnew Lake, and River Valley intrusions; the Murray Pluton (2.39 Ga; Krogh et

al., 1984); the Creighton Pluton (2.33 Ga; Frarey et al., 1982); and, Nipissing Gabbro

suite bodies (2.2 Ga; Corfu and Andrews, 1986; Noble and Lightfoot, 1992). The

Nipissing Gabbro and East Bull Lake suites form sills and dikes, from decametres to

kilometres in thickness, at the base of, and within the volcanic-sedimentary rocks of, the

Huronian Supergroup; only Nipissing Gabbro bodies are clearly intrusive into

sedimentary rocks of the Huronian Supergroup. Northwest-trending magnetite-olivine

gabbro dikes (1.24 Ga; Van Schmus, 1975) of the Sudbury Dike Swarm (Shellnutt, 2000)

crosscut all of the older rock types. Anomalous to potentially economic concentrations of

PGE, along with Cu, Ni and gold (Au), occur most commonly in the East Bull Lake and

Nipissing Gabbro suites. Recent increases in demand for platinum (Pt) and palladium

(Pd) as well as improved Pd and Pt commodity prices, have made the Nipissing Gabbro

and East Bull Lake suites attractive Cu-Ni-PGE exploration targets since the mid to late

1980s.

1.1 General Statement of Objectives

This thesis has two main objectives. The first is to characterize PGE-Cu-Ni sulphide

mineralization in a selected number of Nipissing Gabbro intrusions (Figs. 1-1 and 1-2)

through regional and detailed geological mapping, diamond drill core, assays and

petrography.

2

Figure 1-1. Regional Geology and location of the Superior, Southern (Huronian

Supergroup) and Grenville Geological Provinces in north-central Ontario. The principal

study areas (outlined as A and B) include rocks in the (A) Sault Ste. Marie-Elliot Lake

Area, (B) Sudbury-Espanola Area, and (B) Cobalt Embayment (modified after Bennett et

al., 1991). The Basswood Lake and Appleby Lake intrusions are located within area “A”

and details are shown in Figure 5-20. Details of area “B” are in Figure 1-2.

3

Figure 1-2. Geology of the Superior, Southern and Grenville Geological Provinces in the

Sudbury area (Area B from Figure 1-1), and the locations of selected Nipissing Gabbro

intrusions: 1 = Shakespeare Deposit; 2 = O’Brien; 3 = Big Swan; 4 = Brazil Lake; 5 =

Nairn; 6 = Bell Lake; 7 = Charlton Lake; 8 = AN3 Casson Lake; 9 = Bassoon Lake; 10 =

Louie Lake; 11 = Makada Lake; 12 = Ermatinger (Fox Lake); 13 = Moncrieff; 14 =

Rathbun Lake; 15 = Scadding; 16 = Kukagami Lake (Kelly and Carafel Bay); 17 =

Davis-Kelly; 18 = Chiniguchi River (Janes and Sargesson Lake); and, 19 = Manitou

Lake. Also shown are the locations of the East Bull Lake suite intrusions: EBL = East

Bull Lake; M = Massey; A = Agnew (Shakespeare-Dunlop); D = Drury Twp.; W =

Wisner Twp.; F = Falconbridge Twp.; S = Street Twp.; and, RV = River Valley. The

locations of the Basswood Lake and Appleby Lake intrusions are provided in Figure 1-1

and Figure 5-20. Details of the rectangle over the River Valley intrusion are shown in

Figure 6-1.

4

To further that objective, whole rock analyses, including PGE, S and Se concentrations,

will be used to:

1. Determine the ore-forming potential of Nipissing Gabbro magmas, and

in particular the formation of economic accumulations of Cu-Ni-PGE

sulphides;

2. Determine the controls on sulphide mineralization including an

assessment of the S-saturation of the magma prior to the mineralizing

event and evidence for contamination;

3. Identify and assess the effective nature of various elements as

pathfinders in aiding further mineral exploration; and,

4. Determine a petrogenetic history of Nipissing Gabbro and establish the

tectonic environment in which the intrusions were emplaced.

The second objective is to characterize PGE-Cu-Ni sulphide mineralization along the

northern margin (intrusive contact) of the River Valley intrusion (Fig. 1-2) using regional

and detailed geological mapping, diamond drill core, assays and petrography. In

addition, whole rock analyses, including PGE, S and Se concentrations, will be used to:

1. Determine the ore-forming potential of East Bull Lake-type magmas,

and in particular the formation of Cu-Ni-PGE sulphides in the contact

environment;

2. Determine the controls on sulphide mineralization including an

assessment of the S-saturation status of the magmas and evidence for

contamination;

3. Identify and assess the effective nature of various elements as

pathfinders in aiding further mineral exploration; and,

4. Consider the petrogenesis of Cu-Ni-PGE sulphide mineralization in the

River Valley intrusion.

Fundamental to the objectives of this thesis is determining whether or not the

magmas that produced Nipissing Gabbro and the River Valley intrusion were S-saturated

or S-undersaturated at the time of magma formation. If the magmas were S-saturated

5

then they would have been depleted in the ore-forming chalcophile and/or siderophile

elements (i.e. Cu-Ni-PGE) and are not considered capable of producing substantial sized

(i.e. economic) Ni-Cu-PGE deposits (e.g. Keays, 1995). However, if the magmas were

S-undersaturated, then it is expected that the magmas would have kept their full

compliment of chalcophile and/or siderophile elements and would therefore present

excellent PGE exploration targets. When the magmas became S-saturated, whether

through contamination from S-rich sediments, through an increase in silica content in the

magma, or prolonged fractionation of the magma, they would have formed sulphides that

were strongly enriched in Ni, Cu, Au, PGE and other highly chalcophile and/or

siderophile metals. These sulphides would have formed massive magmatic sulphide

deposits and/or disseminated sulphide mineralization; subsequent remobilization of the

sulphides may have also led to the development of hydrothermal Au and/or Cu-PGE

deposits. The most effective way to test the sulphur-saturation model is through

systematic lithogeochemical sampling of both mineralized and non-mineralized rock

units, followed by a geochemical comparison between the two sample suites (cf. Hoatson

and Keays, 1989; Keays, 1995).

The consequences of this research project will be to develop a model that explains

the distribution of the Cu-Ni-PGE metals that is of general use in the exploration for Cu-

Ni-PGE sulphide ores in geological environments that are similar to those of Nipissing

Gabbro intrusions and the River Valley intrusion, and to quantify the physical and

chemical controls on PGE fractionation as they relate to the sulphur fugacity of parent

magmas and the degree of contamination. In addition, the relationship between East Bull

Lake and Nipissing Gabbro suite magmatism will be explored, examining their spatial

and geochemical characteristics, in the context of the geological environment in which

they occur. Specifically, some comparisons will be made to magmatic suites and their

associated mineralization, and supracrustal sequences that occur in the Fennoscandian

Shield in Finland (e.g., Vogel et al., 1998b; Nykänen et al., 1994).

6

1.2 Location and Access

Nipissing Gabbro intrusions were examined within the Sault Ste. Marie-Elliot Lake

area, the Sudbury-Espanola area and the Cobalt Embayment, spanning the region

between Sault Ste. Marie to the west the west shore of Lake Temagami to the east (Fig.

1-1). Access to most of the study areas can be made by provincial highways and the

numerous logging roads and trails that cover the region. Regional sampling was

concentrated in the Southern Province, extending from Wells Township in the west, to

Clement Township in the east and as far south as Curtin Township, near the north shore

of Lake Huron (Figs. 1-1 and 1-2). In addition, a few samples were collected from

Nipissing Gabbro intrusions associated with Huronian Outliers (Rousell et al., 1997),

located within Archaean rocks, near the Benny Greenstone Belt (Moncrieff and

Ermatinger townships). Semi-detailed lithogeochemical sampling, including diamond

drill core sampling, and geological mapping was done at several sulphide occurrences in

Curtin (AN3 Casson Lake occurrence), Janes (Chiniguchi River intrusion), Kelly

(Kukagami Lake intrusion), and Waters (Makada Lake intrusion) townships. Seven

detailed lithogeochemical traverses were completed across 7 Nipissing Gabbro

intrusions: Appleby Lake, Basswood Lake, Charlton Lake, Bell Lake, Makada Lake,

Kukagami Lake and Manitou Lake intrusions (Figs. 1-1 and 1-2). Details on Township

names and locations within the study area can be found on Ontario Geological Survey

Map 2419 (Sault Ste. Marie-Elliot Lake, 1:253,440 scale) and Map 2361 (Sudbury-

Cobalt, 1:253,440 scale).

The River Valley intrusion is located about 100 road kilometres (~60 km direct)

northeast of the City of Greater Sudbury, Ontario (Fig. 1-2). Work by Pacific North West

Capital Corp. and joint venture partner Anglo American Platinum Corporation Limited

(South Africa) has revealed the presence of several potentially commercial base-metal

sulphide associated PGE deposits along the northern contact of the intrusion; an

independent resource study outlined more than 1 million ounces of combined Pd, Pt and

Au (Indicated and Inferred Resources) from three mineralized zones (Pacific North West

Capital Corp. press release 22/07/04). Rock core from drill hole RV00-22, located at the

Dana Lake North deposit (Dana Township), was examined in detail using both

lithogeochemical and petrological methods. In addition, a suite of surface samples

7

comprising fragment and matrix rock material was collected from cleared areas within

the contact environment.

1.3 Previous Geological Work

Much of the early detailed work on the petrology, structure and mineralization in

Nipissing Gabbro and associated metasedimentary and metavolcanic rocks was

concentrated in the Cobalt-Gowganda region (e.g. Bowen, 1910; Collins, 1913;

Hriskevich, 1968; Jambor, 1971; Conrod, 1989). By the 1980s there was increased

interest in Nipissing Gabbro westward toward the Sudbury and Sault Ste. Marie areas,

with particular attention toward their potential as hosts to PGE, and/or Cu, and/or Ni (e.g.

Lightfoot et al., 1986; Rowell and Edgar, 1986; Lightfoot et al., 1987; Lightfoot and

Naldrett, 1989). The present project builds on the early work but will also supplement

more recent contributions (e.g. Lightfoot et al., 1993; Lightfoot and Naldrett, 1996) and

introduce new approaches that will be of use in exploration for Cu-Ni-PGE-rich sulphides

that are both in, and associated with bodies of Nipissing Gabbro.

In the past most mineral exploration associated with Nipissing Gabbro intrusions was

focused in the very rich Co-Ag camp of Cobalt, Ontario where there is a recognized

connection between Nipissing gabbro intrusions and mineralization (e.g. Card and

Pattison, 1973). Sulphide showings in the Sudbury area have been examined and re-

examined for their Cu-Ni potential with the most notable being the Shakespeare Deposit

located in Shakespeare Township, about 65 km west of the City of Greater Sudbury.

First described in 1929 (Moore, 1929), the original sulphide showing has now been

upgraded to deposit status, containing an Indicated Resource of 12.0 million tonnes

grading 0.35% Ni, 0.36% Cu, 0.02% Co, 0.19 g/t Au, 0.34 g/t Pt and 0.38 g/t Pd (Ursa

Major Minerals Incorporated press release 15/04/04). Interest for PGE sulphide

mineralization in Nipissing Gabbro intrusions began in the late 1980’s but it was not until

1998 that it truly began to escalate, intensifying with a rise in the market price of Pd

(+US$1,000/oz) and Pt (+US$600/oz) in early 2001. Since 1998, the author has been

involved in, or has been consulted on numerous exploration projects aimed at PGE-Cu-Ni

sulphide mineralization in Nipissing Gabbro intrusions throughout the Sudbury region,

including but not limited to those outlined in Figure 1-2.

8

The first geological mapping of the River Valley intrusion was completed by

Lumbers (1971 and 1973) as part of regional mapping in the Nipissing and Sudbury

regions. Lumbers interpreted the bulk of the River Valley intrusion to be located in the

Grenville Province and associated it with other Late Proterozoic anorthosite bodies of the

Grenville Province, and stated that it was intruded across the Grenville Front Boundary

Fault (Lumbers, 1978). More recent work has included geological mapping of the River

Valley intrusion at 1:20 000 scale (e.g., Easton and Hrominchuk, 1999, 2001a, 2001b),

regional mapping at 1:50 000 scale (Easton, 2001), and whole-rock, mineral chemistry

and petrographic studies (Easton and Hrominchuk, 2002; Easton, 2003). Ashwal and

Wooden (1989) published a Pb/Pb whole-rock age for the River Valley intrusion of 2562

± 165 Ma and suggested either an enriched mantle source or crustal contamination of a

mantle-derived magma. Easton (2003) reported a precise U/Pb zircon age of 2475 +2/-1

Ma from a sample collected and analyzed by Larry Heaman at the University of Alberta

(James et al., 2002b).

The earliest recorded exploration activity on the northern portion of the River Valley

intrusion (Dana Township) was by Kennco Explorations (Canada) Ltd. in 1968, at which

time they conducted an airborne magnetometer (mag) and electromagnetic (EM) survey

over Janes, Davis, Henry and Dana Townships. In 1969, J.P. Patrie exposed

disseminated and coarse bleb sulphide mineralization in trenches and pits that now

comprise the main showings on the property. In both cases, the main emphasis was on

the exploration for Cu-Ni sulphide deposits and no assays were reported for PGE. In

1973, the Province of Ontario placed more than 110 Townships in a withdrawn area

referred to as the “Temagami Land Caution” – this region was excluded from any type of

resource development until June of 1996. The northern portion of the River Valley

intrusion was covered by this withdrawn area and as a result most of the intrusion was

never explored for its Cu-Ni-PGE potential. Prospecting in August 1998 in the Dana

Lake area by L. Luhta, R. Bailey and R. Orchard resulted in the initial discovery of PGE

mineralization. Pacific North West Capital Corp. and partners Anglo American Platinum

Corporation Limited began exploration programmes on the intrusion in June 1999.

From 1998 to 2004, the author managed or was consulted on numerous Cu-Ni-PGE

exploration programs for public and private exploration companies, which were directed

9

at Nipissing Gabbro and East Bull Lake suite intrusions. During this time, the author was

involved in several important mineral discoveries within these intrusive suites and was

instrumental in organizing the commercial exploration companies in an effort to both

advance their goals and gain more geologic data for this thesis. In addition, the author

worked with the Ontario Geological Survey to advance their geologic database on the

Nipissing Gabbro and East Bull Lake suites.

1.4 Terminology

The term “Nipissing Diabase” was first used by Miller (1911) to represent the

extensive bodies of massive tholeiitic intrusions that occur at Cobalt, the type area.

Intrusions of Nipissing Diabase are not ordinarily diabasic and as such the term

“Nipissing Gabbro” is used here as a more generic term to describe the intrusions; these

two terms are interchangeable.

Primary igneous textures and features have been preserved in the Nipissing Gabbro

suite and River Valley intrusion rocks, mainly as mineral pseudomorphs. Therefore, the

nomenclature of the International Union of Geological Sciences (IUGS) conventions

have been adopted for assigning names and describing fabrics (LeMaitre, 1989).

Descriptions of layering use the definitions and terminology proposed by Irvine (1982).

The majority of rocks that comprise the Nipissing Gabbro suite and River Valley

intrusion are altered and in general the primary mineral assemblage is not well preserved;

the most pristine mineralogy generally survives within the most central parts of the

intrusions. Regional metamorphism caused the replacement of primary pyroxenes (i.e.

orthopyroxene and clinopyroxene) by amphibole, chlorite and epidote group minerals, an

interpretation based on the preservation of relict cumulate textures and relict pyroxene

crystal morphologies. The term “pyroxene” refers to the primary minerals which are

inferred on the basis of textures of amphibole pseudomorphs. Orthopyroxene and

clinopyroxene are not necessarily discriminated and therefore “gabbro” is used as a

general field term for gabbroic rocks and does not refer only to rocks that may have

consisted of an assemblage of clinopyroxene and plagioclase feldspar. In most cases

plagioclase is partially to completely saussuritized and only rarely unaltered. For the

purpose of simplification, the prefix “meta” has not been used in conjunction with

igneous terminology. Unless otherwise stated, the term PGE refers to the total

10

concentration of Pt, Pd and Au and the abbreviation “3E” refers to the total concentration

of Pt, Pd and Au.

All Universal Transverse Mercator (UTM) coordinates are in Zone 17, NAD 83

datum, unless otherwise stated; geographic Longitude/Latitude coordinates are provided

where UTM coordinates are not available.

1.4.1 Abbreviations

For clarification purposes, some of the more common abbreviations used in this

study include:

boninite :an olivine-bronzite andesite that contains little or no feldspar;

generated in modern subduction zone environments within the

upper lithospheric mantle; fluxing of hydrous fluids derived from

an underlying and subducting slab (oceanic plate) serve to lower

the melting temperature and begin to generate magma from

depleted lithospheric mantle.

chalcophile :a group from the geochemical classification of the elements as

defined by Goldschmidt (1937) whereby specific elements (e.g.

Cu, Zn, As, S, Se) are preferentially incorporated into the sulphide

liquid (chalcophilic).

fenitization :ubiquitous alkali metasomatism of quartzo-feldspathic rocks in

the immediate region of carbonatite complexes.

first-stage magma :a magma which is generated from low degrees of partial melting

(i.e. <25%) of the source region (e.g. upper mantle) and is

therefore S-saturated.

Ga :billion years (ago).

lithophile :a group from the geochemical classification of the elements as


Ti, Zr, Hf, Th, La, Ta, Nb, Rb, Sr) are preferentially incorporated

into the silicate liquid (i.e. the crust).

Ma :million years (ago).

11

metasomatism :the process by which a new mineral of partly or wholly different

chemical composition may grow in the space of an old mineral or

old mineral aggregate without little disturbance of the textural or

structural features.

S-saturated :a magma that is saturated with respect to sulphur.

S-undersaturated :a magma that is undersaturated with respect to sulphur.

saussuritization :the process by which calcic plagioclase is altered into a white to

greenish or greyish mineral aggregate consisting of a mixture of

albite, zoisite or epidote, and variable amounts of calcite, sericite,

prehnite and calcium-aluminium silicates; a feature that is

generally indicative of low temperature alteration.

second-stage magma :a magma which is generated from a source region (e.g. depleted

upper mantle) that has undergone a previous episode of low (i.e.

<25%) partial melting and is therefore S-undersaturated.

siderophile :a group from the geochemical classification of the elements as


Fe, Co, Ni, Os, Ir, Re, Ru, Rh, Pd, Pt, Au) are preferentially

incorporated into the iron liquid (i.e. the core-mantle).

tenor :for platinum-group elements and gold, it is used to define the

metal content of the bulk sulphide fraction.

12

CHAPTER 2: COURSE OF INVESTIGATION

2.1 Field Work

The bulk of the regional and detailed sampling was completed from June to

September 1997 and a major part of the 1998 Summer field season was spent conducting

detailed lithogeochemical traverses across several sills of Nipissing Gabbro and

examining sulphide occurrences in areas southwest and northeast of Sudbury (Figs. 1-1

and 1-2). A total of 199 rock samples were collected and submitted for analysis, of

which 188 samples are from seventeen distinct Nipissing Gabbro intrusions (based on

current geological mapping) and eleven are from the hosting Huronian Supergroup

sedimentary rocks; a listing of these samples, with descriptions, geochemical data and

CIPW normative calculations, is provided in Appendix 1.

Eight lithologic sections were completed across seven Nipissing Gabbro bodies:

Appleby Lake, Basswood Lake, Charlton Lake, Casson Lake (AN3 occurrence), Bell

Lake, Makada Lake, Kukagami Lake and Manitou Lake areas (Figs. 1-1 and 1-2).

Detailed geochemical sampling was completed at three sites with historic sulphide

mineralization: the Rauhala property (Makada Lake, Waters Township), Whalen showing

(Kukagami Lake, Kelly Township), and the Jackie Rastall property (Chiniguchi River,

Janes Township). In order to provide an estimate of the regional background chemical

composition for Nipissing Gabbro and their host rocks, samples were collected from

various Nipissing Gabbro bodies in Porter, Moncrieff, Ermatinger, Foster, Nairn, Louise,

Rathbun, Scadding, Janes and Kelly townships (Fig. 1-2). In addition to the lithologic

sample sections and detailed sampling, diamond drill core from the Jackie Rastall

showing in Janes Township (drill holes JR99-01 and JR99-06), and from the Rauhala

occurrence in Waters Township (drill hole A1-97) were reviewed in detail. A total of

sixty-nine drill core samples, twenty-three from Janes and fourty-six from Waters

townships, were collected and submitted for analysis (Appendix 3). Additional site visits

were conducted on other sulphide showings and exploration properties, generally at the

request of the mineral property owners, including the Shakespeare Deposit (Shakespeare

Township), Bassoon Lake showing (Dieppe Township), and O’Brien showing (Dunlop

Township), from 1999 through 2003 (Fig. 1-2).

13

Data collection on the River Valley intrusion began in the Summer of 1999 and

continued into Fall 2003 as part of ongoing exploration programmes by Pacific North

West Capital Corp. and their joint venture partner Anglo American Platinum Corporation

Limited (Fig. 1-2). In 2002, sixteen samples were collected from surface exposures at the

Dana North and Dana South mineral deposits for use in a detailed study comparing and

contrasting the characteristics of matrix and fragment material within the mineralized

breccia unit. Also in 2002, detailed core logging of drill hole RV00-22 was completed

and a total of twenty-eight core and core pulp samples were submitted for whole-rock

geochemical analysis as part of the detailed study through the mineralized breccia unit at

the Dana North deposit. Pacific North West Capital provided assay data (Pt, Pd, Au, Cu,

Ni), drill core log information and core pulp samples from drill hole RV00-22 from

which 112 of the pulp samples were analyzed for Se and S at the Geoscience

Laboratories, Sudbury.

2.2 Geochemical and Petrographic Analysis

The majority of the lithogeochemical samples (229 samples) were submitted for

analysis at the Geoscience Laboratories in Sudbury, Ontario. Representative rock or core

samples, weighing a minimum of 250 g were collected in the field or from drill core by

the author. The majority of rock and drill core samples were crushed using high chrome

steel mills from which approximately 150 ppm Cr and 0.1% Fe contamination may be

expected. Some of the rock samples were prepared by crushing in a steel-plated jaw

crusher and ground in a 99.8% pure Al2O3 planetary ball mill.

At the Geoscience Laboratories, major-elements (SiO2, TiO2, Al2O3, CaO, Fe2O3,

K2O, MgO, MnO, Na2O, P2O5) were determined by Wavelength Dispersive X-Ray

Fluorescence (WD-XRF) on a fused borate disk. Minor- and trace-elements (Be, Co, Cu,

Mo, Ni, Sc, Sr, V, W, Zn) were determined by Inductively Coupled Plasma – Atomic

Emission Spectroscopy (ICP-AES); the commercial laboratories (i.e. ACTLABS and

XRAL - see below) utilized similar determination techniques. Following an acid digest

(perchloric, hydrochloric, hydrofluoric and nitric), Se was determined by hydride Atomic

Absorption Spectrometry (AAS). Total S was determined using standard LECO-infrared

detection methods. These techniques for Se and S were employed at the Geoscience

Laboratories and at the commercial laboratories (see below).

14

The majority of samples (109 samples) were analyzed for rare-earth (Ce, Dy, Er, Eu,

Gd, Hf, Ho, La, Lu, Nd, Pr, Sm, Tb, Th, Tm, U, Yb, Y) and trace-elements (Cs, Nb, Rb,

Sr, Ta, Zr) using inductively coupled plasma-mass spectrometry (ICP-MS) at the

Geoscience Laboratories in Sudbury; some samples (20 samples) from the River Valley

intrusion were analyzed, using the same technique, at XRAL Laboratories. Complete

digestion of Zr is important if the element is to be relied upon in discrimination plots. All

of the Nipissing Gabbro suite rocks and most of the River Valley intrusion rocks were

digested using the open beaker method; only the fragment and matrix samples from the

River Valley intrusion were digested using the closed beaker method. A consequence of

this is that only the fragment and matrix rocks (16 samples) will have sufficient

(complete) digestion of Zr. Therefore, results obtained from open beaker digestion

represent minimum Zr contents; A.J. Crawford (pers. comm. 2004) suggested that Zr data

collected from standard ICP-MS techniques may be one third to one half less than that

collected by XRF methods. It is also important to note that reliable measurement of Ta

concentrations using standard ICP-MS techniques is considered problematic (A.J.

Crawford, pers. comm. 2004) and these data, along with Zr, should therefore be used

with caution. A review of analytical techniques in the determination of Ta, Zr, Nb, and

Hf is provided by Weyer et al. (2002).

The majority of the platinum-group elements (PGE = Ir, Ru, Rh, Pt, Pd) and gold

(Au) analyses were carried out at the low-level PGE facility of the Geoscience

Laboratories, Sudbury, following the principals and procedures of Jackson et al. (1990)

and Richardson and Burnham (2002). Basically, fifteen grams of powdered rock were

mixed with sodium carbonate, sulphur, silica powder and nickel powder. This mixture

was baked at 1050 C for 1.5 hours in a fire-clay crucible (Nickel Sulphide Fire Assay).

After dissolution of the Ni-sulphide button in concentrated hydrochloric acid, the PGE

were collected by tellurium co-precipitation, vacuum filtered, re-dissolved in acid regia

(digestion using hydrochloric and nitric acids) and brought to volume by deionized water.

The PGE concentrations are then determined by ICP-MS. The limits of detection

(average blank plus three standard deviations) are provided in Appendix 1. At the

commercial laboratories (see below) “exploration grade” concentrations for the platinum-

group elements Pt, Pd and Au are determined following standard lead collection-fire

15

assay techniques, utilizing thirty grams of powdered rock sample, with final

concentrations measured using ICP-MS.

Assay and geochemical data, mainly on drill core samples (RV00-22) from the River

Valley and Chiniguchi River intrusions (JR99-01 and JR99-06), was provided through

exploration work by Pacific North West Capital Corp. (Vancouver) and Goldwright

Explorations Inc. (Sudbury). Analyses for these sample suites were performed by

commercial laboratories XRAL Laboratories (Toronto), ACTLABS (Ancaster),

Accurassay Laboratories (Thunder Bay), Chemex Labs (Vancouver), and Bondar-Clegg

(ALS Chemex) Laboratory (Val d’Or). Analytical techniques and lower limits of

detection varied depending on the laboratory and techniques used but all of the

laboratories followed standard analytical procedures. Unless otherwise indicated the

limits of detection are those listed in Appendix 1. A complete listing of the data and

sample descriptions are provided in Appendix 1.

Thin sections, polished and covered (~30µm thickness), were prepared at the

Department of Earth Sciences, Laurentian University using standard procedures. A total

of 140 thin sections were made - 104 from Nipissing Gabbro rocks and thirty-six from

the River Valley intrusion rocks - in order to determine the amount of alteration and

metamorphism within each specimen, and to ascertain the degree of secondary veining

and/or structural fabrics. Petrographic descriptions and modal percentages of constituent

minerals, completed on the 140 thin sections, are summarized in Appendix 2.

2.3 Presentation and Interpretation of Geochemical Data

Whole-rock major element, trace element, rare-earth element and PGE+Au data are

provided in Appendices 1 and 3. The Mg-number, mainly used as a measure of the

degree of magma differentiation, is defined according to Cox (1980) as:

[1] (wt% MgO/mol. wt) / [(wt% MgO / mol. wt) + (0.85)(wt% Fe2O3* / mol. wt)]

Cox (1980) assumed that 15% of the total Fe in the whole rock is oxidized. The whole

rock analysis presented in this study lists the total iron oxide content as Fe2O3*. Total Fe,

reconstituted to FeO(t), is calculated using the formula:

[2] FeO(t) = FeO + (Fe2O3 x 0.89981)

2.3.1 Presentation and Interpretation

16

Various major, trace, rare-earth and chalcophile/siderophile element plots are

presented for each of the data sets, utilizing bivariate scatter plots, ternary diagrams (i.e.

AFM), chemostratigraphic plots, primitive mantle-normalized multi-element diagrams

(also referred to as spidergrams), chondrite-normalized rare-earth element diagrams, and

primitive mantle-normalized chalcophile/siderophile element diagrams (also referred to

as PGE spider plots). A review of the use of various geochemical plots and

discrimination diagrams is provided by Rollinson (1993).

The CIPW normative calculations of the analysed samples were completed using a

spreadsheet based software program written by Kurt Hollocher (Geology Department,

Union College, Schenectady, New York) and following the methods described by

Johannsen (1931). As only Fe2O3 was measured for all of the whole rock analyses,

CIPW normative calculations for iron were completed using a standard ratio of 0.14 to

represent the molar ratio of (Fe3+/total iron). This value was chosen on the basis of Fe2+

and Fe3+ concentrations reported by Easton (2003) from gabbroic rocks in the River

Valley intrusion. Prior to the Contents of S and CO2 were included in the calculations

but LOI was excluded. The chemical analyses were recalculated to 100% prior to

calculating the normative and all results of the CIPW normative calculations are reported

as weight percent normatives.

Primitive mantle-normalized multi-element diagrams or spidergrams, using primitive

mantle values from McDonough and Sun (1995), are used to display the variations in

Large-ion Lithophile Elements (LILE), rare-earth elements (REE) and High Field

Strength Elements (HFSE) from the various rock suites and to ascertain their most likely

tectonic history. Anomalous patterns exhibited by elements such as Nb, Ta, P and Ti are

of particular importance in these plots as negative Nb+Ta, P and Ti anomalies, coupled

with relative enrichment in the LILE (and LREE and HREE), suggest magma formation

within a subduction zone environment and/or mantle metasomatism and/or interaction

with continental crust. A review of crustal contamination signatures as they relate to

incompatible trace elements in spidergrams is provided by Thompson et al. (1984) but the

reader is cautioned that the extent to which geochemical variations are caused by source

heterogeneity versus crustal contamination is a point of controversy. References to

crustal contamination or crustal assimilation, which are made throughout this study, refer

17

not to the wholesale, physical consumption of the crustal material, but rather to small

amounts of partial melting of the crustal material. Seifert et al. (1992) suggested that 1%

partial melting of crustal material could remove large amounts of incompatible elements

without noticeably affecting the major-element composition.

Chondrite-normalized REE diagrams, using chondrite values from Lodders and

Fegley (1998), are used to display the REE and HFSE characteristics of the rock sample

suites (i.e. LREE/HREE and Eu anomalies) and to determine their most likely tectono-

magmatic history. An overview of the use of REE diagrams for Archaean ultramafic and

mafic rocks is provided by Sun and Nesbitt (1978) and by Wyman (1996).

Primitive mantle-normalized chalcophile/siderophile element diagrams, with their

metals re-calculated into 100% sulphide, are used to compare sulphides that underwent

different degrees of fractionation. The chalcophile and siderophile metals (Ni-Ir-Ru-Rh-

Pt-Pd-Au-Cu) are arranged in order (from left to right) of decreasing melting

temperature, resulting in patterns that document the petrogenesis of the sulphide (Barnes

et al., 1988). Sulphide segregation will deplete all PGE evenly, resulting in little

fractionation, but the crystallization of olivine, oxide (i.e. chromite), some high

temperature platinum-group minerals (PGM), and monosulphide solid solution (mss),

which is pyrrhotite-rich, will preferentially incorporate Os, Ir, Ru and Rh (Maier et al.,

1998); the fractionated sulphide phase will tend to be slightly enriched in Ni and strongly

enriched in Cu, Pt, Pd, and Au. The result is a series of profiles showing flat, negative or

positive slopes: flat patterns indicate mantle and primary partial mantle melts; olivine-

oxide cumulates tend toward negative slopes (i.e. ophiolites) with Os-Ir-Ru strongly

enriched relative to mantle; and, positive slopes (Pt-Pd-Au-Cu > Ni-Ir-Ru-Rh) reflect

more fractionated sulphides, commonly associated with evolved layered intrusions. The

usefulness of chalcophile metal ratio diagrams (Barnes et al., 1988) in determining

whether sulphide ores may have undergone mss fractionation and their application to

mineral exploration is reviewed by Maier et al. (1998).

On some of the diagrams, the chalcophile/siderophile metals and gold have been

normalized to 100% sulphides by using the S contents from the samples and assuming

that the average S content of the sulphides in the samples is 36.5 wt% S. This S value is

the S content in pure FeS (i.e. troilite – natural pyrrhotite will be more S-rich) and it is

18

used assuming that pyrrhotite is the dominant sulphide phase and that 100% sulphide

would therefore contain 36.5 wt% S. Several authors (e.g. Iljina, 1994; Keays and

Lightfoot, 2004) have used similar values in their recalculation of chalcophile/siderophile

metals in 100% sulphide. A review of the calculation and use of sulphide metal contents

in magmatic ore deposits is provided by Kerr (2001).

2.3.2 Element Mobility

Rock samples used in this study have undergone some degree of alteration and have

been subjected to a minimum of greenschist facies metamorphism and, as such the effects

of element mobility on the geochemistry of the rocks should be considered. The

problems of metamorphism and alteration in mafic igneous rocks have long been

recognized and the effects of hydrothermal alteration and greenschist facies

metamorphism are variable with respect to different elements (Pearce and Norry, 1979;

Lesher et al., 1991; Wyman, 1996). Although many of the so-called “immobile”

elements are potentially very mobile in hydrothermal systems, elements such as the

HFSE (i.e. Zr, Y, Nb, Ti, Ta, Hf) are considered by various authors to be mostly

immobile (Pearce and Norry, 1979; Campbell et al., 1984; Rollinson, 1993; Wyman,

1996). In contrast, incompatible LILE such as Cs, Rb, Na, K, Ba and Sr are considered

to be mobile under most circumstances. Elements thought to be slightly mobile include

Si, Al, Mg and Fe, however Si is mobile under some circumstances, as are Mg and Fe,

which are particularly mobile with the introduction of hydrothermal fluids and seawater

(Rollinson, 1993).

2.3.3 Archaean Tectonics and Mantle Chemistry

Compositional characteristics of the Archaean and Proterozoic mantle were different

to those of present day mantle, and as such the interpretation of geochemical data from

Proterozoic mafic igneous rocks must be considered in the context of these potential

differences. A discussion of these proposed differences is beyond the scope of this study

but a review is provided by Bleeker (2002). Various authors have shown that the

principles of uniformitarianism extend back into the Archaean and that tectonic processes

operational in the Archaean are thought to be similar to those in operation in the

Phanerozoic (Windley, 1993). In general, the similarity in these processes justifies the

use of most geochemical diagrams and the application of most theories to the study of

19

Proterozoic rocks. However, significant differences are apparent such as the prolific

occurrence of komatiites in the Archaean and their relative scarcity after ~2.5 Ga, and

their rarity in the Phanerozoic record. This suggests that thermal (Condie, 1989; Zindler

and Hart, 1986) and compositional (Francis, 2003) differences existed in the Archaean

mantle and that compositional differences exist between Archaean and Phanerozoic

volcanic rocks which would reflect these mantle differences.

2.3.4 Partition Coefficients

The affinity of any element for any phase can be expressed in terms of its Nernst

partition coefficient into this particular phase; this is commonly referred to as the “D”

value (e.g. Maier et al., 1998). The partition coefficient is of particular importance to

those elements that are strongly chalcophilic, including Ni, Cu, Se, and PGE. The D

value of an element between a sulphide and silicate melt (assuming equilibrium and a

closed system) is defined as (Naldrett,1981):

[3] Dsulphide/silicate = CC/CL

where CC is the concentration of the metal in the sulphide melt and CL is the

concentration of the metal in the silicate melt. Experimental determinations of D values

have shown that the PGE are extremely chalcophilic (e.g. Peach et al., 1990; Peach and

Mathez, 1996) and Keays (1995) provided a review of the various D values which have

been proposed for the PGE. Partition coefficient estimates for Cu, Ni, and the PGE based

on experimental data and empirical observations vary widely (Peach et al., 1990; Peach et

al., 1994; Keays and Lightfoot, 2004). Unless otherwise stated, partition coefficients

used in this study are DPd = 35,000; DIr = 17,000; DCu = 700; DNi = 250; and, DSe = 700.

The PGE metal contents of the sulphides are closely associated with the mass ratio of the

silicate melt to sulphide melt (R factor) during sulphide segregation (see Section 2.3.5).

2.3.5 Mass Balance (R Factor) Calculations

Campbell and Naldrett (1979) introduced the concept that differing PGE

concentrations may be partly explained by variations in the R factors during the process

of sulphide segregation, where R is the mass ratio of the silicate liquid to the sulphide

liquid. High R factors indicate that relatively few sulphide droplets are segregating and

interacting with the silicate liquid, whereas low R factors signify that many sulphide

droplets are segregating and interacting with the silicate liquid. Lower R factors will

20

result in the effective depletion of the PGE metals from the silicate melt but the PGE will

be diluted (low bulk-PGE contents) and relatively less PGE-enriched than the sulphide

melt that segregated under higher R factor conditions; effectively, the apparent D value

has become smaller.

In order to model the initial chalcophile element contents of the magma(s) that

produced the rocks in this study, it is necessary to first apply Rayleigh’s Law:

[4] CSM = CL x F(D-1)

where CSM is the concentration of the metal in the fractionated silicate melt, CL is the

concentration of the metal in the initial silicate melt, F is the fraction of silicate melt

remaining after fractionation, and D is the distribution coefficient of the metal.

In addition, the metal content of the theoretical initial magma prior to sulphide

segregation is required and this is generally estimated by the R factor equation:

[5] CC = (CL x D x (R+1)) / (R + D)

where CC is the metal concentration (in wt%) in the initial sulphide melt, CL is the metal

concentration in the initial silicate melt, D is the Nernst partition coefficient or D value

for the given element, and R is the R factor of Campbell and Naldrett (1979). This

equation may then be rearranged, solving for R:

[6] R = (CL x D)-(CC x D) / (CC- (CL x D))

Campbell and Barnes (1984) demonstrated that equation [5] may be simplified when D is

much greater than R:

[7] CC = CL x (R + 1)

This equation is generally applicable in the case of PGE due to their very high D values.

Graphical methods to determine R factors have also been developed (Barnes et al., 1993)

and these are reviewed by Maier et al. (1998). As signified by Maier et al. (1998) it is

important to note that because the D values for PGE with respect to sulphide are so much

higher than those of Cu and Ni, relatively small amounts of segregating sulphide (high R

factor) do not significantly deplete the silicate melt in Cu and Ni, but small amounts of

sulphide melt do strongly deplete the silicate magma in PGE. A consequence of this is

that PGE are less likely to form a large proportion of the total metals in large, massive

sulphide deposits and that disseminated sulphide deposits tend to produce the highest

PGE concentrations.

21

CHAPTER 3: REGIONAL GEOLOGY

3.1 General Geology

The Superior, Southern, and Grenville Geological Provinces are present within the

southeastern Canadian Shield in the area between Cobalt and Sault Ste. Marie (Figs. 1-1

and 1-2). The Neoarchaean Superior Province consists mainly of east-trending, granite-

greenstone belts and a variety of granitic and gneissic rocks. These rocks form the

basement upon which rocks of the Palaeoproterozoic Southern Province rocks were

deposited (i.e. Huronian Supergroup) and constitute much of the source terrane for the

Palaeoproterozoic metasedimentary and metavolcanic rocks of the Huronian Supergroup

(Bennett et al., 1991; Card and Jackson, 1995). In addition to Huronian Supergroup

volcano-sedimentary rocks, the Southern Province in Ontario comprises rocks of the

Early Proterozoic (~2.49 Ga) East Bull Lake intrusive suite (Easton, 1999; Vogel et al.,

1999), the ~2.2 Ga Nipissing Gabbro suite, the ~1.85 Ga Sudbury Igneous Complex

(Krogh et al., 1987), anorogenic intrusive rocks emplaced between 1.5 and 1.45 Ga

(Easton, 1998) and 1.24 Ga (Van Schmus, 1975) northwest-trending olivine-magnetite

gabbro dikes of the Sudbury Dike Swarm. The Grenville Province terminates against the

Superior and Southern provinces to the north with the Grenville Front Boundary Fault

marking this juncture and defining the northwest limit of intense deformational events

relating to the Meso- to Neoproterozoic Grenville Orogeny. A summary of the

geological history of the Sudbury region is provided in Table 3-1.

In the Lake Superior region of the Southern Province (Wisconsin, Michigan and

Minnesota), the arcuate Mesoproterozoic (1110-1090 Ma; Thurston, 1991) Mid-continent

Rift includes volcanic rocks (Keweenawan flood basalts) of the ~1.1 Ga Keweenawan

Supergroup (Sutcliffe, 1986), sedimentary rocks of the ~2.2 Ga lower and ~1.85 Ga

upper Marquette Range Supergroup, and the ~2.1 Ga to 1.85 Ga Animikie Group (Fig. 3-

1). Upper Cobalt Group rocks of the Huronian Supergroup, representing passive margin

and glacial deposits, are thought to be equivalent to the rocks of the lower Marquette

Range Supergroup (Hoffman, 1989; Young, 1983). Collision of the Wisconsin Magmatic

Terrane (Hoffman, 1989), interpreted as an island arc, with the Superior Province craton

and passive margin deposits of the Southern Province marked the onset of the ~1.85 Ga

Penokean Orogeny (Bennett et al., 1991).

22

Era/Subdivision Time (Ma) Tectonic Event Ref.Neoarchaean >2500 - -

Palaeoproterozoic 2490-2440 plume-induced rifting, south margin Superior ProvinceHuronian sedimentation, volcanism begins (basin-fill) 1

Palaeoproterozoic 2500-1600 - -2500-2200 Development of the Huronian Magmatic Province 22496-2475 East Bull Lake suite intrusions 32489-2443 Matachewan-Hearst dyke swarm 4

2450 Copper Cliff Formation 52400-2200 BLEZARDIAN DEFORMATION 6

2388 Murray Pluton 52333 Creighton Pluton 72200 plume-induced rifting, northeastern Superior Province 8

2210-2069 Nipissing Gabbro suite 31879-1820 EARLY PENOKEAN DEFORMATION 9

1850 Sudbury Event - Sudbury Igneous Complex 51750-1730 Early Killarney Magmatic Belt (anorogenic) 101740-1700 LATE PENOKEAN DEFORMATION 9

1700 Cutler Pluton 11MesoProterozoic 1600-1000 - -

1470-1450 Late Killarney Magmatic Belt (anorogenic) 101.24 Sudbury dyke swarm 12

1100-1070 GRENVILLE OROGENY 10575 Grenville dyke swarm 10

References: (1) Bennett et al. (1991); (2) Peck et al. (1993a); (3) James et al. (2002a); (4) Fahrig (1987);(5) Krogh et al. (1984); (6) Stockwell (1982); (7) Frarey et al. (1982); (8) Ernst et al. (1999)(9) Easton (2000b); (10) Easton (1992); (11) Wetherill et al. (1960); (12) Van Schmus (1975)

Table 3-1. Tectono-metamorphic history of the Southern Geological Province, Sudbury

region.

23

24

3.2 Huronian Supergroup

The Huronian Supergroup is a sequence of sedimentary and volcanic rocks up to 12

km thick and unconformably overlying 2.8-2.5 Ga Archaean granite-greenstone rocks of

the southern Superior Province (Figs. 1-2 and 3-2); a paleoweathering surface is locally

preserved at the unconformity (Bennett et al., 1991). Volcanic rocks of the Elliot Lake

Group (Thessalon, Elsie Mountain, Stobie, Copper Cliff and Salmay Lake) form the base

of the Huronian Supergroup and are spatially associated with intrusions of the East Bull

Lake suite, in the region west of Sudbury (Fig. 3-2). This spatial association is

interpreted to suggest that the East Bull Lake suite intrusions were cogenetic with the

oldest volcanic rocks of the Elliot Lake Group (Card et al., 1977; Card, 1978; Innes,

1977; Tomlinson, 1996). Card et al. (1977) noted Sudbury-type breccia bodies obscure

the nature of the contact between the Drury Township body and the overlying volcanic-

sedimentary sequence (Stobie and Matinenda formations). Elliot Lake Group

sedimentary rocks of the Matinenda and McKim formations, stratigraphically overly the

volcanic rocks.

Immediately overlying the Elliot Lake Group, rocks of the Huronian Supergroup are

subdivided into three major groups on the basis of the cyclical nature of the sediments

(Bennett et al., 1991), viz. (stratigraphically lowest to highest): Hough Lake Group

(Ramsay Lake, Pecors, Mississagi, and Aweres formations), Quirke Lake Group (Bruce,

Espanola, and Serpent formations), and the Cobalt Group (Gowganda, Lorrain, Gordon

Lake, and Bar River formations). The Quirk Lake and Cobalt groups are separated by an

unconformity, and the groups taper to the north where they onlap the Archaean Superior

Province craton (Bennett et al., 1991).

3.2.1 Elliot Lake Group

The Elliot Lake Group consists of both volcanic and sedimentary rocks. The lowest

formation, Livingstone Creek, consists of basal conglomerate and sandstone and is

observed only in the area around Elliot Lake, Thessalon and Sault Ste. Marie, where it is

100 to 400 m thick (Bennett et al., 1991). The Livingstone Creek Formation is overlain

by the Thessalon Formation, which represents an eroded flood basalt province

(Tomlinson et al., 1999) and records volcanism associated with incipient rifting.

25

26

Volcanic rocks of the Thessalon Formation are interpreted by Jolly (1987) to be

metasomatically modified (possibly by Archaean subduction) mafic continental

tholeiites, with a preserved thickness of between 300 and 1200 metres (Bennett et al.,

1991; Jolly, 1987). The Thessalon Formation is divided into a lower series of 4 volcanic

cycles, dominated by basalt to andesite and capped by a unit of rhyolite, and a single

upper series consisting of basalt to basaltic andesite (Tomlinson et al., 1999). On the

basis of whole rock rare-earth element geochemistry, Tomlinson et al. (1999) suggested

that initial volcanism was likely related to adiabatic up-welling due to passive rifting, and

that partial melting was episodic, involving multiple pulses of magma. Tomlinson (1996)

surmised that the principal magma source for the Thessalon volcanic rocks was

metasomatically-enriched upper mantle, which acquired its geochemical signature from

long-lived subduction-accretion events during the Kenoran Orogeny (~2710 to 2660 Ma;

Thurston, 1991). In the Sudbury area, volcanic rocks of the Elsie Mountain, Stobie,

Copper Cliff and Salmay Lake formations generally lie beneath the capping sedimentary

rock sequences but are also observed interfingered with the upper Matinenda and McKim

formations (Bennett et al., 1991). These eastern volcanic belts have a greater thickness

and may be stratigraphically higher than the Thessalon Formation (Bennett et al., 1991).

3.2.2 Hough Lake, Quirke Lake and Cobalt Groups

The Hough Lake, Quirke Lake and Cobalt groups consist of three sedimentary

cycles; a lower conglomerate, middle mudstone to siltstone or carbonate and an upper

quartz-feldspar arenite to quartz-rich sandstone unit (Bennett et al., 1991). Conglomerate

units of the Ramsey Lake, Bruce and Gowganda formations are interpreted as being

glaciogenic in origin, deposited in a marine environment proximal to an ice shelf (Young,

1983; Fralick and Miall, 1989). Siltstone-sandstone units are thought to represent

deposition during intraglacial or post-glacial periods in either fluvial or marine

environments (Young, 1983; Fralick and Miall, 1989).

3.2.3 Development of the Huronian Supergroup

The Huronian Supergroup and igneous rocks of the Huronian Magmatic Belt ( Peck

et al., 1993a) developed as a result of the passive rift-related break up of the Superior

craton (Bennett et al., 1991; Young, 1995; Vogel et al., 1998a). Huronian Supergroup

deposition is interpreted to be the result of a partial Wilson Cycle, involving rifting,

27

represented by the lower Elliot Lake Group, and the development of a southward-facing

passive margin, represented by the upper Huronian groups (Young, 1983; Hoffman,

1989; Bennett et al., 1991); a schematic interpretation of these tectonic events is shown in

Figure 3-3. Incipient rifting events in the development of the Huronian Supergroup, as

represented by the lower Elliot Lake Group, would have pre-dated the earliest period of

volcanism, the lowermost Thessalon Formation, with deposition of basal conglomerates

and sandstones of the Livingstone Creek Formation (Fig. 3-3a). The main-rifting stage

(Fig. 3-3b) would have seen further extension of the rift basin, deposition of lower Elliot

Lake Group volcanic rocks (Thessalon Formation) and contemporaneous intrusion of

East Bull Lake suite mafic rocks. The stage of late-rifting (Fig. 3-3c) would have seen

deposition of sedimentary rocks of the Matinenda and McKim formations which overly

and are intercalated with volcanic rocks of the Thessalon Formation. Subsequent

sedimentary cycles (conglomerate - mudstone, siltstone or carbonate – sandstone) were

deposited during the passive-margin stage (Fig. 3-3d), characterized by the Hough Lake,

Quirke Lake and Cobalt groups. These cycles are thought to represent deposition in

grabens and other depressed features, during episodic continental glaciation along a

passive continental margin (Hoffman, 1989) or further deposition in an epicratonic basin

(Roscoe and Card, 1993). Within each cycle, deposition of glacial till units was followed

by a passive marine sequence represented by shallow–marine and fluvial sands. Intrusion

of the Nipissing Gabbro suite may have began as early as the late-rift or early break-up

stage (Fig. 3-3c). Geochemical features of Nipissing Gabbro, although generally

interpreted to be related to continental flood basalt magmatism (e.g. Lightfoot and

Naldrett, 1996), are also consistent with magmas that have interacted with crustal

material potentially associated with a subduction zone (see Section 5). This suggests that

magmatism associated with the Nipissing Gabbro suite may have occurred during the

period of early continent-island arc collision, spanning events depicted in Figures 3-3d

and 3-3e.

28

Figure 3-3. Schematic diagrams showing the successive stages in the palaeotectonic model for the development of the Huronian Supergroup sedimentary and volcanic rocks, and associated mafic intrusions (East Bull Lake and Nipissing Gabbro suites) in the Southern Geological Province, Ontario. (A) Incipient Passive Rift Stage (extension): Livingstone Creek Formation deposition within early developed grabens. (B) Main Rift Stage: Eruption of Huronian volcanic rocks and emplacement of East Bull Lake suite intrusions during extension. (C) Late Rift-Early Break-up: eruption of volcanic rocks – volcanics rocks found in Sudbury area - and deposition of Matinenda and McKim formations. Early break-up of the craton with possible subsequent formation of the Wyoming Craton (Roscoe and Card, 1993) (Modified after Bennett et al., 1991).

29

Figure 3-3. Schematic diagrams showing the successive stages in the palaeotectonic model for the development of the Huronian Supergroup sedimentary and volcanic rocks, and associated mafic intrusions (East Bull Lake and Nipissing Gabbro suites) in the Southern Geological Province, Ontario. (D) Passive Margin Stage and Initial Closure: deposition of three successive stages of continental glaciation (Cobalt, Quirke Lake and Hough Lake groups) on attenuated continental margin. This stage, which includes the initial closure of the rift basin due to arc-continent collision, likely marks the start of the Nipissing Gabbro suite intrusive event which continues over a period of ~50 Ma and into the beginning of the next stage, marked by intense collision and subduction events. (E) Collision/Subduction Stage: collision of an island arc with the Superior Craton block and deposition of foredeep sedimentary rocks of the Chelmsford Formation. This stage encompasses the metamorphic and orogenic events of the Penokean Orogeny (Modified after Bennett et al., 1991).

30

It is widely accepted that Huronian Supergroup deposition was complete by ~2.2 Ga,

the accepted age of the Nipissing Gabbro suite (Corfu and Andrews 1986; Noble and

Lightfoot, 1992), with termination of the sedimentary cycles brought about by continent-

arc collision between the Superior-Southern geological provinces and the Wisconsin

Magmatic Arc Terrane (e.g. Young, 1983; Hoffman, 1989). The terminal collisional

event, referred to as the Penokean Orogeny (~1.84 Ga; Holm et al., 2001) is understood

to be responsible for most of the metamorphism and deformation present within the

Huronian Supergroup rocks in Ontario and its equivalent rocks in the Lake Superior

region (Wisconsin, Michigan and Minnesota). The scale and intensity of the Penokean

Orogeny in the Sudbury area remains a contentious issue (e.g. Davidson et al., 1992;

Card 1992; Riller et al., 1999) due mainly to the lack of associated plutonism in Ontario.

3.2.4 Regional Correlation of the Huronian Supergroup

Young (1983) suggested stratigraphic relationships between Early Proterozoic

sedimentary-intrusive successions of the Lake Huron (Sudbury-Blind River) and Lake

Superior (Wisconsin and Minnesota) regions, summarizing this relationship in a regional

depositional and tectonic model. Young’s tectono-sedimentary model proposed that in

the Early Proterozoic the region was the site of an aulacogen (intracratonic graben or

trough) that opened into an ocean somewhere to the east-southeast, in the area that is

presently occupied by the Grenville Province. Specifically, Young (1983) considered the

upper part of the Huronian Supergroup (Gowganda, Lorrain and Gordon Lake

Formations) to be correlative with the lower part of the Chocolay Group (Enchantment

Lake Formation, Mesnard Quartzite, and Kona Dolomite-Wewe Slate) of the ~2.2 Ga

Marquette Range Supergroup (Fig. 3-1). Following deposition of the upper part of the

Huronian Supergroup and lower Chocolay Group, the region was subjected to folding,

uplift and intrusion of the Nipissing Gabbro suite (2.206-2.221 Ga; Noble and Lightfoot,

1992) during the McGregor phase. Young relates the intrusion of Nipissing Gabbro with

similarly timed intrusive events south of Lake Superior (Michigan and Wisconsin) and in

Minnesota (Hanson and Malhotra, 1971).

Young (1995) commented on the strong stratigraphic similarities that exist between

sedimentary sequences of the Huronian Supergroup and the Snowy Pass Supergroup

(Wyoming Province). The Cheyenne Belt of southeastern Wyoming is a major east-

31

west-trending shear zone that separates Archaean gneiss and Early Proterozoic

metasedimentary rocks of the Wyoming Province to the north from Proterozoic

eugeoclinal metamorphic rocks to the south (Karlstrom et al., 1983; Karlstrom and

Houston, 1984). Roscoe and Card (1993) proposed that sedimentary rocks of the Early

Proterozoic Snowy Pass Supergroup (Medicine Bow Mountains) and Snowy Pass Group

(Sierra Madre) are equivalent to Huronian Supergroup rocks. In particular, Roscoe

(1990) suggested that there exists a strong positive correlation between all stratigraphic

units of the Phantom Lake strata, Deep Lake Group, and lower parts of the Libby Group

in Wyoming and every unit in the western part of the Huronian Supergroup in Ontario.

Heaman (1997) offers further correlation between the Wyoming and Superior cratons,

noting that dyke rocks in the Bighorn and Beartooth Mountains of Wyoming share many

similarities with Matachewan dykes of the Southern and Superior Provinces.

Tectonic models proposed by Williams et al. (1991), Heaman (1997) and Roscoe and

Card (1993) suggested that the Wyoming Province was welded onto the southern margin

of the Superior Province at about 2.7 Ga. Sedimentary sequences in the Huronian and

Snowy Pass supergroups contain diagnostic horizons in similar stratigraphic positions

that are consistent with deposition in a single, broad, epicratonic basin that developed

atop a large and contiguous Archaean continent comprising the Superior and Wyoming

cratons (Roscoe and Card, 1993). Widespread intrusion of Nipissing Gabbro suite rocks

at ~2.2 Ga and their ~2.1 Ga (Premo and Van Schmus, 1989) equivalents in the

Wyoming Province approximated the onset of continental fragmentation (Fig. 3-3c). The

Wyoming Province fragment split off along the ~1.85 Ga Manitoulin-Niagara structural

zone and was rotated about 135°, as indicated by foresets and other directional features in

preserved sedimentary remnants within the Medicine Bow Mountains and Sierra Madre

(Roscoe, 1990).

The Hurwitz Group occurs as a widespread succession of predominantly

metasedimentary rocks up to 7 km thick in the Hearne Province that have been

interpreted to represent a passive-margin foredeep sequence (Aspler et al., 1989).

Similarities in the stratigraphy of the Hurwitz Group, Huronian Supergroup (Superior

Province) and Snowy Pass Supergroup (Wyoming Province) led Roscoe (1973) and

Young (1973) to propose a regional stratigraphic correlation between the three

32

sedimentary sequences. Patterson and Heaman (1991) supported this interpretation on

the basis of U-Pb baddeleyite-zircon analysis that yielded a minimum age of 2094 +26/-

17 Ma from a gabbro sill within the lower parts of the Hurwitz Group; the age of the

gabbro sill is within error of the ages proposed for Nipissing Gabbro intrusions in the

Southern Province.

Aspler and Chiarenzelli (1997) concur with previous interpretations of the Hurwitz

Group and its possible correlation with rocks of the Huronian and Snowy Pass

supergroups. In addition, these authors expand on the regional model, suggesting that the

rocks of the Huronian and Snowy Pass supergroups, along with several other passive-

margin sequences, were deposited near the boundary of a possible Early Proterozoic

supercontinent – termed Kenorland by Williams et al. (1991) – that may have included

parts of the Superior, Wyoming, Rae-Hearne and Slave provinces. Alternatively,

Patterson and Heaman (1991) conceded that, despite similarities in age and stratigraphy,

the Hurwitz Group may have been deposited on an unrelated microcontinent.

3.3 East Bull Lake Suite and Associated Rocks

East Bull Lake suite intrusions comprise an east-northeast trending, discontinuous

belt in the region of the ~1.85 Ga Sudbury Igneous Complex (Fig. 1-2). The three largest

and most studied are the East Bull Lake (the type example; Born, 1979; Chubb, 1994;

Peck et al., 2001), Agnew Lake (Vogel, 1996) and River Valley intrusions. Most East

Bull Lake suite intrusions were emplaced between 2.491 and 2.475 Ga (Krogh et al.,

1984; Prevec, 1993) and a summary of geochronology on the rocks of the East Bull Lake

suite is provided in Table 3-2. Intrusions of the East Bull Lake suite may represent the

eroded remnants of layered interconnected sills formed from plagioclase-rich tholeiitic

magmas (Vogel et al., 1998a).

The River Valley intrusion is the first of the East Bull Lake suite intrusions to have

certified Measured and Indicated mineral resources (25.4 million tonnes at 0.98 g/t Pd,

0.34 g/t Pt and 0.06 g/t Au; Pacific North West Capital Corp. Press Release, 22/07/04).

Prior to the work of Ashwal and Wooden (1989), the River Valley intrusion was thought

to be part of the belt of Grenville Province anorthosite massifs that extend from the

eastern USA, through Ontario and Quebec and into Labrador (Fig. 3-4). However,

Ashwal and Wooden (1989) reported a Pb-Pb age of 2560 ± 155 Ma and a Sm-Nd age of

33

2377 ± 155 Ma, and surmised that, despite being located within the southwestern

Grenville Province, the River Valley intrusion was best grouped with similar intrusions

west of Sudbury, now considered part of the East Bull Lake suite.

34

Intrusion Age + - Method Ref(Ma) (Ma) (Ma)

Absolute AgesAgnew Lake 2491 5 5 U/Pb zircon 1

East Bull Lake 2480 10 5 U/Pb baddeleyite,zircon 1

2472 76 76 Nd/Sm whole-rock, mineral 21859 5 5 Ar/Ar hornblende 31725 18 18 K/Ar whole-rock 21155 14 14 K/Ar whole-rock 2

Drury Twp. 1855 10 10 U/Pb zircon 4

Falconbridge Twp. 2441 3 3 U/Pb zircon 4River Valley 2475 2 1 U/Pb baddeleyite, zircon 5

2562 165 165 Pb/Pb whole-rock 62377 68 68 Nd/Sm whole-rock, mineral 62165 130 130 Nd/Sm whole-rock, mineral 62185 105 105 Rb/Sr whole-rock 61960 100 100 Rb/Sr whole-rock 6

Street Twp. 2468 5 5 U/Pb zircon 7Relative AgesRiver Valley 2446 3 3 U/Pb baddeleyite, zircon 8, 9

2460 20 20 U/Pb zircon 7, 92475 25 10 U/Pb zircon 7, 9

Street Twp. 2475 25 10 U/Pb zircon 7, 10

References: (1) Krogh et al. (1984); (2) McCrank et al. (1989); (3) Kamineni (1986); (4) Prevec (1993); (5) Easton et al. (1999); (6) Ashwal and Wooden (1989); (7) Corfu and Easton (2001); (8) Heaman (1997); (9) Easton and Hrominchuk (1999)(10) Easton and Murphy (2002)

Table 3-2. Summary of geochronology on rocks from the East Bull Lake suite of

intrusions (after Easton, 2003). Locations of East Bull Lake suite intrusions are shown in

Figure 1-2.

35

East Bull Lake suite intrusions are thought to have been emplaced into Neoarchaean

rocks at moderate to shallow crustal levels (Peck et al., 1993a; Vogel et al., 1999). East

Bull Lake suite intrusions west of the Sudbury Igneous Complex occur at or near the

Southern-Superior boundary but contact relationships between the intrusions and

surrounding Huronian sedimentary rocks are faulted or sheared and so the original

relationship between them is indefinite (Fig. 3-2). East Bull Lake suite intrusions east of

the Sudbury Igneous Complex, and in particular the River Valley intrusion, were likely

intrusive wholly into Neoarchaean rocks which are now located within the Grenville

Front Tectonic Zone (Fig. 1-2).

East Bull Lake suite intrusions, along with mafic and felsic (bimodal) volcanic rocks

of the Elliot Lake Group (Huronian Supergroup), related felsic plutons such as the

Murray and Creighton granites, and the Matachewan-Hearst Dike Swarm, outline the

trace of a plume-induced, regional, Palaeoproterozoic rifting event that lasted from 2.49

to 2.44 Ga, apparently centred in the area of Sudbury (e.g. James et al., 2002b). James et

al. (2002a) and Easton et al. (2004) presented a summary of the suite of igneous rocks,

referred to as the “rifting suite”, that record the initial trace of this intracontinental rifting

event. From oldest to youngest, they include:

~2490 to 2470 Ma: East Bull Lake intrusive suite

~2490 to 2450 Ma: Elliot Lake Group metavolcanic and minor plutonic rocks

- lowermost stratigraphy in the Huronian Supergroup

2473 and 2446 Ma: Matachewan and Hearst mafic dike swarms, respectively

~2450 to 2460 Ma: Elliot Lake Group/Superior Province granitic intrusions

- Creighton and Murray plutons

This rifting event produced a northeast-trending, southward-deepening basin that

probably resulted in the formation of as not yet identified oceanic crust (e.g. Card et al.

1972; Young 1983; Fahrig 1987; Hoffman 1989; Bennett et al., 1991). The geometry of

the northwest-trending dikes of the regionally extensive Hearst-Matachewan Dike swarm

coupled with their distribution with respect to the Elliot Lake Group rocks are consistent

with a north-northwest oriented arm of a failed rift (e.g. Fahrig 1987; Ernst and Buchan

2001). However, it is presently uncertain as to whether the East Bull Lake suite rocks

occur directly along a cryptic structure, or structures, related to this rift basin, or if the

36

present distribution of the bodies reflects some other emplacement mechanism (James et

al., 2002a). Alapieti et al. (1990), Alapieti and Lahtinen (2002), and Vogel et al. (1998b)

have described correlations with similar suites of Palaeoproterozoic intrusions

(Fennoscandian Layered Intrusive Suite) in the northeastern part of the Fennoscandian

Shield (Finland) that were emplaced in similar tectonic environments (Fig. 3-5); Heaman

(1997) suggested that the two regions may have been part of a more extensive ~2.47 Ga

Large Igneous Province (continental flood basalt magmatism).

3.3.1 Emplacement Models and Depth

Previous research on East Bull Lake suite intrusions in the Southern Province

suggested shallow depths (<8 km) of emplacement, possibly at the contact between the

Archaean basement (Superior Province) and supracrustal rocks of the Huronian

Supergroup (e.g. Card 1978; Peck et al. 1995; Vogel et al. 1998a, 1999). However,

Easton (2000a) suggested that the River Valley intrusion was emplaced at deeper levels

(8-12 km), either at the boundary between Archaean plutonic rocks and greenstone belts

or at the boundary between gneisses and a plutonic rock dominated mid-crustal layer.

Easton (2002) further suggested that several depths of emplacement are recorded within

the East Bull Lake suite east of Sudbury (Street, Loughrin, Henry and River Valley

intrusions), with these bodies possessing subtly different features depending on which

country rock gneiss association they are in contact (Fig. 3-6).

James et al. (2002b) reviewed two proposed models to explain the emplacement

mechanism for the East Bull Lake suite. The first model (Vogel et al., 1999), based on a

geological reconstruction and “unfolding” of the effects of Penokean deformation on the

East Bull Lake and Agnew Lake intrusions, proposes that these two intrusions were part

of an extensive, subhorizontal lopolithic sheet, as much as 2 km thick, 30-50 km north-

south, and more than 100 km east-west. James et al. (2002a) expanded this model to

include all of the East Bull Lake suite intrusions, suggesting that these bodies are

remnants of a larger interconnected intrusive body, analogous to the Great Dyke

(Zimbabwe), that would have been traceable for at least 300 km. An important outcome

of this model is that sulphide mineralization could be dispersed in large volumes of rock

(i.e. disseminated, low sulphide mineralization), resulting in relatively low grade PGE-

Cu-Ni sulphide that present excellent bulk tonnage exploration targets.

37

38

39

In addition, this model allows for the lower stratigraphic sequences and associated

mineralization to occupy rift, fault-related structures or embayments that would have

controlled magma intrusion and replenishment, potentially concentrating base metals as

massive sulphide (Cu-Ni) deposits. These lower sequences and associated mineralization

would not be as extensive or as well connected as the upper portions or main mass of the

intrusion, suggesting that deeper sections of these intrusions are promising in terms of

massive sulphide exploration targets.

In the second model, James et al. (2002a) proposed that intrusions of the East Bull

Lake suite were emplaced as groups of smaller, separate bodies, rather than as one or

possibly two large (now dismembered) intrusive complexes. This model implies that

individual intrusions could have been emplaced at different crustal levels, providing an

explanation for the differences in stratigraphy between the various intrusions as observed

by Easton (2000; 2002). An important consequence of this model is that it allows for

much greater variation in mineralization style and grade between intrusions (Easton et al.,

2004).

3.3.2 Geochemistry and Magma Composition

Although previously described as anorthositic intrusions (e.g. Lumbers, 1971, 1973;

Ashwal and Wooden, 1989), exposures and mapping of the East Bull Lake suite have

shown that they are dominated by leucogabbronorite, gabbronorite and smaller amounts

of gabbro, with anorthosite forming a small proportion of the rocks. Melagabbronorite,

troctolite and melatroctolite also occur in the discrete parts of the stratigraphy. Peck et al.

(2001), Vogel et al. (1999) and James et al. (2002a) demonstrated that plagioclase,

olivine, and orthopyroxene fractionation are responsible for the main chemical variation

of the rocks in the East Bull Lake and Agnew Lake intrusions, with very little

contribution from clinopyroxene. Primitive mantle-normalized rare-earth element (REE)

diagrams from the East Bull Lake suite of intrusions show light rare-earth element

(LREE) enrichment (La/Gd ~3-5), whereas the heavy rare-earth element (HREE) patterns

are nearly flat (Fig. 3-7). Weak to strong, positive Eu anomalies dominate except for the

most fractionated rocks in the Agnew Lake intrusion and local “contaminated” rocks in

the Marginal Zone of the River Valley intrusion.

40

41

Rocks lowest in the stratigraphy of each intrusion have the lowest REE contents

consistent with the petrographic and major element interpretations of the stratigraphy of

the intrusions (James and Born, 1985; Vogel et al, 1999; James et al., 2002b).

East Bull Lake intrusion pyroxenites that occur as inclusions have distinctive

patterns compared to those that occur as poorly formed layers; the pattern of the latter

suggests there may be quite primitive mafic liquids in the magma system very early in its

formation, where mineralization is dominant (James et al., 2002b). The LREE

enrichment patterns could be indicative of crustal contamination of a primitive, mantle-

derived magma that intruded the lower crust or alternatively, the LREE-enrichment might

be due to direct partial melting of an initially enriched, metasomatised mantle source

(Vogel et al., 1998a); the latter scenario is consistent with a plume-generated continental

rift event (James et al., 2002b).

Much of the work aimed at determining the magma composition of the East Bull

Lake suite magma(s) has been based on work in the East Bull Lake and Agnew Lake

intrusions (Peck et al., 1995, 2001; Vogel et al., 1998a, 1999; James et al., 2002a) and

very little work has been done to constrain the magmatic evolution of the River Valley

intrusion; estimates of parental magma compositions are reviewed in the context of the

River Valley intrusion by James et al. (2002b) and Easton et al. (2004). These studies

have demonstrated that the magma(s) that formed the East Bull Lake and Agnew Lake

intrusions were high-Al (16-20 wt% Al2O3), except for mela-cumulates, low-Ti (≤0.5

wt% TiO2) tholeiites, with 100-500 ppm S in unmineralized samples, low Cr2O3 (<250

ppm), Mg-number of 54-60, and Cu/Ni = 0.3-0.8 (James et al., 2002b).

In both the East Bull Lake and Agnew Lake intrusions, there is an abundance of

mafic dykes of the Matachewan Dyke Swarm, which are normally plagioclase-phyric

(Osmani, 1991). Vogel et al. (1999) showed that the oldest of these at the Agnew Lake

intrusion, the Streich Dike, has a composition whose major, trace and REE geochemistry

is suitable as a parent for most rock types in the Agnew Lake intrusion. The Streich Dike

intrudes only the lower part of the Marginal Zone and appears to be a major feeder to the

Agnew Lake intrusion (James et al., 2002b). Peck et al. (1993a, 1995, 2001) also

suggested that the Matachewan Swarm dikes are the most likely candidate for parent

magmas to the East Bull Lake suite intrusions. In contrast to East Bull Lake and Agnew

42

Lake intrusions, mafic dikes are not as abundant within or marginal to the River Valley

intrusion (James et al., 2002b). A sample, from a large area of massive norite in Crerar

Township, interpreted as a potential intrusive feeder dike, has an Mg-number of 73 and a

composition of 13.5 wt% Al2O3, 11.5 wt% MgO and 51.5 wt% SiO2, suggestive of a

boninitic composition (James et al., 2002b).

3.3.3 Sulphide Mineralization

James et al. (2002a) presented a summary of general characteristics common to all of

the East Bull Lake suite intrusions studied to date. One feature, significant to mineral

exploration and economic potential of these intrusions, is the presence of PGE-Cu-Ni

sulphide mineralized fragment-bearing lithologies at or proximal to the footwall or

sidewall contacts or margins of these intrusions, referred to as “contact-type” PGE (Peck

et al., 1993a). These fragment-bearing units range in character from igneous breccias that

are strongly heterolithic and have highly variable fragment size ranges, to inclusion-

bearing units that are moderately heterolithic and have much less variable fragment sizes.

The thickness and length (strike-continuity) of these fragment-bearing zones is variable

but the potential for these targets to contain large tonnages of PGE-Cu-Ni mineralization

makes them attractive exploration targets. Mineralization in the three largest East Bull

Lake suite intrusions is best developed where there is a primary igneous contact with rock

units that represent the lowest or outermost (Marginal Zone or Marginal Series)

stratigraphic zone in the intrusion (James et al., 2002b). Vogel et al. (1999) demonstrated

that mineralized zones of “inclusion-bearing gabbronorite” also occur higher in the

stratigraphy at the Agnew Lake intrusion, and that strataform, reef-like mineralization

can occur in the uppermost part of the intrusion. Vogel et al. (1999) attributed the reef-

like mineralization to late, fractionation-induced, sulphide liquation. Contact-type

mineralized zones normally have <1% Cu+Ni, Cu/Ni = 2-20, and PGE = 0.5-4 g/t over 2-

10 m in drill core, with much narrower intervals as high as 8-16 g/t Pt+Pd (James et al.,

2002b).

Sulphide mineralization in East Bull Lake suite intrusions is commonly hosted in

xenolith-bearing units that typically consists of 1-5% chalcopyrite +/- pyrrhotite,

pentlandite, and minor pyrite intergrown with secondary silicate minerals (epidote, calcic

amphibole, chlorite, quartz, ±biotite). Sulphides textures are primarily disseminated and

43

blebby with minor interstitial and subordinate net-textures. The sulphides occur within

relatively massive, medium- to coarse-grained, and typically vari-textured,

leucogabbronorites and gabbronorites, and in the matrix and mafic cognate xenoliths of

inclusion-rich leucogabbronorites and gabbronorites. Typically, sulphide mineralization

is erratically distributed in the massive rocks, and is so fine-grained and in such small

volume (1-5%) as to exhibit little or no gossan. Detailed reviews of PGE-Cu-Ni

mineralization in the East Bull Lake suite intrusions are provided by Peck et al. (1993a,

1995, 2001), Vogel et al. (1999), Cabri (2001) and James et al. (2002a, 2002b).

3.3.4 Platinum-Group Minerals

Cabri (2001) described the platinum-group minerals (PGM), gold and sulpharsenide

minerals in heavy mineral concentrates (pyrrhotite, chalcopyrite, pentlandite, pyrite and

ilmenite) from the East Bull Lake intrusion, using SEM and semi-quantitative EDS

analysis. Cabri (2001) reported that the PGM consist of six palladium minerals: froodite

(PdBi2), kotulskite (PdTe), merenskyite (PdTe2), michenerite (PdBiTe), and other

unidentified Pd-As and Pd-As-Sb phases; two platinum minerals (sperrylite (PtAs2) and

platarsite (PtAsS); and, a rhodium-arsenide sulphide mineral (hollingsworthite (RhAsS).

The sulpharsenide minerals cobaltite and arsenopyrite contain trace to several weight

percent Pd and Rh. The PGM range in size from <1 µm to 22x32 µm, and occur in all

major sulphide minerals although pyrrhotite is the most common sulphide host. Cabri

(2001) also noted that samples containing the highest concentrations of pyrrhotite and

chalcopyrite had higher PGM contents and PGE concentrations. In studying polished

thin sections, Peck et al. (1993a) noted similar PGM for mineralized samples from

contact-type mineralization in the East Bull Lake intrusion; Peck et al. (1993a) also noted

that much of the PGM were at sulphide-silicate grain boundaries, within secondary

silicates, and were commonly within fractures. Similar sulphide-PGM assemblages from

the Portimo Complex (contact-type mineralization) were described by Iljina (1994).

At the Dana North area in the River Valley intrusion, PGM occur as discrete mineral

phases adjacent to base-metal sulphides, enclosed by base-metal sulphides, enclosed by

silicates, and adjacent to silicates (James et al., 2002b). James (2004) reported on PGM

in 12 polished thin section samples from the River Valley intrusion, using SEM and

semi-quantitative EDS analysis. The study described several discrete PGM phases from

44

the Dana Lake, Lismer’s Ridge, Azen and Razor areas and these are summarized in Table

3-3. PGM range from ~3-30 µm but most are within the range 10-20 µm, and are

dominated by Pd-Bi tellurides, Pd-Sb arsenides, and Pt-arsenides with subordinate Pt-

tellurides, Pd-alloys, Pt-Fe-alloys, Pt-Pd-sulpharsenides, and Pt and Pd-sulphides (James,

2004).

3.3.5 Sulphide and PGE Formation

The requirements for the formation of the sulphide-related PGE mineralization

include a fertile magma, an immiscible sulphide liquid, a sufficiently high R-factor

(silicate to sulphide mass ratio; Lesher and Burnham, 1999) related in part to a turbulent,

convecting magma, and sulphide contamination from an external source (Keays, 1995).

For magmas that may be feeders to these intrusions, Pd and Pt concentrations average

18.9 ppb Pd and 24.20 ppb Pt for the Streich Dike (Vogel et al., 1999) and 72 ppb Pd and

38 ppb Pt for Hearst-Matachewan Swarm dikes (James et al., 2002a). These fertile PGE

compositions are typical of second-stage magmas as described by Hamlyn et al. (1985),

Hamlyn and Keays (1986) and Keays (1995). The potential parent magmas (i.e.

Matachewan Dike Swarm), as well as most rocks in the East Bull Lake suite intrusions

are S-undersaturated (~50-500 ppm S) and therefore, to reach S saturation (~800-1000

ppm S), require contamination and/or significant cooling (James et al., 2002b). In the

mineralized Marginal and Inclusion/Autolith-Bearing zones of the River Valley intrusion,

minor local contamination is indicated by rare footwall xenoliths, and chilled diabase in

the Marginal Zone is evidence of relatively rapid heat loss to the footwall (James et al.,

2002b).

Peck et al. (2001), in modelling the magmas of the East Bull Lake intrusion,

determined that there is insufficient PGE in a single large basal magma pulse or pulses to

form the zones of PGE observed in that intrusion. Instead, Peck et al. (2001) suggested

that the contact region of the intrusion was subjected to multiple injections of S-saturated

magma, that transported 1-5% immiscible sulphide droplets which were capable of

scavenging the PGE in a turbulent environment, for significant periods, prior to

emplacement into the contact region of the intrusion.

45

Area PGM Size (µm) Probable PGM IdentityDana Lake Pt-alloy 1-3 -

Pd-Bi-Te 30 x 10; 5-10 micheneritePtAs 5-10 sperrylite

PdAsSb 5-10 palladium antiminideLismer’s Ridge PtAs 5-20 sperrylite

PdSe 5 palladesitePdAs 1-10 palladoarsenide

RhPtAsS 1-10 hollingsworthitePdTe 1-10 merenskyite

PdAsSb vein-like cluster palladium antiminideAzen Creek Pt-Te±Bi,Fe 2-6 moncheite

Pd-S 3 x 3 vysotskiteRazor Pd-Bi-Te 20 x 20; 15 x 8 michenerite

Table 3-3. Summary of platinum-group minerals noted from the River Valley intrusion

(from James, 2004).

46

3.4 Nipissing Gabbro Suite and Associated Rocks

More than 25% of the areas of the southern Superior and Southern geological

provinces in Ontario are covered by the dominantly gabbroic, tholeiitic, intrusive rocks

referred to collectively as either Nipissing Gabbro or Nipissing Diabase (Miller, 1911).

Considered to be a product of rift-related magmatism (Lightfoot and Naldrett, 1996),

these intrusions are dominantly dikes and sills of irregular shape, and where more or less

linear, they define a broad northeast-southwest trend (Fig. 1-2); faults (primarily

northeast-striking) and may have also played a role in controlling the emplacement of

some of the intrusions. Fieldwork indicates that locally, at the time of intrusion,

sedimentary strata were semi-lithified and that there was significant interaction between

Nipissing magmas and a relatively soft, water-rich sedimentary environment (e.g. Young,

1983; Shaw et al., 1999).

The majority of Nipissing Gabbro intrusions was emplaced into Archaean basement

rocks and sedimentary rocks of the Huronian Supergroup during a magmatic event that

spanned an interval of approximately 15 Ma between 2206 and 2221 Ma (Corfu and

Andrews, 1986; Noble and Lightfoot, 1992; Buchan et al., 1998). A summary of

geochronology on rocks of the Nipissing Gabbro suite is provided in Table 3-4. The

Nipissing Gabbro intrusions were emplaced into the Huronian Supergroup after early

deformation of the Huronian strata during the 2.45-2.3 Ga Blezardian Orogeny

(Stockwell, 1982), but prior to subsequent deformation and metamorphism during the

1.87-1.83 Ga Penokean Orogeny (Card et al., 1972; Morris, 1977). Young (1995)

suggested that some of the Nipissing Gabbro intrusions were emplaced into large-scale

early folds; folds that may have formed as a result of gravity-controlled mass movements

related to extensional tectonics.

Dike swarms similar in age and paleomagnetic pole position to the Nipissing Gabbro

suite include the Senneterre (2.216 Ga), Maguire (~2.23 Ga) and Klotz (2.21 Ga) dike

swarms, all located in the northeastern Superior Province (Buchan et al., 1998). It has

been suggested, mainly on the basis of paleomagnetic data, that there is a second age of

"Nipissing" intrusions, mostly northeast-trending dikes and possibly coincident in age

with the Biscotasing (2.167 Ga) dike swarm (e.g. Buchan and Card, 1985; Buchan et al.,

47

1993). The relationship of these younger "Nipissing" intrusions to the older, more

voluminous sills and intrusions of the Nipissing Gabbro suite have yet to be determined.

Location/Area Age +/- Span Method Ref. (Ma) (Ma) (Ma)

Bruce Mines-Blind River 2170 200 2370-1970 Rb/Sr;wr 1 Bruce Mines-Blind River 2155 80 2235-2075 Rb/Sr;wr 2 Bruce Mines-Blind River 2134 40 2174-2094 Rb/Sr;biotite 3 Bruce Mines-Blind River 1700 55 1755-1645 Rb/Sr;wr;feldspar 2

Gowganda 2162 27 2189-2135 Rb/Sr;wr 4 Gowganda 2116 27 2143-2089 Rb/Sr;wr 3

Wanapitei Lake 2109 40 2149-2069 K/Ar;wr 5 [Rathbun Lake intrusion]

Gowganda 2219.4 3.6/3.5 2223-2216 U/Pb, baddeleyite *6 [Miller Lake intrusion]

Wanapitei Lake 2210 4 2214-2210 U/Pb, baddeleyite *7 [Bonanza Lake intrusion]

New Liskeard/Cobalt 2217.2 4 2221.2-2213 U/Pb, baddeleyite *8 [Kerns intrusion]

New Liskeard/Cobalt 2209.6 3.5/4 2213.1-2206 U/Pb, baddeleyite *8 [Triangle Mountain intrusion]

*most reliable age constraints; wr = whole rock References: (1) Van Schmus et al. (1963); (2) Van Schmus (1965); (3) Buchan et al. (1989); (4) Fairbairn et al. (1969); (5) Rowell (1984); (6) Corfu and Andrews (1986); (7) Conrod (1989); (8) Noble and Lightfoot (1992)

Table 3-4. Summary of the geochronology on rocks from Nipissing Gabbro intrusions

located between Sault Ste. Marie and Cobalt, Ontario.

48

There are conflicting ideas regarding the tectonic setting and source of the Nipissing

Gabbro intrusions. Some workers have suggested that the Nipissing Gabbro intrusions

may represent the feeders of an eroded continental flood basalt system (e.g. Lightfoot et

al., 1987; Bennett, 1997). Alternatively, Fahrig (1987) proposed that a spreading-point

origin for Nipissing Gabbro intrusions was located west-southwest of the Sudbury area,

in the direction of an ocean opening, now represented by rocks of the Animikie Basin. In

contrast, Buchan et al. (1998) suggested a plume-induced, spreading-point origin well

northeast of Sudbury, with the Nipissing Gabbro intrusions being fed laterally by

Senneterre dikes which developed during the break-up of the eastern and northeastern

sides of the Superior Province; the break-up was purportedly initiated by the 2.22 Ga

Ungava and/or 2.17 Ga Biscotasing mantle plumes, located near present day Ungava

Bay. According to Buchan et al. (1998), the Nipissing Gabbro intrusions formed when

laterally-flowing magma, moving through Senneterre dikes, intersected favourable stress

regimes in the subhorizontal sedimentary strata of the Huronian Supergroup, some 1500

km from the proposed plume centre. Data from Anisotropy of Magnetic Susceptibility

studies by Ernst et al. (1999), show a dominantly horizontal flow regime, favouring the

linear source (i.e. dikes) model of Buchan et al. (1998) rather than the centralized plume-

related model (e.g. Lightfoot et al., 1987), which would have produced anisotropy results

indicating vertical flow regimes (i.e. cone sheets, extensive feeder dykes and lopolithic

bodies).

Conventional models for the Nipissing Gabbro suite involve an association with

plume-related magmatism, and are suggestive of an environment favourable for the

formation of economic concentrations of magmatic sulphide minerals rich in Cu-Ni-PGE

(e.g. Lightfoot et al., 1987; Vogel et al., 1998a). Moreover, there are several geochemical

and structural similarities between Nipissing Gabbro intrusions and the intrusions that

host the prolific Ni-Cu-PGE deposits in Noril’sk, Russia (e.g. Lightfoot and Naldrett,

1996) and the large, basin-related Ni-Cu-PGE deposits found in the Insizwa Complex,

southern Africa (e.g. Lightfoot et al., 1984). However, these same geochemical

signatures, which suggest continental flood basalt and mantle plume associations, are also

indicative of subduction related magmatism (i.e. boninites).

49

3.5 Matachewan and Hearst Dike Swarms

The Matachewan and Hearst dike swarms (also referred to as the Hearst-

Matachewan Swarm) cover an area of 500 to 700 km and together are the second largest

dike swarm in the Canadian Shield (Halls, 1988). In the southern Superior Province and

Southern Province of central Ontario, the dike swarm trend north to northwesterly and

have a U-Pb age of 2454±2 Ma (Heaman, 1988). Dikes are generally 10 m across, but up

to 250 m, have vertical to sub-vertical dips, are mainly quartz diabase and are commonly

characterised by blocky phenocrysts of saussuritized plagioclase crystals up to 20 cm in

length (Osmani, 1991). The southern convergence of the Matachewan and Hearst dike

swarms is consistent with a failed-arm environment, with a spreading point toward the

south (Osmani, 1991; Fahrig, 1987), approximating the region of northeast-southwest

Palaeoproterozoic rifting in the Sudbury area.

3.6 Sudbury Dike Swarm and Grenville Dike Swarm

Intrusions of the 1.24 Ga Sudbury Dike Swarm (Van Schmus, 1975; Krogh et al.,

1987) mark the last major magmatic activity in the Southern Province, crosscutting rocks

and structures of the Superior and Southern geological provinces. The dikes extend

southward into the Grenville Front Tectonic Zone of the Grenville Province where they

are displaced by faults related to the Grenville Orogeny. The Sudbury Dike Swarm

extends over a region of approximately 275 km and represents a relatively smaller mafic

event relative to larger dike swarms such as the Mackenzie Dike Swarm which is more

than 2,100 km long (Shellnutt, 2000). Rocks of the Sudbury Dike Swarm are typically

medium- to coarse-grained, olivine-magnetite gabbro dikes that strike ~310° and dip

~90°. The whole rock geochemistry of the Sudbury Dikes is consistent with ocean-island

alkaline basalt, transitional between alkaline and tholeiitic, with positive Eu anomalies

and a within-plate (intra-plate rift) tectonic setting (Shellnutt, 2000).

The Grenville Diabase Dike Swarm was emplaced at ~590 Ma (Kamo et al., 1995)

and is observed cutting country rock and a Sudbury swarm diabase dyke in the area of the

River Valley intrusion, Dana Township (Easton, 2003). Geochemical data on the

Grenville Diabase Dike Swarm in Dana Township are provided by Easton (2003).

50

3.7 Sudbury Igneous Complex

The Sudbury Structure has been variously interpreted as originating from meteorite

impact, impact-induced plutonism and volcanism, and volcanism (Pye et al., 1984).

Nonetheless, the Sudbury Structure is regarded by most as the deformed and eroded

remnant of a 200 to 250 kilometre diameter, multi-ring impact basin (Grieve, 1994),

deformed by Penokean tectono-metamorphism between 1.9 and 1.7 Ga (Easton, 2002).

The core lithologies of the structure, referred to as the Main Mass, are considered by

Lightfoot et al. (2000) to be differentiates of an impact melt sheet (silicates and

sulphides), essentially derived entirely from crustal lithologies (Keays and Lightfoot,

2004) and emplaced at 1.85 Ga (Krogh et al., 1984) into rocks of the Proterozoic

Southern and Archaean Superior geological provinces.

Overlying the Main Mass is the sedimentary Whitewater Group, which in-fills the

central depression immediately above the Sudbury Igneous Complex, and brecciated

footwall rocks around the Sudbury Igneous Complex. The Whitewater Group comprises

breccias of the basal Onaping Formation, pelagic metasedimentary rocks of the Onwatin

Formation, and meta-greywackes of the Chelmsford Formation (Dressler et al., 1991).

Young et al. (2001) interpreted the overlying sedimentary rocks of the Whitewater Group

to represent a preserved portion of a widespread flysch apron that would have spread

across the southern margin of the Superior Province as foreland basin fill, as a

consequence of the closure phase of the Wilson cycle during the Penokean Orogeny.

The southern part of the Sudbury Igneous Complex was weakly metamorphosed by

an event which also retrograded previously metamorphosed rocks of the Huronian

Supergroup, especially along major faults, at ~1.7 Ga (e.g. Schandl et al., 1994; Easton et

al., 1996; Fedo et al., 1997). Magmatism also occurred at 1.75 to 1.73 Ga and at 1.5 to

1.45 Ga in the Killarney Magmatic Belt southwest of Sudbury (van Breemen and

Davidson 1988; Krogh, 1994).

3.8 Regional Metamorphism and Structure

Mesoproterozoic rocks of the Grenville Province (Figs. 1-1 and 1-2) in the Sudbury

area consist mainly of metamorphosed Neoarchaean and Palaeoproterozoic rocks

(Easton, 1992, 2000b). In the Sudbury region, the Grenville Front Boundary Fault, which

marks the northern limit of the collisional Grenville and Penokean orogens at ~1.0 Ga

51

and ~1.75Ga, respectively, extends north-northeast from the northern USA, through the

area south of the Sudbury Igneous Complex, cutting across the northern portion of the

River Valley intrusion (Dana Lake area) and northeastward through the Province of

Quebec (Fig. 1-1). Immediately south of the Grenville Front Boundary Fault lies the

approximately 30 km wide Grenville Front Tectonic Zone (Fig. 1-2). Many lithologies

within the Grenville Front Tectonic Zone can be correlated on the basis of geochemistry

and geochronology with lithologies of the Southern and Superior provinces, including

rocks of both the East Bull Lake and Nipissing Gabbro suites (Easton, 1992, 2000b;

Corfu and Easton, 2001; Easton and Hrominchuk, 1999).

In the Southern Province, rocks of the East Bull Lake and Nipissing Gabbro suites

were affected locally by shock metamorphism at 1.85 Ga due to the Sudbury Event, and

regionally by folding and sub-greenschist to lower amphibolite facies metamorphism at

~1.84 Ga related to the Penokean Orogeny (Easton, 1992; James et al., 2002b). Within

the Grenville Province these same intrusions may have been locally recrystallized by

metamorphism at ~1.7 Ga and ~1.45 Ga, and at ~1.07 to 1.04 Ga by the Grenville

Orogeny (Corfu and Easton, 2001; Easton, 2000b).

With the exception of the central portion of the Southern Province, Nipissing Gabbro

intrusions were subjected to relatively low grades of metamorphism (sub- to lower

greenschist facies) and are little deformed (e.g. Card and Pattison, 1973; Card, 1978).

Within the central part of the Southern Province, between approximately Blind River and

Sudbury, East Bull Lake and Nipissing Gabbro intrusions and Huronian Supergroup

strata were subjected to low-pressure, regional metamorphism up to amphibolite facies

during the Penokean Orogeny (e.g. Card, 1978; Bennett et al., 1991). Although there is

field evidence that the East Bull Lake suite intrusions have been folded (e.g. Vogel et al.,

1998a), East Bull Lake suite and Nipissing Gabbro intrusions normally lack any

perceptible penetrative tectonic fabric, as noted in field observations during the course of

this study.

3.8.1 Regional Albitization

Several regional studies have characterized potassic and sodic metasomatism in the

Southern Province in Ontario and its potential relationship to felsic plutonism and arc

collision (e.g. Siemiatkowska and Martin, 1975; Gates, 1991; Schandl et al., 1994; Fedo

52

et al., 1997). One such study (Gates, 1991), aimed at documenting Au and base metal

mineralization associated with widespread albitization (sodic metasomatism and/or

fenitization), demonstrated a relationship between Au and Ni-Cu±Co sulphide

mineralization, and localized albitization in the area stretching from Temagami (east of

Sudbury) to the Bruce Mines area (west of Sudbury). Schandl et al. (1994) determined a

U-Pb age of 1700 ±2 Ma for albitized rocks associated with a Au mineralizing event in

the Wanapitei Lake area, east of Sudbury; this age suggests that the albitization event was

coeval with a period of granitic plutonism in the Southern Province between 1750 and

1700 Ma (van Breemen and Davidson, 1988; Davidson et al., 1992). Schandl et al.

(1994) concluded that the presence of fine-grained hydrothermal monazite,

fluorocarbonates (bastnäsite and synchysite) and an Y-REE mineral (gadolinite),

combined with elevated rare earth element (REE) concentrations, and the disparity

between the age of albitization (~1700 Ma) and ages (2700, 1800-1900 and 1100 Ma;

Sage, 1991) of known carbonatite-alkalic complexes in the region, suggested that

sodium-rich fluids may have been generated by alkalic or carbonatitic rocks at depth.

Schandl et al. (1994) also demonstrated a positive correlation between Au and Co that

was independent of Na2O, suggesting that the concentration of Au did not occur during

the albitization but was coeval with the partial replacement of albite by chlorite and (or)

sulphides. On the basis of this positive Au-Co correlation, Schandl et al. (1994)

suggested that the Au was more than likely concentrated to economic grade by Co-±Ni-

bearing low pH fluids, which precipitated the Au together with some of the secondary

sulphide and chlorite minerals, utilizing the fractured, albitized rocks (caused by high pH

or peralkaline fluids) that acted as conduits for the mineralizing fluids.

3.8.2 Murray Fault System

The Murray Fault System (or Murray Fault Zone), extending for more than 150 km

through the Southern Province, south of Sudbury and westward along the north shore of

Lake Huron toward Sault Ste. Marie (Figs. 1-1 and 1-2), is a major dextral strike-slip

structure of ductile shear (Williams et al., 1991). Card et al. (1972) suggested, in addition

to being a major regional structure, the Murray Fault System also acts as a distinct

paleoenvironmental facies marker with rocks north of the Murray Fault System

53

interpreted as fluvial and those south of it as deep-water turbidites; this interpretation

implies that the Murray Fault System was active during Huronian Supergroup deposition.

The Murray Fault System marks an abrupt change from dominantly sedimentary and

relatively unstrained, sub-greenschist facies (5 km burial depth) rocks to the north, and

highly strained, lower to middle amphibolite facies (15 to 20 km burial depth) volcanic-

sedimentary rock sequences to the south (Bennett et al., 1991); dip-slip movements of

approximately 10 to 15 km are indicated by this metamorphic distinction. Sedimentary

sequences of the Huronian Supergroup are for the most part thickest in regions south of

the Murray Fault System. Zolnai et al. (1984) suggested that the sedimentary rocks south

of the Murray Fault System accumulated to greater thicknesses than those north of the

Murray Fault System. Subsequently, rocks south of the Murray Fault System were

tectonically buried to middle crustal depths and were then thrust up and over adjacent

Huronian Supergroup rocks to the north along the Murray Fault System; ensuing erosion

would have produced the present day configuration.

East of Sudbury, near the town of Coniston, the Grenville Front Boundary Fault and

the Murray Fault System are thought to merge into the Wanapitei Fault (Davidson, 1997).

This fault can be traced through Street Township, then eastward where it is referred to as

the Ess Creek and Grenville Front Boundary faults (Fig. 1-2), and following the trend of

the Kabikotitwia and Sturgeon Rivers (Easton and Murphy, 2002). Easton et al. (2004)

considered all Huronian strata located west and northwest of the Wanapitei and Ess

Creek faults as north of the Murray Fault System and all Huronian strata preserved within

the Grenville Province to have been originally deposited south of the Murray Fault

System.

54

CHAPTER 4: NIPISSING GABBRO INTRUSIONS

4.1 General Geology and Regional Morphology

The ~2.2 Ga Nipissing Gabbro intrusions are associated with and intrude the

sedimentary rocks of the Huronian Supergroup and their Archaean granite-greenstone

basement rocks within the Southern Province of Ontario (Fig. 1-2). For the most part,

intrusions in the Sault Ste. Marie-Elliot Lake area (Fig. 1-1), north of the Murray Fault

Zone and within several kilometres west of the Sudbury Igneous Complex, are

considered to be weakly to moderately deformed (Fig. 1-1). This contrasts with

intrusions in the Sudbury-Espanola area (Fig. 1-1), south of the Murray Fault Zone,

which are interpreted to be moderately to highly deformed. Contrasting these are

exposures of Nipissing Gabbro intrusions that occur in the belt of Huronian sedimentary

rocks south and southwest of the Sudbury Igneous Complex and north of the Murray

Fault Zone (Figs. 1-1 and 1-2) which are little to moderately deformed. Nipissing

Gabbro intrusions located northeast of the Sudbury Igneous Complex and within the

Cobalt Embayment (Fig. 1-1) are considered to be weakly deformed to locally

undeformed.

In general, it appears as though deformed Nipissing Gabbro intrusions are hosted by

lower sequences of Huronian Supergroup rocks, whereas the relatively undeformed

intrusions are hosted by upper sedimentary sequences. This disparate degree of

deformation and the association with different levels of Huronian Supergroup rocks

suggests that higher level Nipissing Gabbro intrusions are generally less deformed than

those emplaced and subsequently exhumed from lower stratigraphic levels. This may

also in part be related to primary features (i.e. structures and sedimentary bedding planes)

that developed at various stratigraphic depths within the rift basin sedimentary sequences,

controlling the initial emplacement of the Nipissing Gabbro magmas.

4.1.1 Local Morphology

Although many of the Nipissing Gabbro intrusions have been somewhat

metamorphosed and deformed, some of the intrusions are thought to have retained their

primary morphologies as reflected by the current outcrop patterns. Outcrop patterns of

Nipissing Gabbro within the study area include tabular intrusions, open ring structures,

55

and massive irregular shaped bodies (Figs. 1-2 and 5-1). These outcrop patterns are

interpreted to represent four main morphologies (Jambor, 1971; Buchan et al., 1989): (1)

undulating sills and dikes; (2) concordant homogenous sills; (3) cone sheets or ring dikes;

and, (4) lopolithic-like or thick stock-like bodies. Horst and graben structures (block-

faulting) also appear to play a major role in determining the level of stratigraphy of each

intrusion through the study area, and particularly in the regions southwest, south and east

of Sudbury (Fig. 1-2).

The majority of Nipissing Gabbro intrusions are interpreted to occur as near-

horizontal sheets or undulating sills (Fig. 4-1), consisting of basins and arches, and near-

vertical dikes, that are predominantly less than 1000 metres thick (Hriskevich, 1968;

Jambor, 1971; Conrod, 1988, 1989). Disseminated to massive Cu-Ni-PGE sulphide

mineralization in these types of intrusions is concentrated within the basin or limb

portions and pods of dominantly massive pyrrhotite occurring within the arches. Much of

the mineralization is associated with a thick (generally >100 m) orthopyroxene gabbro

unit (Lightfoot and Naldrett, 1996; Jobin-Bevans et al., 1998, 1999). Examples of this

form include the Appleby, Basswood, Louie Lake, and Makada Lake intrusions (Fig. 1-

2).

Tabular homogeneous sills form a second type of intrusion that was recognized in

the study area. These types of intrusions extend in a tabular (linear) manner for several

hundred metres to several 10’s of kilometres and include the Charlton Lake (Casson

Lake), Bell Lake (Nairn), and Manitou Lake intrusions (Fig. 1-2). The gabbroic rocks

within these intrusions exhibit very little across-strike differentiation and remarkable

homogeneity along strike.

Arcuate and open-ring outcroppings of Nipissing Gabbro, described by Buchan et al.

(1989) as cone sheets, comprise a third form of intrusion. These forms are distinguished

by structural features in surrounding sedimentary rocks that suggest the gabbro in these

types of intrusions were emplaced as shallow (<50°), inward-dipping, cone-shaped

intrusions that are tens of metres to several hundred metres thick (Jambor, 1971; Lovell

and Caine, 1970; Jobin-Bevans et al., 1998). These types of intrusions contain

disseminated and blebby sulphides hosted in orthopyroxene gabbro, occurring within a

56

few hundred metres of the basal contact of the intrusions. Examples of this form include

the Kukagami Lake (Photo 4-1) and Rathbun Lake intrusions (Figs. 1-2 and 5-1).

Photo 4-1. Kukagami Lake sill “Kukagami Cliff Section” – the southward dip is apparent

(~40 degrees) as defined by the regular jointing; looking east at south-dipping sill. The

maximum height of the hill is about 15 metres. The approximate trace of the basal

contact is shown.

57 57

58

The fourth type of intrusion, the lopolithic-like form (i.e. saucer-shaped), is rare and

is interpreted to represent deeper “feeder” systems to the stratigraphically higher sill, dike

and cone sheet type of intrusions. These deeper exposures, which are fault bound on a

regional scale, are thought to have been exposed through uplift along the bounding fault

lines (Dressler, 1979; Innes and Colvine, 1979; Jobin-Bevans et al., 1998). In the

lopolithic-like form, disseminated, semi-massive and massive sulphide mineralization is

hosted by orthopyroxene gabbro within tens of metres of the footwall sedimentary rocks,

and within topographic irregularities along the footwall contact. An example of this form

is the Chiniguchi River intrusion in Janes Township (Figs. 1-2 and 5-1).

Contacts between intrusions and the dominantly sedimentary country rocks are not

well exposed and are generally characterized by swampy or low lying areas adjacent to

elevated outcrops of Nipissing Gabbro intrusive rocks or sedimentary rocks. Types of

observable contacts are variable but most commonly comprise sharp, straight contacts

cross-cutting Huronian Supergroup sedimentary rocks and conformable, sill-like contacts

following the bedding of the host Huronian Supergroup rocks (Photo 4-2a); other contact

types include faults and irregular, tongue-like protrusions of Nipissing Gabbro cutting

into Huronian Supergroup rocks (Photo 4-2b); similar contact types were observed by

Conrod (1988).

4.2 General Stratigraphy

The general stratigraphy of Nipissing Gabbro, which has been described in previous

reports (e.g. Hriskevich, 1968; Conrod, 1988; Lightfoot and Naldrett, 1996), is

remarkably consistent within individual intrusions, particularly where the intrusion is

well-differentiated (Fig. 4-2). Small-scale folds are rare in Nipissing Gabbro intrusions

and any recognizable folding appears to be related to large-scale, regional events.

Consequently, the observed stratigraphy within individual intrusions is interpreted to

reflect the original arrangement of layers within magma chambers. The varying

proportion of differentiates and/or hybrid rocks (granophyre, aplite, granite, granodiorite)

versus orthopyroxene gabbro and gabbro in any given intrusion may reflect the reactivity

of the country rock with the magma and the degree of local assimilation and/or

contamination.

59

Photo 4-2. (A) Looking north toward a conformable, sill-like contact that follows the bedding of

the host Huronian Supergroup sedimentary rocks, south end of the Rauhala property, Waters

Township. The contact region is indicated by the white dashed line. The height of the overlying

gabbro unit is about 2 metres. (B) Irregular contact of Nipissing Gabbro cutting into Huronian

Supergroup sedimentary rocks from outcrops near the Grenville Front Boundary Fault, west of

Hwy #805 in the eastern part of Janes Township. The Canadian one dollar coin is about 2.5 cm in

diameter.

60

61

Alternatively, the differing proportion may reflect the relative position of the section

and/or its current level of erosion, and therefore surface exposure, through the intrusion,

if convection played a major role in the development of the intrusion (Conrod, 1988;

Lightfoot and Naldrett, 1989).

Previous work by Jambor (1971), Conrod (1988) and Lightfoot and Naldrett (1996)

produced a type-stratigraphy for Nipissing Gabbro intrusions. This current study, which

integrates geological surface mapping, ground geophysical surveys and diamond drill

hole data, allows for refinement of the stratigraphy into 5 major units (Fig. 4-2). Most of

the major units have good lateral and vertical continuity but individual layers within these

major units can show significant petrologic variations in modal mineralogy and/or

thickness.

Igneous layering is inconspicuous in all of the major units, but where observed, is

typically developed on a centimetre- to decimetre-scale (Photo 4-3). Metre- or

decametre-scale layering may in fact constitute the main style but is less discernable than

the former types due to poor surface exposure; larger-scale layering is more apparent in

drill core intersections. Layering is primarily defined by modal variations in plagioclase

and pyroxene abundance, occasionally by conspicuous concentration of sulphide minerals

(Photo 4-3), and less commonly by an increase in oxide minerals such as magnetite

and/or ilmenite. Textural layering, defined by distinct grain-size variations, has been

recorded in the Nipissing Gabbro suite in a number of localities (e.g. Conrod, 1988; Card

et al., 1975); in the current study area, textural layering has been documented in several

areas (Photo 4-4) but for the most part it is rarely observed. Layering usually strikes

parallel to the upper and lower contacts of the sills and dips range from near vertical to

near horizontal, dependent on the overall orientation and geometry of the intrusive body,

and is often mimicked by strong joint patterns (Photo 4-1).

Most of the Nipissing Gabbro intrusions in the study area show very little

differentiation, consisting almost exclusively of medium-grained gabbro and/or

orthopyroxene gabbro with subordinate quartz gabbro, gabbro-leucogabbro and vari-

textured gabbro. Changes in the stratigraphy are interpreted to mainly represent

decametre-scale layering.

62

Photo 4-3. (A) and (B) Modal and textural layering in Nipissing Gabbro at the Big Swan

property, Porter Township. Note the layer of sulphide-rich, medium- to coarse-grained

gabbro (vari-textured gabbro) in contact with a layer of relatively sulphide-poor, fine- to

medium-grained gabbro. The blue areas are paint for marking the sampling grid. The

hammer handle is about 33 cm long.

63

Photo 4-4. Conspicuous textural layering in outcrop at the Rauhala property, Waters

Township. The hammer handle is about 70 cm long.

Less commonly, some of the intrusions are well differentiated, ranging upward in

composition from basal quartz diabase and/or gabbro which may or may not be chilled,

orthopyroxene gabbro, gabbro, gabbro-leucogabbro, vari-textured gabbro, granophyric

gabbro (includes aplite, granodioritic to granitic rocks and pegmatitic gabbro), and an

upper quartz diabase and/or gabbro which may or may not be chilled (Fig. 4-2). Narrow

(<0.5 m wide), fine-grained gabbro (diabase) dikes are observed cutting through the

orthopyroxene gabbro, gabbro and gabbro-leucogabbro units. In most cases, detailed

characterization of the contacts between each of the major units in the igneous

stratigraphy is made difficult by lack of exposure. However, contacts are generally

transitional, implying a gradational change in composition between the major units (Fig.

4-2).

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4.2.1 Lower & Upper Quartz Diabase-Gabbro Units

Where present, the lower (basal) and upper (capping) quartz diabase to quartz gabbro

units are massive, fine-grained to aphanitic (chilled), and contain <1% fine-grained pyrite

and/or pyrrhotite with rare chalcopyrite. The chilled margin that develops at the contact

with the country rock is normally <20 cm wide and may host anastomosing quartz-

carbonate veins, developed as a result of fracture-fill and/or patches rich in medium-

grained quartz, which is likely a result of localized crustal contamination. The chill is

petrologically equivalent to the fine-grained gabbro dikes, which are observed (rarely) in

the upper parts of the stratigraphy.

Gabbro-sediment breccia is relatively rare and is mainly observed in drill core

samples and only rarely in outcrop. The breccia, which is akin to the Footwall Breccia

Unit described in the River Valley intrusion (see Section 6), occurs proximal to the basal

contact of the intrusions, extending into the footwall rocks (Photo 4-5); these breccias

have been observed at the upper contacts of the intrusions where they extend into the

hangingwall. Sulphide-bearing basal breccia consists of about 60% angular to sub-

angular sediment fragments and about 10% sub-angular to sub-rounded gabbro fragments

within a white to grey, siliceous (minor carbonate), fine-grained (cherty?) cement (Photo

4-6). These basal breccias are locally mineralized with 1-5% disseminated chalcopyrite,

pyrrhotite and pyrite and rarely, semi-massive to massive veins of chalcopyrite,

pyrrhotite and pyrite. These semi-massive to massive sulphide veins are secondary

sulphides, cutting through the lower quartz diabase unit, the overlying transition zone and

extending into or out of the basal portion of the orthopyroxene gabbro unit (e.g. Rathbun

Lake occurrence, Rathbun Township and Rauhala property, Janes Township; Figs. 1.2

and 5-1).

The lower quartz diabase grades upward from chilled to fine-grained nearest the base

to a transition zone of fine-grained and locally medium-grained gabbro that merges into

the overlying orthopyroxene gabbro unit. Lightfoot and Naldrett (1996) described an

upward increase in quartz content toward the overlying orthopyroxene gabbro unit but

this was not observed in this study. The upper quartz diabase, although not as well

defined as the lower quartz diabase and usually absent, is in sharp contact with the

underlying granophyric gabbro.

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Photo 4-5. (A) and (B) Gabbro-sediment breccia occurring along the contact of a Nipissing

Gabbro intrusion in Porter Township, near the Big Swan property. The matrix in the breccia

consists of fine-grained pyroxenitic gabbro and shares many textural similarities with Sudbury

Breccia which occurs in the region. The gabbro inclusion at the foreground in photo (B) is

labelled as Nipissing Gabbro but may be a fragment of East Bull Lake suite intrusion gabbro. The

hammer handle is about 33 cm long.

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Photo 4-6. Sulphide-bearing basal breccia in drill core from the Rastall occurrence, Janes

Township. The pen magnet is about 12.5 cm long.

4.2.2 Orthopyroxene Gabbro (Gabbronorite) Unit

The orthopyroxene gabbro unit (Photo 4-7) has been previously referred to as the

hypersthene zone (Conrod, 1988), gabbronorite (Conrod, 1989), and as both hypersthene

gabbro and gabbronorite (Lightfoot and Naldrett, 1996). This unit consists primarily of

massive, medium-grained, orthopyroxene-bearing gabbro (>10% orthopyroxene

phenocrysts), commonly containing trace to ~1% disseminated sulphide but in many

cases containing 1-5% disseminated and blebby chalcopyrite and pyrrhotite (Photos 4-7a

and 4-8). Rare semi-massive to massive pods, ranging from centimetre- to metre-scale,

of chalcopyrite and/or pyrrhotite are observed and interstitial blue quartz may be

associated with sulphide minerals. In some parts of the study area (e.g. the Makada Lake

intrusion), the orthopyroxene gabbro unit contains metre-scale domains of altered, vari-

textured gabbro that appear to occur at the interface with the overlying gabbro unit; this

variability can make identification of the orthopyroxene unit problematic at the sub-metre

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outcrop scale. Orthopyroxene gabbro weathers dark grey to brown, commonly with

distinct brown to honey-brown phenocrysts of orthopyroxene (Photo 4-9a) and/or

pseudomorphs of tremolite-actinolite and talc after orthopyroxene (Photo 4-7b).

Subordinate rock types include discontinuous layers or pods of melagabbro (>55 to 90%

mafic minerals) and/or pyroxenite.

Centimetre- to metre-scale, modal igneous layering can be present in this unit, but it

is poorly defined and is best discriminated by the presence of centimetre- to decimetre-

scale repeating joints that parallel what is likely the igneous layering and its associated

cooling fronts (Photo 4-1). Rare mafic fragments occur in some of the intrusions,

generally proximal to the basal contact (Photo 4-9b). Within the upper part of this unit

and transitional into the gabbro unit, is an oxide-bearing (1-10% total oxide) gabbro to

orthopyroxene-gabbro. This oxide-bearing gabbro layer has not been recognized in many

of the intrusions, but in the few areas where it does occur (e.g. the Kukagami Lake

intrusion), it has been traced in outcrop for more than 3 km along strike. This unit may

represent a marker horizon that developed in some of the intrusions where fractionation

led to Fe-enrichment in the liquid and concentrated precipitation of oxide minerals

(magnetite > titanomagnetite > ilmenite). The orthopyroxene gabbro is gradational into

the overlying gabbro, marked by a distinct decrease over several centimetres in the

orthopyroxene content, and in particular a decline in the percentage of orthopyroxene

phenocrysts.

4.2.3 Gabbro Unit

The gabbro unit consists of massive, medium-grained, gabbro (25 to <55% mafic

minerals), containing localized <1% disseminated chalcopyrite and pyrrhotite and

subordinate blebby pyrrhotite and chalcopyrite; interstitial blue quartz may be associated

with the sulphide. Centimetre-scale modal layering is rarely observed. Subordinate rock

types include melagabbro and leucogabbro (10 to <25% mafic minerals). Within the

upper part of the gabbro unit and transitional into the gabbro-leucogabbro unit, is an

oxide-bearing (1 to 10% total oxide) gabbro to leucogabbro.

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Photo 4-7. Orthopyroxene-gabbro unit typically found within the lower portions of Nipissing Gabbro intrusions. (A) Medium-grained orthopyroxene gabbro with sulphide staining from Trench 1 at the Rastall occurrence, Janes Township. The Canadian one dollar coin is 2.5 cm in diameter. (B) Medium-grained porphyritic orthopyroxene gabbro with pseudomorphs of tremolite-actinolite and talc after orthopyroxene (hypersthene), from outcrop along Hwy #805, near the Grenville Front Boundary Fault in eastern Janes Township. The Canadian one dollar coin is about 2.5 cm in diameter.

69

Photo 4-8. (A) Typical disseminated and blebby sulphide mineralization in medium-

grained orthopyroxene gabbro from the Rastall occurrence (Trench 1), Janes Township.

The Canadian one dollar coin is about 2.5 cm in diameter. (B) Fine- to medium grained

orthopyroxene gabbro with atypical total disseminated sulphide (>10% sulphide) from

the Rastall occurrence (Trench 4), Janes Township. The Canadian one dollar coin is

about 2.5 cm in diameter.

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Photo 4-9. Orthopyroxene Gabbro Unit. (A) Typical unmineralized, medium-grained

orthopyroxene gabbro with dark brown weathering and distinct brown to honey-brown crystals of

orthopyroxene (hypersthene), generally recessed due to weathering. A centimetre ruler is

provided for scale. (B) Mafic fragment in medium-grained orthopyroxene gabbro to gabbro,

located proximal to the contact with Huronian Supergroup sediment, Porter Township. The

Canadian two dollar coin is about 2.8 cm in diameter.

71

This oxide-bearing layer, which commonly occurs about half to two thirds of the way up

through the exposed stratigraphy, has only been recognized in a few of the intrusions.

However, as with the oxide-bearing gabbro layer at the top of the orthopyroxene gabbro

unit, this unit may represent a marker horizon that developed through Fe-enrichment in

the liquid and subsequent precipitation of oxide minerals (magnetite > titanomagnetite >

ilmenite). The gabbro unit is gradational into the overlying gabbro-leucogabbro, marked

by a gradual increase, over tens of centimetres, in the percentage of plagioclase feldspar

(relative to mafic minerals) and from time to time, the presence of an oxide-bearing

gabbro; the latter may be attributed to a change (increase) in the fugacity (activity) of

oxygen (fO2).

4.2.4 Gabbro-Leucogabbro Unit

This unit is characterized by massive to crudely layered, medium-grained gabbro and

medium-grained leucogabbro. Layering is defined by modal changes in the ratio of

plagioclase and amphibole (after pyroxene) and is commonly decimetre- to metre-scale.

The gabbro-leucogabbro unit contains trace sulphide dominated by disseminated to

blebby pyrrhotite and subordinate chalcopyrite and pyrite. Subordinate rock types

include anorthosite (<10% mafic minerals) and very rarely orthopyroxene gabbro. The

gabbro-leucogabbro unit is gradational into the overlying vari-textured gabbro, marked

by a gradual increase in irregular patches of coarser-grained gabbro.

4.2.5 Vari-Textured Gabbro Unit

As the name implies, the vari-textured (variably textured) unit comprises a textural

mixture of massive gabbroic (gabbro to leucogabbro) rocks, ranging from fine-grained to

coarse-grained (Photo 4-10), with localized, metre-scale regions of gabbro pegmatite;

rare, localized, metre-scale patches or pods of melagabbro were also observed. The

highly variable nature of this unit and general lack of surface exposure, makes field

identification of this unit difficult. This unit generally contains localized trace

disseminated pyrrhotite and chalcopyrite. Gabbro pegmatite contains up to 5% coarse-

grained (>1 cm diameter) blebby and ragged chalcopyrite and pyrrhotite. The vari-

textured gabbro and overlying granophyric gabbro unit are separated by a transition zone

which is characterized by an upward increase, over several tens of centimetres, in

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granophyric textures including micropegmatite and miarolitic cavities, pegmatitic

segregations and aplite dikes.

Photo 4-10. Vari-textured Gabbro Unit. (A) Vari-textured gabbro from outcrop in the

Basswood Lake Intrusion, Wells Township. (B) Close-up of coarser-grained gabbro

patches from the same outcrop as (A). A centimetre ruler is provided for scale.

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4.2.6 Granophyric Gabbro Unit

This uppermost major unit consists of a variety of rock types including massive,

medium- to coarse-grained granophyric gabbro, gabbro to leucogabbro pegmatite, quartz

gabbro, aplite dikes and localized gabbro-sediment breccia. Myrmekitic textures and

miarolitic cavities up to several centimetres in diameter are common, consisting of

quartz, alkali feldspar and carbonate. Lightfoot and Naldrett (1996) described similar

features in the granophyric gabbro unit. The frequent occurrence of gabbro pegmatite

(Photo 4-11), aplite and aplite dikes, granophyric pods and/or dykes (Photo 4-12) and

miarolitic cavities (Photo 4-13a) in the upper sections of Nipissing Gabbro suggests a

well fractionated magma enriched in volatiles at the time of crystallization. In addition,

the siliceous nature of these rocks, along with localized but extensive alteration (i.e.

potassic), and alkali-rich rock types suggests contamination through stoping and

assimilation of the hangingwall country rocks. Massive, pyrrhotite-dominated sulphide

pods, up to 4 metres diameter have been observed in outcrop (e.g. Louie Lake, Louise

Township and Rauhala property, Waters Township) and are commonly located within

tens of metres of the contact with country rocks or in regions inferred to be proximal to

the now eroded hangingwall units. The granophyric gabbro unit contains patches,

generally less than a few metres in strike and width, that contain about 1-3%

disseminated and blebby pyrrhotite, chalcopyrite and pyrite, which may be associated

with interstitial and centimetre-scale patches of blue quartz (Photo 4-13b). Pyrite is

relatively common as fine-grained disseminations and smears along fracture planes.

The upper contact of the granophyric gabbro unit is highly variable; characterizing

this contact region is hampered by a lack of exposure and/or a significant amount of

erosion which has removed this level of the stratigraphy. Aplite dikes, which consist of

plagioclase, alkali feldspar and quartz, can be traced from within the granophyric gabbro

unit, into the hangingwall sedimentary rocks, cross-cutting the chilled margin or upper

quartz diabase-gabbro. Partially assimilated rafts of hangingwall sedimentary rock,

ranging from centimetre- to metre-scale, are common nearer the upper contact. Similar

features were noted by Lightfoot and Naldrett (1996) and Conrod (1988, 1989).

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Photo 4-11. (A) Gabbro pegmatite, termed “snowball” gabbro from what is interpreted as

the uppermost stratigraphy of the Makada Lake Nipissing Gabbro body in Waters

Township. The pencil is about 15 cm. Photo (B) is a close up of the “snowballs” which

consist of feldspar and quartz “eyes” in a mafic matrix. The Canadian two dollar coin is

about 2.8 cm in diameter.

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Photo 4-12. Granophyric Gabbro Unit. (A) Granophyric pod (or dike?) from the upper

portion of the Basswood Lake Intrusion, Wells Township. Note the darker, mafic

(amphibole) rich selvages running the length of the granophyric pod and within a narrow

band nearer the hammer. The hammer handle is about 70 cm long. (B) Close up of photo

(A) showing mafic inclusion within medium- to coarse-grained granophyric gabbro.

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Photo 4-13. Granophyric Gabbro Unit. (A) Miarolitic cavity lined with carbonate and

quartz and hosted by pyrite-bearing granophyric gabbro in the Basswood Lake Intrusion,

Wells Township. (B) Patchy sulphide mineralization (mainly pyrite with subordinate

chalcopyrite) associated with blue to grey quartz in the Basswood Lake Intrusion. A

centimetre ruler is provided for scale.

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4.3 Petrography and Mineralogy

Each stratigraphic unit is characterized by a more or less distinct assemblage of

minerals, alteration styles and associated sulphide and/or oxide minerals. Previous work

describing the petrological and mineralogical variations through Nipissing Gabbro

intrusions includes Hriskevich (1968); Card and Pattison (1973); Conrod (1988, 1989);

and, Lightfoot and Naldrett (1996). A synopsis of the mineralogic and petrographic

features of the rocks is provided in Appendix 2.

Plagioclase feldspar, clinopyroxene and orthopyroxene are the main primocryst

phases forming the rocks of Nipissing Gabbro intrusions; amphibole and magnetite are

late interstitial and/or minor cumulus phases. Plagioclase and clinopyroxene (principally

augite) are modally the most abundant and consequently gabbro is the most common rock

type. Phenocrysts of orthopyroxene (hypersthene) are the distinguishing feature in the

orthopyroxene gabbro unit where they comprise up to 10% of the mode. The presence of

these phenocrysts contributes to the higher MgO compositions of these rocks.

Conrod (1988, 1989) noted the presence of olivine in the “hypersthene zone”, which

is equivalent to the orthopyroxene gabbro unit, and in the chilled basal quartz diabase at

the Cross Lake Intrusion, located near Temagami Lake, east of the current study area;

Hriskevich (1968) made similar observations on rocks from the Cobalt area. However,

no olivine-bearing rocks were observed in either hand specimen or thin section during the

course of this study. The presence of olivine in the chilled diabase, as described by

Conrod (1988, 1989), suggests that olivine was a pre-emplacement, crystallizing phase,

entrained in the early magma.

In general, plagioclase feldspar is altered to saussurite (epidote + clinozoisite),

±chlorite and ±sericite; orthopyroxene to uralite (tremolite-actinolite), tremolite-

actinolite, ±chlorite and rarely talc; clinopyroxene to uralite, tremolite-actinolite,

±chlorite and ±blue-green hornblende; and, olivine to talc-serpentine (±antigorite) and

magnetite assemblages (Conrod, 1988, 1989). Greenschist to amphibolite facies

metamorphism played some role in the development of the observed alteration

assemblages, but the lack of ubiquitous alteration in all lithologies – where present, the

majority of unaltered minerals occur within the central parts of the intrusions - suggests

that localized hydrothermal and deuteric alteration, through the introduction of water,

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silica and carbon dioxide, were the dominate processes. In the descriptions that follow,

the mineral mode by volume percent is specified in parentheses.

4.3.1 Lower & Upper Quartz Diabase-Gabbro Units

These units consist almost entirely of long, radiating plagioclase (40%) and pyroxene

(40%) crystals that together with quartz (10%) and granular interstitial pyroxene (10%)

form a diabasic texture (Photo 4-14). Augite and pigeonite are the main pyroxene

minerals and quartz may occur as discrete grains or as aggregates in association with

potassium feldspar in micropegmatite, granophyre and myrmekitic intergrowths.

Magnetite (titanomagnetite) and subordinate ilmenite form the principal opaque minerals

and accessory minerals include apatite, epidote and rarely titanite. Plagioclase

phenocrysts average about 1.0 mm in diameter and constitute as much as 10% of the

mode. Pyroxene phenocrysts are <0.5 mm in diameter, are rarely observed, and occur in

<5% of the mode; Lightfoot and Naldrett (1996) noted 0.5 mm olivine phenocrysts

altered to antigorite clouded with magnetite. Very fine-grained (<0.1 mm) amphibole

(uralite) and chlorite occur as alteration products after pyroxene and sericite, epidote and

clinozoisite occur as alteration products after plagioclase.

4.3.2 Orthopyroxene Gabbro (Gabbronorite) Unit

This unit is dominated by laths of euhedral plagioclase (55%) and equant subhedral

clinopyroxene grains (35%) which are often enclosed by larger subhedral orthopyroxene

(5-10%) grains. Accessory phases include quartz, biotite, ilmenite and apatite.

Infrequently, this unit contains well-preserved cumulus igneous mineral assemblages

consisting of euhedral clinopyroxene and orthopyroxene with interstitial plagioclase

(Photo 4-15). Olivine was noted by Conrod (1988) but is absent or not recognisable due

to extensive alteration, in any of the samples from this study. Orthopyroxene forms the

most common phenocrysts, averaging about 1.0 mm in diameter and occurring as

equidimensional, subhedral to euhedral grains. Individual columnar, euhedral

phenocrysts from the Kukagami Lake intrusion are up to 5 mm in length. Commonly,

fine-grained amphibole, uralite and chlorite occur as alteration products after pyroxene

(Photo 4-16), minor antigorite and talc/serpentine after orthopyroxene, and sericite,

epidote and clinozoisite occur as alteration products after plagioclase.

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Photo 4-14. Lower and Upper Quartz Diabase-Gabbro Units. (A) Chilled marginal quartz

gabbro (Makada Lake Intrusion, Waters Township) with typical gabbroic texture,

consisting of radiating plagioclase (plag), pyroxene (pyx), and quartz, and phenocrysts of

pyroxene (p-pyx). Plane light. (B) Same view as (A) but in crossed polars. Field of view

is 8 mm wide for both photographs.

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Photo 4-15. Orthopyroxene Gabbro (Gabbronorite) Unit - atypical. (A) Euhedral

clinopyroxene (cpx) and orthopyroxene (opx) with interstitial plagioclase (plag).

Accessory phases include quartz, biotite, ilmenite and apatite. Plane light. (B) Same view

as (A) but in crossed polars. Field of view is 8 mm wide for both photographs.

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Photo 4-16. Orthopyroxene Gabbro (Gabbronorite) Unit - typical. (A) Groundmass and phenocrysts of pyroxene (p-pyx) are commonly replaced by fine-grained amphibole, uralite and chlorite, and sericite, epidote and clinozoisite occur as alteration products after plagioclase (plag). The phenocrysts (p-pyx) were most probably originally hypersthene. Plane light. (B) Same view as (A) but in crossed polars. Field of view is 8 mm wide for both photographs.

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4.3.3 Gabbro Unit

This unit consists of a relatively uniform distribution of euhedral plagioclase laths

(55%) and equant subhedral clinopyroxene (45%); accessory phases include quartz,

biotite, ilmenite, apatite and rare titanite. Mineralogy in this unit is relatively fresh in

comparison to other units. Amphibole and chlorite occur as alteration products after

pyroxene and sericite, epidote and clinozoisite occur as alteration products after

plagioclase.

4.3.4 Gabbro-Leucogabbro Unit

This unit is characterized by variable percentages in euhedral plagioclase laths (45-

75%) and equant subhedral clinopyroxene (25-55%); accessory phases include quartz,

biotite, ilmenite, apatite and rare titanite. Mineralogy in this unit is relatively fresh in

comparison to other units. Amphibole and chlorite occur as alteration products after

pyroxene and sericite, epidote and clinozoisite occur as alteration products after

plagioclase.

4.3.5 Vari-Textured Gabbro Unit

The vari-textured unit consists mainly of elongate, subhedral to euhedral plagioclase

(45%) and subhedral to anhedral pyroxene (45%) crystals which together with quartz

(5%) and granular interstitial pyroxene (5%) form a gabbroic texture; augite is the main

pyroxene mineral. Clinopyroxene forms oikocrystic textures with the plagioclase laths.

Micropegmatite and myrmekitic intergrowths are also noted. Accessory phases include

alkali feldspar, apatite, ilmenite, magnetite (titanomagnetite) and biotite. This unit is

consistently altered with fine-grained amphibole, uralite and chlorite occurring as

alteration products after pyroxene and sericite, epidote and clinozoisite occurring as

alteration products after plagioclase.

4.3.6 Granophyric Gabbro Unit

This unit comprises subhedral plagioclase (50%), subhedral to anhedral pyroxene

(40%) crystals, quartz (5%) and alkali feldspar (5%); augite is the main pyroxene

mineral. Accessory phases include apatite, ilmenite, magnetite (titanomagnetite), biotite

and titanite. Quartz also occurs as aggregates in association with potassium feldspar in

micropegmatite and myrmekitic intergrowths. This unit possesses the greatest degree of

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alteration with amphibole, uralite and chlorite occurring as alteration products after

pyroxene and plagioclase altering to albite, sericite, epidote and clinozoisite; carbonate

occurs as granular aggregates within the groundmass and is likely related to the miarolitic

cavities.

4.4 Mineral Chemistry

With the exception of semi-quantitative electron microprobe studies on platinum-

group minerals (see Section 4.4.5), no quantitative mineral analyses were conducted

during the course of this study. Numerous other authors, including Hriskevich (1968),

Jambor (1971), Card and Pattison (1973), Finn et al. (1982), Conrod (1988, 1989), have

reported mineral chemistries from Nipissing Gabbro intrusions. These data, along with

modal rock compositions, illustrate that most of the rocks in Nipissing Gabbro intrusions

are mafic in composition. Similar compositions for intrusions from the current study are

expected on the basis of similar modal rock compositions.

4.4.1 Olivine

Olivine appears to be extremely rare in Nipissing Gabbro intrusions and where

present is often too altered to obtain a mineral composition. Conrod (1988) reported

chemistry from equant cumulus olivine grains from the Cross Lake intrusion in the

Cobalt area; olivine cores and rims, from the basal quartz diabase, had compositions of

~Fo62 and ~Fo60, respectively. Olivine cores from the orthopyroxene gabbro unit

(hypersthene zone) range upward from ~Fo64 to ~Fo69 and correlate well with nickel

contents in olivine which range from 1430 ppm to 1780 ppm, respectively (Conrod,

1988). Hriskevich (1968), reported olivine compositions (determined optically) from the

Colonial Mine section (Cobalt area) that range from ~Fo70 in the rocks just below the

orthopyroxene gabbro, increasing to a maximum of ~Fo85 in the middle of the

orthopyroxene gabbro, then decreasing to ~Fo70 in the upper part of the orthopyroxene

gabbro unit. Lightfoot et al. (1987) reported slightly enriched Ni compositions for

olivine grains from the Cross Lake intrusion, relative to Ni compositions of olivine with

similar forsterite contents from other mafic intrusions. The relatively high Ni

concentrations of the Cross Lake olivine argues against the significant removal of Ni by a

sulphide phase prior to the crystallization of the olivine in these rocks (Lightfoot et al.,

1987).

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4.4.2 Plagioclase

Plagioclase crystals commonly display Carlsbad and albite twinning with

subordinate pericline and Baveno twinning and normal and oscillatory zoning. Most

authors report an increase in the anorthite content of plagioclase away from the basal

quartz diabase unit, upward into the orthopyroxene gabbro unit, followed by a subtle

decrease through the orthopyroxene gabbro, and a further decrease through the vari-

textured gabbro and granophyric gabbro units (e.g. Lightfoot et al., 1986; Conrod, 1989).

Anorthite contents from plagioclase cores from the Colonial Mine shaft section (Cobalt

area) range from ~An65 in the basal quartz diabase, ~An80 in the orthopyroxene gabbro,

~An70-78 in the vari-textured gabbro and ~An67 in the hangingwall quartz diabase

(Hriskevich, 1968). Anorthite contents from the Portage Bay intrusion (Lake Temagami

area) range from ~An65 in the basal quartz diabase to ~An75 in the orthopyroxene gabbro

(Conrod, 1989).

4.4.3 Pyroxene

Nipissing Gabbro intrusions contain some proportion of orthopyroxene and augite,

with subordinate pigeonite and inverted pigeonite (e.g. Hriskevich, 1968; Dressler, 1979);

Finn et al. (1982) reported normal compositional zoning from Mg-rich cores to Fe-rich

rims in orthopyroxene from the Wanapitei intrusion (Rathbun Lake intrusion). In

general, orthopyroxenes show an increase in Mg-content (enstatite) moving upward and

away from the lower quartz diabase unit and into the lower part of the orthopyroxene

gabbro, followed by a subtle decline in Mg-number (Mg/Mg+Fe) moving up-section

through the orthopyroxene gabbro and finally a decline into and through the vari-textured

gabbro unit (e.g. Hriskevich, 1968; Finn et al., 1982; Naldrett and Lightfoot, 1996). At

the Miller Lake intrusion (Lake Temagami area), orthopyroxene is predominantly

bronzite (cores) and hypersthene (rims) with Mg-numbers from cores ranging 88-61, but

predominantly between 88 and 74; the Mg-number of cores average ~80 (Conrod, 1989).

Clinopyroxene, principally augite, is almost always colourless, is commonly twinned

and in many cases shows herringbone-like exsolution lamellae of orthopyroxene (e.g.

Dressler, 1979). Hriskevich (1968) reported optical composition data for augite crystals

from intrusions in the Cobalt area of Ca42Mg51Fe7 from basal quartz diabase,

Ca38.5Mg49Fe12.5 from pegmatite gabbro, Ca41Mg48Fe11 from vari-textured gabbro, and

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Ca38Mg51Fe11 from olivine-bearing hypersthene gabbro. Jambor (1971) reported

microprobe analyses for zoned clinopyroxene grains from intrusions in the Cobalt-

Gowganda area of 16.4 wt% CaO, 18.9 wt% MgO and 9.9 wt% FeO. Jambor (1971) also

reported compositions for clinopyroxene phenocrysts of 12.9-21.3 wt% CaO, 15.8-19.1

wt% MgO and 7.0-11.9 wt% FeO from basal contact chilled gabbro and 18.7-20.2 wt%

CaO, 15.5-16.8 wt% MgO and 6.6-6.7 wt% FeO from upper contact chilled gabbro.

4.4.4 Sulphides

Disseminated and blebby magmatic sulphides are the two most common primary

textures (Photo 4-17), with subordinate interstitial and net-textured sulphides.

Accumulations of significant sulphide are not as common but span the range from semi-

massive (25 to 70% total sulphide) to massive (>70% total sulphide), as observed at the

Rastall occurrence in Janes Township (Chiniguchi River intrusion). Commonly, primary

magmatic textures are absent, with sulphides replacing primary silicate minerals

(metasomatic) along margins and cleavage planes and occurring as irregularly shaped

granular dispersions enclosed by silicate grains, and as secondary veining (fracture

filling). Sulphide minerals, although highly dependent on the specific mineralizing

environment (i.e. hydrothermal versus magmatic), in order of decreasing abundance

include pyrrhotite, chalcopyrite, pentlandite and pyrite; millerite was reported by Rowell

and Edgar (1986) from the Rathbun Lake occurrence.

4.4.5 Platinum-Group Minerals

Very little work has been published on the composition of platinum-group minerals

(PGM) in Nipissing Gabbro suite intrusions. In this study, semi-quantitative electron

microprobe analyses, carried out at The University of Western Ontario, London,

identified discrete PGM in sulphide-bearing rocks from the Chiniguchi River intrusion

(Janes Township) with compositions that comprise Pd-Bi-Te, Pd-Bi-Sb-(As?)-Te and Pt-

As (likely sperrylite). The PGM, which are associated with both the silicates and

sulphides (chalcopyrite, pyrrhotite and pentlandite), measure from 10 to 25 µm and are

depicted in back-scattered electron (BSE) images in Photo 4-18.

Rowell and Edgar (1986), using semi-quantitative electron microprobe analyses,

determined compositions of 45 PGM grains from the Rathbun Lake occurrence,

Wanapitei Lake intrusion (Fig. 1-2).

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Photo 4-17. Photomicrographs showing magmatic disseminated (ds) and blebby (bs) sulphide mineralization, the two most common forms of sulphide in mineralized orthopyroxene gabbro. (A) and (B) Blebs (primary) of chalcopyrite (cp) and pyrrhotite (po) with disseminated (remobilized) chalcopyrite throughout the groundmass of amphibole (amp) and chlorite (chl) after pyroxene (pyx). Larger amphibole crystals are pseudomorphs after pyroxene phenocrysts. Both photos were taken using a combination of plane and reflected light. Field of view is 8 mm wide for both photographs.

87

Photo 4-18. BSE images of discrete platinum-group minerals in sulphide-bearing rocks from the Chiniguchi River Intrusion, Janes Township; semi-quantitative analysis showed compositions that included Pd-Bi-Te, Pd-Bi-Sb-(As?)-Te, and Pt-As. The dark area comprises gangue silicate minerals. (A) Grains of Pd-Bi-Te occurring on rims of pentlandite (pn) in sample JB97-109. (B) A single grain of Pd-Bi-Sb-Te associated with pyrrhotite (po) and chalcopyrite (cp) in sample JB97-87C.

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Identified PGM included merenskyite (Pd-Bi-Sb-Te), kotulskite (Pd-Bi-Sb-Pt-Te),

temagamite (Pd-Sb-Bi-Te), michenerite (Pd-Bi-Pt-Sb-Te) and sperrylite (Pt-As).

Optically, Rowell and Edgar (1986) identified 70% of the 45 PGM grains as merenskyite,

20% as kotulskite and 5% as michenerite and 5% as temagamite. The majority of grain

size diameters ranged from 1 to 20 µm for merenskyite, <1 to 40 µm for kotulskite, 65-80

µm for michenerite and <20 µm diameter for temagamite; a single sperrylite grain, the

only grain of sperrylite that was identified, had a diameter of 250 µm. Rowell and Edgar

(1986) reported that 64% of the Pd minerals occurred in the gangue, often as clusters of

up to 40 grains, with the remaining 35% of Pd minerals associated with sulphides - 18%

at chalcopyrite-silicate interfaces, 7% as inclusions in chalcopyrite and 11% as inclusions

in pyrite. On the basis of the PGM mineralization, dominated by Pd bismuthotellurides,

and whole-rock PGE geochemistry, Rowell and Edgar (1986) proposed a hydrothermal

origin for the mineralization at the Rathbun Lake occurrence.

4.5 General Geochemistry

Geochemical characteristics of Nipissing Gabbro intrusions have been described by

several authors including Jambor (1971), Card and Pattison (1973), Conrod (1989),

Rowell and Edgar (1986) and Lightfoot and Naldrett (1996). Rocks from the intrusions

are dominantly tholeiitic and sub-alkaline, with evolved rock types and differentiated

intrusions trending toward calc-alkaline affinities (Lightfoot and Naldrett, 1996).

Lightfoot and Naldrett (1989), Lightfoot et al. (1993), and Lightfoot and Naldrett (1996),

in their review of 100 samples (chilled quartz gabbro and least differentiated gabbro)

collected from 15 different Nipissing Gabbro intrusions, proposed that the parental

magma to the Nipissing Gabbro suite was relatively uniform in composition and

characterised by elevated SiO2 (50.0-51.5 wt%), moderate MgO (8-9 wt%), strong light

rare-earth element (LREE) and large ion lithophile element (LILE) enrichment (La/Sm =

2.5-3.5; Th/Nb = 0.7-0.9), epsilon NdCHUR of -2.7 to -5.9 and low 143Nd/144Nd (indicating

enriched mantle or crustal source), and conspicuous negative Nb, Ta, P and Ti anomalies

(relative to LILE and LREE), suggesting crustal interaction and/or contamination. On the

basis of these geochemical characteristics and the outcrop patterns of Nipissing Gabbro,

Lightfoot et al. (1986, 1987) and Lightfoot and Naldrett (1996) surmised that Nipissing

Gabbro represent the intrusive portion of an eroded continental flood basalt, where

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magmas cut through Archaean basement rocks and Huronian Supergroup sedimentary

rocks as dikes, and spread laterally through the Huronian lithologies as sills.

4.5.1 Emplacement Model for Nipissing Gabbro

Lightfoot et al. (1987) and others (e.g. Conrod (1988, 1989); Lightfoot et al., 1993)

have suggested that the calc-alkalic characteristics are the result of pre-emplacement

enrichment of LILE (Cs, Rb, Ba, and Sr) due to interaction with a recycled, Archaean

crustal component , or continental crustal contamination as the magmas evolved in deep

crustal reservoirs (i.e. staging chambers). Lightfoot et al. (1993) surmised that the

parental magmas differentiated at depth, precipitating olivine which is conspicuously

absent from almost all intrusions, and were then subsequently emplaced as uniform low-

Mg magmas, acquiring their LREE enrichment signature from continental crust, perhaps

during migration from the mantle to the surface (e.g. Lightfoot et al., 1993). This

scenario is consistent with the tectonic setting presented in Figure 3-3. In considering the

homogenous nature of the parental magma and the large volume of assimilated crustal

material (>20%) that would be required to produce the observed REE and trace element

signatures, Lightfoot et al. (1993) suggested that the source characteristics of the magmas

may have been acquired as a result of subduction events relating to the earlier Archaean

Kenoran Orogeny. Tomlinson (1996) and Tomlinson et al. (1999) arrived at similar

conclusions for magmas to Early Huronian volcanic rocks of the Elliot Group, suggesting

that the principal magma source inherited its geochemical signature from

metasomatically-enriched upper mantle, which was geochemically modified as a result of

subduction-accretionary events associated with the Kenoran Orogeny.

Work by several authors, including Lightfoot et al. (1987), Conrod (1989) and

Lightfoot and Naldrett (1989), suggests that petrological variations within the intrusions

are largely controlled by the coupling of post-emplacement fractionation and assimilation

processes or assimilation-fractional crystallization (AFC). Lightfoot and Naldrett (1989),

in applying the AFC model to the Kerns sill (Lake Temagami area), determined that

assimilation and fractionation worked in concert to produce a signature whereby the least

fractionated samples are the least contaminated and the most fractionated samples,

(characterized by low Mg-number, Ni and Cr and by high incompatible element

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concentrations), show the largest amount of contamination (characterized by higher

Th/Zr, La/Zr and U/Zr and lower 143Nd/144Nd).

Figure 4-3. Model for the evolution of a Nipissing Gabbro sill through the process of assimilation-fractional crystallization (AFC). Stage 1: Intrusion of laminar to moderately turbulent parental magma into Huronian Supergroup sedimentary rocks and crystallization of chilled margin gabbro along the upper and lower contacts of the sill; Stage 2: Erosion of roof rocks by hot magma, mainly within the arches of the undulatory sills, and crystallization/accumulation of lowermost orthopyroxene gabbro unit, accompanied by precipitation of disseminated sulphide. A double-diffusive interface (DDI) develops between the underlying mafic magma and overlying hybrid aplitic magma; Stage 3: Crystallization of gabbro-leucogabbro and vari-textured gabbro units overlying the orthopyroxene unit, decline in the rate of assimilation of roof rocks and progressive breakdown of the double-diffusive interface as the aplitic magma solidifies (aplite pods and dykes); Stage 4: Complete crystallization of the upper portions of the vari-textured gabbro and breakdown of the double-diffusive interface resulting in the mixing of the remaining aplitic and mafic magmas and crystallization of granophyric rocks. This model is based on observations and geochemical data from the Kerns sill, Lake Temagami area (after Lightfoot and Naldrett, 1989).

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Figure 4-4a. Model for the development of undulatory Nipissing Gabbro intrusions (after Lightfoot and Naldrett, 1996 and Conrod, 1989). Stage 1: Development of auxiliary magma chamber within deeper Archaean crust; crystallization and gravitative settling of olivine ± pyroxene into olivine dominated cumulates; S-saturation of initially S-undersaturated magma through crustal contamination; crystallization and accumulation of Ni-Cu dominated sulphides. Stage 2: Initial displaced magma pulse, comprising moderate to high MgO magmas with abundant orthopyroxene phenocrysts, results in development of undulatory Nipissing Gabbro sill within Huronian Supergroup sequences; possibility for subsequent S-undersaturated magma pulses and resorption of earlier crystallized olivine ± pyroxene and sulphides.

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Figure 4-4b. Model for the development of undulatory Nipissing Gabbro intrusions (after Lightfoot and Naldrett, 1996 and Conrod, 1989). Stage 3: Crystallization of magmas in inflating Nipissing Gabbro sill, accompanied by differentiation, assimilation, and accumulation of orthopyroxene ±sulphide in lower orthopyroxene gabbro units; and, Stage 4: Relaxation and differentiation within Nipissing Gabbro sill; fractionated and contaminated rocks become concentrated within arches and the most primitive rocks (±sulphides) are concentrated in limbs and basins, resulting in the current type-stratigraphy (Fig. 4-2).

93

Their model, also used by Conrod (1989), suggested that early crystallization is

accompanied by little or no contamination (chilled diabase; basal quartz diabase;

hypersthene diabase), followed by moderate contamination (vari-textured diabase), and

finally by substantial contamination (granophyric diabase) in the upper portions of the

sills, accompanied by the assimilation of hangingwall sedimentary rocks and the

formation of aplitic rocks. Schematic representations of the AFC processes as they relate

to Nipissing Gabbro intrusions are shown in Figures 4-3 and 4-4.

4.6 Mineralization

It has long been recognised that the region between Sault Ste. Marie and Cobalt

contains hundreds of Cu-Ni sulphide (and other metals) occurrences that are associated

with intrusive rocks of the Nipissing Gabbro and the East Bull Lake suite, and to a lesser

extent Huronian Supergroup sedimentary rocks (Card and Pattison, 1973). On the basis

of current field observations and earlier work by Card and Pattison (1973), it is noted that

mineralization in Nipissing Gabbro intrusions varies in type and style across the Southern

Province (Fig. 4-5). Quartz-carbonate vein associated Co-Ag-(PGE-Ni) sulphides and

sulpharsenides dominating in the northeast (Cobalt area); predominantly contact related

Cu-Ni-Co-(PGE) are most conspicuous in the region immediately southwest of Cobalt

(Lake Temagami area); intrusion-hosted Ni-Cu-PGE-(Au) sulphides occur in the regions

immediately northeast, south and west-southwest of the City of Greater Sudbury; contact-

related and intrusion-hosted Ni-Cu-Co-PGE sulphides are common in the areas southwest

of Sudbury (most common but not restricted to the area south of the Murray Fault Zone)

and in the Elliot Lake area; and, secondary (late) quartz-carbonate vein associated Cu

sulphides are most common in Nipissing Gabbro intrusions between Blind River and

Sault Ste. Marie. Lightfoot et al. (1987) noted that this variation in type and style of

mineralization appeared unrelated to differences in lithology, degree of metamorphism,

or level of intrusion of the Nipissing Gabbro. Sulphide occurrences from Nipissing

Gabbro in the current study area have been described as magmatic by Lightfoot et al.

(1986, 1987) and Lightfoot et al. (1993), and as hydrothermal by Finn et al. (1982) and

Rowell and Edgar (1986).

PGE-associated sulphide mineralization is dominated by chalcopyrite and pyrrhotite

with subordinate pentlandite and pyrite (James et al., 2002b). The mineralization occurs

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as three main types, viz.: (1) disseminated sulphide mineralization with the most

consistent and persistent PGE contents (i.e. 500-6000 ppb PGE) and moderate base metal

concentrations (i.e. ~0.75-1.0% Cu+Ni); (2) contact-associated, disseminated to semi-

massive sulphide mineralization with very high PGE (i.e. 8,000-123,000 ppb PGE) and

base metal contents (i.e. 1.5-3.0% Cu+Ni); and, (3) massive sulphide mineralization with

typically low PGE (i.e. <250 ppb PGE) and high base metal content (>3% Cu+Ni). Pd:Pt

ratios in mineralized samples are about 5:1, and in non- or poorly mineralized samples

are about 2.5:1; very high PGE concentrations (i.e. >7000 ppb) tend to have high Pd:Pt

ratios (i.e. >10:1); Cu:Ni ratios are commonly 2:1 but may be as high as 40:1 in

remobilized sulphide. Background concentrations of PGE, Au, Cu and Ni are estimated

to have maximum values ~40 ppb Pd, 32 ppb Pt, 9 ppb Au, 94 ppm Cu, and 376 ppm Ni;

these arithmetic averages are based on the analysis of 23 non-mineralized (low-S and

<100 ppm Cu) samples (James et al., 2002b).

Much of the known and potentially economic PGE sulphide mineralization occurs

within the lower to middle parts of the orthopyroxene gabbro unit (e.g. Lightfoot and

Naldrett, 1996; James et al., 2002b), and is generally located within the lower one-third

of the stratigraphy (Figs. 4-1 and 4-2). This style, indicated by type-1 (above), is best

described as stratabound and more precisely as stratiform, and for the most part consists

of 1-5% fine- to medium-grained disseminated and blebby (up to 7 cm diameter)

chalcopyrite, pyrrhotite and pentlandite, with subordinate net-textured sulphide. Blebby

sulphide commonly show segregation textures (Photo 4-19) of pyrrhotite and

chalcopyrite either as blebs with pyrrhotite cores rimmed by chalcopyrite or as blebs with

half pyrrhotite and half chalcopyrite; Lightfoot and Naldrett (1996) reported similar

sulphide segregation textures, referring to the blebby sulphide as globules. This style

(type-1) of mineralization appears to hold the most promise for large-tonnage, moderate-

grade open cast mining. Semi-massive (25-80% total sulphide) and massive (>80% total

sulphide) sulphide is rare, but where observed occurs at or near the basal contact of the

intrusion, toward the base of the orthopyroxene gabbro unit, or within the basal gabbro-

sediment breccia (James et al., 2002b).

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96

Photo 4-19. Orthopyroxene gabbro with disseminated and blebby sulphide from the Bassoon Lake Intrusion, Dieppe Township. (A) Coarse sulphide bleb showing segregation of chalcopyrite (cp) and pyrrhotite (po). A centimetre ruler is provided for scale. (B) Disseminated and blebby sulphide showing segregation textures (chalcopyrite and pyrrhotite) in the coarser blebs. An irregular patch of blue-grey cherty quartz (qtz) is also identified. The Canadian one dollar coin is about 2.5 cm in diameter.

97

Lightfoot et al. (1987), in assuming the chilled margin samples represent parental

magma compositions, suggested that the uniform composition of the parental magma

indicated limited contamination of the magma en route through the crust or through the

assimilation of local country rocks. This implies that magmatic sulphide segregation was

not triggered by crustal contamination from local country rocks but rather from large-

scale, homogeneous contamination. It is therefore likely that the dominant control on

PGE-bearing sulphide mineralization is that of in-situ normal fractional crystallization

within individual bodies, with PGE-rich sulphide precipitation accompanied by

orthopyroxene ± olivine crystallization in the lower orthopyroxene gabbro unit.

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CHAPTER 5: CONSIDERED NIPISSING GABBRO INTRUSIONS

5.1 Introduction and Overview

Over the past six years, exploration for sulphide-associated PGE in Nipissing Gabbro

intrusions has dramatically increased the geochemical database and current understanding

of sulphide mineralization occurring in these intrusions. Of particular note are the

intrusions located within about 100 km of the City of Greater Sudbury (Fig. 1-2),

specifically those located northeast of Sudbury. These include the Kukagami Lake

(Kelly Township), Chiniguchi River (Janes Township), Sargesson Lake (Janes

Township), and Rathbun Lake (Rathbun Township) intrusions, and those located west

and southwest of Sudbury, including the Charlton Lake-Casson Lake (Curtin Township),

Nairn (Nairn Township), Bell Lake (Lorne), Bassoon Lake (Dieppe Township), Louie

Lake (Louise Township), and Makada Lake (Waters Township) intrusions. Other

intrusions which have been the subject of recent exploration activities include the

O’Brien-Big Swan (Dunlop-Porter townships; Card and Palonen, 1976) and the

Shakespeare (Shakespeare Township; Card and Palonen, 1976) intrusions (Fig. 1-2).

Recent diamond drilling programs have been completed by Pacific North West

Capital Corp. and their exploration partner Anglo American Platinum Corporation

Limited on several sulphide occurrences hosted by Nipissing Gabbro intrusions,

including the Jackie Rastall occurrence (3.1 g/t PGE, 1.1% Cu and 0.3% Ni over 15.0

metres), located in the Chiniguchi River intrusion, the Washagami occurrence (3.9 g/t

PGE, 0.44% Cu and 0.30% Ni over 4.4 metres), located in the eastern part of the

Kukagami Lake intrusion, and the Sargesson Lake occurrence (1.34 g/t PGE, 0.19% Cu

and 0.13% Ni over 1.2 metres), located in the Sargesson Lake intrusion, about 3.5 km

east of the Chiniguchi River intrusion (Fig. 5-1). To date, only one deposit of potentially

economic PGE-Cu-Ni sulphide mineralization has been delineated in the Nipissing

Gabbro suite. This is the Shakespeare Deposit (Fig. 1-2), which has an Indicated

Resource, from two deposits, of ~12.0 million tonnes grading 0.35% Ni, 0.36% Cu,

0.02% Co, 0.19 g/t Au, 0.34 g/t Pt, and 0.38 g/t Pd (Ursa Major Minerals Incorporated,

Press Release 15/04/04).

In this chapter, detailed data from individual Nipissing Gabbro intrusions is

presented using various geochemical diagrams and chemostratigraphic plots. In these

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diagrams and plots, the rock sample name, which is mainly based on field classification,

is used as the principal label, with the CIPW normative rock name provided in

parentheses. For example, a label of “quartz gabbro (G)” refers to a field name of “quartz

gabbro” and a CIPW normative classification of gabbro is referenced using “G”.


The locations for Nipissing Gabbro intrusions from which 188 rock samples and 69

drill core samples were collected are shown in Figure 1-2; a summary of the sample

locations is provided in Table 5-1. The 188 samples were collected from what are

considered to be, based on the most current geological mapping (i.e. Ontario Geological

Survey, 1977, 1979), seventeen different Nipissing Gabbro intrusions and their average

geochemical characteristics are summarized in Table 5-2. The data set of 188 samples

includes samples collected from the seven lithogeochemical traverses and the detailed

geochemical sampling sites. Details of the geochemical characteristics of individual

intrusions and the drill core samples are considered separate from the suite of 188

Nipissing Gabbro samples. A detailed listing of Nipissing Gabbro sample data and

descriptions are provided in Appendix 1, petrographic descriptions of the 104 thin

sections are provided in Appendix 2, and diamond drill hole data and logs are provided in

Appendix 3.

CIPW normative calculations were completed on 152 samples (all with <1 wt% S)

and a select number of these are provided in Table 5-3 with a complete listing provided in

Appendix 1; rock types were determined on the basis of the weight percent normative

minerals. Excluding the two samples of aplite, the majority of samples (111) are silica-

oversaturated, quartz-hypersthene-normative and mainly classify as gabbro with

subordinate leucogabbro. Excluding the seven samples of chilled margin, 28 of the

samples are silica-saturated, hypersthene-olivine-normative and mainly classify as

gabbronorite with subordinate leucogabbronorite, melagabbronorite, olivine

leucogabbronorite, leucogabbro and olivine gabbronorite. The seven samples of chilled

margin are silica-oversaturated, quartz-hypersthene-normative and classify as gabbro.

Two samples (JB97-78A and JB97-93) are silica-saturated, hypersthene-olivine-

corundum-normative and classify as olivine gabbronorite and olivine leucogabbronorite.

100 100

101

Area *Property Centre Township Intrusion Code UTM-mE UTM-mN 1W 314386 5139916 Bridgland/Kirkwood/Wells Basswood Lake 2W 319567 5144030 Wells Appleby Lake 3E 554964 5186759 Clement Manitou Lake

4SW 454324 5110831 Curtin Casson Lake (AN3) 5SW 445114 5110204 Curtin Charlton Lake 6NW 450091 5162093 Ermatinger Fox Lake - Outlier 7SW 448725 5122694 Foster Brazil Lake 8E 547360 5171329 Janes Chiniguchi River 9E 551544 5170842 Janes Sargesson lake

10E 536345 5177849 Kelly Kukagami Lake 11E 542511 5173632 Kelly Washagami Lake

12SW 457443 5132222 Lorne Bell Lake 13C 470213 5129272 Louise Louie Lake

14NW 455207 5175760 Moncrieff Geneva Lake - Outlier 15W 439524 5138247 Porter Big Swan 16E 528537 5170552 Scadding Scadding 17C 489666 5136654 Waters Makada Lake

18SW 454323 5129509 Nairn Nairn 19E 526193 5178855 Rathbun Rathbun Lake

Table 5-1. Summary of sample locations in Nipissing Gabbro intrusions in the area Sault

Ste. Marie and Lake Temagami. The approximate centre coordinates of each property are

in NAD83, Zone 17. Area codes are assigned to each of the intrusions/sampling areas for

plotting and reference purposes.

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Area <0.05 wt% S <1 wt% S All Code 59 samples 152 samples 188 samples 1W 6 15 16 2W - 12 12 3E 1 9 9

4SW 4 4 5 5SW 4 10 10 6NW - 1 1 7SW 1 4 5 8E 6 21 34 9E - 1 1 10E 9 23 25 11E 3 7 7

12SW 6 6 6 13C 1 8 15

14NW - 1 1 15W - 1 1 16E 1 3 3 17C 16 26 30

18SW 1 - 6 19E - - 1

Table 5-1 (cont). Summary of sample locations in Nipissing Gabbro intrusions in the area

Sault Ste. Marie and Lake Temagami. The approximate centre coordinates of each

property are in NAD83, Zone 17.

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Area Intrusion S Se S/Se Ni Ir Ru Rh Pt AreaCode wt% ppb - ppm ppb ppb ppb ppb Code1W Basswood Lake AVG: 0.32 821 3859 71 0.24 1.92 1.56 11.28 1W

MED: 0.06 279 2029 60 0.24 0.24 0.43 10.01N: 16 16 16 16 2 7 7 8

2W Appleby Lake AVG: 0.16 458 3564 83 0.59 0.27 5.71 2WMED: 0.09 370 2300 88 0.59 0.21 5.00

N: 12 12 12 12 1 3 53E Manitou Lake AVG: 0.06 255 2226 99 5.00 2.77 2.40 2.11 3E

MED: 0.06 290 2069 110 5.00 2.77 2.40 2.32N: 9 9 9 9 2 1 2 5

4SW Casson Lake AVG: 0.51 1516 3382 428 0.29 0.59 1.61 69.15 4SWMED: 0.04 314 1401 172 0.12 0.27 0.86 21.50

N: 5 5 5 5 5 4 5 55SW Charlton Lake AVG: 0.09 485 1946 169 0.17 0.33 0.53 9.91 5SW

MED: 0.07 303 2413 135 0.17 0.30 0.32 2.47N: 10 10 10 10 2 8 7 10

6NW Fox Lake N=1 0.05 270 1852 78 6NW7SW Brazil Lake AVG: 6.80 11990 5675 1343 0.20 7SW

MED: 0.07 300 2333 89 0.20N: 5 5 5 5 2

8E Chiniguchi River AVG: 1.04 5900 1767 1615 0.73 3.64 105.86 199.94 8EMED: 0.26 1699 1504 434 0.23 3.77 0.75 35.11

N: 34 34 34 34 14 5 17 299E Sargesson lake N=1 0.77 5683 1355 1116 0.26 0.38 1.01 101.00 9E

10E Kukagami Lake AVG: 0.19 760 2526 341 0.26 0.18 2.21 47.54 10EMED: 0.05 229 2314 134 0.13 0.15 0.40 10.59

N: 25 24 24 25 11 7 19 2111E Washagami Lake AVG: 0.05 333 1544 164 0.20 0.89 18.24 11E

MED: 0.05 321 1558 160 0.18 0.88 17.83N: 7 7 7 7 5 5 7

12SW Bell Lake AVG: 0.01 45 1716 301 0.93 1.94 1.83 10.88 12SWMED: 0.01 38 1316 313 1.10 2.16 1.72 11.92

N: 6 6 6 6 6 6 6 613C Louie Lake AVG: 7.14 3485 20490 1044 0.86 1.99 2.45 27.22 13C

MED: 0.13 319 3918 188 0.51 1.60 1.76 10.83N: 15 15 15 15 9 9 10 15

14NW Geneva Lake N=1 0.14 428 3271 44 0.48 0.00 14NW15W Big Swan N=1 0.16 348 4598 45 9.07 15W16E Scadding AVG: 0.05 433 1254 110 0.23 0.50 12.50 16E

MED: 0.05 400 1325 114 0.20 0.50 12.50N: 3 3 3 3 3 1 2

17C Makada Lake AVG: 1.90 335 56720 664 0.56 1.38 1.20 7.35 17CMED: 0.02 85 2485 211 0.46 1.25 0.88 6.30

N: 30 30 30 30 17 19 23 2518SW Nairn AVG: 7.10 9409 7541 5360 7.65 16.38 14.14 62.64 18SW

MED: 8.09 1671 48399 5333 3.02 6.55 3.78 32.25N: 6 6 6 6 5 5 6 6

19E Rathbun Lake N=1 10.50 88425 1187 9367 0.33 7.80 3961.00 19E Table 5-2. Summary of geochemical characteristics, Nipissing Gabbro intrusions.

104

Intrusion Pd Au Cu Pd/Pt Cu/Ni MgO Mg#ppb ppb ppm - - wt%

Basswood Lake 7.60 4.93 436 0.67 6.18 4.73 451.83 4.25 148 0.18 2.46 4.66 4311 16 16 8 16 16 16

Appleby Lake 5.18 16.51 154 0.91 1.87 5.25 462.75 3.61 170 0.55 1.94 5.74 50

6 11 12 3 12 12 12Manitou Lake 3.31 3.27 128 1.57 1.29 6.45 56

2.89 3.15 150 1.24 1.36 6.75 596 7 9 5 9 9

Casson Lake 109.21 39.23 661 1.58 1.55 10.99 7446.50 5.50 108 2.16 0.63 10.92 75

5 5 5 5 5 5Charlton Lake 23.87 6.69 257 2.41 1.52 9.06 69

2.42 2.46 158 0.98 1.17 9.39 6910 10 10 10 10 10 10

Fox Lake 1.93 0.00 170 2.18 5.79 51Brazil Lake 63.65 4.54 132 0.10 7.16 62

63.65 2.20 130 1.46 7.30 632 4 5 5 4

Chiniguchi River 1180.61 145.22 3724 5.90 2.31 8.55 6456.00 21.03 1130 1.59 2.60 8.43 65

32 33 34 29 34 33 33Sargesson lake 116.60 157.30 3217 1.15 2.88 8.99 66Kukagami Lake 169.29 14.07 563 3.56 1.65 8.88 67

11.06 2.88 112 1.04 0.84 8.82 6722 21 25 21 25 25 25

Washagami Lake 58.39 7.05 163 3.20 0.99 8.75 6957.41 4.81 160 3.22 1.00 8.57 68

7 7 7 7 7 7Bell Lake 5.45 1.03 30 0.50 0.10 15.91 79

6.29 0.91 32 0.53 0.10 16.52 796 6 6 6 6 6

Louie Lake 46.93 14.31 448 1.72 0.43 9.45 5513.65 6.37 312 1.26 1.66 10.51 73

15 15 15 15 15 13 13Geneva Lake 0.00 6.67 190 4.32 3.45 31

Big Swan 9.12 26.80 75 1.01 1.67 5.71 53Scadding 7.33 1.93 118 0.59 1.08 7.61 60

5.00 2.10 107 0.40 0.94 8.10 643 3 3 2 3 3

Makada Lake 8.42 22.34 204 1.15 0.31 9.61 646.36 1.82 72 1.01 0.34 9.72 7027 27 30 25 30 30 30

Nairn 50.22 30.61 6353 0.80 1.19 11.35 5837.31 23.75 962 1.16 0.18 11.35 58

6 6 6 6 6 2Rathbun Lake 6230.00 941.00 377129 1.57 40.26 4.23 32

9

5

4

7

6

3

2

Table 5-2 (cont). Summary of geochemical characteristics, Nipissing Gabbro intrusions.

105

Sample JB97-48 JB98-148 RK-2 JB97-19A JB98-121A JB97-87G 44769 44725Township Wells Lorne Waters Kelly Wells Janes Janes Janes

Field Name CM G G qtzG vtG G OPXG GCIPW Name G LGN OGN G LG G GN OLGNNormatives Q-H H-O H-O Q-H Q-H Q-H H-O H-ONorm Class so ss ss so so so ss ss

Norm Mineralsquartz 2.60 2.64 9.27 8.98

plagioclase 44.09 19.87 43.36 43.04 44.87 38.43 48.3 47.84orthoclase 5.91 0.83 5.73 1.71 10.28 3.07 3.84 5.91Nephelinecorundumdiopside 19.77 34.97 21.71 23.20 3.49 15.12 25.56 8.44

hypersthene 22.79 35.28 16.75 26.28 25.48 27.07 11.83 6.96olivine 6.41 9.59 7.03 27.1ilmenite 1.73 0.51 0.55 0.82 3.02 0.87 0.68 0.99

magnetite 2.58 2.12 1.83 1.93 3.04 2.58 1.65 2.17apatite 0.07 0.05 0.07 0.02 0.44 0.16 0.07 0.09zircon 0.03

chromite 0.01pyrite 0.13 0.02 0.02 0.08 0.11 3.99 1.1 0.51calcite 0.36 0.43 0.32

Na2CO3

*Total: 100.03 100.06 100.04 100.04 100.03 100.28 100.06 100.01

Table 5-3. Summary of CIPW normative calculations on 8 rock samples with <1 wt% S.

Rock types are determined on the basis of weight percent normative minerals.

*normalized to 100%; CIPW rock names based on weight % normative minerals

CM=chilled margin; G=gabbro; qtzG=quartz gabbro; OPXG=orthopyroxene gabbro;

OGN=olivine gabbronorite; GN=gabbronorite; OLGN=olivine leucogabbronorite;

LG=leucogabbro; LGN=leucogabbronorite; Normatives: Q=quartz; N=nepheline;

H=hypersthene; O=olivine; C=corundum; Norm Class: su=silica-undersaturated (alkali

basalt); ss=silica-saturated (olivine tholeiites); so=silica-oversaturated (quartz tholeiites).

106

Sample JB97-78A (see Appendix 1), from Waters Township, is described as a sheared

gabbro, containing about 5% disseminated sulphide associated with blue-grey quartz

eyes. Sample JB97-93 (Big Swan, Porter Township; see Appendix 1) is described as a

sheared gabbro, containing disseminated pyrite-arsenopyrite and is proximal to a shear

zone that cuts through the Nipissing Gabbro body. One sample (JB97-54A; see

Appendix 1) is silica-oversaturated, quartz-hypersthene-corundum-normative, classifying

as a leucogabbro. This sample, collected from the Appleby Lake intrusion (Wells

Township), is strongly altered, granophyric gabbro, that occurs proximal to sulphide-

bearing quartz-carbonate veining. One sample (JB97-32; see Appendix 1) is silica-

undersaturated, nepheline-olivine-normative, classifying as an olivine leucogabbronorite.

This sample, collected from Clement Township, is described as a relatively fresh,

massive, medium-grained gabbro.

It is important to note that the lithogeochemical studies reported by Conrod (1988),

Lightfoot and Naldrett (1989), and Lightfoot et al. (1987, 1986, 1991a) have shown wide

compositional ranges within individual units from the intrusions they studied. Wide

compositional variations were also noted from individual intrusions in the current study.

These authors attributed these compositional variances to be reflective of a process

involving strong in-situ differentiation and contamination. Conrod (1988) and Lightfoot

and Naldrett (1996) presented an Assimilation-Fractional Crystallization (AFC) model to

explain many of the wide ranges in composition within individual intrusions (see

previous discussion and Fig. 4-5).

5.2.1 Major Element Variations

Samples with elevated S (>1 wt% S) concentrations are not included in these plots as

high sulphur concentrations skew the major element chemistry in favour of Fe; a further 8

samples have no major element data and so are also removed from the data set. The

majority of Nipissing Gabbro samples plot within the tholeiitic field (Irvine and Baragar,

1971) on the AFM diagram (Fig. 5-2) and classify as sub-alkaline on the basis of the SiO2

versus Na2O+K2O discrimination diagram of Miyashiro (1978). With a few exceptions,

the Nipissing Gabbro sample suite exhibits a strong negative correlation between TiO2

and Mg-number (Fig. 5-3); as TiO2 increases and Mg-number decreases with

107

fractionation. The wide range in values indicate that the Nipissing Gabbro magmas

underwent a considerable amount of in-situ fractionation.

Figure 5-2. AFM diagram showing the major element features of Nipissing Gabbro rocks

from intrusions in the Sudbury region. The majority of lithologies plot along the

tholeiitic trend of Irvine and Baragar (1971); a few samples plot within the calc-alkaline

region. The two samples that plot closest to the Na2O+K2O apex (JB97-65 and JB97-

78B) are aplite dikes.

108

Geochemical characteristics of the samples suite include 45.86-77.93 wt% SiO2 (median

= 51.3 wt% SiO2), 0.14-3.54 wt% TiO2 (median = 0.52 wt% TiO2), 0.13-19.41 wt% MgO

(median = 8.4 wt% MgO), and 22-83 Mg-number (median = 66 Mg-number). Samples

of aplite dike have highest SiO2 (70.6 and 77.9 wt% SiO2) and lowest MgO (0.13-1.11

wt% MgO). Seven samples of chilled margin (quartz gabbro and gabbro/diabase) are

characterized by 49.8-51.9 wt% SiO2 (average = 50.0 wt% SiO2), 0.52-0.89 wt% TiO2

(average = 0.69 wt% TiO2), 6.13-8.43 wt% MgO (average = 7.73 wt% MgO), and 52-66

Mg-number (average = 61 Mg number).

5.2.2 Trace and Rare-Earth Element Variations

Two subsets of the 188 samples of Nipissing Gabbro were generated. The first

(Group-1) is sorted on the basis of location (intrusion/Township) and the second (Group-

2) is sorted on the basis of CIPW normative rock type. Primitive mantle-normalized

multi-element diagrams for Group-1 and Group-2 data are shown in Figures 5-4 and 5-5,

respectively. A summary of the important REE features of these Nipissing Gabbro

samples are provided in Table 5-4. In general, Nipissing Gabbro show strong LILE

enrichment (~10-100 times primitive mantle), moderate LREE enrichment (La/Sm ~1.0-

4.4; average ~2.3), and low to moderate HREE enrichment (~1-10 times primitive

mantle). Most of the Nipissing Gabbro samples display subtle to pronounced negative

Nb+Ta, P* (calculated using P* = P2O5 x 0.43646) and Ti* (calculated using Ti* = TiO2

x 0.59950) anomalies. The average chilled margin pattern is similar and parallel to the

Group-1 and Group-2 data (Figs. 5-5 and 5-6). Patterns for individual chilled margin

samples plot very close together and are consistent between profiles, characterized by

pronounced negative Nb+Ta and P* anomalies and weakly negative Ti* anomalies.

These negative HFSE anomalies (Nb, Ta and Ti*), along with LREE enrichment patterns

and relatively restricted La/Sm ratios are characteristics of enriched mantle magmas

which became contaminated with crustal material during and post-emplacement (Conrod,

1988) and/or within a crustal reservoir (i.e. auxiliary chamber) prior to emplacement

(Lightfoot et al., 1993); continental flood basalts share similar geochemical signatures

(Arndt et al., 1998).

In Figure 5-7, data from 150 Nipissing Gabbro rocks (unmineralized and

mineralized) are plotted using primitive mantle-normalized (Th/Yb)N and (Nb/Th)N,

109

which is useful for modelling the effects of crustal contamination on the composition of a

proposed or known primary melt (e.g. Lesher et al., 2001) and for determining parental

magma sources.

0.1

1.0

10.0

0102030405060708090

Mg-number

TiO

2 (w

t%)

1W2W3E4SW5SW6NW7SW8E9E10E11E12SW13C14NW15W16E17CChilled Margin Avg

fractionation

(152 samples)

Figure 5-3. Variation in Mg-number versus TiO2, showing the relative compositions and

fractionation trends of Nipissing Gabbro samples, sorted by area. Value for average

chilled margin gabbro is from the current study.

110

Intrusion N ∑REE (La/Sm)N (Th/Nb)N Eu/Eu* (La/Yb)CN (La/Sm)CN

Basswood Lake 16 95 2.38 6.59 0.84 4.02 2.35Appleby Lake 12 116 4.16 5.39 0.78 10.11 4.10Manitou Lake 9 59 2.03 2.98 1.06 3.73 2.00

Casson Lake (AN3) 5 24 1.92 4.64 0.98 2.28 1.89Charlton Lake 10 37 2.22 6.73 0.96 3.00 2.19

Fox Lake - Outlier 1 56 1.96 3.88 1.04 3.26 1.93Brazil Lake 5 30 2.29 6.04 1.03 3.00 2.26

Chiniguchi River 34 31 2.06 5.80 0.96 2.69 2.03Sargesson lake 1 32 1.97 5.67 0.89 2.33 1.95Kukagami Lake 25 36 2.14 5.74 0.93 2.73 2.11

Washagami Lake 7 34 1.99 5.76 0.95 2.50 1.96Bell Lake 6 24 1.91 5.17 0.97 2.98 1.89

Louie Lake 15 28 2.49 7.53 0.81 3.45 2.46Geneva Lake - Outlier 1 103 2.10 4.67 0.90 3.85 2.07

Big Swan 1 74 2.03 5.11 0.61 3.23 2.01Scadding 3 41 1.98 4.82 0.99 3.23 1.95

Makada Lake 30 39 2.11 4.81 0.90 3.79 2.09Nairn 6 72 3.75 12.05 0.84 8.16 3.70

Rathbun Lake 1 32 4.72 8.21 1.81 8.11 4.66chilled margin 7 44 2.02 5.08 0.93 2.96 2.46

Table 5-4. Summary of important features for rare-earth elements from Nipissing Gabbro

rocks. Eu/Eu* calculated using the method of Taylor and McLennan (1985). N=primitive

mantle-normalized; CN=chondrite-normalized

111

0.1

1

10

100

1000

Rb Th K* Nb Ta La Ce Sr Nd P* Sm Zr Ti* Tb Y Tm Yb

Sam

ple/

Prim

itive

Man

tle

1W Avg 2W Avg3E Avg 4SW Avg5SW Avg 6NW7SW Avg 8E Avg9E 10E Avg11E Avg 12SW Avg13C Avg 14NW15W 16E Avg17C Avg 18SW Avg19E Avg Chilled Margin

Averages by Area

Figure 5-4. Primitive mantle-normalized multi-element diagrams for Group-1 data, a

subset of 188 samples of Nipissing Gabbro, sorted on the basis of location (Township).

Value for average chilled margin gabbro is from the current study. Normalizing values

are from McDonough and Sun (1995).

112

0.1

1

10

100

1000


Sam

ple/

Prim

itive

Man

tle

Aplite (N=2)Gabbro (N=103)Gabbronorite (N=27)Leucogabbro (N=10)Leucogabbronorite (N=4)Melagabbronorite (N=1)Olivine Gabbronorite (N=2)Olivine Leucogabbronorite (N=3)High Sulphur (>1wt% S) unclassified (N=36)Avg Chilled Margin

Averages by CIPW Rock Type

Figure 5-5. Primitive mantle-normalized multi-element diagrams for Group-2 data, a

subset of 188 samples of Nipissing Gabbro, sorted on the basis of CIPW normative rock

type. Value for average chilled margin gabbro is from the current study. Normalizing

values are from McDonough and Sun (1995).

113

0.1

1

10

100

1000


Sam

ple/

Prim

itive

Man

tle

JB97-48 JB97-49

JB98-224 JB98-207

JB98-239B JB98-239C

JB98-240 Avg Chilled Margin

Chilled Margin Samples

Figure 5-6. Primitive mantle-normalized multi-element diagrams for chilled margin

gabbro samples, Nipissing Gabbro suite. Value for average chilled margin gabbro is

from the current study. Normalizing values are from McDonough and Sun (1995).

114

Distinct negative Nb and Ta anomalies, with respect to primitive mantle-normalized data

and relative to the LILE and LREE, are attributed to crustal contamination (e.g. Cox and

Hawkesworth, 1985); Th is preferentially enriched in continental crust (McDonough and

Sun, 1995). Two of the four mixing curves were constructed by systematic introduction

of a crustal component (i.e. increasing Th) to the initial compositions of N-MORB (Sun

and McDonough, 1989) and average boninite-like rock (Piercey et al., 2001) using

Povungnituk sedimentary rocks (Lesher et al., 2001) to represent continental crust. The

third and fourth mixing curves were constructed by assuming initial primitive boninite

compositions which are predicted to have 25% and 50% less Nb relative to the boninite-

like composition of Piercey et al. (2001).

In Figure 5-7, the vast majority of the rocks plot in reasonably tight cluster that

approximates the mixing line of N-MORB and continental crust, suggesting that the

Nipissing Gabbro magmas originated from a source that was significantly contaminated

by continental crust (~20% contamination). Samples JB97-54A, RK-01, JB97-78A plot

nearer the continental crust end-member, with a composition resulting from assimilation

of local footwall rocks, which have enhanced the crustal signature common to the bulk of

the samples; these samples are extensively altered and contain several percent secondary

sulphide and blue-grey coloured quartz (JB97-78A). It is unlikely that the bulk

contamination signature was derived from local sedimentary rocks as the value for

average Huronian Supergroup sedimentary rocks plots well away from any of the mixing

curves and it would be difficult to model the majority of Nipissing Gabbro samples along

a mixing curve of N-MORB and this average Huronian sediment value.

A number of samples plot below the N-MORB mixing curve and are displaced

toward the mixing curves for Nb-depleted, boninite-like rocks (~25% depleted Nb

relative to N-MORB). These samples have depressed Nb values which indicates that the

magmas from which these rocks formed were derived from a source magma that was

very poor in Nb. Continental flood basalts or boninite-like magmas are good candidates

for this chemistry as both are significantly depleted in Nb relative to N-MORB

(boninites, more so than continental flood basalt), and are both characterized by a

continental crust signatures (Naldrett and Lightfoot, 1993; Crawford et al., 1989).

115

0.01

0.1

1

10

0.1 1 10 100

(Th/Yb)N

(Nb/

Th) N

OPX Gabbro

Gabbro

Chilled Margin

Streich Dike

Povungnituk Sediment

Huronian Sediment Avg

Boninitic Avg

N-MORB

Continental Crust

Boninitic

-25% Nb

E-MORB

-50% Nb

JB97-78A

JB97-54A

RK-01

10% crust

Average Huronian Sediment


(Nb/Th)N using 150 unmineralized and mineralized rock samples of Nipissing Gabbro

intrusions. Continental crust is represented by Povungnituk sedimentary rocks (Lesher et

al., 2001). Data for N-MORB and E-MORB are from Sun and McDonough (1989); data

for Streich Dike, a potential parental magma composition, is from Vogel et al. (1998a);

data for average (N=4) Huronian sedimentary rock is from Easton (2003); data for

average (N=4) Boninitic magma is from Piercey et al. (2001).

116

However, it is important to note that the values for N-MORB and E-MORB are mantle

dependent and that the mantle chemistry in the Proterozoic was probably different than

that of present day.

Some samples plot well above the N-MORB mixing curve and are displaced toward

and above the mixing curve of E-MORB and continental crust (Fig. 5-7). This suggests

the possibility of two different mantle sources; one closer to that of N-MORB with a

significant crustal component (i.e. continental flood basalt), and the second, a hybrid

magma offset toward E-MORB. To test this possibility, the same Nipissing Gabbro suite

(150 samples) was examined in the context of geographic location of the seventeen

different intrusions. Although no correlation could be made between the location of the

intrusions and their respective (Th/Yb)N and (Nb/Th)N values, there was a moderate

correlation between (Th/Yb)N and (Nb/Th)N values and those intrusions that have higher

concentrations of magmatic sulphides, and those with no significant sulphide occurrences

(Fig. 5-7). Samples from intrusions with reasonably PGE-significant sulphide contents

(i.e. Curtin, Foster, Janes, Kelly, and Louise townships) mainly plot below the N-MORB

mixing curve; all of the samples from the Charlton Lake section (Charlton Lake intrusion,

Curtin Township) and the Washagami occurrence (Kukagami Lake intrusion, Kelly

Township) plot below the N-MORB mixing curve. In contrast, samples from intrusions

with no magmatic sulphide occurrences and/or relatively insignificant PGE (Waters,

Scadding, Porter, Moncrieff, Lorne, Ermatinger, Clement, and Wells townships) mainly

plot above the N-MORB mixing curve. In general, Nipissing Gabbro intrusions with

higher concentrations of magmatic sulphides exhibit lower Nb/Ta values, suggesting that

these magmas experienced greater degrees of crustal contamination, perhaps related to

longer residence times in a staging chamber.

Chondrite-normalized REE diagrams for Group-1 and Group-2 data are shown in

Figures 5-8 and 5-9, respectively and summarized in Table 5-4. In general, Nipissing

Gabbro samples show similar and near-parallel patterns with moderate LREE enrichment

(La/Sm ~1.0-4.7; average ~2.3), whereas the HREE show only slight enrichment and are

nearly flat. The degree of fractionation of LREE to HREE, expressed as La/Yb, is

relatively wide, ranging from ~1.4 to 11.2, a reflection of the variety of rock types.

117

1

10

100

1000

La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu

Sam

ple/

Cho

ndrit

e

1W Avg 2W Avg3E Avg 4SW Avg5SW Avg 6NW7SW Avg 8E Avg9E 10E Avg11E Avg 12SW Avg13C Avg 14NW15W 16E Avg17C Avg 18SW Avg19E Avg Chilled Margin

Averages by Area

Figure 5-8. Chondrite-normalized REE diagrams for Group-1 data, a subset of 188

samples of Nipissing Gabbro, sorted on the basis of location (Township). Value for

average chilled margin gabbro is from the current study. Normalizing values are from

Lodders and Fegley (1998).

118

1

10

100

1000


Sam

ple/

Cho

ndrit

e

Aplite (N=2)Gabbro (N=103)Gabbronorite (N=27)Leucogabbro (N=10)Leucogabbronorite (N=4)Melagabbronorite (N=1)Olivine Gabbronorite (N=2)Olivine Leucogabbronorite (N=3)High Sulphur (>1wt% S) unclassified (N=36)Avg Chilled Margin

Averages by CIPW Rock Type

Figure 5-9. Chondrite-normalized REE diagrams for Group-2 data, a subset of 188

samples of Nipissing Gabbro, sorted on the basis of CIPW normative rock type. Value

for average chilled margin gabbro is from the current study. Normalizing values are from

Lodders and Fegley (1998).

119

1

10

100

1000


Sam

ple/

Cho

ndrit

e

JB97-48 JB97-49

JB98-224 JB98-207

JB98-239B JB98-239C

JB98-240 Avg Chilled Margin

Chilled Margin Samples

Figure 5-10. Chondrite-normalized REE diagrams for chilled margin gabbro samples,

Nipissing Gabbro suite. Value for average chilled margin gabbro is from the current

study. Normalizing values are from Lodders and Fegley (1998).

120

Europium anomalies are dominantly weakly negative with positive Eu anomalies for the

average CIPW leucogabbronorite and for average samples from the Clement, Ermatinger,

Foster and Rathbun township suites. Average chilled margin shows a very subtle

negative Eu anomaly (Fig. 5-10) as do the patterns from individual chilled margin

samples, which also have remarkably consistent profiles and narrow ranges in La/Yb

(~2.5-3.6). Conrod (1988) noted positive Eu anomalies in chilled diabase, suggesting

significant plagioclase did not crystallize prior to emplacement. In contrast, data from the

current study and from Lightfoot and Naldrett (1996) show negative Eu anomalies in

chilled diabase, suggesting plagioclase crystallization was at least in part pre-

emplacement.

In both the primitive mantle-normalized and chondrite-normalized plots, average

Huronian Supergroup sediments display a pattern that is similar to that of average aplite,

suggesting a genetic link between the aplite and Huronian Supergroup sediments.

Lightfoot and Naldrett (1989, 1996), in reporting on the prevalence of aplite in the arches

and upper stratigraphy of intrusions and the similarities of their REE patterns with

Huronian Supergroup sediments, suggested that the aplite are a hybrid product resulting

from assimilation of hangingwall rocks.

In Figure 5-11, data from 50 samples of unmineralized and mineralized Nipissing

Gabbro rocks are plotted using the values of Zr/Sm and Nb/Ta. Using the diagram after

Foley et al. (2002), all but one sample (JB98-209C, Louie Lake property) plot with very

low Nb/Ta and Zr/Sm values relative to MORB, continental crust, and modern adakites;

Foley et al. (2002) considered adakites to be rare modern analogues of Archaean crust-

building magmatism, originating by melting of a subducting basalt slab. The samples,

which include chilled margin gabbro, are tightly clustered with low Nb/Ta values similar

to that of adakites and continental crust but are displaced toward anomalously low Zr/Sm

values. These very low Zr/Sm values are probably the result of insufficient digestion

(open beaker digestion – see Section 2.2) of Zr during the ICP-MS analytical process and

so these values are shifted toward the lower left quadrant; ICP-MS Zr data may be one

third to one half less than XRF Zr data (A.J. Crawford, pers. comm., 2004). Assuming

higher Zr compositions would therefore shift these samples toward the fields of

continental crust and adakites.

121

0

5

10

15

20

25

30

1 10 100 1000

Zr/Sm

Nb/

Ta

OPX Gabbro

Gabbro

Chilled Margin

Boninitic Avg

Adakites

MORB

Primitive Mantle(intersection)

Continental Crust

JB98-209C (Louie Lake)

Figure 5-11. Plot of Zr/Sm versus Nb/Ta ratios from whole-rock analyses of 50

unmineralized and mineralized Nipissing Gabbro intrusion samples. The fields of

MORB, continental crust and adakites (modern analogues of early continental crust) are

approximated after Foley et al. (2002). Data for average (N=4) Average boninitic magma

is from Piercey et al. (2001).

122

The Nb/Ta values for the Nipissing Gabbro rocks are low (~6-13 Nb/Ta) relative to N-

MORB (~18 Nb/Ta; Sun and McDonough, 1989), and most plot lower than the field for

continental crust; a similar trend is also exhibited in the samples that plot below the N-

MORB mixing curve in Figure 5-7. These data suggest that the magmas which formed

the Nipissing Gabbro suite underwent significant crustal contamination, recording

signatures indicative of either a subduction zone environment (i.e. back-arc or boninitic

magmas), or more probable, extensive continental flood basalt magmatism.

Fitton et al. (1997) demonstrated that Icelandic basalt and N-MORB define separate

and parallel arrays on a logarithmic plot of Nb/Y vs Zr/Y. These authors found that this

plot could provide a useful discrimination between Icelandic (plume) basalt and N-

MORB whereby Nb, Zr and Y are relatively immobile during alteration of basalt and are

incompatible in the main phases of plagioclase and olivine which crystallize from the

tholeiitic magma at low pressure (Fitton et al., 2000). The value of ∆Nb, the

discrimination value, was defined by Fitton et al. (1997) as the deviation, in log units, of

Nb from the boundary between the Nb/Y vs Zr/Y arrays. Using the method described by

Baksi (2001), concentrations of Nb, Y and Zr from 5 chilled margin samples, presumed

to represent the parent magma, were used to calculate ∆Nb:

[8] ∆Nb = log (Nb/Y) + 1.74 - 1.92 log (Zr/Y)

and to speculate on the probable source of Nipissing Gabbro magmas. Baksi (2001)

proposed that positive ∆Nb values were indicative of deep-mantle sources (e.g. ∆Nb > 0

for Icelandic plumes, Reunion Island hot spot) and that negative ∆Nb values indicated

that the melts were derived from depleted sections of mantle (e.g. ∆Nb < 0 for sub-

continental lithospheric mantle contamination and arc-related magmas); ∆Nb values for

primitive mantle are ~0.18. Baksi (2001) reported conflicting results for ∆Nb in terms of

flood basalts and their inherent connection to mantle plumes (hot spots); although ∆Nb is

positive in some cases, it appears to be masked by sub-continental lithospheric

contamination (i.e. ∆Nb <0) in others. Indications of source from the calculations of

∆Nb for the 5 chilled margin samples are inconclusive as they encompass both weakly

positive (∆Nb = 0.013 and 0.094) and weakly negative (∆Nb = -0.021, -0.003 and -0.008)

values. Applying the calculation to 5 chilled margin samples from Lightfoot and Naldrett

(1996) yielded 4 positive ∆Nb values (∆Nb = 0.07, 0.11, 0.14 and 0.25) and one negative

123

∆Nb value (∆Nb = -0.09). Together, these data from Nipissing Gabbro suggest both

strong mantle signature and weak sub-continental lithospheric mantle contamination,

characteristics that Baksi (2001) proposed are indicative of either continental flood

basalts or a hybrid environment involving a subduction zone (arc lavas) and associated

mantle plume (i.e. the Tonga-Kermadec volcanic arc and Samoan plume).

5.2.3 Chalcophile (PGE, Cu, Ni) Element Variations

The most prevalent type of sulphide mineralization in the Nipissing Gabbro suite is

stratabound PGE sulphide mineralization, which occurs within the lower to middle parts

of the orthopyroxene gabbro unit (e.g. Lightfoot and Naldrett, 1996; Jobin-Bevans et al.,

1998, 1999; James et al., 2002b). This style of sulphide mineralization is dominated by

chalcopyrite and pyrrhotite with subordinate pentlandite and rare pyrite, and generally

consists of 1-5% fine- to medium-grained disseminated and blebby sulphide (see Section

4.6). A summary of the average chalcophile metals plus Au, along with important metal

ratios, for mineralized and unmineralized samples (188 samples) is provided in Table 5-

5; summaries of unmineralized samples (59 samples with <0.05 wt% S) and mineralized

samples (24 samples with >0.05 wt% S) are provided in Tables 5-6 and 5-7, respectively.

Mineralized samples average ~2.7 Pd/Pt (median ~1.6) and ~6.7 Cu/Ni (median ~2.0),

and unmineralized samples average ~2.0 Pd/Pt (median ~1.2) and ~0.7 Cu/Ni (median

~0.7). In general, samples with high PGE concentrations (i.e. >1000 ppb Pt+Pd) have

high Pd/Pt ratios (i.e. >3.0) and high Cu/Ni ratios (i.e. >2.0).

Background concentrations of PGE, Au, Cu and Ni are estimated to have maximum

values of about 3.7 ppb Au (median ~2.9 ppb), 12.4 ppb Pt (median ~10.9 ppb), 20.5 ppb

Pd (median ~14 ppm), 91 ppm Cu (median ~93 ppm), and 149 ppm Ni (median ~140

ppm); these arithmetic averages and median values are based on the 59 unmineralized

(<0.05 wt% S) samples as listed in Table 5-6. James et al. (2002b) reported somewhat

higher estimates of background concentrations with maximum values of ~9 ppb Au, 32

ppb Pt, 40 ppb Pd, 94 ppm Cu, and 376 ppm Ni. PGE concentrations for average chilled

margin (two samples) are ~3.4 ppb Au, ~10.6 ppb Pt, ~11.6 ppb Pd, 120 ppm Ni and 124

ppm Cu with metal ratios of 1.1 Pd/Pt and 1.0 Cu/Ni. The PGE tenor of the chilled

margin samples (~22 ppb Pt+Pd) is high relative to common mafic magmas (e.g. Hamlyn

and Keays, 1986).

124

Selected bivariate plots of chalcophile element concentrations for Nipissing Gabbro

rocks (188 samples) are provided in Figure 5-12. In general, correlations between the

chalcophile elements are good (i.e. Pd-Pt, Cu-Se, Cu-Pd and Cu-Pt), indicating that the

PGE are strongly sulphide controlled; bivariate plots of S-Pd, S-Pt, Ni-Pd and Ni-Pt also

show good correlation.

Intrusion N Pt Pd Ni Cu S/Se Pd/Pt Cu/Ni Cu/Pd Pd/Ir

ppb ppb ppm ppmBasswood Lake 16 6.36 5.81 71 436 3859 0.9 6.2 74939 21.8Appleby Lake 12 3.21 3.53 83 154 3564 1.1 1.9 43631 11.9Manitou Lake 9 1.81 2.83 99 128 2226 1.6 1.3 45163 2.1Charlton Lake 5 69.15 109.21 428 661 3382 1.6 1.5 6055 378.7Charlton Lake 10 9.91 23.87 169 257 1946 2.4 1.5 10750 95.6

Fox Lake (Outlier) 1 1.43 1.93 78 170 1852 1.3 2.2 88083 7.1Brazil Lake 5 1.43 26.59 1343 132 5675 18.6 0.1 4965 98.5

Chiniguchi River 34 171.20 1112.15 1615 3724 1767 6.5 2.3 3349 1969.8Sargesson lake 1 101.00 116.60 1116 3217 1355 1.2 2.9 27590 457.3Kukagami Lake 25 45.45 169.29 341 563 2526 3.7 1.7 3327 643.1

Washagami Lake 7 18.24 58.39 164 163 1544 3.2 1.0 2789 266.8Bell Lake 6 10.88 5.45 301 30 1716 0.5 0.1 5474 5.8

Louie Lake 15 27.22 46.93 1044 448 20490 1.7 0.4 9554 74.8Geneva Lake (Outlier) 1 1.43 1.88 44 190 3271 1.3 4.3 101064 7.0

Big Swan 1 9.07 9.12 45 75 4598 1.0 1.7 8224 33.8Scadding 3 8.81 7.33 110 118 1254 0.8 1.1 16136 31.4

Makada Lake 30 6.53 7.97 664 204 56720 1.2 0.3 25539 18.1Nairn 6 62.64 50.22 5360 6353 7541 0.8 1.2 126502 7.8

Rathbun Lake 1 3961.00 6230.00 9367 377129 1187 1.6 40.3 60534 19110.4Chilled Margin 7 9.44 11.37 117 125 2411 1.2 1.1 11022 53.4

Table 5-5. Summary of average chalcophile metals and ratios from 188 mineralized and

unmineralized Nipissing Gabbro samples.

125

Intrusion N Pt Pd Ni Cu S/Se Pd/Pt Cu/Ni Cu/Pd Pd/Irppb ppb ppm ppm

Basswood Lake 6 11.56 11.41 80 122 1772 1.0 1.5 11 43.9Manitou Lake 1 4.02 4.42 100 150 1444 1.1 1.5 34 0.5Charlton Lake 4 20.44 40.51 173 111 1258 2.0 0.6 3 384.0Charlton Lake 4 6.37 16.41 124 116 1691 2.6 0.9 7 74.6

Brazil Lake 6 1.43 1.69 85 66 2128 1.2 0.8 39 6.3Chiniguchi River 9 17.06 29.04 140 93 1205 1.7 0.7 3 111.0Kukagami Lake 3 9.59 11.14 142 114 1627 1.2 0.8 10 55.8

Washagami Lake 6 25.88 77.60 173 147 1355 3.0 0.8 2 400.0Bell Lake 1 10.88 5.45 301 30 1716 0.5 0.1 5 5.8

Louie Lake 1 33.20 29.80 99 34 2143 0.9 0.3 1 143.3Scadding 16 11.00 14.00 140 86 1400 1.3 0.6 6 35.0

Makada Lake 1 7.03 6.29 240 55 2208 0.9 0.2 9 11.7Nairn 1 2.18 18.07 140 58 568 8.3 0.4 3 66.9

Chilled Margin 2 10.60 11.61 120 124 1834 1.1 1.0 11 43.0AVERAGE: 12.36 20.45 149 91 1578 2.0 0.7 10 103.0

MEDIAN: 10.88 14.00 140 93 1627 1.2 0.7 6 55.8

Table 5-6. Summary of average chalcophile metals and ratios from 59 unmineralized

(<0.05 wt% S) Nipissing Gabbro samples, a subset of the 188 samples, and chilled

margin gabbro samples. The averages from the 59 samples provide an estimate of

background concentrations.

Intrusion N Pt Pd Ni Cu S/Se Pd/Pt Cu/Ni Cu/Pd Pd/Irppb ppb ppm ppm

Charlton Lake 1 264 384 1447 2863 3667 1.5 2.0 7.5 376.5Chiniguchi River 6 457 3419 4559 10342 1648 7.5 2.3 3.0 2421.3Kukagami Lake 2 410 1740 2718 5677 2933 4.2 2.1 3.3 2320.0

Louie Lake 7 44 85 2067 812 21244 1.9 0.4 9.5 68.6Makada Lake 2 15 22 1871 1026 115962 1.5 0.5 47.6 35.8

Nairn 5 75 57 6404 7611 7552 0.8 1.2 134.4 7.4Rathbun Lake 1 3961 6230 9367 377129 1187 1.6 40.3 60.5 19110.4

AVERAGE: 746.5 1705.2 4062 57923 22028 2.7 7.0 38 3477.1MEDIAN: 264.0 384.0 2718 5677 3667 1.6 2.0 10 376.5

Table 5-7. Summary of average chalcophile metals and ratios from 24 mineralized (>0.05

wt% S) Nipissing Gabbro samples, a subset of the 188 samples.

126

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Pd (ppb)

Pt (p

pb)

6NW14NW1W2W15W4SW5SW7SW12SW18SW13C17C3E8E9E10E11E16E19EChilled Margin Avg

(188 samples)(A)

0.01

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1 10 100 1000 10000 100000 1000000

Cu (ppm)

Pd (p

pb)


(188 samples)

(B)

Figure 5-12a. Bivariate plots of whole-rock chalcophile elements Pd-Pt and Cu-Pd (188

Nipissing Gabbro samples). Average chilled margin gabbro is from the current study.

127

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Cu (ppm)

Pt (p

pb)


(188 samples)

(C)

0.1

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1000

10000

1 10 100 1000 10000 100000

Ni (ppm)

Pt (p

pb)


(188 samples)(D)

Figure 5-12b. Bivariate plots of whole-rock chalcophile elements Cu-Pt and Ni-Pt (188

Nipissing Gabbro samples). Average chilled margin gabbro is from the current study.

128

The majority of samples have S/Se ratios that range between 1000 and 5000 (Fig. 5-13a)

which is well within the range of uncontaminated magmatic sulphides (Naldrett, 1981),

approximating that of mantle (~3300 S/Se; McDonough and Sun, 1995). Those samples

that plot higher than 5000 comprise semi-massive to massive (pyrrhotite-dominated)

sulphide mineralization, whereas those samples lower than 1000 can be explained in

terms of S loss, most likely due to secondary processes such as weathering and/or

degassing (Reeves and Keays, 1995), or as a result of relative enrichment in Se, which is

also highly chalcophile (DSe ~700, Keays and Lightfoot, 2004; DSe ~1,770, Peach et al.

1994) and so competes with S in early fractionating sulphides, resulting in lower S/Se

ratios. Sample JB97-39C (18SW; Nairn Township), which has the lowest S/Se value of

568, is a medium-grained quartz gabbro with local patches of <1% disseminated

sulphide. This sample, which has very low visible sulphide, was collected from massive

gabbro immediately adjacent to semi-massive and massive sulphide pod, associated with

blue quartz eyes and hosted by medium- to coarse-grained gabbro (samples JB97-39A

and 39B). It is possible that the S loss noted in JB97-39C was a consequence of the

leaching/migration of sulphur from the host gabbro and accumulation (remobilization)

into a massive sulphide pod. The Rathbun Lake occurrence, considered to be

characteristic of hydrothermal, remobilized Cu-Ni sulphide mineralization (Rowell and

Edgar, 1986), is represented in the current Nipissing Gabbro sample suite by sample

JB98-190E (Pt+Pd = 10191 ppb). In terms of S/Se, this sample plots within the range of

magmatic sulphides (1187 S/Se). However, the Pd/Ir ratio, a measure of hydrothermal

versus magmatic sulphide (Keays et al., 1982), is extremely high at 19,110 Pd/Ir, as is the

Cu/Ni ratio of ~40; the Pd/Pt ratio is also elevated at ~1.6. These signatures of

hydrothermal mineralization (elevated Pd/Ir and Cu/Ni), combined with the magmatic

S/Se value are suggestive of remobilized, hydrothermal sulphide sourced from what was

originally magmatic sulphide.

Concentrations of Pd are plotted against values of (La/Sm)N and (Th/Nb)N in Figures

5-13b and 5-13c, respectively. The Pd versus (La/Sm)N plot, and especially the Pd versus

(Th/Nb)N plot show that most of the rocks have values that are higher than mantle (~5

(Th/Nb)N, ~2 (La/Sm)N) and have fairly constant ratios, indicating a degree of crustal

contamination that is remarkably similar and uniform.

129

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S/Se

Pd (p

pb)

6NW 14NW1W 2W15W 4SW5SW 7SW12SW 18SW13C 17C3E 8E9E 10E11E 16E19E Chilled Margin Avg

(188 samples)

sulphur loss magmatic

contamination

+R-factor

209D

209B117C

39B

33

39A

39C

54A

RK-4

165

83

190E(A)

Figure 5-13a. Bivariate plots of whole-rock S/Se versus Pd for 188 Nipissing Gabbro

rock samples. Average chilled margin gabbro is from the current study.

130

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1000

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(La/Sm)N

Pd (p

pb)


(188 samples) assimilation of crust(contamination)

54A

190E(B)

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100

1000

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(Th/Nb)N

Pd (p

pb)


(188 samples)

assimilation of crust(contamination)

(C)

Figure 5-13bc. Bivariate plots of whole-rock (B) (La/Sm)N-Pd, and (C) (Th/Nb)N-Pd. for

188 Nipissing Gabbro samples. Average chilled margin gabbro is from current study.

131

Given the enormous size of the sampling area and the high variability in rock types

sampled, this suggests that contamination principally occurred either in a large deep-

seated chamber or by the assimilation of country rocks that had very uniform (La/Sm)N

and (Th/Nb)N ratios. As the (Th/Nb)N ratios do not increase significantly with

fractionation, this trend is indicative of bulk contamination. Similar contamination

signatures were reported for crustally contaminated Nadezhdinsky lavas (Siberian Traps)

at Noril’sk (Lightfoot et al., 1994; Lightfoot and Keays, 2004).

Some of the samples from the same intrusions within the main trend (i.e. Makada

Lake (17C), Nairn (18SW), and Louie Lake (13C); Fig. 1-2), have much higher (Th/Nb)N

ratios, suggesting a second phase of contamination, perhaps at a higher crustal level

relative to the deeper chamber, and/or at the site of emplacement which invokes a local

contamination effect. Moreover, these same samples also have counterparts that exhibit

much lower (Th/Nb)N ratios. All of these sample locations show evidence for

assimilation of country rocks (e.g. fragments of local country rock mixed in with

mineralized gabbro) indicating that the signature for local contamination is characterized

by both high and low (Th/Nb)N values, relative to the bulk contamination trend. Perhaps

the most important feature of these plots is that there is no correlation between the

concentrations of Pd and the values of either (La/Sm)N or (Th/Nb)N. This is interpreted

to mean that the main mineralizing event is probably related to the bulk contamination

signature rather than the affects of local country rock contamination.

The bivariate plot of MgO versus Ir, shown in Figure 5-14, can provide a measure of

fractionation whereby the more primitive rocks types will comprise higher MgO and Ir

compositions and increasing fractionation will produce ever lower MgO and Ir

concentrations. Samples that are weakly to strongly mineralized exhibit elevated Ir

concentrations coupled with wide variations in MgO compositions. This indicates that

mineralization can occur in rocks with either high MgO or low MgO and that the

concentration of MgO is not necessarily indicative of the mineralizing potential of the

intrusion.

132

0.01

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10

100

0510152025

MgO (wt%)

Ir (p

pb)


(188 samples)

Figure 5-14. Bivariate scatter diagram of MgO versus Ir for 188 Nipissing gabbro rock

samples. Value for average chilled margin gabbro is from the current study.

Concentrations of Ir that are at or below ~0.1 ppb are at or near the lower limits of

detection.

133

Discrimination plots such as Ni/Cu versus Pd/Ir (Fig. 5-15a) and Cu/Ir versus Ni/Pd

(Fig. 5-15b) are useful to determine the effects of partial melting and if and when,

sulphide segregation occurred (Barnes et al., 1988; Barnes, 1990); increased partial

melting of the mantle lowers Ni/Cu and increases Pd/Ir and increases Cu/Ir and lowers

Ni/Pd. In both discrimination plots, the majority of the mineralized and unmineralized

Nipissing Gabbro samples plot within the region of layered intrusions (Barnes et al.,

1988) with sample JB98-190E from Rathbun Lake (19E) plotting within the field of

hydrothermal or secondary sulphides. A grouping of least fractionated samples, trending

along the positive olivine vector in both discrimination plots (lower right in Ni/Cu-Pd/Ir

and upper left in Cu/Ir-Ni/Pd), mainly consist of samples from Lorne Township (12SW;

Bell Lake intrusion), Waters Township (17C; Makada Lake intrusion) and Nairn

Township (18SW; Nairn Intrusion); these samples also contain elevated MgO and Ir

concentrations (Fig. 5-14). This suggests that these rocks may have been olivine-bearing;

the majority of these same samples are CIPW olivine-normative. Average chilled margin

samples plot within the field of layered intrusions (Barnes et al., 1988) on Cu/Ir versus

Ni/Pd (Fig. 5-15b) and within the overlap region for the fields of layered intrusions and

flood basalts (Barnes et al., 1988) on Ni/Cu versus Pd/Ir (Fig. 5-15a).

The plot of Se versus Pd (Fig. 5-16) is useful for discriminating between rocks that

formed from S-undersaturated (second-stage or fertile) versus S-saturated (first-stage or

infertile) magmas such as MORB (Peck et al., 2001). With the exception of two samples

(JB-98-120 and 121A), all of the unmineralized Nipissing Gabbro samples, including

average chilled margin, plot within the field of S-undersaturated, second-stage magmas,

implying that parental magmas to Nipissing Gabbro were PGE metal-fertile magmas that

had not previously segregated sulphides. The two samples that plot within the first-stage

magma field (1W; Basswood Lake intrusion), are vari-textured to granophyric gabbro

and have very low Pd concentrations. Measurement of Pd concentrations at this low

level could result in erroneous and unreliable data. All six samples from the Lorne

Township (12SW; Bell Lake intrusion) location form a distinct group well within the

field of second-stage (fertile) magmas.

134

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Ni/Cu

Pd/Ir


(all samples - 188)

Rathbun

hydrothermal

increased fractionation

mantle

+olivine

+chromite

(A)

layered intrusions

Figure 5-15a. Discrimination diagram of Ni/Cu versus Pd/Ir for the 188 Nipissing

Gabbro rock samples. This diagram is useful to determine the effects of partial melting

whereby increased partial melting of the mantle lowers Ni/Cu and increases Pd/Ir

(Barnes et al., 1988; Barnes, 1990). The fields of mantle, layered intrusions and

hydrothermal are approximated from Barnes (1990).

135

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Cu/Ir

Ni/P

d


(all samples - 188)

Region Layered Intrusions, Flood Basalts High MgO Basalts and PGE Reefs

S-undersaturation(late S-saturation)

Rathbun - hydrothermal(JB98-190E)

Waters (RK-4)

+olivine

+chromite

+sulphide or PGM

(B)

Figure 15-b. Discrimination diagram of Cu/Ir versus Ni/Pd for the 188 Nipissing Gabbro

rock samples. This diagram is useful to determine the effects of partial melting whereby

increased partial melting of the mantle increases Cu/Ir and lowers Ni/Pd (Barnes et al.,

1988; Barnes, 1990). Average chilled gabbro is from the current study. The overlapping

field of layered intrusions, flood basalts and high MgO basalts is adapted from Barnes

(1990).

136

As discussed earlier, these samples occur along distinct trends in the MgO-Ir, Cu/Ir-Ni-

Pd and Ni/Cu-Pd/Ir plots, indicating that these rocks are much more primitive (olivine-

bearing?) relative to other sampled Nipissing Gabbro rocks.

Primitive mantle-normalized PGE and chalcophile element diagrams (recalculated to

100% sulphide) for average unmineralized samples (59 samples), sorted by location, and

chilled margin gabbro, are shown in Figure 5-17. All of the Nipissing Gabbro sulphides

from mineralized and unmineralized samples are characterized by varying degrees of

positive slopes and define two distinct sets of profiles as shown in Figure 5-17 (<0.05

wt% S) and Figure 5-18 (>0.05 wt% S). In Figure 5-17, unmineralized samples from

Lorne (12SW), Nairn (18SW) and Waters (17C) townships, display profiles that are

relatively elevated in Ni-Ir-Ru-Rh concentrations; samples from the Nairn (18SW)

intrusion show the highest Pd-Au-Cu concentrations. In Figure 5-18, mineralized

samples from Louise (13C), Nairn (18SW) and Waters (17C) townships have sulphide

patterns that are distinctly depleted in Pt-Pd-Au-Cu concentrations; excluding the sample

from Rathbun Lake (19E), which is considered representative of hydrothermal sulphide

(Rowell and Edgar, 1986), mineralized samples from Louise (13C) and Waters (17C)

show the lowest overall PGE concentrations. In Figure 5-18, the sulphide patterns

exhibited by the four averages of mineralized Nipissing Gabbro intrusions (4SW, 8E, 10E

and 19E) closely resemble the profile from East Bull Lake hydrothermal mineralization,

with depleted Ni-, Ir, Ru and Rh versus moderately elevated Pt, Pd, Au and Cu.

The majority of mineralized and unmineralized samples define patterns that are

typical of those displayed by known magmatic sulphides, confirming the magmatic

nature of these sulphides. In addition, the patterns are similar to that of average chilled

margin of Nipissing Gabbro and more significantly, average continental flood basalt

(Naldrett, 1981). Figure 5-17b shows, in detail, the strong similarity between sulphides

from chilled margin samples of Nipissing Gabbro and average flood basalt (Naldrett,

1981). This is important in that it suggests that the magmas which generated the

magmatic PGE in the Nipissing Gabbro suite were probably generated as a result of

continental flood basalt magmatism. The ratio of Pd/Ir can be used to estimate the degree

of fractionation that a magma has undergone, whereby Pd behaves incompatibly and is

concentrated in more fractionated magmas (Keays et al., 1982).

137

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Se (ppb)

Pd (p

pb)

1W4SW5SW7SW12SW18SW13C17C3E8E10E11E16EChilled Margin AvgMORB

(<0.05 wt% S)

First-Stage Magmas (MORB)

Second-Stage Magmas (Fertile)

Average MORB

Figure 5-16. Discrimination diagram of Se versus Pd plotting average unmineralized

samples (59 samples), sorted by location. The plot of Se versus Pd is useful for

discriminating between rocks that formed from S-undersaturated (second-stage or fertile)

versus S-saturated (first-stage or infertile) magmas such as MORB (Peck et al., 2001).

Value for average chilled margin gabbro is from the current study. Value for average

MORB is from Hamlyn and Keays (1986).

138

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Ni Ir Ru Rh Pt Pd Au Cu

Met

al in

100

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ulph

ide/

Prim

itive

Man

tle

1W Avg4SW Avg5SW Avg7SW8E Avg10E Avg11E Avg12SW Avg13C16E17C Avg18SWChilled Margin AvgFlood Basalt AvgEBL Hydrothermal AvgRiver Valley Mineralized

averages with <0.05 wt% S

LORNE

NAIRN

WATERS

River Valley (Breccia Unit)

East Bull Lake - hydrothermal

(A)

Figure 5-17a. Primitive mantle-normalized PGE diagrams (metal in 100% sulphide) for

average unmineralized Nipissing Gabbro (59 samples). Average chilled gabbro and

average mineralized River Valley are from this study; average flood basalt from Naldrett

(1981); average East Bull Lake hydrothermal mineralization from Peck et al. (1993b).

Mantle normalizing values are from Barnes et al. (1988) and McDonough and Sun

(1995).

139

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Met

al in

100

% S

ulph

ide/

Prim

itive

Man

tle

Chilled Margin Avg

JB98-239C

JB98-240

Flood Basalt Avg

Average Flood Basalt (Noril'sk)

(B)

Figure 5-17b Primitive mantle-normalized PGE diagrams (metal in 100% sulphide) for

chilled margin gabbro from Nipissing Gabbro. Average chilled gabbro is from this study.

Average flood basalt (Siberian Traps) is from Naldrett (1981); average East Bull Lake

hydrothermal mineralization from Peck et al. (1993b). Mantle normalizing values are

from Barnes et al. (1988) and McDonough and Sun (1995).

140

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ulph

ide/

Prim

itive

Man

tle

4SW

8E Avg

10E Avg

13C Avg

17C Avg

18SW Avg

19E

Chilled Margin Avg

Flood Basalt Avg

River Valley Mineralized

EBL Hydrothermal Avg

averages with >1.0 wt% S

LOUISENAIRN

WATERS

River Valley (Breccia Unit)

Figure 5-18. Primitive mantle-normalized PGE-chalcophile element diagrams

(recalculated to metals in 100% sulphide) for average mineralized Nipissing Gabbro

samples (24 samples), sorted by location (township). Data for average chilled margin

and average unmineralized River Valley are from this study; average flood basalt is from

Naldrett (1981); data for mineralized River Valley intrusion from this study; average East

Bull Lake hydrothermal mineralization is from Peck et al. (1993b). Mantle normalizing

values are from Barnes et al. (1988) and McDonough and Sun (1995).

141

In Figure 5-17, several samples (Lorne (12SW), Nairn (18SW) and Waters (17C) have

much lower Pd/Ir values relative to that of average continental flood basalt (Naldrett,

1981). Recent work by Lightfoot and Keays (2004) has shown that sulphide from the

Nadezhdinsky flood basalts (Siberian Trap, Noril’sk) contain in general several ppb PGE

and formed by up to 25% fractionation of its parent S-undersaturated magma. The low

Pd/Ir values (Fig. 5-17b), which are due to elevated Ir concentrations, indicates that these

sulphides were formed from magmas that were not as fractionated as those magmas

which produced the sulphides in average continental flood basalt (Naldrett, 1981).

5.2.4 Modelling of Sulphide Compositions

The sulphide compositions of 66 unmineralized (<0.05 wt% S) and 97 mineralized

(>0.05 wt% S) rock samples from various Nipissing Gabbro intrusions were modelled

using the mass balance R factor equation of Campbell and Naldrett (1979) as described in

Section 2.3.5. Utilizing the Pd versus Cu/Pd diagram of Barnes et al. (1993) the

modelling curves (R factor tie lines) are plotted along with the Pd and Cu/Pd values from

the 163 samples (Fig. 5-19). The average Cu and Pd abundances from the 66

unmineralized samples are used as the best estimate for the parental magma composition

(88 ppm Cu, 15 ppb Pd, 5855 Cu/Pd, 0.03 wt% S).

The majority of mineralized sample sulphides can be modelled using R factors that

are much less than 100 (Fig. 5-19), although a number of these samples fall between R

factors of 100 and 1000. The sulphide that can be modelled using the highest R factor

values (i.e. >1000) are primarily from the Chiniguchi River and Kukagami Lake

intrusions, specifically the Rastall (Janes Township) and Washagami Lake (Kelly

Township) occurrences and the Whalen showing in Kelly Township (Fig. 1-2). The

majority of unmineralized sample sulphides can be modelled using R factors of less than

100 and many of these sulphides fall below the sulphide-silicate tie line for R=100,000.

The results suggest that sulphides from the areas with the highest PGE grades (i.e. Rastall

occurrence, Washagami occurrence and Whalen showing; see below) experienced the

highest R factors (~1000 to 2,000). For comparison, it is notable that calculated R factors

for disseminated magmatic sulphide from several intrusions, related to intraplate

magmatism, include 1000 to 20,000 for Noril’sk-Talnakh, 200 to 2000 for Cape Smith,

142

2000 to 10,000 for the Duluth Complex, and 200 to 2000 for the Muskox intrusion

(Barnes et al., 1997).

1

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0.01 0.1 1 10 100 1000 10000 100000 1000000

Pd (ppb)

Cu/

Pd

>0.05 wt% S<0.05 wt% S

MANTLE

DEPLETED

ENRICHED

100%

100%

R=100R=1000

R=10,000

R=100,000

R=2000

0.1%1.0% 10%

Estimated Parental Magma

Figure 5-19. Discrimination plot of Pd versus Cu/Pd showing the sulphide compositions

of 97 mineralized (>0.05 wt% S) and 66 unmineralized (<0.05 wt% S) rocks from

Nipissing Gabbro intrusions. Tie lines are mixing lines between sulphide and silicate melt

at various R factors, ranging from 100 to 100,000, and determined after methods

described by Campbell and Naldrett (1979) and Naldrett (1981). Markers along each of

the mixing lines represent percentages of precipitated sulphide melt at 0.1%, 1.0%, and

10% through to 100% sulphide. The star symbol represents the estimated parental magma

composition derived from the average composition of 66 unmineralized (<0.05 wt% S)

rocks (88 ppm Cu, 15 ppb Pd, 0.03 wt% S), and assuming a sulphide component of 36.5

wt% S. Fields of mantle rocks, and those depleted and enriched in PGE relative to

mantle are taken from Barnes et al. (1993).

143

Most of the mineralized (>0.05 wt% S) samples lie above the Cu/Pd line of mantle

values and the majority of these have values that are above that of mantle and in the field

of depleted PGE (Fig. 5-19). The significance of this is that, prior to their emplacement,

the magmas that formed the Nipissing Gabbro intrusions had probably undergone

sulphide fractionation with the removal of a very small amount of sulphides, possibly

within a staging magma chamber at deeper crustal depths. These magmas, which were S-

saturated, underwent adiabatic decompression during their ascent through the crust,

which increased the S-capacity of the magma (Mavrogenes and O’Neill, 1999) and

returned them to a state of S-undersaturation; a phenomenon that has been recognized in

the East Greenland rifted margin magmas and as an important factor in driving

continental flood basalts to S-undersaturation (Momme et al., 2002b). It appears as

though the magma maintained S-undersaturation en route through the crust until

emplacement as Nipissing Gabbro intrusions in the higher level supracrustal rocks. The

magmas then became S-saturated, likely through normal fractionation and cooling, and

segregated sulphides at the various R factors indicated in Figure 5-19. The majority of

unmineralized and mineralized samples plot with higher Cu/Pd values, indicating that the

magma from which these sulphides precipitated became S-saturated at higher Cu/Pd and

lower Pd values than the estimated initial magma composition (star symbol, Fig. 5-19).

Using the value of average chilled margin gabbro (11.4 ppb Pd, 125 ppm Cu, 10965

Cu/Pd, 0.06 wt% S) as the initial composition of the magma also failed to account for the

distribution of these anomalous samples. This suggests that the estimated initial

composition for Pd (~11-15 ppb) is too high to explain all of the sulphide compositions

and/or that more than one magma composition is required to explain the variations in the

sulphide compositions.

5.3 Basswood Lake Intrusion - Traverse

The Basswood Lake intrusion, a relatively large body of Nipissing Gabbro that

extends parallel to and northeast (~2 km) of the Murray Fault Zone, is located north of

Thessalon on Highway 129, within Bridgland, Wells, Kirkwood and Day Townships

(Figs. 1-2 and 5-20). Fourteen samples were collected along Highway 129 which

provides a well-exposed section (~7 km wide) through the intrusion. This section follows

the same portion of intrusion that was reported on by Lightfoot et al. (1986, 1987, 1993).

144

A sample summary is provided in Table 5-8 and sample locations are shown in Figure 5-

20; a full listing of the data is provided in Appendix 1.

5.3.1 Geology and Mineralization

The Basswood Lake intrusion is hosted by Huronian Supergroup (Gowganda and

Lorrain formations) sedimentary rocks but contacts between the two are not exposed in

the immediate area of the section. Exposed bedrock along the sample section rises from

about 240 m above sea level (ASL) at the southern end, through a central plateau that

ranges from 300-310 m ASL and then increases northward to a peak of about 320 m ASL

at the northern end of the section, at which point overburden covers the bedrock. The

southern margin of the intrusion is locally sheared with numerous narrow (centimetre-

scale) sulphide-bearing (pyrite-chalcopyrite) quartz-carbonate veins occurring within 10s

of metres of the projected contact; Lightfoot et al. (1993) described similar features. The

northern margin of the intrusion is marked by a gradual reduction in grain size

(approaching chilled textures) toward the covered contact region (Fig. 5-20).

From south to north, the sample suite comprises fine- to medium-grained quartz

gabbro, medium-grained orthopyroxene gabbro, medium- to coarse-grained granophyric

and vari-textured gabbro (Photo 4-10), medium- to coarse-grained granophyric gabbro

with pegmatitic patches and aplite veins and dikes (Photo 5-1a), medium-grained quartz

gabbro and orthopyroxene gabbro, and finally fine-grained quartz gabbro. Sample JB97-

65 was collected from an elongate granophyric pod or dike (Photo 4-12), hosted by

medium- to coarse-grained granophyric gabbro, and located about mid-way through the

sample section. Several fragments of sedimentary rock in medium-grained gabbro were

observed in the middle to northern portion of the traverse, in the area of JB97-63 (Photo

5-1b).

Lightfoot et al. (1993) interpreted the Highway 129 section to represent the exposed

basal and upper portion of the sill and described a stratigraphy, from south to north,

consisting of quartz diabase, hypersthene diabase with vari-textured patches, and

granophyric diabase which is transitional into capping quartz diabase. However, current

geochemical evidence and the prevalence of granophyric-aplitic rocks toward the centre

of the section, suggests that this section of the sill represents an unroofed and eroded

antiformal arch portion of the intrusion with lithologies and geochemical trends mirrored

145

on either side of the axial plane (Fig. 5-21). It is notable that the implied strike of the

axial plane (~300 Az) for the antiform parallels that of many of the sulphide-bearing

quartz carbonate veins which cut the intrusive body (i.e. samples JB98-121A, 121B),

suggesting a regional non-penetrative fabric.

Figure 5-20. General geology and sample locations from the Basswood Lake intrusion,

Bridgland, Wells, Kirkwood and Day townships. Geology modified after Ontario

Geological Survey Map 2419 (1979). The location of the Appleby Lake sample section

is outlined and shown in Figure 5-27

146

Sample CIPW S Se Ni Ir Ru Rh Pt PdNorm wt% wt% ppb ppm ppb ppb ppb ppb ppb

JB98-118 G (Q-H) 0.033 187 104 - 0.24 1.08 8.16 23.36JB97-61 OLGN (H-O) 0.070 457 118 - - - - -JB97-62 G (Q-H) 0.040 294 112 - - 1.05 11.13 8.24JB97-63 G (Q-H) 0.080 511 82 - - 0.15 11.02 1.83JB97-64 LG (Q-H) 0.080 361 44 - - - - -JB97-65 aplite 0.130 200 14 - - - - -JB97-66 LG (Q-H) 0.050 288 44 - - - - -

JB98-119 G (Q-H) 0.061 294 60 - 0.14 - - 0.12JB98-120 G (Q-H) 0.016 206 56 - 0.17 - 7.17 0.99

JB98-121A LG (Q-H) 0.044 89 34 0.38 12.08 7.84 - 0.20JB98-121B altered gabbro 4.120 9056 60 - - - - 0.08JB98-122 LG (Q-H) 0.047 253 41 - 0.31 0.14 9.94 2.46JB98-123 GN (H-O) 0.038 201 130 0.10 0.26 0.43 31.50 33.20JB98-124 G (Q-H) 0.052 269 109 - 0.22 0.26 10.07 11.45

Sample CIPW Au Cu S/Se Pd/Pt Cu/Ni Mg# ∑REE (La/Sm)NNorm wt% ppb ppm ppm

JB98-118 G (Q-H) 4.31 140 1765 2.9 1.3 56 64.1 2.39JB97-61 OLGN (H-O) 5.04 78 1532 - 0.7 45 173.3 2.32JB97-62 G (Q-H) 3.79 120 1361 0.7 1.1 54 54.4 2.30JB97-63 G (Q-H) 14.5 264 1566 0.2 3.2 44 90.3 2.61JB97-64 LG (Q-H) 7.6 217 2216 - 4.9 31 110.8 2.60JB97-65 aplite 5.88 91 6500 - 6.5 22 36.1 0.89JB97-66 LG (Q-H) 6.44 111 1736 - 2.5 32 121.7 2.79

JB98-119 G (Q-H) 1.34 279 2075 - 4.7 36 112.1 2.66JB98-120 G (Q-H) 7.36 175 777 0.1 3.1 40 114.7 2.48

JB98-121A LG (Q-H) 1.16 49 4944 - 1.4 38 134.3 2.66JB98-121B altered gabbro 4.19 4769 4549 - 79.5 41 148.5 2.02JB98-122 LG (Q-H) 3.01 155 1858 0.2 3.8 34 141.7 2.73JB98-123 GN (H-O) 6 92 1891 1.1 0.7 72 27.6 1.99JB98-124 G (Q-H) 3.02 108 1933 1.1 1.0 65 41.0 2.21

Table 5-8. Summary of whole-rock geochemical characteristics for samples from the

Basswood Lake intrusion, Kirkwood, Wells and Bridgland townships. "-" below lower

limit of detection; "N" = primitive mantle-normalized; G=gabbro; OLGN=olivine

leucogabbronorite; LG=leucogabbro; GN=gabbronorite; Q-H=quartz-hypersthene; H-

O=hypersthene-olivine. Norm wt% = rock types determined on the basis of weight

percent normative minerals calculated to normative weight percent.

147

There are no known occurrences of significant sulphide mineralization in the

Basswood Lake intrusion. With the exception of sample JB98-121B and to a lesser

extent JB98-121A, none of the samples collected from the Basswood Lake intrusion have

any appreciable (>1%) visible sulphide (Photo 4-13). Sample JB98-121B was collected

from a medium- to coarse-grained, altered granophyric gabbro with disseminated and

stringer sulphide (up to 15% chalcopyrite-pyrite), which occurred within an ~1-2 metre

wide alteration zone (pink- to red-stained hematitic(?) alteration; supergene

mineralization) that continues across the highway exposure and through the area of

sample JB98-121A (Fig. 5-20).

Figure 5-21. Schematic diagram showing the interpreted structure of the Basswood Lake

and Appleby Lake intrusions, Wells Township. The arrows (F) indicate the direction of

migrating fractionated fluids which are expected to accumulate toward the arches of the

sills. HSG=Huronian Supergroup sediments; NG=Nipissing Gabbro; qG=quartz gabbro;

opxG=orthopyroxene gabbro; vtG=vari-textured gabbro; GG=granophyric gabbro;

AP=aplite. The cross section is based on the undulatory model for Nipissing Gabbro

intrusions (Hriskevich, 1968).

148


CIPW normative calculations completed on 12 of the 14 samples, show 10 of the

samples to be quartz-hypersthene-normative (silica-oversaturated) and 2 samples to be

silica-saturated hypersthene-olivine-normative (Table 5-8). Sample JB97-65 is from a

granophyric pod (Photo 4-12) and sample JB98-121B is from an alteration zone with

high S composition. The 10 silica-oversaturated samples classify mainly as CIPW

normative gabbro with subordinate leucogabbro, corresponding to the field assigned

names of gabbro, vari-textured gabbro and granophyric gabbro. The 2 silica-saturated

samples classified as CIPW normative olivine leucogabbronorite (JB97-61) and

gabbronorite (JB98-123), corresponding to the field assigned name of orthopyroxene

gabbro.

The Mg-number, coupled with Ti, may be used as a measure of the degree of

differentiation of a magma whereby decreasing Mg-number accompanied by increasing

Ti indicate increased fractionation. Figure 5-22 plots the 14 samples from the Basswood

Lake intrusion using the calculated Mg-number against wt% TiO2 along with average

chilled margin value from the present study. The least fractionated rocks (JB98-123, 124,

118 and JB97-62), which group in the region of average chilled margin, were collected

from the southern and northern quartz gabbro and orthopyroxene gabbro units. These

contrast the grouping of low Mg-number and high TiO2 rocks which were collected from

the middle region of the section, corresponding to vari-textured and granophyric gabbro.

Sample JB97-61, which has a relatively high Mg-number, is anomalous in that it has the

highest concentration of TiO2. This elevated TiO2 composition may be due to

contamination of the orthopyroxene gabbro unit as a result of AFC processes (Lightfoot

and Naldrett, 1996).

149

Photo 5-1. Basswood Lake Intrusion. (A) Aplite dike cutting medium-grained gabbro.

The hammer handle is about 30 cm long. (B) Sediment fragment in medium-grained

gabbro. The hammer handle is about 30 cm long.

150

Variation in selected major elements across the intrusion are shown in Figure 5-23,

with the major elements plotted against the relative distance through the section. The

concentration of SiO2 and TiO2, along with the variation in Mg-number can provide a

good indication of differentiation trends in magmas, with SiO2 and TiO2 increasing and

Mg-number decreasing with fractionation. Two differentiation trends are recognizable in

the plot of Mg-number; a decreasing, “normal” fractionation trend through the lower half

of the section, followed by an increasing, “reverse” trend through the upper half (Fig. 5-

23). Concentrations of SiO2 show very little variation through the section and TiO2

concentrations (not shown) are highly variable; the extreme variability in the latter is

probably due to AFC processes (Lightfoot and Naldrett, 1996). Although not apparent in

concentrations of SiO2 and TiO2, the mirroring in the Mg-number, provides some

evidence for apparent “inward” crystallization of this intrusion, which would have been

coupled with magmatic fluids migrating upward along the limbs from deeper portions of

the sill fluids, culminating toward the arch region of the sill (Fig. 5-21). Although the

geochemical evidence is not overwhelming, the field evidence and the symmetrical

distribution of the Mg# does provide some support that this section represents an exposed

antiformal or arch section of the sill (Figs. 5-20 and 5-21).


Primitive mantle-normalized multi-element diagrams for the Basswood Lake

intrusion section are shown in Figure 5-24. Except for the granophyric pod sample

(JB97-65), all of the gabbroic rocks show near-parallel patterns with moderate to strong

LILE (Rb, Th, K) enrichment (~10-100 times primitive mantle) with average La/Sm ~2.5

and low to moderate HREE enrichment (~1-10 times primitive mantle). Most of the

gabbroic samples show pronounced negative Nb+Ta and P* anomalies and moderate to

weak negative (or flat) Ti* anomalies; samples JB97-64 and 66, medium- to coarse-

grained gabbro (CIPW leucogabbro), have weak positive Ti* anomalies.

151

JB97-61

JB97-66

JB98-121A

Chilled Margin Avg

0.0

0.5

1.0

1.5

2.0

2.5

3.0

102030405060708090

Mg-number

TiO

2 (w

t%)

JB98-118JB97-61JB97-62JB97-63JB97-64JB97-65JB97-66JB98-119JB98-120JB98-121AJB98-121BJB98-122JB98-123JB98-124Chilled Margin Avg

fractionation

+ aplite olivine leucogabbronorite

B leucogabbro gabbro

U gabbronorite secondary Cu-vein

Figure 5-22. Bivariate scatter plot of 14 samples from the Basswood Lake intrusion using

the calculated Mg-number and wt% TiO2; for comparison, average chilled margin gabbro

from the present study is also shown.

152

Figure 5-23. Profiles through the Basswood Lake intrusion showing stratigraphic

variations in Mg-number and SiO2. The relative vertical scale is in metres.

153

0.1

1

10

100

1000


Sam

ple/

Prim

itive

Man

tle

JB98-118JB97-61JB97-62JB97-63JB97-64JB97-66JB98-119JB98-120JB98-121AJB98-122JB98-123JB98-124Chilled Margin AvgHuronian Sediment AvgAplite Avg (PL)

olivine leucogabbronorite (CIPW)B leucogabbro (CIPW)

gabbro (CIPW)U gabbronorite (CIPW)

(B)

0.1

1

10

100

1000


Sam

ple/

Prim

itive

Man

tle

JB97-65

JB98-121B

JB97-61

Chilled Margin Avg


Aplite Avg (PL)

+ aplite olivine leucogabbronorite (CIPW) secondary Cu-vein

(D)

Figure 5-24. Primitive mantle-normalized multi-element diagrams for rock samples from the Basswood Lake intrusion. (A) Gabbroic samples. (B) Atypical profiles. Mantle normalizing values are from McDonough and Sun (1995).

154


The highest measured Pt+Pd concentrations are from the southernmost and

northernmost samples which also recorded some of the highest MgO concentrations

(Table 5-8). Southern samples JB98-122, 123 and 124 range from 12.4-64.7 ppb Pt+Pd

(Pd/Pt ~1.0; Cu/Ni ~1.9) and northern samples JB98-118, JB97-62 and 63 range from

12.9-31.5 ppb Pt+Pd (Pd/Pt ~1.9; Cu/Ni ~1.9). The highest Ni concentrations also occur

in the northernmost and southern most samples ranging 104-112 ppm in the north and

109-130 ppm in the south.

Selected chalcophile elements and ratios plotted against relative distance through the

intrusion are shown in Figure 5-25. Sample JB98-121B and 121A (Photo 4-13),

considered anomalous in terms of chalcophile elements, tend to disrupt the “normal”

trend on the chemostratigraphic profiles as indicated on each of the plots. The main trend

in the S/Se ratios is similar for both the lower and upper parts of the plot, showing an

initial “inward” decrease, followed by a marked increase through the granophyric gabbro

and reaching maximum in the granophyric pod. Nearly all of the S/Se values are within

the acceptable range of uncontaminated magmatic sulphides (Naldrett, 1981), the

exception being sample JB97-65 (granophyric pod; Photo 4-12) whose S/Se value

(~6500) suggests contamination. The Cu/Ni ratio records a fractionation trend that is

similar to S/Se, with an initial “inward” decrease, followed by a marked increase through

the granophyric gabbro and granophyric pod.

A primitive mantle-normalized PGE and chalcophile element diagram (recalculated

to metals in 100% sulphide) is shown in Figure 5-26. Of the 14 samples analysed for

whole rock PGE, only one sample (JB98-123) assayed above the lower limit of detection

in all of the PGE plus Au. However, for plotting purposes, it is possible to make use of

near compete PGE data from seven of the 14 samples, assigning the average lower limit

of detection for each of the elements that were below detection limits. Patterns from four

of the seven samples are characterized by positive slopes with the Pt-Pd-Au-Cu portion

(~1000 times primitive mantle) of the trends elevated relative to the Ni-Ir-Ru-Rh portion

(~10-500 times chondrite). These samples, which include quartz gabbro, gabbro and

orthopyroxene gabbro, have patterns that are similar to that of the Portimo Dikes from

Finland (Iljina, 1994), although Pd is considerably lower in Nipissing Gabbro samples.

155

Figure 5-25a. Profiles through the Basswood Lake intrusion showing stratigraphic

variations in S/Se. The relative vertical scale is in metres.

156

Figure 5-25b. Profiles through the Basswood Lake intrusion showing stratigraphic

variations in Cu/Ni. The relative vertical scale is in metres.

157

1

10

100

1000

10000

100000

1000000

10000000


Met

al in

100

% S

ulph

ide/

Prim

itive

Man

tle

JB98-118

JB97-62

JB97-63

JB98-121A

JB98-122

JB98-123

JB98-124

Chilled Margin Avg

Flood Basalt Avg

B leucogabbro (CIPW)( gabbro (CIPW)U gabbronorite (CIPW)

JB98-121Aaltered granophyric gabbro


(recalculated to metals in 100% sulphide) for sulphides from Basswood Lake intrusion

rocks. Data for average chilled margin is from this study; data for average flood basalt is

from Naldrett (1981); data for mineralized River Valley intrusion from this study. Mantle

normalizing values are from Barnes et al. (1988) and McDonough and Sun (1995).

158

Contrasting these trends are two samples of granophyric gabbro (JB97-63 and JB98-122)

which display similar overall positive trends but with distinctly depleted Pd and Ni

concentrations; this depletion in Pd and Ni may be attributed to remobilization. Sample

JB98-121A, collected from an altered granophyric gabbro with about 1% disseminated

pyrite, displays elevated Ir-Ru-Rh relative to anomalously depleted Ni-Pt-Pd-Au-Cu; this

chalcophile pattern is interpreted to have resulted from the remobilization of Ni-Pt-Pd-

Au-Cu which are considered much more mobile than the Ir-Ru-Rh.

5.4 Appleby Lake Intrusion - Traverse

The Appleby Lake intrusion, located about 4.5 km northeast of the Basswood Lake

intrusion along Highway 129 in Wells Township, is a relatively narrow (~2 km wide)

body trending 330 degrees (Figs. 1-2, 5-20 and 5-27). A total of 12 samples were

collected along Highway 129, which provides a well-exposed section through the

intrusion; the section is located at about 250 m ASL. A sample summary is provided in

Table 5-9 and sample locations are shown in Figure 5-27; a full listing of the data is

provided in Appendix 1.


At surface, the Appleby Lake intrusion is separated from the Basswood Lake

intrusion, located to the southwest (Fig. 5-20), by sedimentary rocks of the Huronian

Supergroup’s Cobalt Group (Gowganda Formation); it is likely that these two bodies are

connected at depth (Fig. 5-21). Although no contacts with the hosting sedimentary rocks

are exposed in the immediate area of the section, the fine-grained to chilled quartz gabbro

from the northeast end of the section suggests that the contact is within a few metres.

From south to north, the sample suit consists of massive medium-grained gabbro grading

into coarse-grained gabbro, locally altered (pink- to red-stained) medium-grained

granophyric gabbro containing up to 10% disseminated pyrite associated with narrow

(centimetre-scale) quartz-carbonate veinlets, grading into massive medium- to coarse-

grained vari-textured gabbro and granophyric gabbro that is gradational into fine-grained

to chilled quartz gabbro (Fig. 5-27). Current geochemical and especially field evidence,

including the lack of orthopyroxene gabbro and the predominance of granophyric-aplitic

rocks, suggests that this section, as in the Basswood Lake section, represents an unroofed

and eroded antiformal arch portion of an undulating sill (Fig. 5-21).

159

Figure 5-27. General geology and sample locations from the Appleby Lake intrusion in

Wells Township. Geology modified after Ontario Geological Survey Map 2419 (1979).

160

Sample CIPW S Se Ni Ir Ru Rh Pt Pd AuNorm wt% wt% ppb ppm ppb ppb ppb ppb ppb ppb

JB97-48 G (Q-H) 0.060 327 120 - - 0.16 11.20 13.54 3.02JB97-49 G (Q-H) 0.080 364 96 - - - - - -JB97-50 G (Q-H) 0.110 347 65 - - - - 2.06 67.76JB97-51 LG (Q-H) 0.160 345 27 - - - - - 3.41JB97-52 G (Q-H) 0.120 411 60 - - - - - 2.50JB97-53 G (Q-H) 0.100 1395 78 - - - - - 3.47

JB97-54A LG (Q-H-C) 0.930 402 35 - - - 0.16 - 76.10JB97-54B G (Q-H) 0.090 352 79 - - 0.21 - 1.76 6.29JB97-55 G (Q-H) 0.080 358 100 - - - - - 2.71JB97-56 G (Q-H) 0.070 375 110 0.59 - 0.44 4.34 3.44 3.61JB97-57 G (Q-H) 0.080 422 110 - - - 5.00 - 4.21JB97-58 G (Q-H) 0.080 402 110 - - - 7.84 8.42 8.56Sample Cu S/Se Pd/Pt Cu/Ni Mg# ∑REE (La/Sm)N

ppm ppmJB97-48 170 1835 1.2 1.4 56 49 1.62JB97-49 160 2198 - 1.7 52 59 1.97JB97-50 170 3170 - 2.6 41 74 1.98JB97-51 65 4638 - 2.4 25 112 2.23JB97-52 190 2920 - 3.2 36 73 1.95JB97-53 160 717 - 2.1 46 71 1.96

JB97-54A 84 23134 - 2.4 24 688 8.36JB97-54B 170 2557 - 2.2 46 67 1.83JB97-55 170 2235 - 1.7 55 52 1.86JB97-56 160 1867 0.8 1.5 57 48 1.80JB97-57 180 1896 - 1.6 54 53 1.80JB97-58 170 1990 1.1 1.5 54 52 1.76


Appleby Lake intrusion, Wells Township. "-" below lower limit of detection; "N" =

primitive mantle-normalized; G=gabbro; OLGN=olivine leucogabbronorite;

LG=leucogabbro; GN=gabbronorite; Q-H=quartz-hypersthene; H-O=hypersthene-

olivine; Q-H-C=quartz-hypersthene-corundum. Norm wt% = rock types determined on

the basis of weight percent normative minerals calculated to normative weight percent.

161

There are no known significant magmatic sulphide occurrences hosted by the

Appleby Lake intrusion. With the exception of JB97-54A (~10% visible pyrite), none of

the samples collected from the Appleby Lake section have appreciable (>1%) sulphide.


CIPW normative calculations completed on the 12 samples, show 11 of the 12

samples to be quartz-hypersthene normative (silica-oversaturated), with 10 classifying as

gabbro and 1 as leucogabbro (Table 5-9). Sample JB98-54A, classifying as a quartz-

hypersthene-corundum normative (silica-oversaturated) leucogabbro, was collected from

an altered granophyric gabbro with pyrite and quartz-carbonate veining. Figure 5-28, a

plot of Mg-number versus TiO2, is useful for determining the degree of fractionation in

the rock samples. The least fractionated rocks (JB97-55, 56, 57, 58), which group near

the compositional average chilled margin, were collected from the westernmost and

easternmost ends of the section, whereas the more fractionated rocks (JB97-50, 51, 52,

53, 54B) are from the middle region of the section, corresponding to dominantly vari-

textured and granophyric rocks. Weak, “inward” directed fractionation pattern is

interpreted from the geochemical data, similar to that from the Basswood Lake intrusion

(see Section 5.3), and as reported from other Nipissing Gabbro intrusions (e.g. Conrod,

1988; Lightfoot and Naldrett, 1996).

Variation in Mg-number and SiO2 are shown in Figure 5-29, plotted against relative

distance through the section; as in the Basswood Lake intrusion, the concentration of

TiO2 is highly variable (not shown) and SiO2 is reasonably uniform, probably as a result

of AFC processes (Lightfoot and Naldrett, 1996). The Mg-number shows a weakly

developed “inward” directed fractionation trend, with mirroring in the Mg-number from

the top and bottom, toward the central region of the section. As in the Basswood Lake

intrusion, the geochemical evidence is not overwhelming, but the field evidence does

support the interpretation that this section represents an exposed upper portion of a sill

(Fig. 5-21).


Primitive mantle-normalized multi-element diagrams for the gabbroic rocks

collected from the Appleby Lake section are shown in Figure 5-30.

162

0.0

0.5

1.0

1.5

2.0

2.5

102030405060708090

Mg-number

TiO

2 (w

t%)

JB97-48JB97-49JB97-50JB97-51JB97-52JB97-53JB97-54AJB97-54BJB97-55JB97-56JB97-57JB97-58Chilled Margin Avg

fractionation

Ychilled gabbro (gabbro - CIPW)B leucogabbro (CIPW)A gabbro (CIPW)

JB97-54Aaltered granophyric gabbro(~10% pyrite)

Figure 5-28. Bivariate scatter plot of samples from the Appleby Lake intrusion using the

calculated Mg-number and wt% TiO2; for comparison, average chilled margin gabbro


163

Figure 5-29. Profile through the Appleby Lake intrusion showing stratigraphic variations

in Mg-number and SiO2. The relative vertical scale is in metres.

164

All of the gabbroic samples, except JB97-54A (altered granophyric gabbro), show near-

parallel patterns that are similar but elevated relative to average chilled margin, with

moderate to strong LILE enrichment (~10-100 times primitive mantle; average La/Sm

~1.9) and low to moderate HREE enrichment (~1-10 times primitive mantle). As is

typical of Nipissing Gabbro rocks, all of these samples show pronounced negative Nb+Ta

and P* anomalies and subtle negative to flat (slightly positive) Ti* anomalies.


Individual PGE concentrations for most samples were mostly near or below the

lower limits of detection. The highest concentration of Pt+Pd (24.74 ppb; Pd/Pt = 1.2;

Cu/Ni = 1.4) is from chilled quartz gabbro (JB97-48), followed by gabbro samples JB97-

56 (7.78 ppb; Pd/Pt = 0.8; Cu/Ni = 1.5) and JB97-58 (16.26 ppb; Pd/Pt = 1.1; Cu/Ni =

1.6); these samples are from the southernmost and northernmost parts of the sample

section.

Selected chalcophile elements and ratios, plotted against relative distance through the

Appleby section, are shown in Figure 5-31. The plot of S/Se shows a subtle “inward”

increase, from both the upper and lower parts of the section toward the middle where

there is a sudden decrease in S/Se (717; JB97-53) in the vari-textured/granophyric gabbro

unit (JB97-53), suggesting sulphur loss (Reeves and Keays, 1995). Excepting samples

JB97-53 and JB97-54A, all of the S/Se values plot within the acceptable range (~1835-

4638) of uncontaminated magmatic sulphide (Naldrett, 1981). Sample JB97-54A yields

a contamination signature for S/Se (23,134), suggestive of contamination by external

sedimentary-derived sulphur (Naldrett, 1981). The ratio of Cu/Ni records an “inward”

increasing fractionation trend.

A primitive mantle-normalized PGE and chalcophile element diagram (recalculated

to metals in 100% sulphide) is shown in Figure 5-32. Of the 12 samples analyzed for

whole rock PGE, only one sample (JB97-56) assayed above the lower limits of detection

for 4 (Ir, Rh, Pt, Pd) of the 5 PGE; an average lower limit of detection value (0.66 ppb)

was allocated to Ru. This sample, a classified as a gabbro (both in the field and by

CIPW) is characterized by a moderate positive PGE slope (Pt-Pd-Au-Cu > Ni-Ir-Ru-Rh)

that is close to that of average chilled margin gabbro but more significantly, it is similar

to the trend of average continental flood basalt.

165

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(A)Y chilled gabbro (gabbro - CIPW)B leucogabbro (CIPW)A gabbro (CIPW)

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Aplite Avg (PL)

JB97-54Aaltered granophyric gabbro(~10% pyrite)

B leucogabbro (CIPW)(B)

Figure 5-30. Primitive mantle-normalized multi-element diagrams for rock samples from the Appleby Lake intrusion. (A) Gabbroic samples. (B) Atypical profiles. Mantle normalizing values are from McDonough and Sun (1995).

166

Figure 5-31a. Profiles through the Appleby Lake intrusion showing stratigraphic

variations in S/Se. The relative vertical scale is in metres.

167

Figure 5-31b. Profiles through the Appleby Lake intrusion showing stratigraphic

variations in Cu/Ni. The relative vertical scale is in metres.

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A gabbro (CIPW)


(recalculated to metals in 100% sulphide) for sulphides from the Appleby Lake intrusion


from Naldrett (1981). Mantle normalizing values are from Barnes et al. (1988) and

McDonough and Sun (1995).

169

5.5 Charlton Lake Intrusion - Traverse

The Charlton Lake intrusion, located about 65 km southwest of the City of Greater

Sudbury and ~3 km north of the village of Whitefish Falls (Figs. 1-2 and 5-33), extends

for more than 16 km across Mongowin and Curtin townships (Card, 1976). The sample

suite, consisting of 13 samples, was collected from an elevated and relatively well-

exposed section of Nipissing Gabbro along the northeastern shoreline of Charlton Lake

(Fig. 5-33). The section, which is about 320 m wide, exposes gabbroic rocks and the

footwall and hangingwall Huronian sedimentary rocks. A summary of the samples is

provided in Table 5-10 and a complete listing of the data is provided in Appendix 1.


Phemister (1939) suggested that the Charlton Lake intrusion is a sill and current

geochemical and field evidence from the Charlton Lake section supports this

interpretation; the northern contact representing the base of the sill and the southern

margin, the top. In the area of the sample section, the Charlton Lake intrusion is hosted

by Gowganda Formation sedimentary rocks (conglomerate, siltstone, argillite). The

southern contact, interpreted to represent the hangingwall, is partially exposed and

consists primarily of sedimentary-gabbro breccia with fragments of sedimentary rock

10’s of centimetres in size. The contact itself is sharp and irregular, marked by very fine-

grained (chilled) gabbro and altered (bleached) sedimentary rocks; the northern contact

region, interpreted as the footwall, is not exposed. Several percent visible sulphide were

noted from gabbro (JB98-183) and orthopyroxene gabbro (JB98-182), situated about 80

m south of the northern contact (Fig. 5-33).

From north to south, the sample suite comprises massive medium-grained gabbro

which is gradational into massive medium-grained orthopyroxene gabbro, which is in

turn gradational into massive medium-grained to locally coarse-grained gabbro, and

finally fine-grained gabbro. Sample JB98-186, located along the section between

samples JB98-184 and 183, was collected from a felsic dike which cut through the

gabbro.

A number of PGE-Cu-Ni sulphide occurrences are known to be hosted by this

intrusion (Fig. 5-40), concentrated in the area from Upsala Gold Mine to Casson Lake

(~6.5 km long), and including the AN3 showing (see Section 5.6).

170 170

171


JB98-185 sediment 0.085 160 20 0.013 0.680 0.115 0.440 0.518JB98-184 GN (H-O) 0.035 241 175 0.070 0.500 0.663 13.980 55.500JB98-183 GN (H-O) 0.232 1733 511 0.267 0.640 1.820 58.000 156.000JB98-182 GN (H-O) 0.085 422 166 - 0.270 0.126 3.150 3.010JB98-181 G (Q-H) 0.078 364 98 - 0.320 0.480 0.238 0.282JB98-180 G (Q-H) 0.076 234 131 - - - 1.780 1.470JB98-179 G (Q-H) 0.070 366 148 - 0.370 0.092 1.677 1.750JB98-178 G (Q-H) 0.031 155 118 - 0.150 - 1.570 1.830JB98-177 G (Q-H) 0.017 105 83 - 0.190 - 1.320 1.190JB98-175 G (Q-H) 0.034 191 120 - 0.160 0.202 8.600 7.110JB98-174 GN (H-O) 0.285 1036 139 - - 0.320 8.790 10.560JB98-176 sediment 0.005 13 16 0.010 0.150 0.019 0.298 0.142JB98-186 felsic dike 0.005 24 15 0.040 0.044 0.017 0.234 0.399Sample Au Cu S/Se Pd/Pt Cu/Ni Mg# ∑REE (La/Sm)N

ppb ppm ppmJB98-185 1.830 11 5313 1.2 0.6 40 120 4.14JB98-184 4.510 120 1452 4.0 0.7 74 30 2.04JB98-183 33.500 870 1339 2.7 1.7 74 28 2.05JB98-182 2.350 295 2014 1.0 1.8 71 31 1.95JB98-181 1.630 143 2143 1.2 1.5 66 39 2.33JB98-180 1.940 161 3248 0.8 1.2 71 33 2.11JB98-179 2.230 221 1913 1.0 1.5 70 39 2.34JB98-178 2.560 86 2000 1.2 0.7 65 42 2.37JB98-177 1.890 154 1619 0.9 1.9 62 60 2.52JB98-175 3.040 104 1780 0.8 0.9 69 29 1.97JB98-174 13.200 412 2751 1.2 3.0 63 42 2.20JB98-176 1.650 9 3846 0.5 0.6 50 63 3.29JB98-186 0.575 3 2083 1.7 0.2 61 12 1.52


Charlton Lake intrusion, Curtin Township. "-" below lower limit of detection; "N" =

primitive mantle-normalized; G=gabbro; OLGN=olivine leucogabbronorite;

LG=leucogabbro; GN=gabbronorite; Q-H=quartz-hypersthene; H-O=hypersthene-

olivine; Q-H-C=quartz-hypersthene-corundum. Norm wt% = rock types determined on

the basis of weight percent normative minerals calculated to normative weight percent.

172

The dominant style of mineralization is sulphide associated PGE (~1-3% disseminated

chalcopyrite and pyrrhotite) with average values of 0.5-1.5 g/t Pd and 0.25-1.0 g/t Pt,

exposed over widths of 5-30 m (Harron, 2000). A second style of PGE mineralization is

described as cross-cutting, “volatile enriched” hydrothermal mineralization, associated

with elevated chromite, chalcopyrite and pyrrhotite with values up to 8 g/t Pd and 3 g/t Pt

(Harron, 2000). Several Au occurrences (quartz-vein, structurally controlled, and/or

sediment hosted) are also known to occur at or proximal to the contact between the

Nipissing Gabbro intrusion and the hosting sedimentary rocks (Card, 1976).


On the basis of 12 CIPW normative calculations (Table 5-10), 4 of the samples are

hypersthene-olivine-normative (silica-saturated) and classify as gabbronorite, and

correspond with assigned field names of gabbro and orthopyroxene gabbro. The

remaining 8 samples are quartz-hypersthene-normative (silica oversaturated) and classify

as gabbro, corresponding with their gabbro field names.

All of the gabbroic samples plot with higher Mg-number and lower concentrations of

TiO2, relative to average chilled margin gabbro (Fig. 5-34). Assuming that average

chilled margin is representative of parent magma composition, it follows that these higher

MgO and lower TiO2 concentrations reflect higher proportions of orthopyroxene

phenocrysts and/or olivine in these rocks. Variation in selected major elements across the

intrusion are shown in Figure 5-35, plotting major elements against relative distance

through the intrusion from the base (north end) to the upper contact (south end). The

concentration of SiO2 shows subtle variation and only a very slight increase “upward”

through the intrusion, from north to south. The concentration of TiO2 shows a strong

positive fractionation trend increasing from ~0.4 wt% near the base to >0.5 wt% toward

the top. Decreasing Mg-number, characteristic of normal magma differentiation, is

evident from north to south across the intrusion with the highest Mg-numbers in the

lowermost orthopyroxene gabbro (CIPW gabbronorite). Sample JB98-177, which

disrupts the general trends on all of the chemostratigraphic plots, was collected from very

near (~5 m) the contact with Huronian sedimentary rocks (sample JB98-176). Its

uncharacteristic chemistry, including elevated SiO2 and TiO2, suggests contamination,

most probably through interaction with hangingwall Huronian sediment.

173

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JB98-176 (HW)JB98-174JB98-175JB98-177JB98-178JB98-179JB98-180JB98-181JB98-182JB98-183JB98-186JB98-184JB98-185 (FW)Chilled Margin Avg

+ sedimentA gabbro (CIPW)U gabbronorite (CIPW)# felsic dike

fractionation

Figure 5-34. Bivariate scatter plot of samples from the Charlton Lake intrusion using the



174

Figure 5-35a. Profiles through the Charlton Lake intrusion showing stratigraphic


175

Figure 5-35b. Profiles through the Charlton Lake intrusion showing stratigraphic

variations in TiO2. The relative vertical scale is in metres.

176


Variations in Zr and ∑REE plotted against relative distance through the sample

section are shown in Figure 5-36. This chemostratigraphic plot shows a gradual increase

through the intrusion, suggesting normal fractionation from north to south. As was seen

in the major element plots, sample JB98-177 plots outside of the general trend, which is

probably the result of contamination through interaction with hangingwall sedimentary

rocks.

Primitive mantle-normalized multi-element diagrams for the Charlton Lake section

are shown in Figure 5-37. Gabbroic rocks show near-parallel patterns, following closely

the pattern of average chilled margin gabbro, with moderate to strong LILE enrichment

(~10-100 times primitive mantle), an average of ~2.7 La/Sm, and low to moderate HREE

enrichment (~1-10 times primitive mantle). All of the gabbroic samples show

pronounced negative Nb+Ta, P* and Ti* anomalies, a typical feature of Nipissing

Gabbro magmas. The felsic dike (JB98-186) displays the widest variance in trace and

rare-earth elements with anomalously high Th, P* and Zr concentrations and

anomalously low Rb and K* concentrations. These variations suggest that this dike may

be genetically linked to the immediate Huronian sedimentary rocks and may represent

sedimentary derived melt that was sourced from the footwall sedimentary rocks and

“back-injected” into the gabbro.


Within the section sample suite, sulphide occurs in samples JB98-183, collected

from the lowermost gabbro unit, and sample JB98-174, collected from the gabbro unit

proximal to the hangingwall Huronian sediment; as indicated earlier, sample JB98-174

has geochemical signatures indicative of contamination. The sulphides (~1%) are

primarily finely disseminated chalcopyrite and pyrrhotite with subordinate pyrite. The

highest concentrations of Pt+Pd are from samples JB98-183 (~214 ppb Pt+Pd; Pd/Pt

~2.7; Cu/Ni ~1.7) and JB98-184 (~70 ppb Pt+Pd; Pd/Pt ~4.0; Cu/Ni ~0.7) in the

lowermost gabbro (CIPW gabbronorite) and from samples JB98-174 (~19 ppb Pt+Pd;

Pd/Pt ~1.2; Cu/Ni ~3.0) and JB98-175 (~16 ppb Pt+Pd; Pd/Pt ~0.8; Cu/Ni ~0.9) in the

uppermost gabbro.

177

Figure 5-36. Profile through the Charlton Lake intrusion showing stratigraphic variations

in Zr and total rare-earth elements. The relative vertical scale is in metres.

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JB98-175

JB98-177

JB98-178

JB98-179

JB98-180

JB98-181

JB98-182

JB98-183

JB98-184

Chilled Margin Avg

+ sedimentA gabbro (CIPW)) gabbronorite (CIPW)

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JB98-186

Chilled Margin Avg

A gabbro (CIPW)) gabbronorite (CIPW)# felsic dike

(B)

Figure 5-37. Primitive mantle-normalized multi-element diagrams for rock samples from the Charlton Lake intrusion. (A) Gabbroic samples. (B) Atypical profiles. Mantle normalizing values are from McDonough and Sun (1995).

179

Selected chalcophile elements and ratios are plotted against relative distance through

the intrusion in Figure 5-38. The highest S/Se values are from the hangingwall and

footwall sedimentary rocks (3846 and 5313), contrasting the lower S/Se values from the

intrusive rocks which are between 1339 and 3248. The S/Se ratios of the gabbroic rocks

are all within the range of uncontaminated magmatic sulphide (Naldrett, 1981).

Concentrations of S show a general decline from the lowermost gabbro unit (CIPW

gabbronorite) upward or southward into the upper part of the middle gabbro unit, then

increasing toward a maximum S concentration in the upper gabbro (CIPW gabbronorite)

unit. The S maxima from the upper and lower gabbro (CIPW gabbronorite) units are

coincident with the 2 maximum values of Pt+Pd and Cu, suggesting sulphide control on

the PGE.

The ratio of Cu/Pd has been shown to be a useful indicator of whether or not

sulphide segregation has occurred within a magma (Hamlyn et al., 1985; Hoatson and

Keays, 1989). Rocks with Cu/Pd values above 6500 indicate that they may have

crystallized from magma that has lost Pd as a result of earlier sulphide segregation,

whereas magmas with Cu/Pd values below 6500 should contain Pd-rich sulphides. This

ratio is also useful when scrutinizing chemostratigraphic sections, whereby a distinct

increase in the Cu/Pd ratio occurs in the vicinity of PGE-rich horizons (Prendergast and

Keays, 1989; Hoatson and Keays, 1989; Barnes et al., 1992; Maier et al., 1996). In

Figure 5-38a, values of Cu/Pd are <6500 for the first 2 samples in the lowermost gabbro

unit, but quickly jump to ~98,000 and remain above 14,000 for the remainder of the

stratigraphy. This sudden change in the lowermost orthopyroxene gabbro unit suggests

that S-saturation occurred at this point in the stratigraphy.

Reeves and Keays (1995), in their study of the Bucknalla Complex (Australia),

demonstrated that first formed sulphides (precipitating from high Mg, S-undersaturated

magmas) have higher relative Pd/S and Pt/S, which decrease as PGE supply is reduced

and S continues to increase during normal progressive fractionation. The instance of S-

saturation is reflected by the chemostratigraphic plot of Pt/S and Pd/S (Fig. 5-38b) where

the rapid decrease in Pt/S and Pd/S ratios correlate with the rapid increase in Cu/Pd at

sample JB98-182.

180

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gabbro (GN)

gabbro (G)

sediment

gabbro (GN)

NORTH

SOUTH

S/Se Cu/PdS (ppm)

(A)

Figure 5-38a. Profiles through the Charlton Lake intrusion showing stratigraphic

variations in S, S/Se and Cu/Pd. The arrows indicate the direction of sulphide

precipitation (crystallization) fronts. The relative vertical scale is in metres.

181

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NORTH

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Pt+Pd (ppb)Cu/Ni Pd/Pt Pt/S Pd/S

Figure 5-38b. Profiles through the Charlton Lake intrusion showing stratigraphic

variations in Cu/Ni, Pd/Pt, Pt+Pd, Pt/S and Pd/S. The arrows indicate the direction of

sulphide precipitation (crystallization) fronts. The relative vertical scale is in metres.

182

Another trend exhibited by the Pt/S and Pd/S ratios is declining ratios from the top

(south) and base (north) of the intrusion toward the central area of the section. This

suggests that there was co-precipitation of sulphides in the magma along two sulphide

precipitation fronts; one moving downward from the upper part of the sill and the other

moving upward from the lower part of the sill. This is also reflected in the Cu/Pd ratio

which exhibits increasing Cu/Pd from the base upward and from the roof downward; this

trend is weakly reflected in the variation of Mg-number (Fig. 5-35).


metals in 100% sulphide) are provided in Figure 5-39. Of the 13 samples analysed for

whole rock PGE, only five of the samples assayed above the lower limits of detection in

all of the PGE plus Au. However, it is possible to make use of near complete PGE data

from nine of the 13 samples, assigning the average lower limit of detection for each of

the elements that were below detection limits. Excepting samples JB98-181 (gabbro) and

JB98-185 (footwall sediment), all of the samples (two sedimentary rocks, six gabbroic

rocks and one felsic dike) are characterized by positive slopes in the PGE patterns (Pt-Pd-

Au-Cu > Ni-Ir-Ru-Rh). Samples JB98-184 and JB98-183, located at the level in the

intrusion before which S-saturation is thought to have occurred, have the highest

concentrations of Rh-Pt-Pd-Au-Cu, reflecting the change in magma composition at S-

saturation.

The unusual pattern exhibited by JB98-181 (Fig. 5-39), characterized by

anomalously depleted Pt-Pd relative to Ir-Ru-Rh, is interpreted to be the result of

hydrothermal redistribution of Pt and Pd. PGE patterns from the 2 sedimentary rock

samples are similar, although the abundance of PGE in the hangingwall sedimentary rock

sample is about 10 times higher than the footwall sedimentary rock sample. The felsic

dike sample (JB98-186) has a distinct profile but plots within the range of the gabbroic

and sedimentary samples.

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JB98-181

+ sedimentA gabbro (CIPW)) gabbronorite (CIPW)# felsic dike

(A)


(recalculated to metals in 100% sulphide) for sulphides from the Charlton Lake intrusion


from Naldrett (1981). Mantle normalizing values are from Barnes et al. (1988) and


184

5.6 AN3 Occurrence and Traverse

The AN3 PGE-Cu-Ni occurrence, located about 9.5 km east of the Charlton Lake

section (see Section 5.5) and south of Casson Lake (Figs. 1-2, 5-40 and 5-41), is hosted

by the Charlton Lake sill (see Section 5.5). The sample suite, consisting of 5 samples,

was collected along a north-south section through the Nipissing Gabbro sill, about 100 m

east of the AN3 PGE-Cu-Ni occurrence and several hundred metres west of 3 other

cleared areas (AN1 AN2, AN4) that also contain anomalous PGE-Cu-Ni (Fig. 5-41).

One sample, JB98-225A, was collected from the location of the “malachite pit”, about

400 m east of the sample section. A summary of the rock samples is provided in Table 5-

11 and a complete listing of the data is provided in Appendix 1.


The Charlton Lake sill is hosted by Gowganda Formation (Huronian Supergroup)

sedimentary rocks all along its length, from the Charlton Lake section (see Section 5.5)

and eastward through the area of the AN3 occurrence (Fig. 5-40 and 5-41). Several

northwest-trending faults and Sudbury Swarm dikes dissect the intrusion along its length;

displacement along the faults appears to be predominantly strike-slip and on the order of

10’s of metres to a few hundred metres. Numerous outcrops (mainly sedimentary rocks)

in the area contain Sudbury-type breccia (Card, 1976) and Harron (2000) described a

southeast-trending body of Sudbury-type breccia that dissects the sill in the area between

the Upsala and Bousquet Au mines. Locally, the sample section consists of

unmineralized, medium-grained, massive gabbro; neither the north or south contacts with

sedimentary rocks are exposed.

Numerous PGE-Cu-Ni sulphide showings occur along the length of the Charlton

Lake sill and the approximate locations of these are shown in Figure 5-40. A listing of

the highest concentrations of PGE-Au-Cu-Ni are provide in Table 5-12. Sample JB98-

225A, collected from the “malachite pit” (Fig. 5-41) as a example of sulphide

mineralization in the area, is described as a medium-grained gabbro containing ~5%

disseminated sulphide. At this showing, malachite staining is common along fracture

planes in the host gabbro.

In the immediate area of the sample section are the 4 PGE-Cu-Ni showings, AN1,

AN2, AN3 and AN4 (Fig. 5-41) but none of the samples collected from the sample

185

section have any significant sulphide mineralization. Sulphide mineralization at the AN3

occurrence consists of about 2-3% finely disseminated chalcopyrite and pyrrhotite,

hosted by medium-grained vari-textured gabbro with patches of pegmatitic gabbro (Photo

5-2). The sulphide-hosting vari-textured gabbro unit is locally extensively altered with

fibrous fine-grained actinolite-tremolite and chlorite and saussurite (plagioclase).

Exposed contacts between the vari-textured gabbro and surrounding Nipissing Gabbro

rocks to the west and east are sharp (Photo 5-2a), suggesting a pipe-like geometry for the

vari-textured unit.

Harron (2000), drawing on analogies to the UG-2 Reef in the Bushveld Complex,

described this unit as a pegmatoidal layer, 10 m wide (east-west) and up to 30 m thick

(north-south) and in contact with a Cr-rich (1300-5100 ppm Cr) ultramafic unit which is

overlain by a unit of massive actinolite-tremolite (altered gabbro-melagabbro?,

ultramafic?). The continuation of this unit to the east, into the area of the sample section,

was not observed in the field suggesting that this PGE-Cu-Ni occurrence is either a

sulphide showing of limited horizontal or vertical extent, or is a pipe-like structure with

potential for vertical continuation; limited diamond drilling under the AN3 showing in

1996 failed to intersect significant mineralization.


The 4 gabbroic samples are characterized by averages of 49.9 wt% SiO2 (range

49.47-51.16), 0.37 wt% TiO2 (range 0.35-0.40), 10.8 wt% MgO (range 10.46-11.04), and

Mg-number 75 (range 72-76). CIPW calculations on the gabbroic samples classify 3 of

the 4 as hypersthene-olivine-normative (silica-saturated) gabbronorite and one as a

quartz-hypersthene (silica-oversaturated) gabbro (Table 5-11). From north to south, there

is a general increase in the concentrations of SiO2 (49.51 to 51.16) and TiO2 (0.37 to

0.40), and a general decrease in Mg-number (76 to 72). These data suggest that the base

of the sill lies to the north. The rocks from the AN3 section have similar major-element

compositions as those from the Charlton Lake section (see Section 5.5) with higher Mg-

number and MgO concentrations and lower TiO2 concentrations relative to average

chilled margin gabbro.

186

187

188


JB98-228 GN (H-O) 0.009 113.0 166 0.147 0.28 0.91 21.50 46.50JB98-229 GN (H-O) 0.015 153.0 172 0.116 0.26 0.86 17.18 63.80JB98-230 GN (H-O) 0.045 318.0 198 0.114 0.25 0.57 33.40 42.30JB98-231 G (Q-H) 0.044 314.0 155 0.045 - 0.22 9.67 9.44JB98-232 sediment 0.039 84.0 15 0.019 0.05 0.03 0.49 0.51

Sample Au Cu S/Se Pd/Pt Cu/Ni Mg# ∑REE (La/Sm)N

ppb ppm ppm

JB98-228 5.500 69 796 2.2 0.4 76 23 1.79JB98-229 4.570 90 980 3.7 0.5 75 24 1.78JB98-230 15.300 176 1415 1.3 0.9 76 23 1.85JB98-231 4.790 108 1401 1.0 0.7 72 25 2.11JB98-232 1.520 14 4643 1.0 0.9 37 86 3.45


AN3 sample section south of Casson Lake, Charlton Lake intrusion, Curtin Township. "-

" below lower limit of detection; "N" = primitive mantle-normalized; G=gabbro;

OLGN=olivine leucogabbronorite; LG=leucogabbro; GN=gabbronorite; Q-H=quartz-

hypersthene; H-O=hypersthene-olivine; Q-H-C=quartz-hypersthene-corundum. Norm

wt% = rock types determined on the basis of weight percent normative minerals

calculated to normative weight percent.

189


Primitive mantle-normalized multi-element diagrams for the AN3 section are shown

in Figure 5-42. The gabbroic samples have profiles that are typical of Nipissing Gabbro,

with moderate to strong LILE enrichment and pronounced negative Nb+Ta and P*

anomalies; 3 of the 4 samples have weak to moderate Ti* anomalies, with one sample

(JB98-231) showing a slightly positive Ti* anomaly. Ratios in primitive mantle-

normalized (La/Sm)N range from 1.79 in the north to 2.11 in the south, suggesting little if

any crustal contamination and fractionation from north to south.

Location Pd Pt Au Cu Ni Pt+Pd Pd/Pt Cu/Nippm ppm ppm wt% wt% ppm

AN2 2.60 0.50 0.80 0.70 0.26 3.10 5.20 2.69AN3 4.50 3.40 0.90 0.30 0.12 7.90 1.32 2.50AN4 2.20 0.50 0.40 0.60 0.25 2.70 4.40 2.40BP-1 1.40 1.10 4.40 0.40 0.08 2.50 1.27 5.00BP-5 2.10 0.80 0.30 0.90 0.09 2.90 2.63 10.00BP-6 2.40 0.50 0.80 0.70 0.17 2.90 4.80 4.12BP-7 3.50 0.70 0.70 0.30 0.06 4.20 5.00 5.00BP-8 0.70 0.50 0.40 0.40 0.14 1.20 1.40 2.86BP-9 0.90 0.80 0.70 0.30 0.07 1.70 1.13 4.29

BP-10 2.10 0.50 0.90 0.80 0.28 2.60 4.20 2.86BP-11 0.30 0.20 0.10 0.40 0.13 0.50 1.50 3.08BP-12 1.40 0.30 0.60 0.40 0.22 1.70 4.67 1.82

Table 5-12. Summary of the highest concentrations of PGE-Au-Cu-Ni from historical

sampling of the Charlton Lake sill, Curtin Township. Data are reported by MacDonald

Mines Exploration Limited and summarized from Harron (2000). Data from Harron

(2000) and MacDonald Mines Exploration Ltd. (2000).

190

Photo 5-2. Charlton Lake Intrusion, Casson Lake AN3 occurrence. (A) Medium-grained massive gabbro-orthopyroxene gabbro hosting distinct “pipe-like” unit of sulphide (PGE) bearing vari-textured gabbro. Note the irregular nature of the contact. The marker pen is about 14 cm long. (B) Close up of sulphide-bearing vari-textured gabbro as in (A). The Canadian two dollar coin is about 2.8 cm in diameter.

191

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JB98-228

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JB98-232

Chilled Margin Avg

Aplite Avg (PL)


A gabbro (CIPW)) gabbronorite (CIPW)+ sediment

(A)

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JB98-228

JB98-229

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A gabbro (CIPW)) gabbronorite (CIPW)

(B)

Figure 5-42. Primitive mantle-normalized multi-element diagrams for rock samples from the AN3 sample section. (A) All samples. (B) Gabbroic samples. Mantle normalizing values are from McDonough and Sun (1995).

192


Sample JB98-225A, the only sulphide-bearing sample collected from this area, is

characterized by 1.02 ppb Ir, 1.56 ppb Ru, 5.5 ppb Rh, 264 ppb Pt, 384 ppb Pd, 166 ppb

Au, 2863 ppm Cu, 1447 ppm Ni, 1.5 Pd/Pt, and 2.0 Cu/Ni, and a magmatic S/Se value of

3667. Samples collected along the AN3 section contain no visible sulphide with S

compositions from all samples <0.05 wt% S. The highest concentration of PGE from the

sample section is from JB98-229 which contains 81.0 ppb Pt+Pd (3.7 Pd/Pt; 0.5 Cu/Ni).


the sample section in Figure 5-43; the approximate stratigraphic level of the AN3

sulphide mineralization, located about 100 m to the west, is also shown. Two of the 4

samples have S/Se values that are within the range of magmatic sulphides (Naldrett,

1981) and two of the samples have values that are <1000, suggesting S-loss or elevated

Se relative to S. Concentrations of Pt, Pd, Cu and Ni show a decline after reaching

maxima at the projected stratigraphic level of AN3 mineralization (Fig. 5-43).

Conversely, concentrations of S and ratios of S/Se and Cu/Pd show an increase upward

through the section. The Cu/Pd ratio surpasses 6500 in the rock sample immediately

above the estimated stratigraphic level of the AN3 mineralization, suggesting that

sulphide segregation is concentrated at the stratigraphic level coincident with AN3

mineralization.


metals in 100% sulphide) are provided in Figure 5-44, with compositions from the

sample section rocks compared with average chilled margin gabbro (this study), average

flood basalt (Naldrett, 1981) and average hydrothermal mineralization from the East Bull

Lake intrusion (Peck et al., 1993b). All of the samples display positive PGE slopes with

the highest Pd abundances from 3 of the 4 gabbroic samples. These patterns are typical

of magmatic sulphide patterns and are unlike the pattern exhibited by hydrothermal

mineralization.

193

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sediment

gabbro (GN)

gabbro (G)

S/Se

Pd/SePt/Se

Cu (ppm)

Ni (ppm)

S (ppm)

approx. stratigraphic levelof AN3 mineralization

Cu/Pd

Pt (ppb)Pd (ppb)

Figure 5-43. Profiles through the AN3 sample section, showing stratigraphic variations in

Pt/Se, Pd/Se, Pt, Pd, Cu, Ni, S, S/Se and Cu/Pd. The vertical scale is relative.

194

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JB98-228

JB98-229

JB98-230

JB98-231

JB98-232

Chilled Margin Avg

Flood Basalt Avg


A gabbro (CIPW)) gabbronorite (CIPW)+ sediment


(recalculated to metals in 100% sulphide) for sulphides from the AN3 section, located

south of Casson Lake, in the Charlton Lake intrusion, Curtin Township. Data for average

chilled margin is from this study; data for average flood basalt is from Naldrett (1981);

data for average East Bull Lake hydrothermal sulphide mineralization is from Peck et al.

(1993b). Mantle normalizing values are from Barnes et al. (1988) and McDonough and

Sun (1995).

195

5.7 Bell Lake Intrusion - Traverse

The Bell Lake intrusion is located in the northwest corner of Lorne Township, about

35 km southwest of the City of Greater Sudbury (Figs. 1-2 and 5-45). The sample suite

consists of 8 samples (JB98-145 to 151), collected along an ~425 m long traverse that

extends from the edge of Bell Lake northwest to within about 50 m of the CPR railway

tracks (Fig. 5-45). A summary of the samples is provided in Table 5-13 and a complete

listing of the data is provided in Appendix 1.


The Bell Lake intrusion is a relatively long body of Nipissing Gabbro that extends

for more than 10 km toward the southwest through Nairn Township (Ginn, 1965);

northwest-trending faults and Sudbury Dike Swarm dikes dissect the intrusion along its

length (Fig. 5-45). Ginn (1965) described the intrusion as a sill, emplaced concordantly

into Huronian sedimentary rocks. Although equivocal, current geochemical data suggests

that the lower portion of the sill is located to the south, along the north edge of Bell Lake.

The Bell Lake intrusion is sub-parallel to the Murray Fault Zone, which cuts off and

displaces the northeastern portion of the sill as it trends northeastward into Drury

Township. The Wright showing, from which several samples were collected, is located

about 3.75 km toward the southwest in Nairn Township, and is situated within the same

intrusion as the Bell Lake sample section (Fig. 1-2).

Locally, the Bell Lake section exposes gabbroic rocks, hosted by McKim Formation

argillite of the Elliot Lake Group (Fig. 5-45). Contacts between the Huronian sediments

and Nipissing Gabbro are not exposed in the immediate area of the section. From south

to north, the intrusive rocks comprise massive medium-grained quartz gabbro, collected

from within ~50 m of the southern contact, followed by massive fine- to medium-grained

orthopyroxene gabbro, and finally a homogenous unit of massive fine- to medium-

grained gabbro. The final samples along the section (JB98-151A and 151C) were

collected along a northwest ridge overlooking an old pit to the north that contains

sulphide mineralization in heavily gossaned Nipissing Gabbro (Photo 5-3); this pit was

sunk along the contact of the Nipissing Gabbro and Huronian sediments and is believed

to be the sulphide showing described by Ginn (1965) as Bell Lake Nickel - Prospect 8

which was discovered around 1891.

196

Figure 5-45. General geology and sample locations from the Bell Lake intrusion, Lorne

Township. Geology modified after Ginn (1965). Map coordinates are UTM, NAD27-

Zone17.

197

Sample JB98-151C was collected from the gabbro, very near the northern contact (not

exposed). Sample JB98-151A, collected from the same general area as JB98-151C was

described in the field as an altered fine-grained gabbro. In thin section, this sample

consists of an equigranular mosaic of ~45% fine-grained feldspar and quartz, and ~45%

chlorite, with chlorite also occurring as rare pseudomorphs after pyroxene, and ~5%

opaques (likely magnetite); several very fine grains of sulphide were noted.


JB98-151A altered gabbro 0.005 76 347 0.277 0.640 0.673 20.890 29.500JB98-151C GN (H-O) 0.005 19 264 0.841 1.940 1.410 11.690 7.090JB98-150 LG (Q-H) 0.005 44 293 1.146 2.540 1.540 13.260 6.120JB98-149 GN (H-O) 0.005 44 332 1.301 2.500 1.900 12.140 6.480JB98-148 LGN (H-O) 0.008 32 376 1.124 2.380 2.500 12.770 4.300JB98-147 MGN (H-O) 0.005 15 355 1.077 1.680 3.070 10.590 2.260JB98-146 GN (H-O) 0.018 114 188 0.101 0.580 0.530 4.820 6.450JB98-145 sediment 0.005 208 40 0.017 0.085 0.027 0.733 0.543Sample Au Cu S/Se Pd/Pt Cu/Ni Mg# ∑REE (La/Sm)N

ppb ppm ppmJB98-151A 16.700 19 658 1.4 0.1 69 7 5.10JB98-151C 1.430 39 2632 0.6 0.1 77 28 1.86JB98-150 0.645 30 1136 0.5 0.1 78 30 2.67JB98-149 0.763 16 1136 0.5 0.0 81 22 1.75JB98-148 1.060 33 2500 0.3 0.1 81 17 1.70JB98-147 0.730 6 3333 0.2 0.0 82 14 0.98JB98-146 1.540 55 1579 1.3 0.3 73 32 2.14JB98-145 1.380 26 240 0.7 0.7 53 102 3.00


Bell Lake intrusion, Lorne Township. "-" below lower limit of detection; "N" = primitive

mantle-normalized; G=gabbro; OLGN=olivine leucogabbronorite; LG=leucogabbro;

GN=gabbronorite; Q-H=quartz-hypersthene; H-O=hypersthene-olivine; Q-H-C=quartz-

hypersthene-corundum. Norm wt% = rock types determined on the basis of weight


198

On the basis of the hand sample description, its location in the section, the CIPW

normative calculation, and thin section information, this sample is interpreted to represent

an extensively altered fine-grained or chilled gabbro that likely contained pyroxene

(hypersthene?) phenocrysts.

Northeast and southwest from the sample section, there are several magmatic Cu-Ni

sulphide occurrences either entirely within the intrusion or at the contact between the

Nipissing Gabbro and hosting sedimentary rocks (Ginn, 1965). Several samples (JB97-

39A, 39B, 39C, 85A and JB98-117B, 117C) were collected from one of the Cu-Ni

showings in Nairn Township and these samples are included in the regional sample

database. Ginn (1965) also described Cu-Ni sulphide mineralization exposed in an old

pit, located northwest of Bell Lake and at the northwest end of the current sample section

(Fig. 5-45). Ginn (1965) described two pods of olivine diabase and mapped several areas

of olivine diabase within a Nipissing Gabbro sill that parallels the Bell Lake intrusion to

the southwest in Nairn Township.

The northwest region of Lorne Township including the area covered by the current

sample section, was the target of Tearlach Resources Inc. multi-year exploration

programs (2001 to 2003) aimed at delineating a newly recognized portion of the

Worthington Offset dike (Fig. 5-45). Ginn (1965) mapped the fragment-bearing quartz

diorite dike as part of the larger Nipissing Gabbro (Bell Lake intrusion) and surmised that

the Worthington Offset dike previously recognized by Card (1965) to the north in Drury

Township did not continue southward into Lorne Township. Exploration work by

Tearlach, traced the quartz diorite dike from the southwest, about 50 m northeast of the

old pit at the north end of the sample section, toward the northeast where it is cut off by

the Murray Fault (Butler, 2002). A further ~3 km to the east, the Worthington Offset dike

stricto sensu, terminated at its southern end by the Murray Fault, continues northeast

toward the Sudbury Igneous Complex. In the area of the Bell Lake section, the

Worthington Offset dike, which is associated with the magmatic events of Sudbury

Igneous Complex (~1.85 Ga), intruded McKim Formation sediments and is proximal

(~50 m) to the older Bell Lake Nipissing Gabbro intrusion.

199

Photo 5-3. Heavily gossaned Nipissing Gabbro from the northern part of the traverse

across the Bell Lake Intrusion, near sample site JB98-151. This sulphide showing is

described by Ginn (1965) as the Bell Lake Nickel prospect #8 (ca. 1891). The height of

the exposure is about 4 metres.

200

This is important in the context of the sample section, and in particular sample JB98-

151A, because emplacement of the offset dike may have altered the McKim Formation

sediments and/or the northern portion of the Bell Lake intrusion, overprinting earlier

features. Grab samples from the pit located at the northern end of the sample section

were reported by Butler (2002) to assay 0.74% Cu, 0.48% Ni, 0.04% Co, 0.15 g/t Pt and

0.04 g/t Pd (20% visible sulphide), and 0.04% Cu, 1.32% Ni, 0.135% Co, 0.19 g/t Pt and

0.19 g/t Pd (90% visible sulphide). Butler (2002) noted that although the Cu-Ni-Pt-Pd

concentrations are comparable to this portion of the Worthington Offset dike, Co

concentrations in Nipissing Gabbro are enriched by a factor of ~2-3.


CIPW normative calculations were completed on the six gabbroic samples collected

from the Bell Lake intrusion (Table 5-13). Of the six samples, three classify as

hypersthene-olivine-normative (silica-saturated) gabbronorite, one as quartz-hypersthene-

normative (silica-oversaturated) leucogabbro, one as hypersthene-olivine-normative

leucogabbronorite, and one as hypersthene-olivine-normative melagabbronorite. In the

field, the CIPW gabbronorite samples were described as gabbro and quartz gabbro, the

leucogabbro and leucogabbronorite samples were described as gabbro and the CIPW

melagabbronorite was described as orthopyroxene gabbro. CIPW normative calculations

on JB98-151A, show this sample to be olivine-hypersthene-corundum-normative (silica

saturated and peraluminous) with more than 30% normative olivine. The major element

chemistry of the Wright showing samples (JB98-117B and 117C), collected from the

southwest part of the intrusion in Nairn Township, are similar to those of the Bell Lake

intrusion (i.e. ~9.9-12.8 wt% MgO).

All of the gabbroic samples plot with higher Mg-number and lower TiO2

concentrations relative to average chilled margin gabbro (Fig. 5-46). Assuming that

average chilled margin is a good estimate of parent magma composition, it follows that

these rocks are either much more primitive (less fractionated) relative to “normal” or

average Nipissing Gabbro or that they contain a high percentage of orthopyroxene

phenocrysts and/or olivine (now altered). As with other relatively undifferentiated

intrusions that contain massive units of orthopyroxene gabbro, the rocks in the Bell Lake

section probably originally contained upwards of 10% hypersthene phenocrysts.

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JB98-151A (HW)JB98-151CJB98-150JB98-149JB98-148JB98-147JB98-146JB98-145 (FW)Chilled Margin Avg

fractionationg altered gabbro (chill)A melagabbronorite (CIPW)) gabbronorite (CIPW)# leucogabbro (CIPW)D leucogabbronorite (CIPW)

Figure 5-46. Bivariate scatter plot of samples from the Bell Lake intrusion using the



202

Therefore, these rocks that have higher than “normal” MgO compositions are interpreted

to represent hypersthene cumulates and therefore have compositions that, unlike the

chilled margin gabbro, do not represent liquids.

Whole-rock major element compositions show very little variation throughout the

section, averaging about 51.4 wt% SiO2, 16 wt% MgO, 0.35 wt% TiO2 and an Mg-

number of ~79. A very subtle decrease in Mg-number and an increase in TiO2 suggests

that the lower portion of the intrusion is located to the south, along the north edge of Bell

Lake. Sample JB98-151A, an altered chilled gabbro from the northernmost part of the

section, is characterized by low SiO2 (~40 wt%), relatively low TiO2 (~0.1 wt%) and very

high Al2O3 (~24 wt%) which is contrasted by the footwall sediment whose composition

is ~76 wt% SiO2, 0.35 wt% TiO2, and 11.23 wt% Al2O3; loss on ignition for JB98-151A

is ~7 wt%.


Primitive mantle-normalized multi-element diagrams for the Bell Lake section are

shown in Figure 5-47. The gabbroic samples show similar overall trace and rare-earth

element abundances (~1 to 40 times primitive mantle) with moderate LILE enrichment

(~1-50 times primitive mantle), average of ~1.9 (La/Sm)N, and weakly enriched HREE

(~1-3 times primitive mantle); these values are generally lower in comparison to other

Nipissing Gabbro intrusion (e.g. Lightfoot and Naldrett, 1996). As is typical of Nipissing

Gabbro, all of the gabbroic samples display strong negative Nb+Ta and P* anomalies,

and moderate Ti* anomalies, which are features characteristic of magma interacting with

a crustal component. Sample JB98-151A plots well below the range for typical Nipissing

Gabbro, and relative to average chilled gabbro displays pronounced negative Th, Nb, La

and Ce anomalies, a strong positive Sr anomaly, and a weakly positive Ti* anomaly. The

ratio of La/Ce is an important indicator of alteration in volcanic systems (e.g. Wyman,

1996) whereby higher La/Ce ratios suggest increased alteration. Sample JB98-151A has

a higher ratio of (La/Ce)N (~1.42) relative to average gabbroic samples (~1.2) which

suggests that this sample has experienced extensive alteration.

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JB98-150

JB98-149

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JB98-147

JB98-146

Chilled Margin Avg

A melagabbronorite (CIPW)) gabbronorite (CIPW)# leucogabbro (CIPW)D leucogabbronorite (CIPW)

(A)

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JB98-145 (FW)

Chilled Margin Avg

(B)

g altered gabbro (chill)+ sediment

Figure 5-47. Primitive mantle-normalized multi-element diagrams for rock samples from the Bell Lake intrusion, Lorne Township. (A) Gabbroic samples. (B) Atypical profiles. Mantle normalizing values are from McDonough and Sun (1995).

204


None of the samples analyzed have any visible sulphide and moreover, 4 of the 6

gabbroic samples analyzed are below the lower limit of detection for S (generally 0.01

wt% S); in cases where S values are below the lower limit of detection (LLD), a value

equal to 0.5 x LLD is used, and in this case it is 0.005 wt% S. The 6 gabbroic samples

are characterized by averages of ~301 ppm Ni, ~30 ppm Cu, 0.93 ppb Ir, 1.94 ppb Ru,

1.83 ppb Rh, 10.88 ppb Pt, 5.45 ppb Pd, and 1.03 ppb Au. The highest concentration of

Pt+Pd (~21 ppb Pt+Pd; 1.4 Pd/Pt; 0.05 Cu/Ni) is from the uppermost sample (JB98-

151A), which is thought to be an altered and recrystallized gabbro.


the intrusion in Figure 5-48. Concentrations of Se are highest in the lowermost quartz

gabbro and uppermost altered gabbro, lowest in the uppermost gabbro unit, and shows a

progressive increase through the middle region of the intrusion. The ratio of S/Se

increases rapidly through the lowermost quartz gabbro and subsequent orthopyroxene

gabbro, then drops sharply through he middle of the intrusion, before rising again in the

upper gabbro unit and finally dropping off in the uppermost altered gabbro. With the

exception of the uppermost (JB98-151A) and lowermost (JB98-145) samples, all of the

rocks have S/Se ratios that fall within the range of uncontaminated magmatic sulphide

(Naldrett, 1981). Samples JB98-151A and JB98-145 have S/Se values that are <1000

which is indicative of S loss (Reeves and Keays, 1995). Given that almost all of the S

analyses were below the LLD it is possible that S loss affected other samples.

Concentrations of Pt and Pd display a general increase through the intrusion ranging

from ~11 ppb Pt+Pd at the base to a maximum of ~21 ppb Pt+Pd in the uppermost altered

gabbro. The ratio of Pd/Pt is highest in the lowermost quartz gabbro, dropping quickly in

the orthopyroxene gabbro, and then increasing steadily into the upper altered gabbro;

Pd/Ir ratios are highest in the lowermost quartz gabbro and uppermost altered gabbro.

The Cu/Pd ratio displays a general decrease upward through the intrusion, from 8527 in

the lower quartz gabbro to 644 in the upper altered gabbro. Plots of Pt/Se and Pd/Se (Se

was used in place of S as sulphur loss was suspected) exhibit a gradual increase from the

quartz gabbro to the overlying orthopyroxene unit, followed by a gradual increase

through to the uppermost gabbro.

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Concentration and Ratio

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gabbro (GN)

gabbro (LG)

sediment

quartz gabbro (GN)

SOUTH

NORTH

gabbro (GN)

gabbro (LGN)

altered gabbro (chill)

(A)

Pt+Pd (ppb) Cu (ppm) Ni (ppm) S (ppb)Cu/PdS/Se

Figure 5-48a. Profiles through the Bell Lake intrusion sample section, showing

stratigraphic variations in Pt+Pd, Cu, Ni, S/Se, Cu/Pd, and S. The relative vertical scale is

in metres.

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SOUTH

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gabbro (GN)

gabbro (LGN)

altered gabbro (chill)

(B)

Pd/SePt/Se

Cu/Ni Pd/Pt

Figure 5-48b. Profiles through the Bell Lake intrusion sample section, showing

stratigraphic variations in Pd/Se, Pt/Se, Cu/Ni, and Pd/Pt. The relative vertical scale is in

metres.

207

The ratios are nearly identical in the lower quartz gabbro but quickly decouple through

the main body of the intrusion, reflecting high Pt/Pd ratios, followed by a reversal to

higher Pd/Pt in the upper altered gabbro. Concentrations of Ni are relatively steady

throughout the intrusion showing a subtle decrease upward from the orthopyroxene

gabbro to the upper gabbro unit, followed by a slight rise in the uppermost altered

gabbro.

Primitive mantle-normalized PGE and chalcophile element diagrams, with metals

recalculated to 100% sulphide, are shown in Figure 5-49. Three distinct groups are

apparent from this plot; Group-1, comprising the lowermost quartz gabbro (JB98-146),

shows a fractionated, positive slope profile (Fig. 5-49a); Group-2, comprising 5 gabbroic

samples, have elevated Ni, Ir, Ru, Rh and Pt and display only slight positive slopes in Ni-

Ir-Ru-Rh, followed by near-flat to slightly negative slopes in Pt-Pd-Au-Cu (Fig. 5-49a);

Group-3, consists of a sample of altered chilled margin gabbro (JB98-151A) and exhibits

a fractionated, positive slope from Ir through to Au, and a strong negative slope from Au

to Cu. The Group-1 data show typical Nipissing Gabbro fractionation patterns with early

crystallization of olivine and/or oxide and/or monosulphide solid solution (mss) having

depleted the magma in Ni-Ir-Ru-Rh, leaving relatively elevated Pt-Pd-Au-Cu. This

pattern approximates that of average chilled margin and average continental flood basalt.

The Group-3 patterns are very unusual for Nipissing Gabbro and resemble those of near-

mantle or primary partial melts such as the lower group chromitites of the Bushveld

Complex (e.g. Maier et al., 1998). The elevated Ni-Ir-Ru-Rh values reflect the primitive

chemistry of these rocks which have very high MgO compositions (range ~14.4-19.4

wt% MgO) relative to other Nipissing Gabbro (cf. Lightfoot and Naldrett, 1996). This

elevated pattern may also reflect the mineral chemistry of these samples, with the

majority (4 of 5) having >3% normative olivine. As discussed earlier (see Section 5.2.3),

the ratio of Pd/Ir is important in estimating the degree of fractionation in a magma. The

fact that the Group-2 samples have PGE patterns that plot with much lower relative Pd/Ir

values to that of continental flood basalt and typical Nipissing Gabbro, indicates that

these rocks formed from magmas that were not as fractionated as those from average

continental flood basalt.

208

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JB98-151C

JB98-150

JB98-149

JB98-148

JB98-147

JB98-146

Chilled Margin Avg

Flood Basalt Avg

Group-1

Group-2

A melagabbronorite (CIPW)) gabbronorite (CIPW)# leucogabbro (CIPW)D leucogabbronorite (CIPW)

(A)

Figure 5-49a. Primitive mantle-normalized PGE-chalcophile element diagrams

(recalculated to metals in 100% sulphide) for Group-1 and Group-2 sulphides from the

Bell Lake intrusion sample section, Lorne Township. Data for average chilled margin is

from this study; data for average flood basalt is from Naldrett (1981). Mantle


209

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ulph

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JB98-151A (HW)

JB98-145 (FW)

Chilled Margin Avg

Flood Basalt Avg

g altered gabbro (chill)

(B)

Group-3

Group-1


(recalculated to metals in 100% sulphide) for Group-3 sulphides from the Bell Lake

intrusion sample section, Lorne Township. Sample JB98-145 shares similarities to

Group-1 sulphides. Data for average chilled margin is from this study; data for average

flood basalt is from Naldrett (1981). Mantle normalizing values are from Barnes et al.

(1988) and McDonough and Sun (1995).

210

The Group-3 profile is similar to that of Group-1 but with elevated overall PGE

abundance, suggesting further fractionation relative to Group-1; elevated Ni-Ir-Ru-Rh

also reflects the primitive nature of this sample (~11 wt% MgO).

For comparison, 5 of the samples (JB97-39A, 39B, 39C, 85A) collected from the

Wright showing in Nairn Township are considered. These samples, considered to be

from the same intrusion as the Bell Lake section, are characterized by relatively high S

(1.3-15.7 wt%), Ni (1202-13000 ppm) and Cu (650-27583 ppm) concentrations and

anomalous Pt (30.3-218.1 ppb) and Pd (21.4-122.6 ppb) concentrations. In terms of S/Se

ratios, samples with semi-massive to massive sulphide (7.63-15.70 wt% S) show

contamination signatures (11,787-2,461,290 S/Se) whereas samples (JB97-85A and

JB98-117B) with disseminated textured sulphide (1.3-9.4 wt% S) show magmatic

signatures (2369-4134 S/Se). The chondrite-normalized Pd/Ir ratios for samples from the

Nairn site (Fig. 5-2.15a) are similar to those from the Bell Lake sample section (Fig. 5-

49).

5.8 Makada Lake Intrusion – Traverse

The Makada Lake Intrusion, located about 15 km southwest of the City of Greater

Sudbury in the central part of Waters Township, extends for about 5 km in a southwest

direction (~55 Az) along the northwest shore of Makada Lake (Figs. 1-2 and 5-50). The

sample section, which is about 500 m wide, extends north from the northwest shore of

Makada Lake to the northern contact of the intrusion, exposing gabbroic rocks and the

footwall and hangingwall Huronian sedimentary rocks. A total of 22 samples were

collected to construct a lithostratigraphic section through the intrusion, along with an

additional five grab samples collected from various sulphide showings (Fig. 5-51). A

summary of the samples is provided in Table 5-14 and a complete listing of the data is



The Makada Lake intrusion is located about 3.7 km south of the Murray Fault Zone

(Fig. 5-50) and Card (1968) interpreted this and other Nipissing Gabbro bodies in the

region to be sill-like and generally paralleling regional structural trends. Several 050 Az

tight folds occur in the region with anticline and synclines axes traces generally separated

by ~500-1000 m and on the basis of mapping by Card (1968), the Makada Lake sill

211

appears to have intruded folded Huronian sediments and is now, for the most part,

conformable to bedding (Fig. 5-50; Photo 4-2). Faults on the property are generally

oriented at 290-300 Az and 330-350 Az (Fig. 5-51) and are interpreted to have a

dominantly dip-slip component.

Figure 5-50. General geology and location of the sample section for the Makada Lake

intrusion, Waters Township. Geology after Card (1968).

212

Figure 5-51. General geology and locations of samples collected from the Rauhala

property, Makada Lake intrusion, Waters Township.

213


JB97-78A OGN (H-O-C) 0.170 309 94 - - 0.820 5.000 10.410JB97-78B aplite 0.600 1122 68 - - - - 7.480JB97-76A G (Q-H) 0.150 228 170 - - 1.100 9.560 13.450JB97-76B GN (H-O) 0.800 1134 210 - - 0.570 5.460 5.370JB97-77A LGN (H-O) 0.190 321 85 na na na na naJB97-77B GN (H-O) 0.850 1563 190 - - 0.670 9.280 15.170

RK-14 GN (H-O) 0.019 78 138 0.050 0.420 0.520 6.300 8.930RK-19 LGN (H-O) 0.014 85 117 - 0.330 0.410 4.640 5.860RK-13 G (Q-H) 0.021 84 137 0.060 0.350 0.510 6.220 7.800RK-18 LGN (H-O) 0.011 58 342 1.340 2.710 1.800 11.370 5.820

JB97-75 LG (Q-H) 0.030 281 53 - - - - -RK-5 LG (Q-H) 0.038 219 67 - - - 0.200 -RK-2 OGN (H-O) 0.011 35 214 0.220 1.050 1.480 6.240 4.180

JB97-4B G (Q-H) 0.020 101 220 0.302 1.118 0.801 5.851 11.549RK-12 G (Q-H) 0.014 64 327 1.040 2.460 1.540 9.190 5.300RK-7 GN (H-O) 0.013 74 248 0.550 1.410 1.230 7.350 6.360

RK-11 G (Q-H) 0.023 73 346 1.090 2.580 1.840 9.960 5.530JB97-79B G (Q-H) 0.010 73 212 - - - 5.050 10.320

RK-8 GN (H-O) 0.018 87 259 0.570 1.450 1.120 7.630 6.590RK-9 GN (H-O) 0.014 65 338 1.050 2.590 1.590 9.270 5.380

RK-10 GN (H-O) 0.012 61 335 1.100 2.630 1.850 11.060 5.640JB98-114 GN (H-O) 0.014 57 311 0.392 1.250 0.873 5.470 6.070JB98-165 leucogabbro 14.500 80 3062 0.744 1.830 5.020 18.770 30.500JB97-74A gabbro 1.050 1455 210 - - - - 10.430

RK-1 G (Q-H) 0.712 810 500 0.290 0.910 0.880 7.240 9.600RK-3 gabbro 1.410 1292 679 0.460 1.330 1.300 10.700 12.590RK-4 gabbro 36.300 41 10490 - - - - 1.490


Makada Lake intrusion, Waters Township. "-" below lower limit of detection; "N" =

primitive mantle-normalized; "na"=not analyzed; G=gabbro; OLGN=olivine

leucogabbronorite; LG=leucogabbro; GN=gabbronorite; OGN=olivine gabbronorite;

LGN=leucogabbronorite; Q-H=quartz-hypersthene; H-O=hypersthene-olivine; Q-H-

C=quartz-hypersthene-corundum; H-O-C=hypersthene-olivine-corundum.

214


ppb ppm ppmJB97-78A 2.040 82 5502 2.1 0.9 58 64 3.17JB97-78B 3.540 390 5348 - 5.7 46 30 1.58JB97-76A 5.870 45 6579 1.4 0.3 71 41 1.77JB97-76B 3.220 220 7055 1.0 1.0 66 48 0.87JB97-77A na 150 5919 - 1.8 55 60 2.02JB97-77B 288.750 880 5438 1.6 4.6 53 65 1.45

RK-14 1.670 66 2436 1.4 0.5 69 33 2.26RK-19 1.030 60 1647 1.3 0.5 67 33 2.32RK-13 1.230 61 2500 1.3 0.4 68 33 2.19RK-18 1.200 50 1897 0.5 0.1 79 23 1.78

JB97-75 - 112 1068 - 2.1 34 156 2.49RK-5 3.480 136 1735 - 2.0 44 115 2.31RK-2 2.090 14 3143 0.7 0.1 75 23 2.48

JB97-4B 3.689 93 1980 2.0 0.4 72 30 1.90RK-12 1.370 45 2188 0.6 0.1 78 24 1.83RK-7 1.820 71 1757 0.9 0.3 76 27 1.90

RK-11 1.370 50 3151 0.6 0.1 79 22 1.84JB97-79B - 53 1370 2.0 0.3 74 25 1.76

RK-8 1.490 73 2069 0.9 0.3 76 29 2.09RK-9 1.300 46 2154 0.6 0.1 79 24 1.76

RK-10 1.210 46 1967 0.5 0.1 79 24 1.79JB98-114 2.430 37 2456 1.1 0.1 78 19 1.48JB98-165 238.000 1702 1812500 1.6 0.6 29 44 3.90JB97-74A 5.770 278 7216 - 1.3 54 25 3.94

RK-1 8.170 181 8790 1.3 0.4 76 34 2.42RK-3 16.700 349 10913 1.2 0.5 75 26 1.95RK-4 1.720 645 8853659 - 0.1 1 1 3.88

Table 5-14(cont). Summary of whole-rock geochemical characteristics for samples from

the Makada Lake intrusion, Waters Township. "-" below lower limit of detection; "N" =


leucogabbronorite; LG=leucogabbro; GN=gabbronorite; OGN=olivine gabbronorite;

LGN=leucogabbronorite; Q-H=quartz-hypersthene; H-O=hypersthene-olivine; Q-H-

C=quartz-hypersthene-corundum; H-O-C=hypersthene-olivine-corundum.

215

The Makada Lake intrusion is hosted by sulphide-bearing (maximum of ~1% pyrite and

rare chalcopyrite) feldspathic quartzite, arenite and arkose of the Mississagi Formation

(upper Hough Lake Group), cut by magnetite-olivine gabbro of the Sudbury Dike Swarm

(oriented at ~300/90 Az), and cut by mafic, fragment-bearing dikes (oriented at ~80/90

Az) that may be related to the Sudbury Igneous Complex.

The northern contact of the Makada Lake intrusion is not exposed but the southern

contact of the intrusion (Photo 4-2), where exposed, is sharp against the sediments,

marked by fine-grained to chilled gabbroic rocks over widths of about 1 metre; the

sedimentary rocks are locally sheared along the contact region. From south to north, the

sample suite consists of medium-grained orthopyroxene gabbro which is gradational into

a dominantly gabbro unit with subordinate orthopyroxene gabbro, followed by vari-

textured gabbro and gabbro. Granophyric gabbro with aplite dikes and felsic

differentiates occur mainly in the southern area of the section (Fig. 5-51).

The Makada Lake Intrusion is interpreted to represent an upper limb or near-arch

portion of an undulatory sill (Fig. 5-52), and as with other exposures of Nipissing

Gabbro, topography plays a role in terms of exposing various levels of stratigraphy. In

this case, elevation ranges from about 240 m ASL in the north (area of JB97-114),

cresting at about 290 m ASL in the southern half of the section (area of JB97-75), and

then dropping off along the northwest shore of Makada Lake to about 250 m ASL in the

area of the sediment-gabbro contact (JB97-78A,B). A consequence of this gradual rise

and variation in topography from north to south is the exposure of deeper parts of the sill

in the north and higher parts of the sill in the middle and southern areas. For example,

gabbro pegmatite (Photo 4-11), granophyric rocks, aplitic pods, and sedimentary

fragments in gabbro (Photo 5-4a) occur in the middle region of the traverse (Fig. 5-51;

area of Pit #2, #3 and #4), enveloped by massive mafic gabbros north and south from this

region. The stratigraphic location of these mineralized exploration pits and field

evidence for extensive hydrothermal alteration and/or magmatic fluid accumulation (i.e.

pegmatitic textures) in this area, suggests that these pits were proximal to the now eroded

sedimentary roof rocks of the intrusion.

The Makada Lake intrusion is host to several Ni-Cu-PGE sulphide occurrences as

well as several showings of polymetallic Au-Ag-Co-Cu-Ni veins.

216

Figure 5-52. Schematic diagram showing the interpreted structure of the Makada Lake

intrusion, Waters Township. NG=Nipissing Gabbro; opxG=orthopyroxene gabbro;

G=gabbro; vtG=vari-textured gabbro; GG=granophyric gabbro; AP=aplite; FD=felsic

differentiate. The cross section is based on the undulatory model for Nipissing Gabbro

intrusions (Hriskevich, 1968).

217

All of these sulphide occurrences are found within the present study area which is

colloquially referred to as the Rauhala property. The majority of Cu-Ni sulphide

mineralization occurs within the middle region of the sample section where it is exposed

in 3 exploration pits – Pit #2, #3 and #4 (Fig. 5-51). At these locations, sulphides occur

as semi-massive to massive accumulations which appear to be localized into lenses or

pods of limited strike extent; blue quartz “eye”–bearing gabbro is relatively common in

this central area and is commonly directly associated with higher percentages of sulphide

mineralization. Massive and semi-massive sulphide mineralization is dominated by

pyrrhotite, but disseminated chalcopyrite and/or pyrrhotite is relatively common

throughout the Nipissing Gabbro units. Disseminated sulphides (Photo 5-4b), dominated

by pyrrhotite with subordinate chalcopyrite, occur in the gabbroic host rocks, resulting in

a several metre wide mineralized halo, northwest and southeast of the pit area. Up-

section or southward from the pits, toward Makada Lake, sulphide mineralization is

patchy.

Pit #1 consists of highly altered fine-grained gabbro with sediment fragments and

quartz (+/- carbonate) veining, and is located near the contact with quartz arenite; the

sediment is likely a roof pendant or block derived from the now eroded hangingwall

sedimentary rocks; polymetallic veins containing anomalous Ag-Ni-Co-As-Au occur in

this area. Exploration pits Pit #2, Pit #3 and Pit #4, lie along a 060-240 Az trend, located

about 70 m northwest of the highest ridge along the section (Fig. 5-51). Pit #2 contains a

several “boulder” like outcrops of gossanous massive sulphide that are exposed in an ~5

x 5 m sandy and sulphur-rich pit; sulphides are mainly pyrrhotite with subordinate

chalcopyrite. The highest concentrations of Pt+Pd are from samples JB98-165 (~49 ppb

Pt+Pd; 1.6 Pd/Pt; 0.6 Cu/Ni; 0.31% Ni, 0.17% Cu) and RK-3 (~23 ppb Pt+Pd; 1.2 Pd/Pt;

0.5 Cu/Ni), collected from the massive sulphide in Pit #2. Samples RK-1, 3 and 4 were

also collected from Pit #2, with RK-4 assaying 1.05% Ni and 0.07% Cu. Pit #3 contains

numerous rock types arranged in a complicated and highly altered assemblage, including

pegmatitic “golf ball” gabbro, vari-textured gabbro, aplite, sediment, granophyric gabbro

and quartz-bearing gabbro.

218

Photo 5-4. Makada Lake Intrusion. (A) Fragments of Huronian Supergroup sedimentary rocks in fine- to medium-grained gabbro of the Makada Lake Intrusion. The fragments are thought to have been stoped from what was overlying sedimentary roof rocks. The hammer handle is about 90 cm long. (B) Extensively altered gabbro with fine-grained blue quartz and finely disseminated sulphide (ds), dominated by pyrrhotite with subordinate chalcopyrite; sample is from exploration Pit#2 (Figure 5-51). The pen magnet is about 9 cm long.

219

Fine-grained, acicular amphibole and other hydrous phases are common, and together

with other fractionated rock types, and a high degree of alteration, suggests a highly

fluidized system – likely a combination of late magmatic fluids and post-magmatic

hydrothermal fluids. Mineralization consists mainly of finely disseminated pyrrhotite,

pyrite and chalcopyrite as well as fracture and vein-controlled sulphide and localized (cm

wide and cm long) veins of semi-massive pyrrhotite + pyrite > chalcopyrite. Sample

JB97-4B, collected from the northern edge of the pit, assayed 220 ppm Ni, 93 ppm Cu,

5.9 ppb Pt, 11.6 ppb Pd, and 3.7 ppb Au. Pit #4 consists of sedimentary rock fragments

within medium-grained gabbro. It is not clear whether these are fragments of sediment

that have been incorporated into the gabbro during emplacement of if they represent

remnants of the now eroded overlying Huronian sediments. Mineralization is mainly

finely disseminated to locally bleb pyrrhotite, pyrite and chalcopyrite. The gabbroic

rocks have been recrystallized and thoroughly altered along with the sedimentary rocks.

Sample JB97-74A, collected from the edge of this pit, assayed 210 ppm Ni and 278 ppm

Cu and has anomalous PGE. The third highest Pt+Pd concentration is from JB97-77B

(~25 ppb Pt+Pd; 1.6 Pd/Pt, 4.6 Cu/Ni), collected from the southern area of the section.

A diamond drill hole (A1-97), targeting the mineralization under the western edge of

Pit #2 (Fig. 5-51), intersected gabbro over its entire length (~55 m) with one section from

~34 m to 54 m that consisted of ~10% disseminated chalcopyrite and pyrrhotite in an

altered, biotite- and blue quartz-bearing, medium-grained, gabbro; details of this drill

hole are discussed in Section 5.9.


CIPW normative calculations were completed on the 22 of the section samples and

one of the mineralized grab samples (Table 5-14; Appendix 1). Eight of the samples,

classifying as hypersthene-olivine-normative (silica-saturated) gabbronorites, are the

dominant rock type in the northern part of the section and correlate well with

orthopyroxene gabbro. One sample of orthopyroxene gabbro classified as a hypersthene-

olivine-normative, olivine gabbronorite. Six of the samples, classifying as quartz-

hypersthene-normative (silica-oversaturated), correlate with gabbro from the northern

part of the section and two samples of vari-textured gabbro from the south. CIPW

normative calculations for five samples of leucogabbro and vari-textured gabbro,

220

collected from the southern half of the section, result in hypersthene-olivine-normative

leucogabbronorites and quartz-hypersthene-normative leucogabbros.

A plot of Mg-number versus TiO2, useful to determine fractionation patterns, is

provided in Figure 5-53. From north to south, the samples show a reasonably regular

fractionation trend with higher MgO and lower TiO2 rocks from the north and lower

MgO and slightly higher TiO2 in rocks from the south. This trend, along with the

prevalence of orthopyroxene gabbro in the north part of the section, suggests that the

basal or lower portion of the sill is toward the north and that the upper portion of the sill

is toward the south. All but 6 of the samples plot with significantly higher Mg-numbers

and slightly lower TiO2 values relative to average chilled margin. This reflects the high

proportion of orthopyroxene phenocrysts in these rocks and the fact that these rocks are

cumulates, not liquids. Concentrations of MgO in the lowermost 10 samples (northern

part of section) range 10.7 to 17.35 wt% MgO which is very high for Nipissing Gabbro.

For comparison, Lightfoot and Naldrett (1996) reported 8.1 wt% MgO for average

gabbro (21 different intrusions) and 8.8 wt% MgO for average chilled margin (seven

different intrusion).

Variations in selected major elements across the intrusion, using relative distance

from north to south, are provided in Figure 5-54. The concentration of SiO2 shows a very

general increase, except within the upper aplite/differentiate, where it spikes to over 70

wt%, and in the upper granophyric gabbro where it drops to ~48 wt%. Concentrations of

TiO2 exhibit a general increase upward (from north to south) through the intrusion with

several spikes in the upper vari-textured gabbro dominated units. Sample JB97-75

records the highest TiO2 concentration, is located at the highest elevation on the section

and is described as a coarse-grained to pegmatitic gabbro pod. Assuming that the highest

elevation on the section would have been closest to the now eroded hangingwall

sediments, then elevated TiO2 could reflect local contamination from roof rocks and/or an

accumulation of late differentiated (TiO2 enriched) magma toward the roof. Decreasing

Mg-number, characteristic of normal magma differentiation, is evident from north to

south through the intrusion with most of the highest Mg-numbers correlating with the

lowermost orthopyroxene gabbro (CIPW gabbronorite); the lowest Mg-number is from

sample JB97-75.

221

0.0

0.5

1.0

1.5

2.0

2.5

3.0

3.5

4.0

30405060708090

Mg-number

TiO

2 (w

t%)

JB97-78AJB97-78BJB97-76AJB97-76BJB97-77AJB97-77BRK-14RK-19RK-13RK-18JB97-75RK-5RK-2JB97-4BRK-12RK-7RK-11JB97-79BRK-8RK-9RK-10JB98-114Chilled Margin AvgHuronian Sediment Avg

fractionation

g differentiate(?)/aplite(?)A gabbro (CIPW)) gabbronorite (CIPW)B olivine gabbronorite (CIPW)# leucogabbro (CIPW)D leucogabbronorite (CIPW)

gabbro pegmatite pod

Figure 5-53. Bivariate scatter plot of samples from the Makada Lake intrusion using the



222

0

50

100

150

200

250

300

350

400

450

500

30 40 50 60 70 80 90

SiO2 (wt%) and Mg-number

Rel

ativ

e D

ista

nce

(not

to sc

ale)

sediment

granophyric gabbro (OGN)

sediment NORTH

SOUTH

vt gabbro (G)

gabbro (GN)

aplite/differentiate

vt gabbro (GN)

vt gabbro (LGN)

opx gabbro (GN)

gabbro (G)

vt gabbro (LG)

gabbro (GN)

opx gabbro (OGN)

gabbro (LG)

(A)

Mg-numberSiO2

Figure 5-54a. Profiles through the Makada Lake intrusion showing stratigraphic


223

0

50

100

150

200

250

300

350

400

450

500

0.1 1.0 10.0

TiO2 (wt%)

Rel

ativ

e D

ista

nce

(not

to sc

ale)

sediment


sediment NORTH

SOUTH

vt gabbro (G)

gabbro (GN)


vt gabbro (GN)

vt gabbro (LGN)

opx gabbro (GN)

gabbro (G)

vt gabbro (LG)

gabbro (GN)

opx gabbro (OGN)

gabbro (LG)

(B)

Figure 5-54b. Profiles through the Makada Lake intrusion showing stratigraphic


224


Primitive mantle-normalized multi-element diagrams are shown in Figure 5-55.

With the exception of the two CIPW leucogabbro samples (JB97-75 and RK-5), the

gabbroic samples show near-parallel patterns with strong LILE enrichment, follow

closely the pattern of average chilled margin, and have moderate to pronounced negative

Nb+Ta and P* anomalies and moderate to weak Ti* anomalies; features which are typical

of Nipissing Gabbro magmas. Most of the samples with the highest concentrations of S

and visible sulphide, also display the most erratic and varying trace and REE patterns,

suggesting extensive re-mobilization as a result of secondary (post magmatic) processes

such as hydrothermal alteration.


As described earlier, the majority of PGE-Cu-Ni sulphide mineralization occurs

within the middle region of the sample section where it is exposed in three exploration

pits – Pit #2, #3 and #4 (Fig. 5-51). Smaller sulphide showings, commonly hosted by

gabbro-sediment “breccias”, are scattered throughout the southern area of the sample

section. Selected chalcophile elements and their ratios are plotted against the relative

distance through the intrusion, from north to south (Fig. 5-56). There are two

pronounced deflections in the general trends; one is located at ~265 m (between samples

RK-2 and RK-5), corresponding to a change from CIPW gabbronorite (orthopyroxene

gabbro and gabbro) dominated rocks to vari-textured gabbroic rocks; and, a second break

at ~400 m (between samples RK-14 and JB87-77B), which corresponds to samples that

have higher S concentrations and evidence for alteration and contamination from trace

and rare-earth elements. These breaks are best discerned in plots of S, Se, Pt+Pd, Pd/Pt

and Pt/Se-Pd/Se. The prominent drop in Pt+Pd at ~265 m corresponds with a spike in S

concentration, a signature of S-saturation that has been reported from numerous

intrusions (e.g. Reeves and Keays, 1985), and the distinct shift in Cu/Pd values at this

same stratigraphic height (~265 m) suggests that the magma had precipitated sulphide at

this stratigraphic level. In the field, the break at ~265 m (between RK-2 and RK-5)

occurs a few metres south (up-section) of the sulphide mineralized exploration pits.

225

0.1

1

10

100

1000


Sam

ple/

Prim

itive

Man

tle

RK-14RK-19RK-13RK-18JB97-75RK-5RK-2JB97-4BRK-12RK-7RK-11JB97-79BRK-8RK-9RK-10JB98-114Chilled Margin Avg

A gabbro (CIPW)) gabbronorite (CIPW)B olivine gabbronorite (CIPW)# leucogabbro (CIPW)D leucogabbronorite (CIPW)

(B)

0.1

1

10

100

1000


Sam

ple/

Prim

itive

Man

tle

JB97-78A

JB97-78B

JB97-76A

JB97-76B

JB97-77A

JB97-77B

Chilled Margin Avg

(>0.1 wt% S)

g differentiate(?)/aplite(?)A gabbro (CIPW)) gabbronorite (CIPW)B olivine gabbronorite (CIPW)D leucogabbronorite (CIPW)

(C)

Figure 5-55. Primitive mantle-normalized multi-element diagrams for rock samples from the Makada Lake intrusion, Waters Township. (A) Gabbroic samples. (B) Atypical profiles. Mantle normalizing values are from McDonough and Sun (1995).

226

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350

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500

1 10 100 1000 10000 100000 1000000 10000000


Rel

ativ

e D

ista

nce

(not

to sc

ale)

sediment


sediment NORTH

SOUTH

vt gabbro (G)

gabbro (GN)


vt gabbro (GN)

vt gabbro (LGN)

opx gabbro (GN)

gabbro (G)

vt gabbro (LG)

gabbro (GN)

opx gabbro (OGN)

gabbro (LG)

(A)

S (ppb)Pt+Pd (ppb) Cu/PdS/SeNi (ppm)

Cu (ppm)

Figure 5-56a. Profiles through the Makada Lake intrusion sample section, showing

stratigraphic variations in Pt+Pd, Cu, Ni, S/Se, Cu/Pd and S. The relative vertical scale is

in metres.

227

0

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150

200

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300

350

400

450

500

0.0001 0.001 0.01 0.1 1 10

Ratio

Rel

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e D

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nce

(not

to sc

ale)

Pd/Se

Pt/Se

sediment


sediment NORTH

SOUTH

vt gabbro (G)

gabbro (GN)


vt gabbro (GN)

vt gabbro (LGN)

opx gabbro (GN)

gabbro (G)

vt gabbro (LG)

gabbro (GN)

opx gabbro (OGN)

gabbro (LG)

(B)

Cu/Ni Pd/Pt

Figure 5-56b. Profiles through the Makada Lake intrusion sample section, showing

stratigraphic variations in Pd/Se, Pt/Se, Cu/Ni, and Pd/Pt. The relative vertical scale is in

metres.

228

At about 400 m, the values of S/Se increase to >5000 whereas, in contrast, the

samples from the lower two-thirds of the section have S/Se values that are within the

range (1000 to 5000) of uncontaminated magmatic sulphides (Naldrett, 1981).

Coincident with this sudden increase in S/Se at ~400 m is an increase in Cu/Pd and S

(Fig. 5-56). These corresponding increases indicate that sulphide segregation occurred at

~400 m. This sudden increase could be explained by the introduction of external S into

the magma, which would have increased the S/Se values. Alternatively, the segregation

of sulphides may have preferentially removed Se relative to Cu (Se and Cu have similar

partition coefficients), leading to elevated S/Se ratios. In the plots of Pd/Ir and Cu/Ni, the

uppermost samples have elevated values relative to the lower samples, suggesting that

hydrothermal processes were involved in the development of the upper sample sulphides

(Keays et al., 1982).


metals in 100% sulphide) are shown in Figure 5-57. Two distinct groups are apparent

from these plots; Group-1, comprising samples RK-2, 13, 14, 19, JB97-4B and JB98-114,

displays positive slopes that are similar to those of average continental flood basalt and

average chilled margin gabbro; and, Group-2, comprising samples RK-7, 8, 9, 10, 11, 12

and 18, has positive slopes but with pronounced elevation in concentrations of Ni-Ir-Ru-

Rh-Pt relative to average flood basalt and average chilled margin gabbro. Group-1

samples (Fig. 5-57b), collected from sites across the width of the intrusion, show typical

Nipissing gabbro fractionation patterns and correlate mainly with CIPW gabbro and

gabbronorite. Group-2 samples (Fig. 5-57c), collected from sites located mainly in the

northern (lower) parts of the section, have MgO compositions (i.e. ~12-17 wt% MgO)

that are unusually high relative to other Nipissing Gabbro (cf. Lightfoot and Naldrett,

1996), and as seen elsewhere in this study, probably reflect a high proportion of

orthopyroxene phenocrysts and/or olivine. Moreover, as seen in samples from the Bell

Lake section and Nairn location, these PGE patterns, with much lower Pd/Ir values to that

of continental flood basalt, indicate that these rocks formed from magmas that were not

as fractionated as those which formed average continental flood basalt.

229

1

10

100

1000

10000

100000


Met

al in

100

% S

ulph

ide/

Prim

itive

Man

tle

RK-14

RK-19

RK-13

RK-2

JB97-4B

JB98-114

Chilled Margin Avg

Flood Basalt Avg


GROUP-1

A gabbro (CIPW)) gabbronorite (CIPW)B olivine gabbronorite (CIPW)# leucogabbro (CIPW)

(A)


(recalculated to metals in 100% sulphide) for Group-1 sulphides from Makada Lake

intrusion rocks, Waters Township. Data for average chilled margin is from this study;

data for average flood basalt is from Naldrett (1981); data from average East Bull Lake

intrusion hydrothermal sulphide is from Peck et al. (1993b). Mantle normalizing values

are from Barnes et al. (1988) and McDonough and Sun (1995).

230

1

10

100

1000

10000

100000


Met

al in

100

% S

ulph

ide/

Prim

itive

Man

tle

RK-18RK-12RK-7RK-11RK-8RK-9RK-10Chilled Margin AvgFlood Basalt AvgEBL Hydrothermal Avg

GROUP-2

(B)

A gabbro (CIPW)) gabbronorite (CIPW)D leucogabbronorite (CIPW)

Figure 5-57b. Primitive mantle-normalized PGE-chalcophile element diagrams

(recalculated to metals in 100% sulphide) for Group-2 sulphides from Makada Lake

intrusion rocks, Waters Township. Data for average chilled margin is from this study;

data for average flood basalt is from Naldrett (1981); data from average East Bull Lake

intrusion hydrothermal sulphide is from Peck et al. (1993b). Mantle normalizing values

are from Barnes et al. (1988) and McDonough and Sun (1995).

231

0.01

0.1

1

10

100

1000

10000

100000


Met

al in

100

% S

ulph

ide/

Prim

itive

Man

tle

JB97-78AJB97-76AJB97-76BJB98-165JB97-74ARK-1RK-3RK-4Chilled Margin AvgFlood Basalt AvgEBL Hydrothermal Avg

(>0.1 wt% S)A gabbro (CIPW)) gabbronorite (CIPW)B olivine gabbronorite (CIPW)# leucogabbro (CIPW)

(C)

Figure 5-57c. Primitive mantle-normalized PGE-chalcophile element diagrams

(recalculated to metals in 100% sulphide) for high sulphur (>0.05wt% S) samples from

Makada Lake intrusion rocks, Waters Township. Data for average chilled margin is from

this study; data for average flood basalt is from Naldrett (1981); data from average East

Bull Lake intrusion hydrothermal sulphide is from Peck et al. (1993b). Mantle


232

In Figure 5-57c, samples with high S concentrations (>0.1 wt% S) exhibit positive

fractionation patterns and are consistently depleted in PGE relative to average chilled

margin gabbro and average flood basalt; these patterns are interpreted to have resulted

from hydrothermal redistribution of the PGE.

5.9 Makada Lake Intrusion - Drill Hole A1-97

Diamond drill hole A1-97 (360 Az, -45 inclination), located about 30 m south of Pit

#2, targeted the mineralization under the western edge of Pit #2 (Fig. 5-51). The drill

hole intersected gabbro over its entire length (56.4 m) inclusive of an alteration zone

which extended from 37.19 m to 55.10 m. A total of 46 core samples were selected for

PGE, Au, S, Se and multi-element (Co, Cr, Cu, Ni) analyses; a complete listing of these

data is provided in Appendix 3. A summary of the drill hole information and data is

provided in Table 5-15. For the purposes of plotting, a value of one half of the lower

limit of detection is used where elements have concentrations that are below the lower

limits of detection; this is particularly relevant for Au, Pt and Pd, as the majority of

samples have concentrations that are below the lower limit of detection.

On the basis of geochemistry and geology from the surface section, this drill hole is

interpreted to have been drilled down-section toward the base (north) of the intrusion.

The drill hole intersected medium-grained gabbro over the first 36.47 m, followed by

altered gabbro to 55.10 m, and finally fine- to medium-grained gabbro to the end of the

hole; transition between the relatively fresh gabbro and the altered gabbro is gradational

over a few centimetres. The altered gabbro is characterized by green-grey colouration,

diffuse grain boundaries and patches of felt-textured mafic minerals. Within the

alteration zone (from 37.19 to 55.10 m), patches of blue quartz are a prominent feature

from 43.59-49.27 m. From about 49 to 51 metres the percentage of blue quartz decreases

and biotite becomes increasingly common, peaking in the altered biotite-rich gabbro from

51.21-55.10 m.

5.9.1 Chalcophile (PGE, Cu, Ni) and Trace Element Variations

Chalcophile elements (Pt, Pd, Au, Cu, Ni, S, Se) and minor elements (Cr, Co) are

plotted against depth in the drill hole in Figures 5-58 and 5-59. Highest concentrations of

Pt, Pd, Cu and Ni occur over a 0.65 m interval, from 53.95-54.76 m, in the altered biotite-

bearing gabbro.

233

0

10

20

30

40

50

601 10 100 1000 10000 100000 1000000 10000000

concentration (ppb)

Dril

l Hol

e Le

ngth

(m)

Au

SePt

Pd

Ni

Cu S

gabbro

gabbro(altered)

gabbro(altered-blue quartz)

gabbro(altered-biotite)

fg-mg gabbro

surface(A)

Figure 5-58a. Profiles through drill hole A1-97 from the Rauhala property (Makada Lake

intrusion), showing stratigraphic variations in Au, Pd, Pt, Se, Ni, Cu and S. Lower limits

of detection are: 2.5 ppb Au, 5 ppb Pd, 7.5 ppb Pt and 50 ppb Se.

234

0

10

20

30

40

50

6010 100 1000 10000

S/Se

Dril

l Hol

e Le

ngth

(m)

gabbro

gabbro(altered)



fg-mg gabbro

surface(B)

Figure 5-58b. Profiles through drill hole A1-97 from the Rauhala property (Makada Lake

intrusion), showing stratigraphic variations in S/Se.

235

0

10

20

30

40

50

601 10 100 1000 10000

concentration (ppm)

Dril

l Hol

e Le

ngth

(m)

gabbro

gabbro(altered)



fg-mg gabbro

surface

CrCo

(A)

Figure 5-59a. Profiles through drill hole A1-97 from the Rauhala property (Makada Lake

intrusion), showing stratigraphic variations in Co and Cr.

236

0

10

20

30

40

50

600.001 0.01 0.1 1 10

Pt/Se and Pd/Se

Dril

l Hol

e Le

ngth

(m)

Pd/Se

Pt/Se

gabbro

gabbro(altered)



fg-mg gabbro

surface(B)

Figure 5-59b. Profiles through drill hole A1-97 from the Rauhala property (Makada Lake

intrusion), showing stratigraphic variations in Pt/Se and Pd/Se ratios.

237

No Description VS From To Au Pt Pd Cu Ni S Se(m) (m) ppb ppb ppb ppm ppm wt% ppb

LLD --> 5 15 10 5.0 5.0 0.05 1001 mg gabbro 0 2.23 2.43 - - 10 58 47 0.096 1932 mg gabbro 0 4.27 4.57 - - - 84 50 0.037 -3 mg gabbro 0 6.10 6.30 - - - 36 45 0.021 2354 mg gabbro 0 7.32 7.52 - - 15 77 54 0.029 -5 mg gabbro 0 8.53 8.85 - - - 59 54 0.020 -6 mg gabbro 0 10.06 10.26 - - - 55 62 0.018 -7 mg gabbro 0 11.58 11.78 - - - 45 51 0.023 6328 mg gabbro 0 13.11 13.40 - - - 28 54 0.018 3049 mg gabbro 0 14.63 14.85 - - - 19 47 0.011 320

10 mg gabbro 0 16.46 16.66 - - - 21 50 0.016 -11 mg gabbro 0 17.68 17.88 - - - 23 51 0.013 10212 mg gabbro 0 19.20 19.40 - - - 73 80 0.041 81713 mg gabbro 0 20.42 20.62 - - - 76 55 0.032 10414 mg gabbro 0 21.64 21.84 - - - 28 69 0.022 198015 mg gabbro 0 23.77 23.97 - - - 59 53 0.023 57816 mg gabbro 0 25.30 25.50 11 - - 60 57 0.019 68617 mg gabbro 0 26.09 26.29 - - - 51 49 0.016 84518 mg gabbro 0 27.43 27.63 - - - 55 55 0.024 -19 mg gabbro 0 28.96 29.16 - - - 59 55 0.021 -20 mg gabbro 0 30.78 30.98 - - - 60 55 0.036 26921 mg gabbro 0 32.16 32.36 - - - 70 54 0.024 -22 mg gabbro 0 33.68 33.88 - - - 81 50 0.027 -23 mg gabbro 0 35.05 35.25 - - - 80 66 0.025 311

Table 5-15. Summary of chalcophile element concentrations and ratios for samples from

diamond drill hole A1-97, Rauhala property, Makada Lake intrusion, Waters Township.

Sample prefixes = WT99; VS = visible sulphide; LLD=lower limit of detection; "-

"=below detection.

238

No Description VS From To Au Pt Pd Cu Ni S Se(m) (m) ppb ppb ppb ppm ppm wt% ppb

LLD --> 5 15 10 5.0 5.0 0.05 10024 mg gabbro 0 36.27 36.47 9 - - 75 62 0.020 -25 altered gabbro <1 37.19 37.52 - - - 18 45 0.010 14526 altered gabbro <1 38.31 38.59 - - - 9 57 - 47627 altered gabbro <1 38.71 38.93 - - - 29 126 0.041 46628 altered gabbro <1 38.95 39.21 - - - 49 163 0.075 59129 altered gabbro <1 39.62 39.85 - - - 12 183 0.024 170230 altered gabbro <1 40.39 40.63 - - - 11 65 - 55531 altered gabbro <1 40.84 41.06 - - - 9 85 0.026 19532 altered gabbro <1 42.0624 42.2624 - - - 53 62 0.038 -33 altered gabbro; blue qtz 5 43.5864 43.7864 577 - - 55 60 0.016 41034 altered gabbro; blue qtz 5 45.1866 45.42 7 - - 32 65 0.022 57335 altered gabbro; blue qtz 5 46.6344 46.8344 - - - 39 71 0.028 -36 altered gabbro; blue qtz 5 48.1584 48.45 - - - 58 44 0.021 -37 altered gabbro; blue qtz 5 49.0728 49.2728 - - - 69 55 0.024 -38 altered gabbro; biotite 10 51.2064 51.4064 - - - 68 44 0.023 26739 altered gabbro; biotite 10 52.1208 52.3208 8 - - 41 49 0.019 -40 altered gabbro; biotite 10 53.9496 54.2 19 32 167 234 189 0.074 37441 altered gabbro; biotite 10 54.2544 54.4544 62 120 715 484 433 0.172 57142 altered gabbro; biotite 10 54.5592 54.7592 130 217 1033 1077 1101 0.424 113043 altered gabbro; biotite 10 54.864 55.1 9 29 28 45 96 0.019 -44 fg-mg gabbro 55.0164 55.2164 - - - 39 114 0.022 59245 fg-mg gabbro 55.4736 55.6736 10 - - 85 69 0.029 57146 fg-mg gabbro 55.9308 56.11 6 - 11 87 87 0.031 -

Table 5-15 (cont). Summary of chalcophile element concentrations and ratios for samples

from diamond drill hole A1-97, Rauhala property, Makada Lake intrusion, Waters

Township. Sample prefixes = WT99; VS = visible sulphide; LLD=lower limit of

detection; "-"=below detection.

239

Peaks in the concentration of S are coincident with the peaks in Pt-Pd-Cu-Ni, suggesting

sulphide control on the PGE; peaks in Co and Cr are also coincident with the highest

PGE-Cu-Ni mineralization. At approximately 40 m down the hole there are peaks in the

Se, S, Cu and Ni concentrations but all PGE are below the lower limits of detection. This

implies that although the magma continued to precipitate sulphides the availability of

PGE had significantly declined, having been stripped from the magma in earlier forming

sulphides (i.e. from 53.95-54.76 m). Values for S/Se within the PGE-Cu-Ni zone are

within the range of uncontaminated magmatic sulphides (Naldrett, 1981). However,

more than 20 of the samples have S/Se values that are <1000, which can be attributed to

S loss and/or preferential incorporation of Se into the sulphide, relative to S, as discussed

in Section 5.2.3. The six samples with S/Se values >5000, is probably due to the

introduction of external sulphur through local contamination.

5.10 Kukagami Lake Intrusion – Traverse

The Kukagami Lake intrusion, located about 45 km northeast of the City of Greater

Sudbury in Kelly Township, is a northwest-trending body that is exposed for more than

12 km from the southeast quadrant of Kelly Township through to Mackelcan Township

in the northwest (Figs. 1-2, 5-60, 5-61 and 5-62). Samples were collected from four areas

along the strike of the Kukagami Lake sill, encompassing seven samples from the

“Kukagami Cliff” area (Photo 4-1), located at the western “end” of the intrusion (Fig. 5-

61); 15 samples that comprise the lithogeochemical section through the central part of the

intrusion (Fig. 5-61); five samples from the Whalen showing (Kukagami Lake

occurrence; Lightfoot et al., 1993), located about 150 m east of the northern part of the

lithogeochemical section (Fig. 5-61); and, seven samples from the area of the Washagami

Lake occurrence (Fig. 5-62). A summary of the samples is provided in Table 5-16 and a

complete listing of the data is provided in Appendix 1.


Thomson and Card (1963) interpreted the Nipissing Gabbro intrusions in this region

to range from large dikes and sills to small irregularly shaped masses, mapping the

Kukagami Lake body as a sill. On the basis of PGE-Cu-Ni sulphide occurrences and

similar geochemical characteristics, Lightfoot et al. (1993) proposed that the Kukagami

Lake sill and Wanapitei intrusion (Dressler, 1982) are one contiguous sill (Fig. 5-1).

240

Figure 5-60. General geology and location of the Kukagami Lake intrusion, Kelly

Township. Specific sample location areas – Kukagami West and Kukagami East – are

outlined and shown in detail in Figures 5.10-2 and 5.10-3, respectively. Geology is after

Thomson and Card (1963). Map coordinates are UTM, NAD27-Zone17.

241

Figure 5-61. General geology and location of samples collected from the western portion

of the Kukagami Lake intrusion, Kelly Township. Also shown is the location of the

Whalen showing and the Kukagami Cliff area. Geology is after Thomson and Card

(1963). Map coordinates are UTM, NAD27-Zone17.

242

Figure 5-62. General geology and location of samples collected from the eastern portion

of the Kukagami Lake intrusion, Kelly Township. Also shown is the location of the

Washagami Lake occurrence. Geology is after Thomson and Card (1963). Map

coordinates are UTM, NAD27-Zone17.

243


JB97-102 sediment 0.070 300 82 - - - 7.000 5.000JB98-194 G (Q-H) 0.054 292 117 0.053 0.350 0.434 8.350 9.510JB98-195 G (Q-H) 0.056 267 116 - - 0.277 10.610 11.020JB98-196 G (Q-H) 0.032 181 134 - - 0.309 14.450 13.180JB98-197 G (Q-H) 0.058 243 63 - - - - 0.090JB98-198 G (Q-H) 0.085 394 155 - 0.130 - 1.310 1.330JB98-199 G (Q-H) 0.013 204 119 - - - 1.290 0.970JB98-200 GN (H-O) 0.037 261 150 - - 0.098 2.570 2.230JB98-201 G (Q-H) 0.035 212 153 - 0.130 0.096 4.100 3.200JB98-202 G (Q-H) 0.078 311 148 - - 0.142 7.730 7.560JB98-203 G (Q-H) 0.055 147 150 0.050 - 0.387 8.000 9.410JB98-204 G (Q-H) 0.009 100 147 0.056 0.150 0.407 8.540 8.720JB98-205 G (Q-H) 0.016 86 182 0.127 0.190 0.750 9.780 24.600JB98-206 G (Q-H) 0.039 155 146 0.065 0.150 0.446 10.700 10.100JB98-207 G (Q-H) 0.053 168 122 0.070 0.160 0.399 12.340 12.970

JB98-239A sediment 0.115 134 69 0.040 0.130 0.080 1.790 3.120JB97-103E G (Q-H) 0.014 na 125 0.200 - 0.500 15.000 15.000JB97-103D G (Q-H) 0.067 600 148 0.200 - 1.100 12.000 19.000JB97-103C opx gabbro 1.961 6200 2662 0.800 - 12.000 440.000 1550.000JB97-103B GN (H-O) 0.067 700 213 0.500 - 0.700 20.000 55.000JB97-103A opx gabbro 1.734 6400 2773 0.700 - 23.000 380.000 1930.000JB98-239B G (Q-H) 0.086 211 117 - - 0.310 10.400 17.240JB98-239C G (Q-H) 0.040 219 119 - - 0.280 10.590 11.100JB98-240 G (Q-H) 0.044 239 120 - - 0.290 10.610 12.120

JB98-239F G (Q-H) 0.024 180 94 na na na na naJB98-239E G (Q-H) 0.053 237 132 na na na na naJB98-239D GN (H-O) 0.087 221 120 na na na na na

JB97-18 G (Q-H) 0.060 365 150 - - - 4.366 6.156JB97-20 G (Q-H) 0.020 233 140 0.182 - 0.620 27.300 45.041JB97-14 G (Q-H) 0.050 258 160 0.230 - 1.120 32.510 119.000JB97-15 G (Q-H) 0.040 358 130 - - - 1.488 2.671JB97-16 G (Q-H) 0.080 500 180 0.240 - 1.061 28.168 109.656

JB97-19A G (Q-H) 0.040 321 220 0.170 - 0.790 17.830 68.770JB97-19B G (Q-H) 0.070 297 170 0.170 - 0.880 16.050 57.410


Kukagami Lake intrusion, Kelly Township. The main sample section through the

intrusion includes samples JB97-102 through to JB98-239A. "-" below lower limit of

detection; "N" = primitive mantle-normalized; "na"=not analyzed; G=gabbro;

OLGN=olivine leucogabbronorite; LG=leucogabbro; GN=gabbronorite;

opx=orthopyroxene; Q-H=quartz-hypersthene; H-O=hypersthene-olivine; Q-H-C=quartz-



244


ppb ppm ppmJB97-102 1.500 73 2333 0.7 0.9 50 156 4.11JB98-194 3.650 118 1849 1.1 1.0 65 43 2.19JB98-195 2.880 104 2097 1.0 0.9 64 43 2.02JB98-196 - 111 1768 0.9 0.8 70 30 2.05JB98-197 0.820 118 2387 - 1.9 53 60 2.31JB98-198 2.500 227 2157 1.0 1.5 67 39 2.10JB98-199 2.720 138 637 0.8 1.2 66 40 2.22JB98-200 3.700 168 1418 0.9 1.1 70 30 1.98JB98-201 5.300 150 1651 0.8 1.0 72 31 1.93JB98-202 5.740 144 2508 1.0 1.0 68 40 2.02JB98-203 2.470 82 3741 1.2 0.5 72 32 2.19JB98-204 1.970 78 900 1.0 0.5 71 33 2.09JB98-205 2.630 87 1860 2.5 0.5 75 26 2.00JB98-206 3.280 88 2516 0.9 0.6 72 34 2.00JB98-207 4.510 109 3155 1.1 0.9 66 40 2.09

JB98-239A 2.230 40 8582 1.7 0.6 53 129 3.62JB97-103E 1.200 94 - 1.0 0.8 65 36 2.00JB97-103D 1.000 110 1117 1.6 0.7 68 35 2.03JB97-103C 120.000 6259 3162 3.5 2.4 65 29 1.98JB97-103B 2.000 196 957 2.8 0.9 71 29 1.85JB97-103A 120.000 5095 2710 5.1 1.8 64 30 1.87JB98-239B 2.260 77 4076 1.7 0.7 66 40 2.52JB98-239C 3.530 114 1826 1.0 1.0 65 35 2.30JB98-240 3.280 133 1841 1.1 1.1 65 38 2.19

JB98-239F na 73 1333 - 0.8 64 38 2.42JB98-239E na 112 2236 - 0.8 68 34 2.26JB98-239D na 95 3937 - 0.8 68 39 2.60

JB97-18 4.272 170 1644 1.4 1.1 67 37 2.09JB97-20 4.811 120 858 1.6 0.9 68 34 1.96JB97-14 8.010 130 1938 3.7 0.8 70 30 1.91JB97-15 2.257 160 1117 1.8 1.2 65 38 1.94JB97-16 8.586 220 1600 3.9 1.2 67 34 1.86

JB97-19A 17.090 190 1246 3.9 0.9 71 35 2.23JB97-19B 4.330 150 2357 3.6 0.9 71 29 1.89

Table 5-16 (cont). Summary of whole-rock geochemical characteristics for samples from

the Kukagami Lake intrusion, Kelly Township. The main sample section through the

intrusion includes samples JB97-102 through to JB98-239A. "-" below lower limit of

detection; "N" = primitive mantle-normalized; "na"=not analyzed; G=gabbro;

OLGN=olivine leucogabbronorite; LG=leucogabbro; GN=gabbronorite;

opx=orthopyroxene; Q-H=quartz-hypersthene; H-O=hypersthene-olivine; Q-H-C=quartz-

hypersthene-corundum.

245

However, on the basis of field relationships noted during the course of the current study,

it is more likely that the Kukagami Lake intrusion is contiguous with bodies in Davis

Township to the southeast, and perhaps even the Chiniguchi River intrusion in Janes

Township further to the southeast (Fig. 5-1); together these intrusive bodies appear to

form an inward-dipping arcuate shape, indicative of a cone sheet.

The Kukagami Lake sill is hosted by Gowganda Formation (argillite, quartzite) and

subordinate Lorrain Formation (arkose) sedimentary rocks (Thomson and Card, 1963),

and parallels a large Sudbury Swarm dike which extends for more than 25 km (Shellnutt,

2002). On the basis of field observations and the geology of the section through the

intrusion, the base of the intrusion is interpreted to be along the northern contact.

Locally, the Kukagami Lake section provides a near-complete cross-section through

the sill, exposing the basal contact of the intrusion in the north (Fig. 5-61; Photo 5-5a).

Samples JB98-239A and JB97-102 are used as representatives of the footwall and

hangingwall sedimentary rocks, respectively, in the sample section. From north to south,

the intrusive rocks comprise fine-grained to chilled gabbro (±quartz), medium-grained

gabbro (±magnetite), orthopyroxene gabbro (±magnetite), medium-grained gabbro,

medium-grained gabbro (±magnetite), and finally fine- to medium-grained gabbro along

the northern shore of Carafel Bay (Fig. 5-61). Pegmatitic gabbro and vari-textured

gabbro were noted in several outcrops in the region of JB98-196, JB98-197 and JB98-

198, located in the southern part of the section or in the upper portion of the sill

stratigraphy. Several samples of chilled margin gabbro (sample JB98-239A, 239B and

240) were collected from exposures near the Kukagami cliff (Fig. 5-61).

Several PGE-Cu-Ni sulphide showings occur within the Kukagami Lake intrusion,

specifically toward the western segment of the sill (Kukagami Cliff area; Fig. 5-61), the

central portion of the intrusion (Whalen showing; Fig. 5-61), and the eastern portion of

the sill (Washagami Lake occurrence; Fig. 5-62). Lightfoot et al. (1991a) reported values

of 90 ppb Au, 215 ppb Pt, 1840 ppb Pd, 3200 ppm Cu, 1650 ppm Ni, and 1.0 wt% S from

the Kukagami Cliff area and 600 ppb Au, 945 ppb Pt, 4160 ppb Pd, 8000 ppm Cu, 2800

ppm Ni, and 2.1 wt% S from the Whalen showing (Fig. 5-61; Photo 5-5b).

246

Photo 5-5. Kukagami Lake Intrusion. (A) Sharp contact between Huronian Supergroup sedimentary rocks (sediment) and fine- to medium-grained gabbro, from the northern basal contact of the intrusion. The hammer handle is about 33 cm long. (B) Medium-grained orthopyroxene gabbro from the Whalen showing (sample JB98-103A) with disseminated (ds) and blebby sulphide and very fine-grained blue quartz. The pen magnet is about 12 cm long.

247

Patchy sulphide mineralization (~1% pyrrhotite + chalcopyrite) was noted at several

locations within ~100 m of the northern contact of the intrusion, hosted by dark-

weathering, orthopyroxene gabbro. In 1999, Pacific North West Capital Corp. completed

5 diamond drill holes on the Washagami Lake occurrence, also referred to as the Davis-

Kelly property (Meyer et al., 2000); a summary of the drill results is listed in Table 5-17.


Gabbroic samples from the Kukagami Lake intrusion are characterized by averages

of 51.7 wt% SiO2, 0.51 wt% TiO2, 14.1 wt% Al2O3, 8.9 wt% MgO, and an Mg-number of

68. Four samples of chilled margin gabbro average 50.8 wt% SiO2, 0.55 wt% TiO2, 14.6

wt% Al2O3, 8.3 wt% MgO, and an Mg-number of 65. CIPW normative calculations were

completed on 30 of the 32 gabbroic samples collected from the Kukagami Lake sill

(Table 5-16). The majority of samples (27 of 30) classify as quartz-hypersthene-

normative (silica-oversaturated) gabbro with three samples classifying as hypersthene-

olivine-normative (silica-saturated) gabbronorite. In the field, samples described as

orthopyroxene gabbro classified mainly as CIPW gabbro with only one correlating with

CIPW gabbronorite; CIPW gabbro samples cover a range in rock types including gabbro,

vari-textured gabbro, magnetite-bearing gabbro and orthopyroxene gabbro.

With the exception of samples JB98-197, JB98-195 and JB98-194, which are

differentiated rock types within the sill, all of the intrusive rocks from the sample section

and the majority of other samples from other areas of the sill have higher Mg-number and

lower TiO2 concentrations relative to average chilled margin gabbro and relative to the

sample of chilled gabbro collected from the northern margin of the sill (Fig. 5-63).

Assuming that the average chilled margin and chilled margin samples from the Kukagami

Lake sill represent parent magma compositions, then it follows that the rocks within the

main body of the intrusion are much more primitive or less fractionated relative to

“normal” or average Nipissing Gabbro. Much of this sill consists of either massive

orthopyroxene gabbro with ~5-10% phenocrysts of hypersthene (up to 5 mm long) or

orthopyroxene-bearing gabbro with 1-5% primocrysts of orthopyroxene. The primitive

nature of these rocks relative to chilled margin gabbro supports the interpretation that

they are cumulates and that they do not represent the liquids from which the associated

chilled margin gabbro rocks crystallized.

248

DDH From To Interval 3E Cu Ni Cu+Nim m m ppm wt% wt% wt%

DK99-01 20 29.5 9.5 0.55 0.04 0.03 0.0751.2 54.53 3.33 2.66 0.31 0.19 0.5

DK99-02 16 20.5 4.5 0.55 0.04 0.03 0.0726.25 31 4.75 1.26 0.09 0.06 0.15

including 28.5 30 1.5 2.46 0.18 0.11 0.2949.1 53.5 4.4 3.93 0.44 0.3 0.74

including 49.1 52.7 3.6 4.38 0.49 0.33 0.82DK99-03 18.2 19.7 1.5 0.99 0.21 0.08 0.29

31.85 35.6 3.75 1.25 0.12 0.08 0.2DK99-05 28 37.3 9.3 0.16 0.03 0.03 0.06

40.4 41.7 1.7 0.46 0.06 0.05 0.11

Table 5-17. Summary of diamond drill core assay results from the Washagami Lake

occurrence (also referred to as the Davis-Kelly showing), Kelly Township (Meyer et al.,

2000). Diamond drilling was completed in 1999 by Pacific North West Capital Corp..

Values for 3E = Pt+Pd+Au.

249

0.3

0.4

0.5

0.6

0.7

0.8

0.9

3035404550556065707580

Mg-number

TiO

2 (w

t%) JB97-102 (HW)

JB98-194JB98-195JB98-196JB98-197JB98-198JB98-199JB98-200JB98-201JB98-202JB98-203JB98-204JB98-205JB98-206JB98-207JB98-239A (FW)Chilled Margin AvgHuronian Sediment AvgAplite Avg

fractionation

Y mt gabbro (CIPW)A gabbro (CIPW)D vt gabbro) gabbronorite (CIPW)# chilled gabbro+ sediment

vt gabbro

chilled margin

(A)

0.3

0.4

0.5

0.6

0.7

0.8

0.9

3035404550556065707580

Mg-number

TiO

2 (w

t%)

Chilled Margin AvgHuronian Sediment AvgAplite Avg

fractionation

JB98-197Y mt gabbro (CIPW)A gabbro (CIPW)D vt gabbro) gabbronorite (CIPW)# chilled gabbro+ sediment

(B)

Figure 5-63. Bivariate scatter plots of Mg-number and wt% TiO2 for rocks from the Kukagami Lake intrusion. (A) Rocks from the sample section through the intrusion. (B) All samples collected from the intrusion.

250

Variation in selected major elements are plotted against relative distance or

stratigraphic height through the intrusion (Fig. 5-64). The concentration of SiO2 shows

very little variation through the section, averaging ~51.7 wt% SiO2 and the

concentrations of TiO2 display a gradual increase through the section, with the highest

concentration of TiO2, coincident with the highest concentration of SiO2, occurring in the

upper vari-textured gabbro unit (Fig. 5-64). Mg-number shows a slight increase in the

lowermost samples, above the chilled margin, followed by a general decrease upward

through the intrusion, which is indicative of normal fractionation. The Mg-number of the

lower chilled gabbro (Mg-number = 66) approximates that of the uppermost gabbro unit

(Mg-number = 65); the latter was collected from within ~25 m of the hangingwall

sedimentary rocks (Fig. 5-61).


In general, rocks from the sample section show very little variation upward through

the intrusion and disregarding the uppermost gabbro (JB98-194) and lowermost chilled

gabbro (JB98-207), there is only a very subtle upward (north to south) increase in the

ratios of (La/Sm)N, (Th/Nb)N and in concentrations of Zr and ∑REE; this suggests normal

fractionation within the sill with very little in-situ contamination.

Primitive mantle-normalized multi-element diagrams for samples from the

Kukagami Lake intrusion are shown in Figures 5-65 and 5-66. The gabbroic samples

have similar overall trace and rare-earth element abundances (~1-50 times primitive

mantle) with moderate LILE enrichment (~1-50 times primitive mantle), an average of

~2.1 (La/Sm)N, and weakly enriched HREE (~1-6 times primitive mantle); sample JB98-

197, which is a differentiated gabbro from the upper stratigraphy of the intrusion, shows

the highest overall REE abundance. All of the gabbroic examples, excepting sample

JB98-197, display lower overall REE abundances relative to the average chilled margin

gabbro of Lightfoot and Naldrett (1996). All of the gabbroic samples, including JB98-

197, display pronounced negative Nb+Ta anomalies and moderate to strongly negative

P* and Ti* anomalies, which is typical of other Nipissing Gabbro intrusions (Lightfoot

and Naldrett, 1996).

251

0

50

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150

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250

300

350

400

450

500

550

600

650

700

750

800

45 50 55 60 65 70 75 80

SiO2 (wt) and Mg-number

Rel

ativ

e D

ista

nce

(not

to sc

ale)

sediment

sediment NORTH

SOUTH

mt gabbro (G)

gabbro (G)

gabbro (G)

mt gabbro (G)

gabbro (G)

gabbro (GN)

opx gabbro (G)

chilled gabbro (G)

vt gabbro (G)

SiO2 Mg-number

Figure 5-64a. Profiles through the Kukagami Lake intrusion showing stratigraphic


252

0

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250

300

350

400

450

500

550

600

650

700

750

800

0.2 0.3 0.4 0.5 0.6 0.7 0.8 0.9

TiO2 (wt%)

Rel

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e D

ista

nce

(not

to sc

ale)

sediment

sedimentNORTH

SOUTH

mt gabbro (G)

gabbro (G)

gabbro (G)

mt gabbro (G)

gabbro (G)

gabbro (GN)

opx gabbro (G)

chilled gabbro (G)

vt gabbro (G)

Figure 5-64b. Profile through the Kukagami Lake intrusion showing stratigraphic


253

0.1

1

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100

1000


Sam

ple/

Prim

itive

Man

tleJB97-102 (HW)

JB98-194

JB98-195

JB98-196

JB98-197

JB98-198

JB98-199

JB98-200

JB98-201

JB98-202

JB98-203

JB98-204

JB98-205

JB98-206

JB98-207

JB98-239A (FW)

Chilled Margin Avg

(A) g mt gabbro (CIPW)A gabbro (CIPW)D vt gabbro) gabbronorite (CIPW)# chilled gabbro+ sediment

1

10

100


Sam

ple/

Prim

itive

Man

tle

JB97-103E

JB97-103D

JB97-103C

JB97-103B

JB97-103A

Chilled Margin Avg

(B)A gabbro (CIPW)) gabbronorite (CIPW)

Figure 5-65. Primitive mantle-normalized multi-element diagrams for rock samples from the Kukagami Lake intrusion, Kelly Township. (A) Sample Section through sill. (B) Detailed sampling from Whalen sulphide showing. Mantle normalizing values are from McDonough and Sun (1995).

254

1

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ple/

Prim

itive

Man

tle

JB98-207

JB98-239B

JB98-239C

JB98-240

Chilled Margin Avg

(A)

# chilled gabbro

0.1

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10

100


Sam

ple/

Prim

itive

Man

tle

JB98-194JB98-195JB98-196JB98-197JB98-198JB98-199JB98-200JB98-201JB98-202JB98-203JB98-204JB98-205JB98-206JB98-207JB97-103EJB97-103DJB97-103CJB97-103BJB97-103AJB98-239BJB98-239CJB98-240JB98-239FJB98-239EJB98-239DJB97-18JB97-20JB97-14JB97-15JB97-16JB97-19AJB97-19BChilled Margin Avg

(B)g mt gabbro (CIPW)A gabbro (CIPW)D vt gabbro) gabbronorite (CIPW)# chilled gabbro

Figure 5-66. Primitive mantle-normalized multi-element diagrams for rocks from the Kukagami Lake intrusion. (A) Chilled margin gabbro. (B) All gabbroic rocks. Mantle normalizing values are from McDonough and Sun (1995).

255

0.1

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itive

Man

tle

JB98-194JB98-195JB98-197JB98-198JB98-202JB98-203JB98-207JB97-103DJB97-103CJB97-103BJB97-103AJB98-239BJB98-239EJB98-239DJB97-18JB97-16JB97-19BChilled Margin Avg

(C)g mt gabbro (CIPW)A gabbro (CIPW)D vt gabbro) gabbronorite (CIPW)# chilled gabbro

(>0.05 wt% S)

Figure 5-66. Primitive mantle-normalized multi-element diagrams for rocks from the

Kukagami Lake intrusion, Kelly Township. Samples plotted are gabbroic rocks with

elevated sulphur (>0.05 wt% S). Mantle normalizing values are from McDonough and

Sun (1995).

256


As described earlier, there are several sulphide showings containing anomalous

PGE-Cu-Ni mineralization within the Kukagami Lake sill (Figs. 5-61 and 5-62). Five

samples were collected from the immediate area of the Whalen showing (Fig. 5-61) with

maximum values of 120 ppb Au, 440 ppb Pt, 1930 ppb Pd, 5095 ppm Cu, 2773 ppm Ni,

and ~2.0 wt% S. Two samples were collected from the immediate area of the

Washagami Lake occurrence (Fig. 5-62) with maximum values of 17 ppb Au, 18 ppb Pt,

69 ppb Pd, 190ppm Cu, 220 ppm Ni, and 0.07 wt% S. In this area, the highest precious

metals values are from sample JB97-14 (orthopyroxene gabbro or CIPW gabbro), located

about 200 m northwest of the Washagami Lake occurrence, which contains 8 ppb Au, 33

ppb Pt, 119 ppb Pd, 130 ppm Cu, 160 ppm Ni, and 0.05 wt% S.


the intrusion in Figure 5-67. For the most part the concentrations of Pt, Pd, Cu, Ni, and

S, along with the ratios of Cu/Ni and Pd/Pt, show no systematic variation through this

section of the sill and the gabbroic samples have S/Se ratios (~637-3741) that are

generally indicative of uncontaminated magmatic sulphide (Naldrett, 1981). However, of

particular interest are the ratios of Pt/Se, Pd/Se and Cu/Pd which are highest in the

lowermost and uppermost gabbroic units, peaking at ~600 m (Fig. 5-67). These trends

suggest that, as at the Charlton Lake sill (see Section 5.5.4), there was co-precipitation of

sulphides in the magma along two sulphide precipitation fronts; one moving downward

from the upper part of the sill and the other moving upward from the lower part of the

sill.


metals in 100% sulphide) are shown in Figures 5-68 and 5-69. All of the gabbroic

samples from the Kukagami Lake intrusion are characterized by positive slopes with the

Pt-Pd-Au-Cu (~600-20,000 times primitive mantle) portion elevated relative to the Ni-Ir-

Ru-Rh portion (~7-300 times primitive mantle). Although much lower in chalcophile

abundance, the sample of sedimentary rock also features a positive slope and parallels the

patterns of the gabbroic rocks. Most of the gabbroic samples show a peak in Pd, have

Ni/Ir values that are close to 1 or greater (negative slopes) and display profiles that are

similar to average chilled margin and average flood basalt.

257

0

50

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450

500

550

600

650

700

750

800

0.01 0.1 1 10 100 1000 10000 100000 1000000 10000000


Rel

ativ

e D

ista

nce

(not

to sc

ale)

sediment

sediment NORTH

SOUTH

mt gabbro (G)

gabbro (G)

gabbro (G)

mt gabbro (G)

gabbro (G)

gabbro (GN)

opx gabbro (G)

chilled gabbro (G)

vt gabbro (G)

Pd (ppb)

Pt (ppb)

(A)

S (ppb)

Ni (ppm) Cu (ppm) S/Se

Cu/Pd

Figure 5-67a. Profiles through the Kukagami Lake intrusion sample section, showing

stratigraphic variations in Pd, Pt, Ni, Cu, S/Se, Cu/Pd and S. The arrows show the

direction of the sulphide precipitation front. The relative vertical scale is in metres.

258

0

50

100

150

200

250

300

350

400

450

500

550

600

650

700

750

800

0.0001 0.001 0.01 0.1 1 10

Ratio

Rel

ativ

e D

ista

nce

(not

to sc

ale)

sediment

sedimentNORTH

SOUTH

mt gabbro (G)

gabbro (G)

gabbro (G)

mt gabbro (G)

gabbro (G)

gabbro (GN)

opx gabbro (G)

chilled gabbro (G)

vt gabbro (G)

Pt/Se

Pd/PtCu/Ni

Pd/Se

(B)

Figure 5-67b. Profiles through the Kukagami Lake intrusion sample section, showing

stratigraphic variations in Pt/Se, Pd/Se, Cu/Ni and Pd/Pt. The arrows show the direction

of the sulphide precipitation front. The relative vertical scale is in metres.

259

1

10

100

1000

10000

100000


Met

al in

100

% S

ulph

ide/

Prim

itive

Man

tle

JB98-194

JB98-201

JB98-203

JB98-204

JB98-205

JB98-206

JB98-207

JB98-239A (FW)

Chilled Margin Avg

Flood Basalt Avg

g mt gabbro (CIPW)A gabbro (CIPW)# chilled gabbro+ sediment

(A)


(recalculated to metals in 100% sulphide) for sulphides from samples collected through

the Kukagami Lake intrusion. Data for average chilled margin is from this study; data for

average flood basalt is from Naldrett (1981). Mantle normalizing values are from Barnes

et al. (1988) and McDonough and Sun (1995).

260

1

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1000

10000

100000


Met

al in

100

% S

ulph

ide/

Prim

itive

Man

tle

JB97-103E

Chilled Margin Avg

Flood Basalt Avg

A gabbro (CIPW)

(B)


(recalculated to metals in 100% sulphide) for sulphides from detailed sampling at the

Whalen sulphide showing, Kukagami Lake intrusion. Data for average chilled margin is



261

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1000

10000

100000


Met

al in

100

% S

ulph

ide/

Prim

itive

Man

tle

JB98-207

JB98-239B

JB98-239C

JB98-240

Chilled Margin Avg

Flood Basalt Avg

# chilled gabbro

(A)


(recalculated to metals in 100% sulphide) for sulphides from chilled margin gabbro,

Kukagami Lake intrusion. Data for average chilled margin is from this study; data for

average flood basalt is from Naldrett (1981). Mantle normalizing values are from Barnes

et al. (1988) and McDonough and Sun (1995).

262

1

10

100

1000

10000

100000


Met

al in

100

% S

ulph

ide/

Prim

itive

Man

tle

JB98-194

JB98-203

JB98-207

JB98-239B

JB97-16

JB97-19B

Chilled Margin Avg

Flood Basalt Avg

(>0.0.5 wt% S)

A gabbro (CIPW)# chilled gabbro

(B)


(recalculated to metals in 100% sulphide) for sulphides in gabbroic rocks with elevated

sulphur (>0.05 wt% S), Kukagami Lake intrusion. Data for average chilled margin is



263

5.11 Manitou Lake Intrusion – Traverse

The sample section through the Manitou Lake intrusion, located about 65 km

northeast of the City of Greater Sudbury, covers a relatively small portion of a much

larger body of Nipissing Gabbro that extends for more than 20 km to the northeast into

Scholes Township, more than 12 km to the northwest into Afton Township, and more

than 12 km to the southeast into Pardo and Hobbs townships where it terminates against

the Grenville Front Boundary Fault (Figs. 1-2 and 5-1). The sample suite consists of nine

samples, collected immediately west of Manitou Lake in Clement Township along

Highway 805, which provides numerous exposures of gabbroic rock (Fig. 5-70). From

north to south the Manitou Lake section exposes homogenous medium-grained gabbro.

A summary of the samples is provided in Table 5-18 and a complete listing of the data is



The Manitou Lake intrusion is relatively undifferentiated, consisting mainly of

medium-grained two-pyroxene gabbro, with fine-grained gabbro (chill?) noted within 3-

7.5 m of the contact, and occasional patches of coarse-grained gabbro and pods of

pegmatitic gabbro (Meyn, 1977). The intrusion, as described by Meyn (1977), comprises

seven sill-like bodies within Afton, Scholes, Macbeth and Clement townships that are in

sharp contact with Gowganda Formation sedimentary rocks and in intrusive contact

(inferred) with Archaean volcanic and sedimentary rocks. The Manitou Lake intrusion

may be contiguous with the Chiniguchi River intrusion, located ~20 km to the south-

southeast in Janes Township (Dressler, 1979), and connected by Nipissing Gabbro rocks

that are apparently continuous through MacBeth (Meyn, 1977) and McNish (Dressler,

1979) townships (Fig. 5-1). Meyn (1977) also described brecciated contacts consisting of

sediment fragments hosted by finer-grained gabbro, and centimetre- to decametre-scale

fragments of sedimentary rocks hosted completely within gabbro. On the basis of

geochemical analyses and the presence of these fragments, Meyn (1977) suggested that

the Nipissing Gabbro was contaminated from interaction with the surrounding

sedimentary rocks.

264

Figure 5-70. General geology and location of the sample section for the Manitou Lake

intrusion, Clement Township. Geology after Meyn (1977).

265


JB97-32 OLGN (N-O) 0.070 121 95 - - - - -JB97-31 G (Q-H) 0.060 233 38 - - - - -JB97-30 G (Q-H) 0.070 302 110 0.178 - 0.275 2.323 7.314JB97-29 G (Q-H) 0.040 277 100 9.820 2.770 4.520 4.020 4.420JB97-28 G (Q-H) 0.070 311 110 - - - - -JB97-27 G (Q-H) 0.060 293 120 - - - 0.500 0.410JB97-26 G (Q-H) 0.070 309 110 - - - 2.363 3.271JB97-25 G (Q-H) 0.050 290 110 - - - 1.356 2.500JB97-24 G (Q-H) 0.020 155 100 - - - - 1.930Sample Au Cu S/Se Pd/Pt Cu/Ni Mg# ∑REE (La/Sm)N

ppb ppm ppmJB97-32 - 51 5785 - 0.5 48 149 1.08JB97-31 6.444 40 2575 - 1.1 34 87 1.01JB97-30 2.329 140 2318 3.1 1.3 60 43 1.00JB97-29 3.220 150 1444 1.1 1.5 58 44 0.93JB97-28 - 160 2251 - 1.5 59 46 0.90JB97-27 3.150 150 2048 0.8 1.3 63 37 0.85JB97-26 2.847 160 2265 1.4 1.5 60 38 0.91JB97-25 3.210 150 1724 1.8 1.4 61 38 0.96JB97-24 1.689 150 1290 - 1.5 58 44 0.94


Manitou Lake intrusion, Clement Township. "-" below lower limit of detection; "N" =


leucogabbronorite; LG=leucogabbro; GN=gabbronorite; Q-H=quartz-hypersthene; H-

O=hypersthene-olivine; Q-H-C=quartz-hypersthene-corundum; N-O=nepheline-olivine.

Norm wt% = rock types determined on the basis of weight percent normative minerals

calculated to normative weight percent.

266

The intrusion is interpreted to be flat-lying (sill-like) on Archaean sedimentary and

volcanic rocks and Gowganda Formation with preserved thicknesses, estimated from

diamond drill hole intersections, ranging from 45 m to 360 m, with variability in

thicknesses attributed to block-faulting (Meyn, 1977).

There are no known sulphide occurrences in the immediate area of the sample

section, although there are several small sulphide (chalcopyrite-pyrite) showings

documented within the larger intrusive body (Meyn, 1977). This sample suite was

collected mainly to provide background values from what appears to be an extremely

undifferentiated intrusion in proximity to Archaean rocks.


CIPW normative calculations were completed on the nine samples from the Manitou

Lake section (Table 5-18). Eight of the nine samples classify as quartz-hypersthene-

normative (silica-oversaturated) gabbro. One sample (JB97-32) classifies as a nepheline-

olivine-normative (silica-undersaturated) olivine leucogabbronorite with 19.7%

normative olivine, 8% normative diopside, and 1% normative nepheline, suggesting a

slightly more alkalic gabbro relative to typical sub-alkaline Nipissing Gabbro (see

Appendix 1).


Primitive mantle-normalized multi-element diagrams for rocks from the Manitou

Lake section are shown in Figure 5-71. With the exception of sample JB97-32, the

uppermost gabbro, all of the gabbroic rocks show similar trace and rare-earth element

patterns and abundances, with the seven lowermost samples clustering around average

chilled margin gabbro (~1-50 times primitive mantle). These eight samples also display

negative Nb+Ta, P* and Ti* anomalies and moderate LILE enrichment, which are typical

features of Nipissing Gabbro magmas. The pattern of sample JB97-32 is quite different

than that of the other samples, having unusually low Rb and Th values, a positive Sr

peak, and exhibiting positive P* and Ti* anomalies.

267

1

10

100

1000


Sam

ple/

Prim

itive

Man

tle

JB97-32 (S)

JB97-31

JB97-30

JB97-29

JB97-28

JB97-27

JB97-26

JB97-25

JB97-24 (N)

Chilled Margin Avg


Aplite Avg (PL)

A gabbro (CIPW)) olivine leucogabbronorite (CIPW)

Figure 5-71. Primitive mantle-normalized multi-element diagrams for rock samples from

the sample section in the Manitou Lake intrusion, Clement Township. Values for

average chilled margin gabbro (this study), average Huronian Sedimentary rocks (this

study) and average aplite (Lightfoot and Naldrett, 1996) are shown for comparison.

Mantle normalizing values are from McDonough and Sun (1995).

268


None of the samples have visible sulphide and are characterized by average

concentrations of 0.06 wt% S, 128 ppm Cu, and 99 ppm Ni. The highest concentrations

of Pt+Pd are from samples JB97-29 (~8.4 ppb Pt+Pd; 1.1 Pd/Pt; 1.5 Cu/Ni) and JB97-30

(~9.6 ppb Pt+Pd; 3.2 Pd/Pt; 1.3 Cu/Ni). Only 1 sample (JB97-29) analyzed greater than

the lower limits of detection for Ir, Ru, Rh, Pt, Pd and Au. Except for sample JB97-32

(S/Se = 5785) , all of the S/Se ratios plot within the range (1000-5000) of uncontaminated

magmatic sulphide (Naldrett, 1981) and all of the samples, except JB97-27, have Pd/Se

ratios which are indicative of second-stage (fertile) magmas. Elevated values for Cu/Pd

(>>19,000) suggest that these rocks underwent sulphide segregation early on, resulting in

loss of Pd relative to Cu (Barnes et al., 1988; Prendergast and Keays, 1989; Hoatson and

Keays, 1989), which attests to the barren nature of these rocks.

5.12 Chiniguchi River Intrusion - Detail

The Chiniguchi River intrusion is located in Janes Township, about 50 km northeast

of the City of Greater Sudbury (Figs. 1-2 and 5-1). Dressler (1979) mapped and

described the Chiniguchi River intrusion, and other intrusions in the area, as irregularly

shaped or sill-like bodies (Figs. 5-1 and 5-72). Samples were collected from four areas

within the Chiniguchi River intrusion, encompassing 26 samples from the immediate area

of the Jackie Rastall (Rastall) occurrence, two samples from the KTO showing, five

samples from the NKTO showing, one sample from the northeast portion of the intrusion,

and one sample from the chilled margin of the intrusion, west of the Rastall occurrence

(Fig. 5-72). One sample was collected from the Sargesson Lake occurrence (Sargesson

Lake intrusion), located about 3.5 km to the east (Fig. 5-72). A summary of the samples

is provided in Table 5-19 and a complete listing of the data is provided in Appendix 1.


The Chiniguchi River intrusion, the largest continuous body of Nipissing Gabbro in

Janes Township, has an irregular shape with thicknesses, derived from historic diamond

drill hole intersections and current field observations, ranging from a few metres near the

contacts to 767 m within the central parts of the intrusion (Dressler, 1979).

269

Figure 5-72. General geology and location of rock samples from the Chiniguchi River

and Sargesson Lake intrusions, Janes Township. Geology after Dressler (1979).

270


JB98-224 G (Q-H) 0.059 222 122 0.069 - 0.207 9.530 10.720JB97-40A G (Q-H) 0.090 362 120 - - 0.250 - 1.910JB97-40B G (Q-H) 0.970 4892 650 0.170 - 1.000 3.260 5.920JB97-41A G (Q-H) 0.120 620 170 - - - - 2.260JB97-41B G (Q-H) 1.180 5201 850 0.199 - 0.160 4.992 7.777JB97-41C G (Q-H) 0.120 425 150 - - - - 3.364JB97-42A G (Q-H) 0.110 524 160 - - - - -JB97-42B G (Q-H) 1.860 9892 1300 0.310 1.150 0.750 7.100 9.130JB97-67 G (Q-H) 0.032 152 42 - - - 17.000 32.000

JB97-106A G (Q-H) 0.065 400 124 - - 1.100 21.000 38.000JB97-106C G (Q-H) 0.039 400 117 0.200 - 0.700 12.000 20.000JB97-43A G (Q-H) 3.500 21450 5400 2.943 4.998 - 798.710 7223.970JB97-43B G (Q-H) 0.040 201 140 - - 0.610 10.370 20.260JB97-43C G (Q-H) 2.710 16732 4300 1.300 7.190 12.280 284.500 1577.320JB97-43D G (Q-H) 0.390 2757 720 0.250 1.110 1.190 35.450 80.030JB97-95 G (Q-H) 0.450 3525 868 - - - 35.110 66.090JB97-96 - 3.020 18285 4941 1.320 3.770 1754.750 345.100 7135.610

JB97-106B G (Q-H) 0.049 400 121 0.200 - 0.200 11.000 18.000JB97-107 G (Q-H) 0.044 200 178 0.200 - 0.900 28.000 61.000JB97-108 G (Q-H) 0.035 500 149 0.200 - 0.600 11.000 15.000JB97-109 LG (Q-H) 5.323 35190 10560 2.400 - 23.000 1300.000 4560.000JB97-104 G (Q-H) 0.059 500 190 - - 0.600 11.000 6.000JB97-105 G (Q-H) 0.022 200 135 0.500 - 1.400 30.000 40.000JB97-87A G (Q-H) 0.027 204 58 na na na 12.000 25.000JB97-87B G (Q-H) 0.121 640 218 na na na 53.000 335.000JB97-87C G (Q-H) 1.780 8602 3029 na na na 429.000 2750.000JB97-87D G (Q-H) 3.183 15941 4995 na na na 549.000 3218.000JB97-87E G (Q-H) 2.169 12458 3535 na na na 503.000 3364.000JB97-87F G (Q-H) 2.341 11944 3698 na na na 423.000 2438.000JB97-87G G (Q-H) 1.780 8456 2284 na na na 283.000 1541.000JB97-87H G (Q-H) 1.826 8640 2790 na na na 285.000 1623.000JB97-87I G (Q-H) 1.117 5426 1626 na na na 160.000 905.000JB97-87J G (Q-H) 0.716 4700 1014 na na na 126.000 627.000JB97-87K G (Q-H) 0.097 568 161 na na na 17.000 51.000JB97-115* G (Q-H) 0.770 5683 1116 0.255 0.380 1.012 101.000 116.600

Table 5-19. Summary of whole-rock geochemical characteristics for samples from the Chiniguchi River intrusion, Janes Township. One sample (JB97-115) is from the Sargesson Lake intrusion. *sample from Sargesson Lake occurrence; "-" below lower limit of detection; "N" = primitive mantle-normalized; "na"=not analyzed; G=gabbro; OLGN=olivine leucogabbronorite; LG=leucogabbro; GN=gabbronorite; Q-H=quartz-hypersthene; H-O=hypersthene-olivine; Q-H-C=quartz-hypersthene-corundum. Norm wt% = rock types determined on the basis of weight percent normative minerals calculated to normative weight percent.

271


ppb ppm ppmJB98-224 4.730 114 2658 1.1 0.9 60 46 1.80JB97-40A 2.440 160 2486 - 1.3 65 33 2.08JB97-40B 21.030 2300 1983 1.8 3.5 61 33 1.96JB97-41A 4.006 520 1935 - 3.1 66 36 2.16JB97-41B 19.907 3000 2269 1.6 3.5 64 25 2.05JB97-41C 2.275 240 2824 - 1.6 69 28 2.07JB97-42A 4.650 430 2099 - 2.7 68 25 2.07JB97-42B 28.210 4900 1880 1.3 3.8 61 24 1.99JB97-67 1.000 94 2105 1.9 2.2 71 26 1.90

JB97-106A 2.200 90 1625 1.8 0.7 67 34 2.13JB97-106C 1.900 86 975 1.7 0.7 64 38 2.18JB97-43A 462.714 13000 1632 9.0 2.4 56 29 2.02JB97-43B 3.790 110 1990 2.0 0.8 67 37 1.98JB97-43C 352.750 11000 1620 5.5 2.6 58 28 1.94JB97-43D 45.920 1600 1415 2.3 2.2 71 25 1.86JB97-95 44.370 1908 1277 1.9 2.2 70 22 1.51JB97-96 404.250 13069 1652 20.7 2.6 29 2.00

JB97-106B 2.700 71 1225 1.6 0.6 65 35 2.18JB97-107 3.700 129 2200 2.2 0.7 72 24 2.02JB97-108 0.800 87 700 1.4 0.6 69 28 1.91JB97-109 720.000 17080 1513 3.5 1.6 46 52 3.10JB97-104 11.000 250 1180 0.5 1.3 73 22 1.93JB97-105 1.800 77 1100 1.3 0.6 72 22 1.91JB97-87A 3.000 87 1324 2.1 1.5 66 36 2.06JB97-87B 33.000 660 1891 6.3 3.0 65 36 2.04JB97-87C 261.000 7031 2069 6.4 2.3 59 32 2.07JB97-87D 538.000 9458 1997 5.9 1.9 56 30 1.93JB97-87E 455.000 10301 1741 6.7 2.9 59 31 2.16JB97-87F 410.000 9468 1960 5.8 2.6 58 32 2.09JB97-87G 337.000 6227 2105 5.4 2.7 61 30 2.01JB97-87H 279.000 5891 2113 5.7 2.1 62 29 1.99JB97-87I 160.000 3769 2058 5.7 2.3 65 29 2.16JB97-87J 156.000 3072 1523 5.0 3.0 66 29 2.07JB97-87K 15.000 341 1708 3.0 2.1 68 32 2.06JB97-115* 157.300 3217 1355 1.2 2.9 66 32 1.97

Table 5-19 (cont). Summary of whole-rock geochemical characteristics for samples from the Chiniguchi River intrusion, Janes Township. One sample (JB97-115) is from the Sargesson Lake intrusion. *sample from Sargesson Lake occurrence; "-" below lower limit of detection; "N" = primitive mantle-normalized; "na"=not analyzed; G=gabbro; OLGN=olivine leucogabbronorite; LG=leucogabbro; GN=gabbronorite; Q-H=quartz-hypersthene; H-O=hypersthene-olivine; Q-H-C=quartz-hypersthene-corundum.

272

The deepest drill-indicated portion of the intrusion is located in the area of samples 40A

and 40B (Fig. 5-72). Dressler (1979) interpreted the variations in preserved thicknesses

to be the result of either folding of a tabular, sill-like body or the primary shape of an

oblong lopolith-like intrusion. The Chiniguchi River intrusion and its extensions toward

the north and southwest are hosted by Gowganda Formation (greywacke, quartz arenite,

arkose, conglomerate) sedimentary rocks (Dressler, 1979). The Sargesson Lake

intrusion, interpreted to be a satellite intrusion emanating from the Chiniguchi River

intrusion, is hosted by Lorrain Formation (quartz arenite, arkose) sedimentary rocks

which stratigraphically overly the Gowganda Formation; this suggests that the Sargesson

Lake intrusion is located stratigraphically “above” the Chiniguchi River intrusion. A

large Sudbury Swarm dike cuts through the central region of the Chiniguchi Lake

intrusion, striking northwest through the area of the Kukagami Lake and Rathbun Lake

intrusions (Fig. 5-1).

The most common rock types in the Chiniguchi River intrusion are medium-grained

gabbro (locally variable to leucogabbro) and medium-grained orthopyroxene gabbro.

Other rock types, typical of Nipissing Gabbro intrusion, were also noted including vari-

textured gabbro and pegmatitic gabbro; the latter commonly contains bleb chalcopyrite

and pyrrhotite but has only anomalous PGE concentrations (<100 ppb 3E). Contacts with

the Huronian sedimentary rocks are typically sharp, with a chilled to fine-grained gabbro

extending no more than one metre into the main intrusive body; rarely, fragments of

sedimentary rocks were observed in chilled margin gabbro (Photo 5-6a).

Several PGE-Cu-Ni sulphide showings occur within the intrusive bodies in Janes

Township; the two most significant are the Rastall and Sargesson Lake occurrences (Fig.

5-72). At the Rastall occurrence, work by Goldwright Explorations Inc. and Pacific

North West Capital Corp. between 1998 and 2000 included surface trenching and

sampling, and diamond drilling (Jobin-Bevans et al., 1999; Meyer et al., 2000, 2001).

The Rastall occurrence consists of a series of trenches and stripped areas that

intermittently expose sulphide mineralization over a northeast-trending (30°) strike length

of ~500 m (Fig. 5-73). Exposed surface widths of sulphide mineralization range 1-22 m

and are widest in Trench 1 (Photo 5-6b), which is centrally located in the 500 m long

mineralized zone (Fig. 5-73). In general, sulphide mineralization is dominated by

273

chalcopyrite (chalcopyrite to pyrrhotite to pentlandite of 4:2:1), ranges from 1% to 10%

total sulphide and is hosted by medium-grained, massive, orthopyroxene-bearing (1-10%

hypersthene) gabbro. The orthopyroxene-bearing gabbro unit is in gradational contact

with a gabbro unit to the east and is within about 10-50 m of the footwall gabbro-

sediment contact to the west. At surface, the footwall contact of the gabbroic body dips

at about 30-45° southeast and based on the drilling results, shallows to about 25° down-

dip of the surface showings (Fig. 5-74). Surface exposures of semi-massive

mineralization occur as small (<2.0 m diameter) pods rich in chalcopyrite, pyrrhotite and

pentlandite (Fig. 5-7a). Distribution of these pods may be in part structural, whereby

disseminated sulphides have become concentrated along localised fractures and/or faults

and/or joint planes and/or contacts (Photo 5-7b). Sulphide breccia, consisting of

fragments of sedimentary rocks and gabbroic rocks cemented by a mixture of fine-

grained carbonate and chalcopyrite, have been noted in several drill intersections (Photo

4-6).

In addition to diamond drilling, detailed surface sampling using continuous channel

samples was completed by Pacific North West Capital Corp. in 1998. A summary of

results from the diamond drilling and surface channel sampling programs are provided in

Tables 5-20 and 5-21, respectively. In reference to Table 5-21, samples C, D and E were

taken across a northeast-trending gabbro-sediment contact that is exposed in Trench 4

(Fig. 5-73); sample C is located about 9.25 m southeast of sample B, sample D about 0.6

m southwest of sample C, and sample E about 1.5 m southwest of sample C.

Pacific North West Capital Corp. also completed several diamond drill holes at the

Sargesson Lake occurrence, intersecting anomalous PGE-Cu-Ni values over 10’s of

metres (Meyer et al., 2000); a summary of the drill results is provided in Table 5-22.

Sulphide mineralization (chalcopyrite ≈ pyrrhotite > pentlandite) ranges from 1-5% total

sulphide and is as at the Rastall occurrence, hosted by medium-grained, massive,

orthopyroxene-bearing gabbro and gabbro. The orthopyroxene gabbro unit is gradational

into gabbro-leucogabbro toward the southeast and this sulphide-bearing unit occurs

within about 50 m of the footwall gabbro-sediment contact to the northwest. On the basis

of diamond drilling, the footwall contact (northwest) of the gabbroic body dips at about

30-45° southeast.

274

Photo 5-6. Chiniguchi River Intrusion. (A) Fragments of Huronian sedimentary rocks in very-fine-grained to chilled margin gabbro near Trench 4 at the Rastall occurrence, Janes Township. The Canadian 25 cent piece is about 2.2 cm in diameter. (B) Exposed sulphide mineralization (gossan) of Trench 1 at the Rastall occurrence; the sulphides are hosted by orthopyroxene gabbro and gabbro. The photo was taken looking toward the west and the trend of mineralization is from left to right. The surface exposure is about 25 m wide.

275

Figure 5-73. Schematic map of the Rastall property (Janes Township) showing the

locations of drill holes (selected projections and collars), trenches, the contact between

the Nipissing Gabbro intrusion and sedimentary country rocks, and assay values from

drill hole intersections. The cross-section in Figure 5.12-3 is constructed from drill holes

JR99-01, 06 and 11. The composite section examined in Section 5.13 is from drill holes

JR99-01 and 06.

276

Figure 5-74. Schematic drill hole cross-section (looking ~north) through the area of drill

holes JR99-01, 06 and 11 at the Rastall property, Janes Township. The location of

Trench 1 and the general geology and mineralization intersected in the drill holes is also

shown. The composite section examined in Section 5.13 uses data from drill holes JR99-

01 and 06. The location of this drill section is shown in Figure 5.12-2.

277


Samples of gabbroic rock from the Chiniguchi River intrusion are characterized by

averages of 48.9 wt% SiO2, 0.46 wt% TiO2, 13.8 wt% Al2O3, 8.6 wt% MgO, and Mg-

number of 64; the sample (JB97-115) from the Sargesson Lake intrusion is characterized

by 49.9 wt% SiO2, 0.45 wt% TiO2, 13.4 wt% Al2O3, 9.0 wt% MgO, and Mg-number of

66. Gabbroic samples from the Chiniguchi River intrusion with high S (>0.05 wt% S)

are characterized by averages (n=26) of 49.0 wt% SiO2, 0.45 wt% TiO2, 13.5 wt% Al2O3,

8.4 wt% MgO, and Mg-number of 63 and samples with low S (<0.05 wt% S) are

characterized by averages (n=8) of 50.2 wt% SiO2, 0.47 wt% TiO2, 14.4 wt% Al2O3, 8.6

wt% MgO, and Mg-number of 68. CIPW normative calculations were completed on 34

of the 35 samples and these are summarized in Table 5-19. With the exception of sample

JB97-109 which classifies as a quartz-hypersthene-normative leucogabbro, all of the

samples classify as quartz-hypersthene-normative (silica-oversaturated) gabbro.

Drill Hole Location From To Int. 3E Cu Nim m m ppm wt% wt%

JR99-01 ~50 m east of 35 50.05 15.05 3.1 1.08 0.27Trench 1

including -- -- -- 4.64 3.93 1.68 0.26JR99-11 same collar as 32.52 48.68 16.16 2.15 0.64 0.27

JR99-01including -- -- -- 5.67 3.07 0.7 0.31JR99-06 ~30 m south and 10 m east of Trench 1 9.9 23.91 14.01 2.07 0.84 0.35

including -- -- -- 2.4 4.45 0.87 0.47JR99-02 ~0.5 m northwest of channel sample C 7.78 11 3.22 2.49 1.34 0.65

including -- -- -- 0.64 5.25 3.37 1.67JR99-03 ~10 m north of 0 8.68 8.68 4.45 0.69 0.44

JR99-02including -- -- -- 3.06 9.03 1.2 0.91JR99-08 ~30 m south of 35.83 37.37 1.55 6.71 0.35 1.1

JR99-03 Table 5-20. Summary of drill core assay results from diamond drilling by Pacific North West Capital Corp. (1999) at the Rastall property in the Chiniguchi River intrusion, Janes Township. Results are from Jobin-Bevans et al. (1999). Values for 3E = Pt+Pd+Au and Int. = interval.

278

Location Interval Pd Pt Au 3E Cu Nim ppm ppm ppm ppm wt% wt%

Trench 1 13.34 3.52 0.44 0.4 4.36 1.04 0.42including 5.8 -- -- -- 5.08 -- --Trench 10 4.87 1.07 0.19 0.18 1.44 0.33 0.1Trench 4 2.74 2.92 0.62 0.18 3.72 0.51 0.36

(sample A)Trench 4 4.97 3.42 0.73 0.27 4.42 0.55 0.24

(sample B)Trench 4 0.53 31.2 17.2 1.3 49.7 3.41 0.4

(sample C)Trench 4 2.8 13.4 6.2 2.2 21.8 0.61 0.24

(sample D)including 0.8 61.5 18.9 3.2 83.6 1.63 0.08including 0.4 78.4 18.5 5.5 102.4 -- --Trench 4 2.63 -- -- -- 5.2 -- --

(sample E)

Table 5-21. Summary of surface channel sample assay results, collected by Pacific North

West Capital corp. (1998), from the Rastall property in the Chiniguchi River intrusion,

Janes Township. Results are from Jobin-Bevans et al. (1999). Sample B is located about

3.25 m northeast and parallel to sample A – see text for description. Values for 3E =

Pt+Pd+Au.

279

Drill Hole From To Interval 3E Cu Ni Cu+Nim m m ppm wt% wt% wt%

SL99-01 15.1 17 1.9 0.37 0.34 0.12 0.46SL99-01 30 31.2 1.2 1.34 0.19 0.13 0.32SL99-02 25 28.7 3.7 0.41 0.31 0.11 0.42SL99-02 31.25 39.3 8.05 0.33 0.26 0.09 0.35SL99-02 41.45 44 2.55 0.66 0.21 0.13 0.34SL99-03 23 26.55 3.55 0.31 0.05 0.03 0.08SL99-04 8 9.5 1.5 0.3 0.03 0.02 0.05SL99-04 48.6 51.5 2.9 0.71 0.1 0.06 0.16SL99-05 13.5 21 7.5 0.58 0.33 0.14 0.47including 14 17.5 3.5 0.71 0.43 0.18 0.61SL99-05 22.65 25.95 3.3 0.41 0.18 0.08 0.26SL99-06 36.95 37.15 0.2 0.45 0.14 0.11 0.25SL99-06 44.3 55.25 10.95 0.74 0.47 0.21 0.68including 45 53 8 0.88 0.61 0.26 0.87SL99-06 56 58.47 2.47 0.27 0.02 0.06 0.08

Table 5-22. Summary of drill core assay results from diamond drilling by Pacific North

West Capital Corp. (1999) at the Sargesson Lake occurrence in the Sargesson Lake

intrusion, Janes Township. Results are from (Meyer et al., 2000). Values for 3E =

Pt+Pd+Au.

280

Sample JB97-109 is a medium-grained orthopyroxene gabbro containing ~15% visible

sulphide (chalcopyrite, pyrrhotite, pentlandite), collected from the northern part of the

mineralized trend (Trench 4) at the Rastall occurrence (Fig. 5-73; Photo 5-7).

All of the samples plot with much lower TiO2 concentrations than average chilled

margin gabbro and the sample of chilled margin gabbro (JB98-224) from the Chiniguchi

River intrusion, and the vast majority of samples have higher MgO concentrations than

average chilled margin gabbro (Fig. 5-75). This same characteristic is recorded in other

intrusions in this study (i.e. Charlton Lake, Bell Lake, and Kukagami Lake intrusions)

and as in the other intrusions this feature is attributed to the presence of orthopyroxene

phenocrysts in much of the gabbro that makes up the Chiniguchi River intrusion.


Ratios of (La/Sm)N and (Th/Nb)N show little evidence for local crustal contamination

in either the mineralized (>0.05 wt% S) or unmineralized (<0.05 wt% S) rocks and

moreover, the ratios are tightly constrained, ranging ~4-8 (Th/Nb)N and ~1.8-2.2

(La/Sm)N, which suggests a major contamination event in a deeper seated magma

(staging) chamber. As with many of the mineralized Nipissing Gabbro intrusions in this

study (Fig. 5-13), the Pd concentrations from these samples show no correlation with

either of these ratios, indicating that the sulphide mineralizing event was independent of

this major contamination event. The values of the two samples that fall outside of these

ranges are the result of local contamination. For example, sample JB97-109 (5.3 wt% S,

1300 ppb Pt, 4560 ppb Pd, 17080 ppm Cu, 10560 ppm Ni) which has very high ratios, is

extensively altered and was collected from Trench 4 at the Rastall occurrence (Fig. 5-73),

within ~1-2 m from the contact with sedimentary country rock, and proximal to a

sediment-gabbro breccia.

Primitive mantle-normalized multi-element diagrams for samples from the

Chiniguchi River intrusion are shown in Figure 5-76; one sample (JB97-115) is from the

Sargesson Lake intrusion (Fig. 5-72). With the exception of the patterns exhibited by the

LILE, the patterns from all of the rocks are near-parallel and typical of Nipissing Gabbro

with relatively elevated LILE (~1-50 times primitive mantle) and negative Nb+Ta, P*

and T* anomalies; variations in the LILE are likely the result of alteration and subtle re-

mobilization of these elements.

281

Photo 5-7. Chiniguchi River Intrusion, Rastall occurrence (Trench 4). (A) Gossan from semi-massive to massive sulphide mineralization proximal to the contact (shown as dashed line) with sedimentary rocks. At this exposure, the gabbro forms a tongue-like body into the surrounding sediments. The surface exposure is about 6 m wide. (B) Malachite-stained (malachite) sulphide mineralization at the sheared and brecciated (sediment-gabbro breccia) contact with fine-grained (chilled) gabbro. The Canadian one dollar coin is about 2.5 cm in diameter.

282

0.2

0.3

0.4

0.5

0.6

0.7

0.8

0.9

4567891011

MgO (wt%)

TiO

2 (w

t%)

JB98-224JB97-40AJB97-40BJB97-41AJB97-41BJB97-41CJB97-42AJB97-42BJB97-67JB97-106AJB97-106CJB97-43AJB97-43BJB97-43CJB97-43DJB97-95JB97-106BJB97-107JB97-108JB97-109JB97-104JB97-105JB97-87AJB97-87BJB97-87CJB97-87DJB97-87EJB97-87FJB97-87GJB97-87HJB97-87IJB97-87JJB97-87KJB97-115Chilled Margin Avg

fractionation

(B) B A ) gabbro (CIPW)+ leucogabbro (CIPW)D chilled margin gabbro (CIPW gabbro)

Figure 5-75. Bivariate scatter plot of MgO versus TiO2 for rock samples from the

Chiniguchi River and Sargesson Lake (JB97-115) intrusions. Average chilled margin

gabbro is from this study.

283

0.1

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Sam

ple/

Prim

itive

Man

tle

JB98-224

Chilled Margin Avg

D chilled margin gabbro (CIPW gabbro)

(A) CHILLED MARGIN GABBRO

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Sam

ple/

Prim

itive

Man

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JB97-41AJB97-43AJB97-43CJB97-95JB97-96JB97-109JB97-87CChilled Margin Avg

B A ) gabbro (CIPW)+ leucogabbro (CIPW)

(B) ATYPICAL SAMPLE PROFILES

Figure 5-76. Primitive mantle-normalized multi-element diagrams for rock samples from the Chiniguchi River and Sargesson Lake (JB97-115) intrusions, Janes Township. Mantle normalizing values are from McDonough and Sun (1995).

284


Mineralized samples (>500 ppm Cu and >0.1 wt% S) were collected from 4 areas;

15 samples from the Rastall occurrence, one sample from the Sargesson Lake occurrence,

one sample from the KTO showing, and 4 samples from the NKTO showing (Fig. 5-72).

The sulphides are primarily disseminated and bleb textured, ranging from 1-5 volume %,

and dominated by chalcopyrite and pyrrhotite with subordinate pentlandite and rare

pyrite. The highest concentrations of PGE, collected from Trench 1 at the Rastall

occurrence (Fig. 5-73), are from samples JB97-43A (~8023 ppb Pt+Pd; ~9.0 Pd/Pt; ~2.4

Cu/Ni), JB97-96 (~7481 ppb Pt+Pd; ~20.7 Pd/Pt; ~2.7 Cu/Ni), and JB97-109 (~5860

Pt+Pd; ~3.5 Pd/Pt; ~1.6 Cu/Ni); a series of 7 samples, also collected from Trench 1, have

concentrations ranging from 1065 ppb Pt+Pd to 3867 ppb Pt+Pd (average ~5.9 Pd/Pt,

~2.4 Cu/Ni). Metal ratios in the mineralized (>0.05 wt% S) samples average 6.6 Pd/Pt

and 2.3 Cu/Ni with a median of 4.7 Pd/Pt and 3.2 Cu/Ni, and unmineralized (<0.05 wt%

S) samples average 1.8 Pd/Pt and 0.8 Cu/Ni with a median of 1.9 Pd/Pt and 0.7 Cu/Ni.

These high Pd/Pt and Cu/Ni ratios are indicative of fractionated sulphides.

There is strong correlation between concentrations of Cu-Pt and Cu-Pd (Fig. 5-77),

as well as S-Pt and S-Pd, indicating that the PGE are largely sulphide controlled. The

bivariate plots in Figure 5-77 also exhibit two distinct groups. Group-1 consists of

unmineralized and mineralized samples from the Rastall and Sargesson Lake

occurrences, includes the sample of chilled gabbro and average chilled margin gabbro,

and has higher concentrations of Pt and Pd relative to Group-2. Group-2 consists solely

of mineralized samples (>0.05 wt% S) collected from the KTO and NKTO showings

(Fig. 5-73).

With the exception of two unmineralized samples, the whole-rock S/Se

concentrations of the rocks lie within the field of uncontaminated magmatic sulphides

(Naldrett, 1981), between 1000 and 5000 S/Se; the two samples (JB97-106C and JB97-

108) that have <1000 S/Se have probably suffered some loss of S through weathering

(Fig. 5-78a). Figure 5-78b is a plot of Se versus Pd, useful for discriminating between

rocks that formed from S-undersaturated (second-stage or fertile) versus S-saturated

(first-stage or infertile) magmas such as MORB (Peck et al., 2001).

285

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10 100 1000 10000 100000

Cu (ppm)

Pt (p

pb)

JB98-224 Chill

<0.05wt% S

>0.05wt% S

Chilled Margin Avg

Group-1

Group-2

(A)

1

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100

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10 100 1000 10000 100000

Cu (ppm)

Pd (p

pb)

JB98-224 Chill

<0.05wt% S

>0.05wt% S

Chilled Margin Avg

Group-1

Group-2

(B)

Figure 5-77. Scatter plots of whole-rock chalcophile elements for rock samples from the Chiniguchi River and Sargesson Lake intrusions. (A) Variations in Cu and Pt. (B) Variations in Cu and Pd.

286

1

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100

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100 1000 10000

S/Se

Pd (p

pb)

JB98-224 Chill<0.05wt% S>0.05wt% SChilled Margin AvgHuronian Sediment Avg

sulphur loss magmaticcontamination

+R-factor

JB97-115

JB97-108

JB97-106C

(A)

Figure 5-78a. Discrimination diagram of S/Se versus Pd plotting unmineralized (<0.05

wt% S), mineralized (>0.05 wt% S) and chilled gabbro samples from the Chiniguchi

River and Sargesson Lake intrusions, Janes Township. Samples with S/Se ratios that

range 1,000 to 5,000 are within the range of uncontaminated magmatic sulphides

(Naldrett, 1981) and samples with S/Se <1,000 are attributed to sulphur loss through

weathering or other secondary processes (Reeves and Keays, 1995). Value for average

chilled margin gabbro is from the current study.

287

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Se (ppb)

Pd (p

pb)

JB98-224 Chill<0.05wt% S>0.05wt% SChilled Margin AvgHuronian Sediment AvgMORB Avg



Average MORB

41C

41A

42A40A

41B

40B

42B

(B)

Figure 5-78b. Discrimination diagram of Se versus Pd plotting unmineralized (<0.05

wt% S), mineralized (>0.05 wt% S) and chilled gabbro samples from the Chiniguchi

River and Sargesson Lake intrusions, Janes Township. Value for average chilled margin

gabbro is from the current study. Value for average MORB is from Hamlyn and Keays

(1986).

288

All of the unmineralized samples, along with the chilled gabbro and average chilled

gabbro, plot within the field of second-stage magmas, implying that the source magmas

were PGE metal-fertile magmas which had not previously undergone sulphide

segregation. Seven of the samples, all collected from either the KTO or NKTO sample

sites (Fig. 5-72), plot within the field of first-stage or S-saturated magmas. These

sulphides are extremely enriched in base metal concentrations relative to PGE (~71,338

to 536,692 Cu/Pd) and have clearly precipitated from a magma that has already

experienced sulphide segregation. This suggests that this region of the Chiniguchi River

intrusion has either been fed by a S-saturated magma that was severely deleted in PGE or

that there are PGE-rich sulphide elsewhere in the intrusion.

The majority of samples, and in particular all of the unmineralized (<0.05 wt% S)

samples, have Cu/Pd values of <6500; mineralized samples (>0.05 wt% S) and chilled

gabbro have >6500 Cu/Pd values. Hoatson and Keays (1989) suggested that rocks with

Cu/Pd values >6500 have undergone earlier sulphide segregation and would therefore

contain relatively depleted concentrations of Pd. Within the current sample suite, Pd

concentrations are clearly anomalous and perhaps more significantly, unmineralized

samples have Cu/Pd values that are <6500. Assuming that chilled gabbro represents the

composition of a particular parent magma, then it follows that the rocks sampled from

within the intrusion did not form directly from this same magma. Moreover, although

these magmas are likely related, they clearly represent two differing magma

compositions, either as a result of their petrogenesis, their bulk (source) composition, or

both.

Figure 5-79, a discrimination plot of Ni/Cu versus Pd/Ir is useful to determine

whether or not sulphides are magmatic or hydrothermal in origin, with increasing Pd/Ir

and decreasing Ni/Cu values trending towards a hydrothermal origin. The majority of

samples plot within the region of layered intrusions as described by Barnes (1990), and

these sulphides are interpreted to be magmatic. In contrast, 4 of the mineralized samples,

containing some of the highest concentrations of Pt+Pd, plot near or within the field of

hydrothermal mineralization (Barnes, 1990), suggesting remobilized sulphide.

289

0.01

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100

1000

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100000

0.01 0.1 1 10 100 1000

Ni/Cu

Pd/Ir

JB98-224 Chill<0.05wt% S>0.05wt% SChilled Margin AvgHuronian Sediment Avg

hydrothermal

increased fractionation

mantle

+chromite+olivine

JB97-115

96

43A

43C

109

layered intrusions

Figure 5-79. Discrimination diagram of Ni/Cu versus Pd/Ir of mineralized (>0.05 wt%

S), unmineralized (<0.05 wt% S), and chilled margin gabbro samples from the

Chiniguchi River and Sargesson Lake intrusions, Janes Township. The fields of mantle,

layered intrusions and hydrothermal are approximated from Barnes (1990).

290

Primitive mantle-normalized PGE and chalcophile diagrams (recalculated to metal in

100% sulphide) for 15 mineralized and unmineralized samples that have complete or

near-complete PGE data are shown in Figures 5-80 and 5-81; concentrations of PGE that

are below the lower limit of detection, which are more commonly Ir, Ru and Rh, are

assigned the average value of the lower limit of detection (i.e. Ir = 0.27 ppb; Ru = 0.66

ppb; Rh = 0.26 ppb; Pt = 1.43 ppb; Pd = 1.88 ppb). All of the sulphides are characterized

by positive slopes that approximate those profiles of average chilled margin gabbro and

average flood basalt (Naldrett, 1981) and define two distinct sets of profiles. Group-1

comprises unmineralized (<0.05 wt% S) samples and the sample of chilled gabbro (0.059

wt% S), and Group-2 samples comprise mineralized (>0.05 wt% S) samples (Fig. 5-81).

Group-1 samples have higher overall PGE abundances and slightly shallower positive

slopes, relative to Group-2 samples. Conversely, Group-2 samples have steeper positive

slopes and lower PGE abundances, particularly in Ir, Ru and Rh, relative to Group-1 and

are therefore less fractionated than Group-1 sulphides. Three samples (JB97-43A, 96 and

109), which have some of the highest concentrations of Pt+Pd, plot with much different

profiles in comparison to groups 1 and 2 (Fig. 5-80). These samples, which also plot

within or near the field of hydrothermal sulphides on the Ni/Cu versus Pd/Ir diagram

(Fig. 5-79), have patterns that are similar to those of hydrothermal sulphide

mineralization from the East Bull Lake intrusion (Peck et al., 1993a, 1993b) and from the

South Roby Zone, Lac des Iles Complex (J. Hinchey, unpublished data, 2004).

Indications of hydrothermal mineralization, combined with the magmatic S/Se

values and other indications that these sulphides are magmatic, suggest that a number of

the samples from this sample suite have suffered a hydrothermal overprint. This

interpretation is supported by the mineralogy of the Cu-sulphides which tend to be locally

recrystallized along micro-structures and veinlets as observed in hand samples and thin

sections (Appendix 2).

291

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al in

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ulph

ide/

Prim

itive

Man

tle

JB98-224JB97-40BJB97-41BJB97-42BJB97-106CJB97-43AJB97-43CJB97-43DJB97-96JB97-106BJB97-107JB97-108JB97-109JB97-105JB97-115Chilled Margin AvgFlood Basalt Avg

A gabbro (CIPW)+ leucogabbro (CIPW)D chilled margin gabbro (CIPW gabbro)

(A)


(recalculated to metals in 100% sulphide) for sulphides from all rock samples,

Chiniguchi River and Sargesson Lake intrusions, Janes Township. Data for average

chilled margin is from this study and data for average flood basalt is from Naldrett

(1981). Mantle normalizing values are from Barnes et al. (1988) and McDonough and

Sun (1995).

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10000000


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al in

100

% S

ulph

ide/

Prim

itive

Man

tle

JB97-43A

JB97-96

JB97-109

Chilled Margin Avg

Flood Basalt Avg

Lac des Iles SRZ Avg


A gabbro (CIPW)+ leucogabbro (CIPW)

(B)


(recalculated to metals in 100% sulphide) for sulphides with atypical patterns, Chiniguchi

River and Sargesson Lake intrusions, Janes Township. Data for average chilled margin

are from this study; data for average flood basalt is from Naldrett (1981); data for

average Lac des Iles – South Roby Zone (SRZ) is from J. Hinchey (unpublished data,

2004); data for average East Bull Lake intrusion hydrothermal sulphide is from Peck et

al. (1993b). Mantle normalizing values are from Barnes et al. (1988) and McDonough

and Sun (1995).

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al in

100

% S

ulph

ide/

Prim

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Man

tle

JB98-224JB97-106CJB97-106BJB97-107JB97-108JB97-105Chilled Margin AvgFlood Basalt AvgEBL Hydrothermal Avg

A gabbro (CIPW)D chilled margin gabbro (CIPW gabbro)

(A) GROUP-1


(recalculated to metals in 100% sulphide) for sulphides from Group-1 samples,

Chiniguchi River intrusion, Janes Township. Data for average chilled margin is from this

study; data for average flood basalt is from Naldrett (1981); data for average East Bull

Lake intrusion hydrothermal sulphide is from Peck et al. (1993b). Mantle normalizing

values are from Barnes et al. (1988) and McDonough and Sun (1995).

294

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100

% S

ulph

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Prim

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Man

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JB97-40BJB97-41BJB97-42BJB97-43CJB97-43DJB97-115Chilled Margin AvgFlood Basalt AvgEBL Hydrothermal Avg

A gabbro (CIPW)

(B)GROUP-2


(recalculated to metals in 100% sulphide) for sulphides from Group-2 samples,

Chiniguchi River and Sargesson Lake intrusions, Janes Township. Data for average

chilled margin is from this study; data for average flood basalt is from Naldrett (1981);

data for average East Bull Lake intrusion hydrothermal sulphide is from Peck et al.

(1993b). Mantle normalizing values are from Barnes et al. (1988) and McDonough and

Sun (1995).

295

5.13 Rastall Occurrence - Drill Holes JR99-01 and 06

In 1999, Pacific North West Capital Corp. completed a diamond drilling program at

the Rastall occurrence (Figs. 5-1 and 5-72) in Janes Township (Jobin-Bevans et al., 1999;

Meyer et al., 2000, 2001). A portion of the drilling program was targeted at semi-

massive to massive sulphide mineralization intersected at the Rastall occurrence by

Kennco Explorations Inc. (ca. 1968), which reported 1.59% Cu and 1.27% Ni over 10.7

m. This same drill core was re-examined by Falconbridge Ltd. in the late 1980s and was

shown to contain 1.86% Cu, 1.51% Ni, 1780 ppb Pt-Pd-Au over 7.9 m.

Core from two of the diamond drill holes, JR99-01 and JR99-06, was examined as

part of the current study (Fig. 5-73). Diamond drill hole JR99-01 (300 Az, -46

inclination, grid BL0+00/0+29E) is located about 31 m north and 20 m east of JR99-06

(300 Az, -45 inclination, grid L0+31S/0+09E). These 2 drill holes, along with a third

(JR99-11), define a southeast-dipping (25-35°) layer of Cu-Ni-PGE sulphide-bearing

orthopyroxene gabbro with a true width of about 14.0 m and extending a minimum of 60

m down-dip from surface mineralization in Trench 1 (Fig. 5-74). On the basis of field

observations, the increase in the ratio of felsic to mafic minerals in rock samples from

west to east and the increase in the ratio of felsic mafic minerals in core samples upward

through the hole, the western contact is interpreted to be the basal contact of the

intrusion. A total of 23 samples, including a sample of footwall sedimentary rock, were

selected for whole-rock major element, PGE, Au, S, Se, Cu and Ni analyses, comprising

8 samples from drill hole JR99-01 and 15 samples from drill hole JR99-06. These data

were combined into a composite drill hole section (Table 5-23; Fig. 5-74). For the

purposes of plotting, a value of one half of the lower limit of detection is used where

elements have concentrations that are below the lower limits of detection (i.e. Ir = 0.025

ppb; Ru = 0.125 ppb; Rh = 0.125 ppb; Pt = 0.5 ppb; Pd = 0.5 ppb; Au = 0.5 ppb). A

complete listing of the data, along with drill core logs, are provided in Appendix 3.


The 22 core samples of intrusive rocks from the composite drill hole section are

characterized by 48.3 wt% SiO2, 0.42 wt% TiO2, 14.0 wt% Al2O3, 9.1 wt% MgO, and

Mg-number of 67. The main mineralized zone, consisting of 9 core samples from 12.54

m to 23.09 m, is characterized by 47.8 wt% SiO2, 0.42 wt% TiO2, 13.9 wt% Al2O3, 8.5

296

wt% MgO, and Mg-number of 63. All of the samples CIPW normative calculations,

completed on the 22 samples (Table 5-19), classify 17 samples as quartz-hypersthene-

normative (silica-oversaturated) gabbro, 4 samples as hypersthene-olivine-normative

(silica-saturated) gabbronorite (~1.4-7.0 wt% normative olivine), and 1 sample as

hypersthene-olivine-normative olivine leucogabbronorite (~27 wt% normative olivine).

In the field, core samples described as vari-textured gabbro classify as CIPW gabbro

and gabbronorite, orthopyroxene gabbro classify mainly as gabbro and subordinate

gabbronorite, and gabbro classify as gabbro and olivine leucogabbronorite. Except for

sample 44725, a medium-grained massive gabbro (CIPW olivine leucogabbronorite)

which plots in the field of alkaline rocks.

In comparison to average chilled margin gabbro, all of the samples plot with lower

TiO2 compositions and higher MgO concentrations and most of the samples have higher

Mg-numbers (Fig. 5-82). Specifically, gabbroic rocks from the upper portion of the drill

hole have lower TiO2 and generally higher Mg-numbers and MgO concentrations relative

to the gabbroic rocks from the lower portion of the drill hole; rocks from the main

mineralized zone have the lowest Mg-numbers and MgO concentrations. The higher

MgO and lower TiO2 compositions, relative to average chilled margin gabbro, can be

attributed to the presence of orthopyroxene phenocrysts (hypersthene) in most of the core

samples.

Variations in selected major elements are plotted against diamond drill hole depth

(stratigraphic height) in Figures 5-83 and Figure 5-84. Concentrations of SiO2, although

variable in the lowermost samples, display a general increase upward through the drill

hole. Within the main mineralized zone, SiO2 concentrations are generally lower relative

to the underlying gabbro samples, followed by a sharp decrease in SiO2 immediately

above the main mineralized zone, followed by a gradual upward increase (Fig. 5-83).

Concentrations in TiO2 exhibit a gradual upward decline through the drill section (Fig. 5-

83). The highest concentrations are in the lowermost gabbros which may attributed to

contamination from footwall sedimentary rocks.

297

Sample Drill Hole Description CIPW From To Interval CompositeNorm wt% (m) (m) (m) Depth (m)

44731 JR99-01 mg; vt gabbro GN (H-O) 2.50 2.95 0.45 1.0044737 JR99-01 fg-mg; vt gabbro G (Q-H) 5.54 6.16 0.62 4.2144744 JR99-01 mg; opx-gabbro GN (H-O) 9.41 10.41 1.00 8.4644769 JR99-01 mg; opx-gabbro GN (H-O) 14.00 14.45 0.45 12.5044792 JR99-01 mg; opx-gabbro GN (H-O) 17.43 17.95 0.52 16.0044799 JR99-01 mg; opx-gabbro G (Q-H) 20.50 21.25 0.75 19.3044805 JR99-01 mg; opx-gabbro G (Q-H) 24.46 25.07 0.61 23.1244812 JR99-01 mg; opx-gabbro G (Q-H) 29.28 30.15 0.87 28.2044685 JR99-06 mg; opx-gabbro G (Q-H) 10.15 10.45 0.30 33.2044692 JR99-06 mg; opx-gabbro G (Q-H) 12.54 12.75 0.21 35.5044700 JR99-06 mg; opx-gabbro G (Q-H) 15.64 15.98 0.34 38.7344705 JR99-06 mg; opx-gabbro G (Q-H) 17.84 18.27 0.43 41.0244708 JR99-06 mg; opx-gabbro G (Q-H) 19.13 19.50 0.37 42.2544711 JR99-06 mg; opx-gabbro G (Q-H) 20.09 20.45 0.36 43.2044713 JR99-06 mg; opx-gabbro G (Q-H) 20.86 21.33 0.47 44.0844714 JR99-06 mg; opx-gabbro G (Q-H) 21.33 21.87 0.54 44.6244716 JR99-06 mg; opx-gabbro G (Q-H) 22.16 22.41 0.25 45.1644718 JR99-06 mg; opx-gabbro G (Q-H) 22.64 23.09 0.45 45.8444720 JR99-06 mg; opx-gabbro G (Q-H) 23.52 23.91 0.39 46.6644722 JR99-06 mg; gabbro G (Q-H) 24.25 24.75 0.50 47.5044725 JR99-06 mg; gabbro OLGN (H-O) 25.50 25.68 0.18 48.4344758 JR99-06 mg; gabbro G (Q-H) 28.49 29.00 0.51 51.7544861 JR99-06 sediment sediment 44.38 45.74 1.36 68.49

Table 5-23. Summary of drill hole data for the composite drill hole, comprising drill

holes JR99-01 and JR99-06, from the Rastall property, Chiniguchi River intrusion, Janes

Township. "-" below lower limit of detection; "N" = primitive mantle-normalized;

"na"=not analyzed; fg=fine-grained; mg=medium-grained; G=gabbro; OLGN=olivine

leucogabbronorite; LG=leucogabbro; GN=gabbronorite; opx=orthopyroxene; vt=vari-

textured; Q-H=quartz-hypersthene; H-O=hypersthene-olivine; Q-H-C=quartz-



298

Sample Composite Pt Pd Cu Ni S Se Mg#Depth (m) ppb ppb wt% wt% wt% ppb

44731 1.00 15.30 40.00 63 43 0.03 192 7444737 4.21 19.00 68.10 106 60 0.05 280 7544744 8.46 28.00 141.60 193 104 0.09 421 7444769 12.50 38.20 81.90 1635 654 0.50 2564 7444792 16.00 62.50 123.50 2991 1206 0.80 4770 7244799 19.30 42.80 46.70 1759 782 0.44 2614 7244805 23.12 94.30 181.00 4578 1948 1.34 6878 6844812 28.20 92.60 313.00 4489 1625 1.33 6150 6744685 33.20 268.00 858.00 8793 4642 3.23 16912 6144692 35.50 353.00 1540.00 11788 3640 2.82 14415 6244700 38.73 311.00 1617.00 6769 2510 1.69 8242 6544705 41.02 378.00 2009.00 7851 2914 1.92 10290 6344708 42.25 395.00 2119.00 7306 2712 1.84 8235 6344711 43.20 554.00 2677.00 8604 4719 2.65 10718 6144713 44.08 549.00 2482.00 9147 4539 2.61 9990 6144714 44.62 548.00 2118.00 10182 4827 2.83 13462 6044716 45.16 310.00 1603.00 5410 2964 1.75 7320 6544718 45.84 356.00 1624.00 6195 2914 1.83 7545 6444720 46.66 152.00 851.00 2633 1202 0.59 2985 6844722 47.50 13.30 33.40 154 107 0.06 244 6944725 48.43 10.50 19.30 42 101 0.22 155 7644758 51.75 9.90 11.95 76 68 0.06 222 6944861 68.49 1.37 2.84 18 91 0.02 32 77

Table 5-23 (cont). Summary of drill hole data for the composite drill hole, comprising

drill holes JR99-01 and JR99-06, from the Rastall property, Chiniguchi River intrusion,

Janes Township. "-" below lower limit of detection; "N" = primitive mantle-normalized;

"na"=not analyzed; fg=fine-grained; mg=medium-grained; G=gabbro; OLGN=olivine

leucogabbronorite; LG=leucogabbro; GN=gabbronorite; opx=orthopyroxene; vt=vari-

textured; Q-H=quartz-hypersthene; H-O=hypersthene-olivine; Q-H-C=quartz-

hypersthene-corundum.

299

0.30

0.35

0.40

0.45

0.50

0.55

0.60

0.65

0.70

0.75

50556065707580

Mg-number

TiO

2 (w

t%)

4473144737447444476944792447994480544812446854469244700447054470844711447134471444716447184472044722447254475844861Chilled Margin Avg

fractionation

Mineralized Zone

Lower Gabbros

Upper Gabbros

A g gabbro (CIPW)) gabbronorite (CIPW)# olivine leucogabbronorite (CIPW)+ sediment

(A)

0.30

0.35

0.40

0.45

0.50

0.55

0.60

0.65

0.70

0.75

4567891011121314

MgO (wt%)

TiO

2 (w

t%)

4473144737447444476944792447994480544812446854469244700447054470844711447134471444716447184472044722447254475844861Chilled Margin Avg

fractionation

A g gabbro (CIPW)) gabbronorite (CIPW)# olivine leucogabbronorite (CIPW)+ sediment

(B)

Figure 5-82. Bivariate scatter plots of core samples from the composite drill hole from the Rastall property, Chiniguchi River intrusion. (A) Variations in Mg-number and TiO2. (B) Variations in MgO and TiO2. Average chilled margin gabbro is from this study.

300

0

10

20

30

40

50

60

7040 42 44 46 48 50 52 54 56

SiO2 (wt%)

Dril

l Hol

e D

epth

(m)

sediment

gabbro (OLGN)gabbro (G)

gabbro (G)

orthopyroxene gabbro (G)


vt gabbro (G)

vt gabbro (GN)

(A)

main mineralized zone

Figure 5-83a. Profile through the composite drill hole from the Rastall property,

Chiniguchi River intrusion, showing stratigraphic variations in SiO2.

301

0

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20

30

40

50

60

700.3 0.35 0.4 0.45 0.5 0.55 0.6 0.65 0.7

TiO2 (wt%)

Dril

l Hol

e D

epth

(m)

sediment


gabbro (G)



vt gabbro (G)

vt gabbro (GN)

(B)


Figure 5-83b. Profile through the composite drill hole from the Rastall property,

Chiniguchi River intrusion, showing stratigraphic variations in TiO2.

302

0

10

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30

40

50

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7050 55 60 65 70 75 80

Mg-number

Dril

l Hol

e D

epth

(m)

sediment


gabbro (G)



vt gabbro (G)

vt gabbro (GN)

(A)


Figure 5-84a. Profile through the composite drill hole from the Rastall property,

Chiniguchi River intrusion, showing stratigraphic variations in Mg-number.

303

0

10

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30

40

50

60

706 7 8 9 10 11 12 13 14

MgO (wt%)

Dril

l Hol

e D

epth

(m)

sediment


gabbro (G)



vt gabbro (G)

vt gabbro (GN)

(B)


Figure 5-84b. Profile through the composite drill hole from the Rastall property,

Chiniguchi River intrusion, showing stratigraphic variations in MgO.

304

Within the main mineralized zone, TiO2 shows a sharp decline relative to the underlying

gabbros, followed by a gradual decline upward through the remainder of the drill section.

As illustrated in the diagrams of Mg-number and MgO versus TiO2 (Fig. 5-82b),

concentrations of MgO and Mg-numbers are highest in the rocks that underlie the main

mineralized zone, and display a gradual upward increase through the overlying gabbros,

followed by a decrease through the uppermost vari-textured gabbro (Fig. 5-84).

5.13.2 Chalcophile (PGE, Cu, Ni) Elements

Stratabound sulphide mineralization consisting of ~3-5% disseminated sulphide, was

intersected in drill holes JR99-01 and JR99-06, where it is hosted by massive to locally

fractured orthopyroxene gabbro (Fig. 5-83). In the composite drill section, this main

mineralized zone is represented by the interval from 35.50 m to 45.84 m as summarized

in Table 5-23. The main mineralized zone averages 2394 ppb Pt+Pd, 8139 ppm Cu and

3527 ppm Ni (4.7 Pd/Pt; 2.3 Cu/Ni), contrasting the concentrations in 2 unmineralized

(<0.05 wt% S) samples which average 71 ppb Pt+Pd, 84.5 ppm Cu and 51.5 ppm Ni (3.1

Pd/Pt; 1.6 Cu/Ni). The highest individual PGE concentration is from sample 44711

which contains 554 ppb Pt, 2677 ppb Pd, 405 ppb Au, 8604 ppm Cu and 4719 ppm Ni

(4.8 Pd/Pt; 1.8 Cu/Ni).

Selected bivariate plots of chalcophile element concentrations for the drill core

samples are provided in Figure 5-85. Correlations between the chalcophile elements Pt-

Cu and Pd-Cu are very good, indicating that the PGE are strongly sulphide controlled.

All of the samples except 44725, a CIPW olivine leucogabbronorite from the lower part

of the drill hole section, have S/Se values between 1000 and 5000 and plot within the

field of uncontaminated magmatic sulphide (Fig. 5-86a). Sample 44725, which has a

contamination signature suggesting addition of external S, is located within about 20 m of

the footwall sedimentary rocks. In the discrimination diagram of S/Se versus Pd, all of

the samples, and in particular the unmineralized samples, plot within the field of second-

stage, PGE-fertile, magmas (Fig. 5-86b), as described by Peck et al. (2001) and Hamlyn

et al. (1985). All of the samples, except 44725, have restricted MgO compositions (~8.1-

10.1 wt% MgO) with the samples from the main mineralized zone having the highest Ir

concentrations, reflecting the primitive nature of these rocks and their higher PGE

abundances.

305

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Pt (ppb)

Cu

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)

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>0.05wt% S

Main Mineralized Zone

Chilled Margin Avg

(A)

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10000

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1 10 100 1000 10000

Pd (ppb)

Cu

(ppm

)

<0.05wt% S

>0.05wt% S


Chilled Margin Avg

(B)

Figure 5-85. Bivariate scatter plots of whole-rock chalcophile elements for core samples from the Rastall property, Chiniguchi River intrusion, sorted by mineralized (>0.05 wt% S), unmineralized (<0.05 wt% S), and chilled gabbro (JB98-224). (A) Variations in Pt and Cu. (B) Variations in Pd and Cu. Average chilled margin gabbro is from this study.

306

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S/Se

Pd (p

pb)

<0.05wt% S

>0.05wt% S


Chilled Margin Avg

sulphur loss magmatic contamination

+R-factor

44725 (OLGN)

(A)

Figure 5-86a. Discrimination diagram of S/Se versus Pd plotting unmineralized (<0.05

wt% S), mineralized (>0.05 wt% S), and chilled gabbro samples from the Rastall

property, Chiniguchi River intrusion. Samples with S/Se ratios that range 1,000 to 5,000

are within the range of uncontaminated magmatic sulphides (Naldrett, 1981) and samples

with S/Se <1,000 are attributed to sulphur loss through weathering or other secondary

processes (Reeves and Keays, 1995).

307

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Se (ppb)

Pd (p

pb)

<0.05wt% S>0.05wt% SMain Mineralized ZoneChilled Margin AvgMORB Avg



Average MORB

(B)

Figure 5-86b. Discrimination diagram of Se versus Pd plotting unmineralized (<0.05

wt% S), mineralized (>0.05 wt% S) and chilled gabbro samples from the Rastall

property, Chiniguchi River intrusion. Value for average chilled margin gabbro is from

the current study. Value for average MORB is from Hamlyn and Keays (1986).

308

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700.01 0.1 1 10 100 1000 10000 100000


Dril

l Hol

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epth

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gabbro (G)



vt gabbro (G)

vt gabbro (GN)

Cu/Pd

Pt (ppb) Pd (ppb)Pd/SePt/Se


S (ppm)

Cu (ppm)

Ni (ppm)

(A)

Figure 5-87a. Profiles through the composite drill hole from the Rastall property,

Chiniguchi River intrusion, Janes Township, showing stratigraphic variations in Pt/Se,

Pd/Se, Pt, Pd, Cu, Ni, S and Cu/Pd.

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0

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gabbro (G)



vt gabbro (G)

vt gabbro (GN)

S/SePd/PtCu/Ni


Se (ppb)

(B)

Figure 5-87b. Profiles through the composite drill hole from the Rastall property,

Chiniguchi River intrusion, Janes Township, showing stratigraphic variations in Cu/Ni,

Pd/Pt, Se and S/Se.

310

The Ni/Cu and Pd/Ir ratios from these samples are within the range of layered intrusions

with some sulphides (main mineralized zone) having elevated Pd/Ir values, suggesting

that some of the samples have suffered hydrothermal overprint.

Data for selected chalcophile elements and ratios are plotted against drill hole depth

in Figure 5-87. Moving upward in stratigraphy, the transition from non-mineralized

gabbro (lower fine- to medium-grained gabbro) to mineralized gabbro (orthopyroxene-

bearing gabbro) is gradational. In contrast the base of the mineralized zone is marked by

a rapid increase in Pt-Pd and Cu-Ni values over several centimetres. In general,

concentrations of Pt, Pd, Cu, Ni and S, including their maxima, are positively correlated

and the remarkably uniform concentrations through the main mineralized zone testify to

their magmatic origin. Subsequent to peaking within the lower part of the main

mineralized zone, Pt, Pd, Cu, Ni and S exhibit a systematic and gradual decline upward

through the section. The relationship between ratios of Pt/Se and Pd/Se and whole-rock

abundances of Pt, Pd and Se are shown plotted against drill hole depth in Fig. 5-87. The

maxima of Pt, Pd and Se are positively correlated, occurring within the lower part of the

main mineralized zone. However, the maxima for Pt/Se and Pd/Se ratios are offset from

this maxima, with the Pt/Se peak occurring below the main mineralized zone, in the

CIPW olivine leucogabbronorite, and the Pd/Se peak occurring immediately prior to the

main mineralized zone; the peak Se concentration is also offset from peak Pt and Pd

concentrations. The overall decline in Pt/Se and Pd/Se is indicative of precipitation of

PGE-bearing sulphides, with the magma becoming progressively depleted in PGE and

relatively enriched in Se (and S) as the sulphides formed; it is probable that sulphide

fractionation would have also been accompanied by sulphide settling. Barnes et al.

(1988) and Hoatson and Keays (1989) demonstrated that in general, Cu/Pd ratios of

<6500 were indicative of magmas that had not experience sulphide segregation. In

Figure 5-87a, Cu/Pd values are <6500 within the lower portion of the drill hole,

increasing through the main mineralized zone, surpassing 6500 near the upper part of the

main mineralized zone, increasing gradually upward through the section, then declining

through the upper part of the orthopyroxene gabbro and into the vari-textured gabbros.

These data suggest that the magma became S-saturated or was nearly S-saturated at the

stratigraphic level immediately underlying the main mineralized zone, becoming fully S-

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saturated at approximately the 35 m level; similar trends were noted by Reeves and

Keays (1995) in the Bucknalla Complex, Australia. Apart from changes in the total

sulphide content, there are no petrologic breaks between upper and lower mineralized and

non-mineralized rock units. This suggests that the PGE-rich sulphide mineralization in

the main mineralized zone developed through normal fractionation processes, and are

therefore enriched toward the base of the intrusion. However, it is unclear as to whether

the sulphide-rich orthopyroxene gabbro unit is part of a single magma pulse or just one of

several pulses that may have formed the Chiniguchi River intrusion.

Primitive mantle-normalized PGE and chalcophile element diagrams for mineralized

and unmineralized drill core samples shown in Figure 5-88, and are compared to average

chilled margin gabbro (this study), average flood basalt (Naldrett, 1981), average South

Roby Zone from the Lac des Iles Complex (J. Hinchey unpublished data, 2004); and

hydrothermal sulphide mineralization from the East Bull Lake intrusion (Peck et al.,

1993b). All of the samples display positive slopes with elevated Pt, Pd, Au and Cu

relative to Ni, Ir, Ru and Rh and in general follow patterns that are similar to average

chilled margin gabbro and average flood basalt. However, in detail the sulphide patterns

define two groups, distinguished by peaks in the abundance of Pd. Group-1 (Fig. 5-88a),

characterized by Pd peaks that are well above that of average chilled gabbro, comprises

the 3 uppermost samples, all of the samples from the main mineralized zone, and 2

samples that immediately underlie the main mineralized zone. Group-2 (Fig. 5-88b),

characterized by Pd abundances that are lower than Group-1 and lower than average

chilled margin gabbro, comprises 6 samples that immediately overly the main

mineralized zone, and the 2 lowermost gabbroic samples in the section. The majority of

Group-1 and -2 samples display profiles that are similar to that of East Bull Lake

hydrothermal sulphide mineralization but with higher peak Pd abundances in Group-1

and lower Pd abundances in Group-2. The nine core samples from the main mineralized

zone (Fig. 5-88c) have patterns that are similar to the profiles of East Bull Lake

hydrothermal mineralization (Peck, 1993) and remobilized sulphide mineralization from

the South Roby Zone, Lac des Iles Complex (Brügmann et al., 1989), suggesting that

these sulphides have suffered hydrothermal overprint.

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1

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al in

100

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ulph

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Man

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4473144737447444469244700447054470844711447134471444716447184472044722Chilled Margin AvgFlood Basalt AvgEBL Hydrothermal Avg

A g gabbro (CIPW)) gabbronorite (CIPW)

(A)

GROUP-1

Figure 5-88a. Group-1 samples. Primitive mantle-normalized PGE-chalcophile element

diagrams (recalculated to metals in 100% sulphide) for sulphides from the composite

drill hole core samples, Rastall property, Chiniguchi River intrusion, Janes Township.

Data for average chilled margin is from this study; data for average flood basalt is from

Naldrett (1981); data for average East Bull Lake intrusion hydrothermal sulphide is from

Peck et al. (1993b). Mantle normalizing values are from Barnes et al. (1988) and


313

1

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ulph

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4476944792447994480544812446854472544758Chilled Margin AvgFlood Basalt AvgEBL Hydrothermal Avg

(B)

A g gabbro (CIPW)) gabbronorite (CIPW)# olivine leucogabbronorite (CIPW)

GROUP-2

Figure 5-88b. Group-2 samples. Primitive mantle-normalized PGE-chalcophile element

diagrams (recalculated to metals in 100% sulphide) for sulphides from the composite

drill hole core samples, Rastall property, Chiniguchi River intrusion, Janes Township.


Naldrett (1981); data for average East Bull Lake intrusion hydrothermal sulphide is from

Peck et al. (1993b). Mantle normalizing values are from Barnes et al. (1988) and


314

1

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100000


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al in

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ulph

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446924470044705447084471144713447144471644718Chilled Margin AvgFlood Basalt AvgEBL Hydrothermal AvgLac des Iles SRZ Avg

A g gabbro (CIPW)

(C)

Mineralized Zone

Figure 5-88c. Main Mineralized Zone. Primitive mantle-normalized PGE-chalcophile

element diagrams (recalculated to metals in 100% sulphide) for sulphides from the

composite drill hole core samples, Rastall property, Chiniguchi River intrusion, Janes


Naldrett (1981); data for average Lac des Iles – South Roby Zone (SRZ) is from J.

Hinchey (unpublished data, 2004); data for average East Bull Lake intrusion

hydrothermal sulphide is from Peck et al. (1993b). Mantle normalizing values are from

Barnes et al. (1988) and McDonough and Sun (1995).

315

5.14 Summary

Nipissing Gabbro suite intrusions cover more than 25% of the study area where they

form an extensive system of mafic intrusions. The distribution of these sills, dikes and

possible cone sheets suggest that they represent the intrusive portion of an eroded

continental flood basalt (Lightfoot et al., 1986, 1987; Lightfoot and Naldrett, 1996). The

current study has augmented earlier work by such as authors as Lightfoot and Naldrett

(1996) and Conrod (1988), and presents detailed information specifically regarding the

chalcophile elements in these mafic bodies. On the basis of the geochemical data

presented in the current study, and from previous studies (e.g. Lightfoot and Naldrett,

1996), a number of conclusions can be made regarding the chemistry and petrogenesis of

these intrusions in the context of the sulphide mineralization.

Controls on Mineralization

1) The identification of lower portions of the Nipissing Gabbro intrusions and in

particular the identification of the lowermost Orthopyroxene Gabbro (gabbronorite)

Unit. This unit has been identified as the most prospective to host magmatic

sulphides and would most likely be encountered in the least differentiated intrusions.

2) Base metal (Cu, Ni) concentrations with very low PGE were recorded in rocks from

the upper stratigraphy in intrusions that also host significant PGE-rich magmatic

sulphide near the base of the intrusion (e.g. Chiniguchi River intrusion). This

difference in base-metal to PGE concentrations suggests that PGE-rich sulphide

precipitated through normal in-situ fractionation, from the base upwards, resulting in

a sharp increase in the base-metal to PGE ratio, toward the hangingwall of the

intrusion.

Major Element Chemistry

1) Rocks from Nipissing Gabbro intrusions are for the most part sub-alkaline and

tholeiitic but with more evolved rocks trending toward calc-alkaline compositions.

The majority of samples from this study classify as CIPW silica-oversaturated,

quartz-hypersthene-normative gabbro and leucogabbro; several of the more mafic

samples, referred to as orthopyroxene gabbro, classify as CIPW melagabbronorite,

316

olivine gabbronorite and gabbronorite. However, most of the rocks considered to be

orthopyroxene gabbro classified as CIPW gabbro.

2) Geochemical characteristics of the sample suite include median values of ~51.3 wt%

SiO2 (lowest = 45.9 wt%), 0.52 wt% TiO2 (lowest = 0.4 wt%), 8.4 wt% MgO

(highest = 19.41 wt%) and an Mg-number of 66 (highest = 83). Chilled margin

gabbro, considered to be reflective of parental magma compositions, are

characterized by 49.8-51.9 wt% SiO2 (average = 50.0 wt% SiO2), 0.52-0.89 wt%

TiO2 (average = 0.69 wt% TiO2), 6.13-8.43 wt% MgO (average = 7.73 wt% MgO),

and 52-66 Mg-number (average = 61 Mg number).

3) Wide ranges in the relative concentrations of MgO and TiO2 and with the Mg-

number, suggest that the magmas underwent a considerable amount of in situ

fractionation.

Trace Element Geochemistry

1) Primitive mantle-normalized REE patterns for the majority of Nipissing Gabbro

rocks are characterized by LREE enrichment, narrow ranges in (La/Yb)N, and

chondrite-normalized modest positive and negative Eu anomalies. REE patterns

from mineralized samples are similar to those from unmineralized samples,

suggesting a common origin.

2) Consistently low (La/Sm)N values record a crustal contamination signature and

are similar in mineralized and unmineralized rocks, suggesting that the

contamination signature had nothing to do with the mineralizing event. In

addition, the high (Th/Yb)N values (~2-10 times primitive mantle) are interpreted

to be a consequence of crustal contamination of a mantle-derived magma.

3) The majority of REE patterns exhibit LILE enrichment and negative Nb and Ta

anomalies. In each case, however, the negative Nb anomalies are much larger

than those of Ta. The majority of samples have Nb, Ta, Th values that fit a

mixing curve between N-MORB and continental sediments, with values on that

curve that suggest ~20% crustal contamination of the source magma. Continental

flood basalts or boninitic magmas are good candidates for this chemistry,

exhibiting continental crust signatures.

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4) All of the rock samples from the Nipissing Gabbro intrusions have very low

Nb/Ta and Zr/Sm values relative to MORB, primitive mantle, continental crust

and modern adakites. This is interpreted to mean that Nipissing gabbro magmas

interacted with an extensive crustal reservoir, adopting crustal signatures typical

of rift-related magmas and/or continental flood basalt.

Chalcophile Geochemistry

1) The estimated background PGE-Cu-Ni composition for Nipissing Gabbro

intrusions, which also provides an estimate for the parental magma composition,

is ~4 ppb Au, 12 ppb Pt, 21 ppb Pd, 91 ppm Cu and 149 ppm Ni.

2) Good correlations exist between the chalcophile elements indicating that the

majority PGE are strongly sulphide controlled. Metal ratio diagrams (Ni/Cu-

Pd/Ir, Cu/Ir-Ni/Pd, wt% MgO-Pd/Ir; S/Se; Pd/Ir) also support a magmatic origin.

3) Sulphides in chondrite-normalized PGE diagrams exhibit patterns that are

consistent with a magmatic origin for the sulphides. Sulphides from chilled

gabbro and gabbroic rocks have PGE patterns that are most similar to continental

flood basalt, suggesting a common origin. A few PGE patterns with very low

Pd/Ir values suggest that at least some of the rocks were formed from magmas

that were less fractionated that continental flood basalt.

4) Discrimination plots of Se vs Pd show that the magmas from which the sulphides

precipitated were PGE metal-fertile second-stage magmas (S-undersaturated) that

had not previously segregated sulphides to any large degree.

5) Evidence for PGE depletion in sulphide-bearing rocks that potentially overly

PGE-rich mineralization suggests that the sulphides were dissolved in the magmas

when they entered the chamber and that they precipitated under normal

fractionation within the Nipissing Gabbro chamber

6) The majority of the sulphides from mineralized rocks can be modelled using R

factors that are dominantly <1000.

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CHAPTER 6: RIVER VALLEY INTRUSION

6.1 Introduction

Comprehensive and systematic studies of the East Bull Lake suite intrusions began

with the work of Born (1979), who documented the geology of the East Bull Lake

intrusion. Academic studies and minor base metal exploration, focusing mainly on the

East Bull Lake and Agnew Lake intrusions, continued through the 1980’s (e.g. James and

Born, 1985; McCrank et al., 1989) and 1990’s (e.g. Peck and James, 1990; Peck et al.,

1993a). However, it was not until the mid to late 1990’s that base metal and PGE

exploration interests began to shift toward the River Valley intrusion, due in part to the

work of Ashwal and Wooden (1989). Since 1999, the mafic intrusions of the East Bull

Lake intrusive suite, and especially the River Valley intrusion, have been the subject of

ongoing Cu-Ni-PGE mineral exploration. It is this increased economic interest in these

intrusions that has led to a renewed academic interest in the geology, stratigraphy,

geochemistry and mineralogy of the East Bull Lake suite. Moreover, understanding the

geology of the East Bull Lake intrusive suite is of significant importance in

understanding the earliest evolution of the Palaeoproterozoic Southern Province in central

Ontario and there are now numerous professional publications that describe and discuss

the geology, geochemistry, and mineral deposit potential of these intrusions (e.g. James et

al. 2002a, 2002b; Easton, 2000a, 2003).

6.2 General Geology of the River Valley Intrusion

The River Valley intrusion is best exposed in Dana Township (Fig. 6-1) where it

locally exhibits well preserved primary mineralogy and textures and has been the subject

of several recent studies (Easton and Hrominchuk 1999, 2001a, 2001b; James et al.,

2002a, 2002b; Easton 2003; Easton et al., 2004). In comparison to the other East Bull

Lake suite bodies, the River Valley intrusion shows the clearest relationships with other

members of the Palaeoproterozoic rifting suite (Easton et al., 2004). However, studies on

the stratigraphy, geochemistry and mineralization in the River Valley intrusion are

limited in comparison to similar studies on the East Bull Lake (Peck et al., 1993a, 1995,

2001) and Agnew Lake (Vogel et al., 1998a, 1999) intrusions.

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Figure 6-1. General geological map of the River Valley intrusion illustrating the

distribution of stratigraphic zones that form the bulk of the intrusion and locations of

principal PGE sulphide mineralization and occurrences. Many of the northeast-trending

faults (dashed lines) are fault or shear zones that range from a few metres to 10’s of

metres in width. The Dana Lake Shear Zone is considered part of the Grenville Front

Boundary Fault system (solid lines). North of the Sturgeon River Fault Zone, the

intrusion contains large areas of preserved or partly-preserved primary mineralogy,

whereas south of the Sturgeon River Fault, in Crerar Township, the intrusion is

thoroughly recrystallized to upper amphibolite facies rock assemblages (modified after

James et al., 2002b).

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The River Valley intrusion is cut by mafic dikes that are geochemically correlated with

the Hearst-Matachewan Dike Swarm, as well as by felsic intrusive rocks coeval with the

Huronian Supergroup volcanic rocks (Easton and Hrominchuk 1999, 2001b). In addition,

granitic rocks in Street Township, located about 20 km west of the River Valley

intrusion, are dated at 2460±20 Ma and contain inclusions of East Bull Lake suite rocks

(James et al., 2002a). Similar inclusions were also reported by Easton (2003) in granitic

rocks in Henry and Loughrin townships, located immediately east of Street Township.

The River Valley intrusion is also cut by magnetite-olivine diabase dikes of the 1238 Ma

Sudbury Dike Swarm and the 590 Ma Grenville Dike Swarm (Easton, 2000a).

6.2.1 External Contacts

The identification of primary igneous contacts between lithological units, in

particular those that form boundaries to the Marginal Series which hosts the potentially

economic PGE-Cu-Ni sulphide mineralization (Fig. 6-1), is essential to successful

mineral exploration in the River Valley intrusion. Easton (2003) noted that three main

contact types are present between the River Valley intrusion and country rock units in

Dana Township, viz: 1). preserved intrusive contacts; 2). tectonized or disrupted intrusive

contacts, and, 3). wholly tectonic or fault contacts. It is likely that most of the northern

contact of the River Valley intrusion in Dana Township is primary, however, as the

contact is followed southeast it becomes more difficult to confirm the presence of a

primary contact, mainly due to a lack of exposure. In the northwest quadrant of Dana

Township, in the area of Pacific North West Capital Corp.’s Dana North, Dana South,

Lismer’s Ridge North and Lismer’s Ridge South deposits, the north-northeastern contacts

of the intrusion are interpreted as primary, although they are locally cut, with minimal

lateral offset (generally <50m horizontally), by relatively narrow (10’s to 100’s of metres

wide) northeast striking mylonitic zones that are related to the Grenville Front Tectonic

Zone (Fig. 6-1). The nature of the intrusive contact in the area of Azen Creek and

eastward toward the McWilliams Township line is much more obscure as the structures

(faults, folds?) within this region of the intrusion become much more complex.

Easton (2003) suggested that the western contact of the River Valley intrusion, along

Highway 805, in the southern half of Dana Township represents a tectonized igneous

contact and may represent an upper, rather than a basal, contact of the intrusion (Photo 6-

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1a). The northwestern contact is tectonic and is complicated by the presence of several

faults relating to the Grenville Front Boundary Fault, which obscure the relationship

between the River Valley intrusion and the Huronian Supergroup rocks (Fig. 6-1). In this

region, the River Valley intrusion is either in thrust contact with quartzite of the

Mississagi Formation (Davidson 1986) or is in an unclear contact relationship with

bimodal (mafic-felsic) metavolcanic rocks of the lower Huronian Supergroup (Easton and

Hrominchuk, 1999). Easton and Hrominchuk (1999) suggested that the metavolcanic

rocks are ~2460 Ma in age (geochemical correlation) and were therefore probably

deposited post-emplacement of the River Valley intrusion; this supports the interpretation

that the River Valley intrusion is in thrust contact with Huronian Supergroup rocks in this

area.

6.2.2 Country Rocks

Easton (2003) grouped the country rocks to the River Valley intrusion into four

gneissic associations (Culshaw et al., 1988). These units, from northwest to east, are: the

Front, Street, Crerar, Pardo gneiss associations. Easton (2003) considered these four

gneissic associations to represent a southward-deepening section of crust, with exposure

of each section likely the result of north-northwest-directed transport along Grenville-age

thrust faults. Of these four associations, the Pardo gneiss is most relevant to this study as

it lies alongside the northern contact of the River Valley intrusion in Dana Township

(Fig. 6-1). On the basis of field observations and geochemistry, Easton (2003)

considered a fifth gneissic unit, the Red Cedar Lake gneiss, to be a more deformed

(flattened) and cataclastic equivalent of the Pardo gneiss, probably as a result of increased

Grenvillian deformation, and suggested their formation to be between 2685 and 2675 Ma.

The Pardo gneiss consists mainly of fine-grained, biotite quartzofeldspathic gneiss

(metagreywacke) cut by granodioritic and tonalitic leucosome veins (5-25% of the rock)

and medium-grained, granodioritic to monzogranitic gneiss, possible representing

plutonic rocks that intruded the metasedimentary migmatites (Easton, 2003).

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Photo 6-1. (A) Tectonized contact along the western margin (Grenville Front Boundary Fault) of the intrusion, Highway 805, Dana Township. The arrow indicates the plane of foliation. The pen is about 15 cm long. (B) Chaotic Zone, correlative with the Marginal and/or Inclusion/Autolith-bearing zones, was identified by Mustang Minerals Corp. in the eastern part of Dana Township. An eight centimetre ruler is provided for scale.

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Lumbers (1973) mapped metagreywacke and granodiorite immediately north of the

Grenville Front Boundary Fault in Pardo Township, and it is probable that these rocks

represent non-migmatized equivalents of the Pardo gneiss, preserved at higher structural

levels (Easton, 2003). Easton (2003), noting that the gneissosity and folds in the Pardo

gneiss are cut by both Matachewan and Sudbury dike swarms, suggested that the main

migmatitic event affecting the Pardo gneiss occurred prior to 2445 Ma and was likely

Neoarchaean in age. Easton (2003) also noted that the area underlain by the Pardo gneiss

was affected by high-grade metamorphism after 1240 Ma. At several localities along the

northern contact of the River Valley intrusion, Pardo gneiss immediately in contact with

River Valley intrusion rocks show a higher degree of migmatization over several metres

away from the contact, suggesting that contact metamorphism was responsible for further

deformation of the proximal Pardo gneiss.

6.2.3 Structure, Deformation and Metamorphism

Within the River Valley intrusion, in Dana Township, numerous northeast-trending

linear zones of alteration and deformation, generally less than 1 km wide and typically

10’s to 100’s of metres wide, dissect the igneous stratigraphy (Fig. 6-1). These discrete

linear domains comprise steeply-dipping, gneissic rocks (mylonitic) that confine

generally northwest-trending regions or “cores” of relatively unaltered and/or preserved

intrusive rocks that can be kilometres in length, and include preserved magmatic textures,

mineralogy and mineralization within the Marginal Series rocks.

In the northernmost part of the intrusion, in the Dana Lake and Lismer’s Ridge areas,

there is an increase in metamorphic grade southeast into the main Grenville terrain,

ranging from greenschist in the Dana Lake area to amphibolite facies or higher in the

Lismer’s Ridge area, a distance of about 5 km (Fig. 6-1). Moving further southeast along

the contact region, the metamorphic grade increases from upper amphibolite in the Azen

Creek area to granulite facies toward Razor and into McWilliams Township (Fig. 6-1).

The Neoproterozoic to Early Paleozoic Sturgeon River Fault Zone (Fig. 6-1) is an

important northwest-trending structural feature that cuts through the River Valley

intrusion. North of the Sturgeon River Fault, the River Valley intrusion contains large

areas of preserved or partly-preserved primary mineralogy, and deformation is

concentrated along discrete vertical and sub-horizontal shear zones that cut the intrusion

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(Easton and Hrominchuk 1999, 2001b; Hrominchuk 2000). The geometry of the

intrusion north of the Sturgeon River appears to be sheet-like, with igneous layering

generally dipping at 20-30° to the south and southeast (Easton et al., 2004). This

configuration has led to the exposure of the basal contact and/or margin and/or sidewall

of the River Valley intrusion (Marginal Series rocks) for about 10 km along the north and

northeastern margin of the intrusion (Dana Township), providing an extensive

exploration target area for contact-type PGE-Cu-Ni mineralization (Fig. 6-1).

South of the Sturgeon River Fault, in Crerar Township, the River Valley intrusion

consists of a moderately dipping (40-60°), synformal sequence that is more thoroughly

recrystallized to upper amphibolite facies assemblages than the rocks in Dana Township

(Easton and Hrominchuk, 1999, 2001a). Grenvillian deformation is principally

concentrated near the Grenville Front Boundary Fault, along the west side of the

intrusion; work by Tettelaar (2000) and Easton and Hrominchuk (1999), estimated

Grenvillian metamorphic conditions to be 5-7 kb and 625°C.

6.3 Stratigraphy, Mineral Chemistry and Petrography

Easton (2003) presented generalized cross-sections for the East Bull Lake suite

intrusions, correlating the exposed stratigraphy of the northern and southern parts of the

River Valley intrusion with the lower stratigraphy of the East Bull Lake and Agnew Lake

intrusions. Hrominchuk (2000) proposed an estimated 900 m thick stratigraphy for the

northern part of the River Valley intrusion, which is in Dana Township, north of the

Sturgeon River Fault (Fig. 6-1). In this interpretation, the River Valley intrusion consists

of an inclusion-bearing Marginal Zone, which hosts most of the mineralization in the

intrusion, overlain by layered, mainly melanocratic, rocks of the Olivine Gabbronorite

Zone, which are in turn overlain by progressively fractionated rocks of the Gabbronorite

and Leucogabbronorite zones. An autolith-bearing unit, termed the Inclusion/Autolith-

bearing Zone (Hrominchuk, 2000), intrudes the lower Gabbronorite Zone, and like the

Marginal Zone is mineralized (e.g. Azen Creek, Fig. 6-1). Marginal Zone and

Inclusion/Autolith-bearing Zone rocks form a discontinuous, typically disordered and

heterogeneous magmatic assemblage, occurring where primary intrusion contacts are

preserved, and are host to much of the mineralization discovered to date; the Marginal

Zone (Hrominchuk, 2000) is encompassed by rocks of the Marginal Series (see Section

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6.5). Some specific features of these zones are as follows (Hrominchuk, 2000; James et

al., 2002b; Easton, 2003):

1. Marginal Zone (Marginal Series): ~100 m thick, consisting of mineralized

gabbronorite with fragments (gabbronorite/pyroxenite) and scarce footwall

xenoliths (gneisses/granitic). The matrix is composed of primocrysts of

plagioclase (An81-39), inverted pigeonite (En76-44) and augite. Fragments are

variable in size, ranging from metres to decametres in maximum dimension, and

commonly obscure the location of the contact. Small but widespread amounts of

white and/or blue-grey quartz and plagioclase with up to ~An40 compositions

(sodic), suggest local magma contamination. This zone represents the primary

exploration target for PGE-Cu-Ni sulphides comprising PGE-rich disseminated

chalcopyrite, pyrrhotite and pentlandite mineralization (1-5%) which occur in the

matrix assemblage (~70%) and less commonly (~30%) in the mafic fragments.

Fragment-bearing rocks decrease rapidly away from the base of this zone,

generally over widths of about 25-50 m (maximum widths of ~100 m).

2. Olivine Gabbronorite, Gabbronorite and Leucogabbronorite zones: ~700 m

thick sequence of progressively fractionated rock compositions from olivine

melagabbronorite to leucogabbro and anorthosite. The Olivine Gabbronorite

Zone consists of decametre thick, metre-scale layered sequences of troctolite,

melatroctolite and olivine gabbronorite (primocryst olivine, inverted pigeonite,

plagioclase). The Gabbronorite Zone consists of thick, weakly layered or

discontinuously layered norite and gabbronorite (primocryst inverted pigeonite,

plagioclase, ± augite). Leucogabbronorite dominates the Leucogabbronorite Zone

which also consists of massive but localized anorthositic rocks (primocryst

plagioclase, augite, ± orthopyroxene). The compositions of the primocrysts

(plagioclase (An78-56), olivine (Fo76-72), orthopyroxene (En76-56)), and their

stratigraphic distribution above the Marginal Zone, suggests that the upper portion

of the original River Valley intrusion is missing due to tectonism and/or erosion

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(James et al., 2002b). This contrasts with the igneous stratigraphy of the Agnew

Lake intrusion, which is largely intact (Vogel et al., 1998a).

3. Inclusion/Autolith-bearing Zone: intrudes the lower/marginal ~300 m portion of

the River Valley intrusion. At Azen Creek (Fig. 6-1), this zone occurs within

about 300 m of the north contact of the intrusion. This zone is dominated by

fragments of rock types that comprise the Marginal, Olivine Gabbronorite, and

Gabbronorite zones, as well as minor footwall xenoliths. The matrix, consisting

of primocryst olivine (~Fo68), plagioclase (An73-68) and inverted pigeonite (En69-

55), is more mafic in composition than the Marginal Zone which lack olivine.

Like the Marginal Zone, the matrix of the Inclusion/Autolith-bearing Zone

contains PGE that are associated with disseminated chalcopyrite, pyrrhotite and

pentlandite mineralization.

In the eastern part of Dana Township and into McWilliams Township, Pacific North

West Capital Corp. and Mustang Minerals Corp. have identified PGE mineralization

associated with 0.5-5% disseminated chalcopyrite, pyrrhotite and subordinate pentlandite.

This mineralization is hosted by what Mustang Minerals Corp. have termed the “Chaotic

Zone” (PGE occurrence 7, Fig. 6-1; Photo 6-1b). This zone appears to be correlative

with the Breccia Unit of the Marginal Series, is 25-150 m wide in plan view and is

continuous for about 3 km along strike, extending northwest into the Razor PGE

occurrence (PGE occurrence 6, Fig. 6-1). James et al. (2002b) described the Chaotic

Zone matrix as consisting of equigranular, poikilitic and pegmatitic gabbronorite and

melagabbronorite. Autoliths form 50% or more of rocks in this zone and range in

composition from websterite and orthopyroxenite to gabbronorite and anorthosite in

which orthopyroxene, clinopyroxene and plagioclase are the primocryst phases. Mustang

Minerals Corp. have also identified layered olivine-bearing rocks, olivine websterite to

troctolite in composition, which overly the Chaotic Zone and may be correlative with the

Olivine Gabbronorite Zone (Hrominchuk, 2000) and the PGE occurrence at Azen Creek

(PGE occurrence 4, Fig. 6-1).

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The geochemistry of River Valley intrusion rocks is similar to that of other East Bull

Lake suite intrusions; geochemical data for rocks from the River Valley intrusion can be

found in Hrominchuk (2000), Easton and Hrominchuk (2002), James et al. (2002a) and

Easton (2003). A summary of the geochemical features as presented by Hrominchuk

(2000) and Easton et al. (2004) is as follows:

1. Marginal Zone: generally <50 wt% SiO2 and CIPW quartz-normative. Rocks

show much higher Ti, Fe, Rb, Sr, K, Na, P, Ba, Zr and Y contents than in the

overlying units and this is interpreted to be the result of contamination, probably

through wall rock assimilation.

2. Olivine Gabbronorite Zone: olivine-normative rocks, characterized by high

MgO (15-24 wt%) and low SiO2 (38-45 wt%), with anomalous Ni contents

attributed to primocryst olivine.

3. Inclusion/Autolith-bearing Zone: matrix composition is elevated in Mg, Ca, Al,

and Fe, which is consistent with its plagioclase, orthopyroxene and olivine-

dominated mineralogy. The fragments, inclusions and xenoliths of this zone are

extremely varied in composition, partially resorbed and commonly mineralized.

Mafic inclusions are similar to the rocks in the lowest part of the layered Olivine

Gabbronorite Zone.

4. Gabbronorite Zone: gradual fractionation to Si-, Al-, Ca-, Na-, K-rich and Mg-

poor compositions; a trend also observed in the uppermost Leucogabbronorite

Zone.

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Figure 6-2. Generalized geology of the northwest portion of the River Valley intrusion

showing the locations of the (1) Dana North, (2) Dana South, (3) Lismer’s North, and (4)

Lismer’s South PGE-Cu-Ni deposits. Also shown are the approximate locations and

projections of drill holes (A) RV00-22 and (B) DL-14, 15 and 16 (modified after James et

al., 2002b).

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6.5 Marginal Series Stratigraphy, Mineralization and Geochemistry

To date, four contact-type PGE-Cu-Ni deposits have been outlined along the

northern margin of the River Valley intrusion in Dana Township; from northwest to

southeast they are; Dana North, Dana South, Lismer’s North and Lismer’s South (Fig. 6-

2). Small, plug-like alkaline intrusions of unknown age, but considered by Easton (2003)

to be Archaean (2640 Ma), occur along the intrusive contact where they displace the

Marginal Zone rocks (Fig. 6-2). As well, faults related to the Grenville Front Boundary

Fault and a 1.24 Ga Sudbury Dyke Swarm olivine-magnetite gabbro dike cut or displace

the Marginal Zone (Fig. 6-2). Silicate assemblages that host the mineralization in this

part of the River Valley intrusion range from greenschist facies assemblages in the

northwest to amphibolite facies in the southeast, contrasting with the preserved magmatic

assemblages and/or textures that dominate the upper amphibolite to granulite facies

mineralogy in the remainder of the intrusion toward the south-southeast (Fig. 6-1).

A detailed stratigraphy for the variably mineralized Marginal Series rocks has been

developed by the author, on the basis of outcrop mapping and greater than 80,000 metres

of diamond drill core logging as part of the exploration work carried out under author’s

direction (Fig. 6-3). Average PGE and base metal concentrations for the Marginal Series

rocks are provided in Table 6-1. The Marginal Series is in abrupt, intrusive contact to the

east with Neoarchaean-age Pardo gneiss, and bounded to the west by a sequence of

weakly layered to massive leucogabbro, gabbro and melagabbro. The Marginal Series,

which includes the Marginal Zone as described by Hrominchuk (2000), consists of four

distinct units that are capped by the Layered Units and is normally ~100 m wide in plan

view but generally ranges from 10 to 50 metres in width (Fig. 6-3).

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Figure 6-3. Schematic of typical stratigraphy through the Marginal Series rocks

(Marginal Zone) in the River Valley intrusion. The stratigraphy is largely based on the

more than 50,000 metres of diamond drill core from the Dana Lake and Lismer’s Ridge

areas. The Breccia Unit, the primary target for potentially economic PGE-Cu-Ni

mineralization, consists mainly of autoliths (black fragments), with very (<<1%) few

xenoliths (modified after James et al., 2002b).

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Unit n Data Au Pt Pd Ni Cu Pd:Pt Cu:Nippb ppb ppb ppm ppm

*Layered Units 277 average 6.0 22.0 19.4 97.1 70.2 0.8 0.9(LU) median 5.0 20.0 14.0 83.0 78.1 0.7 0.9Inclusion-Bearing Unit 691 average 11.2 60.5 78.0 84.4 122.1 1.1 1.7(IBZ) median 7.0 34.0 32.0 70.0 80.7 0.9 1.1Breccia Unit 2317 average 53.2 253.1 707.2 166.4 803.6 2.3 4.8(BX) median 28.0 120.0 246.0 119.0 517.0 2.3 4.4Boundary Unit 185 average 9.7 45.6 102.4 116.6 223.6 1.9 2.5(BZ) median 7.0 26.0 43.0 87.0 169.0 1.8 1.9Footwall 197 average 6.9 8.9 8.7 120.9 75.5 0.7 0.8(FW) median 4.0 0.0 5.0 129.0 72.7 0.5 0.6Mafic Dikes 68 average 19.2 51.3 109.9 97.4 280.6 1.3 2.8

median 8.0 21.0 17.0 45.0 142.5 0.9 2.7*Mafic Dikes-2 21 average 22.9 19.0 15.7 54.7 42.9 0.8 1.0

median 10.0 19.0 16.0 43.0 40.9 0.7 0.9Felsic Dikes 22 average 10.3 29.9 54.4 24.3 174.2 1.2 7.3

median 9.0 18.0 16.5 16.0 70.3 0.8 3.5 Table 6-1. Average and median values and metal ratios for whole-rock precious and base

metal concentrations from Marginal Series and associated rocks, River Valley Intrusion.

The Layered Units were calculated using samples with <100 ppm Cu (assumed low

sulphur); data from drill core analyses supplied by Pacific North West Capital Corp. and

Anglo American Platinum Corporation Limited. *Averages from the Layered Units and

Mafic Dikes-2 are used as estimates of parental magma compositions – see text for

discussion.

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From the footwall Pardo gneiss (Photo 6-2a), westward into the intrusion, the sequence

and character of the four distinguishable units in the Marginal Series (Photos 6-2 to 6-5)

are:

1. Footwall Breccia Unit (FBX): 5 to 15 metres wide, but may be absent. Consists

of partly rounded to angular, centimetre- to decimetre-size fragments of country

rock (~75% - Pardo gneiss, Archaean gabbro, diabase, diorite) and River Valley

intrusion material (~25% - chilled gabbro and medium-grained melagabbro) in a

matrix of finer grained rock of similar composition and/or aplitic/granitic matrix.

A narrow zone of migmatite at the contact of the intrusion is likely due to contact

metamorphism, and granitic veins can be traced from the Footwall Breccia Unit

into the footwall gneiss. Sulphides are dominantly pyrite and pyrrhotite with

local areas of trace to 1% chalcopyrite + pyrrhotite; PGE concentrations are

normally <25 ppb. The contact between this unit and the overlying Boundary

Unit is gradational, marked by a gradual decrease in the ratio of xenoliths

(country rock fragments) to autoliths (primarily chilled gabbro?) derived from

River Valley intrusion rocks.

2. Boundary Unit (BZ): 5 to 20 metres wide, but may be absent (Photo 6-2b).

Consists of partly rounded to subangular, centimetre- and decimetre-size

fragments of country rock (typically 10-25%), and autoliths of melagabbro,

gabbro and less commonly leucogabbro to anorthosite in a matrix of gabbro to

melagabbro ± aplite/granite, as in the Footwall Breccia Unit. The footwall

xenoliths (mainly alkali granites and granodiorite-tonalite) in the Boundary Unit,

and in the Footwall Breccia Unit, share many similarities to those described by

Peck et al. (2001) for xenoliths in the Border zone of the East Bull Lake intrusion.

In particular, at the River Valley intrusion there is also evidence of in-situ melting

such as granophyric xenomelts in or proximal to the country rock xenoliths and

fragments. Sulphide minerals are mainly pyrite and pyrrhotite, with locally up to

3% chalcopyrite + pyrrhotite; PGE concentrations are typically <75 ppb with

local concentrations >1000 ppb. The contact between this unit and the overlying

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Breccia Unit is sharp to gradational, marked by an abrupt to gradual decrease in

the occurrence of country rock fragments, which become near-absent in the

Breccia Unit.

3. Breccia Unit (BX): in general 20 metres wide but ranges to >100 metres wide

(Photo 6-3). This unit contains as much as 95% fragments that are dominantly

fine-grained gabbro to melagabbro with subordinate medium- to coarse-grained

gabbro and leucogabbro. On the basis of field observations, it is not clear whether

these fragments are autoliths derived locally or from elsewhere in the River

Valley intrusion, or if they are xenoliths. The fragments are hosted by a medium-

grained matrix of similar composition; matrix compositions vary abruptly from

melagabbro to gabbro to leucogabbro over very short distances. Fragments are

partly rounded to rounded, most likely as a result of partial assimilation, and

centimetre to decimetre in size – those greater than a metre (rafts and possibly

pendants) are mainly xenoliths of footwall compositions (gneiss) and these

fragments tend to be larger with increasing proximity to the intrusive contact; a

single fragment of layered gabbroic rocks, presumably derived from the Layered

Units, was observed at the South Zone (Fig. 6-12b). Sulphide minerals comprise

1 to 5% pyrrhotite + chalcopyrite and occur as both blebby and disseminated

textures; PGE contents are highly varied, but most values range from 500-6000

ppb with local concentrations >10,000 ppb. Blue-grey quartz is commonly

associated with sulphide accumulations and higher than average PGE

concentrations suggesting assimilation of local country rock; Peck et al (2001)

attributed the presence of blue quartz to a metasomatic event that was restricted to

the margins of the East Bull Lake intrusion. Notably, the Breccia Unit, which

contains the highest and most persistent PGE-rich sulphide mineralization, has the

smallest proportion of footwall inclusions (<<1%), perhaps an indication that

magma contamination through assimilation of local country rocks is not a major

controlling factor on mineralization (James et al., 2002b). The contact between

the Breccia Unit and the overlying Inclusion-bearing Unit is abrupt, marked by a

rapid increase in the occurrence of felsic autoliths (derived from the overlying

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Layered Units) and a decrease in fine-grained mafic fragments mafic, an increase

in overall fragment size, a decrease in the ratio of fragment to matrix volume, and

a decrease in the volume percent of visible sulphide.

4. Inclusion-bearing Unit (IBZ): 10 to 50 metres wide (Photo 6-4a). This unit

contains >90% autoliths of leucogabbro, subordinate gabbro and lesser

melagabbro in a matrix of either medium-grained leucogabbro or gabbro; the

leucogabbro xenoliths are subangular to partly rounded, dominantly decimetre to

metre in scale, and appear to be inclusions that were stoped from the overlying

Layered Units (the Leucogabbronorite Zone of Hrominchuk, 2000). Sulphide

minerals include trace to 3% pyrrhotite + chalcopyrite; PGE contents range from

100-500 ppb with local concentrations >1000 ppb. The contact between the

Inclusion-bearing Unit and the overlying Layered Units is gradational, marked by

a decrease in recognizable fragments and finally the presence of massive rock

units.

In the Dana Lake area, the overlying Layered Units (LU) consist of massive leucogabbro

and gabbro with subordinate melagabbro. In general, metre- to decametre-scale modal

and textural layering is poorly developed and contacts between layers are almost always

gradational (Photo 6-5). The LU contain only trace (<<1%) sulphide minerals

(chalcopyrite + pyrrhotite) but have PGE concentrations that are anomalous (~22 ppb Pt,

19 ppb Pd) in terms of average mafic rocks (Hamlyn et al., 1985).

Fine-grained gabbro and diabase dikes cut all of the above units as well as the

Layered Units (the Leucogabbronorite Zone of Hrominchuk, 2000) in the main part of the

intrusion (Photo 6-4b). These dikes are metamorphosed at a grade similar to the River

Valley intrusion in the Dana North area, are distinct from younger dikes of the Sudbury

and Grenville swarms (Easton, 2003) and many are plagioclase-phyric, suggestive of

Matachewan Swarm dikes.

An east-west cross section through the Dana South PGE-Cu-Ni Deposit is shown in

Figure 6-4; this section is based on mapping of surface geology and data from more than

40 drill holes in the immediate area (South Zone). The data suggest that the dip of the

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contact of the IBZ and BX with the footwall gneiss in this area ranges from about 65° to

75° west (inward towards the intrusion). However, this dip is highly variable along strike

changing from 65° to 85° west to 65° to 85° east over strike distances of <100 metres; it

is unclear as to whether this variability is a primary feature or is the result of folding.

The attitude of metre-scale layering in the Layered Units (the Leucogabbronorite Zone of

Hrominchuk, 2000) adjacent to the IBZ or BX is poorly constrained but is estimated to be

at ~60-70° west, and possibly shallowing (i.e. <60° dip) westward into the intrusion.

Figure 6-4. Schematic geological section (east-west, looking north) through the

mineralized Dana South deposit. This section is based on data from drill holes DL-14,

DL-15, and DL-16; intersections of sulphide mineralization through the Breccia Unit are

shown as 3E = Pt+Pd+Au (modified after James et al., 2002b).

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Photo 6-2. (A) Typical footwall (hangingwall) paragneiss to the River Valley Intrusion. The Canadian 25 cent piece is about 2.2 cm in diameter. (B) Boundary Unit with light coloured granitic matrix and fine-grained mafic fragments, Lismer’s Ridge area. The hammer handle is about 70 cm long.

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Photo 6-3. (A) Breccia Unit with medium-grained mafic matrix and fine-grained mafic fragments (xenoliths?) from the South Zone, Dana South Deposit. The hammer handle is about 33 cm long. (B) Breccia Unit with medium- to coarse-grained gabbro-leucogabbro matrix and fine- to medium-grained mafic fragments (xenoliths?) from the Central Zone, Dana North Deposit. The pencil is about 18 cm long.

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Photo 6-4. (A) Inclusion-bearing Unit with fine- to medium-grained mafic matrix and medium- to coarse-grained fragments (autoliths) of gabbro-leucogabbro from the South Zone, Dana South Deposit. The hammer handle is about 30 cm long. (B) Fine-grained (diabase) mafic dike cutting through the Breccia and Inclusion-bearing units from the South Zone, Dana South Deposit; the smaller dike is cutting through a felsic fragment (autolith) from the Inclusion-bearing Unit. The hammer handle is about 70 cm long.

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Photo 6-5. (A) Modal and textural layering in olivine gabbronorite from the Razor area, southeast Dana Township. The pen magnet is about 12.5 cm long. (B) Flat-lying layering in olivine gabbronorite from the region south of the Azen Creek Zone, south-central Dana Township. The hammer handle is 33 cm long.

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In Figure 6-4 anomalous PGE values (>500-1000 ppb Pt and/or Pd) occur throughout the

length of all three drill holes and higher-grade intersections are indicated, typically

occurring as a “core” area within the lower one-third of the mineralized zone. Similar

geology, geometry and mineralization occurs within the Marginal Series rocks at the

Dana North PGE-Cu-Ni Deposit (Fig. 6-2).

6.5.1 General Geochemistry

Average and median PGE-Cu-Ni concentrations for mineralized and unmineralized

samples from the Marginal Zone in the River Valley intrusion are listed in Table 6-1.

Data from sulphide-bearing felsic and mafic dykes and the BZ, BX and IBZ all show

moderate to high average Pt+Pd, reaching a maximum in the BX. Samples from the IBZ,

BX, and BZ have average Pd/Pt and Cu/Ni ratios of 1.1 to 2.3 and 1.7 to 4.8,

respectively, which is distinctive from the low sulphide, Cu-poor assemblages of the LU

and Mafic Dikes-2 (Table 6-1); two samples from the latter have average Pd/Pt and

Cu/Ni ratios of 0.8 and 0.95, respectively. The concentrations of PGE in the

unmineralized and mineralized samples are similar to those reported in the East Bull

Lake (Peck et al., 1995) and Agnew Lake intrusions (Pacific North West Capital Corp.

and Anglo American Platinum Corporation Limited, unpublished data). Footwall rocks

have low Pt, Pd and Au (average = 24.4 ppb Pt+Pd+Au), and Pd/Pt and Cu/Ni are <1

(Table 6-1).

Metal values for unmineralized rocks (i.e. samples with <100 ppm Cu and/or <0.05

wt% S) that form large parts of the intrusion and/or which are feeders, are provided by

data from the LU and Mafic Dikes-2 in Table 6-1. These rocks have anomalous PGE

concentrations, averaging ~34-41 ppb Pt+Pd, and their metal ratios, Pd/Pt and Cu/Ni, are

both <1, which is unlike the mineralized samples from the IBZ (~139 ppb Pt+Pd, 1.1

Pd/Pt, 1.7 Cu/Ni) and BX (~960 Pt+Pd, 2.3 Pd/Pt, 4.8 Cu/Ni). Similar PGE

concentrations of 7 ppb Pd and 13 ppb Pt (20 ppb Pt+Pd) are reported from

unmineralized mafic rocks from below the J-M Reef in the Stillwater Complex, Montana

(Peck and Keays, 1990).

Chondrite-normalized PGE diagrams (recalculated to metals in 100% sulphide) for

mineralized (3-5% pyrrhotite + chalcopyrite) and unmineralized samples (<100 ppm Cu

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and/or <0.05 wt% S) from the Dana Lake and Lismer’s Ridge areas are presented in

Figure 6-5.

Figure 6-5. Chondrite-normalized (metals in 100% sulphide) diagram comparing data for

contact-type sulphide mineralization from the Lower Series rocks at East Bull Lake

intrusion (EBLI) and mineralized and non-mineralized rocks from the River Valley (RVI)

intrusion with chalcophile data from the J-M Reef (Stillwater) and the Portimo Complex,

Finland. River Valley data are averages (6 samples) from the Dana Lake and Lismer’s

Ridge areas (after James et al., 2002b). Also included for comparison is structurally

controlled sulphide mineralization from the East Bull Lake intrusion (Parisien Lake

Deformation Zone).

Metal abundances and patterns for mineralized samples from the River Valley intrusion

are very similar to those from the East Bull Lake intrusion, and both data sets show

patterns and absolute abundances that are similar to contact-type, low sulphide PGE

mineralization at the Konttijarvi-Portimo Complex, Finland (Alapieti and Lahtinen,

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2002) and sulphides from the J-M Reef, Stillwater, USA (Barnes and Naldrett, 1985),

both of which are accepted to be magmatic, sulphide-associated PGE deposits. Samples

with trace mineralization show a wide variation in PGE abundance and the pattern from

an average of six unmineralized samples, shown in Figure 6-5, shows a pattern not unlike

the mineralized samples; this suggests that the mineralized and unmineralized rocks are

genetically related. Overall, the PGE patterns are consistent with those of magmatic

sulphides and contrast sharply with the hydrothermal pattern exhibited by structurally-

controlled sulphide mineralization from the Parisien Lake Deformation Zone in the East

Bull Lake intrusion (Peck et al., 1993a).

6.6 Petrology and Geochemistry of Drill Hole RV00-22

Diamond drill hole RV00-22, located in the area of the Dana North deposit, was

completed in July 2000 as part of the initial exploration drilling program by Pacific North

West Capital and Anglo American Platinum Corporation Limited (Fig. 6-2). The drill

hole, drilled at an inclination of 45° toward 86° and totalling 259 m, was collared in the

massive Layered Unit and continued through the Inclusion-bearing, Breccia, Boundary,

and Footwall Breccia units, terminating in the Footwall rocks. A summary of the

stratigraphy recorded in the drill core of RV00-22 and some of the principal geochemical

features are provided in Tables 6-2 and 6-3; the drill core log and complete assay results

are provided in Appendix 3. Selected photographs of the drill core are provided in

Photos 6-6 to 6-9.

Two data sets were compiled from the core samples. The first, referred to as Group-

1, consists of 112 core samples, with ninety-nine of these samples coming from the

logging and sampling efforts of Pacific North West Capital Corp. geologists, sampling at

approximately 1-2 m intervals; these core samples were analyzed for Pt, Pd, Au, Cu and

Ni at XRAL Laboratories and S, Se at the Geoscience Laboratories in Sudbury.

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Unit From To Int n Samples Rock Type(m) (m) (m)

LU 2.50 89.50 87.00 27 22690 to 29642 melagabbro, gabbro, leucogabbro;rare, crude layering

IBZ 91.00 160.80 69.80 20 29643 to 29683 pegmatitic leucogabbro-gabbroBX 160.80 224.93 64.13 55 29684 to 29753 melagabbro-gabbro-leucogabbro fragments in

gabbroic matrix; blue quartz patches and biotiteBZ 229.00 233.20 4.20 4 29754 to 29759 felsic fragments, felsic dykes;

gabbro matrix and gabbro dykesFBX 233.20 241.50 8.30 3 29760 to 29764 felsic gneiss; sheared gabbro

FW 244.00 256.00 12.00 3 RV22-01, 02, 03 felsic gneiss; sheared gabbro Table 6-2a. Summary of drill core log for drill hole RV00-22, Dana Deposit (North),

River Valley intrusion.. LU = Layered Units, IBZ = Inclusion-Bearing Unit, BX =

Breccia Unit, BZ = Boundary Unit, FBX = Footwall Breccia; n = number of samples.

Unit *Avg. 3E Avg. Cu Avg. Ni Pd/Pt Cu/Ni Pd/Cu(ppb) (ppm) (ppm)

LU 61 457 131 0.6 3.5 10620

IBZ 223 63 47 1 1.8 713BX 2380 1317 256 2.7 5.1 1144

BZ 197 217 145 2.2 1.9 3236

FBX 44 82 138 1.6 0.6 16354

FW 6 72 175 1.2 0.4 73937

Table 6-2b. Summary of important whole-rock chalcophile averages and ratios for drill

hole RV00-22, Dana Deposit (North), River Valley intrusion. Values for 3E = Pt+Pd+Au;

LU = Layered Units, IBZ = Inclusion-Bearing Unit, BX = Breccia Unit, BZ = Boundary

Unit, FBX = Footwall Breccia. See Appendix 1 for complete data listing.

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Se S Ni Ir Ru Rh PtUnit ppb wt% ppm ppb ppb ppb ppb

Layered (n=8) A 219 0.06 189.00 0.72 1.13 1.06 16.01metal in 100% sulphide B 36.50 114975.00 438.00 687.42 644.83 9739.42Inclusion-bearing (n=6) A 73 0.02 40.00 2.88 1.75 10.93 99.08metal in 100% sulphide B 36.50 73000.00 5256.00 3193.75 19947.25 180821.00Breccia (n=9) A 2093 0.33 321.00 13.88 4.84 45.39 663.61metal in 100% sulphide B 36.50 35504.55 1535.21 535.33 5020.41 73399.29Boundary (n=1) A 598 0.15 94.00 1.46 0.87 8.50 68.30metal in 100% sulphide B 36.50 22873.33 355.27 211.70 2068.33 16619.67Footwall Breccia (n=1) A 292 0.43 123.00 0.19 0.36 0.69 3.53metal in 100% sulphide B 36.50 10440.70 16.13 30.56 58.57 299.64Footwall (n=3) A 226 0.36 175.00 0.17 0.42 0.17 2.61metal in 100% sulphide B 36.50 17743.06 17.24 42.58 17.24 264.63

Pd Au Cu S/Se Cu/Ni Pd/Pt Pd/IrUnit ppb ppb ppm

Layered (n=8) 15.32 5.08 116.00 2746 0.61 0.96 21.3metal in 100% sulphide 9321.69 3090.33 70566.67Inclusion-bearing (n=6) 412.16 6.57 47.00 2506 1.18 4.16 143.1metal in 100% sulphide 752192.00 11990.25 85775.00Breccia (n=9) 1865.69 109.30 1231.00 1564 3.83 2.81 134.4metal in 100% sulphide 206356.62 12089.24 136156.06Boundary (n=1) 214.00 18.50 476.00 2508 5.06 3.13 146.6metal in 100% sulphide 52073.33 4501.67 115826.67Footwall Breccia (n=1) 4.87 1.71 95.60 14726 0.78 1.38 25.6metal in 100% sulphide 413.38 145.15 8114.88Footwall (n=3) 3.06 0.36 72.00 16077 0.41 1.17 18.0metal in 100% sulphide 310.25 36.50 7300.00

Table 6-3. A: Average whole-rock chalcophile element concentrations for core samples

from drill hole RV00-22 and some important average ratios. B: Concentrations in the

same samples (n = number of samples), recalculated to metal 100% sulphide. See

Appendix 1 for complete data listing.

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An additional 13 “fill-in” samples were subsequently collected and analyzed for Pt, Pd,

Au, Cu, Ni, S and Se at the Geoscience Laboratories in Sudbury; these samples are also

used in the 28 sample set of Group-2. Group-1 data provides a detailed

chemostratigraphic section, in terms of Pt, Pd, Au, Cu, Ni, S and Se, through the

stratigraphy of the Marginal Series rocks (LU to FBX) and into the FW. The second data

set, referred to as Group-2, consists of 28 samples, mainly derived from the original core

pulp samples but also comprising an additional 13 samples from original drill core (also

used in the Group-1 data set), analyzed for PGE (Ir, Ru, Rh, Pd, Pt, Au), and whole-rock

major, trace and rare-earth elements at the Geoscience Laboratories; complete listings of

these data are in Appendix 3. Group-2 data provides more detailed information in terms

of the geochemical variation through the Marginal Series rocks (LU to FBX) rocks.

A total of 21 thin sections from Group-1 were examined in detail and petrographic

descriptions for these samples are provided in Appendix 2. Layered Unit samples (3

samples) comprise medium-grained gabbronorite with relict granular-idiomorphic and

granular-hypidiomorphic textures (Photo 6-9b). Inclusion-bearing Unit samples (2

samples) comprise medium-grained leucogabbro with relict granular-idiomorphic

textures. The 13 samples from the Breccia Unit are dominated by medium-grained

gabbro and subordinate melagabbro with relict granular-idiomorphic and granular-

hypidiomorphic textures (Photo 6-8). Of these 13 samples, 8 have well preserved

igneous textures but 5 samples, which are finer grained, are extensively recrystallized.

Relict igneous textures consist of actinolite and blue-green hornblende pseudomorphing

pyroxene, tremolite after olivine (rare), and plagioclase, replaced in varying degrees, by

sericite, amphibole and saussurite.

All samples possess mineral assemblages (chlorite-actinolite/tremolite) typical of

greenschist facies metamorphism along with evidence for secondary, low-temperature

(hydrothermal) alteration (i.e. saussuritization, secondary quartz, Photo 6-6b). Sulphides

(chalcopyrite > pyrrhotite > pentlandite > pyrite) with magmatic textures (mainly

disseminated and interstitial, Photo 6-8a) are atypical and most sulphides occur as very

fine-grained patches associated with fine- to medium-grained patches of saussuritization

which is within or adjacent to plagioclase grains; these sulphide patches commonly

comprise biotite, blue-green hornblende and epidote.

346

Photo 6-6. Core from diamond drill hole RV00-22. (A) Footwall (RV22-03; 2.1 ppb Pd, 1.7 ppb Pt, 60 ppm Cu, 133 ppm Ni): Fine-grained migmatite with felsic leucosome (cream-white-yellow) and mafic melanosome with several percent disseminated sulphide (ds) and blue quartz (bq); pyrite is dominant with subordinate chalcopyrite and pyrrhotite. (B) Boundary Unit (29756; 214 ppb Pd, 68 ppb Pt, 476 ppm Cu, 94 ppm Ni): Fine- to medium-grained CIPW gabbronorite with saussuritized and epidotized plagioclase grains (a-plag) and fine-grained blue quartz. The Canadian one cent piece is about 1.8 cm in diameter.

347

Photo 6-7. Core from diamond drill hole RV00-22. (A) Breccia Unit (29753; 1102 ppb Pd, 347 ppb Pt, 348 ppm Cu, 341 ppm Ni): CIPW olivine gabbronorite with several % finely disseminated sulphide (chalcopyrite-pyrrhotite) and distinct blue quartz; the latter is often associated with higher PGE grades. (B) Breccia Unit (29733; 872 ppb Pd, 324 ppb Pt, 1130 ppm Cu, 328 ppm Ni): CIPW quartz normative gabbro with several % disseminated sulphide (ds) and a distinct patch of altered cream-white feldspar and blue-grey quartz (bq). The Canadian one cent piece is about 1.8 cm in diameter.

348

Photo 6-8. Core from drill hole RV00-22. (A) Breccia Unit (29707; 1733 ppb Pd, 718 ppb Pt, 2700 ppm Cu, 615 ppm Ni): Medium-grained gabbro with interstitial sulphide (is), disseminated sulphide (ds), and veinlets of remobilized sulphide (vs); chalcopyrite and pyrrhotite are the dominant sulphides. (B) Breccia Unit (29702; 6670 ppb Pd, 2375 ppb Pt, 3600 ppm Cu, 532 ppm Ni): Medium-grained gabbro with disseminated sulphide (ds) and fine-grained blue-grey quartz. The Canadian one cent piece is about 1.8 cm in diameter.

349

Photo 6-9. Core from drill hole RV00-22. (A) Inclusion-bearing Unit (29645; 1864 ppb Pd, 169 ppb Pt, 41 ppm Cu, 44 ppm Ni): Coarser grained gabbroic autolith in medium-grained mafic matrix with trace disseminated sulphide (ds). (B) Layered Unit (22692; 21 ppb Pd, 21 ppb Pt, 117 ppm Cu, 116 ppm Ni): Medium-grained CIPW olivine gabbronorite with minor disseminated sulphide (ds) and relict igneous textures - pyroxene is pseudomorphed by actinolite and blue-green hornblende and plagioclase is replaced in varying degrees by sericite, amphibole (uralite) and saussurite. The Canadian one cent piece is about 1.8 cm in diameter.

350

Fine-grained disseminated chalcopyrite, pyrrhotite and pyrite can occur with tremolite,

which occurs as pseudomorphs after olivine and/or orthopyroxene.


Whole-rock major, trace, rare-earth element, and PGE data for selected samples from

Group-2 (28 samples) data are presented in Table 6-4; a compete listing of the Group-2

data is provided in Appendix 3. All of the samples from the intrusion, with the exception

of sample 29753 from the BX, classify as sub-alkaline rocks (Miyashiro, 1978). CIPW

normative calculations were completed on 25 of the 28 samples and a summary of these

results for selected samples are provided in Table 6-5; rock types were determined on the

basis of the weight percent normative minerals. All eight samples from the LU are

olivine-normative with seven samples classifying as olivine leucogabbronorite and one

sample (29612) classifying as gabbronorite. All six samples from the IBZ are olivine-

normative with three samples classifying as olivine leucogabbronorite and the other three

classifying as leucogabbronorite. Nine of the ten samples from the BX are olivine-

normative with only one sample (29733), a gabbro, being quartz-normative (quartz

oversaturated). Five of the samples are classified as gabbronorite, two as

leucogabbronorite, one as olivine leucogabbronorite and one as olivine gabbronorite.

The single FBX sample is olivine-normative and are classified as leucogabbronorite with

a low (0.18) calculated corundum content, due to an increase in aluminium which could

be a result of interaction with the footwall paragneiss.

Rock compositions from the Breccia Unit typically display the widest variation due

to extreme irregularity in the proportions of fragments and matrix. Estimating the

proportion of fragments and matrix in drill core is also problematic due to a lack of

obvious contacts between fragments and the hosting matrix and in many instances it is

difficult to discern the fragments from the matrix.


Selected major elements for samples from Group-2 are plotted against stratigraphic

height (drill hole depth) in Figure 6-6. Silica concentrations range from 45.26 to 51.09

wt% SiO2 in the intrusion, and samples from the FW, FBX and BZ show the highest

overall wt% SiO2.

351

Sample 22692 29635 29645 29683 29702 29753 29756 29762 RV22-03From (m) 2.5 77 92.5 160 181 224.7 229 236.5 255.78

Unit LU LU IBZ IBZ BX BX BZ FBX FWSiO2 48.62 45.26 49.64 51.09 48.81 45.79 51.18 50.59 55.70TiO2 0.47 0.68 0.39 0.14 0.14 0.27 0.34 0.71 0.37Al2O3 16.84 13.58 22.73 21.85 20.48 16.40 15.79 18.00 19.38

Fe2O3* 12.11 15.56 6.85 5.52 8.70 11.43 11.28 10.40 7.25MnO 0.17 0.21 0.10 0.10 0.12 0.18 0.17 0.13 0.08MgO 8.74 11.01 4.52 5.63 5.98 10.54 8.06 7.21 4.97CaO 9.32 8.40 10.90 10.99 9.67 7.89 9.98 6.18 4.44Na2O 2.24 1.49 3.21 2.90 2.70 2.36 2.10 3.22 4.64K2O 0.63 0.79 0.87 0.80 0.79 0.89 1.00 1.34 1.14P2O5 0.06 0.06 0.05 0.01 0.01 0.03 0.01 0.06 0.05

S 0.06 0.08 0.03 0.01 0.78 0.34 0.15 0.43 0.26Total 101.0 99.4 100.5 100.4 98.9 98.6 100.9 100.2 100.3Mg# 62.68 62.22 60.56 70.36 61.53 68.21 62.45 61.74 61.47

Pt 21.4 9.76 168.6 60.6 2375 347 68.3 3.53 1.71Pd 20.9 12.02 1864 125.5 6670 1102 214 4.87 2.12Ni 116 158 44 19 532 341 94 123 133Cu 117 134 40.5 48.9 3600 348 476 95.6 60La 7.46 6.86 5.61 1.76 2.27 6.09 3.13 17.41 38.80Ce 15.47 14.47 11.73 3.54 4.62 12.04 6.31 29.69 65.62Pr 1.95 1.85 1.47 0.45 0.58 1.44 0.83 3.28 6.57Nd 7.85 7.34 5.71 1.81 2.31 5.90 3.55 11.30 21.86Zr 39.89 48.02 34.60 13.71 9.56 15.30 11.62 30.55 55.50Sm 1.82 1.75 1.28 0.42 0.54 1.26 0.98 1.60 2.60Eu 0.70 0.67 0.64 0.32 0.50 0.70 0.57 1.74 2.30Gd 1.96 1.91 1.40 0.49 0.60 1.31 1.15 1.18 1.88Tb 0.34 0.33 0.24 0.09 0.11 0.21 0.20 0.16 0.21Dy 2.14 2.06 1.48 0.61 0.68 1.32 1.25 0.90 1.06Y 12.97 11.92 8.65 3.48 4.00 7.87 7.79 5.64 6.09

Ho 0.49 0.46 0.33 0.14 0.15 0.28 0.30 0.20 0.22Er 1.39 1.26 0.91 0.36 0.44 0.84 0.86 0.63 0.71Tm 0.21 0.21 0.14 0.06 0.07 0.14 0.14 0.10 0.13Yb 1.37 1.23 0.91 0.38 0.43 0.95 0.88 0.76 0.84Lu 0.22 0.21 0.15 0.06 0.07 0.16 0.15 0.14 0.15

∑REE 44 41 32 11 13 33 21 70 143(Th/Yb)N 5.46 6.27 5.99 9.46 2.83 3.48 3.16 8.55 15.74(Nb/Th)N 0.19 0.20 0.25 0.15 0.18 0.17 0.09 0.14 0.09

Zr/Sm 21.92 27.44 27.03 32.64 17.70 12.14 11.86 19.09 21.35Nb/Ta 13.87 14.80 13.13 5.07 2.13 3.64 2.53 8.73 4.39

Table 6-4. Geochemical data (Group-2) from drill hole RV00-22, Dana North Deposit, River Valley intrusion. Fe2O3*=total iron; SiO2 to Total=wt%; Pt, Pd=ppb; Ni to Lu=ppm; N=primitive mantle-normalized

352

Sample 22692 22696 29601 29607 29612 29618 29622 29635 29645 29662 29670Rock Type OGN OGN OGN OGN GN OGN OGN OGN OLGN LGN OLGN

Unit LU LU LU LU LU LU LU LU IBZ IBZ IBZNorm Minerals

quartzplagioclase 53.91 53.50 56.67 55.81 58.01 47.03 57.45 42.44 73.12 65.43 66.27orthoclase 3.78 3.60 3.60 3.31 4.14 3.13 3.90 4.85 5.20 4.37 2.54corundumdiopside 9.54 8.77 6.71 9.31 8.72 12.07 8.64 11.19 7.03 8.75 5.28

hypersthene 18.03 19.15 16.58 16.50 17.67 19.16 16.81 17.65 0.53 11.42 10.53olivine 10.91 11.35 12.58 11.41 7.90 14.53 9.50 18.85 11.70 7.65 13.32ilmenite 0.91 0.74 0.82 0.89 0.85 0.80 0.84 1.35 0.74 0.49 0.21

magnetite 2.49 2.52 2.52 2.42 2.23 3.00 2.38 3.29 1.41 1.55 1.70apatite 0.14 0.12 0.14 0.12 0.14 0.05 0.09 0.14 0.12 0.07 0.02zircon 0.01 0.01 0.01

chromitepyrite 0.13 0.06 0.13 0.08 0.15 0.11 0.19 0.17 0.06 0.04 0.02calcite 0.16 0.23 0.27 0.16 0.23 0.16 0.25 0.09 0.14 0.25 0.14

*Total: 100.01 100.04 100.02 100.02 100.04 100.04 100.05 100.03 100.05 100.02 100.03

Sample 29683 29689 29696 29702 29707 29717 29721 29733 29744 29756 29762Rock Type LGN GN GN LGN GN GN LGN G OLGN GN LGN

Unit IBZ BX BX BX BX BX BX BX BX BX FBXNorm Minerals

quartz 3.34plagioclase 69.73 52.45 39.35 65.97 55.10 51.10 62.23 32.83 62.15 48.91 59.01orthoclase 4.79 1.77 3.37 4.79 2.25 2.84 2.72 4.37 3.49 5.97 8.16corundum 0.18diopside 8.19 16.09 14.53 5.41 13.34 10.97 9.21 13.02 9.45 15.38

hypersthene 11.08 18.65 35.24 12.85 21.52 30.54 18.46 41.80 10.37 24.64 21.19olivine 4.65 8.73 3.52 7.24 3.59 1.63 5.19 12.14 1.76 6.81ilmenite 0.27 0.25 0.46 0.27 0.36 0.32 0.30 0.55 0.42 0.65 1.39

magnetite 1.13 1.88 2.78 1.81 2.09 2.16 1.65 2.93 1.78 2.31 2.16apatite 0.02 0.02 0.02 0.02 0.02 0.02 0.02 0.05 0.02 0.02 0.14zircon

chromitepyrite 0.02 0.08 0.64 1.70 1.70 0.38 0.11 1.04 0.02 0.32 0.93calcite 0.14 0.09 0.16 0.05 0.14 0.09 0.16 0.11 0.20 0.09 0.07

*Total: 100.02 100.01 100.07 100.11 100.11 100.05 100.05 100.04 100.04 100.05 100.04

Table 6-5. CIPW normative calculations for samples from drill hole RV00-22, Dana North Deposit, River Valley intrusion. CIPW minerals normalized to 100%; rock names based on weight % normative minerals; OGN=olivine gabbronorite; MGN=melagabbronorite; GN=gabbronorite; OMGN=olivine melagabbronorite; OLGN=olivine leucogabbronorite; LG=leucogabbro

353

0

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2750 0.1 0.2 0.3 0.4 0.5 0.6 0.7 0.8

TiO2 (wt%)

Dril

l Hol

e D

epth

(m)

LU

IBZ

BX

FW

FBXBZ

Figure 6-6a. Variation in wt% TiO2 with drill hole depth (metres) from drill hole RV00-

22, Dana North Deposit, River Valley intrusion.

354

0

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2750 2 4 6 8 10 12

MgO (wt%)

Dril

l Hol

e D

epth

(m)

14

LU

IBZ

BX

FW

FBXBZ

Figure 6-6b. Variation in wt% MgO with drill hole depth (metres) from drill hole RV00-

22, Dana North Deposit, River Valley intrusion.

355

There is a slight overall decrease through the anomalous BX, a further decrease through

the IBZ and a still further decrease into the lower LU; silica contents show a gradual

increase upward through the LU. The relative rise in SiO2 values in the BX corresponds

well with the highest Pt+Pd concentrations in this unit, suggesting a relationship between

increased silica content and higher grade PGE. This supports observations that higher

grades of PGE tend to be associated with patches of blue-grey quartz.

The concentration of TiO2 is primarily controlled by the abundance of Fe-Ti oxide

minerals, primarily titanomagnetite, and by fractionation whereby TiO2 behaves

incompatibly. The TiO2 concentration ranges from 0.11 to 0.68 wt% TiO2 in the

intrusion and are highest in the LU, FBX and FW. In the BX, TiO2 is the lowest,

averaging 0.20 wt% and in the overlying IBZ, TiO2 is slightly higher averaging 0.23

wt%; the lowest single value of 0.11 wt% TiO2 comes from the lower IBZ. A maximum

of 0.68 wt% TiO2 is reached just above the contact between the LU and IBZ, followed by

a drop in TiO2 concentrations to an average 0.43 wt% for the remainder of the LU

samples. In the BX itself, the highest TiO2 concentration of 0.28 wt% is coincident with

the only quartz-normative sample (29733). In drill core, this 0.70 m long sample section

contains a high proportion (~10%) of blue quartz which occurs with about 2% finely

disseminated sulphide (Photo 6-7). This association between relatively high SiO2 and

TiO2 whole-rock concentrations suggests that the blue to blue-grey quartz colouration is

due impurities of titanium in the quartz. Ma et al. (2001) presented data which indicated

that sub-micrometre inclusions of ilmenite are a common cause of the blue colour in

quartz.

Concentrations of Fe2O3* range from 5.52 to 15.56 wt% Fe2O3* with the highest

average values (12.54 wt%) occurring in the LU where the samples define a gradual up-

section decrease in Fe2O3*. As with peak TiO2 concentrations, a maximum of 15.56 wt%

Fe2O3* is reached just above the contact between the LU and IBZ, followed by a drop in

Fe2O3* concentrations for the remainder of the LU samples. The concentration of Fe2O3*

is elevated in the BX (average = 10.40 wt%) relative to the IBZ (average = 6.79 wt%)

with values in the BX approaching those in the LU (average = 12.54 wt%). In the BX

itself, and as seen with TiO2, the highest concentration of 13.99 wt% Fe2O3* is coincident

with the only quartz-normative sample (29733).

356

The Mg-number ranges from 0.61 to 0.73 in the intrusion, averaging 0.62 in the LU,

and averaging 0.67 in both the IBZ and BX; the average Mg-number from the LU is the

same as the individual Mg-numbers of the BZ and FBX and the average Mg-number of

the FW. The higher Mg-numbers in the IBZ and BX reflects the primitive (mafic) nature

of the fragments that occur within these units, particularly in the BX where all the

fragments contain >12 wt% MgO (see Section 6.7). Reflecting the high Mg

compositions of the BX fragments, the Mg-number shows an overall increase through the

BX, followed by a relatively sharp decline through the IBZ, and finally a gradual overall

increase in the LU; the increase in Mg-number through the LU is more than likely the

result of fractionation of titanomagnetite and magnetite, which may be what is reflected

in the increased TiO2 and Fe2O3 concentrations in the lower part of the LU.

Compositions of MgO range from as low as 4.3 wt% in the upper part of the IBZ to

11.8 wt% in the BX, with the highest average concentrations occurring in the BX (~9.3

wt% MgO) and LU (~8.9 wt% MgO). Core samples from the LU have the highest CIPW

olivine-normative values (average 12.1% normative olivine) which is reflected in the

high MgO concentrations. Concentrations of MgO mirror those of Fe2O3*, exhibiting the

greatest variation through the BX, and reflecting the variability in the proportion of

fragments to matrix within each of the drill core sample sections; higher MgO and Fe2O3

values are probably a consequence of higher proportions of fragments relative to matrix

(see Section 6.7).

Concentrations of Al2O3 range from 10.95 wt% in the lower BX to 23.49 wt% in the

upper IBZ, share very similar averages in the BX (16.49 wt%) and LU (16.61 wt%) and

is consistently higher in the IBZ where it averages 21.74 wt%. These higher aluminium

contents are reflective of the leucocratic nature of the rocks in the IBZ.


Selected trace elements for samples from Group-2 are plotted against stratigraphic

height (drill hole depth) in Figure 6-7. A summary of the principal trace and rare-earth

element abundances and ratios from of the units is provided in Table 6-6. Relative

abundances of the incompatible trace elements Zr, Y, Nb and La are primarily governed

by the proportions of primocrysts (solid) to interstitial components (liquid) in the sample

and their relative amount of differentiation (Vogel et al., 1999).

357

Unit N Eu/Eu* (La/Sm)N (La/Yb)N (La/Yb)N ∑REERange Range Average Range Range ppm

Layered 8 1.094-1.258 2.97-4.38 3.58 2.58-4.06 24-43Inclusion-bearing 6 1.418-2.502 3.16-4.38 3.40 2.30-4.24 6-32

Breccia 9 1.095-2.669 2.88-4.83 2.88 1.53-4.36 7-24Boundary 1 - - 2.42 - -

Footwall Breccia 1 - - 15.60 - -Footwall 3 2.981-4.073 10.67-14.92 20.31 13.27-31.45 83-143

Table 6-6. Principal features of trace and REE abundances and ratios for each of the units

intersected in drill hole RV00-22, River Valley intrusion. N=number of samples in the

average or range. The value Eu/Eu*= EuN/√[(SmN).(GdN)] was calculated using

Geometric Mean method of Taylor and McLennan (1985) where “N” indicates chondrite

normalized.

358

0

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225

250

2750 10 20 30 40 50

Zr (ppm)

Dril

l Hol

e D

epth

(m)

60

LU

IBZ

BX

FW

FBXBZ

Figure 6-7a. Variation in whole-rock Zr (ppm) against drill hole depth (metres) from drill

hole RV00-22, Dana North Deposit, River Valley intrusion.

359

0

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125

150

175

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225

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2750 2 4 6 8 10

(Th/Nb)N

Dril

l Hol

e D

epth

(m)

12

LU

IBZ

BX

FW

FBXBZ

Figure 6-7b. Variation in primitive mantle-normalized (Th/Nb)N against drill hole depth

(metres) from drill hole RV00-22, Dana North Deposit, River Valley intrusion.

360

The highest average incompatible trace element abundances occur in the LU (Zr = 32, Y

= 11.33, Nb = 1.7, La = 6.23), reflecting the evolved nature of these rocks, whereas the

lowest average abundances occur in the BX (Zr = 9, Y = 5.39, Nb = 0.5, La = 2.87),

reflecting the primitive (high MgO) nature of these rocks. Upward increasing

concentrations in Y and Nb through the IBZ are indicative of normal fractionation.

Although trace element values in the BX are highly variable, they do define a general up-

section decrease in all of these trace elements. This variability and overall decrease could

reflect the influx of new magma(s) and/or subsequent mixing with resident magma and

rocks. There is a general upward increase in (Th/Yb)N with the greatest variation in the

BX. Values of (Th/Yb)N for samples from the BX, IBZ and LU range from about 2 to 10

times that of primitive mantle (primitive mantle Th/Yb ~0.17; McDonough and Sun,

1995) suggesting that these rocks have been crustally contaminated.

Europium is relatively abundant compared to other REE in plagioclase and Eu

anomalies (positive or negative) can be used as a measure of plagioclase fractionation in

a magma. Values of Eu/Eu* are calculated using the geometric mean method of Taylor

and McLennan (1985) whereby calculated Eu/Eu* values >1 are considered positive and

those <1 are considered negative Eu/Eu* anomalies; for simplicity Eu/Eu* anomalies are

referred to as Eu anomalies. The Eu/Eu* values show a gradual decrease with

stratigraphic height through the IBZ and LU with the Eu anomalies becoming less

pronounced upward through the LU. This gradual decrease likely reflects the removal of

plagioclase from the melt through crystal fractionation.

The ratio of (La/Sm)N (normalized to primitive mantle) can provide a good

indication as to whether or not magma has interacted with crustal rocks; higher ratios

suggests increased crustal assimilation. In the plot of (La/Sm)N, the highest values are

within the FBX ((La/Sm)N = 7.03) and FW (average (La/Sm)N = 8.07); these values are

representative of the country rock (FW) and region of mixing/assimilation (FBX). The

one BZ ((La/Sm)N = 2.06) value is slightly lower than the overlying BX (average

(La/Sm)N = 2.55) and the IBZ (average (La/Sm)N = 2.62) is only slightly higher than the

BX and LU (average (La/Sm)N = 2.52). The consistently low (La/Sm)N values through

the BX and IBZ and their similarity with the overlying LU suggests that there was very

little assimilation of local country rock. If local crustal contamination would have played

361

an essential role, then one would expect that values in the BX and BZ would have been

closer to those for the FBX and FW components. This lack of a local contamination

signature in the BX and in the other units of the Marginal Series rocks is an indication

that chemical contamination from local footwall rocks was not a major factor on

mineralization. However, assimilation of crust appears to have driven the magma to S-

saturation and the formation of sulphides in a deep-seated staging magma chamber, as

suggested for the East Bull Lake intrusion (James et al., 2002a).

Chondrite-normalized REE patterns for rocks from the River Valley intrusion are

illustrated in Figure 6-8 and some of the more important features of these plots are

summarized in Table 6-6. All River Valley intrusion rocks have patterns of LREE

enrichment and a narrow range in (La/Yb)N values from 2.42 to 3.58; La/Yb ratios are

used to demonstrate the relative abundance and extent of fractionation of the LREE from

the HREE. Vogel et al. (1999) reported similar REE patterns and a narrow range in

(La/Yb)N (2.0-6.5) from the Agnew Lake intrusion. The greatest range in (La/Yb)N

values are from the IBZ and BX, reflecting the variability in rock types within these

units. All individual samples from the River Valley intrusion units (LU, IBZ, BX and

BZ) have strong positive Eu anomalies with absolute Eu/Eu* values ranging from 1.09 to

2.67, with the highest average value from the IBZ (1.81); the FBX and FW samples have

strong Eu/Eu* values of 3.85 and 3.40, respectively (Table 6-6). The average ∑REE is

highest in the footwall rocks (105 ppm), gradually decreasing through the FBX (69 ppm)

and BZ (20 ppm). Average ∑REE are lowest in the BX (17 ppm) and IBZ (17 ppm) and

are elevated in the LU (37), increasing upward through the LU. The gradual increase in

∑REE with stratigraphic height and a concomitant decrease in the positive Eu/Eu*

anomalies are consistent with closed-system magmatic differentiation dominated by

plagioclase fractionation.

Individual samples from units in the River Valley intrusion show very similar REE

patterns that generally parallel one another (Fig. 6-8).

362

Figure 6-8. Chondrite-normalized rare-earth element plots for average samples from drill

hole RV00-22, Dana North Deposit, River Valley intrusion. “RVI – Parent Magma” may

represent the parental magma composition for the River Valley intrusion (James et al.,

2002a). Data for “Matachewan Dike” is from Easton and Hrominchuk (1999), and data

for “EBLI – Lower Series” and “EBLI – Parent Magma” (estimate of East Bull Lake

intrusion parental magma composition) are from the East Bull Lake intrusion (Peck et al.,

1995). Normalizing values are from Lodders and Fegley (1998).

363

Slight variations in the REE slope between individual samples, approximated by the

(La/Yb)N ratio (Table 6-6), can be attributed to modal differences whereby samples with

lower La/Yb values have higher relative mafic mineral to plagioclase contents and vice

versa, which is consistent with known REE partitioning in minerals (Henderson, 1984).

Heavy REE and LREE patterns in the LU, IBZ and BX range from about 6-30, 1.5-24

and 2-26 times chondrite, respectively. Footwall rocks and FBX show the highest

enrichment in LREE and the IBZ and BX show the lowest LREE and HREE enrichment

patterns. Average chondrite-normalized patterns from the LU, IBZ, BX and BZ bracket

the pattern for an average of nine samples from the East Bull Lake Lower Series (Fig. 6–

10a).

James et al. (2002a) described samples of boninite-like rocks from the River Valley

and East Bull Lake intrusions, and suggested that these may represent boninitic parent

magma compositions for the East Bull Lake suite intrusions. Of particular note is sample

H292 (Fig. 6-10, “RVI Parent Magma”) which is a fine-grained orthopyroxene-phyric

norite from the Marginal Zone in the River Valley intrusion (Dana Township). This

sample exhibits a flat (~10 x chondrite) to very slightly U-shaped REE pattern and has

relatively high SiO2 (51.2 wt%), Al2O3 (13.1 wt%) and MgO (11.5 wt%; Mg-number =

68), and low TiO2 (0.33 wt%) and alkalis (Na2O+K2O = 0.73 wt%); Easton (2003) also

reported data from the same lithology (sample 99RME-2291).

Primitive mantle-normalized multi-element plots for average concentrations in the

River Valley intrusion units and the BX are shown in Figure 6-9. The patterns are sub-

parallel and show the same relative arrangement between units as in the REE patterns in

Figure 6-8. All of the average primitive mantle-normalized patterns for River Valley

intrusion rocks and all but one of the individual samples (LU 29635) show pronounced

positive Sr anomalies which correlate with high modal plagioclase. Of particular

importance in multi-element patterns are negative high field strength element (HFSE)

anomalies (i.e. Nb, Ta and P); Ti shows subtle positive and negative anomalies. The

average patterns from the LU, IBZ and BX have strong negative Nb, Ta and P anomalies

(relative to the LREE) and weak negative Ti anomalies which, along with LREE-

enrichment trends, are characteristics of magma which has interacted with a crustal

reservoir (Lightfoot and Naldrett, 1996).

364

Figure 6-9. Primitive mantle-normalized multi-element diagrams for samples from drill hole RV00-22, Dana North Deposit, River Valley intrusion. (A) Averages from various units of the River Valley intrusion and footwall rocks. (B) Average compositions of River Valley rocks compared with individual Breccia Unit (BX) compositions. Normalizing values are from McDonough and Sun (1995).

365

The pattern for the BZ also shows negative Nb+Ta and P anomalies but a positive Ti

anomaly and although the majority of individual samples from the LU, IBZ and BX are

dominated by negative Nb+Ta, P and Ti anomalies (all samples have negative P

anomalies), there are a few samples from each of these units that display flat to slightly

positive Nb+Ta and/or Ti anomalies (Fig. 6-9). While the majority of REE patterns

exhibit negative Nb and Ta anomalies, it is important to note that, as in the patterns from

Nipissing Gabbro suite rocks, the negative Nb anomalies are much larger than those of

Ta; this is a characteristic of boninitic magmas (Foley et al., 2002).


Contact-type, PGE-bearing sulphide mineralization, occurring at or near the

preserved igneous contact of the River Valley intrusion within the Marginal Series,

consists primarily of chalcopyrite-dominated disseminated sulphide and locally coarse-

grained blebby sulphide. Similar sulphide occurrences have been described in the East

Bull Lake intrusion by Peck et al. (1993a, 1995) and James et al. (2002a), and in the

Agnew Lake intrusion by Vogel et al. (1998a, 1999). A summary of the average

chalcophile metals plus Au, along with important metal ratios for core from drill hole

RV00-22 is provided in Table 6-7. The highest average concentration of Pt+Pd is from

the BX (2271 ppb Pt+Pd) which is consistent with the region of highest visible sulphide.

This unit also show the highest average Pd/Pt (2.7) and Cu/Ni (5.1) and the lowest

average S/Se value (1800). All of the unmineralized (≤0.05 wt% S) samples have high

average Pt+Pd, relative to common mafic magmas (e.g. Crocket, 1981, 2002; Hamlyn et

al., 1985; Keays, 1995) and the BX shows the highest average Pd/Pt (2.0) and Cu/Ni (3.5)

values and the lowest average S/Se value (1578). These ratios contrast sharply with

average values from the South Roby Zone (Lac des Iles intrusion), which has a much

higher Pd/Pt (8.7) value and a lower Cu/Ni (1.0) value (based on 51 samples; J. Hinchey,

unpublished data, 2004), and whose sulphide mineralization has a hydrothermal affinity

(Brügmann et al., 1989).

It is well established that the PGE have extremely high Nernst sulphide-silicate

partition coefficients and are sensitive indicators of sulphide ore-forming processes

(Peach et al., 1990; Peach et al., 1994). In addition, their abundance and distribution

provides a measure of the degree of S-saturation or S-undersaturation of the magma from

366

which the rock crystallized (Hamlyn and Keays, 1986; Keays, 1995; Vogel and Keays,

1997). During the fractionation of S-undersaturated mafic magmas, incompatible

elements such as Cu, S, Se, Pd and Pt become concentrated in the residual silicate melt,

whereas compatible elements such as Ni, Ir, Ru and Os are removed with the early

precipitation of silicate and/or oxide phases (Keays, 1995). Once S-saturation of the

magma is achieved, immiscible magmatic sulphides form and the magma becomes

rapidly depleted in PGE relative to other siderophile and chalcophile elements (i.e. Cu, S

and Se) because of the PGE’s very high affinity for sulphide melt. The ratioing of the

PGE against themselves (i.e. IPGE - Os, Ir, Ru versus PPGE – Rh, Pt, Pd) and against

elements such as Cu, S and Se are therefore widely accepted as useful discriminators in

considering the origin of PGE in mafic rocks (e.g. Peck et al., 1993a, 1993b; Keays,

1995; Seitz and Keays, 1997; James et al., 2002a, 2002b) and in the exploration for PGE

deposits (e.g. Hoatson and Keays, 1989; Reeves and Keays, 1995; Maier et al., 1998).

For example, Hoatson and Keays (1989) used ratios and abundances of PGE from surface

transects across the Munni Munni layered intrusion (Australia) to establish the

stratigraphic level at which reef-type PGE mineralization is concentrated. Subsequent

diamond drilling (ca. 1990) led to the definition of a 1-5 m thick layer of disseminated

PGE-rich sulphides (Barnes et al., 1990, 1992) at the approximate level indicated by

Hoatson and Keays (1989) and demonstrated the practical use of PGE and other

chalcophile elements as a robust technique in mineral exploration.

Selected bivariate plots of the chalcophile element concentrations from the variably

mineralized Group-1 data are provided in Figure 6-10 and Group-2 data in Figure 6-11.

In general, correlations between the chalcophile elements are strongest in the samples

from the mineralized BX, indicating that the PGE in the BX are strongly sulphide

controlled. Correlations between Pt and Pd, Cu and S, and Cu and Se from all units of

the River Valley intrusion are very strong. However, correlations between Cu and Ni, Cu

and Pd, Cu and Pt, Ni and Pd, S and Pt, and S and Pd are all very good in only the BX

and are relatively poor with respect to samples from the LU and IBZ. Nonetheless, the

generally positive correlations between the chalcophile metals in the BX and to a lesser

extent in the LU and IBZ, suggests that PGE distribution in the River Valley intrusion is

strongly controlled by sulphide.

367

Unit N *Au *Pt *Pd *3E *Pt+Pd *Ni *CuAll Samples ppb ppb ppb ppb ppb ppm ppm

Layered 27 8 33 20 61 53 131 457Inclusion-bearing 20 11 90 122 223 212 47 63

Breccia 55 110 573 1697 2380 2271 256 1317Boundary 4 16 55 126 197 181 145 217

Footwall Breccia 3 15 14 16 44 30 138 82Footwall 3 0 3 3 6 6 175 72

N *Au *Pt *Pd *3E *Pt+Pd *Ni *Cuunmineralized** ppb ppb ppb ppb ppb ppm ppm

Layered 12 8 33 21 63 54 116 90Inclusion-bearing 19 11 93 127 232 221 46 61

Breccia 9 26 121 278 425 399 81 191

Unit Se S S/Se Pd/Pt Cu/Ni Cu/PdAll Samples ppb wt%

Layered 218 0.14 6385 0.6 3.5 22328Inclusion-bearing 87 0.02 2648 1.4 1.3 514

Breccia 1942 0.34 1772 3.0 5.1 776Boundary 408 0.28 6928 2.3 1.5 1725

Footwall Breccia 262 0.37 14140 1.2 0.6 5127Footwall 226 0.36 16077 1.2 0.4 23664

Se S S/Se Pd/Pt Cu/Ni Cu/Pdunmineralized** ppb wt%

Layered 140 0.04 3164 0.6 0.8 4260Inclusion-bearing 81 0.02 2601 1.4 1.3 482

Breccia 195 0.03 1569 2.3 2.4 685

Table 6-7. Summary of average chalcophile metals plus Au, along with important metal

ratios for core from drill hole RV00-22, Dana North Deposit, River Valley intrusion.

*assays from XRAL Laboratories (PFN); **unmineralized = <0.05 wt% S; Values for 3E

= Pt+Pd+Au; All other assays from Geoscience Laboratories in Sudbury.

368

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Cu (ppm)

Pt (p

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Layered UnitInclusion-Bearing UnitBreccia UnitBoundary Zone UnitFootwall Breccia UnitFootwall

Figure 6-10. Bivariate scatter plots of chalcophile metal abundances in mineralized and unmineralized samples from drill hole RV00-22, Dana North Deposit, River Valley intrusion.

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Ir (p

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LUIBZBXBZFBXFW

Group-2 Data

(C)

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Pd/Ir

LUIBZBXBZFBXFW

Group-2 Data

(C)

Figure 6-11. Bivariate scatter plots of Group-2 data from drill hole RV00-22. (A) Pd versus Ir and (B) Pd versus Pd/Ir show the moderate to excellent correlation between Pd and Ir, supporting the interpretation that these sulphides are magmatic; some higher Pd/Ir values are probably due to localized hydrothermal redistribution of the sulphide.

370

The poor correlation between the chalcophile elements in the LU and IBZ may be

explained in terms of their wide variation in Pd concentration (Peck et al., 2001). The

moderate to excellent correlation between Pd and Ir in Figure 6-11 clearly supports a

magmatic sulphide controlled origin for the mineralization.

The increase in the Pd/Ir ratio, which increases as Pd increase, is due to the higher

Nernst partition coefficient of Pd (DPd ~35,000; Peach et al., 1990) relative to Ir (DIr

~17,000; Peach et al., 1990) and will increase as a magma becomes more evolved. This

explains the strong enrichment of Pd relative to Ir in some of the BX and IBZ samples

and it is probable that some of these higher values are due to localized remobilization of

the sulphide, related to deuteric and/or hydrothermal (overprint) upgrade of the sulphide.

Figure 6-12 is a plot of Se and Pd data for unmineralized rocks from Group-1 that

have <0.05 wt% S. This plot is useful for discriminating between rocks that formed from

S-undersaturated second-stage versus S-saturated first-stage magmas (Vogel and Keays,

1997; Peck et al., 2001). Second-stage magmas have high PGE (Pd) and low Se and S

tenors whereas first-stage magmas are typified by higher Se and S tenors and lower

relative PGE (Pd) concentrations (Hamlyn et al., 1985; Hamlyn and Keays, 1986).

Sulphur and Se are readily interchangeable in such plots (Peck et al., 1993a) but Se is

much less soluble and less mobile than S under low temperature conditions

(Goldschmidt, 1954). As in the samples from the Nipissing gabbro suite, all of the River

Valley samples plot within the field of fertile second-stage magmas, contrasting with the

field of depleted first-stage magmas in which average mid-ocean ridge basalts (MORB)

plot. This implies that the parental magmas of the River Valley intrusion were S-

undersaturated, PGE-fertile and had not previously segregated sulphides.

Figure 6-13 are plots of S/Se values versus Pt+Pd concentrations for all mineralized

and unmineralized samples from Group-1; in Figure 6-13b, the concentrations of Pt+Pd

have been recalculated to metals in 100% sulphide. All but one of the samples (LU

sample 26875) from the main units of the River Valley intrusion (LU, IBZ and BX) plot

within the range of uncontaminated magmatic sulphides (Naldrett, 1981) and

approximate the estimated S/Se ratio for mantle of ~3300 (McDonough and Sun, 1995).

Recalculating the Pt+Pd concentrations to 100% sulphide (Fig. 6-13b) has the affect of

elevating the IBZ values closer to and overlapping most of the values from the BX,

371

suggesting that the IBZ sulphide contains as much PGE in the sulphide fraction as most

of the samples from the BX.

In Figure 6-14, S/Se ratios from the Group-1 data set is plotted against drill hole

(RV00-22) depth. In the lower IBZ the S/Se values rapidly increase then show a gradual

decline upward through the IBZ.

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10 100 1000 10000 100000

Se (ppb)

Pd (p

pb)

LUIBZBXAVG MORB


Second-Stage Magmas (Fertile)(<0.05wt% S)

MORB

Figure 6-12. Discriminant plot of Se (ppb) versus Pd (ppb) concentrations for

unmineralized (<0.05 wt% S) rocks from drill hole RV00-22, Dana North Deposit, River

Valley intrusion. Field Boundary and average MORB data are from Hamlyn et al.

(1985).

372

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Pt+

Pd (p

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LUIBZBXBZFBXFW

sulphur loss magmaticcontamination(mss fractionation)

+R-factor

Konttijarvi Marginal Series(disseminated sulphide)

J-M Reef(Stillwater)

Merensky Reef(Bushveld)

(A)

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sulphur loss magmaticcontamination(mss fractionation)

+R-factor

(B)

Figure 6-13. Discriminant plots of whole-rock S/Se ratios against (A) whole-rock Pt+Pd (ppb) concentrations and (B) Pt+Pd concentrations recalculated to metals in 100% sulphide; the majority of samples plot within the field of magmatic sulphide (~1,000 to 5,000 S/Se; Naldrett, 1981). River Valley intrusion data are the mineralized (>0.05 wt% S) and unmineralized (<0.05 wt% S) samples from drill hole RV00-22. Data for Merensky Reef and average J-M Reef are from Naldrett (1981); data for average Konttijarvi Marginal Series rocks is from Iljina (1994).

373

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2751000 10000 100000

S/Se

Dril

l Hol

e D

epth

(m)

LU

IBZ

BX

FW

FBX

BZ

Figure 6-14a. Variation in whole-rock S/Se ratios for core samples from drill hole RV00-22, Dana North Deposit, River Valley intrusion.

374

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2751 10 100 1000 10000

Pd (ppb)

Dril

l Hol

e D

epth

(m)

LU

IBZ

BX

FW

FBXBZ

Figure 6-14b. Variation in whole-rock Pd concentrations (ppb) for core samples from drill hole RV00-22, Dana North Deposit, River Valley intrusion.

375

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225

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27510 100 1000 10000

Cu (ppm)

Dril

l Hol

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epth

(m)

LU

IBZ

BX

FW

FBXBZ

Figure 6-15a. Variation in whole-rock Cu contents (ppm) for core samples from drill hole RV00-22, Dana North Deposit, River Valley intrusion.

376

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175

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2750.1 1 10

Pd/Pt

Dril

l Hol

e D

epth

(m)

LU

IBZ

BX

FW

FBXBZ

Figure 6-15b. Variation in whole-rock Pd/Pt ratios for core samples from drill hole RV00-22, Dana North Deposit, River Valley intrusion.

377

Through the LU, the S/Se values show the most consistent values and the highest average

S/Se value (3251) relative to the IBZ and BX. The FW and FBX have the highest S/Se

values which decrease rapidly through the lower BX and decrease further still upward

through the BX. The relatively higher S/Se values toward the base of the BX likely

reflect minor, local crustal contamination. The S/Se data presented in Figures 6-13 and

6-14 are consistent with the interpretation that most of the S in these rocks is magmatic.

The FW samples, along with the BZ and FBX samples, which contain numerous

inclusions of FW rocks, plot within the field of contamination (Fig. 6-13) suggesting

introduction of external sulphur from the immediate footwall rocks. However, the

marked difference between the S/Se ratios of the FW and FBX and the overlying units

(Fig. 6-14a), particularly the BX, suggest that the immediate FW is not likely the source

of the S in the mineralized (BX) zone.

An important trend in Figure 6-13 is the decrease in S/Se ratios with increasing Pd

concentrations; the sulphides with the highest Pd compositions also have the highest Se

values. As Pd and Se are both highly chalcophile elements, this trend can be explained in

terms of the Nernst partition coefficients for Pd and Se (DPd ~35,000 and DSe ~1770;

Peach et al., 1990). These sulphides, assumed to have formed under conditions of high R

factor (R = silicate:sulphide mass ratio; Naldrett et al., 1979), are rich in Pd and Se

because the segregated sulphide liquid came in contact with a large amount of silicate

magma. It is also suggested that these high R factors were not achieved entirely within

the River Valley intrusion, but rather in a deep-seated staging chamber (cf. James et al.,

2002a) where the initial parental magmas were crustally contaminated, as evidenced by

increased (Th/Yb)N values. This interpretation is given a lot of support because there is

no chalcophile metal depletion in the IBZ and LU which overly the BX, as would be

expected if the Pd-rich sulphides had formed in the River Valley intrusion. In

comparison, Keays and Lightfoot (2004) described depletion signatures in Ni, Cu and

PGE from rocks overlying both barren and mineralized sections of the lower contact of

the Sudbury Igneous Complex, reasoning that the sulphides had crystallized within the

complex itself, settling out of the magma and accumulating toward the base of the

complex.

378

Further plots of metal abundances versus drill hole (RV00-22) depth for Group-1

data are provided in Figure 6-15. Concentrations of Pt, Pd, Au, Cu and Ni are all highest

within the BX and with the exception of Cu and Ni, show a gradual decline upward

through the IBZ and LU. The concentrations of Cu and Ni show an upward, stepwise

increase through the IBZ and LU with relatively high Ni concentrations in the LU, most

likely a consequence of higher olivine in these rocks. This variation in Cu/Ni, and in

particular the pronounced increase in Ni in the LU, is best appreciated in the plot of

Cu/Ni which clearly shows a gradual decrease upward through the IBZ and LU relating

to an increase in the modal abundance of olivine and accordingly an increase in silicate-

bound Ni.

Studies by a number of authors (Hamlyn et al., 1985; Hamlyn and Keays, 1986;

Barnes et al., 1988; Hoatson and Keays, 1989; Barnes et al., 1992) have demonstrated

that Cu/Pd ratios could be used not only in ore genesis, to determine whether or not a

magma has experienced sulphide segregation, but also in exploration. Palladium is a

highly incompatible element in S-undersaturated magmas, accumulating in the residual

silicate fraction where it remains dissolved until such time as the magmas become S-

saturated (Keays, 1995). Primitive mantle has a Cu/Pd ratio of ~7700, whereas normal

MORB, which represents a S-saturated magma derived from incomplete (<25%) partial

melting of the upper mantle, has a Cu/Pd ratio of ~16,000 (Hamlyn et al. 1985; Keays,

1995). These authors have suggested that in a S-undersaturated magma, Cu/Pd ratios

would be much lower in the segregating sulphide melt relative to the silicate magma

because of the very high partition coefficient between sulphide and Pd relative to

sulphide and Cu. Barnes et al. (1992), in the their study of the Munni Munni Complex,

demonstrated that the Cu/Pd ratio of S-undersaturated magma is on the order of ~10,000.

Recent work on the Skaergaard Intrusion (Momme, Keays, and Tegner, unpublished data,

2004), which was formed by S-undersaturated magma derived from the Icelandic Plume

(Momme et al., 2003), has shown that the average Cu/Pd ratio of the Skaergaard rocks,

prior to S-saturation is about 13,000. A consequence of this is that rocks with Cu/Pd

ratios below ~10,000 should contain Pd-rich sulphides, whereas rocks with Cu/Pd ratios

>10,000, being S-saturated, may have lost Pd through earlier sulphide segregation. For

379

rocks from the River Valley intrusion, a value of 12,000 Cu/Pd was chosen to mark the

change from S-undersaturation to S-saturation (Fig. 6-16).

0

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150

175

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2751 10 100 1000 10000 100000 1000000

Cu/Pd

Dril

l Hol

e D

epth

(m)

LU

IBZ

BX

FW

FBXBZ

12,000 Cu/Pd

S-saturatedS-undersaturated

Figure 6-16. Variations in the whole-rock Cu/Pd ratio in core samples, plotted against diamond drill hole depth from drill hole RV00-22, River Valley intrusion. The marker line at 12,000 Cu/Pd signifies the approximate point of S-saturation and is based on the work of Hamlyn et al. (1985) and recent data from Momme, Keays, and Tegner (unpublished data, 2004).

380

All samples except 29633 from the LU (Group-1 data) have Cu/Pd values that are

<12,000 and plot as S-undersaturated; sample 29633 (~75 m level) is described as

containing numerous white quartz veins with up to 5% disseminated and veinlet

(secondary) chalcopyrite and should be ignored in terms of Cu/Pd values and S-

saturation.

As a consequence of the very extreme chalcophile nature of Pd relative to Cu,

samples with low Cu/Pd ratios contain PGE-rich sulphides are considered to have formed

under conditions of high R factors. The fact that rocks in the LU, which overly the PGE-

mineralized BX, do not contain significantly high Cu/Pd values suggests that these rocks

were formed from S-undersaturated magmas. The significance of this is that the

sulphides could therefore not have formed in the River Valley chamber but must have

formed at depth, in a staging chamber where the original magmas became crustally

contaminated and possibly driven to S-saturation as a result of this crustal contamination.

Selected bivariate plots for mineralized and unmineralized samples from Group-2 are

shown in Figure 6-17. Values of Pd/Ir increase whereas values of Ni/Cu decrease as

magmas become more evolved (Barnes, 1990) and this relationship allows for

discrimination between primitive (mantle-like) and evolved (continental flood basalt)

magmas. In Figure 6-17a, all of the samples from Group-2 data plot within the field of

layered intrusions (which includes high MgO basalts and flood basalts), as defined by

Barnes (1990). In Figure 6-17b, all of the samples plot along the trend of magmatic

sulphide with samples from the BX and IBZ falling toward the end-member of S-

undersaturated magmas. Figure 6-17c, plots wt% MgO against Pd/Ir ratios with all

samples falling well below the field of remobilized/hydrothermal mineralization as

estimated after Barnes (1990). This plot also attests to the relatively high MgO

concentrations in samples from the LU and BX relative to the IBZ.

Recognizable in all three plots of Figure 6-17, is the magmatic nature of the

sulphides. In these plots, the samples fall well away from the fields of

remobilized/hydrothermal mineralization as represented in Figures 6-17a and 6-17b by

hydrothermal mineralization from the Rathbun Lake (Rowell and Edgar, 1986) and South

Roby Zone, Lac des Iles Complex (J. Hinchey, unpublished data, 2004).

381

0.01

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Ni/Cu

Pd/Ir

LU

IBZ

BX

BZ

FBX

FW

Rathbun Lake Avg

Lac des Iles - SRZ Avg

(A)

re-mobilized/hydrothermal mineralization

mantle

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LUIBZBXBZFBXFWEast Bull LakeStreich DikeRathbun Lake AvgLac des Iles - SRZ Avg

Initially S-undersaturated magmas which underwent S-saturation late in the evolution

of the magma system

S-saturated magmas which lost PGE prior to emplacement

re-mobilized/hydrothermal mineralization

mss fractionation

(B)

Figure 6-17. Bivariate scatter plots of chalcophile metal ratios for mineralized and unmineralized samples (Group-2 data) from diamond drill hole RV00-22, Dana North Deposit, River Valley intrusion. The data in (A) Ni/Cu versus Pd/Ir and (B) Cu/Ir versus Ni/Pd support the interpretation that the majority of the sulphides are magmatic in origin.

382

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4 6 8 10 12

MgO (wt%)

Pd/Ir

14

LU

IBZ

BX

BZ

FBX

FW

(C)

remobilized/hydrothermal mineralization

Figure 6-17 (cont). Bivariate scatter plots of chalcophile metal ratios for mineralized and

unmineralized samples (Group-2 data) from diamond drill hole RV00-22, Dana North

Deposit, River Valley intrusion. (C) All samples lie well below the field of

remobilized/hydrothermal mineralization as estimated from Barnes (1990). Data for East

Bull Lake is from Peck et al. (1995); Streich Dike (Agnew Lake intrusion) is from Vogel

et al. (1999); average Lac des Iles – South Roby Zone (SRZ) is from J. Hinchey

(unpublished data, 2004); average Rathbun Lake is from Rowell and Edgar (1986).

Approximated trends and fields for remobilized/hydrothermal mineralization, layered

intrusions and mantle in (A) and (B) are after Barnes (1990).

383

Although in thin sections and hand specimens there is evidence for significant small-scale

redistribution of the sulphides - nearly all of the samples from the BX and many of the

samples from the IBZ are extensively recrystallized relative to the rocks of the LU - the

PGE are clearly controlled by sulphides (Figs. 6-10 and 6-11) and although originally

magmatic (Fig. 6-13) have been subjected to deuteric and/or hydrothermal redistribution.

Primitive mantle-normalized PGE (recalculated to metal abundance in 100%

sulphide) and chalcophile element diagrams for samples from Group-2 are shown in

Figure 6-18. All of the River Valley intrusion rocks are characterized by a positive slope

with the Pt-Pd-Au-Cu portion of the trends elevated relative to the Ni-Ir-Ru-Rh portion;

the Pt-Pd-Au-Cu portion of the trends range from about 10 times primitive mantle for Pt

and 100,000 times primitive mantle for Pd. The highest average trend is from the BX and

IBZ, which are also consistently higher in Rh, Pt, Pd and Au relative to the LU and BZ.

The FBX and FW patterns show the least enrichment in PGE-Au-Cu-Ni and have

elevated Ni/Ir and Cu/Pd values relative to the other samples. In the LU, IBZ, BX and

BZ, average Ni is depleted relative to average Ir (average Ni/Ir ranges from 0.03 to 0.66)

and in the IBZ, BX and BZ average Cu is depleted relative to Pd (average Cu/Pd ranges

from 0.15 to 0.35). Highest individual values of Ni/Ir (1.23) and Cu/Pd (1.75) are from

the LU, which are about 6-8 times those in the IBZ and BX. The IBZ and LU display

profiles that are broadly similar to the East Bull Lake intrusion and selected deposits such

as the J-M Reef (Stillwater) and the Marginal Series of the Konttijarvi intrusion (Portimo

Complex, Finland), characterized by large positive Pd anomalies, high Pd/Ir ratios and

high Cu/Ni ratios relative to mantle. Profiles from the IBZ and BX are most similar to

the sulphide patterns of the East Bull Lake intrusion, which is part of the same suite of

intrusions as the River Valley intrusion, and the Portimo Complex, which is part of a

geologically similar suite of intrusions in Finland (Iljina, 1994). Overall similarities in

the sulphide patterns and low Ni/Ir and Cu/Pd values in the River Valley intrusion, East

Bull Lake and Portimo Complex sulphides are distinct from the patterns displayed by the

Lac des Iles Complex and flood basalt sulphides which have lower average Ir, Ru and Rh

concentrations and higher Ni/Ir values (Fig. 6-18b). Although the Lac des Iles Complex

sulphides display similar degrees of Pd enrichment they are relatively depleted in Ir when

compared to samples from the River Valley intrusion.

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100

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ulph

ide/

Prim

itive

Man

tle

29689 BX 29696 BX29702 BX 29707 BX29717 BX 29721 BX29733 BX 29744 BX29753 BX LU AVGIBZ AVG BZ AVGFBX AVG FW AVG

(E)

Figure 6-18. Primitive mantle-normalized chalcophile metal abundances (recalculated to metals in 100% sulphide) in core samples from diamond drill hole RV00-22, River Valley intrusion. (A) Average metal abundance for core samples from River Valley units compared with disseminated sulphide mineralization and PGE abundances from other mafic intrusions. (B) Individual values for the BX rocks. Data for “Average EBLI” is from Peck et al. (1995); “Streich Dike” is from Vogel et al. (1999); “J-M Reef” and average “Flood Basalt” are from Naldrett (1981); Portimo is from the Marginal Series in the Konttijarvi intrusive (Iljina, 1994); and, average Lac des Iles – South Roby Zone (SRZ) is from J. Hinchey (unpublished data, 2004). Mantle normalizing values are from Barnes et al. (1988) and McDonough and Sun (1995).

385

Brügmann et al. (1989) interpreted the decoupling of Pd and Ir to be the result of deuteric

fluids which are thought to have dominated the development of sulphide mineralization at

Lac des Iles. Moreover, the average Pd/Ir ratio from the South Roby Zone (>5,000),

which is much higher than average Pd/Ir from the IBZ (143) and BX (149), is more

typical of Pd/Ir ratios reported from hydrothermal sulphide deposits (Keays et al., 1982).

6.7 Petrology and Geochemistry of the Breccia Unit

Sixteen samples, collected from the Breccia Unit at the Central Zone (“CZ” samples)

and South Zone (“SZ” samples), comprise sets of fragments and matrix (Fig. 6-2).

Descriptions of these fragment (“F” samples) and matrix (“M” samples) samples are

provided in Table 6-8 and a summary of the geochemical data is provided in Table 6-9.

A complete listing of the geochemical data for the fragment and matrix samples is

provided in Appendix 1 and petrographic descriptions are provided in Appendix 2. Sets

of the matrix and fragment samples were collected as close to one another as possible as

shown in Photos 6-10 and 6-11.

At the Central Zone, the exposed Breccia Unit comprises mainly fine-grained mafic

fragments hosted by medium- to coarse-grained gabbro and leucogabbro (Photo 6-10).

At the South Zone, the exposed Breccia Unit is dominated by mafic fragments that are

mainly fine-grained melagabbro and gabbro in a matrix of medium-grained gabbro

(Photo 6-11); fine-grained diabase dikes cut many of the fine-grained fragments (Photo 6-

12a). Especially evident at the South Zone, the ratio of mafic to felsic minerals in the

matrix may be widely variable over just a few metres (melagabbro to leucogabbro) with

no discernable break between the different rock types. One relatively large fragment of

layered gabbroic rocks, probably derived through stoping from the overlying Layered

Units, was noted at the South Zone (Photo 6-12b).

All eight matrix samples show well preserved, granular-hypidiomorphic igneous

textures with amphibole pseudomorphing pyroxene (Photo 6-13). In contrast, all eight

fragment samples are extensively recrystallized (Photo 6-14) with only rare preservation

of igneous textures. The matrix and fragment samples, although collected from surface

exposures, are considered to be representative of the fragments and matrix that were

intersected in drill core.

386

Photo 6-10. Central Zone (Dana North Deposit) fragment and matrix sampling from the Breccia Unit. (A) Diamond saw cuts in areas of fragment sample CZF01 and matrix sample CZM01. The cuts are about 22 cm long. (B) Locations of fragment sample CZF02 and matrix sample CZM02 as indicated by the red markers. Note the felsic nature of the matrix in both sample areas as compared to the mafic matrix in Photo 6-11. An eight centimetre ruler is provided for scale.

387

Photo 6-11. South Zone (Dana South Deposit) fragment and matrix sampling from the Breccia Unit. (A) Locations of fragment sample SZF01 and matrix sample SZM01 as labelled. A rock cut from an old sample site is indicated. (B) Locations of fragment sample SZF05 and matrix sample SZM05 as indicated by the red markers. Note the fine-grained nature of the fragments relative to the matrix in both photos. An eight centimetre ruler is provided for scale.

388

Photo 6-12. Fragments in the South Zone (Dana South Deposit). (A) Medium-grained gabbroic matrix hosting a fine-grained fragment that has been cut by a fine-grained diabase dike (arrow is area of cut). (B) Fragment of layered gabbroic rocks in massive medium-grained gabbro; the fragment was most probably derived from the “above” Layered Units. An eight centimetre ruler is provided for scale.

389

Photo 6-13. Photomicrographs typical of the matrix in the Breccia Unit, South Zone, Dana South Deposit. (A) Relict igneous textures with pyroxene (p-pyx) pseudomorphed by amphibole (p-pyx), interstitial plagioclase (plag), and fine-grained amphibole (amp). Plane light. (B) Same view as (A) but in crossed polars. Field of view is 8 mm wide for both photographs.

390

Photo 6-14. Photomicrographs typical of fragments in the Breccia Unit, South Zone, Dana South Deposit. (A) Extensively recrystallized with the mafic nature of the fragments reflected by the high percentage of fine-grained amphibole (amp) and lesser plagioclase (plag). Plane light. (B) Same view as (A) but in crossed polars. Field of view is 8 mm wide for both photographs.

391

Sample Location Type DescriptionSZM-01 SZ matrix massive; ~10 cm from SZF-01SZF-01 SZ fragment massive; subangular; ~20 cm long axisSZM-02 SZ matrix massive; ~50 cm from SZF-02SZF-02 SZ fragment massive; subangular; ~40 cm long axis; minor rusty spotsSZM-03 SZ matrix massive; ~24 cm from SZF-03; bleb and diss cpy-poSZF-03 SZ fragment massive; subangular; ~27 cm long axis; diss cpy-po/blebsSZM-04 SZ matrix massive; ~50 cm from SZF-04; diss cpy-poSZF-04 SZ fragment massive; subrounded; diss cpy-po/blebs; biotiteSZM-05 SZ matrix massive; ~20 cm from SZF-05; diss cpy-poSZF-05 SZ fragment massive; ~30 cm long axis; diss cpy-poCZM-01 CZ matrix massive; ~35 cm from CZF-01; diss/interstitial cpy-poCZF-01 CZ fragment massive; subangular/subrounded; ~40 cm long axis; diss cpy-poCZM-02 CZ matrix massive; ~5 cm from CZF-02; finely diss cpy-po; ~1% blue qtz; biotiteCZF-02 CZ fragment massive; biotite-hematite-K alteration; finely diss cpy-poCZM-03 CZ matrix massive; ~10 cm from CZF-03; finely diss cpy-po/bleb; <1% blue qtz; biotiteCZF-03 CZ fragment massive; subangular/subrounded; ~50 cm long axis; finely diss cpy-po

Sample Location Type Texture Field Name %VSSZM-01 SZ matrix mg gabbro nvSZF-01 SZ fragment fg melagabbro nvSZM-02 SZ matrix mg gabbro nvSZF-02 SZ fragment fg melagabbro trSZM-03 SZ matrix mg gabbro 3SZF-03 SZ fragment fg-mg melagabbro 2SZM-04 SZ matrix mg-cg leucogabbro 2SZF-04 SZ fragment mg melagabbro 3SZM-05 SZ matrix mg gabbro 1SZF-05 SZ fragment fg-mg gabbro 2CZM-01 CZ matrix cg leucogabbro 1-2CZF-01 CZ fragment fg-mg gabbro 1CZM-02 CZ matrix cg leucogabbro <1CZF-02 CZ fragment fg gabbro 1CZM-03 CZ matrix mg-cg gabbro <1CZF-03 CZ fragment fg gabbro 2

Table 6-8. Summary of matrix and fragment samples, collected from the Dana North

(Central Zone=CZ) and Dana South (South Zone=SZ) deposits, River Valley, intrusion.

diss=disseminated.

392


Whole-rock major element, trace element, REE and PGE data for the 16 matrix and

fragment samples are summarized in Table 6-9. A summary of CIPW normative

calculations completed on the 16 matrix and fragment samples is provided in Table 6-10;

rock types were determined on the basis of the weight % normative minerals. Four of the

five fragments collected from the South Zone classify as melagabbronorite and the fifth

as an olivine melagabbronorite. In contrast the matrix samples from the South Zone

classify as gabbronorite, olivine gabbronorite and olivine leucogabbronorite, and are

clearly more felsic than the fragment samples. One sample (fragment SZF05) is CIPW

quartz-normative and therefore quartz oversaturated, suggestive of contamination by

secondary quartz alteration, country rock interaction, or both. Five of the six samples

from the Central Zone classify as gabbronorite and one as a leucogabbronorite. As in the

South Zone, the matrix samples from the Central Zone are much more felsic relative to

the fragment samples. Two samples (matrix CZM01 and fragment CZF01) are only just

CIPW quartz-normative (silica-saturated). This characteristic may be the result of

primary quartz in matrix sample CZM01 but in fragment sample CZF01 it is likely the

result of contamination by secondary quartz alteration, country rock interaction, or both.


Several bivariate scatter plots show the variation in major elements from the

suite of fragments and matrix samples (Fig. 6-19). The plot of MgO versus SiO2 shows

that the matrix samples have elevated SiO2 relative to all fragments, excepting SZF04

which is CIPW quartz-normative, and illustrates the high MgO content of the fragments.

In Figure 6-19b, which plots Ir against MgO, the BX fragments from the South and

Central zones are clearly elevated in MgO relative to the matrix samples; this is in

agreement with the rock types and weight percent normative values from CIPW

normative calculations (Table 6-10). Figure 6-19c, which plots MgO versus Al2O3,

attests to the high aluminium concentration in the matrix samples relative to the

fragments and reflects the felsic nature (feldspar rich) of the matrix magma and of the

Central Zone fragments relative to the South Zone fragments. The scatter plot of Fe2O3*

versus MgO (Fig. 6-19d) clearly demonstrates the higher MgO and Fe contents in the

fragment samples relative to the matrix samples, suggesting that the magma(s) from

393

which the fragments was derived was/were much more primitive than the subsequent

magma(s) which formed the matrix. In Figure 6-19e, the high MgO values in the

fragments contrast those of the matrix and within the matrix samples themselves there is

elevated TiO2 in the Central Zone samples relative to the South Zone, likely reflecting the

more felsic nature of the Central Zone matrix.

Figure 6-19f, a scatter plot of Al2O3/TiO2 versus V, was used by Peck et al. (1993b)

as a fractionation index, utilizing the incompatibility of V in early formed silicate phases

(i.e. plagioclase). Figure 6-19f clearly illustrates that the matrix samples represent much

more fractionated magmas than those of the fragments, particularly the matrix samples

from the South Zone; this is in agreement with the elevated MgO compositions in the

fragments relative to the matrix. Figure 6-19f was also used by Peck et al. (1993b) to

demonstrate the relative proportions of cumulus plagioclase (reflected by increasing

Al2O3) and postcumulus minerals (reflected by increasing TiO2), where rocks with high

Al2O3/TiO2 are plagioclase-rich adcumulates (low cumulate porosity) and rocks with low

Al2O3/TiO2 are pyroxene-rich orthocumulates (high cumulate porosity); this assumes that

plagioclase is the principal cumulus phase. Figure 6-19f shows that the matrix rocks of

the South Zone are dominated by plagioclase-rich adcumulates whereas the fragments

from the South and Central zones trend towards pyroxene-rich cumulates.


The relative amount of differentiation of a magma and/or its amount of interaction

with crustal material (contamination) is reflected by the incompatible trace elements Zr,

Y, Nb, Yb and La, whereby these elements become concentrated in magmas (rocks) that

are either more evolved and/or have interacted with crust. The plot of Zr versus Y (Fig.

6-20a) shows the primitive nature of the South Zone matrix relative to the matrix and

fragment samples from the Central Zone; three fragments (SZF01, SZF02 and SF04)

from the South Zone plot highest in Zr and Y, suggesting they are more evolved than the

other samples and/or they represent rocks that have interacted with crustal material.

Sample SF04 is the only sample that is CIPW quartz-normative, samples SZF01 and

SZF02 are CIPW olivine-normative, and all three samples have some of the highest wt%

TiO2 concentrations, suggesting contamination as the reason for elevated Y and Zr

concentrations.

394

Sample SZM01 SZF01 SZM04 SZF04 CZM01 CZF01 CZM03 CZF03Type M F M F M F M FSiO2 49.67 48.68 48.74 50.79 51.20 47.31 51.19 48.26TiO2 0.27 0.45 0.15 0.84 0.55 0.27 0.43 0.38Al2O3 16.65 5.96 23.47 5.74 19.06 11.58 15.89 11.02Fe2O3* 10.52 14.74 7.70 15.86 8.41 14.61 10.50 15.20MnO 0.18 0.26 0.10 0.25 0.15 0.24 0.19 0.24MgO 8.53 14.73 3.64 12.94 5.33 12.62 7.88 12.00CaO 10.23 12.04 10.15 9.64 11.10 7.55 9.32 7.44Na2O 2.68 0.57 3.15 0.41 2.61 0.35 2.26 0.71K2O 0.33 0.12 0.92 0.86 0.83 0.66 1.05 1.22P2O5 0.01 0.07 0.02 0.08 0.03 0.02 0.05 0.03

S 0.03 0.19 0.77 0.97 0.05 0.15 0.13 0.14Total 100.3 98.7 99.5 98.6 100.4 98.2 99.9 98.7Mg# 65.36 69.93 52.38 65.50 59.60 66.78 63.59 64.76

Pt 13.4 1.4 1637.0 683.0 61.3 8.2 20.7 4.6Pd 18.4 1.8 7164.0 1899.0 125.0 22.6 75.9 4.8Ni 189 399 632 427 107 428 164 308Cu 175 275 2586 2008 319 523 651 486La 2.42 2.68 2.83 10.17 6.61 3.17 6.40 4.53Ce 5.72 8.26 5.82 24.26 13.94 6.48 13.34 9.59Pr 0.79 1.29 0.75 3.11 1.70 0.83 1.71 1.26Nd 3.85 6.44 2.91 13.16 6.66 3.48 7.04 5.22Zr 9.90 46.10 15.30 69.60 38.80 16.20 45.20 21.00Sm 1.04 1.90 0.73 3.12 1.60 0.82 1.62 1.24Eu 0.57 0.41 0.51 0.52 0.72 0.34 0.90 0.61Ti 1223 1996 679 3813 2749 1243 2029 1757Gd 1.21 2.50 0.79 3.25 1.59 1.16 1.84 1.58Tb 0.21 0.39 0.11 0.50 0.30 0.18 0.31 0.27Dy 1.24 2.29 0.71 3.23 1.81 1.15 1.89 1.75Y 7.21 10.76 3.93 17.31 9.07 6.67 10.45 8.76

Ho 0.30 0.45 0.17 0.76 0.37 0.24 0.45 0.37Er 0.87 1.36 0.50 2.12 1.04 0.84 1.25 1.12Tm 0.14 0.21 0.08 0.32 0.16 0.12 0.21 0.17Yb 0.90 1.24 0.53 2.12 1.04 0.82 1.35 0.94Lu 0.16 0.18 0.07 0.32 0.15 0.14 0.22 0.17

∑REE 19.41 29.61 16.50 66.95 37.70 19.76 38.52 28.83(Th/Yb)N 0.52 4.91 4.49 8.40 7.31 3.40 4.98 3.89(Nb/Th)N 0.30 0.12 0.15 0.14 0.13 0.15 0.13 0.13

Zr/Sm 9.52 24.26 20.96 22.31 24.25 19.76 27.90 16.94Nb/Ta 2.22 4.40 2.78 8.75 6.36 6.67 5.91 3.18

Table 6-9. Summary of whole-rock geochemistry for matrix and fragment samples, River Valley, intrusion.

395

Sample SZM01 SZF01 SZM02 SZF02 SZM03 SZF03 SZM04 SZF04

Rock Type OGN MGN GN MGN GN OMGN OLGN MGNNorm Minerals

quartz 5.25plagioclase 56.06 18.82 56.93 21.77 55.86 23.10 75.19 15.17orthoclase 2.01 0.71 2.07 1.36 3.13 0.47 5.56 5.26diopside 14.66 37.99 13.34 36.69 12.54 27.40 2.55 29.95

hypersthene 13.50 34.72 19.41 30.56 19.76 31.46 3.33 37.02olivine 10.76 2.96 5.56 5.40 5.52 13.07 9.82

ilmenite 0.51 0.89 0.40 0.91 0.32 0.47 0.28 1.65magnetite 2.17 3.10 1.91 2.90 2.02 3.28 1.59 3.32

apatite 0.02 0.16 0.05 0.05 0.05 0.05 0.19zircon 0.01 0.01

chromite 0.04 0.09 0.06 0.09 0.06 0.09 0.01 0.04pyrite 0.06 0.42 0.19 0.04 0.78 0.51 1.65 2.12calcite 0.27 0.23 0.20 0.34 0.07 0.20 0.09 0.11

*Total: 100.06 100.10 100.07 100.11 100.11 100.10 100.12 100.09Sample SZM05 SZF05 CZM01 CZF01 CZM02 CZF02 CZM03 CZF03

Rock Type GN MGN LG GN GN GN GN MGNNorm Minerals

quartz 0.23 1.40plagioclase 55.28 26.28 60.76 32.96 51.49 25.78 50.25 30.67orthoclase 1.42 0.95 4.96 4.14 6.09 6.74 6.32 7.56diopside 14.60 26.91 13.98 7.75 14.80 19.52 13.15 11.38

hypersthene 23.44 40.20 16.97 49.56 21.62 35.18 26.49 45.48olivine 2.73 1.16 2.76 8.53 0.33 0.45


apatite 0.05 0.07 0.05 0.09 0.07 0.12 0.07zircon 0.01 0.01

chromite 0.04 0.09 0.03 0.09 0.04 0.09 0.06 0.09pyrite 0.17 0.85 0.11 0.34 0.06 0.06 0.28 0.32calcite 0.11 0.18 0.14 0.07 0.09 0.09

*Total: 100.08 100.14 100.09 100.13 100.07 100.09 100.11 100.10 Table 6-10. CIPW normative calculations for matrix and fragment samples from the

Central Zone (CZ) and South Zone (SZ), River Valley intrusion. *normalized to 100%;

"SZ" = South Zone, "CZ" = Central Zone, "M" = matrix, "F" = fragment; rock names

based on wt% normative minerals; OGN=olivine gabbronorite; MGN=melagabbronorite;

GN=gabbronorite; OMGN=olivine melagabbronorite; OLGN=olivine leucogabbronorite;

LG=leucogabbro.

396

45

46

47

48

49

50

51

52

0 2 4 6 8 10 12 14 16MgO (wt%)

SiO

2 (w

t%)

18

SZ MatrixCZ MatrixSZ FragCZ Frag

(A)

0

2

4

6

8

10

12

14

16

18

0.01 0.1 1 10 100

Ir (ppb)

MgO

(wt%

)


fragments

matrix

(B)

Figure 6-19a-b. Bivariate scatter plots showing the variation in whole-rock major element chemistry from the suite of fragments and matrix samples collected from the South Zone (SZ), Dana South Deposit, and Central Zone (CZ), Dana North Deposit, in the River Valley intrusion.

397

0

5

10

15

20

25

0 2 4 6 8 10 12 14 16 1

MgO (wt%)

Al 2O

3 (w

t%)

8


(C)

0

2

4

6

8

10

12

14

16

18

0 2 4 6 8 10 12 14 16

MgO (wt%)

Fe2O

3* (w

t%)

18


(D)

Figure 6-19c-d. Bivariate scatter plots showing the variation in whole-rock major element chemistry from the suite of fragments and matrix samples collected from the South Zone (SZ), Dana South Deposit, and Central Zone (CZ), Dana North Deposit, in the River Valley intrusion.

398

0

0.1

0.2

0.3

0.4

0.5

0.6

0.7

0.8

0.9

0 2 4 6 8 10 12 14 16 1

MgO (wt%)

TiO

2 (w

t%)

8


(E)

1

10

100

1000

0 50 100 150 200 250 300Al2O3/TiO2

V (p

pm)


increasingfractionation

pyroxene-rich cumulatesplagioclase-rich adcumulates pyroxene-plagioclase mesocumulates

(F)

Figure 6-19e-f. Bivariate scatter plots showing the variation in whole-rock major element chemistry from the suite of fragments and matrix samples collected from the South Zone (SZ), Dana South Deposit, and Central Zone (CZ), Dana North Deposit, in the River Valley intrusion.

399

0

2

4

6

8

10

12

14

16

18

20

0 10 20 30 40 50 60 70 8Zr (ppm)

Y (p

pm)

0


increasing crustalinteraction

&fractionation

(A)

0.0

0.5

1.0

1.5

2.0

2.5

3.0

0 10 20 30 40 50 60 70 8Zr (ppm)

(La/

Sm) N

0


increasing crustalinteraction

&fractionation

(B)

Figure 6-20. Bivariate scatter plots of trace element abundances and primitive mantle-normalized (N) ratio of La/Sm for fragment and matrix samples from the River Valley intrusion.

400

The ratio (La/Sm)N can provide good indications as to whether or not a magma has

interacted with crustal rocks, whereby increased La/Sm values suggest increasing crustal

assimilation. In Figure 6-20b, Zr is plotted against (La/Sm)N values for the matrix and

fragment samples. As in the plot of Y and Zr, the fragments from the South Zone show

the widest distribution with the majority of these samples having the lowest (La/Sm)N

values, reflecting their primitive (mafic) nature. The Central Zone samples show high

(La/Sm)N values and higher Zr concentrations in the matrix relative to the fragments.

This trend attests to the felsic nature of the Central Zone fragments and matrix relative to

the more mafic samples from the South Zone.

In Figure 6-21, Group-2 data from drill hole RV00-22 and data from the fragment

and matrix sample suite is plotted using primitive mantle-normalized (Th/Yb)N and

(Nb/Th)N. Distinct negative Nb and Ta anomalies, with respect to primitive mantle-

normalized data, are attributed to crustal contamination (e.g. Cox and Hawkesworth,

1985) and Th is preferentially enriched in continental crust (McDonough and Sun, 1995).

Plotting (Th/Yb)N against (Nb/Th)N is useful for modelling the effects of crustal

contamination on the composition of a proposed or known primary melt (e.g. Lesher et

al., 2001). Two of the four mixing curves, presented in Figure 6-21, were constructed by

systematic introduction of a crustal component (i.e. increasing Th) to the initial

compositions of N-MORB (Sun and McDonough, 1989), average boninite-like rock

(Piercey et al., 2001); data from the Povungnituk sedimentary rocks (Lesher et al., 2001)

represents continental crust. The third and fourth mixing curves were constructed by

assuming initial primitive boninite compositions that are expected to have 25% and 50%

less Nb relative to the boninite-like composition of Piercey et al. (2001). In Figure 6-21,

some of the rocks from the LU and IBZ plot along or above the N-MORB mixing curve

and suggesting compositions that are mixtures of N-MORB and continental crust (~10-

20% crustal contribution). All other rocks, including those from the BX and all fragment

and matrix samples and several of the LU and IBZ rocks, lie below the N-MORB mixing

curve and are displaced toward the mixing curves for boninite-like rocks and 25% and

50% depleted Nb; this suggests incorporation of some local footwall rocks. However,

more significantly, these depressed Nb values indicate that the BX (matrix and

401

fragments) were derived from a source magma that was very poor in Nb, such as a

boninite which would be much more depleted in Nb relative to N-MORB.

0.01

0.1

1

10

0.1 1 10 100

(Th/Yb)N

(Nb/

Th) N

LUIBZBXBZFBXFWSZ-MatrixSZ-FragmentCZ-MatrixCZ-FragmentStreich DikePovungnituk SedimentHuronian Sediment AvgBoninitic Avg

N-MORB

Continental Crust

Boninitic

-25% Nb

E-MORB

-50% Nb

10% crust


(Nb/Th)N using Group-2 data from drill hole RV00-22 and fragment and matrix samples

from the River Valley intrusion (SZ = South Zone; CZ = Central Zone). Continental crust

is represented by Povungnituk sedimentary rocks (Lesher et al., 12001). Data for N-

MORB and E-MORB are from Sun and McDonough (1989); data for Streich Dike is

from Vogel et al. (1998a); data for average (N=4) Huronian sedimentary rock is from

Easton (2003); data for average (N=4) Boninitic magma is from Piercey et al. (2001).

402

Chondrite-normalized REE patterns for the matrix and fragment samples are

provided in Figure 6-22, and a listing of the more important features of these plots is

summarized in Table 6-11. Average chondrite-normalized REE patterns for all sample

types are all elevated to about 10-20 times chondrite, exhibit LREE enrichment, and with

the exception of the average pattern for all fragments and the South Zone fragments, have

positive Eu anomalies. In general, Central Zone matrix and fragment samples have

patterns that are similar and near-parallel to one another, with LREE enrichment and a

narrow range in (La/Yb)N values (1.74 to 4.33).

Unit N Eu/Eu* La/Sm (La/Yb)N ∑REE ∑REE RangeRange Range Range Average ppm ppm

All Matrix 8 1.330-2.026 2.33-4.13 1.63-4.33 24 13-39All Fragment 8 0.492-1.335 0.90-3.87 0.58-3.28 26 9-67

SZ Matrix 5 1.533-2.026 2.33-3.88 1.63-3.64 15 13-19CZ Matrix 3 1.330-1.588 3.54-4.13 3.23-4.33 37 36-39

SZ Fragment 5 0.492-1.027 0.90-3.26 0.58-3.27 28 9-67CZ Fragment 3 0.977-1.335 2.86-3.87 1.74-3.28 23 20-29

Table 6-11. Principal features of trace and REE abundances and ratios for matrix and

fragment samples from the Central Zone (CZ) and South Zone (CZ), River Valley

intrusion. N=number of samples in the average or range. The value Eu/Eu*=

EuN/√[(SmN).(GdN)] was calculated using Geometric Mean method of Taylor and

McLennan (1985) where “N” indicates chondrite normalized.

403

1

10

100


Sam

ple/

Cho

ndrit

e

SZM01SZM02SZM03SZM04SZM05SZF01SZF02SZF03SZF04SZF05AVG-MAVG-F

(A)

1

10

100


Sam

ple/

Cho

ndrit

e

CZM01

CZM02

CZM03

CZF01

CZF02

CZF03

AVG-M

AVG-F

(B)

Figure 6-22. Chondrite-normalized rare-earth element plots for matrix and fragment samples from the Central (CZ) and South (SZ) zones at the Dana Lake area, River Valley intrusion. (A) Individual fragment and matrix samples from the South Zone. (B) Individual fragment and matrix samples from the Central Zone In each case, samples are compared to average compositions of matrix (AVG-M) and fragments (AVG-F). Normalizing values are from Lodders and Fegley (1998).

404

Fragment samples CZF01 and CZF02 are distinctly lower in total REE relative to the

other Central Zone samples and have very modest positive (CZF01: Eu/Eu*=1.05) to

slightly negative (CZF02: Eu/Eu*=0.98) Eu anomalies. The South Zone matrix and

fragment samples show the greatest range in chondrite-normalized REE patterns. Like

the Central Zone, the matrix samples from the South Zone have patterns that are similar

in total REE, are sub-parallel to one another and have large positive Eu anomalies. In

contrast, fragment samples from the South Zone are quite variable in their REE patterns.

Fragments SZF02 and SZF05 share similar sub-parallel and nearly flat REE patterns

(HREE elevated slightly relative to LREE), elevated about 6 to 9 times chondrite, and

with SZF02 exhibiting a slight negative Eu anomaly and SZF05 a slightly positive Eu

anomaly. These patterns are similar to those of MORB type magmas (Rollinson, 1993).

Fragment SZF04 exhibits a distinct REE pattern with the highest total REE (∑REE = 67

ppm), strong LREE enrichment, a pronounced negative Eu anomaly, and moderate HREE

enrichment. This distinct REE pattern and elevated REE concentrations, along with its

CIPW quartz-normative character, elevated (La/Sm)N value (2.11) and elevated Zr

content suggests interaction with crustal material and contamination. Vogel (1996)

presents similar data for a granite inclusion and a melagabbronorite pod from the Agnew

Lake intrusion which was interpreted to be the result of contamination of the

melagabbronorite pod by a granitic inclusion; the melagabbronorite pod also contained

substantial concentrations of blue quartz. Fragment SZF03 exhibits strong LREE

depletion, a moderate Eu anomaly (Eu/Eu* = 0.83) and the lowest total REE (∑REE = 9

ppm). On the basis of CIPW normative calculation, SZF03 classifies as an olivine

melagabbronorite and has the highest olivine-normative value (13.07 wt% olivine) of all

of the fragment-matrix samples. The potentially primitive nature of this rock with

elevated olivine and nominal plagioclase, would explain the low overall REE and the

distinct REE pattern. Fragment SZF01, elevated to about 10 times chondrite, exhibits a

distinct gull-wing pattern with elevated, concave down LREE, elevated HREE and a

distinct Eu anomaly (Eu/Eu* = 0.57); this REE pattern is similar to tholeiitic basalts (Sun

and Nesbitt, 1978).

The REE patterns for both the fragments and matrix present evidence for crustal

contamination with patterns from the South Zone fragments exhibiting the most dramatic

405

difference between individual samples (Fig. 6-22). The REE profiles exhibited by the

Central Zone and South Zone matrix are similar to the patterns from upper stratigraphy

rocks (i.e. Layered Units) of the River Valley intrusion, suggesting a common origin. In

addition, these samples have REE patterns that are similar to rocks from the Lower, Main

and Upper series of the East Bull Lake intrusion (James et al., 2002a) and from Lower

and Upper series rocks of the Agnew Lake intrusion Vogel (1996). In contrast, the

distinct REE patterns produced by the Central Zone fragments and in particular the South

Zone fragments, coupled with their high MgO concentrations relative to the matrix,

suggests that the fragments are exotic and were not cogenetic with the River Valley

intrusion magmas which formed the PGE-rich sulphide mineralization that occurs in the

matrix of the BX. If these REE patterns are primary then these fragments may represent

xenoliths that crystallized in a staging chamber and were subsequently entrained within

the magma(s) as it/they rose through the crust.

Primitive mantle-normalized multi-element plots for the fragment and matrix

samples are provided in Figure 6-23. The sample patterns are generally sub-parallel and

show the same relative arrangements between samples with the South Zone samples

exhibiting the greatest variation when compared to the Central Zone samples. All matrix

samples have strong positive Sr anomalies, indicative of high modal plagioclase and the

felsic nature of these rocks. Except for fragment CZF01, which is CIPW quartz-

normative, all fragment samples display strong negative Sr anomalies, indicative of low

modal plagioclase and the primitive nature of the fragments, particularly in the South

Zone fragments. All of the South Zone matrix samples display lower HREE (Sm to Yb)

concentrations relative to the South Zone fragments. In contrast, all of the Central Zone

matrix samples exhibit higher HREE (Sm to Yb) concentrations relative to Central Zone

fragments. All of the rocks exhibit negative Nb+Ta, P and Ti anomalies and low average

Nb/Ta values, ranging from 1.1 to 8.8. As discussed earlier, negative anomalies of the

high field strength elements Nb and Ta (strongly incompatible), the first series transition

metal Ti (moderately incompatible) and the alkaline earth element P (moderately

incompatible) are important indicators of a magmas interaction with a crustal reservoir

(Cox and Hawkesworth, 1985; Lightfoot and Naldrett, 1996).

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Figure 6-23. Primitive mantle-normalized multi-element diagrams for matrix and fragment samples from the Central Zone (CZ) and South Zone (SZ) areas of the River Valley intrusion. (A) Averages of matrix and fragment samples. (B) Average compositions of matrix and fragment samples compared with individual matrix samples. Normalizing values are from McDonough and Sun (1995).

407

In Figure 6-24, Group-2 data from drill hole RV00-22 and data from the fragment

and matrix sample suite is plotted using values of Zr/Sm and Nb/Ta (Foley et al., 2002).

Utilizing the diagram from Foley et al. (2002) it is apparent that all of the River Valley

samples plot with very low Nb/Ta and Zr/Sm values relative to MORB, primitive mantle,

continental crust, and modern adakites; Foley et al. (2002) considered adakites to be rare

modern analogues of Archaean crust-building magmatism, originating by melting of a

subducting basalt slab. Specifically, the distribution ranges from low Nb/Ta and low

Zr/Sm toward continental crust and adakites. These patterns are typical of tholeiites that

have been emplaced in a rifted environment, and are similar to those from established

rift-continental flood basalt regions (A.J. Crawford, pers. comm. 2004).

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Figure 6-24. Plot of Zr/Sm versus Nb/Ta ratios from whole-rock analyses of 44 unmineralized and mineralized River Valley intrusion samples (28 from Group-2 drill hole RV00-22, 16 from the fragment-matrix suite). The fields of MORB, continental crust and adakites (modern analogues of early continental crust) are approximated after Foley et al. (2002). Data for average (N=4) Boninitic magma is from Piercey et al. (2001).

408

Unit N Ir Au Pt Pd 3E Pt+Pd Ni CuAll Samples ppb ppb ppb ppb ppb ppb ppm ppmSZ Matrix 5 10.04 75 476 1973 2524 2449 340 1190CZ Matrix 3 0.64 19 30 71 120 101 137 396

SZ Fragment 5 7.94 72 349 1164 1585 1513 451 1076CZ Fragment 3 0.26 17 7 10 34 17 331 395

N Ir Au Pt Pd 3E Pt+Pd Ni Cuunmineralized** ppb ppb ppb ppb ppb ppb ppm ppm

SZ Matrix (SZM01) 1 0.33 8 13 18 40 32 189 175CZ Matrix 2 0.70 13 35 69 117 104 123 269

SZ Fragment (SZF02) 1 3.29 22 210 713 945 923 327 179CZ Fragment (CZF02) 1 0.25 9 7 3 19 10 256 175

Unit Se S S/Se Pd/Pt Cu/Ni Cu/Pd Pd/IrAll Samples ppb wt%SZ Matrix 2011 0.27 1323 4.1 3.5 603 196.5CZ Matrix 247 0.07 2834 2.3 2.9 5572 110.6

SZ Fragment 2295 0.36 1560 3.3 2.4 924 146.6CZ Fragment 766 0.11 1393 1.5 1.2 39089 39.3

Se S S/Se Pd/Pt Cu/Ni Cu/Pd Pd/Irunmineralized** ppb wt%

SZ Matrix (SZM01) 128 0.03 2344 1.4 0.9 9511 55.8CZ Matrix 138 0.04 2909 2.0 2.2 3913 98.2

SZ Fragment (SZF02) 231 0.02 866 3.4 0.5 251 216.7CZ Fragment (CZF02) 77 0.03 3896 0.4 0.7 59524 11.8

Table 6-12. Absolute and average chalcophile abundances and important ratios for matrix

and fragment samples from the Dana Lake area, River Valley intrusion. All assays from

Geoscience Laboratories in Sudbury; **unmineralized = ≤0.05 wt% S; Values for 3E =

Pt+Pd+Au.

409

The similar ratios from Nipissing Gabbro rocks, suggests that both the River Valley

magmas and those that formed the Nipissing Gabbro suite could have been feeders for

continental flood basalts. It should be pointed out, however, that the Zr/Sm and Nb/Ta

values may both be systematically low, and in the case of Zr, this is probably related to

insufficient digestion (open beaker digestion – see Section 2.2) of Zr during the ICP-MS

analytical process; ICP-MS Zr data may be one third to one half less than XRF Zr data

(A.J. Crawford, pers. comm. 2004), Assuming higher Zr compositions would therefore

shift these samples toward the fields of continental crust and adakites. Weyer et al.

(2002) reported a low Nb/Ta value of 4, but lower values, such as the ones in the current

study, are not known from literature.

Sample N Pd/Pt Cu/Ni Pd/Ir Cu/Pd Pd+Pt (ppb) Ni/Pd S/SeSZM01 1.4 0.9 55.8 9511 32 10272 2344SZM02 3.6 2.4 164.4 986 794 406 1164SZM03 3.5 5.2 154.2 1508 1621 291 1454SZM04 4.4 4.1 216.4 361 8801 88 1281SZM05 4.0 2.6 166.4 844 997 327 1196CZM01 2.0 3.0 104.2 2552 186 856 3067CZM02 1.4 1.6 62.5 17520 21 11120 2679CZM03 3.7 4.0 143.2 8577 97 2161 2790SZF01 1.2 0.7 22.4 153631 3 222905 1177SZF02 3.4 0.5 216.7 251 923 459 866SZF03 2.6 1.4 86.2 63929 16 44286 1825SZF04 2.8 4.7 130.1 1057 2582 225 1622SZF05 3.8 3.6 148.0 689 4043 189 1590CZF01 2.8 1.2 75.3 23142 31 18938 944CZF02 0.4 0.7 11.8 59524 10 87075 3896CZF03 1.0 1.6 21.6 102316 9 64842 2219

Average M (all): 8 4.1 3.4 193.3 708.4 1569 209.6 1426Average F (all): 8 3.3 2.0 144.6 1121.8 952 554.8 1532Average M SZ: 5 4.1 3.5 196.5 603.1 2449 172.6 1323Average M CZ: 3 2.3 2.9 110.6 5571.7 101 1921.3 2834Average F SZ: 5 3.3 2.4 146.6 924.2 1513 387.2 1560Average F CZ: 3 1.5 1.2 39.3 39088.8 17 32750.1 1393

Table 6-13. Chalcophile abundances and ratios for matrix and fragment samples, River

Valley intrusion. All assays from Geoscience Laboratories in Sudbury; SZ=South Zone;

CZ=Central Zone; M = matrix; F = fragment.

410


On average, the South Zone samples contain higher average total PGE, Cu, Ni and S

concentrations, higher Pd/Pt and Pd/Ir ratios and lower S/Se and Cu/Pd ratios, relative to

samples from the Central Zone (Tables 6-12 and 6-13). In terms of unmineralized

samples (≤0.05 wt% S), matrix and fragment samples from both zones contain anomalous

to very anomalous PGE concentrations with magmatic S/Se ratios; in particular, SZF02

contains 210 ppb Pt and 713 ppb Pd, with 0.02 wt% S. Positive correlation exists

between the strongly chalcophile metals, suggesting strong sulphide control on the

distribution of the chalcophile metals. For example, there are modest to strong

correlations between Pd and Pt, S and Cu, and S and Ni, and moderate to weak

correlations between Cu and Ni, Cu and Pd, and Cu and Pt.

With the exception of matrix sample SZM01, all of the South Zone matrix samples

have the highest Pd/Ir ratios (Tables 6-12 and 6-13). Values of Pd/Ir increase as magmas

become more evolved (Barnes, 1990) and Pd/Ir values are higher in secondary

(hydrothermal) sulphide mineralization relative to magmatic sulphides (Keays et al.,

1982). The elevated Pd/Ir ratios in the South Zone matrix samples and in the South Zone

fragment sample SZF02 may be indicative of slightly more evolved magma sources

and/or a higher percentage of secondary sulphide mineralization; the latter may be more

applicable to sample SZF02. Except for fragments SZF02, SZF04 and SZF05, the matrix

samples also have much higher PGE concentrations than the fragments, suggesting that

the PGE were introduced by way of the matrix magma(s) and that subsequent

impregnation of the fragments by remobilized sulphides, perhaps by means of deuteric or

hydrothermal fluids, resulted in elevated PGE compositions within select fragments.

S/Se values for mineralized (maximum 3% visible sulphide) and unmineralized

(<0.05 wt% S) matrix and fragment samples from the South and Central zones have

averages of approximately 1500, and range from 866 to 3896 (Fig. 6-25; Table 6-13).

These values are consistent with the interpretation that most of the S in these rocks is

magmatic as these values are typical of magmatic sulphides from other mafic intrusions

(Eckstrand et al., 1989), are well within the range of uncontaminated magmatic sulphides

(Naldrett, 1981; Eckstrand and Hulbert, 1987), and approximate the mantle value of 3333

(McDonough and Sun, 1995).

411

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Figure 6-25. Discriminant plots of whole-rock S/Se ratios against (A) whole-rock Pt+Pd (ppb) concentrations and (B) Pt+Pd concentrations recalculated to metals in 100% sulphide; the majority of samples plot within the field of magmatic sulphide (~1,000 to 5,000 S/Se; Naldrett, 1981). River Valley intrusion data are the mineralized (>0.05 wt% S) and unmineralized (<0.05 wt% S) matrix and fragment samples from the Central Zone (CZ) and South Zone (SZ). Data for Merensky Reef and average J-M Reef are from Naldrett (1981); data for average Konttijarvi Marginal Series rocks is from Iljina (1994).

412

Average S/Se values for matrix and fragment samples from the South Zone are about

1488 and 1416, respectively, and median values are about 1281 and 1590, respectively.

Average S/Se values for matrix and fragment samples from the Central Zone are 2845

and 2353, respectively and median values are about 2790 and 2219, respectively. The

slightly higher average and median S/Se values for Central Zone matrix samples, relative

to Central Zone fragments, is suggestive of minor contamination in the matrix magma.

Samples SZF02 and CZF01, which are extensively recrystallized and altered in thin

section, have S/Se values that are below 1000 which suggests sulphur loss (Reeves and

Keays, 1995), and small-scale redistribution of the chalcophile elements, likely the result

of weathering, secondary alteration and/or metamorphism. The introduction of

sedimentary sulphides is known to result in S/Se values >20,000 (Naldrett, 1981). The

paucity of S/Se values >20,000 in this data set suggests that the introduction of external

sulphur, potentially derived from bordering Archaean paragneiss and Huronian

Supergroup country rocks, was unlikely or minor, and that assimilation and interaction

with the country rocks did not play a major role in the development of the contact-type

sulphide mineralization. Peck et al. (1993a) noted similar S/Se trends from contact-type

mineralization in the East Bull Lake intrusion. It is important to note that in very

dynamic magmatic ore systems (i.e. high R factors) the effects of crustal contamination

are masked by the R factor process (Lesher and Burnham, 1999); a similar affect is noted

for Re-Os isotopes by Lambert et al. (1998).

Figure 6-26a is a plot of Se and Pd data for mineralized and unmineralized fragment

and matrix and RV00-22 drill core samples (Group-1). With the exception of South Zone

fragment SZF01, all of the samples plot within the field of second-stage magmas (S-

undersaturated field), contrasting with the first-stage or depleted magma field in which

average mid-ocean ridge basalts (MORB) plot. As discussed earlier, this implies that the

parental magmas of the River Valley intrusion were introduced into the chamber as PGE

metal-fertile magmas which had not previously segregated sulphides.

Mineralized and unmineralized fragment and matrix and drill hole RV00-22 (Group-

1) core samples are presented on a metal ratio plot of Cu/Pt versus Ni/Pd (Figure 6-26b).

413

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SZ Matrix (<0.05 wt% S)SZ Matrix (>0.05 wt% S)SZ Fragment (<0.05 wt% S)SZ Fragment (>0.05 wt% S)CZ Matrix (<0.05 wt% S)CZ Matrix (>0.05 wt% S)CZ Fragment (<0.05 wt% S)CZ Fragment (>0.05 wt% S)RV00-22 (<0.05 wt% S)RV00-22 (>0.05 wt%S)MORB

Second-Stage Magmas(Fertile)

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DEPLETED

(All Samples: RV00-22 and Matrix-Fragments)

ENRICHED

MANTLE

FloodBasalts

PGE-dominated deposits

increasing PGEin sulphide

Figure 6-26. Plots showing variations in concentrations for mineralized (>0.05 wt% S) and unmineralized (<0.05 wt% S) matrix and fragment samples and Group-1 core samples from drill hole RV00-22. (A) Discriminant plot of Se (ppb) versus Pd (ppb). Fragment and matrix samples are from the Central Zone (CZ) and South Zone (SZ). Field Boundary and average MORB data are from Hamlyn et al. (1985). (B) Plot of Cu/Pt versus Ni/Pd ratios. Fields of mantle rocks, flood basalts, and PGE-dominated deposits (i.e. Reef-type mineralization in the Bushveld, Stillwater and Penikat intrusions) are approximated after Barnes et al. (1993).

414

Several authors (e.g. Barnes et al., 1988; Theriault et al., 2000) have utilized these ratios

to evaluate the effects of partial melting, crystal fractionation, and sulphide segregation

on the PGE composition of sulphides. The plot has been subdivided into three main

fields which allow for the comparison of each sample’s composition and whether or not it

is PGE-enriched or PGE-depleted relative to mantle. The samples span the fields of

PGE-depleted, mantle and PGE-enriched sulphides with the majority plotting within the

enriched field. Except for fragments SZF02, SZF04 and SZF05, which plot within the

field of PGE-enriched sulphides, the matrix samples plot with higher PGE relative to five

of the eight fragment samples; the latter plot well within the field of PGE-depleted

sulphides. The three PGE-rich fragments - SZF02, SZF04 and SZF05 – are suspected of

containing remobilized PGE and also have much higher PGE concentrations than the

matrix, suggesting that the PGE were introduced by way of the matrix magma(s).

Specifically, it is possible that post-crystallization impregnation of the fragments by

remobilized sulphides, perhaps by means of deuteric or hydrothermal fluids, resulted in

elevated PGE compositions within select fragments. Alternatively, if the fragments are

indeed xenoliths, then the PGE-rich sulphides may have co-precipitated early on with the

silicate minerals that comprise the fragments, perhaps within a staging chamber.

Primitive mantle-normalized plots of PGE, Au, Cu and Ni concentrations in 100%

sulphide for the matrix and fragment samples are provided in Figure 6-27. Average

compositions of the fragment and matrix samples are characterized by positive slopes

with the Pt-Pd-Au-Cu portions elevated relative to the Ni-Ir-Ru-Rh portion; the average

matrix and fragment patterns are almost identical. Profiles from the average River Valley

intrusion samples are compared with average values for the J-M Reef (Stillwater),

representing reef-type PGE deposits, average flood basalt related to Cu-Ni-PGE deposits

such as Noril’sk (Russia), average Konttijarvi Marginal Series values from the Portimo

Complex (Finland), representing contact-type mineralization from a similar geological

environment, average values from the East Bull Lake intrusion (contact-type

mineralization), and average values from the South Roby Zone of the Lac des Iles

Complex, representing remobilized/hydrothermal deposits (J. Hinchey, unpublished data,

2004).

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SZM01SZM02SZM03SZM04SZM05Average MatrixSZF01SZF02SZF03SZF04SZF05Average FragmentAverage EBLIAvg SRZ - Lac des Iles

(B)

Figure 6-27ab. Primitive mantle-normalized chalcophile metal abundances (recalculated to metals in 100% sulphide) from matrix and fragment samples, River Valley intrusion. (A) Average metal abundance for matrix and fragment samples from the River Valley intrusion compared with disseminated sulphide mineralization and PGE abundances from other mafic intrusions. (B) Average chalcophile abundance of matrix and fragment samples compared with individual samples from the South Zone, Dana South Deposit.

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(D)

Figure 6-27cd. Primitive mantle-normalized chalcophile metal abundances (recalculated to metals in 100% sulphide) for matrix and fragment samples, River Valley intrusion. (C) Average chalcophile abundance of matrix and fragment samples compared with individual samples from the Central Zone, Dana North Deposit. (D) Average chalcophile abundance of matrix and fragment samples compared with individual matrix samples from the Central and South zones.

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Figure 6-27ef. Primitive mantle-normalized chalcophile metal abundances (recalculated to metals in 100% sulphide) for matrix and fragment samples, River Valley intrusion. (E) Average chalcophile abundance of matrix and fragment samples compared with individual fragment samples from the Central and South zones. (F) Average chalcophile abundance of matrix and fragment samples compared with individual matrix samples from the South Zone.

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Figure 6-27gh. Primitive mantle-normalized chalcophile metal abundances (recalculated to metals in 100% sulphide) for matrix and fragment samples, River Valley intrusion. (G) Average chalcophile abundance of matrix and fragment samples compared with individual fragment samples from the South Zone. (H) Average chalcophile abundance of matrix and fragment samples compared with individual matrix samples from the Central Zone.

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Figure 6-27i. Primitive mantle-normalized chalcophile metal abundances (recalculated to metals in 100% sulphide) for matrix and fragment samples, River Valley intrusion. (I) Average chalcophile abundance of matrix and fragment samples compared with individual fragment samples from the Central Zone. All of the plots in Figure 6-27 (A to I) use Mantle normalizing values are from Barnes et al. (1988) and McDonough and Sun (1995). Data for “Average EBLI” is from Peck et al. (1995); “Streich Dike” is from Vogel et al. (1999); “J-M Reef” and average “Flood Basalt” are from Naldrett (1981); Portimo is from the Marginal Series in the Konttijarvi intrusive (Iljina, 1994); and, average Lac des Iles – South Roby Zone (SRZ) is from J. Hinchey (unpublished data, 2004). Mantle normalizing values are from Barnes et al. (1988) and McDonough and Sun (1995).

420

Platinum-group element profiles from average fragment and matrix compositions are

most similar to the East Bull Lake intrusion but are also similar to the sulphides of the

Konttijarvi Marginal Series (Fig. 6-27a). Average River Valley intrusion, East Bull Lake

and Konttijarvi Marginal Series data are distinguished from flood basalt (Naldrett, 1981)

by distinctly lower Ni/Ir and Cu/Pd values, higher total Pd abundances, and much higher

Ir and Ru abundances (Fig. 6-27a). The average PGE pattern from the Lac des Iles

Complex, considered an example of deuteric or hydrothermally altered sulphide

mineralization (Brügmann et al., 1989), is distinct from the average River Valley

intrusion sulphides with higher Pd abundance and lower Cu, Ir, Ru, Rh and Pt

abundances, suggesting that development of the River Valley intrusion sulphides is

dominated by magmatic processes.

Although patterns of average PGE in sulphide concentrations are quite similar for the

River Valley intrusion samples, in detail there is much more difference when considering

individual matrix and fragment PGE patterns (Fig. 6-27b-i). All of the matrix samples

from the South Zone exhibit patterns that approximate the average matrix and fragment

profile as well as the average East Bull Lake PGE data (Fig. 6-27f); matrix sample

SZM01 is slightly depleted in Ir and Pd, resulting in a lower Pd/Ir value (1.3) relative to

other matrix samples. South Zone fragment samples SZF01 and SZF03 exhibit distinct

PGE profiles in comparison to other fragment samples from the South Zone (Fig. 6-27g),

with depleted overall abundances of PGE (in 100% sulphide), high Ni/Ir values (8.4 and

11.0) and high Cu/Pd values (24.1 and 10.0). These patterns and ratios are very similar to

those reported by James et al. (2002a) for structurally controlled (remobilized)

mineralization in the East Bull Lake intrusion. In the River Valley intrusion rocks, this

may reflect preferential secondary reconcentration of low-melting-point precious metals

(i.e. Pd, Pt and Au) and Cu into the fragments during post-magmatic processes (i.e.

hydrothermal redistribution); the precious metals could have been sourced from new

influxes of magma (matrix) and/or previously existing magmatic sulphide mineralization

(assimilated fragments).

Matrix and fragment samples from the Central Zone show the greatest deviation

from the “normal PGE trend” as established by the average matrix and fragment

compositions from the River Valley intrusion and average composition from the East

421

Bull Lake intrusion (Fig. 6-27c). Central Zone matrix samples CZM01 and CZM03 are

the only two samples of the six that exhibit PGE patterns similar to the “normal PGE

trend” including high abundance in Pd relative to the other metals and low Ni/Ir and

Cu/Pd values; sample CZM03 has a lower total abundance of PGE but follows a similar

step-wise pattern (Fig. 6-27h). Samples CZM02, CZF01, CZF02 and CZF03 share

similar PGE profiles with relatively lower total PGE abundance, low Pd/Ir values, and

high Ni/Ir and Cu/Pd ratios. These patterns and ratios are similar to the South Zone

fragments SZF01 and SZF03, and as in these samples likely record a predominance of

remobilized sulphide mineralization.

6.8 Modelling of Sulphide Compositions

The sulphide compositions of the 128 samples from the River Valley intrusion, 112

from drill hole RV00-22 and 16 from the fragment-matrix sample suite, were modelled

using the mass balance R factor equation of Campbell and Naldrett (1979) as described in

Section 2.3.5. Utilizing the Pd versus Cu/Pd diagram of Barnes et al. (1993) the

modelling curves (R factor curves) are plotted along with the Pd and Cu/Pd values from

the 128 mineralized and unmineralized samples (Fig. 6-28). The average Cu and Pd

abundances of the Layered Units (Group-2 data: 21 ppb Pd, 90 ppm Cu, 4260 Cu/Pd,

0.04wt% S) are used as the best estimate for the parental magma composition as they

represent unmineralized and S-undersaturated magmas.

In Figure 6-28, the majority of LU sulphides and all of the Central Zone fragment

and matrix sulphide can be modelled using R factors of less than 1000. The bulk of the

BX sulphide, along with sulphide from South Zone fragments and matrix can be

modelled with R factors that range from 1000 to 10,000. Sulphide from several BX and

one South Zone fragment can be modelled with R factors between 10,000 and 100,000.

Nearly all of the sulphide from IBZ and a number of BX and LU samples fall below the

sulphide-silicate tie lines for R=10,000 and R=100,000 which suggests loss of Cu,

probably due to hydrothermal redistribution. However, this is not reflected in the S/Se

data in which the IBZ and BX have comparable S/Se ratios and do not show any S loss.

The results suggest that the main mineralized rocks (BX) of the Dana North Deposit at

the River Valley intrusion, experienced R factors between about 1000 and 10,000. In

comparison, Peck et al. (2001) suggested that average disseminated sulphide

422

compositions (25 PGE-rich samples) from the Lower and Marginal Series of the East

Bull Lake intrusion could be modelled using R factors that ranged from 2100 to 6000.

1

10

100

1000

10000

100000

1000000

0.1 1 10 100 1000 10000 100000 1000000

Pd (ppb)

Cu/

Pd

LUIBZBXBZFBXSZ-MatrixSZ-FragmentCZ-MatrixCZ-Fragment

MANTLE

DEPLETED

ENRICHED

100%

100%

R=100

R=1000

R=10,000

R=100,000

R=2000

1.0%

Figure 6-28. Discrimination plot of Pd versus Cu/Pd showing the sulphide compositions

for 128 samples (112 from Group-2 data – drill hole RV00-22, 16 fragment-matrix

samples) from the River Valley intrusion. Tie lines are mixing lines between sulphide and

silicate melt at various R factors, ranging from 100 to 100,000, and determined after

methods described by Campbell and Naldrett (1979) and Naldrett (1981). Markers along

each of the mixing lines represent percentages of precipitated sulphide melt at 0.1%,

1.0%, and 10% through to 100% sulphide. The star symbol represents the estimated

parental magma composition derived from the average composition of 12 unmineralized

(<0.05 wt% S) rocks from the Layered Units (21 ppb Pd, 90 ppm Cu, 4260 Cu/Pd,

0.04wt% S) and assuming a sulphide component of 36.5 wt%. Fields of mantle rocks,

and those depleted and enriched in PGE relative to mantle are taken from Barnes et al.

(1993).

423

Barnes et al. (1997) reported ranges in calculated R factors for disseminated magmatic

sulphide from several intrusions related to intraplate magmatism (mantle plume and rift-

related), including 1000 to 20,000 (Noril’sk-Talnakh), 200 to 2000 (Cape Smith), 2000 to

10,000 (Duluth Complex), and 200 to 2000 (Muskox).

Many of the samples, including most of the LU and many of the IBZ samples, have

Cu/Pd values that are at or above that of mantle (Fig. 6-28). If the LU rocks approximate

the initial chemistry of the parent magmas to the River Valley intrusion, then it is

probable that these magmas became S-saturated early on in a deep seated staging magma

chamber (cf. James et al., 2002a; see Chapter 7). This also suggests that prior to their

emplacement, the magmas underwent some degree of sulphide fractionation with

removal of what was probably a small amount of sulphide. During their ascension

through the crust and into the River Valley magma chamber, these S-saturated magmas

would have become S-undersaturated as a result of adiabatic decompression, which

increases the solubility of S in the melt (Mavrogenes and O’Neill, 1999; Momme et al.,

2002a). Barring any significant contamination en route through the crust, the magmas

would have remained S-undersaturated until emplacement in the upper crust (River

Valley chamber), at which time they became S-saturated, segregating sulphides at

varying R factors (Fig. 6-28). It is evident that some of the magma(s) became S-saturated

and began precipitating sulphide at the Pd-Cu/Pd value indicated by the estimate of initial

magma composition (star symbol, Fig. 6-28). However, it is also apparent that other

magma(s) became S-saturated at higher Cu/Pd and lower Pd values, suggesting that the

estimated initial composition for Pd is too high to explain all of the rock compositions

and/or that magma(s) were introduced which had lower initial Pd composition(s).

424

6.9 Summary

The East Bull Lake suite of intrusions, and specifically the River Valley intrusion,

present excellent exploration targets for contact-type PGE-Cu-Ni sulphide mineralization

and an understanding of the emplacement environment and origin of the PGE-bearing

sulphides is paramount to future discoveries. As with other East Bull Lake suite

intrusions (i.e. East Bull Lake and Agnew Lake) most of the sulphide mineralization

discovered to date has been within fragment-bearing rock units that are concentrated or

localized along the margins (sidewalls and/or basal contacts) of the intrusions; these are

the Marginal Series rocks in the case of the River Valley intrusion. On the basis of this

and previous studies, along with unpublished data from Pacific North West Capital Corp.

and Anglo American Platinum Corporation Limited, a number of conclusions can be

made regarding the chemistry and petrogenesis of the River Valley intrusion in the

context of the sulphide mineralization.

Controls on Mineralization

1) The identification of reasonably preserved primary igneous contacts between the

sulphide-bearing Marginal Series rocks and the migmatitic and/or sedimentary

country rocks is of particular importance in terms of exploration as it is these regions

of the intrusions that show the best preservation of the Marginal Series rocks.

2) Numerous northeast-trending linear fault and shear zones, up to 1 kilometre wide,

dissect the stratigraphy, including that of the mineralized Marginal Series. The

displacement along these linear features appears to be predominantly strike-slip

(currently, the dip-slip components are poorly constrained) and on the order of 10’s

of metres; consequently tracing the strike of the Marginal Series rocks is not

impractical.

3) Preserved regions (blocks) of Marginal Series rocks between the large-scale fault and

shear zones are typically several hundred metres in length and therefore constitute

regions of potentially continuous sulphide mineralization; these are important from

the standpoint of large-tonnage bulk mining operations.

4) There is a regional pattern of metamorphic grade, ranging from greenschist facies in

the northeastern part of the intrusion (i.e. Dana North Deposit, Fig. 6-2) to granulite

425

facies in the furthest southeastern parts of the intrusion (i.e. Razor, Fig. 6-1).

Although yet to be confirmed, there may be an important connection between

metamorphic grade and PGE concentration, as the highest grades and greatest

accumulations of PGE are found in the areas of lower metamorphic grade (i.e. Dana

North and South Deposits).

5) A remarkably consistent stratigraphy for the Marginal Series rocks exists in the

region between the Dana North and the Lismer’s South deposit (Figs. 6-2 and 6-3).

Contact-type disseminated PGE-Cu-Ni sulphide mineralization is concentrated

within the Breccia Unit of the Marginal Series.

6) Anomalous PGE values (>500-1000 ppb Pt and/or Pd) occur throughout the Breccia

Unit with still higher concentrations of PGE (>3000 ppb Pt and/or Pd) occurring as

high-grade regions within the lower one-third of the mineralized zones.

Major Element Geochemistry

1) The rocks of the Marginal Series are sub-alkaline, and on the basis of CIPW

normative calculations, are dominated by olivine-normative gabbronorite to olivine

leucogabbronorite. Fragment compositions (CIPW melagabbronorite and

gabbronorite) and are much more mafic than the hosting matrix.

2) Rocks of the BX have the highest individual (11.8 wt% MgO) and average (~9.3

wt%) MgO compositions, reflecting the high proportion of high magnesian (mafic)

fragments in this unit. The higher MgO compositions of the fragments relative to the

enclosing matrix suggests that the magma(s) from which the fragments were derived

was/were much more primitive than the magma(s) that formed the matrix.

3) In the BX, a strong correlation exists between elevated SiO2, TiO2, Pt+Pd and the

presence of patchy blue quartz, corroborating the empirical observation that higher

PGE concentrations are more commonly associated with blue quartz; Ma et al.

(2001) attributed the anomalously blue colour to sub-micrometre inclusions of

ilmenite in the quartz.

426

Trace Element Geochemistry

1) Chondrite-normalized REE patterns for the vast majority of River Valley rocks

are characterized by LREE enrichment, have narrow ranges in (La/Yb)N, and

display modest positive Eu anomalies. The REE patterns of the BX are similar to

those of the upper stratigraphy rocks, suggesting a common origin.

2) The consistently low (La/Sm)N values through the BX and IBZ and their

similarity to the overlying LU suggests that contamination from local footwall

rocks was insignificant. Moreover, the very high (Th/Yb)N values (~2 to 10 times

that of primitive mantle) are interpreted to be the consequence of extensive crustal

contamination of a mantle-derived magma.

3) The majority of REE patterns exhibit negative Nb and Ta anomalies but in each

case the negative Nb anomalies are much larger than those of Ta. This is a

characteristic feature of boninitic magmas (A.J. Crawford, pers. comm. 2004).

4) All of the samples from the River Valley intrusion have very low Nb/Ta and

Zr/Sm values relative to MORB, primitive mantle, continental crust and modern

adakites. This is interpreted to mean that the River Valley rocks have interacted

with an extensive crustal reservoir, adopting crustal signatures typical of rift-

related magmas and/or continental flood basalt.

5) Five of the six South Zone fragments display very distinct chondrite-normalized

REE patterns and have very high MgO compositions relative to the host matrix.

This suggests that these fragments were not cogenetic with the magmas that

formed the bulk of the River Valley intrusion, but rather that these are xenoliths

that were probably carried into the RV chamber by PGE-rich magmas which are

now represented by the matrix rocks and which probably introduced the bulk of

the PGE-rich sulphides.

Chalcophile Geochemistry

1) The estimated background PGE-Cu-Ni composition for River Valley intrusion

rocks, which also provides an estimate for the parental magma composition, is 6

ppb Au, 22 ppb Pt, 19 ppb Pd, 70 ppm Cu and 97 ppm Ni.

427

2) Strong correlations exist between the chalcophile elements indicating that the

PGE, and particularly that those is in the BX, are strongly sulphide controlled.

Metal ratio diagrams (Ni/Cu vs Pd/Ir, Cu/Ir vs Ni/Pd, wt% MgO vs Pd/Ir) also

support a magmatic origin for the vast majority of the PGE.

3) Sulphides in chondrite-normalized PGE diagrams exhibit patterns that are

consistent with a magmatic origin for the sulphides, with some variations that can

be attributed to local hydrothermal redistribution of the sulphide. Total metal

abundance and patterns for the contact-type disseminated sulphides of the River

Valley intrusion are similar to those from other intrusions with contact-type

mineralization (i.e. East Bull Lake intrusion, Canada; Konttijarvi-Portimo

Complex, Finland) and contrast those with known hydrothermal mineralization

(i.e. Lac des Iles Complex).

4) Discrimination plots of Se versus Pd show that the magmas from which the

sulphides precipitated were PGE metal-fertile second-stage magmas (S-

undersaturated) that had not previously segregated sulphides to any large amount.

Discrimination plots of S/Se versus Pt+Pd add further support to the interpretation

that the sulphide is magmatic in origin, but also indicate that the immediate

footwall rocks are not the source of the S in the mineralized BX.

5) If the PGE-rich sulphides had formed within the River Valley chamber, it would

be expected that the rock units (i.e. the IBZ and LU) overlying the mineralized

unit (i.e. the BX) would be strongly depleted in the PGE, as their counterparts are

in other mineralized layered intrusions and the Sudbury Igneous Complex (Keays

and Lightfoot, 2004). As this is not the case, then the sulphides must have been

formed prior to the River Valley “feeder” magmas entering the River Valley

magma chamber.

6) The Cu/Pd ratios for the all of the River Valley samples are <12,000, the value at

which S-saturation is expected to occur, and therefore represent S-undersaturated

magmas.

7) Samples with low Cu/Pd ratios are considered to have formed under high R factor

conditions. The majority of the sulphides from the BX can be modelled using R

428

factors that range from about 1000 to 10,000 and a small number from the BX can

be modelled with R factors between 10,000 and 100,000.

429

CHAPTER 7: DISCUSSION AND PETROGENESIS

7.1 Summary and Implications

Understanding the behaviour of the chalcophile elements is not only important in

characterizing and understanding the petrogenesis of the PGE-Cu-Ni sulphide

mineralization, but also establishing the metallogenic potential of the Nipissing Gabbro

and East Bull Lake suite of intrusions to host economic accumulations of PGE. The

current study has shown that the magmas which fed the Nipissing Gabbro intrusions and

the River Valley intrusion of the East Bull Lake suite exhibit similar geochemical

characteristics. Of particular petrogenetic importance are the similarities in trace element

features, including:

1) strong LREE and LILE enrichment, a narrow range in La/Yb, and modest positive

to negative Eu anomalies;

2) high Th/Yb (2 to 10 times primitive mantle), La/Sm and Th/Nb values;

3) pronounced negative Nb, Ta and P2O5 anomalies, and in many cases negative Ti;

4) negative anomalies of Nb that are much stronger than those of Ta; and,

5) unusually low Nb/Ta and Zr/Sm compositions.

These are all features of a magma that has interacted with a crustal reservoir (Brügmann

et al., 1993; Lightfoot and Keays, 2004). These magmas also share similar characteristics

in terms of their chalcophile elements, including:

1) anomalously high background compositions for PGE relative to normal mafic

rocks;

2) good correlation between the individual chalcophile elements indicating strong

sulphide control on the PGE;

3) chondrite-normalized PGE patterns consistent with known magmatic sulphides;

and,

4) Se-Pd and Pd-Cu values that are consistent with both S-undersaturated, PGE-un

depleted continental flood basalt (CFB) magmas, second stage boninite magmas,

and PGE-enriched “pregnant” magmas.

430

Although it is recognized that the sulphide present in these intrusions has been subjected

to varying amounts of hydrothermal (deuteric) redistribution, the evidence clearly

indicates that the sulphides found in both the River Valley intrusion and the Nipissing

Gabbro suite are magmatic in origin.

It is apparent from the chalcophile element data (i.e. Pt, Pd, Cu, S, Se) that the

parental magmas which formed the River Valley intrusion and Nipissing Gabbro suite

intrusions were S-undersaturated and PGE-fertile or “pregnant” (Hamlyn and Keays,

1988; Keays et al., 2002; Keays et al., 2004) as described by Peck et al. (2001) for the

East Bull Lake intrusion. These parent magmas must have transported PGE-rich

sulphides into the River Valley and Nipissing Gabbro magma chambers. This is

especially evident from the anomalously high background concentrations of PGE which

are recorded in the unmineralized rocks from the River Valley intrusion (22 ppb Pt, 19

ppb Pd, 70 ppm Cu, 97 ppm Ni) and the Nipissing Gabbro intrusions (12.4 ppb Pt, 20.5

ppb Pd, 91 ppm Cu, 149 ppm Ni). These concentrations are orders of magnitude higher

than MORB, and closer to concentrations recorded from second-stage and boninitic

magmas (Hamlyn and Keays, 1986; Peck et al., 1992), Siliceous High Magnesium

magmas (Sun et al., 1991; Seitz and Keays, 1997) and CFB (Brügmann et al., 1993;

Momme et al., 2002b; Lightfoot and Keays, 2004).

7.2 Parental Magmas and Contamination

S-undersaturated magmas such as boninites and Siliceous High Magnesium Basalt

(SHMB) magmas have been proposed as the most likely candidates for producing fertile

intrusions in terms of PGE concentrations (Hickey and Frey, 1982; Hamlyn et al., 1985;

Hamlyn and Keays, 1986; Keays, 1982, 1995; Seitz and Keays, 1997; Sun et al., 1991).

Distinctive geochemical features of these rocks include (Piercey et al., 2001; Crawford et

al., 1989): 1) high MgO (>10 wt%), Mg-number (≥60), and Al2O3/TiO2 ratios (>35); 2)

low TiO2 (<0.5 wt%); 3) intermediate SiO2 compositions (≥53 wt%); 4) moderate to

strong U-shaped REE patterns; 5) pronounced negative HFSE anomalies (i.e. Nb, Ta, Ti);

and, 6) variable enrichment in LREE, Zr, Rb, Sr, Ba and alkali elements. These

geochemical characteristics are considered evidence that these magmas are second-stage

melts (or even multistage) derived by partial melting of a severely depleted upper mantle

which has been metasomatically enriched as a result of hydrous fluid migration within a

431

subduction zone environment (Hickey and Frey, 1982; Crawford et al., 1989; Peck et al.,

1992). Of particular importance to ore genesis is the second-stage nature of these

magmas which results in sulphides with higher PGE compositions, relative to those

magmas generated by first-stage melts (Hamlyn and Keays, 1986; Keays, 1995).

Primitive mantle-normalized multi-element diagrams, provided in Figure 7-1,

compare the REE and trace element patterns for estimated parental magmas from the

River Valley intrusion (average Layered Units) and Nipissing Gabbro intrusions (average

chilled margin gabbro) with average compositions from N-MORB, E-MORB, boninite

and uncontaminated and heavily contaminated continental flood basalts from the Siberian

Trap. The overall LILE and REE patterns from the River Valley and Nipissing Gabbro

averages are remarkably similar, suggesting similar petrogenesis of the magmas. The

patterns of elevated LILE and LREE, along with the relative depletions in Nb, Ta, P

(wt% P2O5) and Ti (wt% TiO2) for the River Valley and Nipissing Gabbro averages

closely resemble the pattern of heavily contaminated CFB (Fig. 7-1a), contrasting the

patterns of boninite, N-MORB, E-MORB, and uncontaminated CFB. The Siberian Trap

CFB are much more contaminated than the estimated parental magmas for the River

Valley intrusion and Nipissing Gabbro intrusions and this is reflected in their elevated

LILE and REE compositions (Fig. 7-1). Normalizing the average River Valley and

Nipissing Gabbro values against heavily contaminated CFB results in near-flat but saw-

tooth patterns that are slightly less than 1; the pronounced Sr anomaly is probably due to

cumulus plagioclase. These normalized patterns suggest that the estimated parental

magmas to the River Valley and Nipissing Gabbro intrusions were contaminated CFB;

the <1 normalized values reflect the exceptionally contaminated nature of the Siberian

Trap CFB as compared to the River Valley and Nipissing Gabbro parental magmas (Fig.

7-1b).

Some CFB lavas such as those of East Greenland and most of the Siberian Traps,

have high PGE contents and were formed from S-undersaturated and PGE-undepleted

magmas (Brügmann et al., 1993; Momme et al, 2002b; Lightfoot and Keays, 2004).

432

0.1

1

10

100

Rb Th K* Nb Ta La Ce Sr Nd P Sm Zr Ti Tb Y Er Yb

Roc

k/Pr

imiti

ve M

antle

Nipissing Gabbro - Parental MagmaRiver Valley LU - Parental MagmaSiberian Trap - contaminated CFBSiberian Trap - uncontaminatedBoninite - Subduction ZoneN-MORBE-MORB

(A)

Figure 7-1a. Primitive mantle-normalized multi-element diagram comparing estimates of

parental magma compositions for the River Valley intrusion (average Layered Unit) and

Nipissing Gabbro intrusions (average chilled margin gabbro) with heavily contaminated

and uncontaminated Siberian Trap CFB, boninite, N-MORB and E-MORB. Data for N-

MORB is from Fitton et al. (2000); data for E-MORB (Moana Loa) is from Crawford and

Keays (unpublished data); data for boninite is from Crawford and Keays (unpublished

data); data for contaminated and uncontaminated Siberian Trap CFB (Nadezhinsky

Formation) is from Lightfoot and Keays (2004). Normalizing primitive mantle values are

from McDonough and Sun (1995).

433

0.01

0.1

1

10

100

Rb Th K* Nb Ta La Ce Sr Nd P Sm Zr Ti Tb Y Er Yb

Roc

k/Pr

imiti

ve M

antle

Nipissing Gabbro - Parental Magma

River Valley LU - Parental Magma

Siberian Trap - contaminated CFB

Nipissing/Siberian Trap (contaminated CFB)

River Valley LU/Siberian Trap (contaminated CFB)

Normalized to Contaminated CFB

(B)

Figure 7-1b. Primitive mantle-normalized multi-element diagram comparing estimates of

parental magma compositions for the River Valley intrusion (average Layered Unit) and

Nipissing Gabbro intrusions (average chilled margin gabbro) with heavily contaminated

Siberian Trap CFB. The estimates of parental magma compositions for the River Valley

intrusion and Nipissing Gabbro intrusions are normalized to heavily contaminated

Siberian Trap CFB resulting in a saw-tooth pattern that is slightly <1. Data for N-MORB

is from Fitton et al. (2000); data for E-MORB (Moana Loa) is from Crawford and Keays

(unpublished data); data for boninite is from Crawford and Keays (unpublished data);

data for contaminated and uncontaminated Siberian Trap CFB (Nadezhinsky Formation)

is from Lightfoot and Keays (2004). Normalizing primitive mantle values are from


434

The high PGE contents of these lavas poses a yet unresolved problem as traditional

mantle melting models predict that the formation of PGE-undepleted magmas requires a

minimum of 25% partial melting (Lightfoot and Keays, 2004) whereas the REE predict,

for example, that the some of the East Greenland CFB were formed by as little as 5%

partial melting (Tegner et al., 1998).

Momme et al. (2002c) attempted to explain the high PGE contents of the plume-

generated CFB in Iceland with the “Triangular Melting Regime” model. This model,

originally developed by Langmuir et al. (1992) to explain the generation of magmas at

spreading ridges, invokes a melting regime beneath a continental rift that is “triangular”

in form and governed by magma upwelling (ascending mantle plume) and corner flow

(asthenospheric mantle flow) that is perpendicular to the vertical rise of the mantle

plume. The melting regime essentially produces several different melt types from which

to draw parental magmas (Momme et al., 2002b): (1) in the asthenosphere (~120 km

depth), low degrees of melting from the lower “corners” of the upwelling melt triangle

results in high (La/Sm)N, low PGE content, and S-saturated (olivine tholeiite) melts; (2)

at the top of the melting column (~60 km depth) high degrees of melting from the upper

“point” of the upwelling melt triangle (near the top of the asthenosphere/base of the

lithospheric mantle) results in low (La/Sm)N, high PGE content, and S-undersaturated

(picrite) melts; and, (3) within the lower lithospheric mantle, intermediate degrees of

melting result in an ascending melt that has intermediate (La/Sm)N and PGE content. In

applying the Triangular Melting Regime model to Iceland, Momme et al. (2002c)

demonstrated that PGE-undepleted and S-undersaturated magmas can be generated by

11-12% partial melting of a mantle plume.

Lightfoot and Keays (2004), argued that the Triangular Melting Regime model does

not adequately explain the PGE-undepleted nature of those CFB basalts in East

Greenland and Siberia whose REE contents suggest even lower degrees of partial

melting. Alternatively, Lightfoot and Keays (2004), proposed that the Siberian Trap

magmas were formed by the interaction of high MgO (picritic?) magmas, sourced from a

mantle plume, with lithospheric mantle from which S-saturated first-stage melts (MORB-

type magmas) had already been extracted. This lithospheric mantle would have been

depleted in the incompatible elements and in particular, would have been strongly

435

depleted in S, but enriched somewhat in PGE; the PGE would have been retained in the

residual sulphides left behind in the refractory residue as a result of partial melting (i.e. a

source for a second-stage melt). Interaction of the depleted lithospheric mantle with the

plume-sourced picritic melts would have produced a S-undersaturated and PGE-

undepleted (second-stage) magma. It is possible that the plume-sourced high MgO melt

was an alkali picrite or a maymechite (very Mg-rich alkaline volcanic rock), which are

subordinate but important rock types in the Siberian Trap (Arndt et al., 1998).

The current study has demonstrated that unmineralized rocks from the Layered Units

in the River Valley intrusion and most rocks from the Nipissing Gabbro suite exhibit

geochemical homogeneity that can only be accounted for by invoking a single source for

their respective magmas. Of particular note is the consistency in the geochemistry of the

rocks from the Nipissing Gabbro intrusions, which were collected from seventeen

different intrusions with an extensive geographic distribution (Fig. 1-2). Both suites of

rocks also exhibit evidence for significant but reasonably uniform contamination of

mantle-derived magmas, suggesting that the crustal contamination occurred in either a

single large staging chamber or in a section of the crust that had a uniform composition.

Lithogeochemical studies (Conrod, 1988; Lightfoot and Naldrett, 1989) on Nipissing

Gabbro sills have shown that compositional variances in individual intrusions are

reflective of AFC processes, whereby strong in-situ differentiation was coupled with

contamination of the magmas by assimilation of local country rocks. However, these

authors also point out that the contamination signature that is common and consistent

throughout the Nipissing Gabbro intrusions is not related to local contamination but

rather to earlier bulk contamination of the magmas at their source. If the contamination

signatures observed in all the intrusions were due to the assimilation of local lithologies

then one would expect a much wider variation in their composition. Lightfoot and

Naldrett (1989) and Lightfoot et al. (1986, 1987, 1993), primarily on the basis of

geochemical evidence, argued convincingly that the Nipissing Gabbro intrusions

represent the intrusive roots of an eroded continental flood basalt. This magmatic

association would explain the pervasive contamination signature found in nearly all

Nipissing Gabbro rocks and supports the premise for a staging chamber within the

underlying continental crust at mid-crustal levels.

436

7.3 Pregnant Magmas

The term “pregnant magmas” was coined by Hamlyn and Keays (1988) to describe

magmas which had carried sulphides formed in one environment, into the resident

magma chambers of PGE-bearing layered mafic/ultramafic intrusions. These authors

devised the term to describe the processes by which PGE mineralization had formed in

the Panton Sill, located in Western Australia (Hamlyn and Keays, 1979). Basically,

pregnant magmas are formed where parental magmas became S-saturated in “staging

chambers” below the final site of mineralization and/or in the conduits that lead into the

intrusions in which the PGE mineralization is currently found. Although the term was

coined to describe platiniferous horizons in layered intrusions, it is equally applicable to

those deposits in which the ore-forming sulphide melts were carried into the magma

chamber. Excellent examples of pregnant magmas are those that formed the giant

Noril’sk-Talnahk deposits (Brügmann et al., 1993; Lightfoot and Keays, 2004) and the

Voisey’s Bay Ni-Cu-Co sulphide deposits (Naldrett et al., 2000). In both of these

examples, Ni-Cu-PGE sulphide melts are believe to have formed at depth in staging

chambers in which primitive mantle-derived magmas became S-saturated and segregated

Ni-Cu-PGE sulphide liquids due to interaction with mid-crustal rocks. The sulphides

were subsequently carried into their current settings by possibly more primitive and

dynamic magmas which were able to entrain the sulphides, and rock fragments in the

case of Voisey’s Bay, and carry them upwards. The sulphides (and rock fragments) were

deposited when the velocity of the carrier magmas decreased on passing from the magma

conduits into larger chambers. Peck et al. (2001) applied this model to the contact

sulphides in the East Bull Lake Intrusion, arguing that the sulphides had formed at depth

and been carried into the East Bull Lake intrusion as entrained droplets of Ni-Cu-PGE

sulphides. The concept of pregnant magmas is also applicable to the River Valley

intrusion; such a magma could not only have transported the PGE-rich sulphides into the

chamber but also the many xenolith fragments observed in the Breccia Unit of the

Marginal Series. Although the magmas that formed the Nipissing Gabbro suite share

many similarities with the River Valley magmas, they appear to have not been pregnant

magmas but rather their sulphides were dissolved in the parental magmas (probably

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during ascent through the crust), precipitating in-situ (and early-on), during normal

fractionation and cooling of the S-undersaturated silicate magma.

7.4 Genetic Model

There are three principal mechanisms of contamination which may lead to S-

saturation and the precipitation of sulphide (Keays, 1995): 1) the addition of external S

by means of devolitization, partial melting, or bulk assimilation of the S-bearing country

rock; 2) an increase in fO2, leading to a lowering of the FeO content and a reduction in

the S carrying capacity of the magma; and, 3) addition of external silica by assimilation

of siliceous partial melts (assimilation of country rocks or continental lithosphere)

thereby lowering the S solubility of the magma. Perhaps the most important ore-forming

mechanism that has been recognized in many large magmatic PGE-Cu-Ni sulphide

deposits is crustal contamination (e.g. Noril’sk deposits, Li et al.,2003; Duluth Complex,

Theriault et al., 2000; Muskox, Barnes and Francis, 1995; Bushveld Complex, Cawthorn,

1999). Geochemical signatures for magmas from modern subduction zones are

characterized by a mantle source that has been enriched in LILE (i.e. Cs, K, Rb, Sr, Ba),

Th, and commonly by enrichment in LREE (i.e. La, Ce), with relative depletion in HFSE

(i.e. Nb, Ta, Zr, Ti) (Pearce and Norry, 1979; Pearce and Cann, 1993). In contrast,

continental crust assimilation is minimized in oceanic settings, leading to enrichments in

LILE, Th and LREE that are more clearly ascribed to an enriched mantle source (Sun and

Nesbitt, 1978). Of particular significance, however, is that similar signatures can also be

acquired in non-subduction zone settings, such as CFB, through the assimilation of crust

(Sun and McDonough, 1989; Smithies et al., 2004).

Rocks from the Nipissing Gabbro and River Valley intrusions have a distinct crustal

signature, expressed by the relative enrichment in highly incompatible trace elements and

relative depletion in Nb, Ta, and Ti (Fig. 7-1). Geographically, this crustal signature is

pervasive and relatively homogeneous across all of the areas sampled which suggests that

it is not derived from local country rocks but rather from a deeper source. Moreover, the

current study has shown that PGE-rich sulphide mineralization in the fragments and

matrix rocks of the BX from the River Valley intrusion is unrelated to processes within

the present intrusion, but rather that the ore-forming processes were initiated much

earlier. A staging chamber, located at some depth in the crust, is invoked to explain the

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trends noted in the chalcophile and trace elements. The idea of a staging chambers to

explain the extensive crustal contamination signatures and argue against subduction-zone

related magmatism, is noted in other large mafic intrusions. For example, it is largely

accepted that the crustal signature in the Bushveld Complex was acquired by

contamination, both in a lower staging chamber and during ascent of the magmas through

the Kaapvaal crust, rather than during melting of enriched sub-continental lithosphere

(Schiffries and Rye, 1989; Maier et al., 2000). Other examples that invoke assimilation

of crust and the formation of sulphides in a deep-seated staging magma chamber, as

suggested for the East Bull Lake intrusion (Peck et al., 2001) and for other rocks

(Portimo Complex, Iljina and Hanski (2002); Siberian Trap flood basalts, Arndt et al.,

1998; Voisey’s Bay, Naldrett et al., 2000; mafic intrusions, Thompson and Naldrett,

1984).

The striking similarities in magma composition between the two suites, and evidence

for considerable, and potentially economic, accumulations of PGE-Cu-Ni sulphide,

evokes the conclusion that these magma have similar sources and that the sulphides were

subjected to initially similar ore-forming mechanisms, even though their respective

magmatic events are separated by more than 250 Ma. A model to explain the genesis of

the PGE-fertile magmas of the River Valley intrusion and the Nipissing Gabbro suite is

suggested in the context of a mantle plume related, intra-cratonic rift which is widely

accepted to have existed in the region, more or less between ~2.5 and ~2.2 Ga. This does

not imply that a single extremely long-lived (>200 Ma) mantle-plume was responsible for

both of the magmatic events but rather accepts the notion that multi-generations of

mantle plume activity may have been present, with punctuated magmatic activity at ~2.48

Ga and 2~2.2 Ga. Any petrogenetic model must address the elevated PGE concentrations

in the parental magmas, the transport mechanism of the PGE, and the PGE concentration

mechanism(s). The current magmatic model, which is generally applicable to both the

River Valley and Nipissing Gabbro magmas, addresses these parameters, invoking the

development of one or more deep-seated crustal staging chamber(s), and summarized in

Figure 7-2. In the case of the Nipissing Gabbro suite, an alternative model relating to the

source and emplacement mechanism for the parental magmas, as proposed by Buchan et

al. (1998), should be noted. These authors suggest that the Nipissing Gabbro magmas

439

may have been introduced by means of laterally flowing magmas, fed into the region

through the Senneterre Dyke Swarm (see Section 3.4). This model would preclude the

presence of a staging chamber for the Nipissing Gabbro suite in the Sudbury region and

could possibly account for the crustal contamination signature and low R factors of the

magmas. However, assessing the merits of such a model is beyond the scope of this

study.

The first stage of the magmatic model (Fig. 7-2a) is applicable to both the River

Valley and Nipissing Gabbro magmas. Within the respective staging chambers, the S-

undersaturated, primitive mantle-derived magma interacted with crustal lithologies and

introduced crustal S into the magma. The assimilation of crustal material, as indicated by

the crustal trace element and LREE signatures, induced S-saturation and segregation of

PGE-rich sulphides. Assimilation, fractionation and crystallization of the magma (i.e.

AFC processes) would have led to chamber stratification, resulting in the development of

a buoyant feldspathic liquid that rose toward the upper part of the staging chamber, and a

more dense and mafic (ferromagnesian-rich) liquid that settled toward the lower part of

the chamber. The early-formed silicates would have produced mafic (olivine-

orthopyroxene) cumulates and/or chilled phases which are today represented in the River

Valley intrusion by the fine-grained mafic xenoliths in the Breccia Unit; the lack of

olivine-bearing rocks in the Nipissing Gabbro suite also supports such a process. It is

likely that the PGE-rich sulphides observed in the River Valley breccia fragments were

incorporated into the cumulates at this stage. It is important to note that the fragments in

the Breccia Unit are interpreted to have been cumulates and that they are extremely

altered with no textural evidence (i.e. relict textures) to unequivocally identify them as

cumulates; alternatively they could represent chilled margin gabbro and/or pyroxenite

which crystallized early on within the staging chamber.

The second stage of the magmatic model (Fig. 7-2b) is applicable to both the River

Valley and Nipissing Gabbro magmas and their respective staging chambers. As

additional S-undersaturated magma flowed into the staging chamber it would have mixed

with the resident S-saturated magma resulting in the upgrading of PGE tenor in the

resident sulphides (varying R factors) and further segregation of sulphides. The newly

introduced magma would have also displaced some of the modified, S-saturated, PGE-

440

rich sulphide laden magmas out of the staging chamber. The evacuating magmas would

have entrained mafic fragments, derived from early formed cumulates and/or chilled

margin, and PGE-rich sulphide droplets; the sulphide droplets would have continued to

interact with the surrounding silicate liquid upgrading their PGE tenor. In the case of the

River Valley intrusion, these displaced magmas would eventually form the PGE-rich

sulphides that occur in the matrix of the Breccia Unit.

Figure 7-2a. Staging Chamber: S-undersaturated, primitive mantle-derived magmas rise

and form staging chambers at mid-crustal levels. Cooling and crustal contamination

(sulphur source) induces S-saturation and sulphide segregation in the resident magma.

Crystallization and chamber stratification results in a buoyant feldspathic liquid overlying

a more dense mafic liquid. PGE-bearing sulphides form under varying R factors, some

sink and are incorporated into the early formed chilled margin rocks and/or olivine-

orthopyroxene dominated cumulates.

441

In the third stage of the magmatic model, the sulphide (PGE-rich droplets) and

fragment bearing magmas are displaced from the staging chamber and rise through the

crust (Fig. 7-2c). Rapid ascent of the magmas through the crust would have resulted in

adiabatic decompression of the magmas which permitted some or all of the sulphur from

the sulphide melt to be partially or wholly dissolved into the magma. In the case of the

River Valley magmas, the PGE-rich sulphide droplets remained suspended in the S-

saturated magmas and only a small portion of the sulphur from the sulphide melts

(droplets) dissolved into the magma. This, coupled with further interaction between the

silicate liquid and the sulphide droplets, resulted in substantial upgrade of the PGE tenor

in the sulphides. During their ascent, the Nipissing Gabbro magmas became S-

undersaturated and all of the sulphur was dissolved into the magma. The presence of

mafic fragments in the River Valley magmas (Breccia Unit) suggests a very dynamic

magma system, capable of entraining and supporting the fragments as the magmas

ascended through the conduit(s) in the crust. Evidence for this dynamic (turbulent)

magma is accounted for by the high R factors and elevated PGE tenor in the River Valley

intrusion relative to the Nipissing Gabbro suite. The rarity of fragments in the Nipissing

Gabbro suite can be accounted for by lower magma dynamics, as reflected by the low R

factors and relatively low PGE tenor, which resulted in the fragments being “filtered” out

of the ascending magmas. Alternatively, the Nipissing Gabbro magmas may have never

picked up any fragments or the conduits may have been too narrow to allow for the

fragments to be entrained into the final intrusions. Orthopyroxene phenocrysts, common

in nearly all of the Nipissing Gabbro bodies, were either entrained in the ascending

magmas and/or crystallized within the conduit(s) as the magmas ascended through the

crust.

During the final fourth stage of the magmatic model, the magmas were emplaced

into their final magma chambers, where they underwent two very different processes

(Fig. 7-2d). The River Valley magmas, which were S-saturated and “pregnant” with

PGE-rich sulphide droplets, co-precipitated with the silicate minerals that now constitute

the matrix of the Breccia Unit. Convective flow within the magma allowed for further

interaction between the PGE-rich sulphide droplets and the silicate liquid (even higher R

factors), further upgrading the PGE tenor of the sulphides.

442

Figure 7-2b. Displacement: New S-undersaturated, primitive mantle-derived magma

enters the staging chamber and mix with the S-saturated resident magma. The magma

mixing upgrades the PGE tenor in the sulphides under varying R factors. The new

magma also forces the modified, S-saturated, PGE-rich sulphide laden magmas out of the

respective staging chambers. Evacuating magmas entrain mafic fragments derived from

early formed cumulates and/or chilled margin, and PGE-rich sulphide droplets which

continue to interact with the surrounding silicate liquid; these transporting magmas form

the PGE-rich matrix of the Breccia Unit in the River Valley Intrusion.

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Figure 7-2c. Ascent: Displaced magmas, containing PGE-rich sulphide droplets and

fragments, undergo adiabatic decompression permitting some or all of the sulphur from

the sulphide melt to be partially or wholly dissolved into the ascending magma. The

ascending River Valley magmas remain S-saturated and only a small portion of the

sulphur from the sulphide melts is dissolved into the magma, upgrading the PGE tenor of

the sulphide droplets. The ascending Nipissing Gabbro magmas become S-undersaturated

and all of the sulphur is dissolved into the magma. The presence of mafic fragments in

the River Valley magmas (Breccia Unit) suggests a very dynamic magma system which

accounts for the higher R factors and PGE tenor in the River Valley intrusion relative to

the Nipissing Gabbro suite. Fragments are rare in the Nipissing Gabbro suite and this can

be accounted for by lower magma dynamics, as signified by low R factors, resulting in

the fragments being “filtered” out of the ascending magmas.

444

Figure 7-2d. Emplacement: River Valley magmas form the River Valley intrusion

chamber at upper crustal depths (8-12 km). These magmas, which are S-saturated and

“pregnant” with PGE-rich sulphide droplets, co-precipitate with the silicate minerals that

now constitute the matrix of the Breccia Unit. Convective flow within the magma allows

for further interaction between the PGE-rich sulphide droplets and the silicate liquid,

further upgrading the PGE tenor of the sulphides. Nipissing Gabbro magmas, which are

PGE-fertile and S-undersaturated, are emplaced at various levels within the Huronian

Supergroup sedimentary rock sequences. As the magmas cool and crystallize, they

become S-saturated and begin to segregate PGE-rich sulphides, principally within the

massive orthopyroxene gabbro unit within the lower portions of the bodies. The

geochemical characteristics of the River Valley and Nipissing Gabbro suite magmas and

the tectonic setting in which the magmas developed and were emplaced, suggests that

both magmas may have fed continental flood basalts.

445

Significantly, there is almost as much sulphide in the fragments as there is in the matrix;

a similar result is reported Brügmann et al. (1993) for rocks in the Noril’sk region.

Nipissing Gabbro magmas, which at the time of emplacement were PGE-fertile and S-

undersaturated, were emplaced in various forms and at various levels within the Huronian

Supergroup sedimentary rock sequences. As these magmas cooled and crystallized, they

became S-saturated and segregated PGE-rich sulphides through normal fractionation,

principally within the massive orthopyroxene gabbro unit located in the lower portions of

the intrusions.

It is probable that the processes outlined in stages two through four of the magmatic

model would have repeated themselves several times, introducing new batches of magma

into some of the Nipissing Gabbro intrusions and the River Valley intrusion. The

Nipissing Gabbro magmatic event is thought to have spanned a period of about 15 Ma

and Lightfoot and Naldrett (1996) reported evidence for multiple pulses of magma in

some Nipissing Gabbro intrusions. In the River Valley intrusion, field and geochemical

evidence (e.g. stoping of the overlying Layered Units in the Inclusion-bearing Unit and

the distinct PGE-enrichment in the Breccia Unit) suggests that the Marginal Series rocks

represent at least a “second” batch of magma that was introduced into the River Valley

chamber subsequent to crystallization of the bulk of the intrusion (i.e. upper Layered

Units). Although evidence for multiple magma pulses within the Marginal Series’

Breccia Unit itself has yet to be established it is probable that several pulses of PGE-rich

sulphide laden magma were involved.

7.5 Implications to Mineral Exploration

Currently, no economic sulphide deposits have been outlined in either the East Bull

Lake suite intrusions or those of the Nipissing Gabbro suite. However, exploration work

completed to date appears to hold a great deal of promise for the Marginal Series rocks in

the River Valley intrusion, as well as in other East Bull Lake suite intrusions (i.e. East

Bull Lake and Agnew Lake intrusions), and in the stratabound PGE-rich sulphide

mineralization in several Nipissing Gabbro intrusions (e.g. Rastall Occurrence in the

Chiniguchi River intrusion (Janes Township) and the Shakespeare Deposit (Shakespeare

Township).

446

In terms of prospectivity and the potential for economic PGE-Cu-Ni sulphide

deposits, the Nipissing Gabbro intrusions show tremendous possibility. In addition to

confirming that this suite of intrusions indeed have very high background PGE

concentrations, this study demonstrated that many of the Nipissing Gabbro rocks have

very low PGE contents relative to chilled margin, suggesting that the magma(s) became

S-saturated during in-situ fractionation and therefore deposited PGE-bearing sulphides

somewhere in the magma chamber. The bigger question in terms of exploration in these

intrusions is where are these PGE-rich sulphides? Also of significant importance is the

widespread occurrence of this intrusive suite in the Southern Province, the multitude of

mineral occurrences associated with them, and the large volume of magma that is

expected to have moved through the system (Lightfoot and Naldrett, 1996). However,

individual intrusions of Nipissing Gabbro are generally small when compared to those of

the East Bull Lake suite or other classic magmatic sulphide bearing intrusions (i.e.

Muskox, Stillwater, Bushveld), and it is because of this that relatively little exploration

work has focused on magmatic sulphides in these intrusions. Rice (1997), in modelling

the physics of convecting magmas, resolved that economically interesting stratiform PGE

deposits would be restricted to large magma bodies; the smaller the magma chamber, the

thinner the layers and therefore a lower probability of high R factors. On this basis, and

in the context of the typical size of a Nipissing Gabbro body, these intrusions are

considered too small to be of any consequence in terms of generating economic PGE

deposits, despite the fact that Nipissing Gabbro suite intrusions are known to host

stratabound PGE-Cu-Ni mineralization (e.g. Rastall occurrence). It should therefore, be

pointed out that the Konttijarvi body in the Portimo Complex is a relatively small

intrusion (present-day volume of ~0.05 km3; Iljina, 1994) yet it is host to a multi-million

ounce PGE deposit. By comparison, the Chiniguchi River intrusion is estimated to have

a present-day (minimum) volume of ~2 km3, and sills such as the Kukagami Lake

intrusion have estimated present-day volumes of ~0.5 km3. The significance of this is

that the small size of a mafic body does not necessarily make it non-prospective and that

the specific characteristics of the intrusion (i.e. intrusion geometry, magma source

(geochemistry/genesis), R factors, volume of magma introduced), interpreted in the

447

context of the larger tectonic environment, are perhaps of greater significance in mineral

exploration.

The potential for discovery (delineation) of an economic PGE-Cu-Ni deposit or

deposits in the River Valley and East Bull Lake intrusions is promising, especially when

considering their size and the fact that mineral exploration to date has not been very

extensive and/or systematic. An important concept in the exploration for contact-type

PGE deposits is that they are in general analogous to the low-grade, large tonnage Cu-Au

rich porphyry models; a particularly important concept to grasp in the exploration and

economic evaluation of contact-type PGE mineralization. In Canada, there is only one

primary producer of PGE (Pt-Pd), the Lac des Iles mine (Lac des Iles Complex) located

about 100 km north of Thunder Bay, Ontario. The Measured and Indicated resources of

this producing mine total over 145 million tonnes grading 1.57g/t Pd, 0.17g/t Pt, 0.12g/t

Au, 0.06% Cu and 0.05% Ni (North American Palladium Ltd., Press Release, March 5th,

2001). The Konttijarvi and Ahmavaara mineralised zones in the Konttijarvi-Suhanko

intrusion of the Portimo Complex, Finland are direct analogues to the geology and

mineralization described for the East Bull Lake suite and Nipissing Gabbro intrusions

(Vogel et al., 1998b). Gold Fields Limited reported (Press Release, July 23rd, 2001) that

the Konttijarvi deposit contains a Measured, Indicated and Inferred resource of over 43

million tonnes grading 1.42 g/t Pd, 0.39 g/t Pt, 0.1 g/t Au, 0.15% Cu and 0.06% Ni,

including a Measured resource of 11.7 million tonnes grading 1.6 g/t Pd, 0.43 g/t Pt, 0.1

g/t Au, 0.15% Cu and 0.07% Ni (0.5 g/t Pd-Pt-Au cut-off grade). Also in the Portimo

Complex, the Ahmavaara deposit has a reported Measured, Indicated and Inferred

resource of over 74 million tonnes grading 1.05 g/t Pd, 0.22 g/t Pt, 0.12 g/t Au, 0.21% Cu

and 0.09% Ni, including a Measured resource of 11.8 million tonnes grading 1.02 g/t Pd,

0.19 g/t Pt, 0.1 g/t Au, 0.21% Cu and 0.09% Ni. These “real world” examples indicate

that a bulk-tonnage, low-grade PGE operation is possible and it is expected that potential

economic contact-type PGE mineralization may require a minimum 20-50 million tonnes

at grades >2.0 g/t PGE, bearing in mind that these estimates are highly dependent on

commodity prices.

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REFERENCES Alapieti, T.T. and Lahtinen, J.J., 2002. Platinum-group element mineralization in layered

intrusions of northern Finland and the Kola Peninsula, Russia. In The Geology, Geochemistry, Mineralogy and Mineral Beneficiation of Platinum-Group Elements. L.J. Cabri (ed). Canadian Institute of Mining, Metallurgy and Petroleum, Special Volume 54, p. 507-546.

Alapieti, T.T., Filen, B.A., Latinen, J.J., Lavrov, M.M., Smolkin, V.F. and

Viotsekhovsky, S.N., 1990. Early Proterozoic layered intrusions in the northeastern part of the Fennoscandian Shield. Mineralogy and Petrology, v.42, p. 1-22.

Arndt, N., Chauvel, C., Czamanske, G., and Fedorenko, V., 1998. Two mantle sources,

two plumbing systems: tholeiitic and alkaline magmatism of the Maymecha River basin, Siberian flood volcanic province. Contributions to Mineralogy and Petrology, v.133, p. 297-313.

Ashwal, L.D. and Wooden, J.L., 1989. River Valley pluton, Ontario: A late-

Archean/early Proterozoic anorthositic intrusion in the Grenville Province. Geochimica et Cosmochimica Acta, v.53, p.633-641.

Aspler, L.B. and Chiarenzelli, J.R., 1997. Initiation of ~2.45-2.1 Ga intracratonic basin

sedimentation of the Hurwitz Group, Keewatin Hinterland, Northwest Territories, Canada. Precambrian Research, v.81, p. 265-297.

Aspler, L.B., Bursey, T.L., and Miller, A.R., 1989. Sedimentology, structure, and

economic geology of the Poorfish-Windy thrust-fold belt, Ennadai Lake area, District of Keewatin, and the shelf to foredeep transition in the foreland of Trans-Hudson orogen. In Current Research, Part C. Geological Survey of Canada, Paper 89-1C, p. 143-155.

Baksi, A.K., 2001. Search for a deep-mantle component in mafic lavas using Nb-Y-Zr

plot. Canadian Journal of Earth Sciences, v.38, p. 813-824. Barnes, S.J. and Naldrett, A.J., 1985. Geochemistry of the J-M (Howland) reef of the

Stillwater Complex, Minneapolis adit area. I. Sulfide chemistry and sulphide-olivine equilibrium. Economic Geology, v.80, p.627-645.

Barnes, S.J., Keays, R.R., and Hoatson, D.M., 1992. Distribution of sulphides and PGE

within the porphyritic websterite zone of the Munni Munni Complex, Western Australia. Australian Journal of Earth Sciences, v.39, p. 289-302.

Barnes, S.J., McIntyre, J.R., Nisbet, B.W. and Williams, C.R., 1990. Platinum group

element mineralization in the Munni Munni Complex, Western Australia. Mineralogy and Petrology, v.42, p.141-164.

449

Barnes, S.-J., 1990. The use of metal ratios in prospecting for platinum-group element deposits in mafic and ultramafic intrusions. Journal of Geochemical Exploration, v.37, p. 91-99.

Barnes, S.-J. and Francis, D., 1995. The distribution of platinum-group elements, nickel,

copper, and gold in the Muskox Layered Intrusion, Northwest Territories, Canada. Economic Geology, v.90, p. 135-154.

Barnes, S.-J., Zientek, M.L., and Severson, M.J., 1997. Ni, Cu, Au, and platinum-group

element contents of sulphides associated with intraplate magmatism: a synthesis. Canadian Journal of Earth Sciences, v.34, p. 337-351.

Barnes, S.-J., Couture, J.-F., Sawyer, E.W., and Bouchaib, C., 1993. Nickel-copper

occurrences in the Belleterre-Angliers belt of the Pontiac Subprovince and the use of Cu/Pd ratios in interpreting platinum-group element distributions. Economic Geology, v.88, p.1402-1418.

Barnes, S.-J., Boyd, R., Korneliussen, A., Nilsson, L.-P., Often, M., Pedersen, R.B., and

Robins, B., 1988. The use of mantle normalization and metal ratios in discriminating between the effects of partial melting, crystal fractionation and sulphide segregation on platinum-group elements, gold, nickel and copper: examples from Norway. In Geo-platinum 87. H.M. Prichard, P.J. Potts, J.F.W. Bowles and S. Cribb (eds). Elsevier, Barking, p. 113-431.

Bennett, G., 1997. The Huronian – from the bottom – up. In Institute on Lake Superior

Geology, 43rd Annual Meeting, Sudbury, Part 1, Program and Abstracts, p. 7-8. Bennett, G., Dressler, B.O., and Robertson, J.A., 1991. The Huronian Supergroup and

associated intrusive rocks. In Geology of Ontario. P.C. Thurston, H.R. Williams, R.H. Sutcliffe, and G.M. Stott (eds). Ontario Geological Survey, Special Volume 4, Part 1, p. 549-591.

Bleeker, W., 2002. Archaean tectonics: a review with illustrations from the Slave craton.

In The Early Earth: Physical, Chemical and Biological Development. C.M.R. Fowler, C.J. Ebinger, and C.J. Hawkesworth (eds), Geological Society of London, Special Publications 199, p. 151-181.

Born, P., 1979. Geology of the East Bull Lake Layered Gabbro Complex, District of

Algoma, Ontario: unpublished M.Sc. thesis, Laurentian University, Sudbury, Ontario, 147 pp.

Bowen, N.L., 1910. Diabase and Granophyre of the Gowganda Lake District, Ontario.

Journal of Geology, v.18, p. 648-674. Brügmann, G.E., Naldrett, A.J., Asif, M., Lightfoot, P.C., Gorbachev, N.S., and

Fedorenko, V.A., 1993. Siderophile and chalcophile metals as tracers of the

450

evolution of the Siberian Trap in the Noril'sk region, Russia. Geochimica et Cosmochimica Acta, v.57, p. 2001-2018.

Brügmann, G.E., Naldrett, A.J., and MacDonald, A.J., 1989. Magma mixing and

constitutional zone refining in the Lac des Iles Complex, Ontario: Genesis of Platinum-Group Element Mineralization. Economic Geology, v.84, p. 1557-1573.

Buchan, K.L. and Card, K.D., 1985. Preliminary comparison of petrographic and

paleomagnetic characteristics of Nipissing Diabase intrusions in northeastern Ontario. In Current Research, Part A. Geological Survey of Canada, Paper 85-1A, p. 131-140.

Buchan, K.L., Card, K.D., and Chandler, F.W., 1989. Multiple ages of Nipissing Diabase

intrusion: paleomagnetic evidence from the Englehart area, Ontario. Canadian Journal of Earth Sciences, v.26, p. 427-445.

Buchan, K.L., Mortensen, J.K., and Card, K.D., 1993. Northeast-trending Early

Proterozoic dykes of the Superior Province: multiple episodes of emplacement recognized from integrated paleomagnetism and U-Pb geochronology. Canadian Journal of Earth Sciences, 30, p. 1286-1296.

Buchan, K.L., Mortensen, J.K., Card. K.D., and Percival, J.A., 1998. Paleomagnetism

and U-Pb geochronology of diabase dyke swarms of Minto block, Superior Province, Quebec, Canada. Canadian Journal of Earth Sciences, v.35, p. 1054-1069.

Butler, H.R., 2002. Geological Report on the Mystery Offset Dyke Property, Lorne

Township, Ontario. Technical Report for Tearlach Resources Inc., 49 pp. Cabri, L.J., 2001. A mineralogical study of drill core from the Folson lake Project.

Consultants report to Freewest Resources Canada Inc. and Spartan Resources Inc., 18 pp.

Campbell, I.H. and Barnes, S.J., 1984. A model for the geochemistry of the platinum-

group elements in magmatic sulphide deposits. Canadian Mineralogist, v.22, p.151-160.

Campbell, I.H. and Naldrett, A.J., 1979. The influence of silicate:sulphide ratios on the

geochemistry of magmatic sulfides. Economic Geology, v.74, p. 1503-1505. Campbell, I.H., Lesher, C.M., Coad, P., Franklin, J.M., Gorton, M.P., and Thurston, P.C.,

1984. Rare earth element mobility in alteration pipes below massive Cu-Zn sulphide deposits. Chemical Geology, v.45, p. 181-202.

Card, K.D. 1992. Circa 1.75 Ga ages for plutonic rocks from the Southern Province and adjacent Grenville Province: what is the expression of the Penokean orogeny?:

451

Discussion. In Radiogenic Age and Isotopic Studies: Report 6, Geological Survey of Canada Paper 92-2, p. 227-228.

Card, K.D., 1978. Metamorphism of the Middle Precambrian (Aphebian) rocks of the

eastern Southern Province. In Metamorphism in the Canadian Shield. J.A. Fraser and Heywood, W.W. (eds). Geological Survey of Canada, Paper 78-10, p. 269-282.

Card, K.D., 1976. Geology of the Espanola-Whitefish Falls Area, District of Sudbury,

Ontario. Ontario Geological Survey, Report 131, 70 pp. Card, K.D., 1968. Geology of Denison-Waters Area. Ontario Department of Mines,

Geological Report 60, 63 pp. Card, K.D., 1965. Hyman and Drury Townships. Ontario Department of Mines,

Geological Report No. 34, 38 pp. Card, K.D., and Jackson, S.L., 1995. Tectonics and metallogeny of the Early Proterozoic

Huronian Foldbelt and the Sudbury Structure of the Canadian Shield, Field Trip Guidebook. Geological Survey of Canada, Open File 3139, 55 pp.

Card, K.D. and Palonen, P.A., 1976. Geology of the Dunlop-Shakespeare Area, District

of Sudbury. Ontario Division of Mines, Geoscience Report 139, 52 pp. Card, K.D., and Pattison, E.F., 1973. Nipissing diabase of the Southern Province,

Ontario. In Huronian Stratigraphy and Sedimentation. G.M. Young (ed). Geological Association of Canada, Special Paper 12, p. 7-30.

Card, K.D., Innes, D.G., and Debicki, R.L., 1977. Stratigraphy, sedimentology and

petrology of the Huronian Supergroup in the Sudbury – Espanola Area. Ontario Division of Mines, Geoscience Study 16. 99 pp.

Card, K.D., Palonen, P.A., and Siemiatkowska, K.M., 1975. Geology of the Louise-Eden

Area, District of Sudbury. Ontario Division of Mines, Geological Report 124, 66 pp.

Card, K.D., Church, W.R., Franklin, J.M., Frarey, M.J., Robertson, J.A., West, G.F., and

Young G.M., 1972. The Southern Province. In Variation in Tectonic Styles in Canada. R.A. Price and R.J.W. Douglas (eds). Geological Association of Canada, Special Paper 11, p. 336-380.

Cawthorn, R.G., 1999. Platinum-group element mineralization in the Bushveld Complex

– a critical reassessment of geochemical models. South African Journal of Geology, v.102, p. 268-281.

452

Chubb, P.T., 1994. Petrogenesis of the eastern portion of the East Bull Lake gabbro-anorthosite intrusion, District of Sudbury/Algoma, Ontario. unpublished M.Sc. thesis, Laurentian University, Sudbury, Ontario, 230 pp.

Collins, W.H., 1913. The geology of Gowganda mining division, Ontario. Canada

Geological Survey, Memoir 33, 121 pp. Condie, K.C., 1989. Plate Tectonics and Crustal Evolution. Third Edition, Pergamon

Press, Elmsford, N.Y., 476 pp. Conrod, D.M., 1989. The petrology and geochemistry of the Duncan Lake, Beaton Bay,

Milner Lake, and Miller Lake Nipissing Intrusions within the Gowganda Area, District of Timiskaming. Ontario Geological Survey, Open File Report 5701, 210 pp.

Conrod, D.M., 1988. Petrology, geochemistry, and PGE potential of the Nipissing

Intrusions. unpublished M.Sc. thesis, University of Toronto, Toronto, Ontario. Corfu, F. and Andrews, A.J., 1986. A U-Pb age for mineralised Nipissing Diabase,

Gowganda. Canadian Journal of Earth Sciences, v.23, p. 107-109. Corfu, F. and Easton, R.M., 2001. U-Pb evidence for the polymetamorphic history of

Huronian rocks within the Grenville Front tectonic zone east of Sudbury, Ontario, Canada. Chemical Geology, v.172, p. 149-171.

Cox, K.G., 1980. A model for flood basalt vulcanism. Journal of Petrology, v.21, p. 629-

650. Cox, K.G. and Hawkesworth, C.J., 1985. Geochemical stratigraphy of the Deccan Traps

at Mahabaleshwar, western Ghats, India, with implications for open system magmatic processes. Journal of Petrology, v.26, p. 355-377.

Crawford, A J., Falloon, T J., and Green, D.H., 1989. Classification, petrogenesis and

tectonic setting of boninites. In Boninites. A.J. Crawford (ed). Unwin Hyman, London, p.1-49.

Crocket, J.H., 2002. Platinum-Group Element Geochemistry of Mafic and Ultramafic

Rocks. In The Geology, Geochemistry, Mineralogy and Mineral Beneficiation of Platinum-Group Elements. L.J. Cabri (ed). Canadian Institute of Mining, Metallurgy and Petroleum, Special Volume 54, p. 177-210.

Crocket, J.H., 1981. Geochemistry of the platinum-group elements. Canadian Institute of

Mining and Metallurgy, Special Volume 24, p. 47-64.

453

Culshaw, N.G., Corrigan, D., Drage, J., and Wallace, P., 1988. Georgian Bat geological synthesis: Key Harbour to Dillon, Grenville Province of Ontario. In Current Research, Part C, Geological Survey of Canada, Paper 88-1C, p.129-133.

Davidson, A., 1997. New information on the Grenville Front near Sudbury. 43rd Annual

Institute on Lake Superior Geology, Proceedings, v.43, pt.3, 38 pp. Davidson, A., 1986. A new look at the Grenville Front in Ontario. Geological

Association of Canada, Ottawa ’86. Field Trip 15, Guidebook, 31 pp. Davidson, A., van Breemen, O. and Sullivan, R.W. 1992. Circa 1.75 Ga ages for plutonic

rocks from the Southern Province and adjacent Grenville Province: what is the expression of the Penokean orogeny? In Radiogenic Age and Isotopic Studies: Report 6. Geological Survey of Canada Paper 92-2, p. 107-118.

Dressler, B.O., 1982. Geology of the Wanapitei Lake Area, District of Sudbury. Ontario

Geological Survey, Report 213, 131 pp. Dressler, B.O., 1979. Geology of McNish and Janes Townships, District of Sudbury.

Ontario geological Survey, Report 191, 91 pp. Dressler, B.O., Gupta, V.K., and Muir, T.L., 1991. The Sudbury structure. In Geology of

Ontario. P.C. Thurston, H.R. Williams, R.H. Sutcliffe, and G.M. Stott (eds). Ontario Geological Survey, Special Volume 4, Part 1, p. 593-626.

Ernst, R.E. and Buchan, K.L., 2001. The use of mafic dike swarms in identifying and

locating mantle plumes. In Mantle Plumes: Their Identification Through Time. R.E. Ernst and K.L. Buchan (eds). Geological Society of America, Special Paper 352, p. 247-265.

Ernst, R.E., Buchan, K.L. and Palmer, H.C., 1999. Mapping flow patterns in Nipissing

sills to test emplacement patterns. In Abstracts, Tectonic and magmatic Processes in Crustal Growth: A Pan-Lithoprobe Perspective. Web Site: http://cgpd.cgkn.net/panlithoprobe/.

Easton, R.M., 2003. Geology and Mineral Potential of the Paleoproterozoic River Valley

Intrusion and Related Rocks, Grenville Province. Ontario Geological Survey, Open File Report 6123, 172 pp.

Easton, R.M., 2002. Precambrian geology of Street Township, Southern and Grenville

Provinces. Ontario Geological Survey, Open File Report 6078, 149 pp. Easton, R.M., 2000a. Variation in crustal level and large scale tectonic controls on rare-

metal and platinum group element mineralization in the Southern and Grenville Province: In Summary of Field Work and Other Activities 2000. Ontario Geological Survey, Open File Report 6032, p. 28-1 to 28-16.

454

Easton, R.M., 2000b. Metamorphism of the Canadian Shield, Ontario, Canada. II.

Proterozoic Metamorphic History. The Canadian Mineralogist, v.38, p. 319-344. Easton, R.M., 2001. Geology of Glen Afton (River Valley area)(41I/9). Ontario

Geological Survey. Preliminary Map, P.3453 (1:50 000 scale). Easton, R.M., 1999. Platinum group elements, nickel, copper and chromium potential of

mafic rocks within the Grenville Front tectonic zone east of Sudbury. In Summary of Field Work and Other Activities 1998. Ontario Geological Survey, Miscellaneous Paper 169, p.68-69.

Easton, R.M., 1998. New observations related to the mineral potential of the Southern

Province and the Grenville Front tectonic zone east of Sudbury. Ontario geological Survey, Open File Report 5976, 28 pp.

Easton, R.M. 1992. The Grenville Province: In Geology of Ontario, Chapter 19. Ontario

Geological Survey, Special Volume 4, part 2, p. 713-904. Easton, R.M. and Hrominchuk, J.L., 2002. Whole-rock and mineral chemistry, assay, and

petrographic data for the River Valley intrusion, Crerar and Dana townships, Grenville Province, Ontario. Ontario Geological Survey, Miscellaneous Release-Data 95.

Easton, R.M., and Hrominchuk, J.L., 2001a. Precambrian geology, Crerar Township;

Ontario Geological Survey, Preliminary Map P.3432, scale 1:20,000. Easton, R.M., and Hrominchuk, J.L., 2001b. Precambrian geology, Dana Township;

Ontario Geological Survey, Preliminary Map P.3433, scale 1:20,000. Easton, R.M., and Hrominchuk, J.L., 1999. Geology and copper-platinum group element

mineral potential of Dana and Crerar Township, River Valley area, Grenville Province: In Summary of Field Work and Other Activities 1999. Ontario Geological Survey, Open File Report 6000, p. 30-1 to 30-36.

Easton, R.M. and Murphy, E.I., 2002. Precambrian Geology of Street Township, District

of Sudbury. Ontario Geological Survey, Open File Report 6078, 149 pp. Easton, R.M., Davidson, A., and Murphy, E.I., 1999. Transects across the Southern-

Grenville Province Boundary near Sudbury, Ontario. Guidebook #A2, Sudbury ’99. Geological Association of Canada, 52 pp.

Easton, R.M., Jobin-Bevans, L.S., and James, R.S., 2004. Geological Guidebook to the

Paleoproterozoic East Bull Lake Intrusive Suite Plutons at East Bull Lake, Agnew Lake and River Valley, Ontario. Ontario Geological Survey, Open File Report 6135, 84 pp.

455

Easton, R.M., Buckley, S.G., Lobanok, E. and James, R.S., 1996. Grenville-Southern

Province Relationships in Street Township, District of Sudbury: In Summary of Field Work and Other Activities 1996. Ontario Geological Survey, Miscellaneous Paper 166, p. 66-69.

Eckstrand, O.R. and Hulbert, L.J., 1987. Selenium and the source of sulphur in magmatic

nickel and platinum deposits. Geological Association of Canada and Mineralogical Association of Canada, Program Abstracts, 12, 40.

Eckstrand, O.R., Grinenko, L.N., Krouse, H.R., Paktunc, A.D., Schwann, P.L., and

Scoates, R.F.J., 1989. Preliminary data on sulphur isotopes and Se/S ratios, and the source of sulphur in magmatic sulphides from the Fox River Sill, Molson Dykes and Thompson nickel deposits, northern Manitoba. Geological Survey of Canada, Paper 89-1C, p. 235-242.

Fahrig, W.F., 1987. The tectonic settings of continental mafic dyke swarms: failed arm

and early passive margin. In Mafic Dyke Swarms. H.C. Halls and W.F. Fahrig (eds). Geological Association of Canada, Special Paper 34, p. 331-348.

Fairbairn, H.W., Hurley, P.M., Card, K.D., Knight, C.J., 1969. Correlation of

radiometric ages of Nipissing Diabase and Huronian metasediments with Proterozoic orogenic events in Ontario. Canadian Journal of Earth Sciences, 6, p. 489-497.

Fedo, C.M., Young, G.M., Nesbitt, H.W., and Hanchar, J.M. 1997. Potassic and sodic

metasomatism in the Southern Province of the Canadian Shield: evidence from the Paleoproterozoic Serpent Formation, Huronian Supergroup, Canada. Precambrian Research, v.84, p. 17-36.

Finn, G.C., Edgar, A.D., and Rowell, W.F., 1982. Petrology, geochemistry, and economic

potential of the Nipissing Diabase, Grant 100. In Geoscience Research Grant program, Summary of Research 1981-1982. E.G. Pye (ed). Ontario Geological Survey, Miscellaneous paper 103, p. 43-57.

Fitton, J.G., Larsen, L.M., Saunders, A.D., Hardarson, B.S., and Kempton, P.D., 2000.

Palaeogene continental to oceanic magmatism on the SE Greenland continental margin at 63°N: a review of the results of ocean drilling program Legs 152 and 163. Journal of Petrology, v.41, p. 951-966.

Fitton, J.G., Saunders, A.D., Norry, M.J., Hardarson, B.S., and Taylor, R.N., 1997.

Thermal and chemical structure of the Iceland plume. Earth and Planetary Science Letters, v.153, p. 197-208.

456

Foley, S.F., Tiepolo, M., and Vannucci, R., 2002. Growth of early continental crust controlled by melting of amphibolite in subduction zones. Nature, v.417, p. 837-840.

Fralick, P.W. and Miall, A.D. 1989. Sedimentology of the Lower Huronian Supergroup

(Early Proterozoic), Elliot Lake area, Ontario, Canada. Sedimentary Geology, 63, p. 127-153.

Francis, D., 2003. Cratonic mantle roots, remnants of a more chondritic Archean mantle?

Lithos, v.71, p. 135-152. Frarey, M.J., Loveridge, W.D., and Sullivan, R.W., 1982. A U-Pb zircon age for the

Creighton granite, Ontario. In Rb-Sr and U-Pb Isotopic Age Studies, Report 5. Current Research, Part C. Geological Survey of Canada, Paper 82-1C, p. 129-132.

Gates, B.I., 1991. Sudbury mineral occurrence study. Ontario Geological Survey, Open

File Report 5771, 235 pp. Ginn, R.M., 1965. Nairn and Lorne Townships. Ontario Department of Mines,

Geological Report No. 35, 46 pp. Goldschmidt, V.M., 1954. Geochemistry. Clarendon Press, Oxford, 730 pp. Goldschmidt, V.M., 1937. The principles of distribution of chemical elements in minerals

and rocks. Chemical Society of London Journal, pt. 1, p. 655-673. Grieve, R.A.F., 1994. An impact model of the Sudbury Structure. In Proceedings of the

Sudbury-Noril'sk symposium. P.C. Lightfoot and A.J. Naldrett (eds). Ontario Geological Survey, Special Volume 5, p. 119-132.

Halls, H.C., 1988. The Early Proterozoic Matachewan Dike Swarm, Canada: regional

variations in paleomagnetism and alteration and their possible geological significance. Abstract IGCP-257, International Symposium on Mafic Dikes and Related Magmatism, University of Lund, Sweden.

Hamlyn, P.R. and Keays, R. R., 1988. Geochemical criteria for platinum metals

exploration. Final report on project P228 to the Australian Mineral Industries Research Association, 215 pp.

Hamlyn, P.R., and Keays, R.R., 1986. Sulphur saturation and second-stage melts:

Application to the Bushveld Platinum Metal Deposits. Economic Geology, v.81, p. 1431-1445.

457

Hamlyn, P.R. and Keays, R.R., 1979. Origin of chromite compositional variation in the Panton Sill, Western Australia. Contributions to Mineralogy and Petrology, v.69, p. 75-82.

Hamlyn, P.R., Keays, R.R., Cameron, W.E., Cawford, A.J., and Waldron, H.M., 1985.

Precious metals in magnesian, low-Ti lavas: Implications for metallogenesis and sulphur saturation in primary magmas. Geochemica Cosmochimica Acta, v.9, p. 1797-1811.

Hanson, G.N. and Malhotra, R., 1971. K-Ar ages of mafic dikes and evidence for low-

grade metamorphism in northeastern Minnesota. Geological Society of America Bulletin, v.82, p. 1107-1114.

Harron, G.A., 2000. Summary report on Brunne/Stringer option, Curtin Township,

Ontario. Technical report for Macdonald Mines Exploration Ltd., 37 pp. Heaman, L.M., 1997. Global mafic magmatism at 2.45 Ga: Remnants of an ancient large

igneous province? Geology, v.25, p. 299-302. Heaman, L.M., 1989. U-Pb dating of mafic dyke swarms: what are the options?

International Association on Volcanology and Chemistry of the Earth’s Interior, Congress Abstracts. New Mexico Bureau of Mines and Minerals Resource Bulletin, v.131, p. 125.

Heaman, L.M., 1988. A precise U-Pb zircon age for a Hearst Dike. In Program with

Abstracts, Annual Meeting Geological Association of Canada-Mineralogical Association of Canada, v.13, p. A53.

Henderson, P., 1984. Rare Earth Element Geochemistry: Developments in Geochemistry

2. Elsevier Science Publishers B.V., New York. 510 pp. Hickey, R.L. and Frey, F.A., 1982. Geochemical characteristics of boninite series

volcanics: implications for their source. Geochimica et Cosmochimica Acta, v.46, p. 2099-2115.

Hoatson, D.M. and Keays, R.R., 1989. Formation of platiniferous sulphide horizons by

crystal fractionation and magma mixing in the Munni Munni Layered intrusion, West Pilbara Block, Western Australia. Economic Geology, v.84, p.1775-1804.

Hoffman, P.F. 1989. Precambrian Geology and tectonic history of North America: In The

Geology of North America-An Overview. Geological Society of America, Decade of North American Geology, Volume A, p. 447-512.

Holm, D.K., Schneider, D.A., O'Boyle, C., Hamilton, M.A., Jercinovic, M.J. and

Williams, M.L. 2001. Direct timing constraints on Paleoproterozoic metamorphism, southern Lake Superior region: results from SHRIMP and EMP

458

U-Pb dating of metamorphic monazites. Geological Society of America, Abstracts with Program, v.33, no. 6, p. A-401.

Hriskevich, M.E., 1968. Petrology of the Nipissing Diabase Sill of the Cobalt Area,

Ontario, Canada. Geological Society of America Bulletin, v.79, p. 1387-1404. Hrominchuk, J., 2000. Geology, stratigraphy, geochemistry, and copper-nickel-platinum

group element mineralization in the River valley intrusion: In Summary of Field Work and Other Activities 2000. Ontario Geological Survey, Open File Report 6032, p. 29-1 to 29-11.

Iljina, M., 1994. The Portimo Layered Igneous Complex - with emphasis on diverse

sulphide and platinum-group element deposits. Department of Geology, University of Oulu, Finland, Acta Univ. Oul. A 258, 158 pp.

Iljina, M. and Hanski, E., 2002. Multimillion-ounce PGE deposits of the Portimo Layered

Igneous Complex, Finland. In 9th International Platinum Symposium Extended Abstracts. A. Boudreau (ed). 21-25 July, 2002, Billings Montana, USA, 4 pp.

Innes, D.G., 1977. Proterozoic volcanism in the Southern Province of the Canadian

Shield. unpublished MSc thesis, Laurentian University, Sudbury, Ontario, 150 pp.

Innes, D.G. and Colvine, A.C., 1979. Metallogenic development of the eastern part of

the Southern Province of Ontario. In Summary of Field Work, 1979. Ontario Geological Survey, Miscellaneous Paper 90, p. 184-189.

Irvine, T.N., 1982. Terminology for layered intrusions. Journal of Petrology, 23, p. 127-

162. Irvine, T.N. and Baragar, W.R.A., 1971. A guide to the chemical classification of the

common volcanic rocks. Canadian Journal of Earth Sciences, v.8, p. 523-548. Jackson, S.E., Fryer, B.J., Gosse, W., Healey, D.C., Longerich, H.P., and Strong, D.F.,

1990. Determination of the precious metals in geological materials by inductively coupled plasma-mass spectrometry (ICP-MS) with Nickel Sulphide fire-assay collection and tellurium co-precipitation. Chemical Geology, v.83, p. 119-132.

Jambor, J.L., 1971. The Nipissing Diabase. The Canadian Mineralogist, 11, p. 34-75. James, R.S., 2004. Petrology of mineralized and barren rock samples from the Dana,

Lismer’s Ridge, Azen, and Razor Zones of the River Valley intrusion, Dana Township, Sudbury Mining Division, Ontario. Consultants report prepared for Pacific North West Capital Corp. and Anglo American Platinum Corporation Limited, February 25th, 2004.

459

James, R.S. and Born, P., 1985. Geology and geochemistry of the East Bull Lake

intrusion, District of Algoma, Ontario. Canadian Journal of Earth Sciences, v.22, p. 968-979.

James, R.S., Easton, R.M., Peck, D.C., and Hrominchuk, J.L., 2002a. The East Bull Lake

intrusive suite: remnants of a ~2.48 Ga large igneous and metallogenic province in the Sudbury area of the Canadian Shield. Economic Geology, v.96, p.1577-1606.

James, R.S., Jobin-Bevans, S., Easton, R.M., Wood, P., Hrominchuk, Keays, R.R. and

Peck, D.C., 2002b. Platinum-group element mineralization in Paleoproterozoic basic intrusions in Central and northeastern Ontario, Canada. In The Geology, Geochemistry, Mineralogy and Mineral Beneficiation of Platinum-Group Elements. L.J. Cabri (ed). Canadian Institute of Mining, Metallurgy and Petroleum, Special Volume 54, p. 339-365.

Jolly, W.T., 1987. Lithophile elements in Huronian low-Ti continental tholeiites from

Canada and evolution of the Precambrian mantle. Earth and Planetary Science Letters, v.85, p. 401-415.

Jobin-Bevans, L.S., Keays, R.R., and MacRae, N.D., 1999. Project 97012. Cu-Ni-PGE in

Nipissing Diabase: Results from surface and core samples. In Summary of Field Work and Other Activities, 1999. Ontario Geological Survey, Open File Report 6000, p. 33-1-33-5.

Jobin-Bevans, L.S., MacRae, N.D., and Keays, R.R., 1998. Cu-Ni-PGE Potential of the

Nipissing Diabase. In Summary of Field Work and Other Activities, 1998. Ontario Geological Survey, Miscellaneous Paper 169, p. 220-223.

Johannsen, A., 1931. A Descriptive Petrography of the Igneous Rocks, Volume 1 (p. 88-

92). University of Chicago Press, Chicago, 267 pp. Kamineni, D.C., 1986. A petrochemical study of calcic amphiboles from the East Bull

Lake anorthosite-gabbro layered complex, District of Algoma, Ontario. Contributions to Mineralogy and Petrology, v.93, p.471-481.

Kamo, S.L., Krogh, T.E., and Kumarapeli, P.S., 1995. Age of the Grenville dyke swarm,

Ontario-Quebec: Implications for the timing of Iapetan Rifting. Canadian Journal of Earth Sciences, v.32, p. 273-280.

Karlstrom, K.E. and Houston, R.S., 1984. The Cheyenne Belt: Analysis of a Proterozoic

suture in southern Wyoming. Precambrian Research, v.25, p. 415-446. Karlstrom, K.E., Flurkey, A.E., and Houston, R.S., 1983. Stratigraphy and depositional

setting of the Proterozoic Snowy Pass Supergroup, southeastern Wyoming:

460

Record of an early Proterozoic Atlantic-type cratonic margin. Geological Society of America Bulletin, v.94, p. 1257-1274.

Keays, R.R., 1995. The role of komatiitic and picritic magmatism and S-saturation in the

formation of ore deposits. Lithos, v.34, p. 1-18. Keays, R.R., 1982. Palladium and iridium in komatiites and associated rocks: application

to petrogenetic problems. In Komatiites. N.T. Arndt and E.G. Nisbet (eds). Allen and Unwin, Hemel Hempstead, p. 435-457.

Keays, R.R. and Lightfoot, P.C., 2004. Formation of Ni-Cu-Platinum Group element

sulphide mineralisation in the Sudbury Impact Melt Sheet. Mineralogy and Petrology, online publication, September 10, 2004, 42 pp.

Keays, R. R., and others, 2002. Exploration for Platinum Group Element Deposits in

Mafic and Ultramafic Rocks. MRDU (UBC) Short Course on PGE deposits, Vancouver, January 27-28, 2002.

Keays, R. R., Cawthorn, G., Lesher, C. M., and Groves, D. I., 2004. Platinum deposits

and models: conventional and unconventional. Workshop 3 at SEG 2004, October 2, 2004, Perth, Australia.

Keays, R.R., Nickel, E.H., Groves, D.I., and McGoldrick, P.J., 1982. Iridium and

palladium as disciminants of volcanic-exhalative, hydrothermal, and magmatic nickel sulphide mineralization. Economic Geology, v.77, p. 1535-1547.

Kerr, A., 2001. The calculation and use of sulphide metal contents in the study of

magmatic ore deposits: a methodological analysis. Exploration and Mining Geology, v.10, p. 289-301.

Krogh, T.E. 1994. Precise U-Pb ages for Grenvillian and pre-Grenvillian thrusting of

Proterozoic and Archean metamorphic assemblages in the Grenville Front tectonic zone, Canada. Tectonics, v.13, p. 963-982.

Krogh, T.E., Davis, D.W., and Corfu, F., 1984. Precise U-Pb zircon and baddeleyite ages

for the Sudbury Structure. In Geology and Ore Deposits of the Sudbury Structure, E.G. Pye, A.J. Naldrett, and P.E. Giblin (eds). Ontario Geological Survey, Special Volume 1, p. 431-446.

Krogh, T.E., Corfu, F., Davis, D.W., Dunning, G.R., Heaman, L.M., Kamo, S.L.,

Machado, N., Greenhough, J.D., and Nakamura, N., 1987. Precise U-Pb isotopic ages of diabase dykes and mafic to ultramafic rocks using trace amounts of baddeleyite and zircon. In Mafic Dyke Swarms. H.C. Halls and W.F. Fahrig (eds). Geological Association of Canada Special paper 34, p. 147-152.

461

Lambert, D.D., Foster, J.G., Frick, L.R., Ripley, E.M., and Zientek, M.L., 1998. Geodynamics of magmatic Cu-Ni-PGE sulphide deposits: New insights from the Re-Os isotope system. Economic Geology, v.93, p.121-136.

Langmuir, C.H., Klein, E.M., and Plank, T., 1992. Petrological systematics of mid-ocean

ridge basalts: Constraints on melt generation beneath ocean ridges. In Mantle flow and melt generation at mid-ocean ridges. J.P. Morgan, D.K. Blackman, and J.M. Sinton (eds). Geophysical monographs 71, p. 83-275.

LeMaitre, R.W., 1989. A Classification of Igneous Rocks and Glossary of Terms.

Blackwell Scientific Publications, Oxford, U.K., 193 pp. Lesher, C.M. and Burnham, O.M., 1999. Mass balance and mixing in magmatic sulphide

systems. In Dynamic processes in magmatic ore deposits and their application in mineral exploration. R.R. Keays, C.M. Lesher, P.C. Lightfoot, and C.E.G. Farrow (eds). Geological Association of Canada, Short Course Volume 13, p. 413-449.

Lesher, C.M., Burnham, O.M., Keays, R.R., Barnes, S.J., and Hulbert, L., 2001. Trace-

element geochemistry and petrogenesis of barren and ore-associated komatiites. Canadian Mineralogist, v.39, p. 673-696.

Li, C., Ripley, E.M., and Naldrett, A.J., 2003. Compositional variations of olivine and

sulphur isotopes in the Noril’sk and Talnakh intrusions, Siberia: Implications for ore-forming processes in dynamic magma conduits. Economic Geology, v.98, p. 69-86.

Lightfoot, P. C. and Keays, R. R., 2004. Siderophile and chalcophile metal variations in

flood basalts from the Siberian Trap, Noril’sk Region: Implications for the origin of the Ni-Cu-PGE sulfide ores. Economic Geology (in press).

Lightfoot, P.C. and Naldrett, A.J., 1996. Petrology and geochemistry of the Nipissing

Gabbro: Exploration strategies for nickel, copper, and platinum group elements in a large igneous province. Ontario Geological Survey, Study 58, 81 pp.

Lightfoot, P.C. and Naldrett, A.J., 1989. Assimilation and crystallization in basic magma

chambers: trace-element and Nd-isotopic variations in the Kerns sill, Nipissing diabase province, Ontario. Canadian Journal of Earth Sciences, v.26, p. 737-754.

Lightfoot, P.C., DE Souza, H., and Doherty, W., 1993. Differentiation and source of the

Nipissing Diabase intrusions, Ontario, Canada. Canadian Journal of Earth Sciences, 30, p. 1123-1140.

Lightfoot, P.C., DE Souza, H., and Doherty, W., 1991. Mineral potential of the Nipissing

Diabase: some geochemical considerations. In Summary of Fieldwork and Other

462

Activities, 1991. Ontario Geological Survey, Miscellaneous Paper 157, p. 237-246.

Lightfoot, P.C., Keays, R.R. and Doherty, W., 2000. Chemical evolution and origin of

nickel sulphide mineralization in the Sudbury Igneous Complex, Ontario, Canada. Economic Geology, v.96, p. 1855-1875.

Lightfoot, P.C., Naldrett, A.J., and Hawkesworth, C.J., 1984. The geology and

geochemistry of the Waterfall Gorge section of the Insizwa Complex with particular reference to the origin of the Nickel sulfide deposits. Economic Geology, v.79, p. 1857-1879.

Lightfoot, P.C., Conrod, D., Naldrett, A.J. and Evensen, N.M., 1987. Petrologic,

Chemical, Isotopic, and Economic-Potential Studies of the Nipissing Diabase. Grant 230, p. 4-26. In Geoscience Research Grant Program, Summary of Research 1986-1987. V.G. Milne (ed). Ontario Geological Survey, Miscellaneous Paper 136, 241 pp.

Lightfoot, P.C., Conrod, D., Naldrett, A.J., and Evensen, N.M., 1986. Petrologic,

Chemical, Isotopic, and Economic Potential Studies of the Nipissing Diabase. Grant 230, p. 87-106. In Geoscience Research Grant Program, Summary of Research 1985-1986. V.G. Milne (ed). Ontario Geological Survey, Miscellaneous Paper 130, 235 pp.

Lodders, K. and Fegley, B., 1998. The Planetary Scientist’s Companion. Oxford

University Press, Oxford, UK, p. 314-316. Lovell, H.L., and Caine, T.W., 1970. Lake Timiskaming Rift Valley. Ontario

Department of Mines, Miscellaneous Paper 39, 16 pp. Lumbers. S.B., 1973. River Valley area. Ontario Division of Mines. Preliminary Map

P.844 (scale 1:63 360). Lumbers, S.B., 1971. River Valley area. In Summary of Field Work, 1971. Ontario

Department of Mines and Northern Affairs. Miscellaneous Paper 49, p. 90-97. Lumbers, S.B., 1978. Geology of the Grenville Front Tectonic Zone in Ontario. In

Toronto ’78, Field Trips Guidebook. Geological Society of America-Geological Association of Canada-Mineralogical Association of Canada, p. 347-361.

Ma, C., Goreva, J.S., and Rossman, G.R., 2001. Colored varieties of quartz arising from

inclusions. In Abstracts from Eleventh Annual Goldschmidt Conference, May 20-24, Virginia, USA.

463

Maier, W.D., Arndt, N.T., and Curl, E.A., 2000. Progressive crustal contamination of the Bushveld Complex: evidence from Nd isotopic analyses of the cumulate rocks. Contributions to Mineralogy and Petrology, v140, p.316-327.

Maier, W.D., Barnes, S.-J., and de Waal, S.A., 1998. Exploration for magmatic Ni-Cu-

PGE sulphide deposits: a review of recent advances in the use of geochemical tools, and their application to some South African ores. South African Journal of Geology, v.101, p. 237-253.

Maier, W.D., Barnes, S.-J., Teigler, B., De Klerk, W.J., and Mitchell, A.A., 1996. Cu/Pd

and Cu/Pt of silicate rocks in the Bushveld Complex: Implications for platinum-group element exploration. Economic Geology, v.91, p. 1151-1158.

Mavrogenes, J.A., and O’Neill, H.S., 1999. The relative effects of pressure, temperature

and oxygen fugacity on the solubility of sulfide in mafic magmas. Geochimica et Cosmochimica Acta, v.63, p. 1173-1180.

McCrank, G.F.D., Kamineni, D.C., Ejeckam, R.B., and Sikorsky, R., 1989. Geology of

the East Bull Lake gabbro-anorthosite pluton, Algoma District, Ontario, Canadian Journal of Earth Sciences, v.26, p. 357-375.

McDonough, W.F. and Sun, S.-S., 1995. The composition of the Earth. Chemical

Geology, v.120, p. 223-253. Meyer, G., Cosec, M., Grabowski, G.P.B., Guindon, D.L., Hailstone, M., Stephenson, C.,

Wallace, L.M., Debicki, R., and Yule, G., 2001. Report of Activities, 2000, Resident Geologist Program, Kirkland Lake Regional Resident Geologist Report: Kirkland Lake and Sudbury Districts, Ontario Geological Survey, Open File Report 6051, p. 15-18.

Meyer, G., Cosec, M., Grabowski, G.P.B., Guindon, D.L., Chaloux, E.C.,, and Charette,

M., 2000. Report of Activities, 1999, Resident Geologist Program, Kirkland Lake Regional Resident Geologist Report: Kirkland Lake and Sudbury Districts, Ontario Geological Survey, Open File Report 6007, p. 22-27.

Meyn, H.D., 1977. Geology of Afton, Scholes, MacBeth, and Clement Townships,

District of Sudbury and Nipissing. Ontario Geological Survey, Report 170, 77 pp.

Miller, W.G., 1911. Notes on the Cobalt Area. Engineering and Mining Journal, 92, p.

645-649. Miyashiro, A., 1978. Nature of alkalic volcanic rock series. Contributions to Mineralogy

and Petrology, v.66, p. 91-104.

464

Momme, P., Tegner, C., Brooks, C.K., and Keays, R.R., 2002a. The behaviour of platinum-group elements in basalts from the East Greenland rifted margin. Contributions to Mineralogy and Petrology, v143, p. 133-153.

Momme, P., Tegner, C., and Brooks, C.K., 2002b. On the Formation of Platinum Group

Element–Rich Continental Flood Basalt and the Platinova Reefs of the Skaergaard Intrusion. In 9th International Platinum Symposium Extended Abstracts, A. Boudreau (ed), 21-25 July, 2002, Billings Montana, USA, 4 pp.

Momme, P., Oskarsson, N., and Keays R.R., 2002c. Platinum-group elements in the

Icelandic rift system: melting processes and mantle sources beneath Iceland. Chemical Geology, v.196, p. 209-234.

Moore, E.S., 1929. Ore deposits nears the north shore of Lake Huron. Ontario

Department of Mines Annual Report, 1929, v.38, Pt.7, p. 1-51. Morris, W.A., 1977. Paleomagnetism of the Gowganda and Chibougamau Formations:

evidence for 2,200-m.y.-old folding and remagnetization event of the Southern Province. Geology, 5, p. 137-140.

Naldrett, A.J., 1981. Platinum-group element deposits. In Platinum-group elements:

Mineralogy, geology, recovery. L.J. Cabri (ed). Canadian Institute of Mining and Metallurgy, CIM Special Volume 23, p. 197-231.

Naldrett, A.J. and Lightfoot, P.C., 1993. Ni-Cu-PGE ores of the Noril’sk Region Siberia:

a model for gigantic magmatic sulphide deposits associated with flood basalts. Society of Economic Geologists. B.H. Whiting, C.J. Hodgson, and R. Mason (eds). Special Volume No. 2, p. 81-124.

Naldrett, A.J., Asif, M., Krstic, S., and Li, C., 2000. The Composition of Mineralization

at the Voisey’s Bay Ni-Cu Sulfide Deposit, with Special Reference to Platinum-Group Elements, Economic Geology, v.95, p. 845-866

Naldrett, A.J., Hoffman, E.L., Green, A.H., Chou, C.-L., Naldrett, S.R., and Alcock,

R.A., 1979. The composition of Ni-sulfide ores, with particular reference to their content of PGE and Au. Canadian Mineralogist, v.17, p. 403-416.

Noble, S.R., and Lightfoot, P.C., 1992. U-Pb Baddeleyite ages for the Kerns and

Triangle Mountain Intrusions, Nipissing Diabase, Ontario. Canadian Journal of Earth Sciences, v.29, p. 1124-1129.

Nykänen, V.M., Vuollo, J.I., Liipo, J.P., and Piirainen, T.A., 1994. Transitional (2.1 Ga)

Fe-tholeiitic-tholeiitic magmatism in the Fennoscandian Shield signifying lithospheric thinning during Palaeoproterozoic extensional tectonics. Precambrian Research, v.70, p.45-65.

465

Ontario Geological Survey (OGS), 1979. Sault Ste. Marie-Elliot Lake Map 2419 (1:253,440 scale). Geological Compilation Series, Algoma, Manitoulin and Sudbury Districts.

Ontario Geological Survey (OGS), 1977. Sudbury-Cobalt Map 2361 (1:253,440 scale).

Geological Compilation Series, Algoma, Manitoulin, Nipissing, Parry Sound, Sudbury and Timiskaming District.

Osmani, I.A., 1991. Proterozoic Mafic Dike Swarms in the Superior Province of Ontario.

In Geology of Ontario. P.C. Thurston, H.R. Williams, R.H. Sutcliffe, and G.M. Stott (eds). Ontario Geological Survey, Special Volume 4, Part 1, p. 661-681.

Patterson, J.G. and Heaman, L.M., 1991. New geochronologic limits on the depositional

age of the Hurwitz Group, Trans-Hudson hinterland, Canada. Geology, v.19, p. 1137-1140.

Peach, C.L. and Mathez, E.A., 1996. Constraints on the formation of platinum-group

element deposits in igneous rocks. Economic Geology, v.91, p. 439-450. Peach, C.L., Mathez, E.A., and Keays, R.R., 1990. Sulfide melt-silicate melt distribution

coefficients for noble metals and other chalcophile elements as deduced from MORB: Implications for partial melting. Geochimica et Cosmochimica Acta, v. 54, p. 3379-3389.

Peach, C.L., Mathez, E.A., Keays, R.R., and Reeves, S.J., 1994. Experimentally-

determined sulphide-silicate melt partition coefficients for iridium and palladium. Chemical Geology, v.117, p. 361-377.

Pearce, J.A. and Cann, J.R., 1993. Tectonic setting of basic volcanic rocks determined

using trace element analyses. Earth and Planetary Science Letters, v.19, p. 290-300.

Pearce, J.A. and Norry, M.J., 1979. Petrogenetic implications of Ti, Zr, Y and Nb

variations in volcanic rocks. Contributions to Mineralogy and Petrology, v69, p. 33-47.

Peck, D.C., James, R.S., and Chubb, P.T., 1993a. Geological environments for PGE-Cu-

Ni mineralization in the East Bull Lake Gabbro-Anorthosite Intrusion, Ontario. Exploration and Mining Geology, v.2, p. 85-104.

Peck, D.C. and James, R.S., 1990. Mineral potential studies of mafic and ultramafic

intrusive rocks in the Elliot Lake area. In Summary of Field Work and Other Activities, Ontario Geological Survey, Miscellaneous paper 151, p. 62-66.

466

Peck, D.C. and Keays, R.R., 1990. Insights into the behaviour of precious metals in primitive, S-undersaturated magmas: Evidence from the Heazlewood River Complex, Tasmania. Canadian Mineralogist, v.28, p. 553-577.

Peck, D.C., Keays, R.R., and Ford, R.J., 1992. Direct crystallization of refractory

platinum-group element alloys from boninitic magmas: evidence from western Tasmania. Australian Journal of Earth Sciences, v39, p.373-387.

Peck, D.C., James, R.S., Chubb, P.T., Prevec, S.A. and Keays, R.R., 1995. Geology,

Metallogeny and Petrogenesis of the East Bull Lake Intrusion, Ontario. Ontario Geological Survey, Open File Report 5923, 117 pp.

Peck, D.C., Keays, R.R., James, R.S., Chubb, P.T., and Reeves, S.J., 2001. Controls on

the formation of contact-type platinum-group element mineralization in the East Bull Lake Intrusion: Economic Geology, v.96, p. 559-581.

Peck, D.C., James, R.S., Chubb, P.T., Keays, R.R., Reeves, S.J., Lightfoot, P.C., and

Kamineni, D.C., 1993b. Precious-metal, chalcophile-element and rare-earth element Geochemistry of the Bull Lake Area, Districts of Algoma and Sudbury, Ontario. Ontario Geological Survey, Open File Report 5849, 94 pp.

Phemister, T.C., 1939. Notes on several properties in the District of Sudbury. Ontario

Department of Mines, v.48, p.16-28. Piercey, S.J., Murphy, D.C., Mortensen, J.K., and Paradis, S., 2001. Boninitic

magmatism in a continental margin setting, Yukon-Tanana terrane, southeastern Yukon, Canada. Geology, v.29, p.731-734.

Premo, W.R. and Van Schmus, W.R., 1989. Zircon geochronology of Precambrian rocks

in southeastern Wyoming and northern Colorado. In Proterozoic Geology of the Southern Rocky Mountains. J.A. Grambling and B.J. Tewksbury (eds). Geological Society of America Special Paper 235, p. 13-32.

Prendergast, M.D. and Keays, R. R., 1989. Controls of platinum-group element

mineralization and the origin of the PGE-rich Main Sulphide Zone in the Wedza Subchamber of the Great Dyke, Zimbabwe: implications for the genesis of, and exploration for, stratiform PGE mineralization in layered intrusions: In Magmatic Sulphides - the Zimbabwe Volume. M.D. Prendergast and M.J. Jones (eds). Institute of Mining and Metallurgy, London, p. 43-69.

Prevec, S.A., 1993. An isotopic, geochemical and petrographic investigation of the

genesis of early Proterozoic mafic intrusions and associated volcanics near Sudbury, Ontario. unpublished Ph.D. thesis, University of Alberta, Edmonton, Alberta, 223 pp.

467

Pye, E.G., Naldrett, A.J., and Giblin, P.E (eds), 1984. Geology and Ore Deposits of the Sudbury Structure. Ontario Geological Survey Special Volume 1, 603 pp.

Reeves, S.J. and Keays, R.R., 1995. The platinum group element geochemistry of the

Bucknalla Layered Complex, central Queensland. Australian Journal of Earth Sciences, v.42, p. 187-201.

Rice, A., 1997. A model for PGE enrichment due to the splitting of freezing magma

chambers by suspended crystal loads. Exploration and Mining Geology, v.6, p. 129-137.

Richardson, T. and Burnham, O.M., 2002. Precious metal analysis at the Geoscience

Laboratories: results from the new low-level analytical facility. In Summary of Field Work and Other Activities, 2002, Ontario Geological Survey, Open File Report 6100, p. 35-1-35-5.

Riller, U., Schwerdtner, W.M., Halls, H.C., and Card, K.D., 1999. Transpressive

tectonism in the eastern Penokean orogen, Canada: consequences for Proterozoic crustal kinematics and continental fragmentation. Precambrian Research, v.93, p. 51–70.

Rollinson, H., 1993. Using Geochemical Data: Evaluation, Presentation, Interpretation.

Longman Group UK Limited, 352 pp. Roscoe, S.M., 1990. The reappearance of the Huronian in Wyoming. In Institute on

Lake Superior Geology Proceedings, 36th Annual Meeting, Thunder Bay, 1990, Part 1, Abstracts, p. 93.

Roscoe, S.M., 1973. The Huronian Supergroup, a paleoaphebian succession showing

evidence of atmospheric evolution. In Huronian stratigraphy and sedimentation, G.M. Young (ed). Geological Association of Canada, Special Paper 12, p. 31-47.

Roscoe, S.M., and Card, K.D., 1993. The reappearance of the Huronian in Wyoming:

Rifting and drifting of ancient continents. Canadian Journal of Earth Sciences, 30, p. 2475-2480.

Rowell, W.F., 1984. Platinum group elements and gold in the Wanapitei Nipissing-type

intrusion, northeastern Ontario. unpublished M.Sc. thesis, The University of Western Ontario, London, Ontario, 87 pp.

Rowell, W.F. and Edgar, A.D., 1986. Platinum-group element mineralization in a

hydrothermal Cu-Ni sulphide occurrence, Rathbun Lake, Northeastern Ontario. Economic Geology, v81, p. 1272-1277.

468

Rousell, D.H., Gibson, H.L., and Jonasson, I.R., 1997. The tectonic, magmatic and mineralization history of the Sudbury Structure. Exploration and Mining Geology, v.6, p. 1-22.

Sage, R. P., 1991. Alkalic rock, Carbonatite and Kimberlite complexes in Ontario. In

Geology of Ontario. P.C. Thurston, H.R. Williams, R.H. Sutcliffe, and G.M. Stott (eds). Ontario Geological Survey, Special Volume 4, Part 1, p. 683-709.

Seifert, K.E., Peterman, Z.E., and Thieben, S.E., 1992. Possible crustal contamination of

Midcontinent Rift igneous rocks: examples from the Mineral lake intrusions, Wisconsin. Canadian Journal of Earth Sciences, v.29, p. 1140-1153.

Seitz, H.-M. and Keays, R.R., 1997. Platinum group element segregation and

mineralization in a noritic ring complex formed from Proterozoic Siliceous High Magnesium Basalt magmas in the Vestfold Hills, Antarctica. Journal of Petrology, v.38, p. 703-725.

Shellnutt, J.G., 2000. The petrogenesis of the Sudbury Dyke Swarm, Ontario, Canada.

unpublished Undergraduate thesis, Department of Earth Sciences, The University of Western Ontario, London, Ontario, 304 pp.

Schiffries, C.M. and Rye, D.M., 1989. Stable isotope systematics of the Bushveld

Complex: I. Constraints of magmatic processes in layered intrusions. American Journal of Science, v.289, p. 841-875.

Siemiatkowska, K.M. and Martin, R.F., 1975. Fenitization of Mississagi Quartzite,

Sudbury Area, Ontario. Geological Society of America Bulletin, v.86, p. 1109-1122.

Schandl, E.S., Gorton, M.P. and Davis, D.W., 1994. Albitization at 1700+/-2 Ma in the

Sudbury-Wanapitei Lake area, Ontario. Canadian Journal of Earth Sciences, v.31, p. 597-607.

Shaw, C.S.J., Young, G.M., and Fedo, C.M., 1999. Sudbury-type breccias in the

Huronian Gowganda Formation near Whitefish Falls, Ontario: products of diabase intrusion into incompletely consolidated sediments. Canadian Journal of Earth Sciences, v.36, p. 1435-1448.

Smithies, R.H., Champion, D.C., and Sun, S.-S., 2004. Evidence for early LREE-

enriched mantle source regions: diverse magmas from the c. 3.0 Ga Mallina Basin, Pilbara Craton, NW Australia. Journal of Petrology, v.45, p.1515-1537.

Stockwell, C.H., 1982. Proposals for time classification and correlation of Precambrian

rocks and events in Canada and adjacent areas of the Canadian Shield. Geological Survey of Canada, Paper 80-19, 135 pp.

469

Sun, S.-S. and McDonough, W.F., 1989. Chemical and isotopic systematics of oceanic basalts: implications for mantle composition and process. In Magmatism in the Ocean Basins. A.D. Saunders and M.J. Norry (eds). Geological Society Special Publication No. 42, p. 313-345.

Sun, S.-S., and Nesbitt, R.W., 1978. Petrogenesis of Archaean ultrabasic and basic

volcanics: Evidence from Rare Earth elements. Contributions to Mineralogy and Petrology, v.65, p.301-325.

Sun, S.-S., Wallace, D. A., Hoatson, D. M., Glikson, A. K. and Keays, R. R., 1991. Use

of geochemistry as a guide to platinum group element potential of mafic-ultramafic rocks: Examples from the West Pilbara and Halls Creek Mobile Zone, Western Australia: Precambrian Research, v.50, p. 1-35.

Sutcliffe, R.H., 1986. Petrology, mineral chemistry and tectonics of Proterozoic rift-

related igneous rocks at Lake Nipigon, Ontario. unpublished Ph.D. thesis, University of Western Ontario, London, Ontario, 325 pp.

Taylor, S.R. and McLennan, S.M., 1985. The Continental Crust: Its Composition and

Evolution. Blackwell, Oxford, 312 pp. Tegner, C., Lesher, C.E., Larsen, L.M., and Watt, W.S., 1998. Evidence from the rare-

earth element record of mantle melting for cooling of the Tertiary Iceland Plume. Nature, v.395, p. 591-594.

Tettelaar, T. 2000. Petrography and geothermobarometry of variably metamorphosed and

deformed leucogabbronorites of the River Valley intrusion, Grenville Province, Ontario; unpublished B.Sc. thesis, Carleton University, Ottawa, Ontario, 59 pp.

Theriault, R.D., Barnes, S.,-J., and Severson, M.J., 2000. Origin of Cu-Ni-PGE sulphide

mineralization in the Partridge River intrusion, Duluth Complex, Minnesota. Economic Geology, v.95, p. 929-943.

Thompson, J.F.H. and Naldrett, A.J., 1984. Sulphide-silicate reactions as a guide to Ni-

Cu-Co mineralization in central Maine, U.S.A. In Sulphide Deposits in Mafic and Ultramafic Rocks. D.L. Buchanan and M.J. Jones (eds). The Institution of Mining and Metallurgy, Proceedings of IGCP Projects 161 and 91, Third Nickel Sulphide Field Conference, Australia, p. 103-113.

Thompson, R.N., Morrison, M.A., Hendry, G.L., and Parry, S.J., 1984. An assessment of

the relative roles of crust and mantle in magma genesis: an elemental approach. Philosophical Transactions of The Royal Society of London, Series A, v.310, p. 549-590.

Thomson, JAS.E. and Card, K.D., 1963. Kelly and Davis Townships. Ontario

Department of Mines, Geological Report No. 15, 20 pp.

470

Thurston, P.C., 1991. Archean geology of Ontario: Introduction. In Geology of Ontario.

P.C. Thurston, H.R. Williams, R.H. Sutcliffe, and G.M. Stott (eds). Ontario Geological Survey, Special Volume 4, Part 1, p. 73-78.

Tomlinson, K.Y., 1996. The geochemistry and Tectonic setting of Early Precambrian

greenstone belts. unpublished Ph.D. thesis, University of Portsmouth, UK, 287 pp.

Tomlinson, K.Y., Bennett, G., Keays, R.R., and Thurston, P.C., 1999. The Thessalon

volcanic formation: Multiple pulses of magmatism in a continental rift environment. In GAC-MAC Joint Annual Meeting, Sudbury, 1999, Abstract Volume 24, p. 130.

van Breemen, O. and Davidson, A., 1988. Northeast extension of Proterozoic terranes of

mid-continental North America. Geological Society of America Bulletin, v.100, p. 630-638.

Van Schmus, W.R., 1975. On the age of the Sudbury Dike Swarm. Canadian Journal of

Earth Sciences, v.12, p. 1690-1692. Van Schmus, W.R., 1965. The geochronology of the Blind River-Bruce Mines area,

Ontario. Journal of Geology, 73, p. 755-780. Van Schmus, W.R., Wetherill, G.W., and Bickford, M.E., 1963. Rb-Sr age

determinations of the Nipissing diabase, north shore of Lake Huron, Ontario, Canada. Journal of Geophysical Research, v.68, p. 5589-5593.

Vogel. D.C., 1996. The Geology and geochemistry of the Agnew Intrusion: Implications

for the petrogenesis of early Huronian mafic igneous rocks in central Ontario, Canada. unpublished Ph.D. thesis, Laurentian University, Sudbury, Ontario, Volume I, 273 pp.

Vogel, D.C. and Keays, R.R., 1997. The petrogenesis and platinum-group element

geochemistry of the Newer Volcanic Province, Victoria, Australia. Chemical Geology, v.136, p.181-204.

Vogel, D. C., James, R. S., and Keays, R. R., 1998a. The early tectono-magmatic

evolution of the Southern Province: Implications for the Agnew Intrusion, Central Ontario, Canada. Canadian Journal of Earth Sciences, v.35, p. 854-870.

Vogel, D.C., Keays, R.R., James, R.S., and Reeves, S.J., 1999. The geochemistry and

petrogenesis of the Agnew Intrusion, Canada: A product of S-undersaturated, high-Al, low-Ti tholeiitic magmas. Journal of Petrology, v.40, p. 423-450.

471

Vogel, D.C., Vuollo, J.I., Alapieti, T.T., and James, R.S., 1998b. Tectonic, stratigraphic, and geochemical comparisons between ca. 2500-2440 Ma mafic igneous events in the Canadian and Fennoscandian Shields. Precambrian Research, v.92, p. 89-116.

Williams, H., Hoffman, P.F., Lewry, J.E., Monger, J.W.H., and Rivers, T., 1991.

Anatomy of North America: thematic portrayals of the continent. Tectonophysics, v.187, p. 117-134.

Wyman, D.A.(ed.), 1996. Trace Element Geochemistry of Volcanic Rocks: Applications

for Massive Sulphide Exploration. Short Course Notes Volume 12, Geological Association of Canada, Mineral Deposits Division, Winnipeg, 113 pp.

Young, G.M., 1995. The Huronian Supergroup in the context of a Paleoproterozoic

Wilson Cycle in the Great Lakes Region. In The Northern Margin of the Southern Province of the Canadian Shield, Program and Abstracts. The Canadian Mineralogist, v.33, p. 921-922.

Young, G.M., 1983. Tectono-sedimentary history of Early Proterozoic rocks of the

northern Great Lakes region. In Early Proterozoic Geology of the Great Lakes Region. L.G. Medaris (ed). Geological Society of America, Memoir 160, p. 15-32.

Young, G.M., 1973. Tillites and aluminous quartzites as possible time markers for

middle Precambrian (Aphebian) rocks of North America. In Huronian stratigraphy and sedimentation. G.M. Young (ed). Geological Association of Canada, Special Paper 12, p. 97-127.

Young, G.M., Long, D.G.F., Fedo, C.M., and Nesbitt, H.W., 2001. Paleoproterozoic

Huronian basin: Product of a Wilson Cycle punctuated by glaciations and a meteorite impact. Sedimentary Geology, v.141-142, p. 233-254.

Wetherill, G.W., Davis, G.L., and Tilton, G.R., 1960. Age measurements from the Cutler

Batholith, Cutler, Ontario. Journal of Geophysical Research, v.65, p. 2461-2466. Weyer, S., Munker, C., Rehkamper, M., and Mezger, 2002. Determination of ultra-low

Nb, Ta, Zr and Hf concentrations and chondritic Zr/Hf and Nb/Ta ratios by isotope dilution analyses with multiple collector ICP-MS. Chemical Geology, v.187, p. 295-313.

Windley, B.F., 1993. Uniformitarianism today; plate tectonics is the key to the past.

Journal of the Geological Society of London, v.150, Part 1, p. 7-19. Zindler, A. and S.R. Hart, 1986. Chemical geodynamics. Annual Review of Earth and

Planetary Sciences, v.14, p. 493-571.

472

Zolnai, A.I., Price, R.A., and Helmstaedt, H., 1984. Regional cross-section of the Southern Province adjacent to Lake Huron, Ontario: implications for the tectonic significance of the Murray Fault Zone. Canadian Journal of Earth Sciences, v.21, p. 447-456.

473

APPENDIX 1:

SPECIMEN DESCRIPTIONS, WHOLE-ROCK AND CIPW DATA

A) Lower Limits of Detection 474

B) Analytical Method Codes and Explanatory Notes 476

C) Nipissing Gabbro Intrusions – Geochemical Data 477

D) Nipissing Gabbro Intrusions - CIPW Normative Calculations 501

E) River Valley Intrusion - Matrix and Fragment Geochemical Data 523

F) River Valley Intrusion – CIPW Normative Calculations 527

G) River Valley Intrusion – Group-1 Data (RV00-22 core samples) 530

H) River Valley Intrusion – Group-2 Data (RV00-22 core samples) 534

474

(A) LOWER LIMITS OF DETECTION

Laboratory

Element Unit Method* Geo Labs Accurassay ACTLABS Chemex XRAL

SiO2 wt% WD-XRF 0.01 0.01 0.01 0.01 0.01 TiO2 wt% WD-XRF 0.01 0.001 0.005 0.01 0.01 Al2O3 wt% WD-XRF 0.01 0.01 0.01 0.01 0.01 Fe2O3 wt% WD-XRF 0.01 0.01 0.01 0.01 0.01 MnO wt% WD-XRF 0.01 0.01 0.01 0.01 0.01 CaO wt% WD-XRF 0.01 0.01 0.01 0.01 0.01 MgO wt% WD-XRF 0.01 0.01 0.01 0.01 0.01 Na2O wt% WD-XRF 0.01 0.02 0.01 0.01 0.01 K2O wt% WD-XRF 0.01 0.02 0.01 0.01 0.01 P2O5 wt% WD-XRF 0.01 0.02 0.01 0.01 0.01 LOI wt% WD-XRF 0.05 0.01 0.01 0.01 0.01 Be ppm ICP-AES 3 0.1 1 0.1 0.5 Co ppm ICP-AES 5 1 1 1 1 Cu ppm ICP-AES 5 1 1 1 0.5 Mo ppm ICP-AES 8 1 5 1 1 Ni ppm ICP-AES 5 1 1 1 1 Sc ppm ICP-AES 1 na 0.1 0.5 0.5 Sr ppm ICP-AES 1 1 2 1 0.5 V ppm ICP-AES 5 1 5 5 2 W ppm ICP-AES 40 1 3 2 10 Zn ppm ICP-AES 2 1 1 1 0.5 Cr ppm ICP-MS 1 1 1 2 1 La ppm ICP-MS 0.01 na 0.05 0.5 0.1 Ce ppm ICP-MS 0.01 na 1 0.5 0.1 Pr ppm ICP-MS 0.01 na 0.02 0.1 0.2 Nd ppm ICP-MS 0.01 na 1 0.5 0.1 Sm ppm ICP-MS 0.01 na 0.01 0.1 0.1 Eu ppm ICP-MS 0.01 na 0.05 0.1 0.05 Gd ppm ICP-MS 0.01 na 0.02 0.1 0.1 Tb ppm ICP-MS 0.01 na 0.1 0.1 0.1 Dy ppm ICP-MS 0.01 na 0.02 0.1 0.1 Ho ppm ICP-MS 0.01 na 0.01 0.1 0.05 Er ppm ICP-MS 0.01 na 0.01 0.1 0.1 Tm ppm ICP-MS 0.01 na 0.005 0.1 0.1 Yb ppm ICP-MS 0.01 na 0.05 0.1 0.1 Lu ppm ICP-MS 0.01 na 0.01 0.1 0.05

*WD-XRF = Wavelength Dispersive - X-Ray Fluorescence; ICP = inductively coupled plasma; AES = atomic emission spectroscopy; MS = mass spectrometry; AAS = atomic absorption spectrometry; FA = fire assay; † = average limit of detection; na = not applicable

475

Laboratory

Element Unit Method* Geo Labs Accurassay ACTLABS Chemex XRAL

Rb ppm ICP-MS 0.01 na 2 0.2 2 Sr ppm ICP-MS 0.02 na 2 0.1 2 Nb ppm ICP-MS 0.02 na 2 1 2 Cs ppm ICP-MS 0.01 na 0.2 0.1 1 Hf ppm ICP-MS 0.01 na 0.2 1 1 Ta ppm ICP-MS 0.01 na 0.3 0.5 1 Th ppm ICP-MS 0.02 na 0.1 1 0.1 U ppm ICP-MS 0.02 na 0.1 0.5 0.1 Y ppm ICP-MS 0.5 na 1 0.5 1 Zr ppm ICP-MS 1 na 4 0.5 2 Se ppb AAS 7 100 200 200 100 S wt% L-IR 0.01 0.01 0.01 0.01 0.01

Os ppb FA/ICP-MS Na na 2 na 3 Ir ppb FA/ICP-MS †0.27 na 0.1 na 0.1

Ru ppb FA/ICP-MS †0.66 na 5 na 1 Re ppb FA/ICP-MS Na na 5 na 1 Rh ppb FA/ICP-MS †0.26 na 0.2 30 30 Pt ppb FA/ICP-MS †1.43 15 5 5 10 Pd ppb FA/ICP-MS †1.88 10 2-4 2 1 Au ppb FA/ICP-MS †1.42 5 0.5-2 2 5 Ag ppm FA/ICP-MS 0.5 1 0.2 0.2 5

*WD-XRF = Wavelength Dispersive - X-Ray Fluorescence; ICP = inductively coupled plasma; AES = atomic emission spectroscopy; MS = mass spectrometry; AAS = atomic absorption spectrometry; FA = fire assay; † = average limit of detection; na = not applicable

476

(B) ANALYTICAL MTHOD CODES AND EXPLANATORY NOTES: 1Method: 1=WD-XRF, 2=Lebo thermogravimetry, 3=Leco infrared combustion, 4=DCP, 5=ICP-MS, 6=NiS/ICP-MS, 7=AAS-hydride, 8=Fire Assay/DCP 2Sample Type: L=massive/layered unit, M=matrix, F=fragment; b-qtz=blue quartz; Rock Type: Mgab=melagabbro, Lgab=leucogabbro, gab=gabbro 3CIPW Name: OGN=olivine gabbronorite; GN=gabbronorite; OLGN=olivine leucogabbronorite; LGN=leucogabbronorite; G=gabbro Concentrations: Major Element Oxides, S, CO2, and LOI concentrations are in wt% Trace element and Cu-Ni concentrations are in ppm PGE and Se are in ppb Miscellaneous: LLD = lower limit of detection "-" = not detected/determined Fe2O3* = total iron Ti* = calculated from TiO2P* = calculated from P2O5

Sam

ple

Tow

nshi

pSt

udy

Are

aD

escr

iptio

n 1

Roc

k T

ype

Fiel

d N

ame

JB97

-65

Wel

lsB

assw

ood

Lk T

rav

dyke

; with

pos

sibl

e ch

illed

mar

gins

with

gab

bro

aplit

eJB

97-7

8BW

ater

sM

akad

am

g pi

nk g

rani

toid

in c

onta

ct w

ith m

g ga

bbro

on

hill;

apl

itic

phas

e?; d

yke

aplit

eJB

97-4

8W

ells

App

leby

Lk

Trav

App

leby

Lk;

pos

sibl

e ch

illed

mar

gin;

fg d

iaba

se -

qtz?

chill

ed g

abbr

oJB

97-4

9W

ells

App

leby

Lk

Trav

App

leby

Lk;

pos

sibl

e ch

illed

mar

gin;

fg d

iaba

se -

qtz?

chill

ed g

abbr

oJB

98-2

07K

elly

Car

afel

Bay

Tra

vfg

; TR

AV

ERSE

EN

D -

~40m

N. o

f las

t sta

tion

- chi

llch

illed

gab

bro

JB98

-224

Jane

sC

hini

guch

ifg

; chi

lled

mar

gin

chill

ed g

abbr

oJB

98-2

39B

Kel

lyK

ukag

ami C

liff

chill

ed m

argi

n? b

aked

qtz

-gab

bro?

seds

? ~6

m u

p "b

ack"

-sid

e of

hill

; tra

vers

ech

illed

gab

bro

JB98

-239

CK

elly

Kuk

agam

i Clif

ffg

; chi

lled

mar

gin;

~5m

up

side

of h

ill o

n "p

ath"

- w

est e

nd; t

rave

rse

chill

ed g

abbr

oJB

98-2

40K

elly

Kuk

agam

i Clif

ffg

;chi

lled

mar

gin;

from

"ba

ck"

or n

orth

side

of h

ill; f

urth

er e

ast t

han

239

serie

sch

illed

gab

bro

JB97

-4B

Wat

ers

Mak

ada

mg;

bar

ren

gabb

ro fr

om ~

4m so

uth

of p

it ar

ea; g

rid 1

00N

/100

Ega

bbro

JB97

-18

Kel

lyW

asha

gam

i Lak

em

g; e

ast o

f hill

pea

kga

bbro

JB97

-20

Kel

lyW

asha

gam

i Lak

em

g; b

lue

tint t

o pl

ag.;

pos

sibl

e bl

ue q

uartz

?ga

bbro

JB97

-24

Cle

men

tM

anito

u La

ke T

rav

mg;

no

min

eral

izat

ion;

mas

sive

gabb

roJB

97-2

5C

lem

ent

Man

itou

Lake

Tra

vm

g; n

o m

iner

aliz

atio

n; m

assi

vega

bbro

JB97

-26

Cle

men

tM

anito

u La

ke T

rav

mg;

no

min

eral

izat

ion;

mas

sive

gabb

roJB

97-2

7C

lem

ent

Man

itou

Lake

Tra

vm

g; n

o m

iner

aliz

atio

n; m

assi

vega

bbro

JB97

-28

Cle

men

tM

anito

u La

ke T

rav

mg;

no

min

eral

izat

ion;

mas

sive

gabb

roJB

97-2

9C

lem

ent

Man

itou

Lake

Tra

vm

g; n

o m

iner

aliz

atio

n; m

assi

vega

bbro

JB97

-30

Cle

men

tM

anito

u La

ke T

rav

mg;

no

min

eral

izat

ion;

mas

sive

gabb

roJB

97-3

1C

lem

ent

Man

itou

Lake

Tra

vm

g; n

o m

iner

aliz

atio

n; m

assi

vega

bbro

JB97

-32

Cle

men

tM

anito

u La

ke T

rav

mg;

no

min

eral

izat

ion;

mas

sive

gabb

roJB

97-3

3Fo

ster

Bra

zil L

ake

cpy

mai

nly

in th

e Q

-C v

ein;

po

mai

nly

in p

od-li

ke h

oste

d by

mg

Nip

. Gab

.ga

bbro

JB97

-34

Fost

erB

razi

l Lak

efg

-mg;

abo

ut 3

m n

orth

of c

liff-

sedi

men

tsga

bbro

JB97

-36

Fost

erB

razi

l Lak

em

g; ~

60 m

wes

t of t

renc

h; w

ithin

5m

of w

hite

"bu

ll" q

tz v

ein;

alte

red

gabb

roJB

97-3

9AN

airn

Nai

rn W

right

mg;

msv

. sul

phid

es in

Nip

. Gab

bro/

trenc

hes;

>80

% su

lphi

des;

blu

e qu

artz

eye

sga

bbro

JB97

-39B

Nai

rnN

airn

Wrig

htm

g; c

py a

nd p

o in

Nip

. Gab

bro

as u

p to

25%

pat

ches

; blu

e qy

artz

eye

sga

bbro

JB97

-39C

Nai

rnN

airn

Wrig

htm

g; b

lue

qtz.

eye

s up

to 2

5% o

f gab

bro;

wal

l roc

k by

tren

ch b

last

gabb

roJB

97-4

0AJa

nes

Chi

nigu

chi

mg;

S-e

dge

of o

/c; n

on-m

iner

aliz

ed(4

0B?)

; Kirk

land

Tow

nsite

Occ

.; Ja

nes S

outh

gabb

roJB

97-4

0BJa

nes

Chi

nigu

chi

mg;

mag

mat

ic-2

BA

GS;

Kirk

land

Tow

nsite

; Jan

es S

outh

gabb

roJB

97-4

1AJa

nes

Chi

nigu

chi

mg;

mag

mat

ic; e

ast e

nd o

f tre

nch;

NE

of K

irkla

nd T

owns

ite O

cc; b

y sw

amp

gabb

roJB

97-4

1BJa

nes

Chi

nigu

chi

mg;

mid

dle

of tr

ench

; NE

of K

irkla

nd T

owns

ite O

ccur

renc

e; b

y sw

amp

gabb

roJB

97-4

1CJa

nes

Chi

nigu

chi

mg;

non

-min

eral

ized

from

edg

e of

swam

p; N

E of

Kirk

land

Tow

nsite

Occ

gabb

roJB

97-4

2AJa

nes

Chi

nigu

chi

mg;

edg

e of

"pi

t" b

y sw

amp,

~35

m so

uth

of JB

97-4

1; N

E of

K.T

.Oga

bbro

JB97

-42B

Jane

sC

hini

guch

im

g; m

agm

atic

with

onl

y pa

tchy

alte

ratio

n; N

E of

Kirk

land

Tow

nsite

Occ

gabb

ro

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

JB97

-65

JB97

-78B

JB97

-48

JB97

-49

JB98

-207

JB98

-224

JB98

-239

BJB

98-2

39C

JB98

-240

JB97

-4B

JB97

-18

JB97

-20

JB97

-24

JB97

-25

JB97

-26

JB97

-27

JB97

-28

JB97

-29

JB97

-30

JB97

-31

JB97

-32

JB97

-33

JB97

-34

JB97

-36

JB97

-39A

JB97

-39B

JB97

-39C

JB97

-40A

JB97

-40B

JB97

-41A

JB97

-41B

JB97

-41C

JB97

-42A

JB97

-42B

Sulp

hide

/Oxi

deS

SeN

iIr

Ru

Rh

PtPd

Au

Cu

Al2

O3

SiO

2Si

O2

TiO

2w

t%pp

bpp

mpp

bpp

bpp

bpp

bpp

bpp

bpp

mTi

O2

MgO

wt%

wt%

none

0.13

020

0.0

140.

270

0.66

00.

260

1.43

01.

880

5.88

091

8359

977

.93

0.14

d.s.

and

b.s.

0.60

011

22.0

680.

270

0.66

00.

260

1.43

07.

480

3.54

039

018

6470

.55

0.72

none

0.06

032

7.0

120

0.27

00.

660

0.16

011

.196

13.5

403.

020

170

168

51.4

20.

89no

ne0.

080

364.

096

0.27

00.

660

0.26

01.

430

1.88

01.

420

160

158

51.4

50.

89pa

tchy

mag

netis

m (p

o?)

0.05

316

8.0

122

0.07

00.

160

0.39

912

.340

12.9

704.

510

109

256

51.9

20.

570.

059

222.

012

20.

069

0.66

00.

207

9.53

010

.720

4.73

011

417

649

.81

0.81

0.08

621

1.0

117

0.27

00.

660

0.31

010

.400

17.2

402.

260

7729

651

.22

0.52

0.04

021

9.0

119

0.27

00.

660

0.28

010

.590

11.1

003.

530

114

286

50.6

60.

520.

044

239.

012

00.

270

0.66

00.

290

10.6

1012

.120

3.28

013

324

650

.40

0.60

barr

en -

4m so

uth

of p

its 3

&4

0.02

010

1.0

220

0.30

21.

118

0.80

15.

851

11.5

493.

689

9327

551

.54

0.48

sulp

hide

ble

bs a

nd d

.s.0.

060

365.

015

00.

270

0.66

00.

260

4.36

66.

156

4.27

217

027

652

.28

0.53

1% d

.s.0.

020

233.

014

00.

182

0.66

00.

620

27.3

0045

.041

4.81

112

029

651

.78

0.52

none

vis

ible

0.02

015

5.0

100

0.27

00.

660

0.26

01.

430

1.93

01.

689

150

238

51.3

40.

66no

ne v

isib

le0.

050

290.

011

00.

270

0.66

00.

260

1.35

62.

500

3.21

015

026

851

.63

0.61

none

vis

ible

0.07

030

9.0

110

0.27

00.

660

0.26

02.

363

3.27

12.

847

160

258

51.4

70.

63no

ne v

isib

le0.

060

293.

012

00.

270

0.66

00.

260

0.50

00.

410

3.15

015

025

751

.97

0.59

none

vis

ible

0.07

031

1.0

110

0.27

00.

660

0.26

01.

430

1.88

01.

420

160

197

52.1

50.

74no

ne v

isib

le0.

040

277.

010

09.

820

2.77

04.

520

4.02

04.

420

3.22

015

023

851

.95

0.68

none

vis

ible

0.07

030

2.0

110

0.17

80.

660

0.27

52.

323

7.31

42.

329

140

238

51.4

30.

67no

ne v

isib

le0.

060

233.

038

0.27

00.

660

0.26

01.

430

1.88

06.

444

408

1653

.95

1.40

none

vis

ible

0.07

012

1.0

950.

270

0.66

00.

260

1.43

01.

880

1.42

051

78

45.8

62.

51po

, co(

?), p

t, cp

y33

.800

5895

0.0

6360

0.27

00.

660

0.26

01.

430

125.

610

11.9

3026

1na

nana

nano

ne v

isib

le0.

090

379.

089

0.27

00.

660

0.26

01.

430

1.88

01.

840

130

267

51.7

80.

55no

ne v

isib

le0.

030

180.

098

0.27

00.

660

0.26

01.

430

1.88

01.

420

7340

749

.79

0.40

s-m

sv. p

o; m

inor

cpy

,pt(?

)15

.700

1332

0.0

1300

019

.160

39.7

5043

.170

60.7

7064

.620

35.0

9065

0na

nana

nas-

msv

. po;

min

or c

py,p

t(?)

8.54

019

6.0

6900

13.9

5032

.980

32.3

1030

.260

33.4

1031

.450

7900

nana

nana

bleb

s and

d.s.

0.00

588

.014

00.

270

0.66

00.

370

2.18

018

.070

4.91

058

nana

nana

d.s.

0.09

036

2.0

120

0.27

00.

660

0.25

01.

430

1.91

02.

440

160

296

52.0

50.

49d.

s.; p

o an

d cp

y0.

970

4892

.065

00.

170

0.66

01.

000

3.26

05.

920

21.0

3023

0026

649

.85

0.51

d.s.;

po

and

cpy

0.12

062

0.0

170

0.27

00.

660

0.26

01.

430

2.26

04.

006

520

356

50.0

00.

41cp

y=po

1.18

052

01.0

850

0.19

90.

660

0.16

04.

992

7.77

719

.907

3000

335

49.0

40.

39d.

s.0.

120

425.

015

00.

270

0.66

00.

260

1.43

03.

364

2.27

524

031

550

.70

0.42

d.s.

0.11

052

4.0

160

0.27

00.

660

0.26

01.

430

1.88

04.

650

430

365

49.1

70.

36d.

s. po

=cpy

1.86

098

92.0

1300

0.31

01.

150

0.75

07.

100

9.13

028

.210

4900

365

47.5

40.

37

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

JB97

-65

JB97

-78B

JB97

-48

JB97

-49

JB98

-207

JB98

-224

JB98

-239

BJB

98-2

39C

JB98

-240

JB97

-4B

JB97

-18

JB97

-20

JB97

-24

JB97

-25

JB97

-26

JB97

-27

JB97

-28

JB97

-29

JB97

-30

JB97

-31

JB97

-32

JB97

-33

JB97

-34

JB97

-36

JB97

-39A

JB97

-39B

JB97

-39C

JB97

-40A

JB97

-40B

JB97

-41A

JB97

-41B

JB97

-41C

JB97

-42A

JB97

-42B

Al2

O3

Fe2O

3*M

nOM

gOC

aON

a2O

K2O

P2O

5C

O2

SL

OI

M-T

otal

Mg#

Co

Cr*

VC

sR

bT

hU

Nb

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

11.5

51.

080.

010.

130.

536.

910.

110.

020.

320.

130.

6299

.03

2242

536

0.08

1.58

20.9

73.

734.

8412

.93

3.06

0.02

1.11

1.63

6.82

0.74

0.10

1.34

0.60

1.12

98.8

046

33na

330.

4310

.93

0.42

0.82

3.99

14.0

612

.52

0.18

6.78

10.3

31.

990.

980.

030.

160.

060.

9210

0.10

5651

na27

01.

3841

.86

1.62

0.50

3.20

13.6

012

.96

0.21

6.13

8.59

2.52

1.06

0.03

0.21

0.08

1.88

99.3

252

52na

280

1.03

43.2

22.

320.

733.

9214

.28

10.1

90.

178.

4311

.49

2.00

0.57

0.05

na0.

050.

6210

0.29

6641

na21

01.

8918

.84

1.64

0.52

2.24

13.5

212

.39

0.20

7.90

10.2

22.

070.

250.

06na

0.06

2.97

100.

2060

46na

236

0.60

8.08

1.59

0.48

2.85

14.8

39.

860.

158.

3210

.71

1.76

1.05

0.03

na0.

091.

8310

0.28

6637

na20

22.

7946

.38

1.64

0.54

2.19

14.5

710

.55

0.18

8.31

11.1

31.

630.

590.

05na

0.04

2.23

100.

4265

42na

205

1.66

24.8

41.

440.

462.

0014

.42

10.5

30.

178.

2510

.34

1.84

0.74

0.05

na0.

042.

9810

0.32

6541

na20

81.

1728

.34

1.05

0.51

2.25

13.0

39.

740.

1710

.84

12.2

11.

380.

480.

000.

220.

020.

9510

0.82

7246

na23

01.

6619

.10

1.12

0.34

1.91

14.3

79.

910.

178.

5711

.73

1.60

0.60

0.02

0.12

0.06

0.27

100.

0567

43na

220

0.99

16.8

11.

440.

422.

0515

.29

9.30

0.16

8.48

12.4

41.

520.

390.

020.

130.

020.

3210

0.22

6838

na20

00.

7012

.97

1.22

0.36

1.88

14.9

711

.36

0.19

6.67

10.5

92.

270.

610.

040.

230.

021.

1099

.80

5847

na21

00.

7412

.95

1.41

0.41

2.76

15.8

610

.17

0.16

6.85

11.5

32.

060.

520.

030.

170.

050.

5299

.94

6140

na20

01.

4018

.21

1.30

0.37

2.30

15.7

210

.75

0.17

6.84

11.4

32.

080.

450.

040.

130.

070.

3799

.95

6042

na21

00.

9713

.84

1.19

0.36

2.28

14.5

710

.58

0.17

7.86

11.9

01.

920.

460.

030.

270.

060.

4710

0.52

6346

na22

01.

3115

.81

1.22

0.34

2.18

14.1

711

.61

0.19

7.16

11.1

72.

110.

500.

040.

150.

070.

2110

0.05

5946

na24

01.

0416

.47

1.49

0.46

2.87

15.6

411

.00

0.17

6.51

11.0

72.

150.

530.

040.

160.

040.

4210

0.16

5842

na22

01.

2617

.20

1.48

0.41

2.62

15.4

310

.28

0.17

6.75

11.0

72.

040.

670.

040.

160.

070.

9999

.54

6039

na21

02.

0224

.11

1.48

0.44

2.66

11.8

715

.48

0.21

3.42

9.87

0.08

1.24

0.09

0.05

0.06

2.02

99.6

334

46na

340

0.44

35.3

13.

140.

995.

5416

.74

14.7

90.

175.

978.

213.

361.

150.

530.

120.

070.

0599

.34

4850

na19

00.

9721

.43

1.41

0.36

16.4

8na

nana

nana

nana

na0.

1633

.80

na0.

00-

1165

9031

0.07

0.74

0.03

0.08

0.08

14.2

810

.99

0.18

7.29

10.1

41.

970.

790.

030.

410.

091.

9099

.90

6143

na22

01.

3233

.68

1.48

0.44

2.14

16.1

68.

900.

127.

339.

962.

070.

990.

021.

100.

033.

6099

.34

6635

na18

01.

1744

.61

1.13

0.40

1.53

nana

nana

nana

nana

0.14

15.7

0na

0.00

-29

0na

180

0.59

6.58

1.37

0.36

1.46

nana

nana

nana

nana

0.18

8.54

na0.

00-

180

na24

00.

474.

690.

050.

25na

nana

nana

nana

na0.

840.

00na

0.00

-35

na16

02.

5965

.58

6.18

2.70

3.40

14.2

410

.82

0.20

8.65

10.6

91.

690.

460.

030.

160.

090.

7510

0.07

6547

na19

01.

6517

.13

1.38

0.44

1.87

13.1

313

.15

0.22

8.99

10.3

71.

470.

420.

030.

240.

970.

8999

.03

6183

na21

01.

5714

.35

1.12

0.39

1.85

14.4

510

.54

0.20

8.84

9.53

1.74

0.33

0.02

0.84

0.12

3.19

99.2

566

42na

180

1.72

6.89

1.08

0.39

1.42

12.9

012

.49

0.18

9.50

10.6

31.

220.

740.

010.

201.

181.

7398

.83

6487

na19

06.

7129

.78

0.95

0.30

1.36

13.1

510

.03

0.18

9.70

11.2

01.

240.

770.

020.

210.

122.

2299

.63

6946

na19

02.

8231

.43

1.11

0.36

1.48

12.7

910

.81

0.19

9.82

11.3

21.

020.

050.

020.

240.

113.

8699

.41

6877

na17

00.

280.

820.

880.

351.

1813

.29

13.4

00.

189.

0210

.37

1.05

0.68

0.01

0.16

1.86

2.33

98.2

461

110

na18

02.

2424

.42

0.88

0.28

1.14

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

JB97

-65

JB97

-78B

JB97

-48

JB97

-49

JB98

-207

JB98

-224

JB98

-239

BJB

98-2

39C

JB98

-240

JB97

-4B

JB97

-18

JB97

-20

JB97

-24

JB97

-25

JB97

-26

JB97

-27

JB97

-28

JB97

-29

JB97

-30

JB97

-31

JB97

-32

JB97

-33

JB97

-34

JB97

-36

JB97

-39A

JB97

-39B

JB97

-39C

JB97

-40A

JB97

-40B

JB97

-41A

JB97

-41B

JB97

-41C

JB97

-42A

JB97

-42B

Ta

La

Ce

PrSr

Nd

Zr

Hf

SmE

uT

i*G

dT

bD

yY

Ho

Er

Tm

Yb

Lu

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

1.01

2.96

8.45

1.24

14.5

06.

12na

7.66

2.16

0.34

0.08

43.

150.

664.

26 -

0.96

2.62

0.38

2.43

0.34

1.02

4.18

9.98

1.41

41.4

06.

40na

1.85

1.71

0.32

0.43

21.

630.

261.

61 -

0.35

0.94

0.14

0.88

0.13

0.31

6.76

15.5

22.

1315

8.40

9.66

na1.

902.

690.

860.

534

2.94

0.48

3.18

-0.

671.

850.

261.

760.

270.

389.

1620

.28

2.63

189.

0011

.37

na2.

233.

010.

890.

534

3.06

0.49

3.28

-0.

681.

850.

281.

740.

280.

226.

1413

.08

1.72

158.

507.

3844

.81

1.43

1.90

0.64

0.34

22.

220.

392.

4615

.43

0.56

1.62

0.25

1.65

0.24

0.26

6.62

14.5

92.

0146

7.80

9.33

55.7

91.

712.

380.

780.

486

2.86

0.46

2.96

17.2

40.

631.

780.

271.

530.

250.

186.

6313

.78

1.71

223.

407.

3043

.00

1.14

1.70

0.56

0.31

21.

850.

312.

1513

.93

0.47

1.41

0.20

1.31

0.21

0.17

5.63

11.9

31.

5415

5.30

6.36

41.3

01.

161.

580.

530.

312

1.71

0.31

2.07

13.9

80.

481.

270.

201.

290.

190.

235.

8212

.50

1.67

160.

806.

8937

.60

1.21

1.72

0.60

0.36

02.

180.

362.

5513

.04

0.54

1.48

0.24

1.47

0.23

0.13

4.44

9.73

1.27

158.

705.

71na

-1.

510.

540.

288

1.66

0.27

1.85

-0.

391.

110.

161.

040.

160.

145.

6312

.43

1.56

147.

406.

88na

-1.

740.

580.

318

1.94

0.34

2.27

-0.

521.

480.

221.

500.

220.

135.

0711

.12

1.40

134.

506.

32na

-1.

670.

540.

312

1.85

0.33

2.17

-0.

491.

420.

211.

390.

210.

186.

6814

.86

1.94

256.

208.

74na

-2.

230.

800.

396

2.34

0.38

2.45

-0.

541.

470.

221.

340.

210.

165.

7412

.71

1.63

215.

207.

33na

-1.

860.

700.

366

2.04

0.33

2.17

-0.

471.

350.

191.

260.

180.

155.

5612

.64

1.69

219.

907.

37na

-1.

920.

710.

378

2.10

0.35

2.27

-0.

471.

340.

191.

220.

180.

145.

3912

.27

1.63

202.

507.

35na

1.26

1.99

0.70

0.35

42.

060.

352.

24 -

0.49

1.38

0.19

1.26

0.19

0.19

6.82

15.3

72.

0020

4.30

8.99

na1.

602.

380.

810.

444

2.49

0.41

2.59

-0.

581.

580.

231.

470.

220.

186.

7014

.68

1.89

220.

208.

55na

1.58

2.25

0.79

0.40

82.

360.

402.

60 -

0.55

1.56

0.21

1.42

0.21

0.18

6.62

14.5

51.

8921

4.40

8.33

na1.

492.

070.

720.

402

2.32

0.37

2.50

-0.

531.

460.

211.

360.

210.

3613

.44

29.3

03.

8278

2.80

16.8

7na

2.46

4.18

1.59

0.83

94.

330.

744.

79 -

1.07

3.06

0.42

2.54

0.36

0.87

23.8

355

.42

7.40

606.

6032

.97

na4.

666.

902.

261.

505

6.00

0.90

5.67

-1.

163.

190.

462.

890.

440.

030.

647.

400.

231.

101.

11na

0.24

0.20

0.03

-0.

170.

030.

19 -

0.04

0.36

0.03

0.20

0.04

0.15

6.03

13.1

31.

6415

3.30

7.08

na1.

281.

760.

600.

330

1.97

0.33

2.31

-0.

541.

540.

221.

490.

220.

104.

509.

931.

2117

4.60

5.35

na0.

751.

340.

530.

240

1.46

0.26

1.76

-0.

401.

160.

171.

040.

160.

103.

828.

591.

0613

.30

4.57

na0.

861.

020.

27 -

1.02

0.17

1.17

-0.

260.

690.

100.

680.

100.

020.

220.

730.

144.

600.

98na

0.13

0.45

0.22

-0.

550.

100.

77 -

0.18

0.53

0.08

0.59

0.10

0.34

15.3

129

.19

3.26

210.

6012

.38

na2.

162.

280.

78 -

1.69

0.25

1.50

-0.

290.

810.

120.

770.

110.

145.

1111

.01

1.38

136.

705.

95na

1.12

1.59

0.54

0.29

41.

750.

301.

96 -

0.43

1.28

0.20

1.26

0.19

0.15

4.78

10.5

21.

3713

3.00

6.07

na1.

051.

580.

540.

306

1.75

0.32

2.17

-0.

461.

320.

191.

290.

200.

105.

7212

.30

1.53

150.

706.

52na

0.89

1.71

0.63

0.24

61.

860.

301.

95 -

0.41

1.16

0.17

1.08

0.16

0.09

3.71

8.15

1.04

107.

904.

65na

0.84

1.17

0.45

0.23

41.

420.

241.

68 -

0.38

1.06

0.16

1.04

0.16

0.10

4.30

9.43

1.18

135.

805.

02na

0.92

1.34

0.48

0.25

21.

550.

271.

76 -

0.41

1.17

0.17

1.14

0.17

0.08

3.84

8.22

1.03

266.

504.

51na

0.73

1.20

0.56

0.21

61.

420.

241.

68 -

0.37

1.04

0.17

1.04

0.15

0.08

3.57

7.97

1.01

139.

604.

46na

0.74

1.16

0.44

0.22

21.

320.

251.

59 -

0.36

1.03

0.16

1.00

0.14

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

Tow

nshi

pSt

udy

Are

aD

escr

iptio

n 1

Roc

k T

ype

Fiel

d N

ame

JB97

-54B

Wel

lsA

pple

by L

k Tr

avA

pple

by L

k; c

g ga

bbro

cou

ntry

rock

to su

lph;

~3m

eas

t of s

ulph

ide

sect

ion

gabb

roJB

97-5

5W

ells

App

leby

Lk

Trav

App

leby

Lk;

mg-

cg; n

o vi

sibl

e su

lphi

des;

sout

h si

de o

f hig

hway

gabb

roJB

97-5

6W

ells

App

leby

Lk

Trav

App

leby

Lk;

mg;

no

visi

ble

sulp

hide

s; so

uth

side

of h

ighw

ayga

bbro

JB97

-57

Wel

lsA

pple

by L

k Tr

avA

pple

by L

k; m

g; n

o vi

sibl

e su

lphi

des;

sout

h si

de o

f hig

hway

; aug

ite p

heno

crys

ts?

gabb

roJB

97-5

8W

ells

App

leby

Lk

Trav

App

leby

Lk;

mg;

no

visi

ble

sulp

hide

s; so

uth

side

of h

ighw

ayga

bbro

JB97

-62

Wel

lsB

assw

ood

Lk T

rav

fg-m

g; m

agne

tic p

atch

esga

bbro

JB97

-67

Jane

sC

hini

guch

im

g ga

bbro

; lay

erin

g pr

esen

t at 3

0Az

gabb

roJB

97-7

0BLo

uise

Lo

uie

Lake

fg to

mg

gabb

ro fr

om w

all r

ock

arou

nd su

lphi

de ri

ch "

pod"

gabb

roJB

97-7

0CLo

uise

Lo

uie

Lake

mg

opx.

(?) g

abbr

o; N

orth

con

tact

with

sulp

hide

s in

pit;

alte

red

loca

llyga

bbro

JB97

-70D

Loui

se

Loui

e La

kefg

-mg

gabb

ro; f

rom

o/c

abo

ut 8

m so

uthw

est o

f pit

gabb

roJB

97-7

4AW

ater

sM

akad

am

g; a

ltere

d ga

bbro

with

chl

orite

, bio

tite

and

actin

olite

; pit

on h

ill 1

30N

/170

Ega

bbro

JB97

-75

Wat

ers

Mak

ada

cg to

peg

mat

itic;

segg

rega

tion

pod

gabb

roJB

97-7

6AW

ater

sM

akad

am

g; w

allro

ck b

y m

sv. Q

-C v

ein

gabb

roJB

97-7

7AW

ater

sM

akad

acg

gab

bro;

from

pit

on si

de o

f hill

; fro

m fr

esh

rock

gabb

roJB

97-7

7BW

ater

sM

akad

avc

g to

peg

mat

itic

gabb

ro; f

rom

bla

sted

rubb

lega

bbro

JB97

-78A

Wat

ers

Mak

ada

fg a

nd sh

eare

d ga

bbro

with

blu

e qt

z ey

esga

bbro

JB97

-84D

Loui

seLo

uie

Lake

mg;

wal

l roc

k ad

jace

nt to

smal

l pit

with

sulp

hide

sga

bbro

JB97

-87A

Jane

sC

hini

guch

i T1

Det

ail

mg;

TR

AV

ERSE

STA

RT

- nor

th e

nd o

f tre

nch

1 cl

earin

g; h

eadi

ng 1

80ga

bbro

JB97

-87B

Jane

sC

hini

guch

i T1

Det

ail

mg;

tren

ch 1

- tra

vers

ega

bbro

JB97

-87C

Jane

sC

hini

guch

i T1

Det

ail

mg;

tren

ch 1

- ru

sty

area

; tra

vers

ega

bbro

JB97

-87D

Jane

sC

hini

guch

i T1

Det

ail

mg;

tren

ch 1

- ru

sty

area

; tra

vers

ega

bbro

JB97

-87E

Jane

sC

hini

guch

i T1

Det

ail

mg;

tren

ch 1

- ru

sty

area

; tra

vers

ega

bbro

JB97

-87F

Jane

sC

hini

guch

i T1

Det

ail

mg;

tren

ch 1

- ru

sty

area

; tra

vers

ega

bbro

JB97

-87G

Jane

sC

hini

guch

i T1

Det

ail

mg;

tren

ch 1

- ru

sty

area

; tra

vers

ega

bbro

JB97

-87H

Jane

sC

hini

guch

i T1

Det

ail

mg;

tren

ch 1

- ru

sty

area

; tra

vers

ega

bbro

JB97

-87I

Jane

sC

hini

guch

i T1

Det

ail

mg;

tren

ch 1

- ed

ge o

f rus

ty a

rea;

tra

vers

ega

bbro

JB97

-87J

Jane

sC

hini

guch

i T1

Det

ail

mg;

tren

ch 1

- tra

vers

ega

bbro

JB97

-87K

Jane

sC

hini

guch

i T1

Det

ail

mg;

TR

AV

ERSE

EN

D -

trenc

h 1

gabb

roJB

97-9

3Po

rter

Big

Sw

ansh

eare

d; B

ig S

wan

-mai

n sk

arn;

mai

n A

s-sh

ear z

one

that

x-c

uts g

abbr

oga

bbro

JB97

-99

Scad

ding

Scad

ding

mg;

pro

xim

al to

sed-

gabb

ro c

onta

ct; s

imila

r to

Alw

yn; s

wam

p to

Nga

bbro

JB97

-103

EK

elly

Kuk

agam

i Det

ail

mg;

fels

ic in

wea

ther

ing/

colo

ur>p

it sa

mpl

es; a

bout

13.

0m e

ast o

f pit

area

gabb

roJB

97-1

06A

Jane

sC

hini

guch

iTr

ench

T-2

on

Falc

o m

ap; a

bout

13.

5 m

sout

h of

nor

th e

nd o

f tre

nch

gabb

roJB

97-1

06C

Jane

sC

hini

guch

iTr

ench

T-2

on

Falc

o m

ap; a

bout

26.

0 m

sout

h of

nor

th e

nd o

f tre

nch

gabb

roJB

98-1

14W

ater

sM

akad

a Tr

aver

sem

g; n

on-m

agne

tic; m

assi

ve w

ith ir

regu

lar f

ract

ures

gabb

ro

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

JB97

-54B

JB97

-55

JB97

-56

JB97

-57

JB97

-58

JB97

-62

JB97

-67

JB97

-70B

JB97

-70C

JB97

-70D

JB97

-74A

JB97

-75

JB97

-76A

JB97

-77A

JB97

-77B

JB97

-78A

JB97

-84D

JB97

-87A

JB97

-87B

JB97

-87C

JB97

-87D

JB97

-87E

JB97

-87F

JB97

-87G

JB97

-87H

JB97

-87I

JB97

-87J

JB97

-87K

JB97

-93

JB97

-99

JB97

-103

EJB

97-1

06A

JB97

-106

CJB

98-1

14

Sulp

hide

/Oxi

deS

SeN

iIr

Ru

Rh

PtPd

Au

Cu

Al2

O3

SiO

2Si

O2

TiO

2w

t%pp

bpp

mpp

bpp

bpp

bpp

bpp

bpp

bpp

mTi

O2

MgO

wt%

wt%

d.s.

0.09

035

2.0

790.

270

0.66

00.

210

1.43

01.

760

6.29

017

012

1051

.07

1.13

none

0.08

035

8.0

100

0.27

00.

660

0.26

01.

430

1.88

02.

710

170

168

51.5

60.

87no

ne0.

070

375.

011

00.

589

0.66

00.

442

4.34

33.

438

3.61

316

018

851

.48

0.80

none

0.08

042

2.0

110

0.27

00.

660

0.26

05.

000

1.88

04.

210

180

168

51.6

60.

88no

ne0.

080

402.

011

00.

270

0.66

00.

260

7.84

08.

420

8.56

017

015

851

.69

0.93

d.s.;

dis

s. m

agne

tite

0.04

029

4.0

112

0.27

00.

660

1.05

011

.130

8.24

03.

790

120

229

51.9

90.

72no

ne0.

032

152.

042

- -

-17

.000

32.0

001.

000

9436

550

.20

0.40

d.s.

- po>

>cpy

/py

5.11

069

38.0

1069

1.26

01.

710

1.74

010

.670

50.1

605.

100

539

336

50.4

10.

46d.

s.; p

o>>c

py0.

100

407.

018

80.

270

0.66

00.

260

7.40

08.

150

6.37

014

131

450

.68

0.39

none

vis

ible

0.07

032

6.0

180

0.27

00.

660

0.26

06.

500

8.21

05.

170

143

315

51.5

40.

41po

>cpy

+/-

pn?

1.05

014

55.0

210

0.27

00.

660

0.26

01.

430

10.4

305.

770

278

1448

84.2

20.

39po

>cpy

- D

ean

Peke

skis

' are

a0.

030

281.

053

0.27

00.

660

0.26

01.

430

1.88

01.

420

112

417

54.4

03.

54d.

s. - p

o>cp

y0.

150

228.

017

00.

270

0.66

01.

100

9.56

013

.450

5.87

045

206

53.3

70.

73d.

s. an

d bl

ebs;

po>

cpy

0.19

032

1.0

85 -

- -

- -

-15

018

850

.82

0.83

d.s.

and

bleb

- po

>cpy

0.85

015

63.0

190

0.27

00.

660

0.67

09.

280

15.1

7028

8.75

088

012

852

.03

1.02

d.s.

0.17

030

9.0

940.

270

0.66

00.

820

5.00

010

.410

2.04

082

185

48.4

40.

78su

lphi

de b

x-st

ringe

rs a

nd b

.s.0.

040

95.0

930.

270

0.66

00.

260

5.44

06.

430

8.67

018

295

53.0

50.

46d.

s.0.

027

204.

058

- -

-12

.000

25.0

003.

000

8727

650

.77

0.52

d.s.

- int

erst

itial

0.12

164

0.0

218

- -

-53

.000

335.

000

33.0

0066

027

650

.31

0.52

d.s.

- int

erst

itial

1.78

086

02.0

3029

- -

-42

9.00

027

50.0

0026

1.00

070

3130

647

.92

0.45

d.s.

- int

erst

itial

3.18

315

941.

049

95 -

- -

549.

000

3218

.000

538.

000

9458

286

45.0

10.

46d.

s. - i

nter

stiti

al2.

169

1245

8.0

3535

- -

-50

3.00

033

64.0

0045

5.00

010

301

276

47.3

80.

49d.

s. - i

nter

stiti

al2.

341

1194

4.0

3698

- -

-42

3.00

024

38.0

0041

0.00

094

6829

646

.73

0.47

d.s.

- int

erst

itial

1.78

084

56.0

2284

- -

-28

3.00

015

41.0

0033

7.00

062

2731

648

.03

0.44

d.s.

- int

erst

itial

1.82

686

40.0

2790

- -

-28

5.00

016

23.0

0027

9.00

058

9134

647

.92

0.41

d.s.

- int

erst

itial

1.11

754

26.0

1626

- -

-16

0.00

090

5.00

016

0.00

037

6932

648

.75

0.43

d.s.

- int

erst

itial

0.71

647

00.0

1014

- -

-12

6.00

062

7.00

015

6.00

030

7230

648

.25

0.46

d.s.

0.09

756

8.0

161

- -

-17

.000

51.0

0015

.000

341

326

50.3

50.

46se

mi-m

assi

ve0.

160

348.

045

0.27

00.

660

0.26

09.

070

9.12

026

.800

7515

952

.66

1.10

d.s.

- per

vasi

ve a

nd m

agm

atic

0.05

360

0.0

760.

100

0.66

00.

260

1.43

03.

000

1.50

010

714

950

.85

0.98

none

vis

ible

0.01

4 -

125

0.20

00.

660

0.50

015

.000

15.0

001.

200

9425

650

.86

0.56

none

0.06

540

0.0

124

0.27

00.

660

1.10

021

.000

38.0

002.

200

9030

649

.97

0.48

none

0.03

940

0.0

117

0.20

00.

660

0.70

012

.000

20.0

001.

900

8625

649

.55

0.57

none

0.01

457

.031

10.

392

1.25

00.

873

5.47

06.

070

2.43

037

304

50.8

30.

35

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

JB97

-54B

JB97

-55

JB97

-56

JB97

-57

JB97

-58

JB97

-62

JB97

-67

JB97

-70B

JB97

-70C

JB97

-70D

JB97

-74A

JB97

-75

JB97

-76A

JB97

-77A

JB97

-77B

JB97

-78A

JB97

-84D

JB97

-87A

JB97

-87B

JB97

-87C

JB97

-87D

JB97

-87E

JB97

-87F

JB97

-87G

JB97

-87H

JB97

-87I

JB97

-87J

JB97

-87K

JB97

-93

JB97

-99

JB97

-103

EJB

97-1

06A

JB97

-106

CJB

98-1

14

Al2

O3

Fe2O

3*M

nOM

gOC

aON

a2O

K2O

P2O

5C

O2

SL

OI

M-T

otal

Mg#

Co

Cr*

VC

sR

bT

hU

Nb

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

13.2

014

.59

0.19

5.34

8.29

2.93

1.22

0.05

0.16

0.09

1.50

99.5

146

58na

330

0.28

51.9

62.

300.

684.

4814

.06

12.4

20.

196.

529.

122.

161.

470.

030.

090.

081.

2899

.68

5545

na26

01.

0863

.25

1.90

0.55

3.58

14.1

311

.85

0.19

6.74

10.2

42.

130.

960.

010.

140.

071.

0299

.55

5748

na26

01.

2938

.00

1.60

0.47

3.14

13.7

612

.82

0.20

6.40

10.0

22.

130.

920.

030.

160.

080.

9399

.75

5450

na28

01.

2035

.75

1.75

0.53

3.53

13.9

312

.68

0.19

6.38

10.3

02.

270.

640.

030.

180.

080.

9710

0.01

5450

na29

01.

3126

.09

1.74

0.54

3.54

16.1

411

.89

0.18

6.03

9.97

2.42

0.66

0.06

0.04

0.04

0.58

100.

6454

4611

320

61.

2625

.90

2.22

0.69

3.17

14.2

48.

790.

149.

2713

.07

1.54

0.44

0.04

na0.

032.

1510

0.28

7113

7130

2.68

13.9

70.

850.

261.

3715

.22

8.53

0.13

8.68

12.7

11.

660.

440.

030.

165.

112.

0810

0.35

7029

450

018

38.

2359

.93

1.46

0.47

1.94

11.9

49.

900.

1711

.70

11.7

21.

310.

380.

030.

220.

102.

1810

0.40

7347

367

208

1.05

14.7

60.

850.

271.

2312

.56

9.21

0.16

11.2

112

.24

1.32

0.40

0.03

0.23

0.07

1.55

100.

6374

4733

321

00.

5615

.46

0.90

0.28

1.22

5.64

3.45

0.01

1.76

0.40

2.48

0.12

0.01

0.05

1.05

1.69

100.

1754

3419

431

0.11

1.76

4.24

1.76

5.06

12.7

814

.51

0.22

3.15

6.84

2.29

1.48

0.24

0.32

0.03

0.55

100.

0034

4376

236

4.51

67.8

76.

051.

8419

.66

14.8

58.

060.

108.

498.

283.

360.

780.

06na

0.15

1.64

99.7

271

6046

323

41.

2224

.10

2.08

0.75

3.04

15.2

711

.52

0.13

6.00

9.04

3.61

0.90

0.03

0.40

0.19

0.96

99.1

155

37na

230

1.06

20.5

01.

730.

693.

9612

.50

13.9

30.

166.

627.

604.

090.

480.

050.

200.

851.

6210

0.10

5384

na30

00.

4010

.44

1.66

0.75

4.44

13.9

616

.41

0.13

9.68

0.66

0.63

5.97

0.02

0.31

0.17

2.14

98.8

258

36na

360

15.7

140

0.00

4.21

1.65

2.73

13.3

09.

010.

1610

.71

11.4

11.

610.

580.

050.

050.

040.

4510

0.79

7339

500

194

1.36

21.8

01.

650.

532.

2913

.83

10.0

70.

198.

3711

.37

1.14

0.56

0.07

na0.

033.

4510

0.34

6618

8553

1.51

20.3

51.

370.

431.

9913

.94

10.4

80.

188.

3111

.53

1.28

0.71

0.06

na0.

123.

0410

0.36

6520

5747

2.49

29.5

11.

320.

431.

9213

.66

12.9

00.

158.

0210

.30

0.46

0.18

0.07

na1.

783.

9598

.06

5997

159

420.

524.

641.

170.

361.

8313

.06

13.6

10.

167.

4310

.02

1.17

0.65

0.05

na3.

185.

4597

.07

5615

064

372.

7032

.40

1.08

0.32

1.60

13.0

713

.24

0.18

8.06

9.58

0.54

0.49

0.05

na2.

174.

4697

.54

5911

474

482.

0122

.98

1.16

0.37

1.81

13.4

712

.81

0.16

7.61

10.3

60.

670.

300.

06na

2.34

4.19

96.8

358

119

114

440.

8010

.18

1.16

0.35

1.65

13.6

412

.05

0.16

8.22

10.6

90.

160.

490.

07na

1.78

4.38

98.3

361

8877

441.

7620

.25

1.08

0.32

1.60

13.8

711

.64

0.15

8.18

11.2

30.

760.

430.

06na

1.83

3.49

98.1

462

9811

235

1.21

13.1

81.

010.

311.

4013

.70

10.9

30.

168.

5411

.30

0.96

0.52

0.05

na1.

123.

8199

.15

6560

8135

1.82

21.3

41.

030.

321.

5313

.69

10.0

60.

158.

4311

.59

1.17

0.43

0.06

na0.

724.

7999

.08

6649

148

370.

9614

.61

1.00

0.32

1.52

14.5

49.

170.

168.

4312

.28

0.91

0.43

0.07

na0.

103.

4110

0.21

6821

109

370.

9214

.43

1.13

0.35

1.69

16.2

811

.93

0.09

5.71

3.41

3.45

4.06

0.11

0.10

0.16

1.20

100.

0053

948

247

12.1

920

2.08

3.47

1.21

5.70

13.8

713

.91

0.22

5.89

6.69

3.37

1.33

0.11

na0.

053.

0310

0.25

50na

na26

90.

5053

.55

2.49

0.82

3.98

14.2

710

.70

0.19

8.50

11.9

41.

650.

420.

08na

0.01

1.14

100.

3165

nana

215

1.06

14.9

01.

290.

361.

9614

.51

9.61

0.17

8.32

10.9

91.

360.

630.

06na

0.07

3.97

100.

0767

nana

199

1.96

23.3

11.

260.

391.

8814

.13

10.2

50.

187.

9410

.52

1.95

0.62

0.07

na0.

044.

4710

0.25

64na

na20

70.

9021

.05

1.32

0.41

2.62

10.5

08.

790.

1413

.46

11.5

71.

460.

290.

00na

0.01

2.58

99.9

778

52na

230

0.60

6.82

0.79

0.25

1.33

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

JB97

-54B

JB97

-55

JB97

-56

JB97

-57

JB97

-58

JB97

-62

JB97

-67

JB97

-70B

JB97

-70C

JB97

-70D

JB97

-74A

JB97

-75

JB97

-76A

JB97

-77A

JB97

-77B

JB97

-78A

JB97

-84D

JB97

-87A

JB97

-87B

JB97

-87C

JB97

-87D

JB97

-87E

JB97

-87F

JB97

-87G

JB97

-87H

JB97

-87I

JB97

-87J

JB97

-87K

JB97

-93

JB97

-99

JB97

-103

EJB

97-1

06A

JB97

-106

CJB

98-1

14

Ta

La

Ce

PrSr

Nd

Zr

Hf

SmE

uT

i*G

dT

bD

yY

Ho

Er

Tm

Yb

Lu

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

0.30

9.83

22.2

52.

9118

9.10

13.3

0na

2.31

3.47

1.06

0.67

73.

610.

593.

84 -

0.81

2.22

0.32

2.12

0.32

0.26

7.87

17.6

12.

3122

3.50

10.1

2na

2.07

2.74

0.86

0.52

22.

720.

462.

97 -

0.65

1.77

0.25

1.66

0.25

0.36

7.12

15.7

92.

0923

2.20

9.45

na1.

822.

560.

820.

480

2.61

0.44

2.89

-0.

581.

680.

251.

500.

230.

277.

5817

.27

2.29

231.

9010

.43

na2.

022.

720.

880.

528

2.95

0.49

3.27

-0.

691.

820.

281.

780.

260.

527.

5517

.06

2.25

204.

3010

.42

na1.

982.

780.

900.

558

2.95

0.49

3.26

-0.

671.

820.

261.

760.

280.

238.

6619

.91

2.40

203.

5010

.09

na1.

932.

430.

930.

432

2.66

0.45

2.66

-0.

591.

570.

231.

550.

24 -

3.85

8.29

1.05

139.

304.

7130

.43

0.88

1.31

0.45

0.24

01.

610.

281.

8311

.41

0.39

1.16

0.17

1.08

0.17

0.21

5.16

11.2

21.

3831

.40

6.08

na1.

271.

280.

350.

276

1.45

0.26

1.66

-0.

381.

380.

161.

170.

180.

093.

657.

861.

0211

3.80

4.52

na0.

991.

130.

460.

234

1.42

0.27

1.63

-0.

391.

170.

161.

060.

150.

103.

447.

750.

9997

.10

4.37

na1.

081.

270.

400.

246

1.46

0.26

1.65

-0.

411.

150.

161.

120.

160.

755.

1210

.69

1.28

19.5

04.

95na

3.39

0.84

0.26

0.23

40.

600.

090.

38 -

0.10

0.65

0.04

0.34

0.06

1.35

26.2

658

.08

7.22

178.

4029

.63

na5.

326.

821.

832.

122

7.38

1.21

6.85

-1.

504.

060.

563.

810.

550.

255.

9013

.44

1.73

203.

107.

59na

1.72

2.16

0.72

0.43

82.

440.

442.

58 -

0.57

1.60

0.21

1.41

0.21

0.33

9.52

21.0

62.

7431

1.00

11.9

5na

1.35

3.05

1.22

0.49

82.

940.

473.

01 -

0.62

1.72

0.25

1.56

0.25

0.38

8.09

20.9

13.

0117

2.00

13.6

7na

2.20

3.60

0.96

0.61

13.

750.

654.

37 -

0.92

2.52

0.35

2.21

0.31

0.45

12.4

227

.40

3.41

40.2

013

.57

na2.

392.

530.

480.

468

1.79

0.22

1.18

-0.

190.

520.

060.

460.

080.

195.

9012

.42

1.50

105.

006.

62na

1.48

1.52

0.45

0.27

61.

600.

291.

84 -

0.42

1.18

0.16

1.13

0.17

na5.

4811

.85

1.50

140.

206.

5444

.03

1.26

1.72

0.54

0.31

21.

980.

342.

3513

.86

0.50

1.49

0.22

1.39

0.21

na5.

3611

.50

1.45

153.

306.

5242

.38

1.27

1.70

0.56

0.31

21.

990.

342.

3214

.06

0.51

1.49

0.22

1.39

0.22

na4.

8310

.44

1.34

123.

905.

8037

.84

1.15

1.51

0.49

0.27

01.

790.

322.

0912

.64

0.45

1.32

0.20

1.17

0.19

na4.

429.

651.

2512

0.00

5.45

35.4

31.

051.

480.

490.

276

1.68

0.30

2.01

11.8

90.

431.

240.

171.

180.

18na

4.87

10.1

31.

2811

2.30

5.54

39.0

81.

171.

460.

500.

294

1.75

0.31

2.10

12.3

40.

441.

340.

181.

260.

19na

4.84

10.4

61.

3512

9.50

5.75

35.7

51.

101.

500.

520.

282

1.65

0.31

2.10

12.6

40.

451.

330.

191.

200.

19na

4.53

9.84

1.25

116.

305.

3434

.80

1.05

1.46

0.48

0.26

41.

700.

301.

9411

.87

0.44

1.26

0.18

1.17

0.19

na4.

259.

291.

2012

8.40

5.07

31.5

80.

961.

380.

450.

246

1.64

0.28

1.91

11.3

90.

401.

200.

171.

150.

17na

4.42

9.52

1.22

130.

705.

2534

.76

0.99

1.32

0.48

0.25

81.

600.

281.

9911

.79

0.42

1.20

0.17

1.17

0.18

na4.

389.

591.

2415

5.10

5.23

34.0

01.

011.

370.

490.

276

1.72

0.29

1.96

12.1

90.

421.

240.

181.

110.

18na

4.81

10.4

61.

3215

4.70

5.72

37.2

51.

091.

510.

510.

276

1.75

0.30

2.09

12.6

60.

441.

290.

191.

250.

190.

4210

.87

26.0

93.

3216

2.80

13.3

1na

2.39

3.46

0.75

0.65

93.

970.

795.

05 -

1.08

2.80

0.37

2.29

0.29

na9.

7420

.82

2.64

324.

7011

.39

73.0

82.

172.

930.

960.

588

3.26

0.53

3.43

19.3

30.

692.

020.

281.

840.

28na

5.44

11.7

21.

5013

1.30

6.44

45.6

71.

281.

760.

580.

336

2.07

0.36

2.43

14.8

30.

521.

520.

221.

480.

22na

5.34

11.3

01.

4215

4.70

6.14

42.0

81.

181.

620.

530.

288

1.91

0.33

2.17

13.4

30.

461.

400.

201.

270.

21na

6.08

12.6

41.

5917

1.10

6.92

42.9

41.

211.

800.

580.

342

2.16

0.36

2.39

15.0

90.

521.

520.

221.

410.

220.

182.

435.

540.

7811

8.50

3.63

26.8

90.

831.

060.

360.

210

1.22

0.20

1.34

8.49

0.30

0.85

0.12

0.79

0.12

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

Tow

nshi

pSt

udy

Are

aD

escr

iptio

n 1

Roc

k T

ype

Fiel

d N

ame

JB98

-117

BN

airn

Nai

rn W

right

mg;

from

in tr

ench

gabb

roJB

98-1

17C

Nai

rnN

airn

Wrig

htm

g; fr

om in

tren

ch a

rea

- bla

st ro

ck; v

ery

wea

ther

ed; p

od-li

ke su

lphi

des

gabb

roJB

98-1

18W

ells

Bas

swoo

d Lk

Tra

vm

g; <

1% q

tz; b

ase

of la

rge

gabb

ro h

ill, w

est o

f HW

Y#1

29;q

tz?

gabb

roga

bbro

JB98

-148

Lorn

eB

ell L

ake

Trav

fg; s

mal

l o/c

on

N. s

ide

of o

ld ro

ad; ~

75m

at 3

15az

from

stat

. 147

-Tra

vers

ega

bbro

JB98

-149

Lorn

eB

ell L

ake

Trav

fg; s

mal

l o/c

in tr

ees;

~75

m a

t 315

az fr

om st

at. 1

48 -

Trav

erse

gabb

roJB

98-1

50Lo

rne

Bel

l Lak

e Tr

avfg

; rid

ge o

verlo

okin

g sh

allo

w v

alle

y &

pow

er li

nes;

~90

m fr

om st

at. 1

49

gabb

roJB

98-1

51C

Lorn

eB

ell L

ake

Trav

fg; T

RA

VER

SE E

ND

- no

rther

nmos

t edg

e of

ridg

e by

old

pit;

~15

m fr

om st

at. 1

50ga

bbro

JB98

-174

Cur

tinC

harlt

on L

k C

liff

fg; ~

30m

NW

of s

tat.

173;

trav

erse

gabb

roJB

98-1

75C

urtin

Cha

rlton

Lk

Clif

fm

g; ~

5m N

W o

f sta

t. 17

4; tr

aver

sega

bbro

JB98

-177

Cur

tinC

harlt

on L

k C

liff

mg;

~5m

NW

of s

tat.

176;

nea

r con

tact

w g

abbr

o; tr

aver

sega

bbro

JB98

-178

Cur

tinC

harlt

on L

k C

liff

mg;

~50

m N

W o

f sta

t. 17

7; tr

aver

sega

bbro

JB98

-179

Cur

tinC

harlt

on L

k C

liff

mg-

cg; ~

50m

NW

of s

tat.

178;

trav

erse

gabb

roJB

98-1

80C

urtin

Cha

rlton

Lk

Clif

fm

g; ~

50m

NW

of s

tat.

179;

~30

m E

of s

hore

; tra

vers

ega

bbro

JB98

-181

Cur

tinC

harlt

on L

k C

liff

mg-

cg; ~

50m

NW

of s

tat.

180;

~35

m E

of s

hore

; tra

vers

ega

bbro

JB98

-183

Cur

tinC

harlt

on L

k C

liff

mg;

~50

m N

W o

f sta

t. 18

2; ~

15m

E o

f sho

re; t

rave

rse

gabb

roJB

98-1

84C

urtin

Cha

rlton

Lk

Clif

fm

g; ~

50m

NW

of s

tat.

183;

SE

of c

abin

; tra

vers

ega

bbro

JB98

-190

ER

athb

unR

athb

unm

g; R

athb

un L

ake

Show

ing;

from

mai

n pi

t are

aga

bbro

JB98

-194

Kel

lyC

araf

el B

ay T

rav

fg-m

g; T

RA

VER

SE S

TAR

T - ~

7m u

p hi

ll fa

ce fr

om N

. sho

re o

f Car

afel

Bay

gabb

roJB

98-1

95K

elly

Car

afel

Bay

Tra

vm

g; m

t-bea

ring;

~30

m fr

om la

ke sh

ore

- Tra

vers

ega

bbro

JB98

-196

Kel

lyC

araf

el B

ay T

rav

mg;

mt-b

earin

g; ~

75m

from

lake

shor

e; g

rano

phyr

ic ro

ck in

are

a - T

rave

rse

gabb

roJB

98-1

98K

elly

Car

afel

Bay

Tra

vm

g-cg

; ~50

m N

. of l

ast s

tatio

n; fr

om o

vertu

rned

tree

; peg

. in

area

- Tr

aver

sega

bbro

JB98

-199

Kel

lyC

araf

el B

ay T

rav

mg;

~80

m N

. of l

ast;

in tr

ees -

Tra

vers

ega

bbro

JB98

-200

Kel

lyC

araf

el B

ay T

rav

mg;

~10

0m N

. of l

ast -

Tra

vers

ega

bbro

JB98

-201

Kel

lyC

araf

el B

ay T

rav

mg;

~10

0m fr

om la

st; u

p on

hill

ove

r low

are

a - t

rave

rse

gabb

roJB

98-2

02K

elly

Car

afel

Bay

Tra

vm

g; ~

100m

from

last

- tra

vers

ega

bbro

JB98

-203

Kel

lyC

araf

el B

ay T

rav

mg;

on

high

hill

ove

rlook

ing

valle

y; N

/S v

alle

y to

wes

t and

E/W

to so

uth;

trav

erse

gabb

roJB

98-2

05K

elly

Car

afel

Bay

Tra

vm

g; m

t-bea

ring;

hig

hest

poi

nt o

n hi

ll - t

rave

rse

gabb

roJB

98-2

06K

elly

Car

afel

Bay

Tra

vm

g; m

t-bea

ring;

~10

0m N

. of l

ast -

Tra

vers

ega

bbro

JB98

-209

ALo

uise

Loui

e La

kem

g; 3

+00E

Pit

b/w

8+0

0 an

d 8+

50 so

uth;

new

ly b

last

edga

bbro

JB98

-209

BLo

uise

Loui

e La

kem

g; 3

+00E

Pit

b/w

8+0

0 an

d 8+

50 so

uth;

new

ly b

last

edga

bbro

JB98

-209

CLo

uise

Loui

e La

kem

g-cg

; 3+0

0E P

it b/

w 8

+00

and

8+50

sout

h; n

ewly

bla

sted

gabb

roJB

98-2

09D

Loui

seLo

uie

Lake

mg;

3+0

0E P

it b/

w 8

+00

and

8+50

sout

h; n

ewly

bla

sted

; mas

sive

sulp

hide

gabb

roJB

98-2

10A

Loui

seLo

uie

Lake

fg; f

rom

con

tact

are

a w

ith fr

ags o

f sed

in fg

-mg

gabb

roga

bbro

JB98

-212

BLo

uise

Loui

e La

kem

g; la

rge

mai

n pi

t vis

ited

last

yea

r - 1

997

gabb

ro

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

JB98

-117

BJB

98-1

17C

JB98

-118

JB98

-148

JB98

-149

JB98

-150

JB98

-151

CJB

98-1

74JB

98-1

75JB

98-1

77JB

98-1

78JB

98-1

79JB

98-1

80JB

98-1

81JB

98-1

83JB

98-1

84JB

98-1

90E

JB98

-194

JB98

-195

JB98

-196

JB98

-198

JB98

-199

JB98

-200

JB98

-201

JB98

-202

JB98

-203

JB98

-205

JB98

-206

JB98

-209

AJB

98-2

09B

JB98

-209

CJB

98-2

09D

JB98

-210

AJB

98-2

12B

Sulp

hide

/Oxi

deS

SeN

iIr

Ru

Rh

PtPd

Au

Cu

Al2

O3

SiO

2Si

O2

TiO

2w

t%pp

bpp

mpp

bpp

bpp

bpp

bpp

bpp

bpp

mTi

O2

MgO

wt%

wt%

diss

and

ble

b; c

py>p

o>pn

1.30

031

45.0

1202

0.54

51.

190

1.43

032

.000

41.2

0011

.560

695

364

53.4

00.

25po

>cpy

>pn;

mas

sive

7.63

031

.037

663.

020

6.55

06.

090

218.

100

122.

600

84.6

0012

2926

547

.27

0.32

none

0.03

318

7.0

104

0.27

00.

241

1.07

98.

160

23.3

604.

310

140

188

51.4

40.

82no

ne0.

008

32.0

376

1.12

42.

380

2.50

012

.770

4.30

01.

060

3321

352

.19

0.27

none

0.00

544

.033

21.

301

2.50

01.

900

12.1

406.

480

0.76

316

253

51.0

40.

27no

ne0.

005

44.0

293

1.14

62.

540

1.54

013

.260

6.12

00.

645

3021

351

.29

0.40

none

0.00

519

.026

40.

841

1.94

01.

410

11.6

907.

090

1.43

039

214

51.3

30.

44d.

s.; n

ear c

onta

ct w

ith se

ds0.

285

1036

.013

90.

270

0.66

00.

320

8.79

010

.560

13.2

0041

226

750

.66

0.55

<<1%

d.s.

a/w

qtz

vei

ning

0.03

419

1.0

120

0.27

00.

160

0.20

28.

600

7.11

03.

040

104

376

50.1

10.

42d.

s.0.

017

105.

083

0.27

00.

190

0.26

01.

320

1.19

01.

890

154

237

52.6

60.

61no

ne0.

031

155.

011

80.

270

0.15

00.

260

1.57

01.

830

2.56

086

266

50.6

30.

53no

ne0.

070

366.

014

80.

270

0.37

00.

092

1.67

71.

750

2.23

022

125

551

.06

0.50

none

0.07

623

4.0

131

0.27

00.

660

0.26

01.

780

1.47

01.

940

161

305

51.1

90.

44no

ne0.

078

364.

098

0.27

00.

320

0.48

00.

238

0.28

21.

630

143

317

51.0

50.

48d.

s.; ru

sty

patc

hes

0.23

217

33.0

511

0.26

70.

640

1.82

058

.000

156.

000

33.5

0087

031

549

.96

0.41

none

0.03

524

1.0

175

0.07

00.

500

0.66

313

.980

55.5

004.

510

120

325

50.2

70.

44d.

s. an

d bl

eb; c

py >

> po

10.5

0088

425.

093

670.

326

7.80

0C

u-In

t39

61.0

0062

30.0

0094

1.00

037

7129

188

35.0

60.

69no

n-m

agne

tic0.

054

292.

011

70.

053

0.35

00.

434

8.35

09.

510

3.65

011

825

651

.66

0.58

10%

mag

netit

e0.

056

267.

011

60.

270

0.66

00.

277

10.6

1011

.020

2.88

010

425

751

.53

0.57

20-3

0% m

agne

tite

0.03

218

1.0

134

0.27

00.

660

0.30

914

.450

13.1

801.

420

111

356

51.1

90.

43pa

tchy

mag

netis

m (p

o?)

0.08

539

4.0

155

0.27

00.

130

0.26

01.

310

1.33

02.

500

227

246

51.4

70.

54m

ay b

e po

/ no

t mt a

s fin

e ds

0.01

320

4.0

119

0.27

00.

660

0.26

01.

290

0.97

02.

720

138

266

52.0

00.

52pa

tchy

mag

netis

m (p

o?)

0.03

726

1.0

150

0.27

00.

660

0.09

82.

570

2.23

03.

700

168

305

51.1

80.

4310

% m

t; no

v.s.

; dis

s. po

?0.

035

212.

015

30.

270

0.13

00.

096

4.10

03.

200

5.30

015

031

551

.76

0.45

10%

mt;

may

be

diss

. po?

0.07

831

1.0

148

0.27

00.

660

0.14

27.

730

7.56

05.

740

144

246

52.3

50.

57pa

tchy

mag

netis

m (p

o?)

0.05

514

7.0

150

0.05

00.

660

0.38

78.

000

9.41

02.

470

8231

551

.16

0.46

d.s.

0.01

686

.018

20.

127

0.19

00.

750

9.78

024

.600

2.63

087

395

51.0

70.

36pa

tchy

mag

netis

m (p

o?)

0.03

915

5.0

146

0.06

50.

150

0.44

610

.700

10.1

003.

280

8832

551

.92

0.45

d.s./

b.s.

- at c

onta

ct w

wal

l rck

7.39

013

560.

095

70.

512

0.83

02.

930

30.6

007.

910

7.10

014

6343

553

.69

0.15

in m

ain

area

of s

ulph

ide

pod

28.9

003.

531

781.

940

3.61

05.

860

156.

500

173.

700

38.8

0089

141

1020

.42

0.07

wal

l roc

k "a

bove

" su

lph

pod

0.03

315

4.0

990.

208

0.38

01.

170

33.2

0029

.800

2.88

034

416

63.9

00.

20m

assi

ve fr

om p

it29

.700

3.5

3332

1.68

02.

990

4.06

062

.400

278.

000

8.34

070

163

1018

.78

0.04

0.11

431

9.0

122

0.05

50.

140

0.38

410

.830

11.7

805.

580

138

256

51.3

40.

59m

ainl

y po

; cpy

in g

ab0.

125

319.

018

50.

063

0.66

00.

279

10.1

0012

.310

6.89

031

248

449

.82

0.29

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

JB98

-117

BJB

98-1

17C

JB98

-118

JB98

-148

JB98

-149

JB98

-150

JB98

-151

CJB

98-1

74JB

98-1

75JB

98-1

77JB

98-1

78JB

98-1

79JB

98-1

80JB

98-1

81JB

98-1

83JB

98-1

84JB

98-1

90E

JB98

-194

JB98

-195

JB98

-196

JB98

-198

JB98

-199

JB98

-200

JB98

-201

JB98

-202

JB98

-203

JB98

-205

JB98

-206

JB98

-209

AJB

98-2

09B

JB98

-209

CJB

98-2

09D

JB98

-210

AJB

98-2

12B

Al2

O3

Fe2O

3*M

nOM

gOC

aON

a2O

K2O

P2O

5C

O2

SL

OI

M-T

otal

Mg#

Co

Cr*

VC

sR

bT

hU

Nb

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

8.92

13.2

10.

1212

.77

3.16

0.52

0.04

0.04

na1.

307.

4499

.87

6912

9na

337

0.37

2.58

5.32

2.30

3.95

8.18

24.3

10.

089.

931.

630.

490.

580.

04na

7.63

5.32

98.1

549

425

na41

51.

4127

.12

6.03

1.94

4.51

14.9

311

.30

0.18

6.28

8.17

2.98

1.17

0.09

na0.

032.

9310

0.29

5648

na20

01.

5454

.19

2.88

0.85

4.02

5.67

10.2

40.

2018

.69

10.7

11.

130.

140.

02na

0.00

80.

9410

0.20

8166

na27

40.

866.

240.

540.

170.

876.

689.

800.

1917

.41

9.53

1.51

0.13

0.02

na0.

005

3.80

100.

3881

60na

229

0.42

3.97

0.84

0.22

1.12

8.21

10.3

20.

1815

.63

9.15

1.12

0.36

0.02

na0.

005

3.68

100.

3678

58na

222

1.88

19.2

41.

040.

341.

669.

1910

.09

0.19

14.3

99.

271.

760.

430.

03na

0.00

53.

2410

0.36

77na

nana

4.62

27.1

11.

160.

331.

8614

.30

9.98

0.15

7.36

10.6

63.

500.

200.

05na

0.29

2.90

100.

3163

50na

210

0.10

5.66

1.69

0.54

2.17

15.4

08.

770.

148.

4010

.71

1.73

1.11

0.03

na0.

033.

4710

0.29

6935

na18

80.

4144

.09

1.05

0.30

1.46

14.2

610

.03

0.18

7.09

7.70

3.09

0.85

0.04

na0.

023.

6510

0.16

6236

na22

80.

2529

.51

2.66

0.84

3.00

13.8

111

.23

0.19

9.08

9.06

2.06

0.69

0.02

na0.

033.

1010

0.40

6554

na21

60.

2421

.42

1.99

0.58

2.22

12.7

39.

760.

189.

999.

841.

391.

010.

01na

0.07

3.86

100.

3370

46na

221

1.74

52.2

21.

620.

542.

1213

.16

9.51

0.16

9.91

10.1

61.

750.

810.

02na

0.08

3.14

100.

2571

39na

206

1.12

38.3

01.

370.

451.

6314

.68

9.17

0.15

7.60

10.0

62.

060.

860.

03na

0.08

4.18

100.

3266

40na

208

0.81

39.9

01.

690.

562.

0312

.81

9.18

0.15

10.9

910

.98

1.78

0.76

0.01

na0.

233.

0910

0.12

7450

na20

01.

2524

.11

1.13

0.36

1.42

14.0

57.

990.

149.

6911

.88

2.16

0.78

0.03

na0.

042.

8310

0.26

7437

na19

61.

2029

.52

1.02

0.32

1.57

12.4

621

.19

0.07

4.23

0.86

0.02

0.91

0.03

na10

.50

24.4

799

.99

3217

0na

208

2.16

36.0

42.

711.

052.

7714

.63

10.0

60.

178.

1811

.30

1.96

0.58

0.04

na0.

050.

8299

.98

6545

na23

11.

3621

.88

1.70

0.54

2.33

14.4

710

.45

0.18

7.82

11.1

51.

970.

520.

03na

0.06

1.21

99.8

964

44na

236

1.40

22.2

31.

770.

552.

4815

.26

8.89

0.16

8.84

11.8

61.

980.

500.

03na

0.03

1.12

100.

2670

43na

204

1.45

16.1

01.

130.

351.

7012

.84

10.5

50.

189.

2911

.17

1.75

0.61

0.03

na0.

091.

6810

0.11

6750

na24

91.

9523

.24

1.42

0.46

2.08

13.7

410

.28

0.17

8.73

10.9

81.

920.

510.

05na

0.01

0.79

99.6

966

46na

230

0.90

16.7

61.

600.

492.

1013

.01

10.0

20.

1610

.17

11.7

51.

960.

420.

02na

0.04

1.09

100.

2170

47na

217

1.58

14.7

21.

120.

331.

6013

.83

9.09

0.17

10.0

411

.78

1.63

0.50

0.03

na0.

040.

7910

0.07

7244

na21

70.

9213

.67

1.20

0.37

1.55

13.6

59.

690.

178.

8211

.03

1.74

0.69

0.05

na0.

081.

5110

0.27

6844

na23

51.

5022

.62

1.54

0.48

2.24

14.1

08.

760.

179.

8911

.66

1.68

0.64

0.05

na0.

061.

7310

0.30

7240

na20

11.

9824

.50

1.20

0.40

1.65

14.2

08.

110.

1610

.45

13.5

31.

440.

310.

02na

0.02

0.64

100.

2975

40na

198

0.48

9.61

0.80

0.26

1.29

14.3

48.

770.

159.

5111

.74

1.77

0.55

0.03

na0.

040.

7299

.95

7241

na20

30.

9515

.06

1.27

0.38

1.81

6.45

17.3

40.

0810

.51

3.41

0.87

0.11

0.00

na7.

396.

4699

.07

5924

5na

720.

406.

384.

171.

663.

052.

8959

.19

0.02

2.04

0.66

0.01

0.19

0.00

na28

.90

14.7

510

0.24

776

3na

430.

178.

612.

371.

191.

618.

255.

580.

0911

.34

4.98

1.87

0.06

0.03

na0.

033.

7610

0.06

8315

na86

0.52

0.71

1.34

2.88

2.52

60.4

10.

011.

900.

480.

010.

140.

03na

29.7

015

.56

99.8

87

829

na45

0.19

7.26

2.05

0.93

1.35

14.5

09.

110.

148.

3310

.30

2.01

0.98

0.04

na0.

113.

0510

0.39

6836

na21

11.

0241

.90

1.58

0.44

2.22

13.9

58.

090.

1511

.62

11.9

31.

590.

290.

02na

0.13

2.59

100.

3477

28na

163

0.52

11.5

50.

850.

231.

18

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

JB98

-117

BJB

98-1

17C

JB98

-118

JB98

-148

JB98

-149

JB98

-150

JB98

-151

CJB

98-1

74JB

98-1

75JB

98-1

77JB

98-1

78JB

98-1

79JB

98-1

80JB

98-1

81JB

98-1

83JB

98-1

84JB

98-1

90E

JB98

-194

JB98

-195

JB98

-196

JB98

-198

JB98

-199

JB98

-200

JB98

-201

JB98

-202

JB98

-203

JB98

-205

JB98

-206

JB98

-209

AJB

98-2

09B

JB98

-209

CJB

98-2

09D

JB98

-210

AJB

98-2

12B

Ta

La

Ce

PrSr

Nd

Zr

Hf

SmE

uT

i*G

dT

bD

yY

Ho

Er

Tm

Yb

Lu

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

0.46

16.5

332

.08

3.71

6.90

13.9

277

.96

2.61

2.57

0.64

0.15

02.

420.

382.

7816

.75

0.54

1.74

0.25

1.84

0.30

0.43

15.2

030

.29

3.72

17.9

013

.78

77.7

12.

542.

720.

250.

192

2.20

0.34

2.31

13.7

90.

451.

450.

201.

400.

220.

3910

.94

22.5

42.

9323

5.50

12.3

666

.32

2.15

2.96

0.99

0.49

23.

020.

493.

1417

.96

0.67

1.91

0.24

1.67

0.26

0.13

2.39

5.10

0.71

60.5

03.

0919

.72

0.64

0.91

0.28

0.16

21.

020.

181.

307.

400.

260.

750.

100.

650.

110.

143.

127.

151.

0058

.50

4.35

19.4

20.

671.

150.

380.

162

1.22

0.20

1.32

7.90

0.28

0.78

0.11

0.70

0.11

0.19

5.21

10.2

91.

3196

.80

5.60

31.1

61.

011.

260.

460.

240

1.44

0.24

1.65

9.88

0.35

0.98

0.14

0.92

0.14

0.20

4.12

8.91

1.20

135.

205.

3734

.07

1.06

1.43

0.45

0.26

41.

590.

261.

7410

.93

0.38

1.04

0.15

0.99

0.15

0.23

6.66

13.6

61.

8120

9.30

7.48

45.1

91.

391.

960.

750.

330

2.28

0.38

2.59

16.0

90.

581.

640.

231.

470.

240.

184.

249.

151.

2119

1.50

5.46

31.8

60.

941.

390.

510.

252

1.55

0.27

1.94

12.7

00.

481.

270.

181.

240.

200.

2910

.37

20.9

62.

6815

9.10

10.9

762

.05

1.92

2.66

0.81

0.36

62.

730.

443.

2519

.74

0.67

1.92

0.27

1.74

0.28

0.24

7.10

14.4

01.

8613

5.10

7.92

42.5

41.

451.

940.

600.

318

1.99

0.36

2.30

14.0

20.

481.

400.

201.

350.

220.

226.

4413

.35

1.65

154.

107.

0640

.52

1.30

1.78

0.54

0.30

01.

900.

332.

2214

.04

0.49

1.39

0.20

1.36

0.21

0.18

5.33

10.6

61.

4113

4.80

6.03

33.8

11.

121.

630.

580.

264

1.79

0.31

2.03

12.3

10.

441.

250.

181.

320.

210.

226.

3212

.83

1.65

171.

706.

8640

.48

1.34

1.75

0.58

0.28

82.

040.

362.

3614

.02

0.48

1.43

0.21

1.48

0.21

0.16

4.38

9.13

1.17

148.

105.

1529

.17

0.99

1.38

0.46

0.24

61.

600.

271.

8011

.42

0.39

1.20

0.18

1.16

0.17

0.17

4.46

9.31

1.27

155.

805.

3234

.54

1.13

1.41

0.47

0.26

41.

750.

292.

0112

.50

0.43

1.22

0.18

1.25

0.18

0.29

7.15

13.5

31.

5275

.40

5.42

34.6

11.

190.

980.

510.

414

0.75

0.13

0.85

5.07

0.17

0.53

0.08

0.60

0.09

0.24

6.82

13.9

41.

8213

6.70

7.84

45.3

01.

522.

010.

650.

348

2.32

0.40

2.71

15.9

20.

561.

640.

231.

580.

260.

266.

7614

.05

1.82

153.

207.

9748

.34

1.50

2.16

0.66

0.34

22.

350.

402.

7216

.31

0.58

1.72

0.25

1.67

0.25

0.18

4.64

9.78

1.32

156.

605.

5933

.88

1.12

1.46

0.50

0.25

81.

650.

292.

0112

.38

0.41

1.34

0.18

1.13

0.19

0.22

5.86

12.3

31.

6215

3.60

7.09

40.2

61.

441.

800.

620.

324

2.15

0.38

2.49

15.4

90.

541.

600.

231.

700.

250.

216.

4213

.14

1.71

148.

307.

2144

.31

1.44

1.87

0.60

0.31

22.

270.

392.

5315

.37

0.53

1.59

0.24

1.54

0.24

0.16

4.54

9.40

1.27

123.

405.

3932

.88

1.10

1.48

0.50

0.25

81.

770.

301.

9612

.08

0.43

1.24

0.19

1.23

0.21

0.18

4.63

9.82

1.29

135.

505.

6835

.54

1.15

1.55

0.50

0.27

01.

720.

302.

0312

.52

0.44

1.30

0.18

1.32

0.18

0.22

6.20

13.0

91.

7315

0.50

7.49

45.2

61.

581.

980.

560.

342

2.13

0.36

2.52

15.7

90.

531.

580.

241.

490.

240.

185.

0110

.34

1.41

135.

305.

7735

.03

1.14

1.48

0.49

0.27

61.

760.

292.

1412

.79

0.44

1.29

0.19

1.21

0.20

0.15

3.84

7.94

1.08

119.

904.

7028

.06

0.93

1.24

0.41

0.21

61.

530.

271.

8110

.92

0.38

1.09

0.16

1.10

0.17

0.19

5.20

10.8

61.

4116

3.20

6.28

37.7

41.

181.

680.

580.

270

1.87

0.30

2.18

13.4

20.

491.

380.

201.

240.

200.

367.

5416

.12

1.92

19.9

07.

5876

.31

2.46

1.36

0.29

0.09

01.

250.

181.

327.

720.

250.

850.

140.

870.

130.

244.

169.

141.

1211

.30

4.34

28.4

40.

960.

800.

170.

042

0.68

0.10

0.72

3.59

0.11

0.38

0.06

0.36

0.05

0.40

10.6

524

.99

3.13

28.8

012

.32

95.6

63.

092.

250.

300.

120

1.68

0.24

1.59

3.73

0.30

0.95

0.12

0.72

0.11

0.19

3.58

8.04

0.96

8.70

3.69

41.6

11.

140.

610.

140.

024

0.50

0.07

0.50

3.19

0.10

0.32

0.05

0.30

0.05

0.21

6.01

12.5

81.

6515

4.90

6.99

46.5

31.

451.

710.

520.

354

2.10

0.37

2.42

14.1

30.

521.

450.

201.

390.

200.

144.

057.

841.

0011

5.90

4.08

24.0

70.

780.

960.

380.

174

1.12

0.20

1.41

8.28

0.30

0.93

0.14

0.90

0.12

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

Tow

nshi

pSt

udy

Are

aD

escr

iptio

n 1

Roc

k T

ype

Fiel

d N

ame

JB98

-225

AC

urtin

Cas

son

mg;

"m

alac

hite

pit"

; ne

ar L

2+00

Wga

bbro

JB98

-228

Cur

tinC

asso

n A

N3

Trav

mg;

TR

AV

ERSE

STA

RT

- Eas

t of A

N-3

; hea

din

180;

~10

m n

orth

of t

rail

gabb

roJB

98-2

29C

urtin

Cas

son

AN

3 Tr

avm

g; ~

50m

sout

h of

228

- Tr

aver

sega

bbro

JB98

-230

Cur

tinC

asso

n A

N3

Trav

mg;

~50

m so

uth

of 2

29 -

Trav

erse

gabb

roJB

98-2

31C

urtin

Cas

son

AN

3 Tr

avm

g; ~

75m

sout

h of

230

- Tr

aver

se; e

dge

of h

illga

bbro

JB98

-239

DK

elly

Kuk

agam

i Clif

ffg

-mg;

~9.

5m u

p si

de o

f hill

on

"pat

h" -

wes

t end

; tra

vers

ega

bbro

JB98

-239

EK

elly

Kuk

agam

i Clif

fm

g; ~

13.5

m u

p si

de o

f hill

on

"pat

h" -

wes

t end

; tra

vers

ega

bbro

JB98

-239

FK

elly

Kuk

agam

i Clif

fm

g; T

RA

VER

SE E

ND

; ~16

.25m

up

hill

on "

path

" - w

est e

nd; v

t gab

bro

area

gabb

roR

K-1

Wat

ers

Mak

ada

Trav

erse

mg-

vcg;

grid

115

N/1

20E;

from

pit#

2; m

iner

aliz

edga

bbro

RK

-2W

ater

sM

akad

a Tr

aver

sem

g-vc

g; g

rid 1

15N

/120

E; fr

om p

it#2;

min

eral

ized

gabb

roR

K-3

Wat

ers

Mak

ada

Trav

erse

mg-

vcg;

grid

115

N/1

20E;

from

pit#

2; m

iner

aliz

edga

bbro

RK

-4W

ater

sM

akad

a Tr

aver

sem

g-vc

g; g

rid 1

15N

/120

E; fr

om p

it#2;

min

eral

ized

gabb

roR

K-5

Wat

ers

Mak

ada

Trav

erse

mg;

grid

40N

/85E

gabb

roR

K-7

Wat

ers

Mak

ada

Trav

erse

fg-m

g; g

rid 1

30N

/55E

gabb

roR

K-8

Wat

ers

Mak

ada

Trav

erse

mg;

grid

180

N/3

5Ega

bbro

RK

-9W

ater

sM

akad

a Tr

aver

sem

g; g

rid 2

40N

/15E

gabb

roR

K-1

0W

ater

sM

akad

a Tr

aver

sem

g-cg

; grid

260

N/2

0Wga

bbro

RK

-11

Wat

ers

Mak

ada

Trav

erse

mg;

grid

70N

/60W

gabb

roR

K-1

2W

ater

sM

akad

a Tr

aver

sem

g; g

rid 4

0N/8

0Wga

bbro

RK

-13

Wat

ers

Mak

ada

Trav

erse

mg-

cg; g

rid 2

40S/

110W

gabb

roR

K-1

4W

ater

sM

akad

a Tr

aver

sem

g; g

rid 3

40S/

110W

gabb

roR

K-1

5W

ater

sM

akad

a Tr

aver

sem

g; n

orth

east

of p

rope

rty g

ridga

bbro

RK

-16

Wat

ers

Mak

ada

Trav

erse

mg;

nor

thea

st o

f pro

perty

grid

gabb

roR

K-1

7W

ater

sM

akad

a Tr

aver

sem

g; n

orth

east

of p

rope

rty g

ridga

bbro

RK

-18

Wat

ers

Mak

ada

Trav

erse

cg-v

cg; g

rid 6

0S/6

0Ega

bbro

RK

-19

Wat

ers

Mak

ada

Trav

erse

cg-p

eg; g

rid 1

50S/

110E

gabb

roJB

97-5

0W

ells

App

leby

Lk

Trav

App

leby

Lk;

mg-

vcg

gabb

ro w

pin

k st

aine

d fs

par

gran

oph

gabb

roJB

97-5

4AW

ells

App

leby

Lk

Trav

App

leby

Lk;

Q-C

vei

ns in

alte

red

and

pink

stai

ned

gabb

ro(?

); ~2

' wid

e se

ctio

ngr

anop

h ga

bbro

JB97

-63

Wel

lsB

assw

ood

Lk T

rav

mg

gabb

ro w

pin

k fs

par s

tain

ing

gran

oph

gabb

roJB

98-1

22B

ridgl

and

Bas

swoo

d Lk

Tra

vm

g-cg

; S. o

f #12

9; ra

diat

ing

amph

ib. l

aths

; pin

k fs

par;

gran

ophy

ric g

abbr

ogr

anop

h ga

bbro

JB97

-14

Kel

lyW

asha

gam

i Lak

em

g; so

uth

edge

of h

igh

o/c

hill

opx

gabb

roJB

97-1

5K

elly

Was

haga

mi L

ake

mg;

sout

h ed

ge o

f nex

t hig

h o/

c hi

llop

x ga

bbro

JB97

-16

Kel

lyW

asha

gam

i Lak

em

g; so

uth

edge

of s

mal

l kno

b so

uth

of p

eak

but o

n cl

aim

line

opx

gabb

roJB

97-4

3AJa

nes

Chi

nigu

chi

mg;

po

slig

htly

> th

an c

py b

ut c

lose

to 1

:1 ra

tio; F

alco

-tren

ches

opx

gabb

ro

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

JB98

-225

AJB

98-2

28JB

98-2

29JB

98-2

30JB

98-2

31JB

98-2

39D

JB98

-239

EJB

98-2

39F

RK

-1R

K-2

RK

-3R

K-4

RK

-5R

K-7

RK

-8R

K-9

RK

-10

RK

-11

RK

-12

RK

-13

RK

-14

RK

-15

RK

-16

RK

-17

RK

-18

RK

-19

JB97

-50

JB97

-54A

JB97

-63

JB98

-122

JB97

-14

JB97

-15

JB97

-16

JB97

-43A

Sulp

hide

/Oxi

deS

SeN

iIr

Ru

Rh

PtPd

Au

Cu

Al2

O3

SiO

2Si

O2

TiO

2w

t%pp

bpp

mpp

bpp

bpp

bpp

bpp

bpp

bpp

mTi

O2

MgO

wt%

wt%

2.45

066

81.0

1447

1.02

01.

560

5.51

026

4.00

038

4.00

016

6.00

028

6334

448

.01

0.35

0.00

911

3.0

166

0.14

70.

280

0.91

021

.500

46.5

005.

500

6938

549

.51

0.37

0.01

515

3.0

172

0.11

60.

260

0.86

017

.180

63.8

004.

570

9038

449

.47

0.35

0.04

531

8.0

198

0.11

40.

250

0.57

033

.400

42.3

0015

.300

176

405

49.5

00.

350.

044

314.

015

50.

045

0.66

00.

224

9.67

09.

440

4.79

010

830

551

.16

0.40

0.08

722

1.0

120

- -

- -

- -

9528

651

.07

0.53

0.05

323

7.0

132

- -

- -

- -

112

286

50.5

40.

530.

024

180.

094

- -

- -

- -

7330

750

.93

0.52

0.71

281

0.0

500

0.29

00.

910

0.88

07.

240

9.60

08.

170

181

214

56.6

70.

330.

011

35.0

214

0.22

01.

050

1.48

06.

240

4.18

02.

090

1444

551

.30

0.28

1.41

012

92.0

679

0.46

01.

330

1.30

010

.700

12.5

9016

.700

349

194

55.5

10.

3536

.300

41.0

1049

00.

270

0.66

00.

260

1.43

01.

490

1.72

064

55

10.

450.

160.

038

219.

067

0.27

00.

660

0.26

00.

200

1.88

03.

480

136

1214

53.7

41.

190.

013

74.0

248

0.55

01.

410

1.23

07.

350

6.36

01.

820

7125

451

.08

0.43

0.01

887

.025

90.

570

1.45

01.

120

7.63

06.

590

1.49

073

234

51.9

10.

470.

014

65.0

338

1.05

02.

590

1.59

09.

270

5.38

01.

300

4615

352

.45

0.41

0.01

261

.033

51.

100

2.63

01.

850

11.0

605.

640

1.21

046

153

52.3

80.

410.

023

73.0

346

1.09

02.

580

1.84

09.

960

5.53

01.

370

5016

352

.78

0.38

0.01

464

.032

71.

040

2.46

01.

540

9.19

05.

300

1.37

045

153

52.7

90.

420.

021

84.0

137

0.06

00.

350

0.51

06.

220

7.80

01.

230

6134

751

.05

0.49

0.01

978

.013

80.

050

0.42

00.

520

6.30

08.

930

1.67

066

337

50.8

20.

500.

014

80.0

117

0.27

00.

310

0.44

04.

400

5.27

01.

100

6336

850

.75

0.50

0.01

142

.020

70.

140

0.91

00.

800

4.36

05.

940

1.42

038

475

50.5

60.

300.

021

88.0

176

0.15

00.

670

0.49

03.

120

4.44

01.

510

7326

550

.95

0.52

0.01

158

.034

21.

340

2.71

01.

800

11.3

705.

820

1.20

050

153

52.4

40.

390.

014

85.0

117

0.27

00.

330

0.41

04.

640

5.86

01.

030

6039

850

.74

0.48

none

0.11

034

7.0

650.

270

0.66

00.

260

1.43

02.

060

67.7

6017

09

1151

.72

1.37

d.s.

w v

eins

and

blo

bs o

f py

0.93

040

2.0

350.

270

0.66

00.

260

0.16

01.

880

76.1

0084

2325

51.4

90.

48no

ne0.

080

511.

082

0.27

00.

660

0.15

011

.020

1.83

014

.500

264

1311

52.4

11.

09no

ne v

isib

le0.

047

253.

041

0.27

00.

310

0.14

39.

940

2.46

03.

010

155

818

54.9

51.

54d.

s.0.

050

258.

016

00.

230

0.66

01.

120

32.5

1011

9.00

08.

010

130

336

50.4

10.

46d.

s.0.

040

358.

013

00.

270

0.66

00.

260

1.48

82.

671

2.25

716

025

651

.98

0.56

sulp

hide

ble

bs a

nd d

.s.0.

080

500.

018

00.

240

0.66

01.

061

28.1

6810

9.65

68.

586

220

276

51.7

20.

54d.

s. po

=cpy

3.50

021

450.

054

002.

943

4.99

80.

260

798.

710

7223

.970

462.

714

1300

029

645

.86

0.45

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

JB98

-225

AJB

98-2

28JB

98-2

29JB

98-2

30JB

98-2

31JB

98-2

39D

JB98

-239

EJB

98-2

39F

RK

-1R

K-2

RK

-3R

K-4

RK

-5R

K-7

RK

-8R

K-9

RK

-10

RK

-11

RK

-12

RK

-13

RK

-14

RK

-15

RK

-16

RK

-17

RK

-18

RK

-19

JB97

-50

JB97

-54A

JB97

-63

JB98

-122

JB97

-14

JB97

-15

JB97

-16

JB97

-43A

Al2

O3

Fe2O

3*M

nOM

gOC

aON

a2O

K2O

P2O

5C

O2

SL

OI

M-T

otal

Mg#

Co

Cr*

VC

sR

bT

hU

Nb

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

11.9

211

.86

0.16

11.6

710

.43

1.60

0.63

0.02

na2.

453.

7210

0.37

7083

na19

40.

2122

.56

0.88

0.28

1.23

14.1

07.

610.

1510

.46

13.2

71.

480.

580.

01na

0.01

2.76

100.

3076

33na

181

0.40

20.1

50.

540.

231.

0813

.40

8.38

0.16

11.0

412

.55

1.33

0.39

0.03

na0.

023.

2410

0.34

7533

na18

60.

1812

.76

0.74

0.22

1.08

13.9

18.

140.

1610

.84

12.7

71.

420.

390.

01na

0.05

2.91

100.

4076

38na

180

0.44

11.6

10.

760.

221.

1612

.17

9.77

0.17

10.9

211

.40

1.17

0.58

0.02

na0.

042.

5810

0.34

7241

na19

90.

3517

.47

0.54

0.58

1.71

14.8

39.

390.

168.

4010

.58

2.26

0.74

0.05

na0.

092.

3010

0.31

6836

na20

33.

0529

.12

1.66

0.59

2.28

14.9

89.

300.

168.

5411

.55

1.70

0.65

0.04

na0.

052.

4010

0.39

6838

na20

81.

7826

.70

1.35

0.41

1.92

15.3

79.

970.

157.

6511

.01

1.78

0.36

0.03

na0.

022.

5410

0.31

6438

na21

11.

0611

.06

1.60

0.47

2.06

6.77

10.4

10.

1514

.56

4.11

0.36

1.05

0.03

0.06

0.71

5.36

99.8

076

70na

152

2.60

41.4

43.

181.

571.

4612

.39

8.71

0.14

11.1

79.

302.

710.

940.

030.

180.

013.

0810

0.05

7546

na20

60.

8534

.22

0.71

0.30

0.88

6.79

11.2

20.

1614

.46

4.52

0.70

0.83

0.02

0.03

1.41

5.25

99.8

175

97na

146

1.51

33.3

42.

791.

441.

960.

7676

.50

0.03

0.39

0.04

0.12

0.01

0.01

na36

.30

23.4

410

1.91

111

45na

380.

050.

043.

041.

4614

.83

11.2

50.

163.

828.

563.

350.

970.

160.

080.

041.

8899

.91

4436

na22

02.

0735

.19

4.57

1.34

7.10

10.8

49.

430.

1812

.55

11.5

51.

560.

540.

040.

130.

011.

6299

.82

7647

na22

30.

9314

.74

0.93

0.31

1.60

10.6

09.

560.

1812

.99

11.2

81.

640.

500.

040.

070.

020.

9810

0.15

7648

na23

20.

7816

.17

1.01

0.32

1.70

6.09

10.3

20.

1916

.35

11.9

91.

410.

210.

020.

060.

010.

6010

0.04

7958

na28

70.

457.

960.

780.

261.

275.

9810

.36

0.21

16.3

811

.80

1.16

0.21

0.03

0.07

0.01

0.82

99.7

479

58na

279

0.60

8.10

0.77

0.26

1.27

6.07

10.5

70.

2017

.35

10.9

60.

980.

190.

020.

020.

020.

4399

.93

7959

na26

40.

377.

300.

710.

231.

156.

2110

.49

0.20

16.4

111

.94

0.95

0.21

0.04

0.02

0.01

0.43

100.

0978

56na

276

0.42

7.76

0.77

0.24

1.27

16.7

18.

620.

157.

8011

.53

2.07

0.51

0.05

0.02

0.02

0.93

99.9

168

36na

177

0.74

15.3

21.

180.

371.

9716

.74

8.12

0.15

7.72

11.4

42.

740.

480.

030.

020.

021.

1599

.89

6934

na16

70.

7814

.94

1.11

0.36

1.89

18.1

87.

420.

146.

6211

.69

2.56

0.54

0.05

0.04

0.01

1.71

100.

1667

31na

154

0.96

16.0

81.

260.

402.

0713

.99

6.97

0.14

11.0

512

.12

2.11

0.55

0.02

0.05

0.01

2.58

100.

3979

36na

196

1.38

15.6

60.

530.

160.

8613

.66

9.08

0.16

9.76

11.6

82.

200.

450.

120.

020.

021.

4099

.98

7141

na20

71.

0014

.60

1.26

0.39

2.06

5.85

10.7

20.

2117

.31

11.0

41.

010.

210.

04na

0.01

0.68

99.9

079

58na

265

0.43

7.58

0.78

0.26

1.29

18.6

07.

690.

136.

7111

.72

2.53

0.56

0.04

0.02

0.01

1.08

100.

2867

30na

158

0.76

18.1

51.

220.

392.

0613

.00

15.5

60.

234.

647.

192.

522.

050.

050.

190.

111.

2699

.59

4162

na44

00.

6610

0.07

2.77

0.86

4.82

11.0

415

.71

0.12

2.09

7.22

4.74

0.07

0.11

6.06

0.93

5.86

98.9

324

380

na71

0.22

0.78

8.24

18.3

05.

4414

.52

13.8

50.

224.

716.

763.

451.

600.

110.

290.

081.

5010

0.22

4452

7523

50.

4465

.46

4.42

1.41

5.41

12.7

814

.16

0.16

3.09

5.93

3.61

1.79

0.16

na0.

051.

9310

0.10

3441

na22

40.

7374

.19

6.81

2.11

12.0

915

.22

8.53

0.13

8.68

12.7

11.

660.

440.

030.

270.

052.

0810

0.35

7035

na21

00.

7116

.76

0.98

0.35

1.36

14.0

310

.46

0.19

8.49

12.0

21.

590.

460.

030.

170.

040.

3810

0.19

6545

na24

00.

8715

.66

1.32

0.37

2.07

14.3

89.

930.

178.

5712

.80

1.45

0.46

0.02

0.16

0.08

0.25

100.

2967

41na

230

0.75

12.9

61.

140.

341.

8212

.96

14.1

80.

167.

6910

.39

1.01

0.56

0.02

0.13

3.50

2.75

96.0

356

170

na19

01.

6021

.74

1.09

0.31

1.43

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

JB98

-225

AJB

98-2

28JB

98-2

29JB

98-2

30JB

98-2

31JB

98-2

39D

JB98

-239

EJB

98-2

39F

RK

-1R

K-2

RK

-3R

K-4

RK

-5R

K-7

RK

-8R

K-9

RK

-10

RK

-11

RK

-12

RK

-13

RK

-14

RK

-15

RK

-16

RK

-17

RK

-18

RK

-19

JB97

-50

JB97

-54A

JB97

-63

JB98

-122

JB97

-14

JB97

-15

JB97

-16

JB97

-43A

Ta

La

Ce

PrSr

Nd

Zr

Hf

SmE

uT

i*G

dT

bD

yY

Ho

Er

Tm

Yb

Lu

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

0.16

3.76

8.22

1.11

104.

404.

9728

.35

0.95

1.18

0.40

0.21

01.

500.

251.

7710

.59

0.37

1.18

0.15

1.10

0.16

0.14

3.10

6.87

0.93

136.

804.

0722

.42

0.66

1.12

0.39

0.22

21.

380.

251.

779.

780.

371.

070.

140.

960.

170.

173.

286.

980.

9811

2.50

4.23

24.7

80.

881.

190.

440.

210

1.49

0.26

1.83

10.4

80.

381.

100.

181.

040.

180.

163.

296.

970.

9612

1.70

4.25

24.4

10.

811.

150.

430.

210

1.30

0.26

1.61

9.83

0.35

1.07

0.15

1.06

0.16

0.21

3.75

8.14

1.09

100.

704.

6618

.10

0.49

1.15

0.39

0.24

01.

310.

211.

516.

040.

330.

900.

130.

980.

130.

176.

6413

.74

1.75

152.

206.

8646

.57

1.28

1.65

0.51

0.31

81.

800.

312.

0713

.81

0.47

1.32

0.19

1.26

0.20

0.16

5.42

11.1

71.

4018

1.40

6.01

39.7

41.

111.

550.

510.

318

1.72

0.30

2.06

13.7

30.

431.

320.

191.

290.

200.

176.

2612

.95

1.68

190.

706.

8143

.62

1.26

1.67

0.60

0.31

21.

910.

342.

2414

.35

0.49

1.38

0.21

1.46

0.21

na5.

8312

.62

1.61

4.60

6.78

na1.

951.

560.

360.

198

1.51

0.23

1.37

-0.

270.

840.

120.

770.

12na

3.76

8.00

1.00

245.

204.

30na

0.71

0.98

0.45

0.16

81.

090.

171.

10 -

0.22

0.65

0.09

0.61

0.09

na3.

898.

941.

164.

204.

94na

2.10

1.29

0.30

0.21

01.

370.

221.

33 -

0.27

0.81

0.11

0.77

0.12

na0.

120.

240.

03 -

0.14

na0.

240.

02 -

0.09

60.

020.

03 -

0.01

- -

-na

19.4

041

.38

5.18

237.

9022

.45

na4.

075.

421.

370.

713

5.72

0.88

5.47

-1.

103.

150.

432.

800.

42na

4.03

8.96

1.18

163.

905.

23na

1.13

1.37

0.47

0.25

81.

520.

241.

67 -

0.33

0.95

0.13

0.86

0.13

na4.

559.

651.

2313

3.70

5.53

na1.

191.

410.

460.

282

1.64

0.28

1.73

-0.

341.

000.

140.

890.

14na

3.40

7.36

0.96

67.6

04.

46na

1.23

1.25

0.37

0.24

61.

450.

241.

58 -

0.33

0.97

0.14

0.87

0.14

na3.

447.

520.

9870

.50

4.52

na1.

071.

240.

400.

246

1.47

0.25

1.58

-0.

330.

950.

130.

880.

14na

3.19

6.90

0.91

65.2

04.

19na

0.97

1.12

0.35

0.22

81.

300.

221.

46 -

0.30

0.88

0.12

0.78

0.12

na3.

467.

360.

9867

.80

4.51

na0.

981.

220.

380.

252

1.47

0.24

1.56

-0.

320.

950.

130.

850.

13na

5.42

11.3

81.

4522

0.80

6.37

na1.

341.

600.

570.

294

1.73

0.28

1.81

-0.

371.

050.

150.

940.

15na

5.34

11.2

01.

4222

5.70

6.17

na1.

301.

530.

580.

300

1.74

0.28

1.76

-0.

351.

000.

140.

900.

14na

5.59

11.3

81.

4023

6.80

6.16

na1.

351.

520.

600.

300

1.73

0.26

1.72

-0.

330.

990.

140.

890.

14na

2.56

5.51

0.72

204.

503.

29na

0.73

0.90

0.37

0.18

01.

070.

171.

14 -

0.23

0.67

0.09

0.64

0.10

na5.

6912

.04

1.54

171.

506.

73na

1.30

1.69

0.59

0.31

21.

870.

301.

94 -

0.39

1.14

0.16

1.03

0.15

na3.

417.

420.

9759

.00

4.48

na1.

081.

240.

370.

234

1.41

0.23

1.52

-0.

320.

960.

130.

650.

13na

5.59

11.4

31.

4324

9.10

6.42

na1.

351.

560.

620.

288

1.71

0.28

1.72

-0.

341.

020.

140.

690.

140.

3911

.41

25.1

73.

2314

8.00

14.3

6na

2.73

3.72

1.14

0.82

13.

870.

634.

08 -

0.84

2.36

0.34

2.20

0.32

0.50

250.

0025

0.00

30.9

933

.70

111.

81na

6.20

19.3

32.

020.

288

11.0

71.

155.

63 -

0.81

2.25

0.28

1.91

0.32

0.44

15.4

933

.69

4.15

186.

7017

.00

na3.

153.

841.

260.

653

4.16

0.70

3.94

-0.

882.

350.

342.

190.

350.

8925

.45

52.0

76.

5817

7.80

26.7

614

1.41

4.41

6.03

1.59

0.92

36.

281.

006.

5736

.90

1.27

3.72

0.53

3.33

0.54

0.09

4.31

9.78

1.26

168.

105.

55na

-1.

460.

510.

276

1.68

0.30

2.04

-0.

451.

330.

201.

300.

200.

145.

5812

.68

1.59

139.

106.

99na

-1.

860.

600.

336

2.07

0.36

2.48

-0.

551.

580.

231.

540.

220.

124.

9210

.81

1.38

121.

606.

27na

-1.

710.

540.

324

1.90

0.35

2.37

-0.

541.

550.

221.

480.

230.

104.

259.

351.

2011

8.50

5.36

na0.

951.

360.

500.

270

1.65

0.28

1.86

-0.

421.

200.

181.

170.

17

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

Tow

nshi

pSt

udy

Are

aD

escr

iptio

n 1

Roc

k T

ype

Fiel

d N

ame

JB97

-43B

Jane

sC

hini

guch

im

g; e

dge

of c

lear

ed a

rea

at w

est e

dge

of o

/c; F

alco

-tren

ches

opx

gabb

roJB

97-4

3CJa

nes

Chi

nigu

chi

mg;

eas

t edg

e of

cle

ared

are

a; F

alco

-tren

ches

opx

gabb

roJB

97-4

3DJa

nes

Chi

nigu

chi

mg;

on

edge

of h

igh

hill

to e

ast o

f cle

ared

are

a; F

alco

-tren

ches

opx

gabb

roJB

97-6

1W

ells

Bas

swoo

d Lk

Tra

vf.g

.-m.g

. gab

bro

- aug

ite p

heno

crys

ts?

opx

gabb

roJB

97-7

6BW

ater

sM

akad

afg

-mg

gabb

ro w

ith fe

lted

text

ure

opx

gabb

roJB

97-8

5AN

airn

Nai

rn W

right

mg;

ver

y m

afic

- m

elag

abbr

o?op

x ga

bbro

JB97

-95

Jane

sC

hini

guch

im

g; e

astw

ard

cont

inua

tion?

of T

1 tre

nch;

W e

dge

of ri

dge

east

of T

1op

x ga

bbro

JB97

-96

Jane

sC

hini

guch

im

g; fr

esh

blas

t - 2

pie

ces;

Bria

n to

ok 3

; bla

sted

are

a of

T1

opx

gabb

roJB

97-1

03A

Kel

lyK

ukag

ami D

etai

lm

g; P

GE-

rich

laye

r?; e

dge

of ri

dge

at b

ase

of b

last

ed p

it; S

edg

e of

ridg

eop

x ga

bbro

JB97

-103

BK

elly

Kuk

agam

i Det

ail

mg;

abo

ut 0

.6 m

"ab

ove"

103

Aop

x ga

bbro

JB97

-103

CK

elly

Kuk

agam

i Det

ail

mg;

abo

ut 1

.0 m

"ab

ove"

103

Aop

x ga

bbro

JB97

-103

DK

elly

Kuk

agam

i Det

ail

mg;

abo

ut 6

.0 m

eas

t of p

it ar

eaop

x ga

bbro

JB97

-106

BJa

nes

Chi

nigu

chi

Tren

ch T

-2 o

n Fa

lco

map

; abo

ut 2

3.0

m so

uth

of n

orth

end

of t

renc

h op

x ga

bbro

JB97

-107

Jane

sC

hini

guch

iE

of c

lear

ed a

rea

num

ber T

-4 o

n Fa

lcon

brid

ge m

ap; o

n to

p of

hill

;op

x ga

bbro

JB97

-108

Jane

sC

hini

guch

iE

of T

renc

h T-

4 on

Fal

co m

ap; 5

m b

elow

sam

ple

107

on ri

dge

opx

gabb

roJB

97-1

09Ja

nes

Chi

nigu

chi

sulp

h-ve

in a

t ~24

0az;

mel

agab

bro

in o

ld N

-S tr

ench

; upp

er a

rea

of T

4op

x ga

bbro

JB98

-123

Brid

glan

dB

assw

ood

Lk T

rav

mg;

N. s

ide

#129

; N. o

f Tw

p. L

ine;

wea

ther

s to

brow

n pi

ts (o

px?)

opx

gabb

roJB

98-1

47Lo

rne

Bel

l Lak

e Tr

avfg

-mg;

~75

m a

t 315

az fr

om st

at. 1

46 -

Trav

erse

opx

gabb

roJB

98-1

82C

urtin

Cha

rlton

Lk

Clif

fm

g; ~

15m

NW

of s

tat.

181;

~50

m E

of s

hore

; tra

vers

eop

x ga

bbro

JB98

-204

Kel

lyC

araf

el B

ay T

rav

mg;

mt-b

earin

g; o

n hi

gh c

liff w

est o

f lak

e ov

erlo

okin

g va

lley-

trave

rse

opx

gabb

roJB

98-2

12A

Loui

seLo

uie

Lake

mg;

smal

l pit

east

of l

arge

r and

mai

n pi

t are

aop

x ga

bbro

JB97

-37

Fost

erB

razi

l Lak

em

g; ~

75m

wes

t of t

renc

h; h

ighl

y fr

actu

red

- loc

ally

c.g

. to

near

peg

.le

ucog

abbr

oJB

97-4

7Er

mat

inge

rFo

x La

ke R

oad

in A

rche

an; m

g ga

bbro

; up

to 3

0% e

pido

tele

ucog

abbr

oJB

97-7

9BW

ater

sM

akad

afg

gab

bro

from

o/c

on

wes

t sid

e of

road

- hi

ll of

gab

bro;

grid

230

N/1

60E

leuc

ogab

bro

JB97

-104

Jane

sC

hini

guch

im

g; lo

catio

ns o

n Fa

lcon

brid

ge m

ap; o

n to

p of

hill

tow

ard

sout

heas

t edg

ele

ucog

abbr

oJB

98-1

15Ja

nes

Sarg

esso

nm

g; c

py>p

o>pn

in 3

40 A

z tre

ndin

g rid

ge o

f gab

bro

leuc

ogab

bro

JB98

-165

Wat

ers

Mak

ada

Det

ail

mg;

det

ail g

rid: 0

+2.5

S/0

+25

E; ~

20%

blu

e qt

z ey

esle

ucog

abbr

oJB

97-7

1Lo

uise

Lo

uie

Lake

mg

gabb

ro; s

outh

side

of l

arge

exp

ansi

ve o

/cm

elag

abbr

oJB

97-8

0ALo

uise

Loui

e La

kem

g; fe

lsic

gab

bro

from

wes

t sid

e of

hill

- no

n-m

tm

elag

abbr

oJB

97-8

3Lo

uise

Loui

e La

kem

g; sm

all m

afic

gab

bro

"pod

" at

SE

edge

of h

ill; a

rea

of v

cg to

nea

r-pe

g ga

bbro

mel

agab

bro

JB97

-84E

Loui

seLo

uie

Lake

mg;

nea

r mel

agab

bro;

alte

red

to fe

lty te

xtur

em

elag

abbr

oJB

98-1

97K

elly

Car

afel

Bay

Tra

vm

g; m

t-bea

ring;

~40

m N

. of l

ast s

tatio

n - T

rave

rse

mt g

abbr

oJB

98-1

24K

irkw

ood

Bas

swoo

d Lk

Tra

vfg

-mg;

E. s

ide

#129

; pos

sibl

y qt

z-ga

bbro

; bec

omes

mor

e fg

sout

h al

ong

o/c

qtz

gabb

roJB

98-1

46Lo

rne

Bel

l Lak

e Tr

avm

g; ~

50m

at 3

15az

from

stat

. 145

- Tr

aver

seqt

z ga

bbro

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

JB97

-43B

JB97

-43C

JB97

-43D

JB97

-61

JB97

-76B

JB97

-85A

JB97

-95

JB97

-96

JB97

-103

AJB

97-1

03B

JB97

-103

CJB

97-1

03D

JB97

-106

BJB

97-1

07JB

97-1

08JB

97-1

09JB

98-1

23JB

98-1

47JB

98-1

82JB

98-2

04JB

98-2

12A

JB97

-37

JB97

-47

JB97

-79B

JB97

-104

JB98

-115

JB98

-165

JB97

-71

JB97

-80A

JB97

-83

JB97

-84E

JB98

-197

JB98

-124

JB98

-146

Sulp

hide

/Oxi

deS

SeN

iIr

Ru

Rh

PtPd

Au

Cu

Al2

O3

SiO

2Si

O2

TiO

2w

t%pp

bpp

mpp

bpp

bpp

bpp

bpp

bpp

bpp

mTi

O2

MgO

wt%

wt%

none

vis

ible

0.04

020

1.0

140

0.27

00.

660

0.61

010

.370

20.2

603.

790

110

276

51.1

10.

54d.

s. po

=cpy

2.71

016

732.

043

001.

300

7.19

012

.280

284.

500

1577

.320

352.

750

1100

029

546

.19

0.43

d.s.

po=c

py0.

390

2757

.072

00.

250

1.11

01.

190

35.4

5080

.030

45.9

2016

0038

649

.63

0.39

none

0.07

045

7.0

118

0.27

00.

660

0.26

01.

430

1.88

05.

040

786

947

.69

2.70

d.s.

- po>

cpy

0.80

011

34.0

210

0.27

00.

660

0.57

05.

460

5.37

03.

220

220

187

53.1

90.

74d.

s. an

d b.

s.9.

400

3967

5.0

7153

1.55

01.

440

1.46

032

.500

21.4

0016

.050

2758

3na

nana

nacp

y, p

o, p

n?0.

450

3525

.086

80.

270

0.66

00.

260

35.1

1066

.090

44.3

7019

0832

550

.28

0.44

cpy,

po,

pn

3.02

018

285.

049

411.

320

3.77

017

54.7

5034

5.10

071

35.6

1040

4.25

013

069

nana

nana

d.s a

nd b

.s. -

look

mag

mat

ic1.

734

6400

.027

730.

700

0.66

023

.000

380.

000

1930

.000

120.

000

5095

305

48.5

80.

41d.

s.0.

067

700.

021

30.

500

0.66

00.

700

20.0

0055

.000

2.00

019

628

550

.78

0.44

d.s.

and

b.s.

1.96

162

00.0

2662

0.80

00.

660

12.0

0044

0.00

015

50.0

0012

0.00

062

5929

548

.23

0.42

d.s.

0.06

760

0.0

148

0.20

00.

660

1.10

012

.000

19.0

001.

000

110

276

50.3

40.

51d.

s.0.

049

400.

012

10.

200

0.66

00.

200

11.0

0018

.000

2.70

071

256

49.5

10.

56d.

s.; w

ith <

1% m

agne

tite

0.04

420

0.0

178

0.20

00.

660

0.90

028

.000

61.0

003.

700

129

375

49.8

90.

39b.

s. an

d d.

s.0.

035

500.

014

90.

200

0.66

00.

600

11.0

0015

.000

0.80

087

335

50.9

00.

43d.

s. an

d b.

s. 5.

323

3519

0.0

1056

02.

400

0.66

023

.000

1300

.000

4560

.000

720.

000

1708

024

742

.57

0.55

none

vis

ible

0.03

820

1.0

130

0.09

90.

263

0.42

531

.500

33.2

006.

000

9238

650

.90

0.41

none

0.00

515

.035

51.

077

1.68

03.

070

10.5

902.

260

0.73

06

193

51.1

70.

24d.

s. &

b.s.

; po>

cpy;

2m

x2m

0.08

542

2.0

166

0.27

00.

270

0.12

63.

150

3.01

02.

350

295

295

50.1

70.

41pa

tchy

mag

netis

m (p

o?)

0.00

910

0.0

147

0.05

60.

150

0.40

78.

540

8.72

01.

970

7830

551

.72

0.48

po a

nd c

py a

s d.s.

and

b.s.

2.77

029

06.0

502

0.26

60.

530

0.61

010

.320

13.6

5044

.600

546

103

49.8

70.

65no

ne v

isib

le0.

070

300.

083

0.27

00.

660

0.23

01.

430

1.88

02.

320

130

268

52.0

40.

55no

ne0.

050

270.

078

0.27

00.

660

0.26

01.

430

1.93

01.

420

170

169

52.1

70.

89no

ne v

isib

le0.

010

73.0

212

0.27

00.

660

0.26

05.

050

10.3

201.

420

5332

551

.81

0.42

d.s.

0.05

950

0.0

190

0.27

00.

660

0.60

011

.000

6.00

011

.000

250

415

49.8

20.

32bl

eb a

nd d

iss.

0.77

056

83.0

1116

0.25

50.

380

1.01

210

1.00

011

6.60

015

7.30

032

1730

649

.89

0.45

po>>

cpy

as d

.s./b

.s.14

.500

80.0

3062

0.74

41.

830

5.02

018

.770

30.5

0023

8.00

017

0229

741

.70

0.21

none

vis

ible

0.05

024

8.0

162

0.27

00.

660

0.26

06.

320

5.48

03.

830

151

545

49.8

60.

27no

ne v

isib

le0.

040

258.

016

60.

270

0.66

00.

260

20.2

7024

.670

3.30

010

635

550

.86

0.40

b.s.

and

d.s.

- bre

ccia

?9.

880

59.0

1490

0.27

01.

600

1.77

026

.560

28.2

6063

.420

874

nana

nana

po>c

py>p

y>pn

22.8

0026

685.

039

391.

800

6.09

05.

660

11.1

6045

.370

4.67

066

8na

nana

nam

ainl

y po

; 5%

mag

netit

e?0.

058

243.

063

0.27

00.

660

0.26

01.

430

0.09

00.

820

118

189

52.9

20.

80no

ne v

isib

le0.

052

269.

010

90.

270

0.22

00.

260

10.0

7011

.450

3.02

010

826

751

.86

0.57

none

0.01

811

4.0

188

0.10

10.

580

0.53

04.

820

6.45

01.

540

5530

551

.20

0.47

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

JB97

-43B

JB97

-43C

JB97

-43D

JB97

-61

JB97

-76B

JB97

-85A

JB97

-95

JB97

-96

JB97

-103

AJB

97-1

03B

JB97

-103

CJB

97-1

03D

JB97

-106

BJB

97-1

07JB

97-1

08JB

97-1

09JB

98-1

23JB

98-1

47JB

98-1

82JB

98-2

04JB

98-2

12A

JB97

-37

JB97

-47

JB97

-79B

JB97

-104

JB98

-115

JB98

-165

JB97

-71

JB97

-80A

JB97

-83

JB97

-84E

JB98

-197

JB98

-124

JB98

-146

Al2

O3

Fe2O

3*M

nOM

gOC

aON

a2O

K2O

P2O

5C

O2

SL

OI

M-T

otal

Mg#

Co

Cr*

VC

sR

bT

hU

Nb

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

14.6

29.

460.

178.

2012

.32

1.41

0.48

0.03

0.31

0.04

2.12

100.

4667

37na

210

1.24

18.0

91.

360.

401.

9212

.48

14.3

00.

178.

4710

.81

1.41

0.16

0.02

0.12

2.71

2.02

96.4

658

140

na19

00.

554.

121.

060.

301.

2014

.84

8.50

0.13

8.85

13.1

71.

320.

340.

020.

390.

392.

0599

.24

7150

na18

01.

269.

840.

860.

261.

0615

.12

15.3

70.

195.

437.

563.

191.

480.

550.

090.

070.

5599

.83

4557

117

241

1.98

36.1

22.

810.

8414

.94

13.5

59.

060.

077.

588.

964.

080.

450.

130.

370.

801.

2999

.10

6640

na23

00.

309.

450.

982.

549.

42na

nana

nana

nana

na0.

299.

40na

0.00

-17

817

994

0.66

4.91

10.3

26.

006.

8013

.91

9.32

0.16

9.41

12.7

11.

240.

550.

040.

180.

451.

3899

.44

7056

500

195

2.57

18.8

30.

100.

301.

28na

nana

nana

nana

na0.

103.

02na

0.00

-16

239

018

90.

807.

781.

080.

321.

1412

.42

11.9

80.

179.

1512

.27

1.12

0.34

0.05

na1.

732.

1098

.59

64na

na20

21.

2512

.38

0.97

0.29

1.62

12.3

79.

920.

1710

.47

13.2

01.

460.

340.

06na

0.07

0.99

100.

2071

nana

214

1.12

12.1

50.

920.

291.

4612

.01

11.8

10.

169.

5212

.25

0.36

0.36

0.06

na1.

962.

5597

.73

65na

na19

91.

9713

.73

1.05

0.32

1.51

13.6

010

.07

0.18

9.15

12.3

41.

420.

610.

04na

0.07

1.88

100.

1468

nana

209

2.66

19.7

31.

200.

392.

4214

.19

10.5

30.

178.

3610

.94

1.99

0.41

0.05

na0.

053.

5610

0.27

65na

na19

30.

5613

.54

1.23

0.40

1.76

14.4

38.

600.

149.

2813

.43

1.25

0.53

0.05

na0.

041.

9899

.97

72na

na19

32.

0113

.09

0.79

0.23

1.36

14.0

69.

530.

159.

2612

.72

1.08

0.49

0.05

na0.

040.

8599

.52

69na

na20

40.

8312

.55

0.94

0.29

1.49

13.0

316

.64

0.13

6.03

5.69

2.43

0.11

0.07

na5.

324.

5191

.76

4628

3na

191

0.42

1.86

3.34

1.09

2.65

15.4

08.

360.

159.

1212

.63

2.10

0.32

0.03

na0.

040.

6810

0.10

7236

na18

10.

4710

.02

0.97

0.30

1.46

4.47

9.70

0.22

19.4

110

.87

0.86

0.04

0.01

na0.

005

3.27

100.

2682

73na

225

0.15

1.43

0.38

0.15

1.01

12.0

49.

840.

1810

.48

10.4

12.

120.

680.

03na

0.09

3.82

100.

1871

49na

214

1.12

22.3

11.

160.

391.

5414

.45

9.06

0.17

9.44

12.6

41.

590.

370.

03na

0.01

0.35

100.

3071

44na

217

0.78

13.1

61.

150.

371.

706.

2117

.57

0.24

15.0

76.

670.

270.

060.

05na

2.77

3.51

100.

1767

134

na20

60.

354.

242.

080.

622.

7914

.55

11.0

10.

196.

7210

.54

1.98

0.67

0.03

0.16

0.07

1.26

99.5

459

42na

230

1.26

22.7

21.

500.

462.

1013

.88

12.8

90.

205.

799.

912.

400.

490.

020.

240.

051.

0299

.66

5158

na30

00.

9021

.85

2.41

0.68

5.21

13.5

98.

690.

1410

.72

11.6

21.

720.

520.

030.

130.

011.

2410

0.50

7442

500

219

1.62

22.9

10.

960.

301.

5513

.19

9.20

0.15

10.4

812

.33

0.64

0.32

0.04

na0.

063.

7510

0.24

73na

na18

50.

869.

630.

710.

221.

0913

.36

10.8

10.

188.

9910

.56

1.72

0.54

0.03

na0.

773.

1899

.71

6672

na20

30.

7619

.58

1.15

0.36

1.70

6.10

32.4

30.

035.

591.

210.

861.

130.

02na

14.5

07.

4796

.75

2945

7na

922.

2152

.84

5.36

2.42

2.40

14.6

78.

150.

169.

9612

.29

1.38

0.68

0.02

0.36

0.05

2.54

99.9

874

4031

717

40.

8626

.37

0.53

0.16

0.68

14.0

38.

470.

169.

8312

.42

1.57

0.74

0.03

0.20

0.04

1.56

100.

0773

3850

019

21.

2318

.10

0.79

0.25

1.20

nana

nana

nana

nana

0.10

9.88

na0.

00-

405

500

105

0.17

1.71

2.62

1.29

1.36

nana

nana

nana

nana

0.12

22.8

0na

0.00

-10

9150

099

0.97

7.48

0.43

0.15

0.67

14.0

612

.19

0.21

6.01

9.95

2.11

0.77

0.08

na0.

060.

9110

0.01

5346

na27

52.

1828

.19

2.33

0.70

3.31

14.6

09.

800.

157.

7011

.01

2.03

0.83

0.05

na0.

051.

6210

0.22

6543

na22

31.

2030

.32

1.66

0.50

2.38

14.0

68.

340.

159.

9311

.35

2.16

0.31

0.02

na0.

018

2.33

100.

3273

45na

215

0.87

11.6

71.

270.

361.

96

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

JB97

-43B

JB97

-43C

JB97

-43D

JB97

-61

JB97

-76B

JB97

-85A

JB97

-95

JB97

-96

JB97

-103

AJB

97-1

03B

JB97

-103

CJB

97-1

03D

JB97

-106

BJB

97-1

07JB

97-1

08JB

97-1

09JB

98-1

23JB

98-1

47JB

98-1

82JB

98-2

04JB

98-2

12A

JB97

-37

JB97

-47

JB97

-79B

JB97

-104

JB98

-115

JB98

-165

JB97

-71

JB97

-80A

JB97

-83

JB97

-84E

JB98

-197

JB98

-124

JB98

-146

Ta

La

Ce

PrSr

Nd

Zr

Hf

SmE

uT

i*G

dT

bD

yY

Ho

Er

Tm

Yb

Lu

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

0.13

5.48

12.1

41.

5513

8.30

6.78

na1.

101.

790.

600.

324

2.00

0.34

2.36

-0.

491.

440.

221.

460.

210.

104.

189.

141.

1910

7.00

5.20

na0.

871.

390.

480.

258

1.62

0.28

1.84

-0.

401.

190.

171.

090.

160.

083.

547.

841.

0113

9.80

4.43

na0.

801.

230.

430.

234

1.51

0.26

1.72

-0.

391.

090.

161.

070.

150.

8828

.30

64.5

18.

2937

2.20

35.8

2na

5.81

7.87

2.61

1.61

97.

631.

266.

77 -

1.47

3.95

0.57

3.67

0.54

0.83

4.43

12.7

02.

1118

0.70

10.5

2na

1.31

3.28

0.57

0.44

43.

430.

614.

08 -

0.87

2.34

0.34

1.98

0.28

0.92

37.1

477

.55

8.67

224.

7031

.47

na4.

396.

161.

80 -

5.48

0.90

4.64

-0.

962.

430.

352.

080.

320.

112.

716.

940.

9210

8.80

4.08

na0.

481.

160.

380.

264

1.38

0.25

1.62

-0.

360.

990.

141.

000.

150.

104.

219.

521.

2211

8.90

5.23

na1.

071.

360.

48 -

1.62

0.29

1.86

-0.

421.

230.

181.

210.

18na

4.34

9.56

1.25

107.

605.

4933

.60

1.01

1.50

0.49

0.24

61.

800.

312.

0712

.91

0.46

1.34

0.20

1.30

0.20

na4.

159.

011.

1711

6.70

5.21

33.7

91.

001.

450.

490.

264

1.78

0.31

2.11

12.8

90.

461.

380.

201.

300.

20na

4.33

9.21

1.18

116.

005.

2435

.17

1.03

1.41

0.47

0.25

21.

710.

302.

0212

.35

0.43

1.31

0.19

1.23

0.19

na5.

2211

.13

1.41

141.

506.

1842

.36

1.22

1.66

0.53

0.30

62.

000.

342.

3614

.16

0.50

1.49

0.22

1.45

0.22

na5.

5211

.79

1.47

155.

206.

2842

.04

1.18

1.64

0.54

0.33

61.

900.

332.

2513

.79

0.49

1.41

0.20

1.34

0.21

na3.

597.

670.

9813

5.60

4.30

28.4

40.

831.

150.

420.

234

1.46

0.25

1.72

10.7

10.

381.

080.

161.

050.

16na

4.02

8.70

1.12

138.

304.

9532

.90

0.97

1.36

0.46

0.25

81.

700.

291.

9612

.18

0.42

1.26

0.18

1.15

0.18

na9.

5920

.51

2.42

291.

809.

1135

.64

1.27

2.00

0.52

0.33

01.

930.

312.

0911

.75

0.44

1.26

0.17

1.19

0.18

0.19

4.06

8.66

1.16

130.

005.

0130

.96

0.99

1.32

0.51

0.24

61.

660.

301.

8911

.94

0.43

1.19

0.16

1.11

0.17

0.14

1.40

3.35

0.63

8.10

3.21

21.0

50.

590.

920.

310.

144

1.05

0.18

1.15

7.30

0.25

0.72

0.10

0.70

0.09

0.17

4.76

9.80

1.29

144.

005.

3531

.57

1.06

1.58

0.47

0.24

61.

590.

292.

0111

.91

0.43

1.28

0.19

1.28

0.20

0.19

5.12

10.5

11.

3813

6.20

6.10

35.8

11.

141.

580.

530.

288

1.84

0.34

2.12

13.4

70.

471.

300.

191.

180.

200.

265.

5012

.26

1.55

3.70

6.90

52.9

21.

771.

700.

360.

390

2.06

0.36

2.36

14.2

70.

541.

640.

241.

580.

240.

156.

0713

.06

1.62

148.

807.

01na

1.24

1.84

0.62

0.33

02.

050.

342.

22 -

0.52

1.48

0.22

1.49

0.21

0.27

8.48

18.8

02.

4622

5.50

10.7

0na

2.17

2.80

0.96

0.53

42.

830.

483.

20 -

0.67

1.84

0.26

1.77

0.26

0.15

3.49

8.17

1.08

169.

604.

85na

1.03

1.28

0.48

0.25

21.

480.

261.

60 -

0.34

1.03

0.14

0.85

0.13

na3.

146.

680.

8713

7.40

3.83

25.3

50.

701.

050.

360.

192

1.32

0.22

1.55

9.66

0.33

0.99

0.14

0.94

0.14

0.18

4.73

10.0

71.

3314

1.00

5.74

38.7

91.

171.

550.

490.

270

1.79

0.30

2.25

14.1

80.

461.

340.

181.

380.

190.

349.

0618

.05

2.14

33.3

08.

4410

2.89

3.19

1.50

0.28

0.12

61.

250.

201.

227.

080.

220.

750.

110.

800.

110.

062.

405.

400.

7013

3.10

3.07

na0.

750.

780.

370.

162

1.02

0.19

1.26

-0.

290.

820.

120.

830.

120.

123.

668.

381.

0915

6.20

5.37

na1.

011.

260.

460.

240

1.49

0.27

1.74

-0.

401.

180.

161.

110.

160.

151.

734.

820.

652.

402.

85na

1.76

0.85

0.18

-0.

870.

150.

85 -

0.19

0.59

0.09

0.65

0.11

0.06

1.66

4.16

0.45

7.30

1.87

na0.

520.

440.

11 -

0.50

0.09

0.61

-0.

140.

460.

060.

460.

070.

309.

7819

.81

2.57

170.

1010

.84

65.4

52.

212.

740.

900.

480

3.05

0.55

3.58

22.4

90.

812.

190.

322.

200.

330.

246.

3913

.20

1.75

163.

107.

4446

.62

1.53

1.87

0.67

0.34

22.

230.

392.

6216

.39

0.58

1.75

0.24

1.61

0.25

0.23

5.13

10.9

91.

4919

3.10

6.09

37.5

21.

111.

550.

540.

282

1.64

0.26

1.93

10.9

40.

371.

060.

150.

920.

16

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

Tow

nshi

pSt

udy

Are

aD

escr

iptio

n 1

Roc

k T

ype

Fiel

d N

ame

JB97

-19A

Kel

lyW

asha

gam

i Lak

em

g; m

iner

aliz

atio

n a/

w p

enet

rativ

e fr

actu

re sy

stem

; cle

ared

o/c

wes

t sid

e of

val

ley

vt g

abbr

oJB

97-1

9BK

elly

Was

haga

mi L

ake

pegm

atoi

dal g

abbr

o in

are

a; n

o m

iner

aliz

atio

n ~2

m n

orth

of 1

9Avt

gab

bro

JB97

-38

Fost

erB

razi

l Lak

em

g; 1

5m e

ast o

f tre

nch;

var

i-tex

ture

d; h

ighl

y fr

actu

red

vt g

abbr

oJB

97-4

5M

oncr

ieff

Gen

eva

Lake

in A

rche

an; "

vari-

text

" ga

bbro

; up

to 3

0% e

pido

tevt

gab

bro

JB97

-51

Wel

lsA

pple

by L

k Tr

avA

pple

by L

k; m

g-vc

g ga

bbro

; var

i-tex

t. w

mic

ro-p

egm

atite

vt g

abbr

oJB

97-5

2W

ells

App

leby

Lk

Trav

App

leby

Lk;

mg-

vcg

gabb

ro; v

ari-t

ext.

w m

icro

-peg

mat

itevt

gab

bro

JB97

-53

Wel

lsA

pple

by L

k Tr

avA

pple

by L

k; m

g-vc

g ga

bbro

; var

i-tex

t. w

mic

ro-p

egm

atite

vt g

abbr

oJB

97-5

9W

ells

Bas

swoo

d Lk

Tra

vM

issi

ssag

i Riv

er; m

g-cg

gab

ro; l

ocal

ly v

cg to

mic

ro-p

eg.;

road

cut

on

way

to D

amvt

gab

bro

JB97

-60

Wel

lsB

assw

ood

Lk T

rav

Mis

siss

agi R

iver

; mg-

cg g

abro

; loc

ally

vcg

to m

icro

-peg

.; ro

ad c

ut o

n w

ay to

Dam

vt g

abbr

oJB

97-6

4W

ells

Bas

swoo

d Lk

Tra

vm

g-cg

; loc

ally

vcg

to m

icro

-peg

.;aci

cula

r am

ph.;

pink

fspa

rvt

gab

bro

JB97

-66

Wel

lsB

assw

ood

Lk T

rav

m.g

. gab

bro;

lim

ited

patc

hes o

f pin

k fs

par a

nd m

icro

-peg

.vt

gab

bro

JB97

-98

Scad

ding

Scad

ding

mg;

d.s.

& b

leb

sulp

hide

; eas

t sid

e of

Kuk

agam

i Lk.

Rd.

- ne

wly

bla

sted

o/c

vt g

abbr

oJB

97-1

00Sc

addi

ngSc

addi

ngm

g; n

r. "G

arba

ge D

ump

Rd"

-Fe-

carb

-Au?

; bas

e of

hill

; var

i-tex

t. to

hill

top

vt g

abbr

oJB

97-1

05Ja

nes

Chi

nigu

chi

peg-

vari-

text

. gab

bro;

pat

ches

of f

elte

d am

phib

ole;

on

hillt

opvt

gab

bro

JB98

-119

Wel

lsB

assw

ood

Lk T

rav

mg;

W o

f HW

Y#1

29;

30%

pin

k fs

par;

pegm

atiti

c po

ds; g

rano

phyr

ic g

abbr

ovt

gab

bro

JB98

-120

Wel

lsB

assw

ood

Lk T

rav

mg;

E o

f HW

Y#1

29; p

egm

atiti

c an

d an

orth

ositi

c pa

rts; g

rano

phyr

ic g

abbr

ovt

gab

bro

JB98

-121

AW

ells

Bas

swoo

d Lk

Tra

vm

g; N

. sid

e of

HW

Y#1

29; l

ocal

ly p

eg. w

eath

ers d

eep

red-

brow

nvt

gab

bro

JB98

-121

BW

ells

Bas

swoo

d Lk

Tra

vm

g; S

. sid

e of

HW

Y#1

29; g

ener

ally

sam

e as

121

A b

ut c

ut b

y cp

y-qt

z ve

ins

vt g

abbr

o

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

JB97

-19A

JB97

-19B

JB97

-38

JB97

-45

JB97

-51

JB97

-52

JB97

-53

JB97

-59

JB97

-60

JB97

-64

JB97

-66

JB97

-98

JB97

-100

JB97

-105

JB98

-119

JB98

-120

JB98

-121

AJB

98-1

21B

Sulp

hide

/Oxi

deS

SeN

iIr

Ru

Rh

PtPd

Au

Cu

Al2

O3

SiO

2Si

O2

TiO

2w

t%pp

bpp

mpp

bpp

bpp

bpp

bpp

bpp

bpp

mTi

O2

MgO

wt%

wt%

d.s.

and

cpy

strin

gers

0.04

032

1.0

220

0.17

00.

660

0.79

017

.830

68.7

7017

.090

190

335

50.1

20.

42bl

eb a

nd d

.s.0.

070

297.

017

00.

170

0.66

00.

880

16.0

5057

.410

4.33

015

032

650

.73

0.46

none

vis

ible

0.03

014

1.0

850.

270

0.66

00.

160

1.43

01.

690

2.08

066

307

51.4

40.

51no

ne v

isib

le0.

140

428.

044

0.27

00.

660

0.48

01.

430

1.88

06.

670

190

615

51.9

71.

95no

ne0.

160

345.

027

0.27

00.

660

0.26

01.

430

1.88

03.

410

656

2053

.67

2.04

none

0.12

041

1.0

600.

270

0.66

00.

260

1.43

01.

880

2.50

019

09

1250

.62

1.40

d.s.

0.10

013

95.0

780.

270

0.66

00.

260

1.43

01.

880

3.47

016

012

1052

.13

1.10

up to

5%

mag

netit

e0.

110

410.

057

0.27

00.

660

0.26

01.

430

1.88

04.

070

160

1011

52.4

31.

29up

to 5

% m

agne

tite

0.10

066

.063

0.27

00.

660

0.26

01.

270

1.65

01.

090

160

1111

52.4

21.

25no

ne0.

080

361.

044

0.27

00.

660

0.26

01.

430

1.88

07.

600

217

718

53.2

21.

98no

ne0.

050

288.

044

0.27

00.

660

0.26

01.

430

1.88

06.

440

111

617

52.5

52.

27bl

ebs

0.06

840

0.0

114

0.20

00.

660

0.26

014

.000

5.00

02.

200

162

266

49.7

90.

54no

ne v

isib

le0.

042

300.

014

00.

400

0.66

00.

500

11.0

0014

.000

2.10

086

246

49.8

10.

58d.

s.0.

022

200.

013

50.

500

0.66

01.

400

30.0

0040

.000

1.80

077

476

49.4

10.

34no

ne0.

061

294.

060

0.27

00.

140

0.26

01.

430

0.12

11.

340

279

815

52.7

21.

71no

ne0.

016

206.

056

0.27

00.

170

0.26

07.

170

0.98

87.

360

175

1014

53.7

61.

35cp

y, p

y>po

0.04

489

.034

0.38

112

.080

7.84

01.

430

0.20

41.

160

498

1455

.21

1.52

d.s.

and

b.s.;

"m

afic

" ga

bbro

4.12

090

56.0

600.

270

0.66

00.

260

1.43

00.

079

4.19

047

695

853

.18

1.89

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

JB97

-19A

JB97

-19B

JB97

-38

JB97

-45

JB97

-51

JB97

-52

JB97

-53

JB97

-59

JB97

-60

JB97

-64

JB97

-66

JB97

-98

JB97

-100

JB97

-105

JB98

-119

JB98

-120

JB98

-121

AJB

98-1

21B

Al2

O3

Fe2O

3*M

nOM

gOC

aON

a2O

K2O

P2O

5C

O2

SL

OI

M-T

otal

Mg#

Co

Cr*

VC

sR

bT

hU

Nb

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

wt%

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

13.8

29.

200.

199.

8612

.13

1.18

0.28

0.01

0.14

0.04

2.81

100.

0271

39na

200

0.16

2.92

0.80

0.25

1.06

14.8

98.

240.

168.

6212

.62

1.32

0.83

0.02

0.21

0.07

2.10

99.9

971

36na

200

1.70

31.2

41.

000.

301.

2715

.40

9.17

0.10

7.30

9.21

2.93

1.26

0.03

0.31

0.03

2.25

99.6

065

33na

180

0.66

32.8

61.

610.

542.

1312

.19

18.0

90.

223.

456.

483.

240.

840.

090.

090.

141.

0399

.55

3164

na57

00.

4633

.91

3.93

1.18

7.06

12.2

818

.51

0.19

2.70

4.09

4.43

1.04

0.09

0.18

0.16

0.63

99.6

725

54na

320

0.22

46.1

04.

591.

588.

0513

.05

17.6

50.

264.

194.

753.

231.

750.

050.

300.

121.

6498

.59

3665

na44

00.

4075

.45

3.04

0.92

5.11

13.3

913

.98

0.22

5.09

7.59

2.57

1.81

0.05

0.19

0.10

1.46

99.3

946

57na

300

0.66

78.9

32.

640.

824.

9213

.15

15.3

30.

214.

608.

582.

461.

090.

050.

150.

110.

6499

.83

4158

na38

02.

2850

.90

2.85

0.89

5.14

13.1

714

.96

0.20

4.85

8.77

2.40

1.05

0.05

0.13

0.10

0.73

99.8

543

56na

370

1.72

41.3

92.

920.

865.

1113

.04

15.5

40.

183.

046.

763.

251.

660.

150.

100.

081.

0699

.88

3150

4631

00.

2243

.02

5.29

1.72

7.91

13.3

815

.71

0.19

3.13

6.68

3.56

1.29

0.13

0.06

0.05

1.16

100.

0532

4963

528

0.52

54.6

06.

372.

027.

1814

.23

10.6

80.

198.

1010

.76

1.75

0.76

0.06

na0.

073.

4310

0.29

64na

na19

40.

8627

.52

0.92

0.28

1.67

13.6

910

.49

0.14

8.85

11.3

71.

300.

850.

08na

0.04

3.14

100.

3066

nana

203

0.30

31.5

61.

010.

322.

0415

.82

7.70

0.15

8.45

13.1

61.

470.

320.

04na

0.02

3.17

100.

0372

nana

166

0.56

11.1

20.

700.

211.

2513

.36

14.3

90.

173.

557.

362.

921.

140.

15na

0.06

2.20

99.6

736

53na

511

0.52

46.1

65.

451.

756.

8713

.36

13.3

30.

203.

827.

132.

981.

670.

13na

0.02

2.04

99.7

740

48na

264

0.59

75.1

15.

471.

647.

3812

.51

14.3

40.

223.

813.

823.

431.

660.

18na

0.04

2.96

99.6

638

47na

237

0.95

58.5

76.

992.

289.

0510

.12

21.6

50.

086.

340.

730.

460.

040.

18na

4.12

4.16

98.8

341

61na

176

0.32

1.36

11.2

76.

7216

.82

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sam

ple

JB97

-19A

JB97

-19B

JB97

-38

JB97

-45

JB97

-51

JB97

-52

JB97

-53

JB97

-59

JB97

-60

JB97

-64

JB97

-66

JB97

-98

JB97

-100

JB97

-105

JB98

-119

JB98

-120

JB98

-121

AJB

98-1

21B

Ta

La

Ce

PrSr

Nd

Zr

Hf

SmE

uT

i*G

dT

bD

yY

Ho

Er

Tm

Yb

Lu

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

ppm

0.08

5.66

12.2

71.

4717

3.30

6.39

na -

1.64

0.52

0.25

21.

770.

302.

00 -

0.47

1.30

0.19

1.23

0.17

0.08

4.19

9.53

1.20

162.

805.

42na

-1.

430.

490.

276

1.60

0.28

2.00

-0.

451.

320.

191.

200.

180.

155.

8712

.33

1.45

189.

605.

98na

1.05

1.39

0.53

0.30

61.

430.

241.

62 -

0.37

1.08

0.15

1.03

0.16

0.52

16.1

835

.82

4.65

220.

4020

.28

na3.

344.

981.

491.

169

5.13

0.84

5.49

-1.

093.

020.

432.

860.

410.

5418

.11

39.6

15.

0312

5.50

21.7

9na

4.21

5.24

1.67

1.22

35.

250.

885.

63 -

1.20

3.20

0.48

3.15

0.46

0.36

11.3

324

.88

3.28

122.

5014

.31

na2.

813.

751.

110.

839

3.80

0.64

4.06

-0.

852.

370.

342.

260.

350.

3510

.99

24.3

73.

1417

6.30

13.9

6na

2.74

3.62

1.09

0.65

93.

640.

613.

93 -

0.83

2.30

0.35

2.24

0.34

0.53

11.6

225

.69

3.35

196.

0014

.84

na2.

703.

671.

200.

773

3.92

0.65

4.08

-0.

852.

400.

342.

250.

330.

4111

.73

26.1

13.

3721

9.40

15.0

4na

2.99

3.79

1.13

0.74

93.

890.

644.

19 -

0.86

2.42

0.35

2.32

0.33

0.59

19.0

742

.09

5.18

141.

5020

.78

na4.

044.

741.

271.

187

4.97

0.81

4.68

-1.

042.

730.

402.

630.

390.

9521

.72

46.3

55.

7116

9.80

22.7

9na

4.16

5.03

1.43

1.36

15.

300.

885.

06 -

1.08

2.96

0.40

2.61

0.40

na4.

439.

541.

2426

7.90

5.56

33.8

60.

981.

500.

560.

324

1.72

0.28

1.82

10.2

20.

371.

050.

150.

950.

14na

4.52

9.94

1.31

160.

105.

9840

.32

1.19

1.68

0.59

0.34

81.

950.

322.

0512

.12

0.42

1.25

0.17

1.15

0.17

na3.

206.

820.

8717

4.40

3.93

26.5

90.

761.

080.

380.

204

1.33

0.22

1.58

9.79

0.33

0.99

0.14

0.94

0.15

0.57

20.1

140

.91

5.29

243.

4021

.60

119.

693.

714.

881.

451.

025

4.92

0.76

5.03

28.7

81.

012.

910.

382.

500.

390.

5619

.78

41.2

65.

4221

7.10

22.0

012

6.84

3.83

5.16

1.33

0.80

96.

360.

795.

0730

.18

1.06

3.04

0.41

2.57

0.40

0.71

23.5

450

.53

6.38

111.

0025

.47

152.

784.

685.

721.

440.

911

5.55

0.90

6.08

34.5

91.

223.

430.

483.

090.

461.

2820

.62

42.1

65.

557.

1022

.70

203.

096.

686.

591.

731.

133

10.5

62.

1315

.22

84.2

53.

288.

881.

196.

880.

99

APP

END

IX 1

: (C

) Nip

issi

ng G

abbr

o - G

eoch

emic

al D

ata

Sample JB97-65 JB97-78B JB97-48 JB97-49 JB98-207 JB98-224 JB98-239B JB98-239CTownship Wells Waters Wells Wells Kelly Janes Kelly Kelly

Field Name A A CM CM CM CM CM CMCIPW Name - - G G G G G GNormatives Q-H Q-H-C Q-H Q-H Q-H Q-H Q-H Q-HNorm Class so so so so so so so so

Norm Mineralsquartz 36.99 27.22 2.60 2.75 1.45 1.49 1.27 2.06

plagioclase 59.38 56.07 44.09 45.54 45.74 46.11 45.41 45.68orthoclase 0.65 4.37 5.91 6.50 3.43 1.54 6.32 3.60Nephelinecorundum 1.31diopside 0.32 19.77 15.83 23.38 20.13 19.58 20.33

hypersthene 1.11 4.44 22.79 24.19 22.61 26.29 24.11 24.93olivineilmenite 0.27 1.37 1.73 1.75 1.10 1.60 1.01 1.01

magnetite 0.22 0.62 2.58 2.73 2.09 2.61 2.04 2.20apatite 0.05 0.23 0.07 0.07 0.12 0.14 0.07 0.12zircon 0.01 0.01 0.01 0.01

chromite 0.01pyrite 0.28 1.27 0.13 0.17 0.11 0.13 0.19 0.08calcite 0.73 2.69 0.36 0.50

Na2CO3 0.40*Total: 100.01 99.99 100.03 100.03 100.04 100.05 100.01 100.02

*normalized to 100%; CIPW rock names based on weight % normative mineralsA = aplite; CM=chilled margin; G=gabbro; LG=leucogabbro; OPXG=orthopyroxene gabbro; MG=melagabbro; mtG=mt-bearing gabbroGG=Granophyric Gabbro; vtG=vari-textured Gabbro; qtzG=quartz GabbroOGN=olivine gabbronorite; MGN=melagabbronorite; GN=gabbronorite; OMGN=olivine melagabbronorite;OLGN=olivine leucogabbronorite; LG=leucogabbro; LGN=leucogabbronoriteNormatives: Q=quartz; N=nepheline; H=hypersthene; O=olivine; C=corundumNorm Class: su=silica-undersaturated(alkali basalt); ss=silica-saturated(olivine tholeiites); so=silica-oversaturated (quartz tholeiites);

APPENDIX 1: (D) Nipissing Gabbro CIPW Normatives

SampleTownship

Field NameCIPW NameNormativesNorm Class

Norm Mineralsquartz

plagioclaseorthoclaseNephelinecorundumdiopside

hyperstheneolivineilmenite

magnetiteapatitezircon

chromitepyritecalcite

Na2CO3

*Total:

JB98-240 JB97-4B JB97-18 JB97-20 JB97-24 JB97-25 JB97-26 JB97-27 JB97-28Kelly Waters Kelly Kelly Clement Clement Clement Clement ClementCM G G G G G G G GG G G G G G G G G

Q-H Q-H Q-H Q-H Q-H Q-H Q-H Q-H Q-Hso so so so so so so so so

1.40 1.13 3.40 3.16 2.25 2.65 2.49 2.62 3.1846.11 39.93 44.16 46.97 49.08 50.56 50.37 46.28 46.004.55 2.84 3.60 2.30 3.66 3.13 2.72 2.72 2.95

18.72 25.45 22.25 22.11 18.55 19.51 19.48 22.48 22.0225.64 27.25 23.13 22.20 22.18 20.36 21.01 21.83 21.47

1.18 0.91 1.01 0.99 1.27 1.18 1.22 1.12 1.422.22 1.99 2.03 1.90 2.35 2.09 2.20 2.16 2.380.12 0.05 0.05 0.09 0.07 0.09 0.07 0.090.01

0.11 0.04 0.13 0.04 0.04 0.11 0.15 0.13 0.150.50 0.27 0.30 0.52 0.39 0.30 0.61 0.34

100.06 100.04 100.03 100.02 99.99 100.05 100.03 100.02 100.00


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

JB97-29 JB97-30 JB97-31 JB97-32 JB97-34 JB97-36 JB97-40A JB97-40B JB97-41AClement Clement Clement Clement Foster Foster Janes Janes Janes

G G G G G G G G GG G G OLGN G G G G G

Q-H Q-H Q-H N-O Q-H Q-H Q-H Q-H Q-Hso so so su so so so so so

3.20 3.03 19.50 4.06 2.02 3.79 2.74 3.8950.14 49.26 30.12 54.78 45.58 51.39 44.81 41.17 47.203.19 4.02 7.62 6.91 4.79 6.09 2.78 2.54 2.01

1.01

18.50 19.06 17.56 8.00 16.60 8.88 18.16 18.17 9.5720.90 20.62 18.78 24.41 26.25 26.70 29.05 32.04

19.741.31 1.29 2.75 4.86 1.06 0.80 0.95 0.99 0.822.26 2.13 3.26 3.06 2.29 1.88 2.23 2.71 2.230.09 0.09 0.21 1.25 0.07 0.05 0.07 0.07 0.05

0.08 0.15 0.13 0.15 0.19 0.06 0.19 2.10 0.250.36 0.36 0.11 0.27 0.96 2.59 0.36 0.55 1.98

100.03 100.01 100.04 100.03 100.01 100.01 100.04 100.09 100.04


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

JB97-41C JB97-42A JB97-54B JB97-55 JB97-56 JB97-57 JB97-58 JB97-62 JB97-67Janes Janes Wells Wells Wells Wells Wells Wells Janes

G G G G G G G G GG G G G G G G G G

Q-H Q-H Q-H Q-H Q-H Q-H Q-H Q-H Q-Hso so so so so so so so so

2.73 4.10 0.73 1.96 2.45 3.28 3.30 2.48 0.1639.78 40.86 45.41 43.71 45.22 44.18 45.95 52.14 44.844.67 0.30 7.45 8.92 5.79 5.56 3.84 3.96 2.66

21.83 20.87 17.76 17.15 20.04 19.68 20.12 14.73 28.2227.29 30.01 22.74 23.57 22.01 22.36 21.72 22.55 21.37

0.82 0.72 2.20 1.69 1.56 1.71 1.80 1.39 0.782.10 2.31 3.06 2.58 2.46 2.65 2.62 2.44 1.830.05 0.05 0.12 0.07 0.02 0.07 0.07 0.14 0.09

0.03 0.010.25 0.25 0.19 0.17 0.15 0.17 0.17 0.08 0.060.50 0.57 0.36 0.20 0.32 0.36 0.41 0.09

100.02 100.04 100.02 100.02 100.02 100.02 100.00 100.03 100.02


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

JB97-70C JB97-70D JB97-75 JB97-76A JB97-77A JB97-77B JB97-78A JB97-84DLouise Louise Waters Waters Waters Waters Waters Louise

G G G G G G G GG G LG G LGN GN OGN G

Q-H Q-H Q-H Q-H H-O H-O H-O-C Q-Hso so so so ss ss ss so

0.81 1.76 13.87 0.25 2.3937.52 38.87 40.18 52.86 54.56 49.76 6.85 41.152.30 2.42 8.86 4.73 5.44 2.90 36.88 3.43

6.2725.58 26.14 8.72 14.54 16.38 18.36 23.1630.18 27.38 17.22 24.05 10.40 18.23 37.55 26.83

7.83 3.53 6.280.76 0.80 6.82 1.42 1.61 1.98 1.54 0.872.06 1.90 2.99 1.68 2.39 2.87 3.48 1.840.07 0.07 0.56 0.14 0.07 0.12 0.05 0.12

0.07 0.07 0.01 0.10 0.100.21 0.15 0.06 0.32 0.40 1.82 0.38 0.080.52 0.52 0.73 0.93 0.45 0.73 0.11

100.08 100.08 100.02 100.09 100.01 100.02 100.01 100.08


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

JB97-87A JB97-87B JB97-87J JB97-87K JB97-93 JB97-99 JB97-103E JB97-106AJanes Janes Janes Janes Porter Scadding Kelly Janes

G G G G G G G GG G G G OLGN GN G G

Q-H Q-H Q-H Q-H H-O-C H-O Q-H Q-Hso so so so ss ss so so

5.20 3.12 3.24 5.39 1.65 3.3942.31 42.50 43.24 43.73 45.75 49.27 45.02 45.263.43 4.37 2.72 2.66 24.47 8.16 2.54 3.90

0.4921.25 22.53 22.71 22.16 11.93 23.64 19.2724.45 23.86 23.35 22.85 11.36 21.31 23.66 24.93

12.52 4.101.03 1.03 0.93 0.91 2.13 1.94 1.08 0.952.13 2.20 2.17 1.94 2.46 2.94 2.20 2.040.16 0.14 0.14 0.16 0.25 0.25 0.19 0.140.01 0.01 0.01 0.01 0.01 0.010.01 0.01 0.03 0.03 0.010.06 0.28 1.61 0.21 0.34 0.13 0.02 0.15

0.23

100.04 100.05 100.14 100.05 100.01 100.04 100.01 100.04


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

JB97-106C JB98-114 JB98-118 JB98-148 JB98-149 JB98-150 JB98-151C JB98-174Janes Waters Wells Lorne Lorne Lorne Lorne Curtin

G G G G G G G GG GN G LGN GN LG GN GN

Q-H H-O Q-H H-O H-O Q-H H-O H-Oso ss so ss ss so ss ss

1.06 0.24 0.8046.83 34.75 50.94 19.87 24.91 26.91 32.00 54.023.84 1.77 7.15 0.83 0.83 2.25 2.66 1.24

20.46 30.01 13.77 34.97 30.14 24.26 24.98 25.1824.24 28.48 23.63 35.28 34.62 42.78 34.15 7.05

2.48 6.41 6.88 3.17 8.631.14 0.68 1.61 0.51 0.53 0.80 0.87 1.082.19 1.84 2.38 2.12 2.07 2.19 2.13 2.090.16 0.21 0.05 0.05 0.05 0.07 0.120.01 0.01 0.01

0.08 0.02 0.06 0.02 0.02 0.02 0.02 0.61

100.01 100.03 100.00 100.06 100.05 100.06 100.05 100.03


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

JB98-175 JB98-177 JB98-178 JB98-179 JB98-180 JB98-181 JB98-183 JB98-184Curtin Curtin Curtin Curtin Curtin Curtin Curtin Curtin

G G G G G G G GG G G G G G GN GN

Q-H Q-H Q-H Q-H Q-H Q-H H-O H-Oso so so so so so ss ss

0.14 2.23 0.65 2.74 1.37 2.5447.44 50.89 45.48 38.92 42.02 47.89 41.25 46.096.86 5.26 4.25 6.26 4.96 5.32 4.67 4.79

18.58 13.23 15.64 19.69 20.70 18.34 24.84 27.0324.17 24.93 30.47 29.17 27.89 22.77 20.88 12.36

5.18 7.080.84 1.22 1.04 0.99 0.87 0.95 0.80 0.851.86 2.13 2.36 2.07 2.00 1.96 1.93 1.680.07 0.09 0.05 0.02 0.05 0.07 0.02 0.07

0.01 0.01 0.01 0.01

0.08 0.04 0.06 0.15 0.17 0.17 0.51 0.08

100.04 100.03 100.01 100.02 100.03 100.02 100.08 100.03


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

JB98-194 JB98-195 JB98-196 JB98-198 JB98-199 JB98-200 JB98-201 JB98-202Kelly Kelly Kelly Kelly Kelly Kelly Kelly Kelly

G G G G G G G GG G G G G GN G G

Q-H Q-H Q-H Q-H Q-H H-O Q-H Q-Hso so so so so ss so so

1.81 2.40 0.07 1.80 2.40 1.40 3.4046.76 46.78 48.80 41.16 44.51 42.76 43.36 43.013.49 3.13 3.01 3.66 3.07 2.54 3.01 4.14

21.88 21.75 22.55 24.86 22.27 26.92 24.06 22.3922.68 22.49 22.80 25.03 24.50 22.66 25.32 23.69

2.111.12 1.10 0.84 1.04 1.01 0.84 0.87 1.102.07 2.17 1.83 2.19 2.13 2.07 1.87 2.000.09 0.07 0.07 0.07 0.12 0.05 0.07 0.120.01 0.01 0.01 0.01 0.01

0.11 0.13 0.06 0.19 0.02 0.08 0.08 0.17

100.02 100.03 100.03 100.01 100.04 100.03 100.04 100.03


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

JB98-203 JB98-205 JB98-206 JB98-209C JB98-210A JB98-212B JB98-228 JB98-229Kelly Kelly Kelly Louise Louise Louise Curtin Curtin

G G G G G G G GG G G G G GN GN GN

Q-H Q-H Q-H Q-H Q-H H-O H-O H-Oso so so so so ss ss ss

0.52 0.03 1.43 25.40 1.5744.23 44.00 45.23 31.06 46.21 44.81 44.01 42.233.84 1.83 3.31 0.35 5.97 1.77 3.55 2.36

23.51 28.95 23.43 8.79 19.48 23.97 29.63 27.2424.98 22.77 23.81 32.67 23.38 22.28 15.08 23.43

4.62 5.42 2.190.89 0.68 0.87 0.40 1.16 0.57 0.72 0.681.81 1.67 1.81 1.17 1.91 1.70 1.59 1.770.12 0.05 0.07 0.07 0.09 0.05 0.02 0.07

0.01 0.01 0.01

0.13 0.04 0.08 0.06 0.25 0.28 0.02 0.04

100.03 100.02 100.05 99.98 100.03 100.05 100.04 100.01


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

JB98-230 JB98-231 JB98-239D JB98-239E JB98-239F RK-1 RK-2 RK-5 RK-7Curtin Curtin Kelly Kelly Kelly Waters Waters Waters Waters

G G G G G G G G GGN G GN G G G OGN LG GNH-O Q-H H-O Q-H Q-H Q-H H-O Q-H H-Oss so ss so so so ss so ss

2.42 1.11 3.36 17.14 5.3443.84 37.28 48.56 46.99 49.49 17.82 43.36 52.39 35.052.36 3.55 4.49 3.96 2.19 6.56 5.73 5.91 3.25

27.33 25.19 20.08 21.54 18.19 5.17 21.71 15.92 29.0520.39 28.63 23.51 23.24 23.56 48.67 16.75 15.15 27.113.59 0.08 9.59 2.340.68 0.78 1.03 1.04 1.03 0.66 0.55 2.32 0.841.71 2.04 1.96 1.94 2.09 2.25 1.83 2.35 1.960.02 0.05 0.12 0.09 0.07 0.07 0.07 0.37 0.09

0.01 0.01 0.01

0.11 0.11 0.19 0.11 0.04 1.59 0.02 0.08 0.020.14 0.43 0.18 0.32

100.03 100.05 100.03 100.03 100.03 100.07 100.04 100.01 100.03


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

RK-8 RK-9 RK-10 RK-11 RK-12 RK-13 RK-14 RK-15 RK-16 RK-17 RK-18Waters Waters Waters Waters Waters Waters Waters Waters Waters Waters Waters

G G G G G G G G G G GGN GN GN G G G GN LG GN GN LGNH-O H-O H-O Q-H Q-H Q-H H-O H-O H-O H-O H-Oss ss ss so so so ss ss ss ss ss

0.16 0.59 0.7634.52 21.92 20.71 20.15 20.36 53.23 56.21 59.48 46.17 45.67 19.713.01 1.24 1.24 1.12 1.24 3.07 2.90 3.25 3.37 2.72 1.24

28.78 40.05 38.72 34.50 37.96 18.22 20.26 17.44 26.91 25.65 35.6128.73 29.13 35.15 41.06 36.78 21.83 12.14 15.64 13.21 19.45 39.261.85 4.57 1.04 5.71 1.48 8.17 3.28 1.130.91 0.80 0.80 0.74 0.82 0.95 0.97 0.97 0.59 1.01 0.761.97 2.13 2.15 2.17 2.16 1.78 1.68 1.54 1.45 1.88 2.220.09 0.05 0.07 0.05 0.09 0.12 0.07 0.12 0.05 0.28 0.09

0.04 0.02 0.02 0.04 0.02 0.04 0.04 0.02 0.02 0.04 0.020.16 0.14 0.16 0.05 0.05 0.05 0.05 0.09 0.11 0.05

100.06 100.05 100.06 100.04 100.07 100.05 100.03 100.03 100.05 100.03 100.04


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

RK-19 JB97-50 JB97-54A JB97-63 JB98-122 JB97-14 JB97-15 JB97-16 JB97-43BWaters Wells Wells Wells Bridgland Kelly Kelly Kelly Janes

G GG GG GG GG OPXG OPXG OPXG OPXGLGN G LG G LG G G G GH-O Q-H Q-H-C Q-H Q-H Q-H Q-H Q-H Q-Hss so so so so so so so so

2.75 16.73 0.83 6.26 1.03 3.38 2.94 3.9060.02 40.51 34.46 49.64 45.28 47.85 43.61 43.90 45.043.37 12.47 0.41 9.63 10.93 2.66 2.72 2.72 2.90

4.4116.58 13.89 9.94 13.16 23.51 23.53 25.35 22.3014.42 23.69 23.54 23.89 17.92 21.50 23.04 21.47 22.012.980.93 2.68 0.93 2.11 3.02 0.89 1.06 1.03 1.041.58 3.25 3.23 2.87 2.96 1.77 2.15 2.03 1.960.09 0.12 0.25 0.25 0.37 0.07 0.07 0.05 0.07

0.030.01

0.02 0.23 1.99 0.17 0.11 0.11 0.08 0.17 0.080.05 0.45 12.79 0.68 0.64 0.39 0.36 0.73

1.24100.04 100.04 99.98 100.02 100.04 100.03 100.03 100.02 100.03


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

JB97-43D JB97-61 JB97-76B JB97-95 JB97-103B JB97-103D JB97-106B JB97-107Janes Wells Waters Janes Kelly Kelly Janes Janes

OPXG OPXG OPXG OPXG OPXG OPXG OPXG OPXGG OLGN GN G GN G G G

Q-H H-O H-O Q-H H-O Q-H Q-H Q-Hso ss ss so ss so so so

2.13 2.03 0.96 0.09 0.6346.01 50.50 52.78 42.16 39.14 42.00 47.38 43.962.07 8.92 2.72 3.31 2.07 3.72 2.54 3.19

24.28 9.26 19.72 25.54 31.97 26.75 21.64 28.3321.26 9.94 17.63 22.77 23.63 23.26 24.79 21.14

11.35 1.00 0.040.76 5.22 1.42 0.85 0.85 0.99 1.10 0.761.77 3.18 1.87 1.93 2.04 2.10 2.23 1.800.05 1.30 0.30 0.09 0.14 0.09 0.12 0.12

0.01 0.010.03 0.10

0.85 0.15 1.72 0.98 0.15 0.15 0.11 0.110.91 0.20 0.86 0.41

100.09 100.05 100.02 100.17 100.03 100.03 100.01 100.04


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

JB97-108 JB98-123 JB98-147 JB98-182 JB98-204 JB97-37 JB97-47 JB97-79BJanes Bridgland Lorne Curtin Kelly Foster Ermatinger Waters

OPXG OPXG OPXG OPXG OPXG LG LG LGG GN MGN GN G G G G

Q-H H-O H-O H-O Q-H Q-H Q-H Q-Hso ss ss ss so so so so

3.09 1.59 4.53 4.89 0.6342.08 50.08 16.11 41.08 45.02 46.71 46.98 42.952.95 1.89 0.24 4.20 2.19 4.08 2.95 3.13

25.45 25.24 37.81 25.54 25.58 18.81 18.57 23.5523.43 16.87 37.80 21.25 22.80 21.93 21.52 26.76

3.28 5.54 4.800.84 0.80 0.47 0.82 0.91 1.06 1.73 0.821.97 1.73 2.04 2.09 1.86 2.29 2.67 1.780.12 0.07 0.02 0.07 0.07 0.07 0.05 0.07

0.100.08 0.08 0.02 0.19 0.02 0.15 0.11 0.02

0.36 0.57 0.30

100.01 100.04 100.05 100.04 100.04 99.99 100.04 100.11


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

JB97-104 JB98-115 JB97-71 JB97-80A JB98-197 JB98-124 JB98-146 JB97-19AJanes Janes Louise Louise Kelly Kirkwood Lorne KellyLG LG MG MG mtG qtzG qtzG qtzGG G G G G G GN G

Q-H Q-H Q-H Q-H Q-H Q-H H-O Q-Hso so so so so so ss so

4.00 1.73 0.13 0.17 5.77 2.07 2.6439.26 43.24 44.78 43.19 45.34 46.49 47.30 43.041.95 3.31 4.14 4.43 4.61 5.02 1.89 1.71

24.30 21.15 22.22 25.65 18.77 21.76 23.61 23.2027.71 25.77 25.50 23.41 21.13 21.32 23.85 26.28

0.620.63 0.89 0.53 0.78 1.56 1.10 0.91 0.821.96 2.28 1.70 1.75 2.52 2.03 1.74 1.930.09 0.07 0.05 0.07 0.19 0.12 0.05 0.02

0.01 0.01 0.01 0.010.07 0.10

0.13 1.70 0.11 0.08 0.13 0.11 0.04 0.080.84 0.45 0.32

100.03 100.15 100.07 100.08 100.03 100.03 100.02 100.04


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

JB97-19B JB97-38 JB97-45 JB97-51 JB97-52 JB97-53 JB97-59 JB97-60 JB97-64Kelly Foster Moncrieff Wells Wells Wells Wells Wells WellsvtG vtG vtG vtG vtG vtG vtG vtG vtGG GN G LG G G G G LG

Q-H H-O Q-H Q-H Q-H Q-H Q-H Q-H Q-Hso ss so so so so so so so

2.30 5.37 4.23 1.31 3.09 5.35 5.33 5.3444.55 51.52 44.91 49.14 45.15 42.66 43.26 43.22 44.645.02 7.68 5.08 6.26 10.81 11.05 6.56 6.32 10.05

23.97 15.48 13.02 7.06 4.84 14.21 16.91 17.43 13.8720.87 18.10 23.33 24.53 30.31 23.15 21.59 21.59 18.28

3.440.89 1.01 3.82 3.97 2.77 2.15 2.49 2.41 3.861.71 1.91 3.78 3.84 3.74 2.93 3.18 3.10 3.230.05 0.07 0.21 0.21 0.12 0.12 0.12 0.12 0.35

0.010.15 0.06 0.30 0.34 0.28 0.21 0.23 0.21 0.170.50 0.73 0.20 0.41 0.71 0.45 0.34 0.30 0.23

100.01 100.00 100.02 99.99 100.04 100.02 100.03 100.03 100.03


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

JB97-66 JB97-98 JB97-100 JB97-105 JB98-119 JB98-120 JB98-121A JB97-41BWells Scadding Scadding Janes Wells Wells Wells JanesvtG vtG vtG vtG vtG vtG vtG GLG G G G G G LG GQ-H Q-H Q-H Q-H Q-H Q-H Q-H Q-Hso so so so so so so so

4.05 0.96 1.60 0.88 6.98 6.08 9.27 1.7147.98 45.33 41.56 49.96 46.40 44.86 44.87 38.857.80 4.67 5.20 1.95 6.97 10.22 10.28 4.49

13.30 20.70 22.76 24.76 13.66 14.34 3.49 19.9118.67 24.75 25.28 20.04 19.08 18.69 25.48 28.71

4.41 1.06 1.14 0.66 3.38 2.66 3.02 0.763.26 2.26 2.20 1.62 3.03 2.80 3.04 2.610.30 0.14 0.19 0.09 0.37 0.30 0.44 0.02

0.01 0.03 0.03 0.030.010.11 0.15 0.08 0.04 0.13 0.04 0.11 2.570.14 0.48

100.03 100.02 100.02 100.00 100.03 100.02 100.03 100.11


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

JB97-42B JB97-43A JB97-43C JB97-109 JB97-87C JB97-87D JB97-87E JB97-87FJanes Janes Janes Janes Janes Janes Janes Janes

G OPXG OPXG OPXG G G G GG G G LG G G G G

Q-H Q-H Q-H Q-H Q-H Q-H Q-H Q-Hso so so so so so so so

1.98 3.79 1.29 2.37 8.50 2.61 7.79 7.1039.69 39.41 40.78 49.27 40.70 40.99 38.63 41.034.14 3.49 1.00 0.71 1.12 4.08 3.07 1.89

17.55 18.29 21.74 3.15 13.83 18.24 13.38 15.8328.80 23.68 25.55 28.39 28.40 23.49 28.69 25.47

0.72 0.89 0.85 1.14 0.89 0.93 0.99 0.952.81 3.00 3.02 3.71 2.77 2.94 2.86 2.770.02 0.05 0.05 0.19 0.16 0.12 0.12 0.14

0.01 0.010.03 0.01 0.01 0.03

4.07 7.76 5.98 12.38 3.99 7.21 4.90 5.280.39 0.32 0.27

100.17 100.68 100.53 101.31 100.40 100.62 100.45 100.49


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

JB97-87G JB97-87H JB97-87I 44731 44737 44744 44769 44792 44799 44805Janes Janes Janes Janes Janes Janes Janes Janes Janes Janes

G G G vtG vtG OPXG OPXG OPXG OPXG OPXGG G G GN G GN GN GN G G

Q-H Q-H Q-H H-O Q-H H-O H-O H-O Q-H Q-Hso so so ss so ss ss ss so so

8.98 5.47 4.36 0.8 0.7 1.0838.43 41.50 41.55 48.6 44.96 44.86 48.3 43.16 44.37 45.173.07 2.66 3.19 4.25 2.3 2.36 3.84 2.54 2.6 1.89

15.12 18.92 20.64 26.73 29.37 29.21 25.56 27.02 24.64 23.4527.07 24.33 24.69 10.94 20.19 19.27 11.83 21.5 24.11 22.71

7.06 1.58 7.03 1.370.87 0.82 0.85 0.76 0.7 0.76 0.68 0.8 0.8 0.782.58 2.48 2.32 1.57 1.54 1.7 1.65 1.91 1.84 2.10.16 0.14 0.12 0.05 0.05 0.09 0.07 0.07 0.07 0.07

0.01 0.03 0.013.99 4.05 2.48 0.06 0.11 0.19 1.1 1.76 0.98 2.99

100.28 100.40 100.21 100.02 100.02 100.02 100.06 100.13 100.11 100.24


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

44812 44685 44692 44700 44705 44708 44711 44713 44714 44716 44718Janes Janes Janes Janes Janes Janes Janes Janes Janes Janes Janes

OPXG OPXG OPXG OPXG OPXG OPXG OPXG OPXG OPXG OPXG OPXGG G G G G G G G G G G

Q-H Q-H Q-H Q-H Q-H Q-H Q-H Q-H Q-H Q-H Q-Hso so so so so so so so so so so

2.46 2.04 4.33 1.37 3.66 3.25 3.15 4.8 4.4 3.43 1.6144.85 41.91 40.64 46.43 44.21 44.74 42.76 41.19 40.54 44.49 45.281.89 2.54 3.19 1.89 2.19 2.01 2.01 2.01 2.13 2.13 2.07

20.87 20.06 17.52 20.51 20.2 20.54 19.12 17.53 18.43 16.92 18.5124.08 23.4 25.17 23.23 22.57 22.46 24.38 25.79 25.34 26.14 25.38

0.84 0.78 0.8 0.87 0.84 0.84 0.74 0.74 0.78 0.93 0.932.15 2.67 2.6 2.28 2.35 2.33 2.61 2.7 2.78 2.32 2.420.07 0.02 0.07 0.05 0.05 0.07 0.09 0.09 0.05 0.07 0.07

2.99 7.15 6.11 3.71 4.3 4.09 5.73 5.7 6.15 3.94 4.09

100.20 100.57 100.43 100.34 100.37 100.33 100.59 100.55 100.60 100.37 100.36


SampleTownship


Norm Mineralsquartz





Na2CO3

*Total:

44720 44722 44725 44758Janes Janes Janes Janes

OPXG G G GG G OLGN G

Q-H Q-H H-O Q-Hso so ss so

0.81 2.64 2.2245.5 46.48 47.84 45.32.25 2.66 5.91 3.19

22.01 20.96 8.44 21.8325.12 24.27 6.96 24.34

27.10.95 0.91 0.99 0.972.13 1.9 2.17 1.940.07 0.07 0.09 0.09

1.31 0.13 0.51 0.13

100.15 100.02 100.01 100.01


Sample No. LLD Method1 SZM01 SZM02 SZM03 SZM04 SZM05 CZM01 CZM02Field Name gab gab gab Lgab gab Lgab Lgab

CIPW3 OGN GN GN OLGN GN Lgab GNTexture mg mg mg mg-cg mg cg cgFeature2 massive massive massive massive massive massive b-qtz; biot

V-S 0 0 3 2 1 2 <1Type2 M M M M M M M

Strat. Unit BX BX BX BX BX BX BXSiO2 0.01 1 49.67 50.27 50.05 48.74 50.42 51.20 51.32TiO2 0.01 1 0.27 0.21 0.17 0.15 0.19 0.55 0.46Al2O3 0.01 1 16.65 17.24 17.08 23.47 16.90 19.06 16.12

Fe2O3* 0.01 1 10.52 9.29 9.73 7.70 9.61 8.41 10.51MnO 0.01 1 0.18 0.16 0.17 0.10 0.17 0.15 0.19MgO 0.01 1 8.53 8.44 8.33 3.64 8.55 5.33 7.60CaO 0.01 1 10.23 10.37 9.96 10.15 10.69 11.10 9.69Na2O 0.01 1 2.68 2.48 2.44 3.15 2.24 2.61 2.45K2O 0.01 1 0.33 0.34 0.52 0.92 0.24 0.83 1.02P2O5 0.01 1 0.01 0.01 0.02 0.02 0.02 0.03 0.04CO2 0.03 3 0.12 0.09 0.03 0.04 0.02 0.08 0.03

S 0.01 3 0.03 0.09 0.36 0.77 0.08 0.05 0.03LOI 0.05 2 1.27 1.35 1.46 1.47 1.17 1.14 0.80

Total: 100.34 100.17 99.91 99.51 100.22 100.42 100.20Mg# 65 68 67 52 67 60 63Cs 0.007 5 0.227 0.238 0.322 0.729 0.212 0.785 0.993Rb 0.050 5 4.140 6.080 13.210 16.960 3.770 22.410 30.440Ba 1.000 5 76 84 74 141 57 268 336Th 0.060 5 0.080 0.080 0.170 0.410 0.060 1.310 0.840U 0.007 5 0.035 0.027 0.042 0.170 0.020 0.429 0.240

Nb 0.200 5 0.200 0.200 0.400 0.500 0.100 1.400 1.200Ta 0.170 5 0.090 0.180 0.090 0.180 0.090 0.220 0.220La 0.020 5 2.420 1.970 2.010 2.830 1.680 6.610 5.730Ce 0.070 5 5.720 4.300 4.140 5.820 3.650 13.940 12.050Pr 0.006 5 0.786 0.581 0.570 0.746 0.542 1.703 1.595Sr 0.500 5 360 342 365 510 284 648 406Nd 0.030 5 3.850 2.600 2.500 2.910 2.270 6.660 6.380Zr 4.000 5 9.900 9.300 9.100 15.300 9.200 38.800 28.000Hf 0.100 5 0.300 0.300 0.300 0.400 0.300 1.100 0.800Sm 0.010 5 1.040 0.770 0.630 0.730 0.660 1.600 1.620Eu 0.005 5 0.565 0.398 0.401 0.506 0.393 0.717 0.774Ti 10.000 5 1223 1020 743 679 879 2749 2081Gd 0.009 5 1.206 0.761 0.821 0.789 0.911 1.593 1.931Tb 0.003 5 0.213 0.140 0.151 0.108 0.157 0.302 0.297Dy 0.008 5 1.244 1.012 0.909 0.711 0.921 1.813 1.875Y 0.020 5 7.210 6.110 4.240 3.930 5.170 9.070 9.940Ho 0.003 5 0.297 0.220 0.206 0.172 0.232 0.366 0.420Er 0.008 5 0.872 0.668 0.602 0.497 0.641 1.042 1.304Tm 0.003 5 0.137 0.097 0.083 0.078 0.106 0.162 0.172Yb 0.010 5 0.900 0.760 0.590 0.530 0.700 1.040 1.160Lu 0.003 5 0.155 0.102 0.088 0.073 0.103 0.153 0.198

∑REE 19.41 14.38 13.70 16.50 12.97 37.70 35.51Se 8 7 128 773 2476 6011 669 163 112Ni 3 4 189 253 367 632 261 107 139Ir 0.04 6 0.33 3.79 8.18 33.10 4.79 1.20 0.20

Ru 0.13 6 0.21 1.80 2.59 20.20 2.29 1.90 0.30

APPENDIX 1: (E) River Valley - Matrix/Fragment

Sample No. LLD Method1 SZM01 SZM02 SZM03 SZM04 SZM05 CZM01 CZM02Field Name gab gab gab Lgab gab Lgab Lgab

CIPW3 OGN GN GN OLGN GN Lgab GNTexture mg mg mg mg-cg mg cg cgFeature2 massive massive massive massive massive massive b-qtz; biot

V-S 0 0 3 2 1 2 <1Type2 M M M M M M M

Strat. Unit BX BX BX BX BX BX BXRh 0.08 6 1.15 18.90 40.60 156.00 25.30 5.49 0.40Pt 0.14 6 13.40 171.00 360.00 1637.00 200.00 61.30 8.98Pd 0.11 6 18.40 623.00 1261.00 7164.00 797.00 125.00 12.50Au 0.71 6 7.73 34.70 88.70 192.00 53.20 19.50 7.38Cu 3 4 175.0 614.0 1901.0 2586.0 673.0 319.0 219.0

Pd+Pt 32 794 1621 8801 997 186 21Pd/Ir 55.76 164.38 154.16 216.44 166.39 104.17 62.50Cu/Ni 0.9 2.4 5.2 4.1 2.6 3.0 1.6S/Se 2344 1164 1454 1281 1196 3067 2679Pd/Pt 1.4 3.6 3.5 4.4 4.0 2.0 1.4

Notes: Major Element Oxides, S, CO2, and LOI are in wt. percent; trace element contents are in ppm; Cu-Ni contents are in ppm; PGE and Se contents are in ppbLLD=lower limit of detection; "-" = not detected/determined1Method: 1=WD-XRF, 2=Lebo thermogravimetry, 3=Leco infrared combustion, 4=DCP, 5=ICP-MS, 6=NiS/ICP-MS, 7=AAS-hydride,8=Fire Assay/DCP2Sample Type/Features: M=matrix; F=fragment; b-qtz=blue quartz; biot=biotite; hem=hematiteRock Type: Mgab=melagabbro, Lgab=leucogabbro;gab=gabbro; V-S=visible sulphide3CIPW Name: OGN=olivine gabbronorite; MGN=melagabbronorite; GN=gabbronorite; OMGN=olivine melagabbronorite; OLGN=olivine leucogabbronorite; LG=leucogabbro


Sample No.Field Name

CIPW3

TextureFeature2

V-SType2

Strat. UnitSiO2

TiO2

Al2O3

Fe2O3*MnOMgOCaONa2OK2OP2O5

CO2

SLOI

Total:Mg#CsRbBaThU

NbTaLaCePrSrNdZrHfSmEuTiGdTbDyYHoErTmYbLu

∑REESeNiIr

Ru

CZM03 SZF01 SZF02 SZF03 SZF04 SZF05 CZF01 CZF02 CZF03gab Mgab Mgab Mgab Mgab gab gab gab gabGN MGN MGN OMGN MGN MGN GN GN MGN

mg-cg fg fg fg-mg mg fg-mg fg-mg fg fgb-qtz; biot massive massive massive biot massive massive biot-hem massive

<1 0 0 2 3 2 1 1 2M F F F F F F F FBX BX BX BX BX BX BX BX BX

51.19 48.68 48.77 46.05 50.79 48.39 47.31 47.10 48.260.43 0.45 0.46 0.24 0.84 0.27 0.27 0.37 0.38

15.89 5.96 6.92 7.51 5.74 8.47 11.58 9.34 11.0210.50 14.74 13.81 15.44 15.86 14.52 14.61 15.86 15.200.19 0.26 0.26 0.28 0.25 0.25 0.24 0.26 0.247.88 14.73 14.56 16.09 12.94 13.85 12.62 13.33 12.009.32 12.04 12.08 10.33 9.64 10.46 7.55 8.60 7.442.26 0.57 0.72 0.45 0.41 0.66 0.35 0.57 0.711.05 0.12 0.22 0.08 0.86 0.15 0.66 1.09 1.220.05 0.07 0.02 0.01 0.08 0.01 0.02 0.03 0.030.04 0.10 0.15 0.09 0.05 0.05 0.06 0.02 0.040.13 0.19 0.02 0.23 0.97 0.38 0.15 0.03 0.141.13 1.11 1.21 2.43 1.23 1.80 3.04 1.98 2.22

99.89 98.72 99.04 98.91 98.63 98.83 98.24 98.53 98.7264 70 71 71 66 69 67 66 65

1.052 0.122 0.202 0.151 1.645 0.153 0.806 1.533 1.70635.050 0.920 4.470 1.080 36.640 1.350 20.710 36.900 43.360

397 90 64 20 352 99 251 356 4611.160 1.050 0.490 0.130 3.070 0.100 0.480 0.480 0.6300.256 0.348 0.137 0.037 0.820 0.028 0.115 0.157 0.1501.300 1.100 0.800 0.300 3.500 0.100 0.600 0.700 0.7000.220 0.250 0.210 0.090 0.400 0.090 0.090 0.190 0.2206.400 2.680 2.100 0.610 10.170 1.340 3.170 2.660 4.53013.340 8.260 5.290 1.510 24.260 3.380 6.480 5.920 9.5901.706 1.286 0.807 0.269 3.110 0.492 0.831 0.789 1.259393 12 34 7 11 27 117 11 70

7.040 6.440 3.610 1.430 13.160 2.580 3.480 3.450 5.22045.200 46.100 23.200 11.100 69.600 9.900 16.200 19.600 21.0001.200 1.500 0.800 0.400 2.100 0.400 0.500 0.700 0.6001.620 1.900 1.240 0.680 3.120 0.760 0.820 0.930 1.2400.901 0.411 0.461 0.228 0.516 0.317 0.339 0.356 0.6142029 1996 2192 1074 3813 1248 1243 1732 17571.836 2.502 1.784 1.019 3.249 1.157 1.164 1.318 1.5760.306 0.394 0.361 0.178 0.501 0.214 0.182 0.236 0.2741.894 2.291 2.232 1.222 3.226 1.227 1.146 1.461 1.75310.450 10.760 11.410 5.720 17.310 7.020 6.670 7.650 8.7600.447 0.450 0.474 0.261 0.764 0.295 0.240 0.333 0.3721.254 1.359 1.530 0.762 2.115 0.847 0.839 0.974 1.1230.211 0.213 0.216 0.100 0.318 0.153 0.116 0.143 0.1651.350 1.240 1.380 0.710 2.120 0.930 0.820 1.040 0.9400.218 0.179 0.211 0.115 0.319 0.142 0.135 0.157 0.17238.52 29.61 21.70 9.09 66.95 13.83 19.76 19.77 28.83466 1614 231 1260 5981 2389 1589 77 631164 399 327 496 427 605 428 256 3080.53 0.08 3.29 0.13 14.60 21.60 0.30 0.25 0.220.59 0.33 1.60 0.26 6.98 10.10 0.44 0.30 0.38


Sample No.Field Name

CIPW3

TextureFeature2

V-SType2

Strat. UnitRhPtPdAuCu

Pd+PtPd/IrCu/NiS/SePd/Pt

CZM03 SZF01 SZF02 SZF03 SZF04 SZF05 CZF01 CZF02 CZF03gab Mgab Mgab Mgab Mgab gab gab gab gabGN MGN MGN OMGN MGN MGN GN GN MGN

mg-cg fg fg fg-mg mg fg-mg fg-mg fg fgb-qtz; biot massive massive massive biot massive massive biot-hem massive

<1 0 0 2 3 2 1 1 2M F F F F F F F FBX BX BX BX BX BX BX BX BX2.21 0.10 16.60 0.28 75.10 103.00 0.46 0.39 0.33

20.70 1.44 210.00 4.31 683.00 847.00 8.16 7.20 4.6175.90 1.79 713.00 11.20 1899.00 3196.00 22.60 2.94 4.7528.90 7.91 22.40 23.10 143.00 164.00 24.60 8.72 17.90651.0 275.0 179.0 716.0 2008.0 2202.0 523.0 175.0 486.0

97 3 923 16 2582 4043 31 10 9143.21 22.38 216.72 86.15 130.07 147.96 75.33 11.76 21.59

4.0 0.7 0.5 1.4 4.7 3.6 1.2 0.7 1.62790 1177 866 1825 1622 1590 944 3896 22193.7 1.2 3.4 2.6 2.8 3.8 2.8 0.4 1.0


Sample SZM01 SZF01 SZM02 SZF02 SZM03 SZF03 SZM04 SZF04Rock Type OGN MGN GN MGN GN OMGN OLGN MGN

Norm Mineralsquartz 5.25

plagioclase 56.06 18.82 56.93 21.77 55.86 23.10 75.19 15.17orthoclase 2.01 0.71 2.07 1.36 3.13 0.47 5.56 5.26diopside 14.66 37.99 13.34 36.69 12.54 27.40 2.55 29.95

hypersthene 13.50 34.72 19.41 30.56 19.76 31.46 3.33 37.02olivine 10.76 2.96 5.56 5.40 5.52 13.07 9.82


apatite 0.02 0.16 0.05 0.05 0.05 0.05 0.19zircon 0.01 0.01

chromite 0.04 0.09 0.06 0.09 0.06 0.09 0.01 0.04pyrite 0.06 0.42 0.19 0.04 0.78 0.51 1.65 2.12calcite 0.27 0.23 0.20 0.34 0.07 0.20 0.09 0.11

*Total: 100.06 100.10 100.07 100.11 100.11 100.10 100.12 100.09Sample SZM05 SZF05 CZM01 CZF01 CZM02 CZF02 CZM03 CZF03

Rock Type GN MGN LG GN GN GN GN MGNNorm Minerals

quartz 0.23 1.40plagioclase 55.28 26.28 60.76 32.96 51.49 25.78 50.25 30.67orthoclase 1.42 0.95 4.96 4.14 6.09 6.74 6.32 7.56diopside 14.60 26.91 13.98 7.75 14.80 19.52 13.15 11.38

hypersthene 23.44 40.20 16.97 49.56 21.62 35.18 26.49 45.48olivine 2.73 1.16 2.76 8.53 0.33 0.45


apatite 0.05 0.07 0.05 0.09 0.07 0.12 0.07zircon 0.01 0.01

chromite 0.04 0.09 0.03 0.09 0.04 0.09 0.06 0.09pyrite 0.17 0.85 0.11 0.34 0.06 0.06 0.28 0.32calcite 0.11 0.18 0.14 0.07 0.09 0.09

*Total: 100.08 100.14 100.09 100.13 100.07 100.09 100.11 100.10*normalized to 100%; "SZ" = South Zone, "CZ" = Central Zone"M" = matrix, "F" = fragment; rock names based on weight % normative mineralsOGN=olivine gabbronorite; MGN=melagabbronorite; GN=gabbronorite; OMGN=olivine melagabbronorite;OLGN=olivine leucogabbronorite; LG=leucogabbro

APPENDIX 1: (F) River Valley Intrusion - CIPW Matrix/Fragment

Sample 22692 22696 29601 29607 29612 29618 29622 29635 29645 29654Rock Type OGN OGN OGN OGN GN OGN OGN OGN OLGN LGN

Unit LU LU LU LU LU LU LU LU IBZ IBZNorm Minerals

quartzplagioclase 53.91 53.50 56.67 55.81 58.01 47.03 57.45 42.44 73.12 73.99orthoclase 3.78 3.60 3.60 3.31 4.14 3.13 3.90 4.85 5.20 5.26corundumdiopside 9.54 8.77 6.71 9.31 8.72 12.07 8.64 11.19 7.03 5.17

hypersthene 18.03 19.15 16.58 16.50 17.67 19.16 16.81 17.65 0.53 6.78olivine 10.91 11.35 12.58 11.41 7.90 14.53 9.50 18.85 11.70 6.68ilmenite 0.91 0.74 0.82 0.89 0.85 0.80 0.84 1.35 0.74 0.59

magnetite 2.49 2.52 2.52 2.42 2.23 3.00 2.38 3.29 1.41 1.23apatite 0.14 0.12 0.14 0.12 0.14 0.05 0.09 0.14 0.12 0.09zircon 0.01 0.01 0.01

chromitepyrite 0.13 0.06 0.13 0.08 0.15 0.11 0.19 0.17 0.06 0.04calcite 0.16 0.23 0.27 0.16 0.23 0.16 0.25 0.09 0.14 0.16

*Total: 100.01 100.04 100.02 100.02 100.04 100.04 100.05 100.03 100.05 99.99

Sample 29702 29707 29717 29721 29733 29744 29753 29756 29762Rock Type LGN GN GN LGN G OLGN OGN GN LGN

Unit BX BX BX BX BX BX BX BX FBXNorm Minerals

quartz 3.34plagioclase 65.97 55.10 51.10 62.23 32.83 62.15 54.09 48.91 59.01orthoclase 4.79 2.25 2.84 2.72 4.37 3.49 5.50 5.97 8.16corundum 0.18diopside 5.41 13.34 10.97 9.21 13.02 9.45 5.85 15.38

hypersthene 12.85 21.52 30.54 18.46 41.80 10.37 6.62 24.64 21.19olivine 7.24 3.59 1.63 5.19 12.14 23.95 1.76 6.81ilmenite 0.27 0.36 0.32 0.30 0.55 0.42 0.53 0.65 1.39

magnetite 1.81 2.09 2.16 1.65 2.93 1.78 2.44 2.31 2.16apatite 0.02 0.02 0.02 0.02 0.05 0.02 0.07 0.02 0.14zircon

chromitepyrite 1.70 1.70 0.38 0.11 1.04 0.02 0.76 0.32 0.93calcite 0.05 0.14 0.09 0.16 0.11 0.20 0.25 0.09 0.07

*Total: 100.11 100.11 100.05 100.05 100.04 100.04 100.06 100.05 100.04*normalized to 100%; rock names based on weight % normative mineralsOGN=olivine gabbronorite; MGN=melagabbronorite; GN=gabbronorite; OMGN=olivine melagabbronorite;OLGN=olivine leucogabbronorite; LG=leucogabbro

APPENDIX 1: (F) River Valley Intrusion - CIPW RV00-22

Sample 29662 29670 29676 29683 29689 29696Rock Type LGN OLGN LGN LGN GN GN

Unit IBZ IBZ IBZ IBZ BX BXNorm Minerals

quartzplagioclase 65.43 66.27 64.30 69.73 52.45 39.35orthoclase 4.37 2.54 2.95 4.79 1.77 3.37corundumdiopside 8.75 5.28 13.44 8.19 16.09 14.53

hypersthene 11.42 10.53 10.15 11.08 18.65 35.24olivine 7.65 13.32 6.87 4.65 8.73 3.52ilmenite 0.49 0.21 0.28 0.27 0.25 0.46

magnetite 1.55 1.70 1.36 1.13 1.88 2.78apatite 0.07 0.02 0.02 0.02 0.02 0.02zircon

chromitepyrite 0.04 0.02 0.04 0.02 0.08 0.64calcite 0.25 0.14 0.59 0.14 0.09 0.16

*Total: 100.02 100.03 100.00 100.02 100.01 100.07

APPENDIX 1: (F) River Valley Intrusion - CIPW RV00-22

Sample From To Interval Tag No. Au(ppb) Pt(ppb) Pd(ppb) Ni(ppm) Cu(ppm) Strat1 0.00 1.00 1.00 22690 8 39 27 91 86.5 LU2 1.00 2.50 1.50 22691 14 33 27 102 77.4 LU3 2.50 4.00 1.50 22692 7 41 29 116 117 LU4 4.00 5.50 1.50 22693 8 48 29 112 112 LU5 5.50 7.00 1.50 22694 16 42 31 102 103 LU6 7.00 8.50 1.50 22695 7 25 23 108 95.5 LU7 8.50 10.00 1.50 22696 9 53 26 105 110 LU8 10.00 12.00 2.00 22697 5 14 10 105 96.3 LU9 12.00 14.00 2.00 22698 6 27 19 90 84.5 LU10 14.00 16.00 2.00 22699 10 29 22 88 99.5 LU11 16.00 18.00 2.00 22700 7 37 23 101 107 LU12 18.00 20.00 2.00 29601 8 30 22 79 77.5 LU13 20.00 22.00 2.00 29602 9 32 17 89 96.8 LU14 22.00 24.00 2.00 29603 7 20 17 79 94.2 LU15 24.00 26.00 2.00 29604 5 10 12 78 97.5 LU16 26.00 28.00 2.00 29605 9 45 29 79 83.1 LU17 28.00 30.00 2.00 29606 10 36 33 76 102 LU18 30.00 32.00 2.00 29607 7 36 29 87 93 LU19 32.00 34.00 2.00 29608 7 31 23 105 92.9 LU20 34.00 36.00 2.00 29609 9 29 31 90 95.9 LU21 36.00 38.00 2.00 29610 7 22 18 89 116 LU22 38.00 40.00 2.00 29611 7 23 19 77 94.6 LU23 40.00 42.00 2.00 29612 3 25 11 76 64.7 LU24 42.00 44.00 2.00 29613 5 24 13 81 116 LU25 44.00 46.00 2.00 29614 5 24 14 75 51.3 LU26 46.00 48.00 2.00 29615 6 16 12 72 81.6 LU27 48.00 49.35 1.35 29616 1 22 8 76 47 LU28 49.35 50.85 1.50 29617 3 0 0 23 21.7 LU29 50.85 52.00 1.15 29618 4 18 11 78 97.8 LU30 52.00 54.00 2.00 29619 3 28 16 90 101 LU31 54.00 56.00 2.00 29620 3 20 11 91 90.8 LU32 56.00 58.00 2.00 29621 3 28 13 103 87.9 LU33 58.00 60.00 2.00 29622 3 0 8 94 92 LU34 60.00 61.75 1.75 29623 13 56 27 138 21.1 LU35 61.75 62.60 0.85 29624 12 33 14 24 37.1 LU36 62.60 64.00 1.40 29625 10 36 17 109 67.3 LU37 64.00 66.10 2.10 29626 10 40 24 113 84.8 LU38 66.10 67.40 1.30 29627 9 49 27 172 78.4 LU39 67.40 68.85 1.45 29628 12 44 38 90 143 LU40 68.85 70.20 1.35 29629 13 31 30 113 108 LU41 70.20 72.20 2.00 29630 10 49 29 96 119 LU42 72.20 74.00 1.80 29631 10 38 23 107 132 LU43 74.00 75.18 1.18 29632 8 41 16 120 55.9 LU44 75.18 75.30 0.12 29633 10 59 17 279 9590 LU45 75.30 77.00 1.70 29634 10 27 26 112 118 LU46 77.00 79.00 2.00 29635 12 33 15 158 134 LU47 79.00 81.00 2.00 29636 9 19 12 179 82.7 LU48 81.00 81.40 0.40 29637 11 23 10 212 164 LU49 81.40 82.80 1.40 29638 7 15 10 136 99.2 LU50 82.80 85.00 2.20 29639 10 31 20 90 108 LU51 85.00 86.50 1.50 29640 11 44 33 104 145 LU52 86.50 88.00 1.50 29641 11 31 22 155 118 LU

APPENDIX 1: (G) River Valley Intrusion - Group-1 Data RV00-22

Sample From To Interval Tag No. Au(ppb) Pt(ppb) Pd(ppb) Ni(ppm) Cu(ppm) Strat53 88.00 89.50 1.50 29642 8 33 22 93 113 LU54 89.50 91.00 1.50 29643 9 24 20 57 33.4 IBZ55 91.00 92.50 1.50 29644 7 26 17 63 84.8 IBZ56 92.50 94.00 1.50 29645 12 208 581 44 40.5 IBZ57 94.00 95.50 1.50 29646 6 30 21 41 43.7 IBZ58 95.50 97.00 1.50 29647 4 23 12 30 96.9 IBZ59 97.00 98.50 1.50 29648 4 24 14 85 45.5 IBZ60 98.50 100.00 1.50 29649 5 25 18 77 45.9 IBZ61 100.00 102.00 2.00 29650 5 15 15 65 55 IBZ62 102.00 104.00 2.00 29651 12 28 17 78 125 IBZ63 104.00 106.00 2.00 29652 6 34 13 49 54 IBZ64 106.00 108.00 2.00 29653 11 24 13 50 86.8 IBZ65 108.00 110.00 2.00 29654 5 33 13 27 47.9 IBZ66 110.00 112.00 2.00 29655 6 24 11 63 40.4 IBZ67 112.00 114.00 2.00 29656 5 34 11 30 54.9 IBZ68 114.00 116.00 2.00 29657 3 31 19 31 46.6 IBZ69 116.00 118.00 2.00 29658 6 30 18 30 60.9 IBZ70 118.00 120.00 2.00 29659 4 32 17 34 34.2 IBZ71 120.00 122.30 2.30 29660 3 32 20 41 33.9 IBZ72 122.30 124.00 1.70 29661 9 129 222 61 59.1 IBZ73 124.00 126.00 2.00 29662 4 87 86 40 36 IBZ74 126.00 128.00 2.00 29663 9 72 59 28 145 IBZ75 128.00 130.00 2.00 29664 9 84 63 32 96.6 IBZ76 130.00 132.00 2.00 29665 9 68 56 29 121 IBZ77 132.00 134.00 2.00 29666 14 58 49 34 109 IBZ78 134.00 135.50 1.50 29667 7 83 90 18 41.1 IBZ79 135.50 136.55 1.05 29668 8 38 64 23 54.6 IBZ80 136.55 138.00 1.45 29669 3 53 62 63 33.7 IBZ81 138.00 140.00 2.00 29670 7 198 192 81 13.6 IBZ82 140.00 142.00 2.00 29671 6 170 257 60 29.6 IBZ83 142.00 144.00 2.00 29672 2 45 65 87 22.8 IBZ84 144.00 146.00 2.00 29673 6 110 131 69 27.1 IBZ85 146.00 148.00 2.00 29674 5 101 121 109 10.7 IBZ86 148.00 150.00 2.00 29675 16 70 66 27 73.6 IBZ87 150.00 152.00 2.00 29676 14 134 130 27 95.9 IBZ88 152.00 152.90 0.90 29677 10 118 105 30 53.3 IBZ89 152.90 154.00 1.10 29678 9 32 17 15 82.1 IBZ90 154.00 155.50 1.50 29679 38 125 109 32 57.3 IBZ91 155.50 157.00 1.50 29680 7 89 62 32 42.4 IBZ92 157.00 158.50 1.50 29681 27 287 520 26 116 IBZ93 158.50 160.00 1.50 29682 12 153 202 25 49.3 IBZ94 160.00 160.80 0.80 29683 34 206 331 19 48.9 IBZ95 160.80 161.80 1.00 29684 26 76 108 48 305 BX96 161.80 162.50 0.70 29685 52 304 600 62 335 BX97 162.50 163.00 0.50 29686 30 124 144 73 414 BX98 163.00 165.00 2.00 29687 37 156 273 28 62.1 BX99 165.00 166.65 1.65 29688 28 80 139 141 368 BX

100 166.65 167.50 0.85 29689 19 74 204 68 262 BX101 167.50 168.50 1.00 29690 23 93 122 55 243 BX102 168.50 170.15 1.65 29691 7 68 94 44 283 BX103 170.15 171.15 1.00 29692 36 141 289 34 274 BX104 171.15 172.00 0.85 29693 27 94 225 47 203 BX


Sample From To Interval Tag No. Au(ppb) Pt(ppb) Pd(ppb) Ni(ppm) Cu(ppm) Strat105 172.00 173.00 1.00 29694 13 53 87 58 56.7 BX106 173.00 173.50 0.50 29695 45 166 391 123 553 BX107 173.50 175.00 1.50 29696 119 553 1173 156 1220 BX108 175.00 176.25 1.25 29697 76 359 818 132 735 BX109 176.25 177.75 1.50 29698 57 162 269 123 783 BX110 177.75 179.40 1.65 29699 52 143 224 145 719 BX111 179.40 179.90 0.50 29700 138 672 1750 276 1690 BX112 179.90 181.00 1.10 29701 247 1613 4834 491 2310 BX113 181.00 181.85 0.85 29702 443 2310 6600 532 3600 BX114 181.85 182.90 1.05 29703 345 1510 4915 330 2770 BX115 182.90 184.40 1.50 29704 17 70 66 25 149 BX116 184.40 184.60 0.20 29705 323 576 1958 195 2290 BX117 184.60 185.05 0.45 29706 66 396 1131 107 607 BX118 185.05 185.65 0.60 29707 151 1639 3400 108 621 BX119 185.65 186.40 0.75 29708 98 552 1387 161 1080 BX120 186.40 187.00 0.60 29709 50 256 674 78 388 BX121 187.00 187.45 0.45 29710 130 709 2173 230 1460 BX122 187.45 188.30 0.85 29711 105 422 1133 166 1300 BX123 188.30 190.00 1.70 29712 25 172 400 109 162 BX124 190.00 190.50 0.50 29713 184 895 3001 260 1890 BX125 190.50 191.30 0.80 29714 40 206 516 116 395 BX126 191.30 191.65 0.35 29715 143 1212 3160 435 1650 BX127 191.65 193.00 1.35 29716 26 138 330 95 285 BX128 193.00 193.70 0.70 29717 75 436 1112 172 825 BX129 193.70 194.50 0.80 29718 128 653 1583 394 1850 BX130 194.50 196.00 1.50 29719 94 429 1178 196 1140 BX131 196.00 197.15 1.15 29720 152 826 2719 372 2180 BX132 197.15 198.55 1.40 29721 71 328 937 383 2240 BX133 198.55 199.30 0.75 29722 13 50 90 23 151 BX134 199.30 200.00 0.70 29723 47 601 2203 247 805 BX135 200.00 201.00 1.00 29724 129 494 1648 285 1700 BX136 201.00 202.00 1.00 29725 160 959 3603 356 2090 BX137 202.00 202.80 0.80 29726 266 1044 3976 442 3550 BX138 202.80 203.05 0.25 29727 315 2001 9140 696 4940 BX139 203.05 203.55 0.50 29728 307 879 3251 386 3400 BX140 203.55 204.10 0.55 29729 50 195 627 96 677 BX141 204.10 205.30 1.20 29730 29 175 431 102 320 BX142 205.30 206.35 1.05 29731 33 162 438 109 505 BX143 206.35 207.05 0.70 29732 112 557 1525 414 1930 BX144 207.05 207.75 0.70 29733 63 339 943 328 1130 BX145 207.75 208.75 1.00 29734 43 516 1609 258 433 BX146 208.75 209.65 0.90 29735 121 865 2661 439 1680 BX147 209.65 210.20 0.55 29736 85 604 1889 259 1080 BX148 210.20 211.00 0.80 29737 77 337 1247 244 1200 BX149 211.00 211.60 0.60 29738 119 598 1826 324 1410 BX150 211.60 212.50 0.90 29739 59 218 492 111 745 BX151 212.50 213.10 0.60 29740 71 489 1300 312 1010 BX152 213.10 213.50 0.40 29741 123 645 1836 530 2210 BX153 213.50 214.15 0.65 29742 106 398 1124 442 1630 BX154 214.15 215.30 1.15 29743 86 303 824 365 1020 BX155 215.30 216.80 1.50 29744 16 166 512 109 151 BX156 216.80 217.60 0.80 29745 99 634 1717 320 1400 BX


Sample From To Interval Tag No. Au(ppb) Pt(ppb) Pd(ppb) Ni(ppm) Cu(ppm) Strat157 217.60 219.00 1.40 29746 35 293 859 185 597 BX158 219.00 220.00 1.00 29747 109 586 1798 258 1250 BX159 220.00 220.85 0.85 29748 75 401 1054 243 1050 BX160 220.85 221.40 0.55 29749 63 581 1708 311 1090 BX161 221.40 222.30 0.90 29750 160 742 2104 502 2090 BX162 222.30 223.00 0.70 29751 65 370 1162 259 1190 BX163 223.00 224.50 1.50 29752 24 102 194 142 392 BX164 224.50 225.70 1.20 29753 26 115 309 119 357 BX165 225.70 227.25 1.55 29754 40 171 373 151 743 BZ166 227.25 229.00 1.75 29755 21 65 110 88 414 BZ167 229.00 229.70 0.70 29756 26 79 191 94 476 BZ168 229.70 231.00 1.30 29757 12 45 68 147 164 BZ169 231.00 232.00 1.00 29758 17 56 175 176 145 BZ170 232.00 233.20 1.20 29759 9 40 70 163 84.3 BZ171 233.20 235.00 1.80 29760 20 15 19 144 90.1 FBX172 235.00 236.50 1.50 29761 13 24 19 170 114 FBX173 236.50 238.00 1.50 29762 7 21 14 123 95.6 FBX174 238.00 239.50 1.50 29763 22 28 16 137 88.9 FBX175 239.50 241.50 2.00 29764 17 0 15 148 60.4 FBX


LLD Method1 Sample No. 22692 22696 29601 29607 29612 29618 29622 29635Field Name Mgab Mgab Mgab Mgab Mgab Mgab Mgab Mgab

CIPW3 OGN OGN OGN OGN GN OGN OGN OGNTexture mg-cg mg-cg mg-cg mg-cg mg-cg mg-cg mg-cg mg-cgFeature massive massive massive massive massive massive massive massiveType L L L L L L L L

Interval (m) 1.50 0.52 0.46 2.00 0.39 0.28 0.28 2.00Depth (m) 4.00 9.56 18.68 32.00 40.49 51.89 59.21 79.00Strat. Unit LU LU LU LU LU LU LU LU

0.01 1 SiO2 48.62 48.38 47.58 48.99 49.30 46.20 48.86 45.260.01 1 TiO2 0.47 0.38 0.42 0.46 0.44 0.40 0.43 0.680.01 1 Al2O3 16.84 16.74 17.80 17.08 18.18 14.64 17.98 13.580.01 1 Fe2O3* 12.11 12.16 12.14 11.75 10.87 14.22 11.51 15.560.01 1 MnO 0.17 0.18 0.18 0.17 0.16 0.19 0.16 0.210.01 1 MgO 8.74 9.10 8.37 8.54 7.47 10.01 7.65 11.010.01 1 CaO 9.32 9.20 9.31 9.20 9.70 9.18 9.62 8.400.01 1 Na2O 2.24 2.15 2.16 2.50 2.41 1.68 2.37 1.490.01 1 K2O 0.63 0.60 0.60 0.55 0.69 0.51 0.65 0.790.01 1 P2O5 0.06 0.05 0.06 0.05 0.06 0.02 0.04 0.060.03 3 CO2 0.07 0.10 0.12 0.07 0.10 0.07 0.11 0.040.01 3 S 0.06 0.03 0.06 0.04 0.07 0.05 0.09 0.080.05 2 LOI 1.82 2.19 2.17 1.82 1.73 2.37 1.85 2.37

Total: 101.02 101.12 100.80 101.11 101.01 99.41 101.12 99.42Mg# 63 64 62 63 62 62 61 62

0.007 5 Cs 0.910 1.023 0.926 0.680 0.904 0.623 0.729 1.3800.007 5 U 0.280 0.262 0.272 0.290 0.260 0.308 0.211 0.2800.050 5 Rb 18.450 17.630 18.160 15.050 20.420 13.890 17.790 25.8100.060 5 Th 1.290 1.020 1.200 1.560 1.150 0.560 1.050 1.3300.200 5 Nb 2.080 1.500 1.700 1.990 1.600 1.200 1.200 2.2200.200 5 Ta 0.100 0.240 0.220 0.100 0.230 0.220 0.220 0.1000.020 5 La 7.460 6.060 7.090 6.620 6.560 3.560 5.600 6.8600.070 5 Ce 15.470 12.730 14.560 13.860 13.790 7.680 11.380 14.4700.006 5 Pr 1.950 1.609 1.819 1.750 1.717 0.983 1.454 1.8500.500 5 Sr 251.010 239.100 234.400 286.850 281.800 174.700 285.100 145.3300.030 5 Nd 7.850 6.660 7.480 6.820 7.380 4.070 5.810 7.3404.000 5 Zr 39.890 22.100 29.800 44.090 27.800 18.600 21.900 48.0200.100 5 Hf 1.120 0.600 0.700 1.220 0.800 0.500 0.600 1.3400.010 5 Sm 1.820 1.600 1.620 1.590 1.640 1.200 1.540 1.7500.005 5 Eu 0.700 0.603 0.687 0.650 0.706 0.510 0.649 0.6700.009 5 Gd 1.960 1.752 1.843 1.780 1.940 1.264 1.658 1.9100.006 5 Tb 0.340 0.299 0.313 0.300 0.283 0.248 0.247 0.3300.008 5 Dy 2.140 1.869 1.966 1.880 1.932 1.612 1.704 2.0600.020 5 Y 12.970 11.640 11.910 11.040 11.760 9.250 10.140 11.9200.003 5 Ho 0.490 0.421 0.400 0.430 0.400 0.305 0.353 0.4600.008 5 Er 1.390 1.245 1.198 1.200 1.267 1.033 1.030 1.2600.003 5 Tm 0.210 0.169 0.178 0.190 0.172 0.159 0.172 0.2100.010 5 Yb 1.370 1.160 1.240 1.110 1.210 0.940 1.140 1.2300.003 5 Lu 0.222 0.186 0.183 0.183 0.177 0.144 0.143 0.209

7 7 Se 160 157 230 141 264 206 349 2411 4 Ni 116 237 242 87 216 238 219 158

0.04 6 Ir 0.39 0.86 0.92 0.35 0.60 1.15 1.23 0.280.13 6 Ru 0.24 1.32 2.53 0.18 1.02 1.93 1.65 0.200.08 6 Rh 0.90 1.05 1.03 0.91 0.79 1.19 1.87 0.730.14 6 Pt 21.40 19.40 15.40 13.23 13.50 18.50 16.90 9.760.11 6 Pd 20.90 19.10 13.20 13.05 13.00 16.40 14.20 12.020.71 6 Au 4.41 4.57 5.29 4.43 4.02 4.04 5.20 8.690.50 4 Cu 117.0 68.0 123.0 93.0 139.0 100.0 157.0 134.0

APPENDIX 1: (H) River Valley Intrusion - Group-2 RV00-22

LLD Method1 Sample No.Field Name

CIPW3TextureFeatureType

Interval (m)Depth (m)Strat. Unit

0.01 1 SiO20.01 1 TiO20.01 1 Al2O30.01 1 Fe2O3*0.01 1 MnO0.01 1 MgO0.01 1 CaO0.01 1 Na2O0.01 1 K2O0.01 1 P2O50.03 3 CO20.01 3 S0.05 2 LOI

Total:Mg#

0.007 5 Cs0.007 5 U0.050 5 Rb0.060 5 Th0.200 5 Nb0.200 5 Ta0.020 5 La0.070 5 Ce0.006 5 Pr0.500 5 Sr0.030 5 Nd4.000 5 Zr0.100 5 Hf0.010 5 Sm0.005 5 Eu0.009 5 Gd0.006 5 Tb0.008 5 Dy0.020 5 Y0.003 5 Ho0.008 5 Er0.003 5 Tm0.010 5 Yb0.003 5 Lu

7 7 Se1 4 Ni

0.04 6 Ir0.13 6 Ru0.08 6 Rh0.14 6 Pt0.11 6 Pd0.71 6 Au0.50 4 Cu

29645 29654 29662 29670 29676 29683 29689 29696Lgab-gab Lgab-gab gab gab-Mgab gab gab gab-Mgab gabOLGN LGN LGN OLGN LGN LGN GN GNcg-peg cg-peg cg-peg mg-cg cg-peg cg-peg mg mg

massive massive b-qtz massive b-qtz b-qtz massive massiveF F M-F M M M M-F M

1.50 2.00 2.00 2.00 2.00 0.80 0.85 0.5194.00 110.00 126.00 140.00 152.00 160.80 167.50 174.51IBZ IBZ IBZ IBZ IBZ IBZ BX BX

49.64 49.81 49.59 47.53 49.66 51.09 48.83 47.940.39 0.31 0.26 0.11 0.15 0.14 0.13 0.2322.73 23.49 20.87 21.21 20.30 21.85 16.14 12.606.85 5.99 7.52 8.18 6.65 5.52 9.03 13.080.10 0.09 0.13 0.13 0.12 0.10 0.17 0.214.52 4.32 6.52 8.06 6.90 5.63 10.23 11.4210.90 11.17 11.10 10.89 12.32 10.99 10.90 9.033.21 2.88 2.47 2.09 2.40 2.90 1.93 1.210.87 0.88 0.73 0.42 0.49 0.80 0.29 0.540.05 0.04 0.03 0.01 0.01 0.01 0.01 0.010.06 0.07 0.11 0.06 0.26 0.06 0.04 0.070.03 0.02 0.02 0.01 0.02 0.01 0.04 0.291.23 1.34 1.51 2.17 1.31 1.35 1.90 2.31

100.49 100.33 100.73 100.80 100.30 100.40 99.55 98.5661 63 67 70 71 70 73 67

0.860 0.980 0.670 0.440 0.610 0.780 0.290 0.8690.310 0.210 0.120 0.030 0.270 0.590 0.020 0.188

21.230 21.000 18.850 10.550 10.170 19.730 7.560 17.5400.940 0.700 0.490 0.130 0.280 0.620 0.060 0.4701.970 1.410 0.920 0.300 0.380 0.760 0.140 0.5000.100 0.100 0.100 0.750 0.100 0.100 0.100 0.2405.610 4.480 2.590 1.090 1.960 1.760 0.920 2.680

11.730 9.280 5.250 2.050 4.110 3.540 1.790 5.5701.470 1.160 0.660 0.260 0.540 0.450 0.240 0.718

397.210 352.720 344.290 293.970 391.890 432.550 239.320 146.1005.710 4.550 2.660 1.020 2.220 1.810 1.100 3.080

34.600 31.360 21.560 6.360 10.260 13.710 2.000 8.3001.030 0.830 0.600 0.200 0.310 0.390 0.140 0.2001.280 1.080 0.650 0.260 0.620 0.420 0.320 0.8100.640 0.520 0.370 0.230 0.390 0.320 0.260 0.3451.400 1.150 0.760 0.300 0.740 0.490 0.430 0.8720.240 0.180 0.140 0.050 0.130 0.090 0.080 0.1421.480 1.150 0.860 0.340 0.820 0.610 0.550 0.8748.650 7.000 4.860 2.070 5.210 3.480 3.360 5.8500.330 0.270 0.200 0.080 0.190 0.140 0.120 0.2240.910 0.710 0.570 0.240 0.540 0.360 0.400 0.7110.140 0.110 0.090 0.040 0.090 0.060 0.060 0.1080.910 0.720 0.520 0.240 0.580 0.380 0.410 0.7300.146 0.106 0.083 0.041 0.094 0.062 0.064 0.106

97 89 63 26 98 66 252 221944 27 40 81 27 19 68 419

2.95 1.05 3.18 6.09 2.32 1.70 1.53 5.432.13 0.93 1.11 1.60 1.58 3.12 0.55 1.4713.50 2.44 11.67 24.80 7.44 5.73 6.35 25.10

168.60 11.78 66.00 177.30 110.20 60.60 74.50 332.001864.00 10.26 85.20 188.00 200.00 125.50 164.20 763.00

8.18 2.54 2.64 2.96 14.90 8.20 22.50 54.8040.5 47.9 36.0 13.6 95.9 48.9 262.0 1820.0






Total:Mg#


7 7 Se1 4 Ni

0.04 6 Ir0.13 6 Ru0.08 6 Rh0.14 6 Pt0.11 6 Pd0.71 6 Au0.50 4 Cu

29702 29707 29717 29721 29733 29744 29753gab-Lgab-Mgab gab gab gab gab-Mgab-Lgab gab gab

LGN GN GN LGN G OLGN OGNmg mg mg fg-mg mg mg mg

massive massive massive massive massive massive massiveM-F M M M M-F M M0.85 0.48 0.70 0.51 0.70 0.37 0.23

181.85 185.58 193.70 198.01 207.75 215.87 224.93BX BX BX BX BX BX BX

48.81 49.80 50.41 50.58 50.61 49.40 45.790.14 0.19 0.17 0.16 0.28 0.22 0.27

20.48 17.26 16.19 19.13 10.95 19.24 16.408.70 10.22 10.45 7.99 13.99 8.67 11.430.12 0.17 0.18 0.14 0.20 0.15 0.185.98 8.36 9.69 7.73 11.76 8.01 10.549.67 10.64 9.63 10.21 7.88 10.27 7.892.70 2.18 1.89 2.62 1.01 2.63 2.360.79 0.38 0.47 0.45 0.72 0.58 0.890.01 0.01 0.01 0.01 0.02 0.01 0.030.02 0.06 0.04 0.07 0.05 0.09 0.100.78 0.79 0.18 0.05 0.47 0.01 0.341.46 1.31 2.03 1.69 2.42 1.89 2.81

98.86 100.52 101.12 100.72 99.83 101.07 98.5862 66 68 69 66 68 68

0.520 0.363 0.530 0.556 1.220 0.605 1.5710.080 0.133 0.090 0.122 1.120 0.123 2.80023.450 10.020 13.670 13.210 26.760 17.880 29.7200.210 0.310 0.290 0.340 1.560 0.210 0.5700.320 0.400 0.340 0.400 1.420 0.200 0.8000.100 0.100 0.100 0.170 0.100 0.100 0.2202.270 2.220 2.440 2.740 4.160 2.300 6.0904.620 4.520 4.720 5.480 8.640 4.570 12.0400.580 0.579 0.600 0.682 1.070 0.591 1.435

450.000 369.700 314.510 425.000 153.260 401.100 382.4002.310 2.530 2.370 2.750 4.000 2.520 5.9009.560 5.000 8.810 5.300 26.180 4.400 15.3000.270 0.200 0.260 0.200 0.780 0.200 0.5000.540 0.730 0.560 0.740 0.950 0.640 1.2600.500 0.426 0.370 0.392 0.360 0.445 0.6990.600 0.666 0.660 0.712 1.050 0.807 1.3120.110 0.116 0.120 0.117 0.190 0.140 0.2070.680 0.828 0.750 0.768 1.170 0.880 1.3174.000 5.230 4.680 4.630 7.290 5.570 7.8700.150 0.185 0.180 0.156 0.300 0.201 0.2800.440 0.609 0.500 0.541 0.820 0.611 0.8410.070 0.086 0.080 0.072 0.150 0.105 0.1350.430 0.610 0.550 0.590 0.910 0.710 0.9500.072 0.095 0.095 0.092 0.158 0.095 0.1625230 5792 963 317 2183 40 1837532 615 172 261 328 151 341

54.40 5.13 8.42 27.60 7.99 6.14 8.2415.60 1.54 4.15 11.20 3.72 2.83 2.5194.47 25.20 40.30 125.40 30.82 22.80 38.10

2375.00 718.00 439.00 1085.00 324.00 278.00 347.006670.00 1733.00 1099.00 3593.00 872.00 795.00 1102.00376.00 246.00 60.60 65.80 62.70 47.20 48.103600.0 2700.0 825.0 377.0 1130.0 20.0 348.0






Total:Mg#


7 7 Se1 4 Ni

0.04 6 Ir0.13 6 Ru0.08 6 Rh0.14 6 Pt0.11 6 Pd0.71 6 Au0.50 4 Cu

29756 29762 RV22-01 RV22-02 RV22-03gab-Mgab gneiss

GN LGN - - -mg fg-mg fg fg fg

sheared foliated foliated foliated foliated; blue qtzM-F FBX gneiss gneiss gneiss0.70 1.50 0.30 0.26 0.22

229.70 238.00 244.30 250.26 256.00BZ FBX FW FW FW

51.18 50.59 48.69 51.69 55.700.34 0.71 0.45 0.46 0.37

15.79 18.00 19.22 18.12 19.3811.28 10.40 11.38 10.40 7.250.17 0.13 0.13 0.13 0.088.06 7.21 8.45 7.32 4.979.98 6.18 3.76 5.63 4.442.10 3.22 3.67 3.25 4.641.00 1.34 1.20 1.29 1.140.01 0.06 0.05 0.03 0.050.04 0.03 0.02 0.02 0.030.15 0.43 0.47 0.36 0.260.98 2.33 3.49 2.48 2.27

100.91 100.19 100.49 100.79 100.2762 62 63 62 61

1.720 2.310 2.170 2.292 1.9500.510 0.820 1.500 0.914 1.93335.160 44.470 36.000 37.360 30.9300.480 1.120 1.120 1.380 2.2800.380 1.310 180.000 1.100 1.8000.100 0.100 0.270 0.270 0.4103.130 17.410 22.400 20.460 38.8006.310 29.690 39.900 36.370 65.6200.830 3.280 4.180 3.898 6.571

450.000 450.000 726.000 887.700 1065.0003.550 11.300 14.600 13.200 21.86011.620 30.550 30.600 28.800 55.5000.410 0.920 0.900 0.900 1.8000.980 1.600 2.100 1.840 2.6000.570 1.740 1.700 2.126 2.2961.150 1.180 1.430 1.367 1.8760.200 0.160 0.198 0.190 0.2111.250 0.900 1.160 1.040 1.0627.790 5.640 7.000 5.910 6.0900.300 0.200 0.246 0.214 0.2230.860 0.630 0.773 0.742 0.7080.140 0.100 0.130 0.143 0.1270.880 0.760 0.940 1.050 0.8400.147 0.136 0.159 0.167 0.154598 292 217 277 18494 123 200 191 133

1.46 0.19 0.13 0.28 0.100.87 0.36 0.36 0.59 0.328.50 0.69 0.19 0.20 0.11

68.30 3.53 3.01 3.10 1.71214.00 4.87 3.90 3.15 2.1218.50 1.71 0.36 0.36 0.36476.0 95.6 61.0 96.0 60.0


538

APPENDIX 2:

PETROGRAPHIC DESCRIPTIONS

A) Nipissing Gabbro intrusions (Hand Specimens) 539 B) River Valley intrusion (Matrix/Fragment Specimens, DDH RV00-22) 553 NOTES AND KEY: 1specific pyroxene not discernable 2primarily after pyroxene and biotite - not included in the mode total "x"=present in trace amounts "msv"=massive Field Names: A = aplite; CM=chilled margin; G=gabbro; LG=leucogabbro; OPXG=orthopyroxene gabbro; MG=melagabbro; mtG=mt-bearing gabbro GG=Granophyric Gabbro; vtG=vari-textured Gabbro; qtzG=quartz Gabbro CIPW Names: OGN=olivine gabbronorite; MGN=melagabbronorite; GN=gabbronorite; OMGN=olivine melagabbronorite OLGN=olivine leucogabbronorite; LG=leucogabbro; LGN=leucogabbronorite Normatives and CIPW Classification: Q=quartz; N=nepheline; H=hypersthene; O=olivine; C=corundum su=silica-undersaturated (alkali basalt); ss=silica-saturated (olivine tholeiites); so=silica-oversaturated (quartz tholeiites) Textures (petrographic descriptions): EA=extensively altered g-h=granular hypidiomorphic d-i=diabasic-isogranular g-i=granular-idiomorphic qcpV=contains qtz-cpy veins gb=granoblastic g-m=granular mosaic porph=porphyritic

Sample JB97-65 JB97-78B JB97-48 JB97-49 JB98-207 JB98-224 JB98-239B JB98-239CTownship Wells Waters Wells Wells Kelly Janes Kelly Kelly

Intrusion/Area 1W 17C 1W 1W 10E 8E 10E 10EField Name A A CM CM CM CM CM CMRock Name A A CM CM CM CM CM CM

Grain fg fg-mg fg fg fg vfg vfg fgMain Texture g-i g-m d-i d-i d-i d-i d-i d-i

2nd Texture porph porph porphComments qtz-carb vein

CIPW Name - - G G G G G GNormatives Q-H Q-H-C Q-H Q-H Q-H Q-H Q-H Q-H

MineralsQuartz 50 35 2 2 1 3 2 2

Plagioclase 30 43 40 40 50 40 43 43K-spar 20 20

1Pyroxene 53 53 47OrthopyroxeneClinopyroxene 49 5 55 55

PigeoniteGranophyre x xMyrmekite x x

Biotite 1 x x x x xEpidote x 5 5 x 3 x xApatite x x x x xTitanite x x

LeucoxeneZircon

Opaques x 1 x x x 2 x xAlteration

2Amphibole 53 53 45 45 45 45Carbonate x2Chlorite x 1 x x x x x xSericite x x x x x x x x

Saussurite x x x x x x x xTotal Mode: 100 100 100 100 100 100 100 100

APPENDIX 2: (A) Nipissing Gabbro Intrusions

SampleTownship

Intrusion/AreaField NameRock Name

GrainMain Texture

2nd TextureComments

CIPW NameNormatives

MineralsQuartz

PlagioclaseK-spar

1PyroxeneOrthopyroxeneClinopyroxene

PigeoniteGranophyreMyrmekite

BiotiteEpidoteApatiteTitanite

LeucoxeneZircon

OpaquesAlteration

2AmphiboleCarbonate2ChloriteSericite

SaussuriteTotal Mode:

JB98-240 JB97-40B JB97-55 JB97-56 JB97-57 JB97-58 JB97-62 JB97-77BKelly Janes Wells Wells Wells Wells Wells Waters10E 8E 1W 1W 1W 1W 1W 17CCM G G G G G G GCM G G G G G G Gvfg mg mg mg mg mg mg mgd-i g-h g-h g-i g-i g-i g-i g-m

porphhigh epidote

G G G G G G G GNQ-H Q-H Q-H Q-H Q-H Q-H Q-H H-O

2 5 x x x x x43 27 45 45 50 50 50 42

135 46

5 5 555 50 50 50 50 45

x x x x xx

x x x x x x 10x 30 x x x x xx x x x

xx 3 x x x x x 1

45 40 45 45 40 40x x

x x x x x x x xx x x x x x x xx x x x x x x x

100 100 100 100 100 100 100 100


SampleTownship


GrainMain Texture

2nd TextureComments

CIPW NameNormatives

MineralsQuartz

PlagioclaseK-spar




LeucoxeneZircon

OpaquesAlteration



JB97-84D JB97-87A JB97-87B JB97-87J JB97-87K JB97-99 JB97-103ELouise Janes Janes Janes Janes Scadding Kelly

13C 8E 8E 8E 8E 16E 10EG G G G G G G

MG GN GN G G CM Gmg mg mg mg mg fg mgg-m g-i g-i g-h g-h d-i g-i

porph porph

G G G G G GN GQ-H Q-H Q-H Q-H Q-H H-O Q-H

2 2 1 4 5 10 x27 43 43 32 35 40 50x

47 45 59 542 5 2 5

70 5 3 50 45

1 x

x xx x x 3 2 x x

x x xx

1 1 2 2 2 x x

60 45 35 55 55 40 40x xx x x x x x xx x x x x x xx x x x x x x

100 100 100 100 100 100 100


SampleTownship


GrainMain Texture

2nd TextureComments

CIPW NameNormatives

MineralsQuartz

PlagioclaseK-spar




LeucoxeneZircon

OpaquesAlteration



JB97-106A JB97-106C JB98-114 JB98-150 JB98-151C JB98-175 JB98-178Janes Janes Waters Lorne Lorne Curtin Curtin

8E 8E 17C 12SW 12SW 5SW 5SWG G G G G G GG G MG MG MG G G

mg fg-mg mg mg mg mg mgg-h g-h g-m g-h g-h g-h g-h

G G GN LG GN G GQ-H Q-H H-O Q-H H-O Q-H Q-H

3 5 1 1 x x40 40 40 25 24 49 49

46 53 60 502

74 75 48

1 1 1

x x x x10 x x x x x xx x x x x

x x

1 1 x x x x x

46 50 55 45 50x

x x x x x x xx x x x x x xx x x x x x x

100 100 100 100 100 100 100


SampleTownship


GrainMain Texture

2nd TextureComments

CIPW NameNormatives

MineralsQuartz

PlagioclaseK-spar




LeucoxeneZircon

OpaquesAlteration



JB98-194 JB98-195 JB98-196 JB98-198 JB98-199 JB98-200 JB98-201 JB98-202Kelly Kelly Kelly Kelly Kelly Kelly Kelly Kelly10E 10E 10E 10E 10E 10E 10E 10EG G G G G G G G

CM G G OPXG G G OPXG Gfg fg-mg mg mg mg mg mg mgd-i d-i g-i g-i g-i g-i g-i g-i

porph porph

G G G G G GN G GQ-H Q-H Q-H Q-H Q-H H-O Q-H Q-H

3 5 x 1 x x 150 47 50 45 55 45 45 44

5 5 5 5 5 547 48 45 50 39 50 50 50

x x x x x xx x x x x x xx x

x x x x x x x x

x x 5 45 30 45 10 30


100 100 100 100 100 100 100 100


SampleTownship


GrainMain Texture

2nd TextureComments

CIPW NameNormatives

MineralsQuartz

PlagioclaseK-spar




LeucoxeneZircon

OpaquesAlteration



JB98-203 JB98-205 JB98-206 JB98-209C JB98-210A JB98-228 JB98-229 JB98-230Kelly Kelly Kelly Louise Louise Curtin Curtin Curtin10E 10E 10E 13C 13C 4SW 4SW 4SWG G G G G G G G

OPXG mtG OPXG MG CM OPXG OPXG Gmg mg mg mg vfg-fg mg mg mgg-i g-i g-i EA d-i g-h g-h g-i

porph porph porph porph

G G G G G GN GN GNQ-H Q-H Q-H Q-H Q-H H-O H-O H-O

x x 20 5 x 1 x45 49 45 19 45 48 45 45

60 49 555 5 5 5 5

50 46 50 44 45

x x x xx x 2 3 x

x 1 1 x

x x 1 1 x x x

35 25 45 60 45 35x

x x x x x x x xx x x x x x xx x x x x x x

100 100 100 100 100 100 100 100


SampleTownship


GrainMain Texture

2nd TextureComments

CIPW NameNormatives

MineralsQuartz

PlagioclaseK-spar




LeucoxeneZircon

OpaquesAlteration



JB98-231 JB98-239D JB98-239E JB98-239F JB97-50 JB97-43B JB97-43DCurtin Kelly Kelly Kelly Wells Janes Janes4SW 10E 10E 10E 1W 8E 8E

G G G G GG OPXG OPXGG G G G GG MG OPXG

mg fg-mg mg mg mg-cg mg mgg-h g-i g-i g-i g-h g-h g-h

porph porph

G GN G G G G GQ-H H-O Q-H Q-H Q-H Q-H Q-H

5 1 1 x 5 6 548 49 45 50 48 31 37

45 54 522

50 54 50 40x

2 x 3

x x x xx x x x 2 3 1x x x

x

x x x x 5 3 3

45 30 35 35 50 45x


100 100 100 100 100 100 100


SampleTownship


GrainMain Texture

2nd TextureComments

CIPW NameNormatives

MineralsQuartz

PlagioclaseK-spar




LeucoxeneZircon

OpaquesAlteration



JB97-103B JB97-103D JB97-106B JB97-107 JB97-108 JB98-182 JB98-204Kelly Kelly Janes Janes Janes Curtin Kelly10E 10E 8E 8E 8E 5SW 10E

OPXG OPXG OPXG OPXG OPXG OPXG OPXGOPXG OPXG OPXG OPXG OPXG OPXG OPXG

mg mg mg fg-mg mg mg mgg-i g-i g-h g-i g-m g-h g-i

porph porph porph porph porph porphprimary minerals

GN G G G G GN GH-O Q-H Q-H Q-H Q-H H-O Q-H

x 1 5 1 2 x x50 55 38 38 40 45 45

40 40 5 435 5 5 10 17 2 5

45 39 10 10 35 10 50

1 x

x x x xx x x x x x xx x x

x

x x 1 1 1 x x

5 10 40 5 30 x


100 100 100 100 100 100 100


SampleTownship


GrainMain Texture

2nd TextureComments

CIPW NameNormatives

MineralsQuartz

PlagioclaseK-spar




LeucoxeneZircon

OpaquesAlteration



JB97-47 JB97-104 JB98-115 JB97-80A JB98-197 JB98-124 JB97-45 JB97-51Ermatinger Janes Janes Louise Kelly Kirkwood Moncrieff Wells

6NW 8E 9E 13C 10E 1W 14NW 1WLG LG LG MG mtG qtzG vtG vtGG G G MG G G G vtG

mg mg mg mg mg mg mg mgg-m g-h g-h g-h g-i g-h g-h g-i

porph

G G G G G G G LGQ-H Q-H Q-H Q-H Q-H Q-H Q-H Q-H

5 5 1 x 1 2 10 343 48 44 39 55 45 50 52

48 43 375 5

55 60 39 48 45

3 x x x x

x x x xx 3 x x x 2 x

x x x xx

x1 1 x 1 x x 1 x

35 43 50 40 25 x 37 35


100 100 100 100 100 100 100 100


SampleTownship


GrainMain Texture

2nd TextureComments

CIPW NameNormatives

MineralsQuartz

PlagioclaseK-spar




LeucoxeneZircon

OpaquesAlteration



JB97-52 JB97-59 JB97-60 JB97-64 JB97-66A JB97-98 JB97-100 JB97-105Wells Wells Wells Wells Wells Scadding Scadding Janes1W 1W 1W 1W 1W 16E 16E 8EvtG vtG vtG vtG vtG vtG vtG vtGvtG vtG vtG vtG vtG G G Gmg mg mg mg mg mg mg mgg-i g-i g-i g-i g-i g-h g-h g-h

G G G LG LG G G GQ-H Q-H Q-H Q-H Q-H Q-H Q-H Q-H

1 x x 2 10 1 10 550 50 50 50 40 44 35 30

505 5

49 45 45 48 45 55 45

x x xx

x x x x xx x x x 5 x 10 15x x x x xx x

xx x x x x x x x

30 40 40 35 30 35 40 55

x x x x x x x xx x x x x x xx x x x x x x

100 100 100 100 100 100 100 100


SampleTownship


GrainMain Texture

2nd TextureComments

CIPW NameNormatives

MineralsQuartz

PlagioclaseK-spar




LeucoxeneZircon

OpaquesAlteration



JB97-43C JB97-109 JB97-87C JB97-87D JB97-87E JB97-87F JB97-87GJanes Janes Janes Janes Janes Janes Janes

8E 8E 8E 8E 8E 8E 8EOPXG OPXG G G G G G

GN G GN GN MG G GNmg mg mg mg mg mg mgg-h g-h g-h g-i g-i g-h g-h

porph porph porph porph porphhigh epidote

G LG G G G G GQ-H Q-H Q-H Q-H Q-H Q-H Q-H

2 5 3 3 10 5 1039 25 35 33 20 35 32

46 33 54 47 42 53 345 3 2 5 5

5 10 5 10

x x x 1

x 2 x x x x3 20 3 5 11 5

x x xx

5 15 2 5 2 2 3

45 33 40 40 40 50 40x xx x x x x xx x x x x xx x x x x x

100 100 100 100 100 100 100


SampleTownship


GrainMain Texture

2nd TextureComments

CIPW NameNormatives

MineralsQuartz

PlagioclaseK-spar




LeucoxeneZircon

OpaquesAlteration



JB97-87H JB97-87I JB97-9A JB97-12 JB98-121B1 JB98-121B2 JB98-225AJanes Janes Kirkwood Kirkwood Wells Wells Curtin

8E 8E 1W 1W 1W 1W 4SWG G OPXG vtG vtG vtG GG GN OPXG vtG vtG vtG OPXG

mg mg mg mg mg mg mgg-h g-h g-h g-h qcpV qcpV g-h

porph porph porph

G G - - - - -Q-H Q-H - - - - -

5 5 x 5 25 25 x30 37 45 35 15 15 45

10 5 548 45 55 55

2 5 52 3 50 37 45

x xx

x x 3 x10 5 x 10 x x xx x x x x x

x x x

5 3 x x x x 5

45 45 40 45 45 50 5x xx x x x x x xx x x x x x xx x x x x x x

100 100 100 100 100 100 100


SampleTownship


GrainMain Texture

2nd TextureComments

CIPW NameNormatives

MineralsQuartz

PlagioclaseK-spar




LeucoxeneZircon

OpaquesAlteration



JB98-186 JB97-46 JB97-103A JB97-103C JB98-209A JB98-209B JB98-209DCurtin Moncrieff Kelly Kelly Louise Louise Louise5SW 14NW 10E 10E 13C 13C 13C

A vtG OPXG OPXG G G GA G OPXG OPXG EA EA EA

fg-mg mg mg mg mg mg mgg-i g-h g-i g-i EA EA EA

porph porphhigh sulphide msv sulphide msv sulphide

- - - - - - - - - - - - - -

30 15 x x30 40 50 5040

355 5

45 45

x x xx 10 x x

x x

x x x

x 35 35 40xx x xx x xx x x

100 100 100 100 0 0 0


SampleTownship


GrainMain Texture

2nd TextureComments

CIPW NameNormatives

MineralsQuartz

PlagioclaseK-spar




LeucoxeneZircon

OpaquesAlteration



JB98-212A JB97-72B JB98-165 JB98-117B JB98-117C JB98-190E JB98-138Louise Louise Waters Nairn Nairn Rathbun Davis

13C 13C 17C 18SW 18SW 19E -OPXG G LG G G G mtG

MG GN EA G MG EA mtGmg mg fg-mg mg-cg mg fg-mg mgEA g-h EA g-i g-h EA g-h

porphhigh sulphide high sulphide high sulphide high sulphide

- - - - - - - - - - - - - -

2 2 6 10 10 5 220 30 1 37 27 15 40

10 575 60 2 25 20

3 515 53

x 16 2 2 3x 5 1 1 2 5

x x x

3 x 75 15 15 75 x

80 60 2 32 20 5 40x x

x x x x x xx x x x x x xx x x x x x x

100 100 100 100 100 100 100


Sample DDH/Area Type FieldName Strat RockName Grain Texture %Plag %Kspar22692 RV00-22 - melagabbro LU gabbronorite mg-cg granular-idiomorphic 50 -29607 RV00-22 - melagabbro LU gabbronorite mg granular-hypidiomorphic 40 -29635 RV00-22 - melagabbro LU gabbronorite mg granular-hypidiomorphic 40 -29645 RV00-22 - leucogabbro IBZ leucogabbro mg granular-idiomorphic 70 -29654 RV00-22 - leucogabbro IBZ leucogabbro mg granular-idiomorphic 60 -29662 RV00-22 - gabbro BX gabbro mg recrystallized 47 -29670 RV00-22 - melagabbro BX gabbro mg granular-idiomorphic 55 -29676 RV00-22 - gabbro BX gabbro mg granular-idiomorphic 55 -29683 RV00-22 - gabbro BX gabbro mg recrystallized 55 -29689 RV00-22 - gabbro BX gabbro mg granular-idiomorphic 50 -29697 RV00-22 - gabbro BX gabbro fg diabasic-isogranular 35 -29702 RV00-22 - gabbro BX gabbro mg-cg granular-idiomorphic 55 -29705 RV00-22 - gabbro BX gabbro mg recrystallized 55 -29717 RV00-22 - gabbro BX gabbro mg granular-idiomorphic 55 -29723 RV00-22 - gabbro BX gabbro mg granular-hypidiomorphic 52 -29733 RV00-22 - gabbro BX melagabbro mg granular-hypidiomorphic 10 -29743 RV00-22 - gabbro BX melagabbro fg-mg extensively recrystallized 10 -29751 RV00-22 - gabbro BX gabbro fg-mg extensively recrystallized 45 -29756 RV00-22 - gabbro BZ melagabbro fg-mg extensively recrystallized 10 -29762 RV00-22 - gneiss FW schist fg extensively recrystallized - -

SZF-01 South Zone fragment melagabbro BX melagabbro fg recrystallized 20 -SZM-01 South Zone matrix gabbro BX gabbro mg granular-hypidiomorphic 50 -SZF-02 South Zone fragment melagabbro BX melagabbro mg extensively recrystallized 15 -SZM-02 South Zone matrix gabbro BX gabbro mg granular-hypidiomorphic 45 -SZF-03 South Zone fragment melagabbro BX melagabbro mg recrystallized 25 -SZM-03 South Zone matrix gabbro BX gabbro mg granular-hypidiomorphic 38 -SZF-04 South Zone fragment melagabbro BX melagabbro mg extensively recrystallized 10 -SZM-04 South Zone matrix leucogabbro BX leucogabbro mg-cg granular-hypidiomorphic 70 -SZF-05 South Zone fragment gabbro BX gabbro mg extensively recrystallized 45 -SZM-05 South Zone matrix gabbro BX gabbro mg granular-hypidiomorphic 45 -CZF-01 Central Zone fragment gabbro BX gabbro mg extensively recrystallized 35 -CZM-01 Central Zone matrix leucogabbro BX gabbro mg-cg granular-hypidiomorphic 30 -CZF-02 Central Zone fragment gabbro BX gabbro mg extensively recrystallized 35 -CZM-02 Central Zone matrix leucogabbro BX gabbro mg granular-hypidiomorphic 30 -CZF-03 Central Zone fragment gabbro BX gabbro mg extensively recrystallized 35 -CZM-03 Central Zone matrix gabbro BX gabbro mg granular-hypidiomorphic 30 -

APPENDIX 2: (B) River Valley Intrusion - Matrix/Fragment RV00-22

Sample2269229607296352964529654296622967029676296832968929697297022970529717297232973329743297512975629762

SZF-01SZM-01SZF-02SZM-02SZF-03SZM-03SZF-04SZM-04SZF-05SZM-05CZF-01CZM-01CZF-02CZM-02CZF-03CZM-03

Qtz %Ol %Pyx Cpx Opx - - 50 x nd - - 60 x nd - - 60 x nd - - 28 x nd - - 20 x nd - - 50 x nd - - 45 x1 x2 - - 40 x nd - - 45 x nd - - 50 x nd - - 47 x nd - - 40 x nd - - 45 x nd - - 38 x nd - - 40 x nd - - 82 x nd - - 45 x nd - - 45 x nd - - 68 x nd - - - - - - - 79 x nd - - 50 x nd - - 84 x nd - - 53 x nd - - 75 x nd - - 50 x nd - - 72 x nd - - 25 x nd - - 47 x nd - - 50 x nd - - 38 x nd - - 45 x nd - - 38 x nd - - 45 x nd - - 38 x nd - - 45 x nd

Major (>10%)


Sample2269229607296352964529654296622967029676296832968929697297022970529717297232973329743297512975629762


Pig Qtz Amp Ol Biot Ox Sulp Ep Ep Ap Qtz Biot Ox Sulp Zr Ttn Amp Chl Sericnd - - 2 - - - - x x x x x x - - pyx pyx/plag plagnd - - 2 - - - - x x x x x x - - pyx pyx/plag plagnd - - 5 - - - - x - x x x x - - pyx pyx/plag plagnd 2 - - - - - 10 - x - - x x - x pyx pyx/plag plagnd 10 - - - - - 10 - x - x x x - - pyx pyx/plag plagnd 1 - - - - - 2 - - - - - x - - pyx pyx/plag plagnd - - - - - - - x x x - - - - pyx pyx/plag plagnd - - - - - - 5 - - x - x x - - pyx pyx/plag plagnd - - - - - - - x - x - x x - - pyx pyx/plag plagnd - - - - - - - x - - - x x - - pyx pyx/plag plagnd 5 - - - 2 1 10 - - - - - - - - pyx pyx/plag plagnd - - - - - - 5 - - x - x x - - pyx pyx/plag plagnd - - - - - - - x - - - x x - - pyx pyx plagnd - - - - - 2 5 - - x x - - - - pyx pyx/plag plagnd - - - - - 3 5 - - x x - - - - pyx pyx/plag plagnd 1 - - 5 - 2 - x - - - x - - - pyx pyx/plag plagnd 5 - - 15 - 5 20 - - - - x - - - pyx pyx/plag plagnd 3 - - 5 - 2 10 - - - - x - - - pyx pyx/plag plagnd 1 - - 10 - 1 10 - - - - - - - x pyx pyx/plag plag - - - - - - - - - - - - - - - - pyx pyx/plag plagnd - - - - - 1 - x - x - - - - - pyx pyx/plag plagnd - - - - - - - x - x - - x - x pyx pyx/plag plagnd - - - - - 1 - x - x - x x - - pyx pyx/plag plagnd - - - - - 1 1 - - x x - - - x pyx pyx/plag plagnd - - - - - - - x - x - - x - x pyx pyx/plag plagnd - - - - - 2 10 - x x - - - - - pyx pyx/plag plagnd 5 - - 10 - 3 5 - x - - - - x - pyx pyx/plag plagnd - - - - - 2 3 - - x x - - - - pyx pyx/plag plagnd 3 - - - - 2 3 - x - - - - - x pyx pyx/plag plagnd - - - - - - 5 - x x - - x - x pyx pyx/plag plagnd 5 - - 10 - 2 10 - x - - - - - x pyx pyx/plag plagnd 1 - - 10 2 2 10 - x - - - - - - pyx pyx/plag plagnd 5 - - 10 - 2 10 - x - - - - - x pyx pyx/plag plagnd 1 - - 10 2 2 10 - x - - - - - - pyx pyx/plag plagnd 5 - - 10 - 2 10 - x - - - - - x pyx pyx/plag plagnd 1 - - 5 1 1 5 - x - - - - - - pyx pyx/plag plag

SecondaryAccessory (<1%)Minor (<10%)


Sample2269229607296352964529654296622967029676296832968929697297022970529717297232973329743297512975629762


Sauss Alteration Featuresplag plag-->actin/hbld; pyx-->actinplag plag-->actin/hbld; pyx-->actinplag plag-->actin/hbld; pyx-->actinplag plag-->sauss; pyx-->actinplag plag-->sauss/hbld; pyx-->actin/hbld; plag-->fspar+qtzplag plag-->sauss/hbld; pyx-->actin/hbldplag plag-->sauss/hbld; pyx-->actin/hbld; plag-->albite+qtzplag plag-->sauss/hbld; pyx-->actin/hbld; plag-->albite+qtzplag plag-->sauss/hbld; pyx-->actin/hbldplag plag-->sauss/hbld; pyx-->actin/hbldplag plag-->sauss/hbld; pyx-->actin/hbldplag plag-->sauss/hbld; pyx-->actin/hbld; plag-->albite+qtzplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld/exsolution; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag extensively recrystallized - probably orthogneissplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbldplag plag-->sauss/actin/hbld; pyx-->actin/hbld


Sample2269229607296352964529654296622967029676296832968929697297022970529717297232973329743297512975629762


General Features Commentsrelict igneous textures altered olivines completely gone to tremolite?relict igneous textures altered olivines completely gone to tremolite?relict igneous textures altered olivines completely gone to tremolite?relict igneous textures much more epidote than in previous samplesrelict igneous textures much more epidote than in previous samplesrelict igneous textures shear zone cuts samplerelict igneous textures zones of amphibole as relict phenocrystsrelict igneous texturesrelict igneous textures cut by albite-qtz veinrelict igneous textures

granular-idiomorphic to diabase-isogranularrelict igneous textures

relict igneous textures; extensive alteration STRONGLY ALTEREDrelict igneous textures

exsolution textures of fspar-qtz in plag replacement or exsolution of plagstrongly altered and recrystallized increase in biotite - introduction of K

biotite-epidote coincident w elevated sulphide foliated mafic; anorthositic fragment in mafic hostbiotite-epidote coincident w elevated sulphide foliated; kink bands/strain zones; microshearsbiotite-epidote coincident w elevated sulphide very fg titanite; abundant primary(?) epidote

weakly foliated; rich in epidote/biotite actin-hbld-biot-ep-titan-po matrtixextensively altered

extensively altered relict igneous texturespyx extensively alterered moderately altered

plag altered to qtz-albite intergrowth altered plag-pyx; relict igneous texturespyx strongly altered relative to plag relict igneous textures

qtz-biot patches with sulphides relict igneous textureschlorite-epidote-sulphide patches relict igneous textures

edpidote with sulphide poor relict igneous texturespyx strongly altered relative to plag relict igneous textures

edpidote, chlorite, qtz and titanite with sulphide poor relict igneous texturessulphide with biotite, epidote and muscovite plag altered to qtz-albite intergrowth

poor relict igneous texturessulphide with biotite, epidote and muscovite plag altered to qtz-albite intergrowthedpidote, chlorite, qtz, biotite with sulphide poor relict igneous textures

sulphide with biotite, epidote, qtz poor relict igneous textures


558

APPENDIX 3:

DIAMOND DRILL HOLE DATA LISTING AND DRILL CORE LOGS A) JR99-01, JR99-06 (Rastall property, Chiniguchi River intrusion) 559 B) A197 (Rauhala property, Makada Lake intrusion) 564 C) RV00-22 (Dana North Deposit, River Valley intrusion) 565

JR99-01Sample From To Interval Pd Au Pt Cu Ni

(m) (m) (m) (ppb) (ppb) (ppb) (ppm) (ppm)

1 2.50 2.95 0.45 41 0 0 63 432 2.95 3.57 0.62 94 9 15 211 773 3.57 4.11 0.54 1063 82 207 1596 12604 4.11 4.68 0.57 54 0 0 131 765 4.68 5.00 0.32 330 28 66 552 2936 5.00 5.54 0.54 381 32 74 652 3407 5.54 6.16 0.62 78 6 23 106 608 6.16 6.69 0.53 167 15 29 283 1549 6.69 7.00 0.31 46 0 0 109 65

10 7.00 7.53 0.53 23 0 0 62 41chk 10 7.00 7.53 0.53 28 0 0avg 10 7.00 7.53 0.53 25.5 0 0

11 7.53 8.00 0.47 11 0 0 53 4612 8.00 8.77 0.77 21 0 0 78 5213 8.77 9.41 0.64 45 6 15 83 5914 9.41 10.41 1.00 153 12 30 193 10415 10.41 10.89 0.48 218 14 42 239 13416 10.89 11.47 0.58 53 7 17 101 5917 11.47 12.21 0.74 31 0 0 73 5118 12.21 12.68 0.47 309 18 55 318 16419 12.68 13.33 0.65 149 31 40 835 319

chk 19 12.68 13.33 0.65 140 30 36avg 19 12.68 13.33 0.65 144.5 30.5 38

20 13.33 14.00 0.67 108 48 43 997 41021 14.00 14.45 0.45 105 49 60 1635 65422 14.45 15.11 0.66 74 37 41 1297 49923 15.11 15.61 0.50 100 53 37 1474 64624 15.61 16.21 0.60 125 52 34 1632 63925 16.21 16.56 0.35 137 32 37 874 358

chk 25 16.21 16.56 0.35 123 25 30avg 25 16.21 16.56 0.35 130 28.5 33.5

26 16.56 17.00 0.44 136 74 56 2191 84427 17.00 17.43 0.43 183 105 82 3390 131828 17.43 17.95 0.52 148 105 60 2991 120629 17.95 18.45 0.50 233 178 104 4938 209730 18.45 18.88 0.43 199 125 93 3593 152031 18.88 19.33 0.45 196 115 54 3407 109632 19.33 19.68 0.35 95 55 41 1863 69733 19.68 20.00 0.32 140 91 57 2948 119334 20.00 20.50 0.50 149 104 52 3503 150735 20.50 21.25 0.75 82 54 61 1759 78236 21.39 21.99 0.60 258 222 126 5766 271737 21.99 22.50 0.51 292 234 133 6235 2615

chk 37 21.99 22.50 0.51 269 197 115 6774 2683avg 37 21.99 22.50 0.51 280.5 215.5 124

38 22.50 23.00 0.50 277 213 125 6774 2683

APPENDIX 3: (A) Drill Hole Composite - Chiniguchi River Intrusion


(m) (m) (m) (ppb) (ppb) (ppb) (ppm) (ppm)39 23.00 23.69 0.69 267 192 107 5596 228740 23.69 24.46 0.77 237 190 113 5657 247541 24.46 25.07 0.61 243 178 106 4578 194842 25.07 25.72 0.65 243 163 103 4632 214743 25.72 26.51 0.79 287 218 132 5861 239344 26.51 27.20 0.69 252 264 115 5664 216945 27.20 27.91 0.71 267 162 116 4481 207046 27.91 28.47 0.56 95 42 23 4733 184547 28.47 29.28 0.81 199 96 63 6198 203348 29.28 30.15 0.87 190 76 53 4489 162549 30.15 30.89 0.74 233 95 63 4476 188050 30.89 31.50 0.61 147 74 36 2896 107751 31.50 32.00 0.50 201 77 56 4070 162052 32.00 32.75 0.75 626 267 181 7344 318253 32.75 33.44 0.69 645 279 198 6382 266554 33.44 34.44 1.00 682 218 180 5112 211055 34.44 35.00 0.56 905 220 206 5511 2245

chk 55 34.44 35.00 0.56 731 153 136avg 55 34.44 35.00 0.56 818 186.5 171

56 35.00 35.75 0.75 1082 270 227 7255 345057 35.75 36.42 0.67 1205 245 224 5756 257858 36.42 37.30 0.88 1660 369 311 11973 336559 37.30 38.00 0.70 1797 445 378 11329 464360 38.00 38.74 0.74 1944 387 364 11979 549361 38.74 39.49 0.75 1862 315 344 9825 321562 39.49 40.13 0.64 1834 207 325 7705 311163 40.13 40.73 0.60 3527 272 486 10491 5214

chk 63 40.13 40.73 0.60 3928 309 516avg 63 40.13 40.73 0.60 3727.5 290.5 501

64 40.73 41.00 0.27 5830 329 571 4232 3493chk 64 40.73 41.00 0.27 5697 267 627avg 64 40.73 41.00 0.27 5763.5 298 599

65 41.00 41.62 0.62 5394 293 589 13885 4312chk 65 41.00 41.62 0.62 5132 368 491avg 65 41.00 41.62 0.62 5263 330.5 540

66 41.62 41.87 0.25 2083 30 274 101016 171767 41.87 42.09 0.22 4513 35 510 7051 2406

chk 67 41.87 42.09 0.22 4551 27 459avg 67 41.87 42.09 0.22 4532 31 484.5

68 42.09 42.57 0.48 2501 81 347 19088 206469 42.57 43.24 0.67 2762 200 387 8380 229470 43.24 43.59 0.35 3484 26 565 2261 2337

chk 70 43.24 43.59 0.35 2628 20 427avg 70 43.24 43.59 0.35 3056 23 496

71 43.59 43.85 0.26 1733 21 241 988 120672 43.85 44.77 0.92 1890 23 280 759 892

chk 72 43.85 44.77 0.92 2260 15 282



(m) (m) (m) (ppb) (ppb) (ppb) (ppm) (ppm)avg 72 43.85 44.77 0.92 2075 19 281

73 44.77 45.25 0.48 276 0 52 163 53774 45.25 46.35 1.10 1792 18 251 110 147875 46.35 47.11 0.76 3709 181 462 5221 3168

chk 75 46.35 47.11 0.76 3456 133 420avg 75 46.35 47.11 0.76 3582.5 157 441

76 47.11 47.87 0.76 1996 157 274 3611 146677 47.87 48.72 0.85 2701 191 342 5624 220678 48.72 49.76 1.04 3299 207 417 6235 2633

chk 78 48.72 49.76 1.04 3112 199 410avg 78 48.72 49.76 1.04 3205.5 203 413.5

79 49.76 50.05 0.29 2151 165 326 4100 174380 50.05 51.08 1.03 62 12 21 170 9381 51.08 52.03 0.95 0 7 0 126 64

chk 81 51.08 52.03 0.95 22 5 0avg 81 51.08 52.03 0.95 11 6 0

82 52.03 53.19 1.16 22 5 0 115 7483 53.19 54.48 1.29 18 0 16 118 7784 54.48 55.75 1.27 13 0 0 86 6585 55.75 56.70 0.95 11 0 0 116 7786 56.70 57.67 0.97 16 0 0 123 7687 57.67 58.79 1.12 14 0 0 125 8588 58.79 59.95 1.16 13 0 0 105 7189 59.95 60.96 1.01 12 0 0 103 7490 60.96 62.10 1.14 12 0 0 102 70

chk 90 60.96 62.10 1.14 12 0 0avg 90 60.96 62.10 1.14 12 0 0

91 62.10 62.69 0.59 13 0 0 136 7092 62.69 62.93 0.24 0 9 0 240 7993 62.93 64.01 1.08 23 0 15 103 7494 64.01 65.06 1.05 54 7 16 148 7695 65.06 66.35 1.29 244 15 28 415 14596 66.35 67.23 0.88 181 5 0 119 10197 67.23 68.08 0.85 14 0 0 90 65



(m) (m) (m) (ppb) (ppb) (ppb) (ppm) (ppm)

1 9.90 10.15 0.25 762 261 248 10438 37142 10.15 10.45 0.30 823 274 256 8793 46423 10.45 10.75 0.30 904 346 192 11179 50174 10.75 11.00 0.25 1046 309 292 11543 48055 11.00 11.32 0.32 683 210 228 11718 47196 11.32 11.72 0.40 1030 224 268 12323 52707 11.72 12.06 0.34 1226 231 303 14019 41538 12.06 12.54 0.48 1430 288 286 7334 31729 12.54 12.75 0.21 1706 358 330 11788 3640

10 12.75 13.22 0.47 2064 424 336 10898 3426chk 10 12.75 13.22 0.47 1906 319 347avg 10 12.75 13.22 0.47 1985 372 342

11 13.22 13.70 0.48 1953 322 359 7463 303012 13.70 14.00 0.30 1974 317 341 7447 286313 14.00 14.45 0.45 2145 354 359 7533 291814 14.45 14.83 0.38 2163 355 358 8115 311715 14.83 15.27 0.44 2155 341 324 8280 299516 15.27 15.64 0.37 1926 279 0 7043 278317 15.64 15.98 0.34 1904 268 311 6769 251018 15.98 16.38 0.40 2177 331 358 7990 313619 16.38 16.88 0.50 2301 315 375 8359 3506

chk 19 16.38 16.88 0.50 2145 269 344avg 19 16.38 16.88 0.50 2223 292 360

20 16.88 17.41 0.53 2322 557 331 7975 338421 17.41 17.84 0.43 1643 256 288 8118 277422 17.84 18.27 0.43 2012 316 331 7851 291423 18.27 18.67 0.40 2056 314 339 6413 243524 18.67 19.13 0.46 1973 276 317 8127 306225 19.13 19.50 0.37 2159 262 317 7306 271226 19.50 19.76 0.26 2566 236 355 7789 338727 19.76 20.09 0.33 3738 370 493 8763 438228 20.09 20.45 0.36 3522 333 455 8604 471929 20.45 20.86 0.41 2813 259 392 8758 518330 20.86 21.33 0.47 3702 360 508 9147 453931 21.33 21.87 0.54 4557 427 600 10182 482732 21.87 22.16 0.29 3452 255 494 6644 437833 22.16 22.41 0.25 2170 173 332 5410 296434 22.41 22.64 0.23 2350 167 326 6090 292735 22.64 23.09 0.45 2346 198 356 6195 291436 23.09 23.52 0.43 2273 170 324 6113 2668

chk 36 23.09 23.52 0.43 2446 165 320avg 36 23.09 23.52 0.43 2360 168 322

37 23.52 23.91 0.39 1082 80 151 2633 120238 23.91 24.25 0.34 76 0 0 226 10639 24.25 24.75 0.50 46 0 0 154 10740 24.75 25.14 0.39 17 0 0 115 94



(m) (m) (m) (ppb) (ppb) (ppb) (ppm) (ppm)41 25.14 25.50 0.36 15 0 0 120 8042 25.50 25.68 0.18 15 0 0 42 10143 25.68 25.89 0.21 0 0 0 70 7244 25.89 26.58 0.69 15 0 0 35 9445 26.58 27.13 0.55 0 0 0 110 80

chk 45 26.58 27.13 0.55 11 0 0avg 45 26.58 27.13 0.55 6 0 0

46 27.13 27.74 0.61 11 0 0 89 8047 27.74 28.08 0.34 11 0 0 100 8448 28.08 28.49 0.41 12 0 0 84 6049 28.49 29.00 0.51 38 6 0 76 6850 29.00 29.48 0.48 23 0 0 75 6451 29.48 30.46 0.98 18 0 0 77 6852 30.46 31.42 0.96 20 0 0 79 6353 31.42 32.00 0.58 30 0 17 83 6654 32.00 32.96 0.96 36 0 19 89 6755 32.96 33.87 0.91 22 0 0 76 59

chk 55 32.96 33.87 0.91 15 0 0avg 55 32.96 33.87 0.91 19 0 0

56 33.87 34.25 0.38 15 0 0 22 8057 34.25 34.56 0.31 0 0 0 17 10058 34.56 35.48 0.92 0 0 0 48 9559 35.48 36.36 0.88 0 0 0 69 7960 36.36 37.50 1.14 16 0 0 108 8061 37.50 38.50 1.00 18 0 0 92 72

chk 61 37.50 38.50 1.00 10 0 0avg 61 37.50 38.50 1.00 14 0 0

62 38.50 39.50 1.00 13 0 0 93 7363 39.50 40.50 1.00 16 0 0 92 7364 40.50 41.32 0.82 12 0 0 77 6665 41.32 42.45 1.13 0 0 0 65 8866 42.45 43.14 0.69 0 0 0 115 7367 43.45 44.38 0.93 0 0 0 74 8568 44.38 45.74 1.36 0 0 0 18 9169 46.30 47.00 0.70 0 0 0 11 58


DDH A1-97: J. Rauhala, Waters TownshipTtl Length: 54.25m (178 ft.) - original invoice indicates 178ft hole (May 20-1997)Dip: -45az: 360casing: 2.1m (7 ft.)notes: end of hole is at depth of ~40m (131.4 ft.) verticalnotes: casing still in place; intervals indicate starting point of sampling only

Sample Interval (ft) Interval (m) Description1 7.3 2.23 gabbro2 14 4.27 gabbro3 20 6.10 gabbro4 24 7.32 gabbro5 28 8.53 gabbro6 33 10.06 gabbro7 38 11.58 gabbro8 43 13.11 gabbro9 48 14.63 gabbro

10 54 16.46 gabbro11 58 17.68 gabbro12 63 19.20 gabbro13 67 20.42 gabbro14 71 21.64 gabbro15 78 23.77 gabbro16 83 25.30 gabbro17 85.6 26.09 gabbro18 90 27.43 gabbro19 95 28.96 gabbro20 101 30.78 gabbro21 105.5 32.16 gabbro22 110.5 33.68 gabbro23 115 35.05 gabbro24 119 36.27 gabbro

25a,b,c 122 37.19 start of alteration zone26a 125.7 38.31 alteration zone26b 127 38.71 alteration zone27a 127.8 38.95 alteration zone27b 130 39.62 alteration zone27c 132.5 40.39 alteration zone28 134 40.84 alteration zone29 138 42.06 alteration zone30 143 43.59 blue quartz eyes with ~10% sulphide (max.)31 148.25 45.19 blue quartz eyes with ~10% sulphide (max.)32 153 46.63 blue quartz eyes with ~10% sulphide (max.)33 158 48.16 blue quartz eyes with ~10% sulphide (max.)34 161 49.07 blue quartz eyes with ~10% sulphide (max.)35 168 51.21 biotite alteration with 5-15% diss. sulphide36 171 52.12 biotite alteration with 5-15% diss. sulphide37 177 53.95 biotite alteration with 5-15% diss. sulphide38 178 54.25 biotite alteration with 5-15% diss. sulphide39 179 54.56 biotite alteration with 5-15% diss. sulphide40 180 54.86 biotite alteration with 5-15% diss. sulphide41 180.5 55.02 fg-mg gabbro42 182 55.47 fg-mg gabbro43 183.5 55.93 fg-mg gabbro

APPENDIX 3: (B) Drill Hole A1-97 Makada Lake Intrusion

From

ToR

ock

Type

%V

SFr

omTo

Inte

rval

Au

PtPd

Rh

Ni

Cu

Pd:P

tC

u:N

i(m

)(m

)(U

nit)

(max

)(m

)(m

)(m

)(p

pb)

(ppb

)(p

pb)

(ppb

)(p

pm)

(ppm

)0.

0054

.90

mel

agab

bro

nil

0.00

1.00

1.00

839

2791

870.

71.

0ni

l1.

002.

501.

5014

3327

102

770.

80.

8LA

YER

ED U

NIT

nil

2.50

4.00

1.50

741

2911

611

70.

71.

0ni

l4.

005.

501.

508

4829

112

112

0.6

1.0

(0.0

0 to

89.

5m)

nil

5.50

7.00

1.50

1642

3110

210

30.

71.

0ni

l7.

008.

501.

507

2523

108

960.

90.

9ni

l8.

5010

.00

1.50

953

2610

511

00.

51.

0SU

MM

AR

Yni

l10

.00

12.0

02.

005

1410

105

960.

70.

9LU

: 226

90 to

296

42ni

l12

.00

14.0

02.

006

2719

9085

0.7

0.9

IBZ:

296

43 to

296

83ni

l14

.00

16.0

02.

0010

2922

8810

00.

81.

1B

X: 2

9684

to 2

9753

nil

16.0

018

.00

2.00

737

2310

110

70.

61.

1B

Z: 2

9754

to 2

9759

nil

18.0

020

.00

2.00

830

2279

780.

71.

0FB

X: 2

9760

to 2

9764

nil

20.0

022

.00

2.00

932

1789

970.

51.

1FW

: RV

00-0

1 to

03

nil

22.0

024

.00

2.00

720

1779

940.

91.

2ni

l24

.00

26.0

02.

005

1012

7898

1.2

1.3

nil

26.0

028

.00

2.00

945

2979

830.

61.

1ni

l28

.00

30.0

02.

0010

3633

7610

20.

91.

3ni

l30

.00

32.0

02.

007

3629

8793

0.8

1.1

nil

32.0

034

.00

2.00

731

2310

593

0.7

0.9

nil

34.0

036

.00

2.00

929

3190

961.

11.

1ni

l36

.00

38.0

02.

007

2218

8911

60.

81.

3ni

l38

.00

40.0

02.

007

2319

7795

0.8

1.2

nil

40.0

042

.00

2.00

325

1176

650.

40.

9ni

l42

.00

44.0

02.

005

2413

8111

60.

51.

4ni

l44

.00

46.0

02.

005

2414

7551

0.6

0.7

nil

46.0

048

.00

2.00

616

1272

820.

81.

1ni

l48

.00

49.3

51.

351

228

7647

0.4

0.6

nil

49.3

550

.85

1.50

30

023

220.

9

Hol

e N

o.:

RV

00-2

2C

olla

r Bea

ring:

86C

olla

r Dip

:

-45

Cas

ing:

1m

NW

D

epth

: 25

9.0m

Grid

Nor

th:

450

[517

2419

.22m

N]

Grid

Eas

t: -3

40[5

5514

6.44

mE]

Elev

atio

n: +

325.

24m

MSL

APP

END

IX 3

: (C

) Dril

l Hol

e R

V00

-22

Riv

er V

alle

y In

trusi

on

From

ToR

ock

Type

%V

SFr

omTo

Inte

rval

Au

PtPd

Rh

Ni

Cu

Pd:P

tC

u:N

i(m

)(m

)(U

nit)

(max

)(m

)(m

)(m

)(p

pb)

(ppb

)(p

pb)

(ppb

)(p

pm)

(ppm

)ni

l50

.85

52.0

01.

154

1811

7898

0.6

1.3

nil

52.0

054

.00

2.00

328

1690

101

0.6

1.1

54.9

055

.00

faul

t zon

eni

l54

.00

56.0

02.

003

2011

9191

0.6

1.0

nil

56.0

058

.00

2.00

328

1310

388

0.5

0.9

nil

58.0

060

.00

2.00

30

894

921.

055

.00

89.5

0m

elag

abbr

oni

l60

.00

61.7

51.

7513

5627

138

210.

50.

2ni

l61

.75

62.6

00.

8512

3314

2437

0.4

1.5

LAY

ERED

UN

ITni

l62

.60

64.0

01.

4010

3617

109

670.

50.

6ni

l64

.00

66.1

02.

1010

4024

113

850.

60.

8(0

.00

to 8

9.5m

)ni

l66

.10

67.4

01.

309

4927

172

780.

60.

5tr

67.4

068

.85

1.45

1244

3890

143

0.9

1.6

nil

68.8

570

.20

1.35

1331

3011

310

81.

01.

0ni

l70

.20

72.2

02.

0010

4929

9611

90.

61.

2ni

l72

.20

74.0

01.

8010

3823

107

132

0.6

1.2

nil

74.0

075

.18

1.18

841

1612

056

0.4

0.5

5 C

p75

.18

75.3

00.

1210

5917

279

9590

0.3

34.4

tr75

.30

77.0

01.

7010

2726

112

118

1.0

1.1

nil

77.0

079

.00

2.00

1233

1515

813

40.

50.

8ni

l79

.00

81.0

02.

009

1912

179

830.

60.

52

81.0

081

.40

0.40

1123

1021

216

40.

40.

8tr

81.4

082

.80

1.40

715

1013

699

0.7

0.7

tr82

.80

85.0

02.

2010

3120

9010

80.

61.

2tr

85.0

086

.50

1.50

1144

3310

414

50.

81.

4tr

86.5

088

.00

1.50

1131

2215

511

80.

70.

8tr

88.0

089

.50

1.50

833

2293

113

0.7

1.2

89.5

012

2.30

pegm

atiti

ctr

89.5

091

.00

1.50

924

2057

330.

80.

6le

ucog

abbr

o w

tr

91.0

092

.50

1.50

726

1763

850.

71.

315

% g

abbr

otr

92.5

094

.00

1.50

1220

858

144

412.

80.

9

Grid

Nor

th:

450

[517

2419

.22m

N]

Grid

Eas

t: -3

40[5

5514

6.44

mE]

Col

lar D

ip:

-4

5C

asin

g:

1m N

W

Hol

e N

o.:

RV

00-2

2C

olla

r Bea

ring:

86D

epth

: 25

9.0m

Elev

atio

n: +

325.

24m

MSL

APP

END

IX 3

: (C

) Dril

l Hol

e R

V00

-22

Riv

er V

alle

y In

trusi

on

From

ToR

ock

Type

%V

SFr

omTo

Inte

rval

Au

PtPd

Rh

Ni

Cu

Pd:P

tC

u:N

i(m

)(m

)(U

nit)

(max

)(m

)(m

)(m

)(p

pb)

(ppb

)(p

pb)

(ppb

)(p

pm)

(ppm

)IN

CLU

SIO

N -B

EAR

ING

tr94

.00

95.5

01.

506

3021

4144

0.7

1.1

UN

ITtr

95.5

097

.00

1.50

423

1230

970.

53.

2(8

9.5

to 1

60.8

m)

tr97

.00

98.5

01.

504

2414

8546

0.6

0.5

tr98

.50

100.

001.

505

2518

7746

0.7

0.6

89.5

012

2.30

pegm

atiti

ctr

100.

0010

2.00

2.00

515

1565

551.

00.

8(c

ont.)

leuc

ogab

bro

w

tr10

2.00

104.

002.

0012

2817

7812

50.

61.

615

% g

abbr

otr

104.

0010

6.00

2.00

634

1349

540.

41.

1(c

ont.)

tr10

6.00

108.

002.

0011

2413

5087

0.5

1.7

tr10

8.00

110.

002.

005

3313

2748

0.4

1.8

tr11

0.00

112.

002.

006

2411

6340

0.5

0.6

INC

LUSI

ON

-BEA

RIN

Gtr

112.

0011

4.00

2.00

534

1130

550.

31.

8U

NIT

tr11

4.00

116.

002.

003

3119

3147

0.6

1.5

(89.

5 to

160

.8m

)tr

116.

0011

8.00

2.00

630

1830

610.

62.

0tr

118.

0012

0.00

2.00

432

1734

340.

51.

0tr

120.

0012

2.30

2.30

332

2041

340.

60.

8in

crea

sed

PGE

tr12

2.30

124.

001.

709

129

222

6159

1.7

1.0

122.

3013

4.00

gabb

rotr

124.

0012

6.00

2.00

487

8640

361.

00.

9tr

126.

0012

8.00

2.00

972

5928

145

0.8

5.2

INC

LUSI

ON

-BEA

RIN

Gtr

128.

0013

0.00

2.00

984

6332

970.

83.

0U

NIT

tr13

0.00

132.

002.

009

6856

2912

10.

84.

2(8

9.5

to 1

60.8

m)

tr13

2.00

134.

002.

0014

5849

3410

90.

83.

213

4.00

136.

55le

ucog

abbr

oni

l13

4.00

135.

501.

507

8390

1841

1.1

2.3

nil

135.

5013

6.55

1.05

838

6423

551.

72.

413

6.55

148.

00ga

bbro

to m

ela-

tr13

6.55

138.

001.

453

5362

6334

1.2

0.5

gabb

rotr

138.

0014

0.00

2.00

719

819

281

141.

00.

2tr

140.

0014

2.00

2.00

617

025

760

301.

50.

5IN

CLU

SIO

N -B

EAR

ING

tr14

2.00

144.

002.

002

4565

8723

1.4

0.3

UN

ITtr

144.

0014

6.00

2.00

611

013

169

271.

20.

4

Hol

e N

o.:

RV

00-2

2C

olla

r Bea

ring:

86G

rid N

orth

: 45

0 [5

1724

19.2

2mN

]G

rid E

ast:

-340

[555

146.

44m

E]C

olla

r Dip

:

-45

Cas

ing:

1m

NW

D

epth

: 25

9.0m

Elev

atio

n: +

325.

24m

MSL

APP

END

IX 3

: (C

) Dril

l Hol

e R

V00

-22

Riv

er V

alle

y In

trusi

on

From

ToR

ock

Type

%V

SFr

omTo

Inte

rval

Au

PtPd

Rh

Ni

Cu

Pd:P

tC

u:N

i(m

)(m

)(U

nit)

(max

)(m

)(m

)(m

)(p

pb)

(ppb

)(p

pb)

(ppb

)(p

pm)

(ppm

)tr

146.

0014

8.00

2.00

510

112

110

911

1.2

0.1

148.

0015

2.90

gabb

rotr

148.

0015

0.00

2.00

1670

6627

740.

92.

7IN

CLU

SIO

N -B

EAR

ING

tr15

0.00

152.

002.

0014

134

130

2796

1.0

3.6

UN

ITtr

152.

0015

2.90

0.90

1011

810

530

530.

91.

8(8

9.5

to 1

60.8

m)

152.

9015

4.00

gran

ite d

yke

tr15

2.90

154.

001.

109

3217

1582

0.5

5.5

tr15

4.00

155.

501.

5038

125

109

3257

0.9

1.8

tr15

5.50

157.

001.

507

8962

3242

0.7

1.3

154.

0016

0.80

gabb

rotr

157.

0015

8.50

1.50

2728

752

026

116

1.8

4.5

tr15

8.50

160.

001.

5012

153

202

2549

1.3

2.0

tr16

0.00

160.

800.

8034

206

331

1949

1.6

2.6

160.

8022

9.70

gabb

ro b

recc

ia0.

516

0.80

161.

801.

0026

7610

848

305

1.4

6.4

<0.5

161.

8016

2.50

0.70

5230

460

062

335

2.0

5.4

BR

ECC

IA U

NIT

<116

2.50

163.

000.

5030

124

144

7341

41.

25.

7tr

163.

0016

5.00

2.00

3715

627

328

621.

82.

2(1

60.8

to 2

25.7

m)

tr16

5.00

166.

651.

6528

8013

914

136

81.

72.

6<0

.516

6.65

167.

500.

8519

7420

468

262

2.8

3.9

tr16

7.50

168.

501.

0023

9312

255

243

1.3

4.4

<0.5

168.

5017

0.15

1.65

768

9444

283

1.4

6.4

<0.5

170.

1517

1.15

1.00

3614

128

934

274

2.0

8.1

<0.5

171.

1517

2.00

0.85

2794

225

4720

32.

44.

3<0

.517

2.00

173.

001.

0013

5387

5857

1.6

1.0

<0.5

173.

0017

3.50

0.50

4516

639

112

355

32.

44.

5<0

.517

3.50

175.

001.

5011

955

311

7340

156

1220

2.1

7.8

<117

5.00

176.

251.

2576

359

818

2213

273

52.

35.

6<0

.517

6.25

177.

751.

5057

162

269

1012

378

31.

76.

4tr

177.

7517

9.40

1.65

5214

322

40

145

719

1.6

5.0

<0.5

179.

4017

9.90

0.50

138

672

1750

4327

616

902.

66.

1

Grid

Nor

th:

450

[517

2419

.22m

N]

Grid

Eas

t: -3

40[5

5514

6.44

mE]

Col

lar D

ip:

-4

5C

asin

g:

1m N

W

Hol

e N

o.:

RV

00-2

2C

olla

r Bea

ring:

86D

epth

: 25

9.0m

Elev

atio

n: +

325.

24m

MSL

APP

END

IX 3

: (C

) Dril

l Hol

e R

V00

-22

Riv

er V

alle

y In

trusi

on

From

ToR

ock

Type

%V

SFr

omTo

Inte

rval

Au

PtPd

Rh

Ni

Cu

Pd:P

tC

u:N

i(m

)(m

)(U

nit)

(max

)(m

)(m

)(m

)(p

pb)

(ppb

)(p

pb)

(ppb

)(p

pm)

(ppm

)1-

217

9.90

181.

001.

1024

716

1348

3410

749

123

103.

04.

716

0.80

229.

70ga

bbro

bre

ccia

2-3

181.

0018

1.85

0.85

443

2310

6600

178

532

3600

2.9

6.8

(con

t.)(c

ont.)

3-4

181.

8518

2.90

1.05

345

1510

4915

117

330

2770

3.3

8.4

<0.5

182.

9018

4.40

1.50

1770

666

2514

90.

96.

0B

REC

CIA

UN

IT2

184.

4018

4.60

0.20

323

576

1958

1619

522

903.

411

.7tr

184.

6018

5.05

0.45

6639

611

3123

107

607

2.9

5.7

(160

.8 to

225

.7m

)2

185.

0518

5.65

0.60

151

1639

3400

7210

862

12.

15.

8<1

185.

6518

6.40

0.75

9855

213

8740

161

1080

2.5

6.7

<0.5

186.

4018

7.00

0.60

5025

667

414

7838

82.

65.

01-

218

7.00

187.

450.

4513

070

921

7353

230

1460

3.1

6.3

<118

7.45

188.

300.

8510

542

211

3331

166

1300

2.7

7.8

<0.5

188.

3019

0.00

1.70

2517

240

010

109

162

2.3

1.5

219

0.00

190.

500.

5018

489

530

0171

260

1890

3.4

7.3

<0.5

190.

5019

1.30

0.80

4020

651

615

116

395

2.5

3.4

119

1.30

191.

650.

3514

312

1231

6099

435

1650

2.6

3.8

<0.5

191.

6519

3.00

1.35

2613

833

07

9528

52.

43.

0<0

.519

3.00

193.

700.

7075

436

1112

3217

282

52.

64.

81-

1.5

193.

7019

4.50

0.80

128

653

1583

4439

418

502.

44.

7<1

194.

5019

6.00

1.50

9442

911

7831

196

1140

2.7

5.8

219

6.00

197.

151.

1515

282

627

1957

372

2180

3.3

5.9

0.5

197.

1519

8.55

1.40

7132

893

722

383

2240

2.9

5.8

tr19

8.55

199.

300.

7513

5090

023

151

1.8

6.6

0.5

199.

3020

0.00

0.70

4760

122

0399

247

805

3.7

3.3

120

0.00

201.

001.

0012

949

416

4846

285

1700

3.3

6.0

<120

1.00

202.

001.

0016

095

936

0380

356

2090

3.8

5.9

<120

2.00

202.

800.

8026

610

4439

7697

442

3550

3.8

8.0

3-5

202.

8020

3.05

0.25

315

2001

9140

159

696

4940

4.6

7.1

320

3.05

203.

550.

5030

787

932

5172

386

3400

3.7

8.8

Hol

e N

o.:

RV

00-2

2C

olla

r Bea

ring:

86G

rid N

orth

: 45

0 [5

1724

19.2

2mN

]G

rid E

ast:

-340

[555

146.

44m

E]C

olla

r Dip

:

-45

Cas

ing:

1m

NW

D

epth

: 25

9.0m

Elev

atio

n: +

325.

24m

MSL

APP

END

IX 3

: (C

) Dril

l Hol

e R

V00

-22

Riv

er V

alle

y In

trusi

on

From

ToR

ock

Type

%V

SFr

omTo

Inte

rval

Au

PtPd

Rh

Ni

Cu

Pd:P

tC

u:N

i(m

)(m

)(U

nit)

(max

)(m

)(m

)(m

)(p

pb)

(ppb

)(p

pb)

(ppb

)(p

pm)

(ppm

)<0

.520

3.55

204.

100.

5550

195

627

2096

677

3.2

7.1

<0.5

204.

1020

5.30

1.20

2917

543

115

102

320

2.5

3.1

<120

5.30

206.

351.

0533

162

438

1310

950

52.

74.

63-

520

6.35

207.

050.

7011

255

715

2539

414

1930

2.7

4.7

160.

8022

9.70

gabb

ro b

recc

ia<1

207.

0520

7.75

0.70

6333

994

328

328

1130

2.8

3.4

(con

t.)(c

ont.)

<0.5

207.

7520

8.75

1.00

4351

616

0942

258

433

3.1

1.7

1-2

208.

7520

9.65

0.90

121

865

2661

8443

916

803.

13.

80.

520

9.65

210.

200.

5585

604

1889

4825

910

803.

14.

2B

REC

CIA

UN

IT<1

210.

2021

1.00

0.80

7733

712

4733

244

1200

3.7

4.9

<121

1.00

211.

600.

6011

959

818

2649

324

1410

3.1

4.4

(160

.8 to

225

.7m

)<0

.521

1.60

212.

500.

9059

218

492

1511

174

52.

36.

7<1

212.

5021

3.10

0.60

7148

913

0047

312

1010

2.7

3.2

621

3.10

213.

500.

4012

364

518

3650

530

2210

2.8

4.2

121

3.50

214.

150.

6510

639

811

2433

442

1630

2.8

3.7

<121

4.15

215.

301.

1586

303

824

2336

510

202.

72.

8<0

.521

5.30

216.

801.

5016

166

512

1310

915

13.

11.

4<1

216.

8021

7.60

0.80

9963

417

1753

320

1400

2.7

4.4

<0.5

217.

6021

9.00

1.40

3529

385

937

185

597

2.9

3.2

121

9.00

220.

001.

0010

958

617

9851

258

1250

3.1

4.8

122

0.00

220.

850.

8575

401

1054

3124

310

502.

64.

3<0

.522

0.85

221.

400.

5563

581

1708

4931

110

902.

93.

51-

222

1.40

222.

300.

9016

074

221

0455

502

2090

2.8

4.2

tr22

2.30

223.

000.

7065

370

1162

2825

911

903.

14.

6<0

.522

3.00

224.

501.

5024

102

194

142

392

1.9

2.8

tr22

4.50

225.

701.

2026

115

309

119

357

2.7

3.0

BO

UN

DA

RY

UN

IT<0

.522

5.70

227.

251.

5540

171

373

151

743

2.2

4.9

tr22

7.25

229.

001.

7521

6511

088

414

1.7

4.7

(225

.7 to

233

.2m

)tr

229.

0022

9.70

0.70

2679

191

9447

62.

45.

1

Grid

Nor

th:

450

[517

2419

.22m

N]

Grid

Eas

t: -3

40[5

5514

6.44

mE]

Col

lar D

ip:

-4

5C

asin

g:

1m N

W

Hol

e N

o.:

RV

00-2

2C

olla

r Bea

ring:

86D

epth

: 25

9.0m

Elev

atio

n: +

325.

24m

MSL

APP

END

IX 3

: (C

) Dril

l Hol

e R

V00

-22

Riv

er V

alle

y In

trusi

on

From

ToR

ock

Type

%V

SFr

omTo

Inte

rval

Au

PtPd

Rh

Ni

Cu

Pd:P

tC

u:N

i(m

)(m

)(U

nit)

(max

)(m

)(m

)(m

)(p

pb)

(ppb

)(p

pb)

(ppb

)(p

pm)

(ppm

)22

9.70

259.

00sh

eare

d tr

229.

7023

1.00

1.30

1245

6814

716

41.

51.

1ga

bbro

(?) f

ootw

all

tr23

1.00

232.

001.

0017

5617

517

614

53.

10.

8tr

232.

0023

3.20

1.20

940

7016

384

1.8

0.5

FOO

TWA

LL B

REC

CIA

tr23

3.20

235.

001.

8020

1519

144

901.

30.

6tr

235.

0023

6.50

1.50

1324

1917

011

40.

80.

7(2

33.2

to 2

48.0

m)

tr23

6.50

238.

001.

507

2114

123

960.

70.

8tr

238.

0023

9.50

1.50

2228

1613

789

0.6

0.6

tr23

9.50

241.

502.

0017

015

148

600.

4

2% p

y24

4.00

244.

300.

30

FOO

TWA

LL

(248

.0 to

259

.0m

)10

% p

y25

0.00

250.

260.

265%

py

255.

7825

6.00

0.22

Col

lar D

ip:

-4

5C

asin

g:

1m N

W

Hol

e N

o.:

RV

00-2

2C

olla

r Bea

ring:

86D

epth

: 25

9.0m

Elev

atio

n: +

325.

24m

MSL

Grid

Nor

th:

450

[517

2419

.22m

N]

Grid

Eas

t: -3

40[5

5514

6.44

mE]

APP

END

IX 3

: (C

) Dril

l Hol

e R

V00

-22

Riv

er V

alle

y In

trusi

on

572

VITA Name: Laurence Scott Jobin-Bevans Post-secondary The University of Manitoba Education and Winnipeg, Manitoba, Canada Degrees: 1991-1995 B.Sc.(hons) The University of Manitoba Winnipeg, Manitoba, Canada 1995-1997 M.Sc. Honours and Paul R. Beaudoin Memorial Geochemistry Scholarship Awards: 1993

Mark G. Smerchanski Memorial Prize 1994 Dr. George Brownell Memorial Prize 1994 NSERC Postgraduate Scholarship (M.Sc.) 1995-1997 C.K. Bell Memorial Research Prize 1996 The University of Western Ontario, Graduate Tuition Scholarship 1997-1999 CIM Graduate Thesis Award (M.Sc.) 1998 NSERC Postgraduate Scholarship (Ph.D.) 1997-1999 Hugh E. McKinstry Fund Scholarship 1998 Province of Ontario Graduate Scholarship 1999-2001

Related Work Teaching Assistant Experience: The University of Western Ontario 1997-1998 Projects Manager Pacific North West Capital Corp. 1999-2004 Publications: Easton, R.M., Jobin-Bevans, L.S. and James, R.S., 2004. Geological Guidebook to the Paleoproterozoic East Bull Lake Intrusive Suite Plutons at East Bull Lake, Agnew Lake and River Valley, Ontario. Ontario Geological Survey, Open File Report 6135, 84 pp.

573

James, R.S., Jobin-Bevans, S., Easton, R.M., Wood, P., Hrominchuk, Keays, R.R. and Peck, D.C., 2002. Platinum-group element mineralization in Paleoproterozoic basic intrusions in Central and northeastern Ontario, Canada. In: The Geology, Geochemistry, Mineralogy and Mineral Beneficiation of Platinum-Group Elements. Edited by L.J. Cabri. Canadian Institute of Mining, Metallurgy and Petroleum, Special Volume 54, p. 339-365. Jobin-Bevans, L.S., Keays, R.R. and MacRae, N.D., 1999. Project 97012. Cu-Ni-PGE in Nipissing Diabase: Results from surface and core samples. In: Summary of Field Work and Other Activities, 1999. Ontario Geological Survey, Open File Report 6000, p. 33-1-33-5. Jobin-Bevans, L.S., MacRae, N.D. and Keays, R.R., 1998. Cu-Ni-PGE Potential of the Nipissing Diabase. In: Summary of Field Work and Other Activities. Ontario Geological Survey, Miscellaneous Paper 169, p. 220-223.

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