Volume I

GEOLOGIC SUMMARY REPORT OF THE

19 8 8 EXPLORATION PROGRAM SUNNYSIDE TAR SANDS PROJECT

CARBON COUNTY UTAH

for GENE E. TAMPA

DIRECTOR TAR SANDS AND SHALE PROJECTS AMOCO CORPORATION CHICAGO, ILLINOIS

by WM. S. CALKIN, D.Sc. CONSULTING GEOLOGIST GOLDEN, COLORADO

June 1, 1989 0093?

WILLIAM S. CALKIN, D.Sc. CONSULTING GEOLOGIST

25200 VILLAGE CIRCLE • GOLDEN, COLORADO 80401-9642 • PHONE (303) 526-0711

June 1, 1989

Mr. Gene E. Tampa Director Tar Sands and Shale Projects Amoco Corporation MC 29 03 200 East Randolph Drive Chicago, Illinois 60680

Dear Mr. Tampa:

This three volume report on the Sunnyside Tar Sands project is a summary of the drilling results, geological field and office work completed for the 1988 exploration program. The report contains some important additions to previous exploration programs. The field work was completed with the very capable and helpful assistance of Rob Roy.

The summary and conclusions as well as recommendations occur at the beginning of the report. All photographs, figures and tables are in numerical order in the Appendix at the end of the written report in Volume I. The Regional Map, Geology Map, Tar Sand Isopach Map, Deposition Dip Section, Depositional Strike Section, Structure Contour Map of Blue Marker and Base of Saturation Map are in Volume -II. The fifteen strip logs of three measured sections and twelve drill holes are in Volume III.

The support and cooperation of Amoco during both the field and research phases of this tar sands project is gratefully acknow­ledged. The excellent drafting was completed by Shari Foos of Amoco Production in Denver.

Ten copies of this report have been made, and eight copies will be sent to your office for distribution. Two copies have been retained here in Denver...one copy for John Rozelle and one copy for myself. If there are any questions regarding the geological aspects of the Sunnyside Tar Sands project that need clarifica­tion, please contact me.

Sincerely,

Wm. S. Calkin

00933

Volume I

LIST OF FIGURES

Figure 1. General Location Map, Sunnyside Tar Sands (red dot), Uinta Basin, Utah.

Figure 2. Area Location Map, Sunnyside Tar Sands.

Figure 3. Location of Mt. Bartles-Bruin Point Segmented Flexure, Measured Sections of 1986-88 and Drill Sites of 1988, Sunnyside Tar Sands Area, Carbon County, Utah.

Figure 4. Leasehold and Fee Ownership Map, Sunnyside Tar Sands, Carbon County, Utah.

Figure 5. Surface Ownership Map, Sunnyside Tar Sands, Carbon County, Utah.

Figure 6. Northeast Portion of Energy Resources of Utah.

Figure 7. Paleogeography of the Paleocene (66-58Ma), Northeast Utah.

Figure 8. Paleogeography of the Eocene (58-37Ma), Northeast Utah.

Figure 9. Stratigraphic Section and Isopach Maps of Uinta Basin.

Figure 10. Northeast Utah Correlation Chart.

Figure 11. Index Map of Uinta and Piceance Creek Basins.

Figure 12. West to East Cross Section of the Uinta Basin Looking North.

Figure 13. Idealized Section of Bruin Point Subdelta Showing Tar Zones and Depositional Environments.

Figure 14. Idealized Section of Dry Canyon Subdelta Showing Tar Zones and Depositional Environments.

Figure 15. Stratigraphic Markers in the Parachute Creek Member, Sunnyside Tar Sands, Carbon County, Utah.

Figure 16A. Wavy Bedded Tuff and Mahogany Zone, A-64, Well Log and Lithology Correlations.

Figure 16B. Wavy Bedded Tuff and Mahogany Zone, A-71, Well Log and Lithology Correlations.

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Figure 17. Oil-Shale Zonation and Important Markers in the Green River Formation.

Figure 18. Rich and Lean Oil Shale Zones in the Green River Formation, Piceance Creek Basin, Colorado.

Figure 19. Detail of Mahogany Oil Shale Terminology.

Figure 20A. R-5 Oil Shale, CD-I, Well Log and Lithology Correlations.

Figure 20B. R-5 Oil Shale, A-71, Well Log and Lithology Correlations.

Figure 20C. R-5 Oil Shale, A-72, Well Log and Lithology Correlations.

Figure 21A. Blue Marker, CD-I, Well Log and Lithology Correlations.

Figure 21B. Blue Marker, A-71, Well Log and Lithology Correlations.

Figure 21C. Blue Marker, A-72, Well Log and Lithology Correlations.

Figure 22. Important Stratigraphic Markers in the Green River Formation, Sunnyside Tar Sands, Carbon County, Utah.

Figure 23. Well Log Shapes and Grain Size Distribution.

Figure 24. Well Log Shapes and Depositional Settings.

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Volume I

LIST OF TABLES

Table 1A. Summary of 1988 Drill Hole Data.

Table IB. Available Well Logs from 1988 Drill Holes.

Table 2. Status of 1988 Drill Holes.

Table 3. Blue Marker Data Base.

Table 4. Lithology of Sunnyside Delta Complex and its Two Subdeltas.

Table 5. Rock Type Characteristics, Sunnyside Tar Sands.

Table 6. Mean Composition of Bituminous Sandstones, Sunnyside Tar Sands.

Table 7. Core Sample and Well Log Correlations, Sunnyside Tar Sands.

Table 8. Drill Core Tar Zone Data, Bruin Point Subdelta.

Table 9. Drill Core Tar Zone Data, Dry Canyon Subdelta.

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Volume I

TABLE OF CONTENTS

SUMMARY AND CONCLUSIONS 1

RECOMMENDATIONS 4

INTRODUCTION 5

GEOGRAPHIC SETTING 6

Location 6

Access 6

LAND STATUS 8

REGIONAL SETTING 9

Geology 9 Geophysics 11

Aeromagnetics 11 Gravity 12 Seismic 12

GEOLOGY OF PROJECT AREA 14

Structure 14

Structure Contour Map of Blue Marker 15

Green River Formation 16

Parachute Creek Member 18

Wavy Bedded Tuff 19 Mahogany Oil Shale 20 R-5 Oil Shale 22 Lower Tuff 23 Blue Marker 24

Garden Gulch Member 26

Douglas Creek Member 28

Sunnyside Delta Complex 30

Bruin Point Subdelta 32 Dry Canyon Subdelta 33 Whitmore Canyon Subdelta 35

Shales Carbonates

35 38

TAR SANDS 41

Maps and Sections 41

Tar Sand Isopach Map 41 Deposition Dip Section 42 Deposition Strike Section 42 Base of Saturation Map 4 3

Sheet Sands and Channel Sands 4 4 Depositional Environments 4 5

Sedimentary Structures 4 6 Lag Deposits 49 Textures 4 9 Mineral Composition 50

Interpretation 52

DRILL HOLE AND MEASURED SECTION SYNTHESIS 55

Drill Hole Data 55

1988 Drilling Program 56

Highlights of 1988 Drill Hole Strip Logs 57

Measured Section Data 65

Highlights of 1988 Measured Section

Strip Logs 67

WELL LOGS 69

Gamma-Density-Caliper 69 Multi-Channel Sonic 7 0 Focused Electric 71 Tar Sand Analysis 71 Well Log Interpretation 72

SURFACE GAMMA RAY LOGS 75

RERERENCES 77

APPENDIX Photos 1-7 Figures 1-24 Tables 1-9 00938

SUMMARY AND CONCLUSIONS

1. The distribution of tar sands in the Sunnyside deposit is controlled by both structure and lithology. The structural control is associated with a northwest trending flexure that segments a large monocline which slopes gently into the Uinta Basin. The lithologic control is determined by porous and permeable sandstones deposited in the Sunnyside delta complex.

2. The Mt. Bartles-Bruin Point segmented flexure is the mega control for the distribution of bitumen. The western (updip) segment contains 4-12wt% bitumen in sand­stones that dip 7-12 northeast. The central segment contains 4-7wt% bitumen in sandstones that dip 4-7° northeast. The eastern (downdip) segment contains 0-4wt% bitumen in sandstones that dip 3-4 northeast. In 19 88 eight of twelve drill holes were completed in the eastern and central segments. The results of these eight drill holes indicate limited quantities of low to moderately saturated sandstones. The 1988 drilling program confirms that the most important tar sands exist west of Range Creek, updip from the main axis of the flexure and within the western segment. The segmented flexure has a subtle surface expression. Aero-magnetic, gravity and seismic information indicate the presence of a subsurface fault in the vicinity of the Roan Cliffs. This northwest trending subsurface fault has a vertical dis­placement of 2500-6000 feet with the relative movement up on the San Rafael side and down on the Uinta Basin side. The Mt. Bartles-Bruin Point segmented flexure represents the surface expression of this subsurface fault.

3. The bituminous sandstones are characterized by good lateral continuity and can be separated into sheet sands and channel sands. The majority of the tar sands are sheet sands. A minority of the tar sands are channel sands. The bitumen is of Tertiary age and is mainly associated with fine grained to very fine grained quartz-feldspar sandstones with an average porosity of 27 percent and an average permeability of 812 milli-darcys. Minor amounts of bitumen are associated with siltstones (average porosity of 22 percent and average permeability of 64md) and limestones (average porosity of 18 percent and average permeability of lmd). Fifteen numbered tar zones exist and can be correlated on the basis of surface and subsurface gamma ray logs coupled with stratigraphy.

4. The Tar Sand Isopach Map illustrates three distinct features about the Sunnyside Tar Sands deposit. First, the thickest portion of the tar sands exist beneath Bruin Point in the western segment of the flexure. Second, the tar sands are concentrated within a long and narrow northwest trending

1 00939

belt with decreased bitumen in the lateral extremities. This belt is six to eight miles long parallel to depositional strike and one to two miles wide parallel to depositional dip. Third, a subsurface CC^-rich gas zone exists near the base of the tar sands in an area between Bruin Point and Range Creek.

5. The Structure Contour Map of the Blue Marker at the base of the Parachute Creek Member illustrates two important factors. First, a basic ramp structure with no closure exists in the Bruin Point area. Second, there is a noticeable change in the strike of the structure contour lines near the Bruin Point area.

6. The Base of Saturation Map shows that the basic dip slope ramp contains a large central swale three miles long by two miles wide. This central swale coincides with the vast majority of the tar sands and contains two areas of local depressions. The northwest depression is associated with the thickest tar sand package beneath Bruin Point. The southeast depression is near a structural intersection and may be part of a conduit system that served as an avenue for emplacement of oil that was later degraded to bitumen.

7. The Sunnyside Tar Sands area exists within the Eocene Green River Formation that has been separated into three members. The Douglas Creek Member is at the base, characterized by bituminous sandstones with intervening red shales and represents the delta facies. The Garden Gulch Member is in the middle, characterized by bituminous sandstones with intervening green shales and limestones, and represents the shore facies. The Parachute Creek Member is at the top, characterized by gray shales, oil shales and limited bitu­minous sandstones; it represents the lake facies.

8. Core logging and field work has defined five signifi­cant markers within the Parachute Creek Member. These are the Wavy Bedded Tuff, Mahogany oil shale, R-5 oil shale, lower tuff and Blue Marker. The Wavy Bedded Tuff has an age date of 47.0±1.8my, while the lower tuff has an age date of 51.45±2.0my. The Blue Marker exists at the base of the Parachute Creek Member and has a distinct gamma ray log and lithologic expression.

9. The carbonate-rich interval is seventy feet thick and represents an important regional stratigraphic marker. It exists within the middle portion of the Garden Gulch Member and encompasses Zones 25 and 26. The vast majority of the tar sands package exists below the carbonate-rich interval.

00940 2

10. The Sunnyside delta complex was formed in river-delta-beach-nearshore environments associated with the margins of Lake Uinta during Eocene time some 58-45 million years ago. The outcrops along the Roan Cliffs represent stacked fluvial-deltaic and shoreline sequences. The Sunnyside delta complex consists of 15-36 stacked intervals of sandstone-shale-limestone-unconformity sequences. These lithologic sequences represent repeated cycles formed by regressions and transgressions related to fluctuating lake levels caused by alternating wet and dry climatic cycles.

11. The Sunnyside Tar Sands deposit formed within a delta complex that is divided into three subdeltas. The Bruin Point, Dry Canyon and Whitmore Canyon subdeltas are delineated on the Tar Sand Isopach Map. The most productive portions of the tar sands are in the proximal portions along the Roan Cliff face where the main saturated zones are thickest and of the highest and most consistent grades. Thinning of the bituminous sandstones is pronounced from proximal to medial to distal portions of the subdeltas over distances that range from one to four miles down depositional dip.

3 0094l

RECOMMENDATIONS

1. An isopach map of each numbered tar sand should be made from the mine model data base. These fifteen individual isopach maps will define the distribution and depositional patterns of the major tar sands. These results will lead to a better understanding of the tar sands deposit and be useful for the selection of additional drill sites.

2. The continued use of the surface gamma ray logs within measured sections is highly recommended as it is a vital geophysical tool to establish numbered tar zones.

3. The hot spot in the south area near the South Knoll contains some near-surface rich tar sands as determined in 1988 by three of twelve drill holes and measured section No. 3 at the South Overlook. This south area needs to be more completely evaluated as a pilot mine area. Drill holes to investigate the potential for a pilot mine in the south area should be laid out one year prior to the drilling schedule.

4

009

INTRODUCTION

The 1988 field program focused on completion and logging of twelve core drill holes and three measured sections. Five marker beds were established within the Parachute Creek Member and include the Wavy Bedded Tuff, Mahogany oil shale, R-5 oil shale, lower tuff and Blue Marker containing the R-2 oil shale.

The field season extended from June 7-0ctober 21, and included 104.5 working days. A breakdown of these working days includes 10.5 days for organization; 12.5 days for field geology; 17 days at the drill sites for coordination of dozer work, drillers, well logger and surveyors plus stopping the holes; 44.5 days for logging core and 20 days for travel. The weather was abnormally dry and road conditions were generally excellent. Exceptions include a 12" snowstorm on September 12, heavy rains on September 21, and rain with 4" of snow on October 12. The normal wet season that occurs in late August-early September did not occur in 1988.

This report focuses on the results of the 1988 drilling program and is a continuation of previous exploration reports. Seven photographs included in this volume are used to highlight aspects of the Sunnyside Tar Sands project. Volume II contains seven large maps. Volume III contains fifteen strip logs. Both core logging and field work were used to determine the lithologic characteristics and environments of deposition associated with the Sunnyside Tar Sands deposit, and this data is summarized in Table 5. This field and core data was used in conjunction with the gamma ray well logs to correlate and determine numbered tar zones. The numbered tar zones and bitumen content (analyzed by Core Labs, Inc.) appear on the strip logs and in Tables 8 and 9. The use of numbered tar zones has established continuity between the field data and drill hole data throughout the Sunnyside Tar Sands area.

00943

5

GEOGRAPHIC SETTING

Location

The Sunnyside Tar Sands area is located in northeastern Utah about one hundred miles southeast of Salt Lake City and about thirty miles east of Price as shown in Figures 1 and 6. The Sunnyside Tar Sands area is located in the southwest portion of the Uinta Basin, centered near Bruin Point and located about six miles northeast of the coal mining town of Sunnyside as seen from Figures 1 and 2. The principal physio­graphic features in the area are highlighted in Figure 2 and consist of the Book Cliffs, Roan Cliffs and West Tavaputs Plateau. The location of the newly defined Mt. Bartles-Bruin Point flexure is indicated on Figures 2 and 3.

Access

Access to Bruin Point is via the town of Sunnyside, up Whitmore Canyon and up Water Canyon. The last two miles to Bruin Point contain steep grades of fifteen to twenty percent. Roads to Bruin Point and Mt. Bartles are from two entirely different routes.

Access to Mt. Bartles is from Wellington via Nine Mile Canyon, across Nine Mile Creek and up Harmon Canyon (located 32.7 miles from the Wellington turnoff) or up Prickly Pear Canyon (located 8.6 miles down Nine Mile Canyon from Harmon Canyon). Within Harmon Canyon the road travels along the creek bed for half-a-mile and passage can be difficult to impossible. Two landslide areas exist in Harmon Canyon with the most dangerous just above the half-a-mile creek passage. The BLM no longer maintains Harmon Canyon on a yearly basis. Within Prickly Pear Canyon the road is generally clear and of moderate grade as it was used between 19 59-19 81 to transport oil and gas drilling equipment for nine exploration holes located in the vicinity of the Stone Cabin gas field (abandoned). Most of the oil and gas wells are within two to four miles of the abandoned landing strip and were drilled to depths of 5600-7200 feet. The roads up Harmon Canyon and Prickly Pear Canyon join at a stock pond above the abandoned landing strip near the top of Harmon Canyon (Figure 2). Final access to the Mt. Bartles area is controlled by a locked gate located near the "W" in West Tavaputs Plateau of Figure 2. The combination to the locked gate can be obtained at the Calder ranch located about 1.5 miles east of Harmon Canyon.

0094* 6

Access to the Whitmore Canyon area is via dirt roads adjacent to Grassy Trail Reservoir and up the Right Fork of Whitmore Canyon (Figure 2). Access to the Grassy Trail Reservoir is via a locked gate controlled by the coal mine at Sunnyside. Another locked gate exists up the Right Fork of Whitmore Canyon and is controlled by Jay Pagano of Wellington.

Access to the proposed plant site for tar sand processing in Clark Valley is via Sunnyside, the golf course road, and 3.7 miles on a dirt road along the base of the Book Cliffs to the mouth of B Canyon (Figure 2). Another access exists by turning north off Route 123 at 2.7 miles from Sunnyside Junction. Then at 1.1 miles turn right and head in a north­east direction for 3.3 miles to a dirt road junction located near the proposed 5500 foot wide tailings dam between two natural abutments. Hence 3.2 miles on the right fork to the proposed plant site.

LAND STATUS

The land status of the area encompassing and surrounding the Sunnyside Tar Sands is shown in Figure 4 (Leasehold and Fee Ownership) and Figure 5 (Surface Ownership). The data base for both Figures 4 and 5 is Map 1-4, Sunnyside Combined Hydrocarbon Lease Conversion, draft Environmental Impact Statement, BLM, November 1983. Figure 4 reflects the purchase of Mono Power's interests by Amoco. Numerous leases controlled by Amoco within the Sunnyside Tar Sand area exist in a checker­board pattern and total 29.6875 sections or 19,000 acres. Amoco fee lands total 1.75 sections or 1120 acres.

Within the main portion of the Sunnyside Tar Sands deposit only three important blocks are not controlled by Amoco (Figure 4) and include: (1) fee land totalling 1.125 sections, or 7 20 acres, controlled by Coca Mines and commonly referred to as h Mt. Mary's Parish and h Crosby Corporation; (2) fee land of Gibbs Heirs that totals one section or 640 acres; and (3) a lease controlled by Great National Corporation for h section or 160 acres.

Figure 5 indicates that much of the surface ownership near Bruin Point is controlled by Amoco, Coca Mines and Gibbs Heirs. Other surface in the Sunnyside Tar Sand area is con­trolled by the BLM and private ownership. The road from the Asphalt Mine to Bruin Point is a county designated road with a 25-foot right-of-way.

8

00946

REGIONAL SETTING

Geology

The late Cretaceous and early Tertiary geology of north­eastern Utah is briefly presented to clarify the structural setting and regional framework associated with the Sunnyside Tar Sands. The structural setting forms the basis for an understanding of the northwest trending Mt. Bartles-Bruin Point flexure. The regional framework sets the stage for paleo-drainage conditions and the formation of the Sunnyside delta complex in ancestral Lake Uinta.

The Sunnyside Tar Sands area is located about eighty miles east of the Cordilleran overthrust belt, about sixty miles northeast of the center of the San Rafael Swell and within the southwestern portion of the Uinta Basin. The Cordilleran overthrust belt complex is a major tectonic element in North America and was caused by compression of the westward-moving subducted Pacific plate during the late Cretaceous to Eocene time. That portion of the Cordilleran overthrust belt in Utah is variously known as the Sevier overthrust belt, Wasatch Line or Cordilleran hingeline.

The northeast trending Colorado Lineament and the north­west trending Olympic-Wichita Lineament represent ancestral zones of crustal weakness established in basement complexes during Precambrian time. These zones of crustal weakness have repeatedly been reactivated throughout different portions of geologic time and frequently control regional structural fabric. In Pennsylvanian time the Paradox Basin of southeastern Utah formed as a pull apart feature at the junction of the Colorado and Olympic-Wichita Lineaments (Stevenson and Baars, 1986). Northwest trending structures dominate the regional fabric of eastern Utah as seen in Figure 6 and on various geological maps of the State of Utah. These maps include: (1) Geologic Map of Utah (1963) compiled by W.L. Stokes at a scale of 1:250,000; (2) Geologic Map of Utah (1980) compiled by L.F. Hintze at a scale of 1:500,000; and (3) Energy Resources Map of Utah (1983) at a scale of 1:500,000. The latter has been reduced to form Figure 6 which shows the north­west trending structural element in the right half. In the lower right portion both the Moab fault zone and the Paradox fold and fault belt have a northwest trend. In the upper right portion south of Vernal numerous gilsonite veins have a north­west trend. The Book Cliffs between Sunnyside and Price have a northwest trend. This northwest trend is a dominant topographic and geologic feature and related to Precambrian basement and the late Paleozoic Uncompahgre uplift that exists beneath the south­west portion of the Uinta Basin (Figure 9).

9 0094?

The Rocky Mountain foreland province exists to the east of the Sevier overthrust belt and contains Laramide uplifts of north-south, northwest and east-west trends. The distribu­tion of these three trends and their time of movement is briefly discussed below based on Greis (1983):

(1) The north-south trending Laramide uplifts are the oldest in age and formed in late Cretaceous (i.e., Campanian and Maestrichtian time of Figure 10) and include the Colorado Front Range west of Denver and the San Rafael Swell west of Green River. The San Rafael Swell formed in late Cretaceous during a time interval of 3-15my (million years) and between 73-58Ma (millions of years before present) at low uplift rates of 0.36-0.07mm/yr (Lawton, 1983) .

(2) The northwest trending Laramide uplifts are intermediate in age and formed in early Paleogene (i.e., early to middle Paleocene of Figure 10) and include the Uncompahgre Uplift in western Colorado and portions of eastern Utah.

(3) The east-west trending Laramide uplifts are the youngest in age and formed in late Paleogene (i.e., early to middle Eocene of Figure 10) and include the Uinta Mountains that form the north side of the Uinta Basin.

During the thirty-five million years between late Cretaceous (70Ma) and late Eocene (35Ma) some 15,000 feet of sediments accumulated in northeastern Utah. After the east­ward retreat of the late Cretaceous seaway, two different lake centers formed within regional tectonic depressions. First, Lake Flagstaff formed in the structural basin between the Sevier Orogenic Belt and the San Rafael Swell. These lacustrine sediments form the Flagstaff Formation whose distribution is seen in Figure 7. Later Lake Uinta formed in the structural basin between the San Rafael Swell, Uinta Uplift and Uncompahgre Uplift. These lacustrine sediments form the Green River Formation whose distribution is seen in Figure 8. The regional stratigraphic position of the Flagstaff and Green River Formations are illustrated in Figure 9. In middle Eocene-during the maximum extent of Lake Uinta numerous intervals of oil shale were formed and include the Mahogany oil shale. During late Eocene Lake Uinta regressed and at the end of Eocene time Lake Uinta dried up. Within the Uinta Basin sandstones derived from the Uinta Uplift are dominated by quartz, while those sandstones derived from the Uncompahgre Uplift are dominated by quartz and feldspar.

io 00948

Above data summaried from Bruhn, Picard and Beck (1983). A correlation chart of Cretaceous and Tertiary rock formations in northeastern Utah is shown in Figure 10.

Geophysics

Regional geophysical data in northeastern Utah includes aeromagnetics, gravity and seismic. This data illustrates a dominant northwestern structural trend in the Sunnyside area, and two different authors suggest a major subsurface fault in the vicinity of Sunnyside. The surface expression of this fault is suggested to represent the Mt. Bartles-Bruin Point flexure first recognized and mapped by Calkin and Grette during the 198 6 and 198 7 field seasons.

The geophysical interpretations were enhanced by four maps at the same scale. The Geological Highway Map of Utah (Hintze, 1982) and the Aeromagnetic Map of Utah (Zietz, et al, 1976) were both published at a scale of 1:1,000,000. The gravity and basement maps (Smith and Cook, 19 85) were enlarged to a scale of 1:1,000,000. These four maps (geology, aeromagnetics, basement and gravity) appear in the 19 87 Exploration Report. The buried Uncompahgre uplift exists within the southern portion of the Uinta Basin (Figure 9) and has a significant influence on the overlying strata.

Aeromagnetics

In northeastern Utah the broad features of the aero­magnetic map indicate northwest trends and east-west trends. The northwest trends exist within the central portion and southwest margin of the Uinta Basin and coincide with the Uncompahgre structural trend of intermediate Laramide age. The east-west trends exist on the southern and northern margins of the Uinta Basin and correspond to the Uinta Mountain structural trend of youngest Laramide age.

An aeromagnetic high of 11,480 gammas is centered in a valley one to two miles south of Sunnyside. This valley is at the base of the Book Cliffs and near the town of Columbia. Correlation of this aeromagnetic high at Sunnyside with the basement map indicates that the Sunnyside high is near the structural intersection of a basement complex that plunges northward from the San Rafael Swell and a basement complex that plunges northwestward from the Uncompahgre uplift. Smith and Cook (19 85) state that from an area ten miles south of Price hence eastward toward Sunnyside the basement rises about 7500 feet within twenty-four miles. The presence of a shallow basement complex near Sunnyside explains this prominant aeromagnetic high.

11 00949

Gravity

The Bouguer Gravity Map of northeastern Utah was compiled and interpreted by Smith and Cook (1985) . A major northwest trending subsurface fault is associated with the gravity low in the area of the Sunnyside Tar Sands. Gravity anomalies are caused by vertical and lateral variations in the density of the rocks in the subsurface and are strongly influenced by changes in depth to Precambrian basement. The gravity map of northeastern Utah is characterized by two major trends containing three significant highs and two prominent lows.

The two major trends are oriented northwest and east-west and correspond to two of the three structural trends of Laramide uplifts. The northwest trend extends from southeast of Crescent Junction to north of Sunnyside. This northwest trend contains the Sunnyside Tar Sands area and encompasses the trend of intermediate Laramide age. The east-west trend is in the northern portion, coincides with the Uinta Mountains and corresponds to the trend of youngest Laramide age.

The three significant highs include: (1) a broad area south of Price associated with the large anticlinal system of the San Rafael Swell; (2) the elongated high associated with the Uinta Mountains; and (3) a high near Cisco that is part of the plunging nose of the Uncompahgre uplift.

The two prominent lows help to define the northwest structural trend and include an area southeast of Crescent Junction and an area near Sunnyside. The elongated low southeast of Crescent Junction represents the Salt Valley gravity low and is caused by the low density evaporites in the core of the Salt Valley anticline (Smith and Cook, 1985). Salt Valley parallels the southwest flank of the Uncompahgre uplift. The prominent Sunnyside low is centered on Bruin Point and the Sunnyside Tar Sands area. This Sunnyside low is interpreted by Smith and Cook (1985) to contain a zone of subsurface faulting with up to 6000 feet of vertical displace­ment. The Uinta Basin is on the downthrown side. This fault lies east of Sunnyside and extends for ten miles to the northwest and about sixteen miles to the southeast. The surface expression of this subsurface fault is represented by the Mt. Bartles-Bruin Point flexure.

Seismic

The seismic data in the Sunnyside area is from Tibbetts, et al (1966) and indicates the following: (1) a northwest trending fault exists in the Sunnyside area and has a strata-graphic separation of about 2 500 feet with relative movement

12 00950

up on the San Rafael side and down on the Uinta Basin side; (2) when extended to the southeast along the northwestern regional structural trend the trace of the fault passes into the area of Turtle Canyon (located off the lower portion of Range Creek in Sections 32 and 33, T17S, R16E) where there is subsurface evidence of major faulting; (3) on Range Creek at the abandoned pump station (located about four miles east of the Sunnyside coal mine and 1500 feet upstream from Amoco Production Kaiser Steel No. 1, see Regional Map) the depth to the Paleozoic carbonates is about 12,000 feet and regional dip is about 4 NE into the Uinta Basin; and (4) the thickness of the sediments that overlie the Paleozoic carbonate reflector ranges from 4000 feet in Clark Valley to 12,000 feet in Range Creek. Clark Valley and Range Creek are about eleven miles apart.

00S51

13

GEOLOGY OF PROJECT AREA

The Sunnyside Tar Sands area is located thirty miles east of Price and is well-exposed along the Roan Cliffs. The tar sands are localized within the Sunnyside fluvial-deltaic complex that formed during the Eocene and are contained within the Green River Formation. The source for the quartz-feldspar rich sandstones was the Uncompahgre Uplift. The Sunnyside Tar Sands area contains an important northwest trending segmented flexure (Figures 2 and 3). The flexure and sandstone reservoir rocks have localized the distribution of bitumen.

Structure

The area contains a segmented flexure associated with a monoclinal dip slope. The flexure has a subtle surface expression and distinct structural evidence exists in limited and remote areas. The dips in the Bruin Point area of the Roan Cliffs are commonly 7-12 NE, while dips in the West Tavaputs Plateau are commonly 3-4 NE. The change in these dips was first documented in the early part of the 1986 field season while measuring sections in the peripheral hydro­carbon leases located in the West Tavaputs Plateau.

The general structural evidence for this flexure includes: (1) northwest trending drainages and lineaments that parallel the regional northwest structural fabric and (2) changes in dips associated with different portions of the flexure. (1) In the late part of the 1986 field season views north of Mt. Bartles from Measured Section 37 located a distinct lineament in Sheep Canyon. This lineament with associated landslides were examined on foot in June, 19 87. The area is characterized by anomalously high 30-90 dips in numerous large debris masses of chaotic blocks that moved downdip. These chaotic slump blocks are associated with en-echelon 20-30 foot deep troughs elongated parallel to the trend of the flexure. This Sheep Canyon area represents the northern part of the flexure zone as shown on Figure 3, Regional Map and Geology Map. The southern part of the flexure zone follows the pronounced topographic lineament associated with the upper portion of Range Creek. (2) The Mt. Bartles-Bruin Point flexure has divided the Sunnyside Tar Sand area into three different segments. Each segment is characterized by different dips and bitumen content (see Figure 3 and the Depositional Dip Section of Volume II). The eastern segment exists in the West Tavaputs Plateau and is characterized by 3-4° northeast dips and sandstones that contain 0-4wt% bitumen. The central segment is characterized by 4-7 northeast dips and sandstones that contain 4-7wt%

14 00952

bitumen. The western segment exists along the Roan Cliffs and is characterized by 7-12 northeast dips with sandstones that contain 4-12wt% bitumen. Thus, this northwest trending Mt. Bartles-Bruin Point flexure has gentle dips of 3-4 NE on the downthrown side and steeper dips of 7-12° NE on the upthrown side. In addition tar sands of 4-12wt% bitumen persist in the upsthrown side, while tar sands of 0-4wt% bitumen persist in the downthrown side. Clearly, the flexure has an important in­fluence on the distribution of the bitumen content.

The specific structural evidence used to define the Mt. Bartles-Bruin Point segmented flexure includes: changes in dip with accompanying changes in bitumen content; chaotic slump blocks and associated linear troughs; mini-anticlines (see Photo 4); isolated linear troughs; dip reversals of sandstone zones; slickensides; and northwest trending pyrite veinlets. The subtle changes in monoclinal dips are best seen in views perpendicular to dip that look down the axis of the northwest-southeast trending structure. Without a near-perpendicular view the subtle changes in true dip merge almost imperceptibly into a continuous low apparent dip. Detailed field evidence of the flexure is noted on the Geology Map in Volume II and exists in four specific localities of T13S, R14E. In section 7, NE/4 two mini-anticlines exist and one is shown in Photo 4. In section 17, NW/4 multiple thin northwest trending pyrite veinlets are exposed along a pronounced curvature of a creek bed. In section 20, NW/4 excellent slickensides were found along a massive northwest trending joint. In section 28, SE/4 dip reversals of sandstone zones (i.e., 3-10° SW instead of 4-7 NE) were mapped along poorly accessible exposures adjacent to creek bottoms.

Structure Contour Map of Blue Marker

The segmented flexure is associated with a monoclinal dip slope or ramp that contains no closure as determined by the Structure Contour Map of the Blue Marker in Volume II. The Blue Marker is the distinct marker horizon at the base of the Parachute Creek Member. It is well recognized throughout the project area in drill core, on gamma ray well logs, in outcrop, and by surface gamma ray logs (see Figures 15, 21 and 22 and strip log MS-59 in Volume III). Elevations of the Blue Marker from drill holes and measured sections exist in Table 3. This data was used to construct the Structure Contour Map of the Blue Marker. Data points from drill holes and well logs are considered accurate to within 1-2 feet. Data points from measured sections are considered accurate to within 5-10 feet.

15 00953

The Structure Contour Map of the Blue Marker illustrates two important factors: (1) basic ramp structure with no closure and (2) change in strike near Bruin Point. Factor (1): A basic ramp structure is established by the uniform dips of the Blue Marker. The dip direction coincides with the depositional dip direction which slopes downdip toward the Uinta Basin and updip toward the Roan Cliffs (see Photo 1). The uniform spacing of the structure contours in the northeast portion of the Structure Contour Map indicate uniform dips of 3-4 degrees that steepen to uniform dips of 6-8 degrees toward the Roan Cliffs. Regional dips of the Blue Marker within the West Tavaputs Plateau and toward Nine Mile Canyon are N54 W, 2°NE. These more gentle dips toward the Uinta Basin were determined by a three point problem of the Blue Marker from outcrops in MS-29, upper Harmon Canyon and upper Prickly Pear Canyon. These three Blue Marker outcrops are essentially 26,000, 36,000 and 38,000 feet apart with a maximum elevation difference of 1155 feet for the Blue Marker. Factor (2): There is a noticeable change in strike of the structure contour lines near Bruin Point. From Bruin Point to Mt. Bartles the strike is N45-50 W. From Bruin Point to South Knoll the strike is N20 VJ. This change in strike is associated with a pivot area near Bruin Point and the thickest accumulation of tar sands (see Tar Sand Isopach Map).

The Structure Contour Map also illustrates the lack of any closure centered on Bruin Point. Some closure was initially suggested by cross sections and eyeballing in the field. The Blue Marker in the Bruin Point area is near 10080 feet in elevation. The Blue Marker in the Mt. Bartles area (5 miles northwest of Bruin Point) and the South Knoll area (2 miles southeast of Bruin Point) are both near 9780 feet in elevation. This 300 foot difference in elevation is explained by the fact that the Blue Marker in the Bruin Point area is some 2500 feet updip from the Blue Marker at Mt. Bartles and South Knoll; this data equates to a dip of seven degrees that is characteristic of the western segment of the Mt. Bartles-Bruin Point flexure. As determined from the Structure Contour Map, Bruin Point is located in the most updip portion of the project area, and there is no closure associated with the Sunnyside Tar Sands deposit.

Green River Formation

The early sediments that formed within Eocene Lake Uinta belong to the Green River Formation, and their distribution within the Uinta and Piceance Creek Basins is shown in Figure 11. The late sediments that formed within the central portion of Lake Uinta belong to the Uinta Formation or saline facies, and their distribution is also shown in Figure 11. The tar sands

16 009S4

in the Sunnyside area are confined to rocks within the Green River Formation and its three members. These consist from top to bottom of the Parachute Creek Member, Garden Gulch Member and Douglas Creek Member. In Figure 12 a cross section of the Uinta Basin illustrates commonly used stratigraphic terminology east and west of the Green River. The area of the Sunnyside Tar Sands has been projected twenty miles downdip to show its relative stratigraphic portion within Figure 12.

The Green River has eroded a formidable canyon that geo­graphically separates the Uinta basin into a western and eastern portion (see Figures 11 and 12). The eastern Uinta basin and the Piceance Creek basin are locally grouped together, and the stratigraphic terminology for the Green River Formation developed by Bradley (1931) has been used throughout this geographically contiguous area. The Green River Formation was separated into three members consisting of the Parachute, Garden Gulch and Douglas Creek Members. Unfortunately, the rock units in the western Uinta basin have a different stratigraphic terminology for the Green River Formation with the exception of the Parachute Creek Member. Figures 11-14 along with the following discussion help to clarify this some­what confusing difference in two sets of terminology that exist for the western Uinta basin.

The first set of stratigraphic terminology in the western Uinta basin was developed in the oil fields and includes the green shale facies, delta facies and black shale facies (see Figure 12). The green shale facies roughly equates to the Garden Gulch Member. The delta and black shale facies roughly equate to the Douglas Creek Member. Carbonate rocks dominated by micrites and biomicrites are scattered throughout the Green River Formation and help to differentiate the Green River Formation from the underlying Wasatch or Colton Formations (Picard, et al, 1973). The second set of terminology developed in the western Uinta basin was introduced by Fouch (1975) and Ryer, et al (1976) of the U.S. Geol. Survey. They added different terminology and defined the stratigraphic units on the basis of open lacustrine, marginal lacustrine and alluvial lithologic assemblages with no reference to the Parachute Creek, Garden Gulch or Douglas Creek Members. The open lacustrine rocks were deposited in open lake environments and consist of organic rich claystones and carbonates. The marginal lacustrine rocks were deposited in deltaic, interdeltaic and lake-margin carbonate-flat environments and consist of sandstones, clay-stones and weakly indurated clay carbonates. The alluvial rocks were deposited peripheral to the marginal lacustrine environments.

Within the Sunnyside Tar Sands area geological mapping in 1980 separated the rocks into the Parachute Creek, Garden Gulch and Douglas Creek Members of the Green River Formation.

17 00955

Specific field criteria were used to distinguish these three members as discussed under each specific member. After the Green River Formation was separated into these three members, it was realized that the Parachute Creek Member represents the lake or gray shale facies, the Garden Gulch Member represents the shore or green shale facies, and the Douglas Creek Member represents the delta or red shale facies. These relationships are shown in Figures 13 and 14 and combine the two sets of different terminology in the western Uinta basin with the standard terminology of the eastern Uinta basin into a coherent grouping. Once these three dominant facies were recognized, it became much easier to conceptualize the Sunnyside delta complex.

Parachute Creek Member

The Parachute Creek Member is insignificant as a reservoir for tar sands, and it contains less than five percent of the bituminous sandstones in the entire Sunnyside Tar Sands deposit. However, the Parachute Creek Member is the most important member for stratigraphic correlation. It contains five significant markers which are the Wavy Bedded Tuff, Mahogany oil shale, R-5 oil shale, lower tuff and Blue Marker. Since the beginning of the project in 19 80 the Parachute Creek Member was recognized and mapped on the basis of undifferentiated oil shale units and thin laminated buff to olive gray shales. For many years the Parachute Creek Member continued to receive little attention as it contained insignificant quantities of bituminous sandstones. Extensive field mapping on peripheral hydrocarbon leases in the West Tavaputs Plateau during 1986 and 1987 coupled with about 4000 feet of Parachute core from 11 drill holes during the 1988 drilling season have established five significant markers within the Parachute Creek Member. Their consistent stratigraphic position is shown in Figure 15. The distribution of the Mahogany oil shale (R-7), R-5 oil shale and Blue Marker (R-2) in the Sunnyside Tar Sands area are noted on the Geology Map, Volume II.

The thickness of the Parachute Creek Member depends on its location in the Sunnyside Tar Sands area. Near Bruin Point it is almost 100 feet thick, while near Mt. Bartles it is almost 200 feet thick. In the Roan Cliff portions of the Dry Canyon and Whitmore Canyon subdeltas it is eroded away. In areas of the West Tavaputs Plateau it is 200-600 feet thick. The true thickness of the Parachute Creek Member is not known. The Horse Bench Sandstone which exists above the top of the Parachute Creek Member has not been defined in the Sunnyside Tar Sands area. Excellent and almost continuous exposures of the Parachute Creek Member exist in a minor drainage about 1700 feet northeast of drill hole CD-2.

009^6

18

Wavy Bedded Tuff

Numerous scattered outcrops of the two foot thick Wavy Bedded Tuff exist in the West Tavaputs Plateau and occur near the upper topographic limits of the Parachute Creek Member. Good exposures are located at the Pan American-Nutter Corporation No. 1 drill pad as seen in Photo 3. This outcrop is located near A-72 and RCT-11 (see Geology Map) and can readily be reached by jeep. During the 19 86-1987 field seasons exposures of the Wavy Bedded Tuff (Fouch, et al, 1976) were examined in the Gate Canyon road (T11S, R15E, section 17, SE/4, east side of road) off Nine Mile Canyon to establish field criteria for recognition of this tuff unit within the Mt. Bartles area. The Wavy Bedded Tuff was first recognized in the project area in MS-56, then MS-57 and later numerous locations throughout the Mt. Bartles area and the Bruin Point area east of Range Creek.

The Wavy Bedded Tuff outcrops as a resistant volcanic air fall tuff within the open lacustrine shales of the Parachute Creek Member. Loose rock fragments commonly exist on the slopes that mantle the Wavy Bedded Tuff and outcrops are relatively rare. The resistant volcanic rock fragments have characteristic thumb sized cavities of weathered out ash fragments that range in size from roughly 0.6-1.0 inches in diameter. The unweathered rock has a color of very pale orange (10YR 8/2) to yellowish gray (5Y 8/1), while the weathered rock has a color of grayish orange (10YR 7/4) to grayish yellowish orange (10YR 7/6) . Within the lower six inches of the tuff fresh biotite grains make up 10-15% of the rock and the black medium sized grains (range fU-cL) are readily apparent. Once the field criteria for recognition was completed the Wavy Bedded Tuff became relatively easy to locate with careful scrutiny and knowledge of its stratigraphic position. The Wavy Bedded Tuff exists 35 feet above the Mahogany oil shale (see Figure 15) and its presence is critical for the positive field identification of the Mahogany oil shale as shown on the Geology Map, Volume II. The Wavy Bedded Tuff is more easily recognized in outcrop or drill core than picked from gamma ray and density well logs (see Figures 16A and 16B).

In November 1988 three samples of the Wavy Bedded Tuff were submitted to Geochron Laboratories for age dating of the fresh biotite. The samples and results are:

Sample Age

drill core: A-71, 261.5-263.2 ft. 47.1 ± 1.8 my (split of basal 8 inches)

outcrop: MS-56 46.6 ± 1.8 my outcrop: PanAmer-Nutter Corp. No. 1 47.3 ± 1.8 my

X = 47.0 + 1.8 my

19 009^

Mahogany Oil Shale

The Mahogany oil shale crops out in numerous locations to the east of the main axis of the Mt. Bartles-Bruin Point flexure as seen on the Geology Map, Volume II. The twenty foot thick Mahogany oil shale exists thirty-five feet below the Wavy Bedded Tuff and outcrops as an oil shale doublet with paper shale textures immediately above the brown cliff in the distal portions of the Bruin Point subdelta (see Photo 1). Four drill holes east of Range Creek and three drill holes near Mt. Bartles firmly establish its vertical position thirty-five feet below the Wavy Bedded Tuff. The density well log of the Mahogany oil shale has a character­istic pattern of three nearly equal prongs that from peak to peak form a line with a steep positive slope as seen in Figures 16A and 16B. The low density prongs are caused by intervals of rich oil shale. The Mahogany oil shale forms an important marker in the West Tavaputs Plateau.

In the Sunnyside Tar Sands area the oil shales from the Mahogany (R-7) to the Blue Marker (R-2) encompass a vertical distance of nearly 300 feet (see Figure 15). In the Piceance Creek basin 100 miles to the east of Bruin Point (see Figure 11) the oil shales from the Mahogany (R-7) to the Blue Marker (R-2) encompass a vertical distance of nearly 1200 feet (see Figures 17 and 18) or four times the thickness of the oil shale interval in the Sunnyside Tar Sands area. In the Piceance Creek Basin the Green River Formation contains rich and lean oil shale units that are largely confined to the Parachute Creek Member and have been used for stratigraphic correlation (Ziemba, 1974, and Figure 17). The various rich (R) and lean (L) zones of oil shale in the Piceance Creek Basin are noted in Figures 17 and 18. The rich and lean zones were defined on the basis of oil shale assay histograms and no field criteria is recognized to distinguish each particular rich and lean zone (personal communication, Bill Cashion, November, 1987). The detail of the R-l through R-6 oil shale intervals is given in Figure 18. R-7 corresponds to the Mahogany zone and R-8 refers to the multiple thin oil shale intervals in the upper oil shale zone above R-7 (Figure 19). For reference and correlation this upper oil shale zone (R-8) is well exposed on the west side of Gate Canyon (T11S, R15E, section 17, SE/4).

The purpose of this paragraph is to clarify Mahogany oil shale terminology as summarized from Donnell (1961), Cashion (1967), Dyni (1974), and Stanfield, et al (1960). The Mahogany name is derived from the fact that polished surfaces of dark gray oil shale resemble old mahogany wood. The Mahogany ledge is a 2-60 foot thick outcrop sequence of

00958

20

rich oil shale beds that commonly form a cliff. The top and bottom of the Mahogany ledge are bounded by lean oil shale which weather more rapidly than rich oil shales. These lean oil shales create weathered indentations or grooves into the cliff and gave rise to the terminology of A-groove (top weathered groove) and B-groove (bottom weathered groove). The subsurface equivalent of the Mahogany ledge is the Mahogany zone. Resistivity well logs through the Mahogany zone show that low resistivity values are characteristic of lean oil shale while high resistivity values are associated with rich oil shales. Thus, the A-groove and B-groove patterns have an expression in both the surface and subsurface.

In the Sunnyside Tar Sand area the Mahogany ledge does not form cliffs high enough to express the A- and B-groove concept. The seven drill holes that cored through the Mahogany zone had fluid levels below the Mahogany so resistivity data is not available. Drill core does show that the top and bottom of R-7 and R-5 oil shale intervals are characterized by lean oil shale and/or marlstone IFC's.

The Mahogany oil shale formed in Lake Uinta during the middle Eocene under some unique depositional conditions. The precusor of oil shale is organic ooze derived from blue green algae (Cane, 1976 and Bradley, 1970). The rate of growth of blue green algae depends partly on the water com­position and uncontrolled growth is called an algal bloom. Algal blooms can create local anoxic conditions and may have been an important factor in the formation of oil shale. According to Smith (1983) the Eh (oxidation-reduction potential) and pH limits of oil shale deposition are Eh minus 1 ± 0.5 and pH 8.75 ± .025. Some specific conditions for oil shale deposition stated by Robinson (1976) are: (1) pH = 8.0-10.0 and Eh of minus 0.3-0.45V at pH8 and Eh of minus 0.4-0.58V at pHIO; (2) salinity fluctuated from fresh water to saline water containing 461 ppm dissolved salts; and (3) average annual air tempera­ture of 66-67°F. The organic composition of the Mahogany zone in the Piceance Creek basin is C = 80.5, H = 10.3, N = 2.4, S = 1.0 and 0 = 5.8 (Smith, 1961). The Mahogany oil shale formed -4 8 my ago as determined by calculated sedimentation rates between the Wavy Bedded Tuff (47 my) and the lower tuff (51.4 5 my) mentioned in the lower tuff Section, Parachute Creek Member. Mauger (1977) indicates the Mahogany oil shale formed between 4 5-4 6 million years ago.

The richness of oil shale can be determined qualitatively by a kerogen color index or quantitatively by density well logs. Oil shale content increases with the intensity of brown color as determined by detailed core logging and use of

21 00959

the GSA Rock Color Chart (Goddard, et al, 1963). The results are as follows:

Color Hue and croma Kerogen content

very pale orange 10YR 8/2 very lean pale yellowish brown 10YR 6/2 lean dark yellowish brown 10YR 4/2 moderate disky yellowish brown 10YR 2/2 rich

Some of these color distinctions are shown in Photo 6. Increased kerogen content is reflected by decreased formation density. Density log values were related to assay yields by Tixier and Curtis (1967) with the linear equation:

yield(gpt) = 154.81-59.43 x log density(g/cc)

With this equation a density of 2.0 = 36 gpt; 2.1 = 30 gpt and 2.2 = 24 gpt. Using this equation and density values from drill logs in the Sunnyside Tar Sands area the twenty foot thick Mahogany zone averages 10 gpt with maximum values near 15 gpt.

R-5 Oil Shale

The R-5 oil shale is an important local marker within the Sunnyside Tar Sand area as it outcrops west of Range Creek (see Geology Map, Volume II) and has more extensive exposures and well log intercepts than the R-7 oil shale. The R-5 oil shale is located 145 feet below the Wavy Bedded Tuff and 9 0 feet below the Mahogany oil shale as shown in Figure 15. The surface expression of the R-5 oil shale is shown in Photos 1 and 2. The R-5 oil shale zone is commonly twenty feet thick and outcrops as an oil shale doublet that can readily be confused with the Mahogany R-7 oil shale unless additional field or well log criteria are applied. The density well log of the R-5 oil shale has a characteristic pattern of three unequal prongs that from peak to peak form a line with a moderate negative slope as seen in Figures 20A, 20B and 20C. The density well log pattern of the R-5 oil shale (Figure 20) is distinct from the density well log pattern of the Mahogany (R-7) oil shale (Figure 16). The R-5 oil shale has A- and B-groove patterns in resistivity logs within drill hole CD-I. Thus the A- and B-groove concept is not unique to the R-7 oil shale and may be common to various oil shale intervals. Prior to the definitive data from the 1988 drilling program the R-7 (Mahogany) and R-5 oil shales were often mistakenly identified. For example, Photo 4 (1986 Report) illustrates the R-5 oil shale, not the Mahogany

22

00960

as stated in the 1986 Report. Also in Figure 22 (1987 Report) the indicated Mahogany intervals in MS-32 and Amoco No. 6 3 both represent the R-5 oil shale.

The various springs in the Sunnyside Tar Sands area are confined to the Parachute Creek Member and associated with definite oil shale intervals. Springs are often located just above oil shale intervals (Ertl, 1967). The oil shale commonly serves as a confining bed or aquiclude. Sediments above and below the oil shale are generally more permeable, and the groundwater preferentially passes through more permeable and well jointed beds. In the Mt. Bartles area the Stone Cabin Spring produces ~15,000 gpd and is located slightly above the R-5 oil shale. In the Bruin Point area the North Spring (~25,000 gpd) and the South Spring ("125,000 gpd) are located slightly above the R-2 oil shale.

Lower Tuff

This biotite-rich tuff is 0-16 inches thick and is frequently found in drill core and rarely found in outcrop. The lower tuff is located 215 feet below the Wavy Bedded Tuff, 50 feet below the base of the R-5 oil shale and 140 feet above the Blue Marker (R-2) as seen in Figure 15. The initial position of this lower tuff was established in drill holes BP-IA and RCT-12 from detailed logging of core which located this one inch thick biotite-rich tuff. When MS-29 was re­examined shallow digging 50-60 feet below the base of the uppermost oil shale (R-5) located a one foot thick biotite rich tuff. In 1987 three samples of the lower tuff were sub­mitted to Geochron Laboratories for age dating of the fresh biotite concentrates. The sample results are:

Sample Age

16" outcrop: MS-29 @ 51.5 ± 2.0 my -50' below base R-5

1.5" drill core: BP-IA @ 51.4 ± 2.0 my -235'&56' below base R-5

1.0" drill core: RCT-12 @ biotite mass -249'&56' below base R-5 insufficient

X = 51.45 ± 2.0 my

The lower tuff (51.45 my) is separated from the Wavy Bedded Tuff (47.0 my) by 215 feet of sediments, chiefly shales. Both these biotite-rich tuffs represent time-stratigraphic units. Between these two tuffs average rates of sedimentation are ~1.5mm per 100 years, -one foot per 20,000 years or ~5 feet per 100,000 years.

00961 23

Blue Marker

The Blue Marker or the R-2 oil shale is the most distinctive and widespread marker in the project area. The Blue Marker is recognized in outcrop by a 1-3 foot thick oil shale interval that weathers into thin slabs of oil shale referred to as dinner plates. The weathered surface of these thin dinner plate slabs enhances the appearance of numerous small dis­articulated fossil fish fragments. This is the. only oil

'shale interval that contains abundant fossil fish fragments. About 1-1*5 feet below the dinner plate oil shale a 0.5-1.5 inch thick friable lignite coal seam commonly exists. The dinner plate oil shale and coal seam are part of the distinctive marker in the downhole gamma ray logs that have been used extensively for correlation between project drill holes. Photo 6 shows the Blue Marker in drill core from drill hole CD-I.

The Blue Marker is found near the characteristic color change in shales of the Parachute Creek and Garden Gulch Members. The shales of the Parachute Creek Member are dominantly light olive gray with a rock-color designation (Goddard, 1963) of 5Y 6/1 to 6/2. The shales of the Garden Gulch Member are dominantly greenish gray with a rock-color designation of 5GY 6/1. These color differences as well as a change in the gamma ray background values are recognizable in the surface and subsurface (see Table 5). Surface gamma ray background values in the Parachute Creek Member are between 200-225cps with low values from 180-190cps with a number of high peaks from 300-500cps. In the vicinity of the color change the reading interval for the surface spectrometer is decreased to two to five foot spacings to make a more detailed gamma ray strip log. The strip log of MS-59 (in Volume III) contains a plot of the surface gamma ray log. Comparisons of the surface pattern in MS-59 with subsurface log patterns in Figures 21A, 2IB and 21C show nearly identical patterns.

This distinctive marker at the base of the Parachute Creek Member has been used since 1980 by John Rozelle in correlation of well logs. The RC marker noted in the drill hole files from Mono Power exists at the base of the Parachute Creek Member. Field mapping, drill hole lithology and gamma ray logs from both the surface and subsurface all define the same marker at the base of the Parachute Creek Member.

Comparisons of well logs from the Sunnyside Tar Sands project and Rio Blanco Tract C-1 project show nearly identical doublet patterns of gamma rays near the base of the Parachute Creek Member (Figure 21, 1987 Report). This doublet pattern has the same characteristic peaks and troughs in the log

24

00962

pattern over many miles of separation. This widely recognized marker in the Sunnyside Tar Sands area is equivalent to the Blue Marker as used by Dyni (1967) and Ziemba (1974) within the Piceance Creek Basin.

The thin coal seam within the doublet pattern of the Blue Marker is so thin it has a poor well log response. Nevertheless, because of its nearly ubiquitos occurrence in drill core and measured sections, this thin coal seam has been selected as the finite, limit of the Blue Marker. Table 3 contains the Blue Marker data base used to make the Structure Contour Map of the Blue Marker (see Volume II) discussed under Geology of Project Area, Structure.

The thin coal seam of the Blue Marker was formed from a shoreline marsh deposited during the major transgressive event (i.e., expansion of Lake Uinta) in early Parachute Creek time. Five coal samples were submitted to Core Laboratories for vitrinite reflectance to determine the thermal maturity of coal within the Sunnyside Tar Sands area. The list of samples and results are as follows:

Vitrinite Sample Reflectance

outcrop: MS-50, Blue Marker 0.29* outcrop: Bruin Point road, Blue Marker 0.28* outcrop: MS-56, Blue Marker 0.26* core: A-65, -489 ft, above limestone 0.34

IFC 12 ft above base of Zone 33 (see strip log)

core: A-72, -881 ft, above ostracodal 0.47 packstone & 25 feet above Zone 33 (see strip log)

*Core Lab note: outcrop samples contain poorly preserved vitrinite. True vitrinite reflectance may be slightly higher.

These values of vitrinite reflectance are all less than 0.5; near the upper range of diagenesis; below the onset of oil generation at 0.6 for Type I (algal kerogens) and Type II (marine organic matter); and below the onset of gas generation at 0.7 for Type III (terrestrial organic matter, i.e., humus and coal) as discussed by Waples (1980) and Tissot and Welte (1978). Coal from an outcrop of the Blackhawk Fm. in Horse Canyon (some 7 miles southeast of Sunnyside) has a vitrinite reflectance of 0.58 (Nuccio and Johnson, 1988). The near surface coals in the Sunnyside and Bruin Point area have values of vitrinite reflectance that are below the onset of oil and gas generation.

00963 25

Garden Gulch Member

The Garden Gulch Member contains: (1) roughly forty percent of the tar sands; (2) the carbonate interval; and (3) an abundant fossil assemblage. The Garden Gulch Member represents a shore facies that formed in marginal lacustrine environments. This member is characterized by numerous bituminous sandstones, abundant fossiliferous limestones, massive poorly bedded greenish gray shales and thinly bedded mixed colored shales.

The carbonate interval is commonly seventy feet thick and can be divided into an upper, middle and lower part (see Figure 22). The upper part consists of the twenty-five foot thick Zone 25 that is ostracod-rich. The top of Zone 25 is characterized by a prominent gamma ray peak of 500-600 API units. The twenty foot thick middle part is dominated by light greenish gray shales that are partly bioturbated. The lower part consists of the twenty-five foot thick ostracod-rich Zone 26 and contains no prominent gamma ray peaks. Near the Roan Cliffs the carbonate interval is 50-60 feet thick. In the West Tavaputs Plateau the carbonate interval is 70-12 0 feet thick. The carbonate interval is a biostratigraphic unit and persists with good definition throughout the entire Sunnyside Tar Sands area. It can be used to determine stratigraphic position in both the surface and subsurface.

The limestones within the carbonate interval weather to a characteristic light brown (5YR hue-5/6chroma) to grayish orange (10YR-7/4) color and are recognizable from a distance. The term micrite is used for a carbonate mud, while the term biomicrite represents a carbonate mud with ten to seventy-five percent biota. The volume of limestones are about half micrite and half biomicrite. Limestone intervals commonly have the bio­micrite on top and the micrite on the bottom. The biomicrite contains intervals with abundant algal stromatolites and massive ostracod beds. Beds with more than seventy-five percent ostracods are coquina-like and represent grainstones. Some algal-rich beds are boundstones and consist of thin multiple algal laminae or thick masses of spherical algal heads. The flat laminated micrite zones are locally cracked, curled or buckled and form tepee-like structures. Tepee structures were classically interpreted to have formed in peritidal marine environments (Asserato and Kendall, 19 77).

The top of the carbonate interval, or top of Zone 25, is commonly located 250 feet below the Blue Marker (see Figure 22). No oil shales have been located with the Garden Gulch Member. The Orange Marker that exists below the Blue Marker in Figures 17 and 18 has not been recognized in the project area. The Orange Marker roughly correlates with the wide­spread Carbonate Marker of the Uinta Basin (Johnson, 1985,

26 00964

and Fouch, et al, 1976). In the Sunnyside Tar Sands area the Orange Marker and Carbonate Marker should be located at the top of Zone 25.

The Garden Gulch Member contains the most significant fossil assemblages within the Sunnyside delta complex. The limestones contain numerous intervals of ostracods, algal laminated sediments and algal heads. The most prominent algal head zone exists in MS-41 at the base of Zone 32 where a three foot interval with large algal heads are well-exposed along the jeep road that follows the crest of Whitmore Ridge. Black garpike fish scales and turtle bone fragments are common in local intervals of intraformational conglomerates (IFC's) found in basal portions of bituminous sandstones. Rare occurrences of gastropods, turtle plates and flora (mainly palm fronds and woody fragments) preferentially occur in the Garden Gulch Member.

Ostracods are the most abundant biota within the lime­stones of the carbonate interval and the limestones below the base of nearly every bituminous sandstone. Ostracods are abundant in sublittoral environments and commonly indicate paleoshorelines. Ostracods are microscopic benthic crustaceans that moult their bivalve shells eight times during their life­time and each time a larger carapace replaces the previous one (DeDeckker and Forester, 1988). In Zones 25 and 26 the largest ostracods are commonly 0.5-1.Omm in length and 0.25mm wide. Detailed examination with a ten power hand lens indicates there is a normal distribution of population sizes from juvenile to adult ostracods whose bivalves have remained mostly articulated. This type of population distribution indicates no winnowing or redistribution of shell sizes and suggests low energy conditions prevailed in both life and death assemblages (Whatley, 1988). Within Zones 25 and 26 numerous ostracod coquina beds are frequently 1-3 feet thick and almost wholly composed of ostracod shells. Aspects of moulting and population distribution make one realize that the ideal population is only a small fraction (i.e., 1/8) of the number of ostracod shells. The ostracod shell repre­sents a thick carapace of low Mg calcite that consists of a laminated chitin-protein complex; analysis of these shells and the Sr/Ca ratio can be used to determine paleosalinity and paleotemperatures (Neale, 1988). Ostracod populations are greatly affected by changes in water level (i.e., multiple transgressions and regressions of Lake Uinta), salinity, water composition and temperature (DeDeckker and Forester, 1988). Ostracods can be separated into marine, brackish and fresh water taxa. Swain (1964) has described six fresh water ostracod zones (plus a barren zone) within the Uinta and Piceance Creek basin. The barren zone commonly exists between the Mahogany oil shale and the Blue Marker. Within the Sunnyside Tar Sand area no ostracods are found within the Parachute Creek

27 00^65

Member. Within the Uinta Basin Hemicryprinotus watsonensis is the most abundant ostracod species and frequently forms coquinas several feet thick (Swain, 1964). Based on index photographs of catalogued ostracods, the ostracods in the coquina beds of Zones 25 and 26 are suggested to be Hemicryprinotus watsonensis. Knowledge of ostracod paleo-ecology leads to a better understanding of the cyclic deposition of limestones that occur below the base of numerous bituminous sandstones in the project area.

The colored shales associated with the Garden Gulch Member are distinctive. The abundant massive green shales have a distinct greenish gray (5GY 6/1) color and are readily apparent in the field. The greenish gray shales were deposited in shallow oxygenated waters. The mixed colored shales include shales of purple, olive gray, greenish gray and reddish brown colors and were deposited under alternating wet and dry condi­tions associated with shallow water environments. The colors formed during long time intervals after deposition. The Garden Gulch/Douglas Creek contact is transitional and characterized by green shales above, mixed colored shales in the thick transitional interval and red shales below.

The true thickness of the Garden Gulch Member depends on its location in the Sunnyside delta complex. Proximal portions near the Roan Cliffs are commonly 200-400 feet thick. Distal portions in the West Tavaputs Plateau near Dry Creek Canyon and South Ridge are commonly 600-800 feet thick.

Douglas Creek Member

The Douglas Creek Member contains the highest grades and most significant volumes of bituminous sandstones in the entire Sunnyside Tar Sands deposit. This member is characterized by multiple thick bituminous sandstones that outcrop along the Roan Cliffs and thin downdip toward the West Tavaputs Plateau. Approximately sixty percent of the tar sands in the entire Sunnyside delta complex are located within the Douglas Creek Member. This member represents the delta facies and is dominated by red shales and thick bituminous sandstones with thin limestones below their base.

The red shales and limestones within the Douglas Creek Member are important lithologic factors and help to define marsh and nearshore environments. Red shales coupled with carbonized and pyritized plant fragments help define the marsh environment. Thin coal lenses and rare log fragments exist within protions of this member and are exposed in the north pit of the Asphalt Mine. The coal formed in transitional

28

00966

areas between marsh and distributary channel environments. The limestones within the Douglas Creek Member consist of algal and ostracodal zones. The algal zones range from one to three feet thick with single algal heads one to two feet across. These thin but prominent algal stromatolite zones attest to minor lake transgressions within the Douglas Creek Member. Zones of ostracodal limestones one to five feet thick exist within all portions of the Douglas Creek Member. On the surface these ostracod zones have a white oolitic texture caused by combinations of wave agitation at the lake shore­line, carbonate overgrowths and weathering. Swain (196 4) noted that calcite overgrowths are present on some ostracod bivalves and form oolitic textures. The lower ostracod zones help to establish control on the lower limits of the Douglas Creek Member.

The Wasatch (Colton) Formation is stratigraphically below the Green River Formation (see Figures 9 and 10). The Wasatch Formation is used in areas that are not underlain by the Flagstaff Limestone (see Figures 10 and 12). The Wasatch Formation is of continental origin, and the Green River Formation is of lacustrine origin. The placement of the Green River/ Wasatch conformable contact differs among geologists. In the Sunnyside Tar Sands area Holmes, et al (194 8) placed this contact at the beginning of the red beds located at some 9600 feet in elevation near drill hole GN-3 and the top of MS-45 (Geology Map, Volume II). Many other geologists have followed the format of Holmes, et al (1948) and place the tar sands within the Wasatch Formation. I believe the contact near 9600 feet represents the Garden Gulch/Douglas Creek contact not the Green River/Wasatch contact. Murany (1964) states that ostracodal-oolitic limestones are a characteristic of the lower black shale facies and all limestones that outcrop in the Sunnyside Tar Sands area are part of the Green River Formation. Below the Asphalt Mine in Water Canyon various limestone units exist down to elevations of some 8400 feet. The limestones are of lacustrine origin and considered part of the Green River Formation. The Douglas Creek Member exists between elevations of 9600-8400 feet and is 1200 feet thick. The bituminous sandstones stop at about 8800 feet in the vicinity of the Asphalt Mine. The upper 8 00 feet of the Douglas Creek Member is bituminous and the lower 400 feet is nonbituminous. In the middle portions of Water Canyon exposures of the Wasatch Formation are roughly 800 feet thick and exist at elevations between 7600-8400 feet. In the eastern portion of the Uinta Basin at Raven Ridge (Figure 11) the Wasatch Formation is 850 feet thick (Murany, 1964).

All tar sands in the Bruin Point area are located within the Green River Formation and mainly confined to the upper half of the Douglas Creek Member and the Garden Gulch Member. In distal portions of the Sunnyside delta complex tar sands

29 00961

within the Douglas Creek Member are limited. In the West Tavaputs Plateau the Douglas Creek Member commonly exists below the base of saturation and thus contains only non-bituminous sandstones.

Sunnyside Delta Complex

The Sunnyside delta complex is a sequence of laterally continuous, vertically stacked bituminous sandstones alter­nating with red, green and gray shales. The system contains fluvial, deltaic, marsh, bay, beach and nearshore deposits that formed at the margin of ancient Lake Uinta. The delta system is well-exposed along the Roan Cliffs over heights of 500-1500 feet and for distances of 7-9 miles along depositional strike. The delta system is only partially exposed for distances of 2-5 miles along depositional dip within Range Creek and Dry Creek Canyon. These relationships are best seen on the Depositional Strike Section, Depositional Dip Section and the Tar Sand Isopach Map. The extensive exposures are considered to be unique and offer an excellent opportunity to examine a lacustrine delta complex. In 1986, 19 87 and 19 8 8 distal areas of the delta system were examined and this created a different perspective from early work in the proximal areas along the Roan Cliffs. During the 198 8 drilling season four drill holes were drilled in proximal portions of the delta, while eight drill holes were drilled in distal portions of the delta.

The arbitrary limits of the Sunnyside delta complex are confined to the distribution of tar sands and its boundaries are defined by tar sands with MSAT's totalling at least 50 feet. MSAT represents the total footage of main saturated zones that are at least ten feet thick and contain at least ten gallons of bitumen per ton. The numerous bituminous sandstone deposits represent distributary channel, distributary mouth bar and beach deposits that form relatively continuous sheets of bituminous sandstones. The lateral continuity of these sandstone deposits is caused by a combination of factors that include: (1) bifurcating distributary channel deposits, (2) shoaled distributary mouth bars and (3) reworking of the distributary mouth bars by waves and longshore currents to form beach and nearshore sandstone deposits.

The Sunnyside delta complex has been divided into three separate areas that include the Bruin Point, Dry Canyon and Whitmore Canyon subdeltas (see Tar Sand Isopach Map). The Sunnyside delta complex has been separated into these three subdeltas on the basis of field expression, lithology, tar sand distribution and environments of deposition. An under­standing of this delta complex and its subdeltas helps to comprehend the distribution of the tar sands.

30 009^8

The Sunnyside delta complex was formed in river-delta-beach-nearshore environments associated with the margins of Lake Uinta during Eocene time some 58-45 million years ago. The shoreline or depositional strike is parallel to the Roan Cliffs and oriented N40-50 W. Various grades of tar sands are distributed parallel to the ancient shoreline over distances of seven to nine miles. The tar sands are distributed along depositional dip for distances of two to five miles. Exposures along depositional dip are limited but exist along Dry Canyon ridge and in Dry Canyon.

During its development the Sunnyside delta complex experienced two major prograding phases, one major trans-gressive phase and multiple minor regressions (low lake-level stage) and transgressions (high lake-level stage). The first major prograding phase occurred in Douglas Creek time when massive volumes of fine grained sand slowly prograded into Lake Uinta; this phase was largely confined to the Bruin Point subdelta. The second major prograding phase occurred during Garden Gulch time when massive volumes of fine grained sand again slowly prograded into Lake Uinta; this phase was largely confined to the Dry Canyon and Whitmore Canyon sub-deltas. The major transgressive phase occurred during Parachute Creek time when Lake Uinta continued to grow in size and advanced over the entire Sunnyside delta complex.

Numerous minor transgressions and regressions formed cyclic deposition throughout the history of the Sunnyside delta complex. At least eleven to fifteen minor cycles exist and consist of repeated cycles of sandstone-shale-limestone-unconformity sequences. Each cycle has a combined thickness of some fifty to one hundred-fifty feet. Each cycle begins with sandstone deposition, is followed by shale deposition, then limestone deposition and ends with an unconformity. From sandstone to shale to limestone each cycle represents a fining upward sequence. The sandstones and shales are relatively thick units, while the limestones are thin units. The sandstone-shale and shale-limestone contacts are normally gradational but can be abrupt. A relatively flat unconformity (erosion surface) exists on top of the limestone units. The sandstones formed during relatively wet conditions, and the limestones formed during relatively dry conditions. These repeated cycles formed from alternating wet and dry climatic cycles and re­sulted in multi-stacked lithologic sequences in the vicinity of Bruin Point. The overall lithology of the Sunnyside delta complex based on 47,418 feet of Amoco drill core is: 33.1% sandstone; 10.6% siltstone; 47.9% shale; 6.8% limestone; 1.5% conglomerate; and trace amounts of volcanic tuffs (see Table 4).

0096§

31

The relative stratigraphic position of sandstones suggests that the Bruin Point subdelta is the oldest and the Whitmore Canyon subdelta is the youngest. Within the Bruin Point sub-delta the tar sands are largely confined to the Douglas Creek Member. Within the Dry Canyon and the Whitmore Canyon sub-deltas the tar sands are largely confined to the Garden Gulch Member. The Tar Sand Isopach Map indicates a dominant northwest trend of the bituminous sandstones with the thickest concentra­tions in the vicinity of Bruin Point. This northwest trend parallels the ancient shoreline and represents depositional strike. The main drainage that formed the delta complex flowed northeast and represents the direction of depositional dip.

Bruin Point Subdelta

The Bruin Point subdelta is characterized by four to fifteen zones of bituminous sandstones with consistently high bitumen content and intervening red shales. The Bruin Point subdelta represents the primary center of deposition within the Sunnyside delta complex. The thickest tar sand accumulations in the Sunnyside delta complex exist near Bruin Point (see Tar Sand Isopach Map). Large areas of cumulative MSAT's (main saturated zones) up to 300-700 feet thick are localized in the area of Bruin Point to Range Creek. The Bruin Point subdelta was the area of principal investigation in 1978, 1980, 1981 and part of 1988. Twenty measured sections have been completed in proximal, medial and distal portions of the Bruin Point subdelta. Thirty-three of sixty deep Amoco drill holes have been completed in the Bruin Point subdelta. The tar sands are localized within a nine hundred foot thick zone near the Roan Cliff face that thins over a distance of two miles to a two hundred foot thick zone in the vicinity of Range Creek (see Depositional Dip Section). The Bruin Point subdelta contains about seventy percent of the total mineable tar sands within the entire Sunnyside delta complex. The tar sands are associated with distributary channels, distributary mouth bars and beach-bar deposits (see Figure 13).

The Bruin Point subdelta has a large arcuate or lobate shape as seen on the Tar Sand Isopach Map. The cause of this lobate shape is suggested to be from extensive sediment influx and partial modification by waves in the shore margin of Lake Uinta. The Bruin Point subdelta is considered to be fifty to seventy-five percent fluvial-dominated and twenty-five to fifty percent wave-influenced.

The overall lithology of the Bruin Point subdelta based on 30,49 7 feet of Amoco drill core is: 30.7% sandstone; 11.0% siltstone; 50.5% shale, 6.7% limestone; 1.5% conglomerate;

32 ootf°

and trace amounts of volcanic tuffs (see Table 4). The siltstones and conglomerates are commonly associated with the sandstones. If the lithology is tabulated by delta, shore and lake facies, changes in the percent sandstone, shale, limestone and siltstone-conglomerate are dramatic as listed below:

Lithology Delta Shore Lake

%SS 53.8 24.9 6.7 %SH 27.9 52.5 83.7 %LS 1.6 11.0 2.3

%SL & %CG 16.7 11.6 7.1

The sandstone content decreases rapidly from delta to shore to lake. The shale content increases rapidly from delta to shore to lake. Limestone content increases significantly in shore environments. The siltstone-conglomerate content decreases gradually from delta to shore to lake.

Dry Canyon Subdelta

The Dry Canyon subdelta is characterized by three to seven zones of bituminous sandstone with consistently high bitumen content and intervening green shales. The Dry Canyon subdelta represents the secondary center of deposition within the Sunnyside delta complex. The Dry Canyon subdelta contains elongated areas of cumulative MSAT's up to 200-400 feet thick (see Tar Sand Isopach Map). The Dry Canyon subdelta was the principal area of investigation in 1982, 1984, 1986 and 1987. Thirty measured sections have been completed in proximal, medial and distal portions of the Dry Canyon sub-delta. Twenty-seven of sixty deep Amoco drill holes have been completed in the Dry Canyon subdelta. The major tar sands are localized within a four hundred foot thick zone on the Roan Cliff face that thins downdip over a distance of one mile to a two hundred foot thick zone beneath the Dry Canyon ridge road. This subdelta contains about thirty percent of the total mineable tar sands within the entire Sunnyside delta complex. The tar sands are primarily contained within distributary channels, distributary mouth bars and beach bar deposits (see Figure 14).

The Dry Canyon subdelta is a fluvial-dominated elongated delta system as suggested by the three mile long Dry Canyon distributary-like ridge that extends northeast from the Arco water tank. The elongated type delta system is characterized by fluvial dominance and weak wave energy. Within the well-dissected Dry Canyon subdelta much of the present topographic expression is an expression of paleogeomorphology. Present topographic ridges and bulges are underlain by tar sands as determined by both field work and drill hole information.

33 oo9n

The overall lithology of the Dry Canyon subdelta based on 16,291 feet of Amoco drill core is: 37.3% sandstone; 9.8% siltstone; 44.1% shale; 7.1% limestone; 1.7% conglomerate; and trace amounts of volcanic tuffs (see Table 4). If the lithology is tabulated by delta, shore and lake facies changes in percent sandstone, shale, limestone and siltstone-conglomerate are significant as listed below:

Lithology Delta Shore Lake

%SS 36.1 40.4 8.6 %SH 44.2 40.6 84.7 %LS 3.3 8.2 0.5

%SL & %CG 16.4 11.2 5.9

Only limited differences in lithology content exist between delta and shore facies with the exception of percent limestone. Dramatic differences in lithology content exist from shore to lake facies.

The Dry Canyon and Bruin Point subdeltas have different configurations (see Tar Sand Isopach Map). They are adjacent to each other and interfinger near their transitional boundary in the "NOL" and "Lazy L" areas. Near this transi­tional boundary of the Bruin Point and Dry Canyon subdeltas there is an abrupt four hundred foot change in elevation at 20,000 NW to 22,000 NW (see Regional Map). Within the Dry Canyon subdelta the Parachute Creek Member has been completely eroded away along the Roan Cliffs with the exception of the Mt. Bartles area (see Geology Map). Within the Bruin Point subdelta the Parachute Creek Member is commonly 100-300 feet thick. The lithology of the Dry Canyon and Bruin Point subdeltas is listed in Table 4 and can easily be compared. The differences are biased by no data from the eroded Parachute Creek Member in the Dry Canyon subdelta. If only the Garden Gulch Member is examined, the lithologic differences between the Dry Canyon and Bruin Point subdeltas are more pronounced as listed below:

Garden Gulch Member

Lithology Dry Canyon Bruin Point Subdelta Subdelta

SS% 40.0 24.9 SH% 40.6 52.5 LS% 8.2 11.0

Within the Dry Canyon subdelta the Garden Gulch Member has a sixty percent increase in sandstone content and a twenty-three percent decrease in shale content. This indicates

34 o o ^ *

that the amount of sandstone deposition increased during Garden Gulch time in the vicinity of the Dry Canyon subdelta. It also indicates that the lateral accumulation of sandstone occurred in a northwest direction from the Bruin Point sub-delta to the Dry Canyon subdelta and that the Dry Canyon subdelta is younger than the Bruin Point subdelta.

Whitmore Canyon Subdelta

The Whitmore Canyon subdelta is characterized by four to six zones of bituminous sandstones of variable bitumen content and intervening mixed colored shales. The Whitmore Canyon subdelta represents the wanning stages of deltaic deposi­tion within the Sunnyside delta complex. Nine of fifty-nine measured sections have been completed within proximal, medial and distal portions of the Whitmore Canyon subdelta. Limited information from twelve drill holes of GNC and Mono Power are available and listed on the Regional Map. The core has not been examined for Amoco. The area contains a major tar sand strip 2-3 miles long by 1000-2000 feet wide (see Tar Sand Isopach Map). This elongated strip contains cumulative MSAT's up to 100-200 feet thick. No mine model data on mineable tar sands exists within this subdelta. This subdelta is suggested to contain some five percent of the total tar sands within the entire Sunnyside delta complex. The principal portion of the tar sands are localized in the Garden Gulch Member. The Parachute Creek Member has been eroded away except in distal portions northeast of Mt. Bartles.

The Whitmore Canyon subdelta represents a lower delta plain to delta fringe sequence of distributary channel, distributary mouth bar, and beach deposits dominated by intervening mixed color shales and algal-ostracodal limestones formed in interdistributary bays. Red shales of the lower delta plain environments exist near the oil/water contact shown on the extreme left side of the Geology Map in sections 2 3 and 14 of T13S, R13E.

Shales

Red, green, gray and mixed colored shales have been utilized in field mapping to help distinguish the three separate members of the Green River Formation. The red shales are a characteristic feature of the Douglas Creek Member. The green shales are a characteristic feature of the Garden Gulch Member. The mixed colored shales are transitional to both the Garden Gulch and Douglas Creek members. The gray shales are a characteristic feature of

35 00913

the Parachute Creek Member. These four types of shales repre­sent almost half the rocks in the area (see Table 4).

The most obvious feature of any shale is its color, and these colors are the best guide for stratigraphic subdivision and correlation of shales (Potter, Maynard and Pryor (1980)). Shale color or pigmentation is controlled by the oxidation state of iron and carbon content. The color of shales can be separated into two trends as summarized from Potter, Maynard and Pryor (19 80), Braunagel and Stanley (19 77), McBride (1974) :

Trend I:

GREENISH GRAY grades to PURPLE grades to RED

increasing Fe and decreasing free iron

>

2 + decreasing Fe and decreasing carbon content

>

Trend II:

GREENISH GRAY grades to GRAY grades to BLACK

increasing carbon content

The oxidation state of iron has a controlling influence on the color of the shales as determined by MacCarthy (1926). Purely ferric colors are red, orange and yellow. Purely ferrous colors are blue or colorless. Purple colors are mixtures of reds and blues. Green colors are mixtures of blues and yellows:

"Red and purple rocks owe their color to pervasive hematite grain coatings and crystals intergrown with clay; brown rocks owe their color to faint or localized iron-oxide grain coatings; and gray rocks to organic matter and authigenic iron sulfide. Green rocks owe their color to chlorite and illite and to the absence of hematite, organic matter and sulfides. Olive and yellow claystone colors are imparted by color mixing of green clay and black organic matter." (McBride, 1974, p. 760).

36 009" 4

The greenish gray color of the two shale color trends is represented by the 5GY (hue) - 6/1 (chroma) color designation of the Geological Society of America rock color chart (Goddard, et al, 1963). Based on field relationships and information from the literature the red, green, mixed colored and gray shales within the Sunnyside delta complex are inter­preted to represent distinct environmental conditions.

The greenish gray shales of the Garden Gulch Member are one of its most characteristic features and have the same color designation (5GY-6/1) as noted in the two shale color trends. Both micrites and biomicrites are associated with the green shales. The green shales readily crumble to form small cube-like fragments. Turtle fossils are found within the green shales of the Garden Gulch Member and indicate burial before the bone material was completely oxidized. The green shales of the Garden Gulch Member are calcareous and were deposited in shallow water environments under moderate oxygenated conditions in nearshore margins of Lake Uinta. Dirt roads containing green shales remain well-drained even after considerable precipitation.

The mixed colored shales are characteristic of transitional environments associated with both the Garden Gulch and Douglas Creek Members. These mixed colored shales contain different proportions of red, green, olive, yellow, brown and purple colors. The purple color represents grayish red purple with a rock color designation of 5RP-4/2. These mixed colored shales are calcareous and were deposited in interdistributary bays and inlets or lagoons that experienced alternate wetting and drying. This resulted in complex reducing and oxidizing conditions that formed the variegated colors.

The red shales of the Douglas Creek Member are grayish red (5R-4/2 to 10R-4/2) to dark reddish brown (10R-3/4). The red shales are slightly more resistant to weathering than the green shales. Dirt roads containing red shales do not drain well and often are slippery. The red shales are non-calcareous and were deposited in marsh environments under dominantly oxidizing conditions. Thin discontinuous pods/ seams/seamlets of coal are localized within the red shales of the Douglas Creek Member. The small to moderate volumes of green shales that exist beneath the massive sandstones in the north and south pits of the Asphalt Mine probably formed as the result of groundwater seepage from the overlying sand­stones. This groundwater seepage forms green shales from red shales by reduction of the ferric iron content.

The gray shales of the Parachute Creek Member are light olive gray with a 5Y-7/2 to 5Y-5/2 rock color designation. Oil shales are associated with these gray colored shales.

Catfish-like and herring-like fish fossils are found within the dinner plate oil shale of the Blue Marker at the base of the Parachute Creek Member. The gray shales were deposited in shallow to moderate water depths under low to very low oxygenated conditions. Dirt roads containing gray shales are extremely slippery after significant wetting and create mobility problems for all vehicles. The gray shales of the Parachute Creek Member commonly contain an extensive vertical fracture system that hinders core recovery and water return during drilling operations. Water associated with this vertical fracture system and oil shale zones causes local springs such as North Spring, South Spring and Stone Cabin Spring. Artesian flow in drill holes is very rare and has occurred only in Amoco No. 2, 14 and 17.

Additional supporting evidence on the color of shales and their environmental interpretation exists from China, England, Louisiana and Mexico. In northeast China a middle Cretaceous lacustrine delta complex formed in the Songliao basin. As described by Shice and Hengjian (1981), red shales developed mainly in the floor plain facies; gray and green shales developed mainly in the deltaic distributary plain; grayish black shales developed mainly in the delta front facies; and black shales developed mainly in the semi-deep to deep lake facies. In England the greenish gray (5GY-6/1) to olive gray (5Y-4/1) clays of the Cretaceous Weald Clay of south­eastern England were deposited in shallow oxygenated brackish water marine environments; ostracods are commonly associated with the greenish gray (5GY-4/1) or light olive gray (5Y-6/1) clay as noted by MacDougall and Prentice (1964) . In Louisiana within the modern Mississippi River delta color laminations are considered to be the result of alternate wetting and drying of muds deposited in brackish and saline marshes (Saxena, 1976). In northeastern Mexico near Monterrey and Saltillo late Cretaceous to Paleocene delta plain deposits are characterized by an eighty percent abundance of red beds. Green colored shales often underlie massive sandstone beds; groundwater seepage out of these overlying massive sandstone beds formed the green colored shales by reduction of the ferric iron content in red shales (McBride, 1974). Red to purple colors develop in delta plain facies and gray colors develop in prodelta and shelf facies. Development of color within sediments is a post-depositional feature requiring hundreds to thousands of years (McBride, 1974).

Carbonates

Carbonates represent a significant and repeated minor lithologic component of the Sunnyside delta complex (see Table 4). Almost seven percent of all the rocks in the delta complex are carbonates (limestones and dolomites). Limestones are the most prevalant carbonate. Thin limestones

38 QO^S

two to five feet thick commonly exist at the eroded top of each lithologic sequence containing sandstone-shale-limestone. Limestones exist within all three members of the Green River Formation but are most abundant within Zones 25 and 26 of the Garden Gulch Member.

The relatively thin carbonates consist of micrites and biomicrites. Thin intervals of laminated algal mats often cap micrite intervals. The biomicrites contain laminated algal mats, algal stromatolites, ostracods, turtle fragments, fish scales and biota trash. The biota-rich biomicrites represent grainstones (ostracod coquina) or boundstones (algal mats and algal stromatolites). Ostracod coquinas are more abundant and laterally persistant than zones of algal mats or algal stromatolites. In this lacustrine delta complex ostracods are by far the most abundant fossil fauna, while blue-green algal types are by far the most abundant fossil flora. Local intervals of whole and broken algal stromatolites with cabbage head-like shapes are well exposed in the upper portion of MS-41 and the lower portion of MS-3. Cycles of carbonate deposition are five to fifteen feet thick with a range of one to thirty feet. Thin intercalated shales often exist within the thicker carbonate intervals.

Sedimentary structures associated with the carbonates include small scale trough cross bedding, planar bedding, mudcracks and tepee structures. The latter are localized within algal laminated beds or the upper portions of micrites. These small pseudo-anticlinal features have cross sections that look like American Indian tents, hence the name tepee. Buckling of carbonate sediments forms the tepee structure and is caused by expansion of carbonate-rich material. The expansion is the result of carbonate crystallization and cementation processes associated with repeated drying and wetting conditions that persist in peritidal areas of lagoonal and back-barrier environments (Assereto and Kendall, 1977). Tepee structures were recorded in MS-38 and MS-44, which are both located in the Whitmore Canyon subdelta. These tepee structures formed within lacustrine carbonate mud flats that experienced subaerial exposure.

Field examples indicate the presence of minor cycles of carbonate deposition. When two types of limestones are present there commonly is a lower micrite interval overlain by a biomicrite interval as in MS-51 below Zone 32 at -210' and -220'. A six foot cyclic interval of micrite-biomicrite-micrite-biomicrite exists in MS-56 below Zone 23. These minor cyclic sequences are evident within some carbonates and indicate rhythmic changes associated with fluctuating lake levels during semi-arid conditions. In MS-47 Zone 26 contains a five foot thick basal micrite, a five foot thick biomicrite in the middle and a one foot thick algal-rich limestone at the top.

This eleven foot thick interval is interpreted as a shallowing upward cycle and developed under conditions that changed from nearshore to shoreline to lagoonal marsh and were caused by a lowering of the lake level. In MS-56 at the top of the Garden Gulch Member there is a seven foot thick micrite-rich interval that contains (1) a six inch thick brown to black shale with plant debris and (2) thin coal seamlets (1.0" and 0.5" thick) at the base and in the middle. The presence of coal with carbonates indicates that lagoonal type vegetation existed during periods of carbonate deposition.

40

009^

TAR SANDS

Over ninety-five percent of the bitumen in the Sunnyside delta complex is associated with porous and permeable sand­stones. These reservoir rocks are separated into sheet sands and channel sands. The fifteen major bituminous zones have designated numbers (see Figures 13 and 14) and are largely confined to the Douglas Creek and Garden Gulch Members. These numbers were established in 1982 and determined on the basis of downhole gamma ray logs. Surface gamma ray logs have been used since 1986 to determine the outcrops of numbered tar zones along measured sections. The bituminous sandstones are remarkably uniform in texture, grain size and mineral composition. The bituminous sandstones are well sorted, fine to very fine grained and dominated by grains of quartz and feldspars. Both the sheet sands and channel sands contain less than five percent silt and clay.

Maps and Sections

Tar Sand Isopach Map

The Tar Sand Isopach Map (see Volume II) shows three distinct factors about the Sunnyside Tar Sands deposit. First, the thickest portion of the tar sands exist near Bruin Point in the western segment of the flexure. These tar sands are concentrated in areas updip from the main axis of the Mt. Bartles-Bruin Point flexure and located in the highest topographic areas. Tar sands in the central segment are diminished in extent and concentration. Tar sands in the eastern segment are even further diminished in extent and concentration. Second, the tar sands are concentrated within a long and narrow northwest trending belt. This long seven to nine mile belt corresponds to the depositional strike of the sediments, while the narrow one to four mile wide portion corresponds to the depositional dip. Most of the major (400-700 MSAT) and minor (100-400 MSAT) tar sands are confined to this long narrow belt. Four small areas of minor tar sands exist along the ridge tops in the Whitmore Canyon subdelta area. Two isolated areas of minor tar sands exist east of the main axis of the flexure. Areas of limited (0-100 MSAT) tar sands exist adjacent to areas of minor tar sands. Third, in the subsurface a CC^-rich gas zone exists above the base of the tar sands in the area between Range Creek and Bruin Point outlined on the Tar Sand Isopach Map. These gases are commonly entrapped in weak to poorly saturated sands slightly above the barren sands. These gases average (N=2) 98.5% C02, 1.4% CO, 0.04% methane and 0.06% other gases with no detectable H-S.

009^

41

Depositional Dip Section

The Depositional Dip Section (see Volume II) illustrates: (1) the distribution of the numbered tar zones and stratigraphic units; and (2) the Mt. Bartles-Bruin Point flexure system is divided into a western, central and eastern segment.

(1) In the Sunnyside Tar Sands deposit numbered tar zones were established by use of geophysical and geological data. Gamma ray well logs, frequency and thickness of intercepts in drill holes and assay data were compiled on a hole by hole basis by John Rozelle. Initially some thirty-five specific tar sand intervals were defined. These intervals were then correlated with detailed lithology and depositional environments of core logs to establish numbered tar zones. From this investigation fifteen tar zones were selected and represent the major mineable tar zones. These tar zones were numbered according to their stratigraphic position by a two digit number code. The first digit applies to the member (i.e., 1 for Tgp, 2 for Tgg and 3 and 4 for Tgd) and the second digit applies to its vertical position with number 1 at the highest elevation. These major numbered tar zones include Zones 11, 21, 23, 25, 26, 31, 33, 35, 36, 37, 38, 41, 42, 43, 45. Zones 25 and 26 are bituminous limestones and all the other zones are bituminous sandstones. When the gamma ray well log, density well log, lithology and environ­ments of deposition are used in combination, numbered tar zones can be determined for the drill core data.

(2) The Mt. Bartles-Bruin Point flexure has been divided into three segments. The western segment contains the vast majority of the tar sands that are concentrated in a wedge shaped area. Here the tar sands occur as thick rich (7-12wt% bitumen) tar zones that average about fifty feet thick (range 10-180 feet). In the central segment the tar sands are thin (10-20 feet thick) and of moderate grade (4-7wt% bitumen). In the eastern segment the tar sands are thin (10-20 feet) and of low grade (0-4wt% bitumen). The sixty foot carbonate-rich interval is persistent within the western, central and eastern segments and represents an important regional stratigraphic interval. Important marker beds (Wavy Bedded Tuff, R-7 oil shale, R-5 oil shale, and the Blue Marker) exist within the eastern central and western segments of the flexure.

Depositional Strike Section

Depositional Strike Section (see Volume II) illustrates the extent and shape of the Sunnyside Tar Sands deposit. The distribution of the tar sands has been separated into north,

42 00980

central and south areas. The north area contains the Dry Canyon subdelta. The central area contains the thickest portion of tar sands and is part of the Bruin Point sub-delta. The south area is part of the Bruin Point subdelta and encompasses the newly named South Knoll region within the Sunnyside Municipal Watershed.

The major tar sands are contained within an area 1200 feet deep in the center x 100 feet deep on the sides x 33,000 feet long. The bowl shape of the tar sands deposit is apparent by the curvature of the base of saturation that is near 8800 feet at the Asphalt Mine, near 9400 feet at Mount Bartles, and near 9 80 0 on Patmos Ridge. The 70 foot carbonate-rich interval exists throughout the Roan Cliff face except where removed by erosion. The vast majority of the tar sands exist below the carbonate-rich interval.

The irregular changes in dip of the tar zones on the section are only apparent and caused by the irregular line of section. In the central portion the dips are relatively uniform as this part of the section is nearly parallel to depositional strike. In the south portion the line of section is about forty-five degrees to the depositional strike. The zig-zag nature of the line of section (i.e., this fence diagram) causes local distortions. The apparent anticline from Mt. Bartles to USGS Bruin does not exist as determined by the Structure Contour Map of Blue Marker and discussed under Geology of Project Area, Structure. The 6 3 foot thick collivium at drill hole RCT-14 is highly anomalous and exists in the saddle that separates the central area from the south area. This saddle may be associated with a secondary northeast trending fault.

Base of Saturation Map

The nearly horizontal base of saturation slopes at an average rate of 30 ft/1000 ft, while the beds dip at an average rate of 120 ft/1000 ft. This difference in slope causes the base of saturation to rise downdip relative to the numbered tar zones. The Base of Saturation Map (see Volume II) shows two distinct factors.

First, a basic dip slope ramp contains a large central swale. This large central swale is three miles long and two miles wide. This area of the central swale coincides with the vast majority of the tar sands as seen by overlaying the Base of Saturation Map on the Tar Sand Isopach Map. The northeast portion of this swale is associated with the main axis of the flexure (see Geology Map) and the change in strike of the Blue Marker (see Structure Contour Map).

43 009^

Second, the swale contains two areas of local depressions. A northwest depression area contains two adjacent depressions that collectively are four thousand feet long by two thousand feet wide. This collective northwest depression is associated with the area of thickest tar sands below Bruin Point, USGS Bruin and the favorite lunch spot. A southeast depression is some thirty-five hundred feet long by one thousand feet wide and is one to three hundred feet lower in elevation than the collective northwest depression. This southeast depression is near the structural intersection of the mapped Mt. Bartles-Bruin Point flexure in Range Creek and the unmapped cross fault in the saddle at drill hole RCT-14. This southeast depression is at a structural intersection and may be part of a conduit system which serves as an avenue for emplacement of oil which was later degraded to bitumen. Oil analysis by the Amoco Laboratories at Tulsa indicate the oil in the Sunnyside Tar Sands deposit is of Tertiary origin and contains no bimodal Cretaceous oil.

Sheet Sands and Channel Sands

The geometry in outcrops indicates the tar sands can be separated into sheet sands and channel sands. The channel sands represent some twenty-five percent of the bituminous sandstones and are preferentially found in the lower part of the tar sands package. The sheet sands represent some seventy-five percent of the bituminous sandstones and are preferentially found in the upper part of the tar sands package.

The sheet sands, as the name implies, are relatively thin laterally continuous sand bodies. The sheet sands frequently rest unconformably on limestones. The sheet sands are tens of feet thick with an average thickness of 30-40 feet. The dominant sheet-like nature of the bituminous sandstone is well-illustrated in Photos 3 and 4, 1987 Report. The sheet sands are laterally continuous for hundreds to thousands of feet as determined by drill holes at spacings of 1000-1500 feet and measured sections at spacings of 1000-3000 feet.

The channel sands have a distinct basal scour and contain a thick central body of sandstone that may abruptly terminate laterally or extend as thin lateral wings of sandstone. The channel sands have 5-50 foot deep basal scours with 5-15 feet as a common range. The most extensive mapped basal scour of 48 feet is associated with Zone 35 in MS-3. The channel sands are tens to a few hundreds of feet thick with an average thickness approaching 70-80 feet. The channel sands contain numerous stacked sets of sandstone intervals. Clay plugs and swales are not common in the channel sands but a shale-filled swale is well-exposed in the north pit of the Asphalt

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Mine. Some channel sands cut into delta plain sediments (north pit of the Asphalt Mine and on the road to Bruin Point near the 9000 foot elevation contour below the major switchback at drill hole location GN-4). Some channel sands cut into the lacustrine shoreline sediments (MS-3, Zone 35). The channel sands often grade laterally into sheet sands.

The geometry of the sandstone reservoirs is critical to the evaluation of the Sunnyside Tar Sands project. The Roan Cliffs represent a stacked sequence of shorelines from ancient Lake Uinta. Channel sands are more dominant landward of the shoreline, and sheet sands are more prevalent lakeward of the shoreline. In the immediate vicinity of the shoreline the sheet sands and channel sands merge and the sheet-like nature dominates. The major tar sands are concentrated in the immediate vicinity of the ancient shorelines over distances of 7-9 miles along depositional strike and over distances of 1000-10,000 feet along depositional dip (see Tar Sand Isopach Map, Depositional Dip Section and Depositional Strike Section, Volume II).

The lateral continuity of the numbered tar zones along depositional strike is pronounced with minimal thickening and thinning (see Depositional Strike Section). The lateral con­tinuity of the numbered tar zones along depositional dip shows marked thinning in a downdip direction. The individual numbered tar zones are commonly 40-150 feet thick in the proximal portions of the Roan Cliffs and commonly 10-30 feet thick in the distal portions east of Range Creek. The thinning of tar sands from proximal to medial areas is seventy percent. The thinning of tar sands from medial to distal areas is eighty-five percent. This pronounced thinning of tar sands toward the Uinta Basin is apparent from the Tar Sand Isopach Map and in the Depositional Dip Section.

Depositional Environments

Field studies indicate that the bituminous sandstones formed in four principal environments of deposition: distributary channels (DC); distributary mouth bars (DMB); beaches (B) and beach-bar (BB) deposits. The characteristics of the different rock types in the Sunnyside Tar Sands area are summarized in Table 5. The determination of these four environments of sandstone deposition is based on many factors that include: (1) vertically and laterally adjacent shales and carbonates; (2) vertical sequence of sedimentary structures within the sandstones; (3) types and position of lag deposits; (4) minor vertical changes in sandstone grain size; and (5) associated biota (flora and fauna).

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Item (1): shales and carbonates. The color of the adjacent shale is indicative of particular environments such as gray (lake), green (nearshore), red (marsh) or mixed color (bay). The laterally or vertically adjacent shales and lacustrine carbonates bracket the sandstone location and serve as a guide to determination of sandstone depositional environments. The sandstones frequently exist unconformably above a partially eroded 2-10 foot thick limestone interval and indicate pro-gradation of sands across subaerially exposed carbonate mud flats or nearshore environments. In some locations the middle portions of certain massive sandstone bodies contain isolated internal limestone pods (2-5 feet long x 1 foot thick) or disseminated concentrations of 5-20% ostracods. These internal complexities indicate aqueous conditions and suggest DMB environments.

Item (2): sedimentary structures. A characteristic pattern of sedimentary structures is indicative of channel, mouth bar or beach deposition. This and minor occurrences of bioturbation are discussed in more detail separately.

Item (3): lag deposits. The types and position of lag deposits is a helpful guide in determining sandstone depositional environments and is discussed in more detail separately.

Item (4): grain size. The fine to very fine grain size of the tar sands is so uniformly consistent that megascopic differences in grain size are difficult to ascertain in the field even with a ten-power hand lens. Grain size changes within the bituminous sandstones and resulting fining upward or coarsening upward cycles are not well defined.

Item (5): associated biota. The presence of biota trash is a helpful criteria for a beach (B) deposit. Plants and wood fragments are rare but helpful criteria for deposits of distributary channels (DC). Disseminations of ostracods within tar sands are helpful criteria for a B, BB or DMB deposits.

Sedimentary Structures

The dominant sedimentary structures in the tar sands include trough cross bedding, horizontal (planar) bedding and ripple laminations. Planar cross bedding is usually limited and often represents a phase of trough cross bedding due to the angle of view. Distorted/contorted bedding caused by liquefaction in water saturated sediments exists in portions of massive sandstone units. Hummocky cross stratification is rare in the Roan Cliffs but has been observed a number of times in the West Tavaputs Plateau. Epsilon cross bedding

46

is essentially absent. The vertical succession of sedimentary structures or bedforms is a significant criteria to help determine sandstone depositional environments.

During the deposition of sand the sedimentary structures that form reflect the bedforms that develop during two types of flow regimes. The lower flow regime is characterized by tranquil to low flow, and the sand grains are influenced primarily by forces of gravity and secondarily by forces of inertia. The tranquil or lower flow regime is characterized by bedforms of plane beds that form without water movement, ripples, dunes and transitions to rapid flow bedforms. The upper flow regime is characterized by turbulent to high flow and the sand grains are influenced primarily by forces of inertia and secondarily by forces of gravity. The rapid, turbulent or upper flow regime is characterized by plane beds that form with water movement, standing sand waves and antidunes. The median grain size in the Sunnyside tar sands is 0.20mm. Bedforms of the lower flow regime dominate the Sunnyside tar sands.

During the deposition the vertical sequence of sedimentary structures represents the bedforms that develop during rela­tively decreasing or relatively increasing flow regime con­ditions. At the Sunnyside Tar Sands area the most prevalent vertical sequence of sedimentary structures is basal scour -> trough cross bedding -> planar bedding -> ripple laminations. The DC deposits are characterized by a basal scour, trough cross bedding in the lower portion, planar bedding in the middle and ripple laminations in the upper portion. The second most prevalent vertical sequence of sedimentary structures is basal planar bedding -> trough cross bedding. B and BB deposits are dominated by trough cross bedding near the base and horizontal (planar) bedding at the top. The DMB deposits contain the most complex and variable sets of sedimentary structures but are dominated by trough cross bedding and planar bedding as well as limited bedforms caused by liquefaction.

Hummocky cross stratification is a bedform associated with storm waves. In July or August of 19 87 a major storm on Great Salt Lake caused eight to ten foot waves and waves of these heights or greater do occur on other large lakes. In the Great Lakes high winds cause storm surges that represent an abnormal sudden rise of the lake level; these storm surges average about 1.7 feet and range from 0.47-4.7 feet (Murty and Polavarapu, 1975). Storm waves and storm surges existed in ancient Lake Uinta and help to explain the presence of hummocky cross stratification in sandstones.

0

47

The average paleocurrents flowed northeast. Eighty-eight paleocurrent measurements by Banks (1981) have a vector re­sultant of N45 E with the main grouping between N30-60°E. The second grouping is between N60-90°E. The third grouping is between N to N60°W.

Epsilon bedding is well-recognized as a characteristic feature of a channel meander belt and is formed by lateral accretion of point bars. The Sunnyside Tar Sand area lacks any significant volumes of epsilon cross bedding, and upward increases of silt and shale partings or drapes are not characteristic of the bituminous sandstones.

Diagnostic sequences of sedimentary structures are helpful criteria in the evaluation of sandstone depositional environments but are not solely unique to a single or specific environment. The classical vertical sequence of point bars formed at river bends in meandering streams is trough cross bedding -»• horizontal bedding -»• ripple laminations (Visher, 1965 and Stear, 1983) or channel floor erosion and lag deposits -»- plane beds -»- large ripples -»- small ripples -»• overbank flooding (Allen, 1963). These point bar systems often contain fully developed fining upward sequences of sedimentary structures. The vertical sequence of estuary (that part of a river affected by tides) deposits progress from lag deposits to predominantly crossbedded deposits to predominantly horizontally bedded deposits at the top. Klein (1963) noted that the vertical sequence of sedimentary structures in channel deposits and estuarine deposits is essentially the same and that the only major difference is in the type of basal lag deposit.

Three types of minor occurrences of bioturbation (churning of sediments by organisms) are found within sediments of the Sunnyside delta complex and are usually of a weak to moderate intensity. The three types of burrows occur within the bioturbated intervals and include: (1) deformed; (2) small size; and (3) moderate size. (1) The deformed burrows are only associated with oil shale intervals in the Parachute Creek Member, were made in a soupy mud and later deformed or distorted by soft sediment deformation. The majority of these deformed burrows are of a vertical nature, while a minority is of a horizontal nature. Jordan (1985, p. 228, photo D) has an excellent photo that depicts this type of deformed bioturbation. (2) the small size burrows (X = 0.1" D, range 0.05-0.2" D) are vertical and associated with greenish gray and mixed colored shales in_the Garden Gulch Member. (3) the moderate size burrows (X = 0.25, range 0.2-0.5" D) are vertical and associated with siltstones and some sandstones in the Garden Gulch and Douglas Creek Members.

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Lag Deposits

The numerous intraformational conglomerates (IFC's) that are frequently associated with the Sunnyside Tar Sands represent lag deposits. IFC's commonly occur at or near the base but also occur within middle portions of some tar sands. These IFC's contain rip-up clasts from nearby or adjacent environments and represent intrabasinal clasts. Extrabasinal clasts of igneous and metamorphic rock fragments are not megascopically present. The composition of these IFC's is shale-rich; limestone-rich; biota-rich (fish scales, ostracods, turtle bone fragments or algal stromatolites); or combinations of these three.

The composition of the lag deposit is an important factor in the interpretation of sandstone depositional environments. Klein (1967) noted that tidal channel deposits are almost exclusively floored by shell lag deposits; estuarine channels are floored by a mixture of shell lag and clay chips; and fluvial channels are floored by gravel, clay pebbles and logs. The most common lag deposits in the Sunnyside Tar Sands area are mixtures of shale, shale-limestone-biota and limestone-biota. These latter two mixtures are similar to those of estuarine channels but may also represent shore lag deposits formed by storm surges, storm waves and transgressive high stand lake levels. Microtides probably existed in ancient Lake Uinta with normal magnitudes of 2-4 inches. Microtides can be a minor factor in the development of lag deposits. Microtidal data for large lakes has not been found in the literature. Lake Michigan supposedly has microtides in the range of 3-4 inches.

Textures

Grain size, shape and sorting of the individual sand-size particles were determined from thin sections by Banks (19 81) and Remy (19 84). The grain size of the bituminous sandstones is relatively uniform from tar zone to tar zone. The average grain size based on sixty-one samples is:

18% medium sand (0.5-0.25mm or 500-250 microns) 54% fine sand (0.25-0.125mm or 250-125 microns) 23% very fine sand (0.125-0.0625mm or 125-62 microns) 5% silt and clay (<0.0625mm or <62 microns)

100s

No reliable standard grain size analyses are available within the bituminous sandstones to determine vertical changes in grain size (i.e., fining upward or coarsening upward). The common cylinder shape of the gamma ray well logs within ^

49

sandstones also suggests uniform grain size. In outcrop the relatively uniform megascopic grain size masks any definite upward fining or coarsening upward sequence. Nevertheless, a subtle upward fining trend is suggested to exist within the bituminous sandstones near the Roan Cliffs. Coarsening upward trends within the tar sands are rarely apparent but exist in the West Tavaputs Plateau. The overall sandstone-shale-limestone cycles certainly indicate a fining upward sequence.

The degree of sorting based on fifty-five surface samples of Banks (1981) is: 37% well sorted, 53% moderately well sorted, 2% moderately sorted and 8% poorly sorted. The distribution of grain shapes based on fifty-five surface samples of Banks (1981) is:

shape

angular subangular subrounded rounded well rounded

fine sand

39% 29% 19% 10% 3%

very fine sand

49% 26% 16% 7% 2%

100% 100%

The bituminous sandstones have an average porosity of 27% and average permeability of 812 millidarcys. Minor amounts of bitumen are localized in less porous and less permeable siltstones and limestones. The bituminous silt-stones have an average porosity of 22% and an average per­meability of 64md. The bituminous limestones have an average porosity of 18% and an average permeability of one millidarcy. These average values were obtained from numerous determinations by Core Labs.

Mineral Composition

The Sunnyside bituminous sandstones are feldspathic arenites as determined by petrographic studies of Banks (1981) and Remy (1984). The detailed results of thin section investigations are listed in Table 6 and indicate the following compositions: 70% major framework grains; 3% minor framework grains; 7% cement and matrix; and 20% voids (porosity and/or bitumen).

The major framework grains represent 70% of the sand­stones and consist of 33% quartz, 29% feldspars and 8% rock fragments. The feldspars consist of 17% plagioclase and 12% K-feldspar (orthoclase 9%, microcline 3%). All the

50 V

9%%

feldspar grains are partially weathered and have undergone some degree of in-situ dissolution. This weakened state coupled with the multiple pronounced feldspar cleavages makes all the feldspar grains (29% of the rock) highly susceptible to mechanical breakdown by grinding. The natural "fines" content of these bituminous sandstones is 5% (i.e., silt and clay sized particles less than 62 microns). But the "fines" content can easily be increased to 20% by grinding.

The minor framework grains represent 3% of the sandstones and consist of 9.5% mica, 0.4% accessory minerals and 2.1% allochems. Mica is a principal minor framework mineral. The mica group consists of 75% muscovite, 20% biotite and 5% chlorite (Remy, 1984) . Medium to fine grained muscovite is the only readily distinguishable megascopic minor framework mineral and has been used as a partial guide to help distinguish DC deposits (<1% muscovite) from DMB deposits (1-3% muscovite). Commonly the muscovite is crinkled. Thin section work by Remy (1984) indicates this crinkled texture is caused by compaction.

The cementing agents for the bituminous sandstones consist of roughly 1% calcite, 2% dolomite and 2% hematite. The 3.8% hematite cement in surface samples of Banks (1981) is much higher than the 1.0% of hematite in core samples of Remy (19 84) and reflects the oxidation differences between the surface and subsurface samples. Detailed petrographic work by Remy (1984) indicates that carbonate cements are the most abundant cement in all sandstones, make up 3.2% of the rock and consist of 1.2% calcite and 2% iron-rich dolomites. Calcite cement is more abundant in the beach to beach bar deposits. Iron-rich dolomite cement is more abundant in the distributary mouth bar and distributary channel deposits. Muller, et al (1977) state that within lake deposits calcite is a primary carbonate and dolomite is a secondary carbonate. In the Sunnyside Tar Sands area carbonate grains are localized within beach to beach-bar sandstone deposits and contain an average of 6.4% ostracods, 5.8% carbonate intraclasts and trace oolites (Remy, 19 84). Carbonate grains are not common in distributary channel and distributary mouth bar deposits.

The bituminous sandstones of the Green River Formation in the southern margins of the Uinta Basin are of a feldspathic petrofacies while those at Raven Ridge in the northern margins of the Uinta Basin are of a quartzolithic petrofacies (Dickinson, Lawton and Inman, 19 86) . The feldspar-rich bituminous sandstones of Sunnyside and P.R. Spring (Figure 11) were derived from a source area to the south in the Uncompahgre Uplift. The quartz-rich bituminous sandstones of Raven Ridge were derived from a source area to the north in the Uinta Mountains. The tar sands at Whiterocks and Asphalt Ridge (Figure 11) do not exist within the Green River Formation.

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Interpretation

In the Sunnyside delta complex the bituminous sandstones can readily be separated into sheet sands and channel sands on the basis of basal scour and sheet-like geometry. Separa­tion of sheet sands and channel sands into specific sandstone depositional environments is more difficult and more subjective. The rocks of this lacustrine delta complex contain a multiplicity of sedimentology characteristics. Based on specific multiple criteria the sandstone depositional environments are interpreted to represent distributary channels (DC), distributary mouth bars (DMB) and beach (B) to beach bar (BB) deposits. The specific multiple criteria are based on sedimentary structures, biota and lithology that have developed while logging core and measuring sections. Grain size is not a diagnostic feature as all the sandstones are megascopically similar. Distributary channels (DC) and beach (B) to beach bar deposits (BB) can be considered as the two end members with distributary mouth bars (DMB) transitional to both.

Distributary channels (DC) are distinguished by the following criteria: basal scours; channel lag deposits or IFC's (intraformational conglomerates) with nonbituminous shale and siltstone intraclasts; sedimentary structures that are largely trough cross bedding at the base and planar bedded at the top; one percent muscovite content; no or very limited bioturbation; and an association with red shales. D C s are shoestring-like with abrupt lateral changes and are often 30-250 feet thick. D C s are more prevalent in the basal portions of the tar sands.

Distributary mouth bars (DMB) are distinguished by the following criteria: basal and internal IFC's with limestone intraclasts including transported algal stromatolites; sedimentary structures that include flip-flops of either planar beds or trough cross bedding at the base and the other at the top; an upward fining sequence of sedimentary structures with trough cross bedding -*• horizontal bedding -*• ripple laminations; high concentrations of 2-3% muscovite and muscovite laminae; internal distorted bedding caused by liquefaction; local rich bitumen content that is sap-like and often oozes from outcrops with southern exposures; nontransported internal limestone pods; local fish scales; occasional zones a few inches thick with numerous ostracods in a sand matrix; bioturbation near the top; and an association with green or mixed colored shales. DMB's range in thickness from some 30-220 feet and are abundant in the middle portion of the tar sands. In MS-54 Zones 37 and 38 have a combined thickness of 222 feet and represent continuous deposition associated with a DMB.

52 00«*°

Beach (B) to beach bar (BB) deposits are distinguished by the following criteria: predominance of planar bedding with some trough cross bedding; algal limestones unconformably below the base; thin internal biota trash zones; nearby mud-cracks; adjacent green, gray or mixed colored shales. These deposits are thin laterally continuous sheets often 5-15 feet thick. B to BB deposits represent a continuum of the sub-aerial beach to subaqueous shoreface to nearshore and deposits. In addition the beach bar deposits may grade laterally into shoaled areas of distributary mouth bar deposits. B and BB deposits are more prevalent in the upper portions of the tar sands and distal portions of the delta complex.

A lacustrine delta complex existed in the Bruin Point area during Green River time and was determined from the following criteria: gray, green, red and mixed colored shales; cyclic sequences of sandstone-shale-limestone-unconformity; textural and biological compositional features of the carbonates; distribution and thickness of sandstones; types of lag deposits; sedimentary structures; textures; and mineral composition. The sandstones were deposited as distributary channels, distributary mouth bars and beach to beach bar deposits in areas near the lake shoreline.

A key task in regard to the numbered tar zones is to determine the sandstone geometry and establish the environment of deposition. Where is this tar sand outcrop located relative to land, shoreline or lake in Green River time? Answers to this question help in the continuing evaluation of the bituminous sandstones. The interpretation of field data is enhanced by application of thoughts of other authors. "The most favorable environmental setting for oil-productive sheet sandstones is marginal marine" (Campbell, 1976, p. 1018). This quotation may be applied to the Sunnyside Tar Sands area by using marginal lacustrine instead of marginal marine. The principal of lateral migration or accumulation is one of the single most important concepts associated with deltaic sandstone deposition (Weimer, 1976). Sheet sands as described by Stear (1983) are products of lateral channel migration and the bulk of sedimentary structures include trough cross bedding and horizontal bedding. Lateral migration is a significant factor in the development of sheet sands in the Sunnyside Tar Sands area. Dean and Fouch (1983) show some excellent colored photographs of lacustrine environments. In their Figure 66, which is located in Nine Mile Canyon of the West Tavaputs Plateau, channel-formed sandstones overlie and locally scour stromatolitic algal boundstone; fluvial deposits exist on top of a carbonate complex that formed in shallow waters of Lake Uinta. Similar cycles of deposition are frequently apparent in the Sunnyside delta complex.

53 Q0^ V

Field and literature studies indicate that the deposi-tional environments of the Athabasca Oil Sands are distinctly different than those of the Sunnyside Tar Sands. The Athabasca Oil Sands were formed from a mega-scale meandering channel deposit near an estuary and are characterized by a consistent vertical sequence of sedimentary structures in four distinct facies associated with the McMurray Formation. As described by Mossop (19 80), Mossop and Flach (19 82 and 1983) and Flach (1984) these four distinct facies from bottom to top are: (1) a locally developed basal scour with lag deposits 0-30 feet thick; (2) a lower member of thick bedded sand 3-24 meters thick with trough cross bedding; (3) a 17-22 meter thick middle member with thick sets of solitary epsilon cross strata. The epsilon cross strata are very large scale uniformly dipping planar-like beds with average dips of 10-12 degrees; and (4) a 15 meter thick upper member with horizontal bedding. The key characteristics of a meandering channel deposit as stated by Mossop and Flach (1982, p. 12) are a well defined scour base; upward fining in the sand fraction with an upward increase in the proportion of shale; diminishing flow regime upward in the sequence; and unidirectional paleocurrents essentially parallel to the strike of the epsilon cross strata. The fining upward trend of grain size in the oil sands was determined by standard grain size analysis and is due largely to an upward increase in the proportion of silt and shale partings associated with clay drapes (Mossop and Flach, 19 82).

54 oft*

DRILL HOLE AND MEASURED SECTION SYNTHESIS

Since 1980 over 47,000 feet of drill core has been logged and almost 44,000 feet of measured sections have been completed. This combination of outcrop and drill core studies has been an indispensable aid in defining the geology and numbered tar zones in the project area. Field work associated with measured sections in peripheral areas has located the Mt. Bartles-Bruin Point segmented flexure. Both field work and drill core in peripheral areas has established important markers within the Parachute Creek Member. The important markers are the Wavy Bedded Tuff, Mahogany oil shale, Blue Marker and carbonate interval. These important markers permit distinct correlations to be made with the established geological framework of the Uinta Basin shown in Figure 12.

Repeated cycles of sandstone ->- shale ->- limestone ->- erosion exist in all drill holes and measured sections. These cycles end with an unconformity at the top of a limestone interval. Next a sandstone interval is deposited which grades upward into a shale interval that in turn grades upward into a limestone interval which is followed by another erosion interval. Then the sandstone-shale-limestone-erosion cycle is repeated. At least fifteen major and eleven minor cycles of these repeated intervals exist in the Sunnyside Tar Sands area. The explanation for these repeated cycles is either structural or climatic. Structural evidence of intermittent and repeated uplift is not evident. The repetition of these sandstone-shale-limestone-erosion cycles is caused by climatic cycles. Influxes of sand are associated with wet conditions and high lake levels. The limestones developed during dry conditions and low lake levels. Milankovitch climatic cycles of roughly 100,000, 40,000 and 20,000 years are caused by changes in the earth's orbital geometry (Berger, A., et al, 1984 and Hays, et al, 1976). Milankovitch climatic cycles are the most probable cause of the repeated sandstone-shale-limestone-erosion cycles that exist within the Green River Formation of Eocene age. The terminal Eocene event was a major decrease in temperature of 10-12 C within one to two million years (Wolfe, 1978). For the Bruin Point area paleolatitudes of 23-30 N are inferred from flora evidence of MacGinitie (1969), while maps by Habicht (1979) indicate paleolatitudes near 40 N.

Drill Hole Data

Over 47,000 feet of drill core has been logged during five drilling seasons, and preservation of this data is important for continued synthesis and mine model studies. Data from these yearly records has been used to determine i\C^^

55

7268 9208 11720 7364

11858 47418 feet

the lithology of the Sunnyside Tar Sands area (see Table 4). The yearly totals of the five drilling seasons are tabulated below:

Year Drill Holes Total Footage

1980 1,4,8-11* 19 81 12,13,14,16,17,21,22,24,26** 1982 31-48*** 1984 49-54 and 60-63**** 1988 64-72 and CD-I,2,3

Notes: * drill holes 2,3,5-7 were drilled by Amoco Production in 1978 and not included

** drill holes 15,18,20,23,(25=geotechnical) are shallow pilot mine holes in the central area and not included

*** drill holes 27-30 are shallow pilot mine holes in the central area and not included

**** drill holes 55-59 are shallow pilot mine holes in the north area and not included

The location of all drill holes is shown on both the Regional Map and Geology Map. General data on the saturation, elevations and depths of all drill holes is tabulated on the Regional Map. Specific data on numbered tar zones from all project drill holes has been carefully updated and compiled for reference in Tables 8 and 9.

1988 Drilling Program

Twelve core drill holes totaling 11,858 feet were com­pleted in two geographically separated areas. Near Bruin Point (central and south areas) nine holes totaled 9858 feet. Near Mt. Bartles three holes totaled 2000 feet. These drill hole locations are shown in Figure 3.

After BLM permission was granted the drilling program proceeded with the following sequence: site-preparation by a dozer; drilling operations by Boyles Bros.; stopping the drill hole in nonbituminous sandstones below the base of saturation; well log analysis by BPB Instruments; plugging of the holes by Boyles Bros, with "holeplug" (graded bentonite rock chips from NL Baroid); surveying of the drill holes by Intermountain Technical Services; and site reclamation by Jerry Jensen.

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« « * •

The drilling operations started on June 20 and terminated on October 14 with two Longyear 44 rigs and one Longyear 34 rig. Boyles Bros, completed 11858 feet of drilling in 198 drilling days for an average of 60 ft/day per rig with a range of 0-210 ft/ten hour shift. Core recovery averaged 98.1% for the entire 11858 feet with a range of 94.6 to 99.8% per hole. The drill foreman, Tony Robinson, completed seven drill holes and sixty-three percent of all drilled footage. All drill holes are NX size and 2.9 80 inches in diameter. Four different types of bits were used and include the Chris, Geoset, 5 per carat diamond, and tungsten carbide. The Chris bit was the most effective as it permits greater water circulation at the cutting surface.

Lithology logs at a scale of 1"=10 ft were carefully made from the core of each drill hole in the core shack located in Price. Core logging proceeded at an average rate of 267 feet per day. Later these lithology logs were condensed to form strip logs at a scale of 1"=50 ft. The strip logs for all twelve holes are found in Volume III. Summary data from all 19 88 drill holes is listed in Table 1A and IB. The status of all 1988 drill holes is listed in Table 2.

Highlights of 1988 Drill Hole Strip Logs

The strip logs represent a synthesis and quick look at the geological data available from each drill hole. The strip logs illustrate the vertical position of the numbered tar zones along with their bitumen content as well as various lithologic data. After completion of the strip logs the highlights or salient observations were recorded at the base of each strip log. For convenience the highlights of each drill hole strip log are listed below.

CD-I Highlights

1. TSAT 52' DSAT 453' or 8242 ft elevation MSAT 19' BSAT >500' TD 500'

2. Hole has one MSAT within first 500 ft. Zone 22 is 19 ft thick, exists between depths of 453-472 ft and contains 11.3 gpt.

3. The Mahogany zone (R-7), R-5, and the Blue Marker (R-2) at the base of the Parachute are well developed.

4. Oil shale zones R-2 through R-7 all exist. Their location is based on stratigraphic position and gamma ray well log correlation.

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Zones R-7 (23 ft thick), upper 23 ft of R-5 and R-2 (3 ft thick) are well defined on gamma ray well logs.

5. The lower tuff exists but the upper tuff (Wavy Bedded Tuff) was reworked and locally dispersed by shallow lake processes.

CD-2 Highlights

1. TSAT 20 ft DSAT >500' or <8358 ft elevation MSAT -0- BSAT >500' TD 500'

2. No significant tar sands or MSAT's were encountered.

3. The three important markers within the Parachute Creek Member (i.e., Wavy Bedded Tuff, Mahogany zone and Blue Marker) all exist within this hole.

4. This hole illustrates the stratigraphic position and thickness of oil shale zones R-2 through R-8, and the stratigraphic position of both the upper tuff (Wavy Bedded Tuff) and the lower tuff.

5. Algal stromatolites, soft sediment deforma­tion and thin coal seamlets are sometimes associated with oil shales.

CD-3 Highlights

1. TSAT 273' DSAT 376' or 8692 ft elevation MSAT 35' BSAT >1000' TD 1000'

2. This hole contains only two thin MSAT's. Zone 21 is 13 ft thick (375-388 ft deep) and averages 16 gpt. Zone 22 is 22 ft thick (438-460 ft deep) and averages 13 gpt.

3. The deep tar sands contain less than 10 gpt and minor amounts of CO_ gas.

4. Two of the three important markers within the Parachute Creek Member (i.e., Mahogany zone and Blue Marker) exist within the drill core. The Wavy Bedded Tuff outcrops near the drill collar.

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5. This hole illustrates the stratigraphic posi­tion and thickness of oil shale zones R-2 through R-8 and the stratigraphic position of both the upper (i.e., Wavy Bedded Tuff) and lower tuff.

6. The oil shale content increases with the intensity of the brown color as described in the R-5 oil shale zone and determined from the GSA rock color chart.

7. Zones 25 and 26 encompass about 75 ft, are important biostratigraphic units and defined by multiple ostracod-rich intervals. The top of Zone 25 is about 250 ft below the Blue Marker and has a gamma ray well log kick of 610 API units.

A-64 Highlights

1. TSAT 180' DSAT 293' or 9560' MSAT 40.5' BSAT 1121' or 8732' TD 1179'

2. Hole has only two thin MSAT's. Zone 10 is 9.5 ft thick with 18.2 gpt from 293.1-302.6 ft. Zone 31 is 15 ft thick with 21.8 gpt from 916-931 ft.

3. All oil shale intervals from R-2 through R-8 are expressed within this hole, especially R-8, R-7, R-5 and R-2.

4. Blue Marker with 0.5" coal seam is well expressed in core and on gamma ray well log.

5. Wavy Bedded Tuff is 20.5 inches thick.

6. Zones 25 and 26 encompass about 7 5 ft, are important biostratigraphic units and defined by multiple ostracod-rich intervals. The top of Zone 25 is about 240 ft below the Blue Marker and has a gamma ray well log kick of 570 API units.

A-65 Highlights

1. TSAT 754' DSAT 410' or elevation 9694 ft MSAT 588' BSAT 1272' or elevation 8832 ft TD 2365'

2. Drill hole bridged at 740' and dry. Gamma ray log to 740' only well log available. Density log could not be completed as caliper arms stuck in hole twice when extended. 00997

59

3. Drill hole located at junction of Bruin Point and Dry Canyon subdeltas.

4. Fourteen MSAT's - bitumen content mean 16.7 gpt (range 12-21.6 gpt).

5. Increased percentage of carbonates in lower Tgp near Bruin Point suggesting shoaled area.

6. Four foot thick Blue Marker with 0.5" coal seam well expressed.

7. Zones 25 and 26 are important ostracod-rich biostratigraphic units, i.e., biozones. They encompass 55 ft and are located about 225 ft below the Blue Marker. The top of Zone 25 has a gamma ray kick of 570 API units.

A-66 Highlights

1. TSAT 203' DSAT 408' or 8407' elevation MSAT 29' BSAT 818 or 7997' elevation TD 849'

2. Only two thin MSAT's are present. Zone 22 is 18.2 ft thick from 407.5-425.7 ft and contains 18.6 gpt, while Zone 23 is 10.6 ft thick from 457.7-468.3 ft and contains 15.0 gpt. Tar zone 11 is 33.5 ft thick from 205.5-239 ft but contains only 9.5 gpt.

3. Oil shale zones R-2 (7 ft thick) and R-5 (22 ft thick) are well developed, while oil shale zones R-3 (3.5 ft thick) and R-4 (5.5 ft thick) are poorly developed.

4. Based on associated mudcracks; low relief (1-3" high) algal stromatolites; coal seams in R-2; and thin marlstone intraformational conglomerates (storm lag deposits); the oil shales formed in relatively shallow water lacustrine environments.

5. The ostracod-rich biostratigraphic units in Zones 25 and 26 encompass about 7 5 ft. The top of Zone 25 is marked by a gamma ray well log kick of 275 API units.

A-67 Highlights

1. TSAT 280' DSAT 418' or 9718 ft MSAT 192' BSAT 718' or 9000 ft TD 749'

2. The six MSAT's are divisible into upper (Zones 21 and 22), middle (Zones 31,32 and 33) and lower (Zone 36) groups. The upper group contains tar zones 21 and 22 between depths of 171-235 ft with bitumen values of 12.4-15.6 gpt. The middle group contains portions of three separate MSAT's (31,32 and 33) that total 82 feet and average 22 gpt (range 21.7-23.3 gpt). The lower group contains tar zone 36 from 682-718 ft that averages 19.6 gpt, however, this same zone from 692-718 ft averages 22.3 gpt.

3. The Blue Marker at the base of the Parachute is well defined with a 4.8 ft oil shale interval (R-2) and a 0.5" coal seam at a depth of 136 ft or 9582 ft in elevation.

4. Zones 25 and 26 represent important biostrati-graphic units, encompass about 55 ft, and are located about 225 ft below the Blue Marker. The top of Zone 25 has a gamma ray well log kick of 570 API units.

A-68 Highlights

1. TSAT 291' DSAT 615' or 9078 ft MSAT 153' BSAT 1210' or 8483 ft TD 1236'

2. Ostracod-rich Zones 25 and 26 represent important regional biostratigraphic units that encompass about 55 ft and are located about 320 ft below the Blue Marker.

3. Three marginal MSAT's occur above Zones 25 and 26, while three marginal MSAT's occur below Zones 25 and 26.

4. With two exceptions the hole contains six marginal MSAT's that are commonly thin (12-23 ft thick) and contain only 12-15 gpt. First, a twelve foot interval of Zone 22 (690-702) contains 20 gpt. Second, Zone 35 contains a 73 ft interval (1105-1178) that averages 13 gpt.

5. All oil shale intervals R-0 through R-8 are present with the exception of R-3.

6. Oil shale often exists immediately above sandstone as observed within three oil shale intervals (i.e., base of R-8, R-7 and R-4).

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7. The Wavy Bedded Tuff is 19" thick and represents an excellent marker bed of time-stratigraphic importance.

8. In the Parachute the only biota are low relief algal stromatolites.

9. In the Garden Gulch the dominant biota are ostracods with minor amounts algal stromatolites of moderate relief, gar-pike fish scales and turtle bone fragments.

A-69 Highlights

1. TSAT 575' DSAT 178' or 9512 ft MSAT 276' BSAT >1169' or <8521 ft TD 1169'

2. Major tar sands can be categorized into four groups based on bitumen content. The single most important group (Zones 35 and 36) exists from 672-801 ft and contains one massive tar sand interval with values of 8-12wt% bitumen (i.e., 129 ft averaging 22.4 gpt). The second most important group contains four separate tar zones (23, 31, 32 and 33) between depths of 250-575 ft with bitumen values of 15-18 gpt. The third group contains two separate tar zones (21 and 22) between depths of 175-225 ft with bitumen values of 10-14 gpt. The fourth and least important group contains four separate tar zones (37, 38, 41 and 42) between depths of 900-1169 ft with bitumen values near 9 gpt and some associated C0_ gas.

3. Below 890 ft the tar zones contain discrete specks of hydrocarbons with visual estimates of l-2wt% bitumen. Analysis by Core Labs indicates 3-4wt% bitumen.

4. Base of saturation not reached in this hole but at least near or below 8500 ft in elevation. This is 500 ft below BSAT of 9000 ft in Amoco-67 located about 1000 ft to the southeast; and also 300 ft below base of saturation at 8800 ft in tar sand mine some 9000 ft to the northwest.

5. Vertical fractures are common within drill hole and highly anomalous in four intervals (635-643; 860-862; 914-920; 1067-1074).

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6. Items 3-5 suggest this anomalous hole is associated with a conduit system.

7. Blue Marker is well-defined (4.5 ft thick with 0.5" coal seam at 121 ft).

8. Zones 25 and 26 represent important bio-stratigraphic units, encompass about 60 ft and are located about 2 30 ft below the Blue Marker.

A-70 Highlights

1. TSAT 577* DSAT 357' or 9210 ft MSAT 374' BSAT 1085' or 8482 ft TD 1099'

2. The numerous major tar zones or MSAT"s can be divided into upper, middle and lower groups based on bitumen content and vertical position. The upper group exists above the carbonate-rich Zones 25 and 26 and contains tar zones 22 and 23 with bitumen values near 13 gpt. The middle group exists between depths of 350-660 ft and contains tar zones 31, 32 and 33, 34 and 35; tar zones 31 and 34 have bitumen values near 15 gpt, while tar zones 32 and 33 and 35 have bitumen values near 19 gpt. The lower group contains tar zones 36, 37, 38, 41 and 42 with bitumen values between 10-13 gpt with associated CO- gases.

3. Ostracod-rich Zones 25 and 26 represent important biostratigraphic units of regional extent and encompass about 55 ft.

4. Base of saturation in this hole is at 8482 ft and 200 feet lower than BSAT of 8682 ft in Amoco No. 10 located about 110 0 ft northwest. Amoco No. 13 is located about 1100 ft northeast and has a BSAT of 8647 ft. The base of satura­tion in Amoco No. 70 is anomalously deep by about 200 ft.

A-71 Highlights

1. TSAT 245' DSAT 633' or 8946* elevation MSAT 128' BSAT 1185 or 8 399' elevation TD 1239'

2. Three tar zones (21, 22, 24) exist above Zones 25 and 26 at depths between 630-870 ft and contain 16-19 gpt. Three tar zones

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(31, 32, 33) exist below Zones 25 and 26 at depths between 940-1140 ft and contain 12-16 gpt.

3. The top of Zone 25 was eroded off and the high gamma ray kick near 6 00 API units that normally exists is absent, but a small kick of 250 API units exists.

4. Oil shale zones R-8, R-7, R-5 and R-2 are well developed, while oil shale zones R-4 and R-3 are poorly developed. Oil shale zone R-6 is absent, as usual.

5. Zones of oil shale are often immediately above sandstone/siltstone intervals as seen at the base of R-8, R-7 and R-4.

6. Algal mats and algal stromatolites of low relief are internally associated with oil shale intervals, and the oil shales represent algal derived kerogen.

7. Algal structures, plant fragments and abundant thin 1-2" IFC's suggest the algal kerogen formed in shallow to shoaled lacustrine areas.

A-72 Highlights

1. TSAT 185' DSAT 759' or 8732 ft elevation MSAT 26' BSAT 968' or 8523 ft elevation TD 1009'

2. Hole contains one true MSAT (tar sands at least 10 feet thick and containing at least 10 gpt). This is Zone 31 which is 26 ft thick (759-785 ft deep) and contains 18.0 gpt. Two other tar sand intervals are not true MSAT's. Zone 21 is 9.4 ft thick (439.6-449 ft deep) and contains 10 gpt; Zone 33 is 17.3 ft thick (905.7-923 ft deep) and contains 9.7 gpt.

3. Within the Parachute Creek Member oil shale zones R-2, R-5, R-7 and R-8 are well developed. Oil shale zones R-3 and R-4 are poorly developed. Oil shale zone R-6 is absent.

4. There are numerous examples of oil shale within and adjacent (i.e., interbedded) to algal stromatolites.

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5. Below the Mahogany Zone (R-7) the 30-35 ft thick sandstone/siltstone/shale unit is equivalent to the Brown Cliff in outcrop. At the surface the overlying Mahogany Ledge commonly outcrops as an oil shale doublet of paper shales.

6. Within the Parachute Creek Member both an upper and lower tuff bed exist. The upper tuff bed is a formal unit and represents the Wavy Bedded Tuff.

7. Seven designated intervals (one 9 ft void; three highly fractured; one highly slickensided; one moderately fractured; one with limonite fractures near 700 ft deep) attest to the presence of a major structure in the vicinity of Range Creek.

8. Zones 25 and 26 encompass about 60 ft and represent important biostratigraphic zones. The top of Zone 25 is about 245 ft below the Blue Marker.

Measured Section Data

Almost 44,000 feet of measured sections have been completed during seven field seasons. This outcrop informa­tion has been vital to the geological interpretation of the Sunnyside Tar Sands deposit. The yearly total of completed measured sections is listed below:

Year Measured Section Vertical Height

1980 1981 1982 1984 1986 1987 1988

1- 6 7-11

12-17 18-26 27-44 45-56 57-59

6437 4105 3930 6966

12365 8391 1533

43727 feet

The cumulative thickness of MSAT's (main saturated zones) differs within different portions of the Sunnyside delta complex. The locations of all measured sections were categorized by proximal, medial and distal positions within the Bruin Point, Dry Canyon and Whitmore Canyon subdeltas. Proximal portions are within ±0.5 miles of the Roan Cliff

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face. Medial portions are within 0.5-1.5 miles downdip of the Roan Cliff face. Distal portions are 1.5-4 miles downdip of the Roan Cliff face. Totals of cumulative MSAT thickness by proximal, medial and distal position are listed below:

Cumulative MSAT Thickness

Subdelta Proximal Medial Distal

Bruin Point 342 109 39 Dry Canyon 231 81 6 Whitmore Canyon 122 21 0

This data shows dramatic differences of bitumen content. Clearly the proximal portions of the subdeltas near the Roan Cliffs contain the thickest accumulations of saturated sandstones. The decreases from proximal to medial to distal are pronounced. The Bruin Point subdelta contains the largest volumes of saturated sandstones. The Dry Canyon subdelta contains about thirty percent less than the Bruin Point subdelta. The Whitmore Canyon subdelta contains almost sixty-five percent less than the Bruin Point subdelta. The proximal, medial and distal positions of the Bruin Point and Dry Canyon subdeltas roughly correspond, respectively, to the western, central and eastern segments of the flexure. The proximal deltaic position and the western segment of the flexure clearly have the highest concentrations of bitumen (see Tar Sand Isopach Map); and both factors are important for the distribution of bituminous sands within the Sunnyside Tar Sands deposit.

Thickness values of numbered tar zones within proximal, medial and distal portions of three subdeltas are listed below:

Average Thickness of Numbered Tar Zones

Subdelta Proximal Medial Distal

Bruin Point 43 27 22 Dry Canyon 44 23 17 Whitmore Canyon 30 25 17

This data indicates definite thinning of the numbered tar zones from proximal to medial to distal portions of the subdeltas.

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Highlights of 1988 Measured Section Strip Logs

After the completion of each measured section field high­lights were noted. After completion of the strip log these field highlights and other salient data were recorded at the bottom of each strip log (see Volume III). For convenience these highlights are listed below.

MS-57 Highlights

1. TSAT 163' DSAT 986' or 8709 ft elevation MSAT 79' BSAT >1046' or >8649 ft elevation VH 1049'

2. Parachute Creek Member is 540 ft thick with no MSAT's.

3. Five tar zones but only three true MSAT's that total 58 ft as determined from analysis of surface composite samples 57-1, 57-5, 57-6, and 57-7. MSAT of 79' by averaging high

and moderate bitumen values.

4. Located three markers

a) dinner plate oil shale of Blue Marker b) Mahogany Ledge above Brown Cliff c) Wavy Bedded Tuff

5. Vertical distance between base of Mahogany and dinner plate oil shale about 300 ft.

6. MS-57 replaced MS-Range Creek I completed by E.A. Ziemba of Pan Am, 1964.

MS-58 Highlights

1. No tar sands in this 355 ft section that exists mainly in the Parachute Creek Member.

2. Located the Blue Marker and the lower portion of the Mahogany Ledge.

3. About 250 ft between the base of the Mahogany and the Blue Marker.

MS-59 Highlights

19 86 purpose: establish Tgp/Tgg contact and effectiveness of surface gamma ray instrument to define Blue Marker.

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1988 purpose: illustrate abundance of carbonate near base of Tgp in immediate area of Bruin Point.

1. The Blue Marker is well defined by the out­crop lithology and surface gamma ray log. The 0.5" coal seam (located 1.5 ft below the dinner plate oil shale) has been noted throughout the project area.

2. There is a high percentage of carbonates that formed in a shoaled area near Bruin Point. The presence of algal mats, algal stromatolites, tepee-like structures and mudcracks help to define shallow water environments during early Parachute Creek time.

3. This measured section is at the top of the road to Bruin Point and encompasses 129 vertical feet. The lower 111 feet were completed in 1986 and the upper 18 feet were completed in 1988.

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WELL LOGS

Whenever possible three well logs were run on each drill hole to obtain data for identification and correlation. The three logs include gairana-density-caliper, focused electric and multi-channel sonic. Attempts to complete the three logs were dependent on downhole conditions and fluid levels. The gamma-density-caliper log can be made in either air or fluid filled holes. But the focused electric and multi-channel sonic logs must have fluid in the hole for the sonde to function. The gamma log has proved to be the most beneficial log for geological investigations within the Sunnyside Tar Sands deposit. A summary of the correlation of typical well log responses and core samples is listed in Table 7.

During the 1988 drilling season well logs were completed by BPB Instruments, Inc. of Grand Junction, Colorado. These logs are of excellent quality and have single print-out sheets for each log. The BPB logs were initially run at a scale of 1"=10' to correspond to the scale of the detailed core logs completed on each drill hole. The logs were also reduced to a scale of 1"=50' to correspond to the scale of all strip logs.

Gamma-Density-Caliper

The gamma-density-caliper log is obtained from one tool and utilized to test natural radioactivity levels, determine differences in rock density and check the uniformity in hole size. This tool or sonde operates effectively in cased or uncased holes and in air or fluid media.

The gamma log reflects natural radioactivity which is usually low in sandstones and limestones but higher in shales. Within the Sunnyside Tar Sands area the gamma responses commonly range between 100-200 API units with local kicks in the range of 400-800 and sometimes up to 1,000. Correlations of high gamma responses with the core logs indicate high responses are usually related to biota concentrations of black fish scales, bone fragments and/or ostracods.

The gamma log is often used as a sand and shale indicator. Bituminous sandstones have distinct gamma ray responses of 100±30 API units. These values form an identifiable bulge at sandstone intervals (see Figure 21B, 595-600 ft and 631-642 ft; and Figure 21C, 437-448 ft). Gamma responses in shales range from 70-170±20 API units (see Table 7). Correlation of the different colored shales (gray, green, mixed and red) with gamma responses shows that each colored

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shale type has a distinct set of values (see Table 7). When core is not available, specific shale identification is possible. Knowledge of different colored shales is important for stratigraphic correlation.

The density log is a reflection of the electron density of the rock material. Density values can be read directly from the log and are relative in an air filled hole but absolute in a water filled hole. Typical density values are listed in Table 7. The low density values of oil shale and their patterns are particularly helpful for identification and correlation. The density patterns of the R-7 oil shale (see Figures 16A and 16B) and the R-5 oil shale (see Figures 20A, 20B and 20C) are uniquely different and can be used for identification as discussed separately (see the Parachute Creek Member portion of this report).

The caliper log indicates the size of the drill hole. All holes were NX size and are 2.980 inches in diameter. With few exceptions the three inch hole diameter remains constant. The exceptions are caused by minor caving and voids associated with the Parachute Creek Member. Pronounced variations in hole diameter exist in A-67 (60-70 ft, hole diameter 5-8 inches) and A-72 (617-626 ft, hole diameter at least one foot).

Multi-Channel Sonic

The sonic log represents a recording of the time required for a sound/acoustic wave to travel through typically one foot of rock formation. This internal transit time is given in microseconds per foot. The transit time is a function of the lithology, porosity and type of fluid in the pore space; if the lithology is known, good porosity values can be obtained by utilizing the sonic log (Schlumberger, 1972).

Within the Sunnyside Tar Sands area the interval transit time has a range from 65-100 microseconds per foot (see Table 7). The sonic log has been utilized to obtain primary porosity values. Primary porosity values of bituminous sandstones and limestones were determined by (1) obtaining the interval transit time in microseconds per foot from the sonic log, (2) determining the lithology from the drill hole core logs and (3) utilizing the log interpretation charts from Schlumberger (1972). Porosity values determined from sonic logs are considered by the well logging industry to be better and more specific than porosity values determined from density logs. The bituminous sandstones have a porosity range between 20-34% with 25-27% porosity as the most prevalent. The higher porosity values appear near the top

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of distributary mouth bar deposits, while some of the lower porosity values are associated with beach to nearshore bar deposits. The bituminous limestones have porosities that range from 15-26%. Porosities of 20-26% are commonly associated with ostracodal limestones, coquinas or biomicrites. Porosities of 15-20% are commonly associated with the more dense limestones or micrites. The various porosity values are essentially the same as porosity values determined by Core Labs.

Focused Electric

Resistivity logs are obtained by passing a current through the rocks, measuring the voltages and determining the resistivity values. Conventional electric logs are greatly affected by conditions in the borehole and adjacent formations. These variable conditions can be minimized by the use of focusing currents to control the path taken by the measured current (Schlumberger, 1972). The focused-electric logs must be completed with fluid in the hole and represent a calibrated resistivity of the rock units. Impermeable beds such as a shale are electrically conductive due to the presence of ion-bearing water and have low resistivity values; permeable beds are less electrically conductive and have higher resistivity values (Merkel, 1979). Within the Sunnyside Tar Sands area shales tend to have low resistivity values that range from 40-300 ohm/meters (see Table 7). The presence of hydrocarbons causes higher resistivity values since hydro­carbons are normally insulators (Schlumberger, 1972). Within the Sunnyside Tar Sands area bituminous zones cause resistivity values to increase dramatically with values up to 20,000 ohm/meters for bituminous sandstones and values up to 10,000 ohm/meters for bituminous limestones (see Table 7).

Tar Sand Analysis

The bitumen content of tar sands can be done by direct and indirect methods. Direct analysis of core provides the best measurements of bitumen content and has been the only method utilized for the Sunnyside Tar Sands project. The indirect method utilized the focused-electric, neutron and density logs with a computer program to determine the grade of bitumen. Drill holes within the Sunnyside Tar Sands deposit are rarely full of water after the drilling is terminated. The indirect method was first attempted in 1984 but the low fluid level in many drill holes presented so many problems all attempts to fully investigate the indirect method were

71 01009

terminated. In 1988 fluid levels in twelve drill holes ranged from -92 ft to -1179 ft (see Table IB) with an average fluid level of -538 ft. Drill core and direct core analysis will always be necessary for reliable results of bitumen content.

Well Log Interpretation

In a clastic sequence well log patterns often reflect changes in the grain size distribution of sand-silt-clay content. The well logs that best reflect the sand-silt-clay content are the gamma ray (GR) and spontaneous potential (SP). The GR and SP log curves are controlled by grain size distribution, have been recognized as sedimentation curves and can be used for sedimentological analysis to determine depositional settings (Serra and Sulpice, 1975; Merkel, 1979; and Cant, 1984). The GR log has been used throughout the Sunnyside Tar Sands project as it requires no fluid in the hole. The SP log requires fluid in the hole.

On both the GR and SP logs the so-called shale line is nearest the hole, while the so-called sand line is further away from the hole. Thus portions of the curve nearest the hole represent a high shale content and portions of the curve away from the hole represent a high sandstone content (see Figure 2 3). Deflections in the curve represent changes in energy conditions and grain size. Abrupt or large deflections in the curve indicate rapid changes in energy levels during deposition that result in rapid grain size changes. Small deflections indicate small changes in the energy conditions that result in gradual changes in grain size. Smooth patterns indicate homogeneity and relatively constant energy levels with limited change in grain size. Serrated patterns indicate heterogeneity and fluctuating energy levels with frequent changes in grain size (see Figure 23).

The GR or SP log curves have three fundamental shapes: (1) bell; (2) cylinder; and (3) funnel. Each shape developes under specific conditions and is associated with definite depositional settings. Each type of log curve is not absolutely unique to one environment as seen in Figure 24. (1) The bell shaped curve is shown in Figures 23 and 24 and represents a fining upward sequence. The abrupt basal deflection is associated with an unconformity and a rapid increase toward the sand line. The curve then slowly continues to slope inward toward the shale line and indicates a con­tinuing decrease in energy conditions with a continuing decrease in grain size. This fining upward sequence is commonly associated with channel sands and transgressive sands.

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Bell shaped curves exist within the Sunnyside Tar Sands deposit. Near the base of the tar sands package they represent channel sands. Near the upper portion of the tar sands package and above it, the bell shaped curves represent transgressive sands. (2) The cylinder shaped curve is shown in Figures 23 and 24 and is characterized by abrupt changes at both the top and bottom of the curve with a near-vertical smooth or serrated edge along the sand line. This type of curve represents a well sorted sand with uniform grain size. This curve is indicative of sedimentation related to both fluvial and regressive (prograding) processes and is associated with distributary channels of delta complexes (Merkel, 19 79). Cylinder shaped curves are the most abundant type of GR log curves within both the Bruin Point and Dry Canyon subdeltas. (3) The funnel shaped curve is shown in Figures 23 and 24 and represents a coarsening upward sequence. The bottom of the curve shows a gradual slope outward from the shale line toward the sand line and indicates a continuing increase in energy conditions with a continuing increase in grain size. The top of the curve has an abrupt deflection back to the shale line. This coarsening upward sequence is commonly associated with distributary mouth bars in the delta fringe. Funnel shaped curves are not abundant in the Bruin Point or Dry Canyon subdeltas but do exist near the top of the tar sands package.

The shapes of the well log curves have been utilized to help delineate sedimentation patterns and help define environments of deposition. Bell shaped curves indicate meander belt channel sands within the fluvial systems that extend into the upper delta plain. Cylinder shaped curves indicate distributary channels within the lower delta plain. Funnel shaped curves indicate distributary mouth bar deposits in the delta fringe. The Bruin Point-Mt. Bartles area is located on the shores of ancient Lake Uinta where the upper and lower portions of the delta plain and delta fringe were confined to a relatively short horizontal distance. Distributary bars form at fluvial outlets where the flow spreads laterally and the deposits are modified by waves and long shore currents (Berg, 1986). In the Sunnyside Tar Sands area the waves and shore currents were significant factors in ancient Lake Uinta, while tides and slumping were insignifi­cant factors.

In the Sunnyside delta complex shoreline environments prevailed and the DC, DMB and B-BB deposits have been modified by lake shore processes. Weakly modified cylinder shaped curves are the most prevalent type of well log curve. Bell shaped curves exist near the base of the tar sands, cylinder shaped curves prevail near the middle portion of the tar sands and funnel shaped curves are present in the distal portions of the tar sand deposit. Beach and nearshore

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bar deposits tend to have a serrated cylinder shaped or a weakly defined funnel shaped curve. High gamma responses exist at the base of numbered tar zones with a ninety percent frequency of occurrence (John Rozelle, personal communication) and these high gamma responses commonly reflect limestone units. The presence of limestones beneath most bituminous sandstones indicates the proximity to an ancient shoreline.

Within the Sunnyside Tar Sands area outcrops, drill core and well logs have been used to study lithology, sedimentary structures and biota. All these factors have been used to determine the various markers and environments of deposition associated with the Sunnyside delta complex.

Vertical profile refers to the vertical stratigraphic succession of sedimentary structures and depositional environ­ments. Sedimentary environments that are areally and laterally adjacent to each other succeed each other vertically and form a vertical sequence that defines depositional sequences (Visher, 1965 and Reineck and Singh, 1980) . In the Sunnyside Tar Sands area the depositional sequence is sandstone-shale-limestone-erosion. This vertical profile represents a large scale fining upward sequence indicative of transgressive environments. Within this overall transgressive system the sandstones represent a fluvial-deltaic regressive system. Thus the vertical profile contains an early regressive part and a later transgressive part followed by an unconformity. This vertical profile oscillated back and forth at least fifteen times in the Bruin Point area to form a stacked sequence of channel sands and sheet sands at the shoreline of ancient Lake Uinta.

A brief geological story describes the conditions associated with Milankovitch climatic cycles that helped to form the Sunnyside delta complex. At the time of an unconformity the lake level was low and erosion occurred to form minor scours in the limestones. Then the wet portion of the climatic cycle began and caused the lake water levels to rise with an influx of fluvial-deltaic sands. The rising lake level helped to spread the shoreline deltaic sands into sheet sands. Then as the lake level continued to rise shales were deposited. Later as the dry portion of the climatic cycle began to dominate, sediment influx decreased and the limestones started to form in shallow clear waters. As the dry climatic cycle continued, the lake level continued to drop. Then carbonate mud flats formed and eventually were exposed to erosion to form an unconformity. Then the depositional sequence of sandstone-shale-limestone-erosion was repeated again.

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74

SURFACE GAMMA RAY LOGS

The surface gamma ray logs completed along measured sections have proved to be highly valuable for determination and correlation of numbered tar zones and delineation of marker horizons. The gamma ray readings are obtained from a portable 3.3 pound Urtec gamma ray spectrometer. The idea to use this exploration method evolved from two factors. First, the successful use of gamma ray well logs to establish numbered tar zones and, second, a short article by Chamberlain (1984) describing the successful use of surface gamma ray logs for correlations in areas of abundant outcrops and sparse well control.

In 1986 four old measured sections were selected and reoccupied to evaluate the validity of this new surface exploration method. A methodology was developed and correla­tions of surface gamma ray logs with downhole gamma ray logs from Amoco drill holes was completed. After encouraging results the used Urtec minispec UG-135 was purchased for the project and used in MS 27-59.

The field method includes the following three items: (1) Select a base station at least thirty feet from the vehicle and take a reading at the beginning and end of each day. Adjustments to recorded readings should be made if significant differences exist. No adjustments are normally necessary as the diurnal changes are ±10cps. (2) Readings are taken 6 inches above the ground or 6 inches away from an outcrop to maximize reliable and consistent results. Gamma ray values are read off the digital readout for the first full 10 second period and recorded in a notebook. The meter mode is set at tc(10), which is the ten second count mode. The audio switch is kept at 250cps for normal background. High gamma ray values near 400-500cps cause the instrument to release a high pitch sound. When no noise occurs the gamma ray values are below background levels and the audio switch can be put to a lower level. Care should be taken to check for higher readings in nearby outcrops. (3) Readings are taken at consistent slope distances of 5, 10 or 20 foot intervals along the 100 foot tape, depending on the desired reading interval, steepness of slope and differences in lithology. Any anomalously high or low readings should be recorded regardless of the footage.

The surface gamma ray values range from 180-2500cps with normal values of 250-300cps. Values of 200-230cps commonly exist in the Parachute Creek Member. Values less than 200cps are associated with oil shale. Values greater than 350cps are considered anomalous and termed spikes, kicks or peaks. Gamma ray values from the minispec are re­corded in cycles per second (cps), while gamma ray values

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from well logs are recorded in American Petroleum Institute (API) units. Calibration of cps to API units can only be accomplished at the API test pit in Houston.

Later strip logs at a scale of 1"=10* are made of these recorded surface gamma ray values. The strip logs commonly show distinct patterns and at least three spikes of high gamma ray values per measured section. The gamma ray patterns, tar sand intervals, detailed lithology and environments of deposition are all utilized to correlate intervals and select numbered tar zones. The minispec is invaluable for correla­tion of measured sections as it establishes definite picks and removes the guess work. When the detailed surface gamma ray log on the MS-59 strip log is compared with gamma ray well logs in Figures 21A, 21B and 21C, it is clear that the gamma ray patterns of the Blue Marker are nearly identical. The detailed surface gamma ray logs coupled with detailed measured section data are a powerful field method to establish numbered tar zones and locate marker horizons.

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Weimer, R.J., 1976, Deltaic and shallow marine sandstones: sedimentation, tectonics and petroleum occurrences: Amer. Assoc. Petrol. Geol. Continuing Education Course Note Series No. 2.

Whatley, R.C., 1988, Population structure of ostracods: some general principles for the recognition of paleoenviron-ments in Ostracods in the Earth Sciences, eds., P. DeDeckker, J.P. Colin and J.P. Peypouquet, p. 245-256.

Wolf, J.A., 1978, A paleobotanical interpretation of Tertiary climates in the Northern Hemisphere: American Scientist, v. 66, p. 694-703.

, 1983, Late Cretaceous and Paleogene nonmarine climates in North America in Paleoclimatic and Mineral Deposits: U.S. Geol. Survey Circ. 822, p. 30-31.

85 01023

Ziemba, E.A., 1974, Oil shale geology, Federal Tract C-a, Rio Blanco County, Colorado in Energy Resources of the Piceance Creek Basin, Colorado, ed., D.K. Murray, Rocky Mtn. Assoc. Geol., p. 123-129.

Zietz, I., Shuey, R., and Kirby, J.R., Jr., 1976, Aeromagnetic Map of Utah: U.S. Geol. Survey Map GP-907.

01024

86

APPENDIX

01025

Photo 1. West Tavaputs Plateau from Mount Bartles

This view from near Mt. Bartles looks east to southeast across gently dipping slopes of the West Tavaputs Plateau which tilt toward the Uinta Basin. This photo illustrates some of the general and detailed rela­tionships of the four marker beds within the Parachute Creek Member of the Green River Formation. These four marker beds include from top to bottom the Wavy Bedded Tuff, R-7 oil shale, R-5 oil shale and Blue Marker at the base of the Parachute, see Figures 15 and 22 . The near brown cliff in the central portion is associated with the R-5 oil shale horizon, while the distant brown cliff on the right portion is associated with the R-7 oil shale horizon.

upper yellow dot: Desolation Canyon of the Green River some 20 miles away. light blue dot: location of Photo 2, 2500 feet away on near brown cliff. left yellow dot: top of MS-29, 23,000 feet away. First measured section with excellent exposures of

numerous oil shale intervals. R-5 oil shale well exposed below base of distant brown cliff. Separate views of MS-29 are shown as Photos 3 and 4 of the 1986 Exploration Report. The oil shale doublet shown in Photo 4 of 1986 is now identified as R-5 oil shale and is 190-214 feet above the Blue Marker,

right yellow dot: dot is 17,000 feet away at beginning of Dry Creek Canyon that continues past bottom of MS-29 for 15 miles downstream to Nine Mile Canyon,

two red dots: location of MS-32 with R-5 oil shale above top red dot and Blue Marker near lower red dot. Vertical distance from base of R-5 oil shale to Blue Marker is 215 feet and about equal to that of MS-29. Laterally to the left of the lower red dot toward the large aspen in the central foreground note the vegetation change where dense grasses dominate upper slopes somewhat below the near brown cliff but change abruptly to more open sage dominated slopes near and below the Blue Marker,

three dark blue dots: location of MS-15 with middle dot near Blue Marker at base of grassy slope. This noted vegetation change at the Blue Marker persists throughout the West Tavaputs Plateau. R-7 oil shale interval near upper blue dot and above distant brown cliff. R-5 oil shale not exposed,

two orange dots: location of MS-56 (22,000 feet away) in hidden minor drainage. Wavy Bedded Tuff first located near upper orange dot and above R-7 oil shale interval (Mahogany Ledge) that outcrops immediately above distant brown cliff. R-5 oil shale exposed some 35 feet below base of distant brown cliff. R-5 oil shale is 175-195 feet above Blue Marker,

green dot: near Amoco drill hole A-66; 0-18 feet no core recovery; top of R-5 oil shale at -100 feet; Blue vji.'5 Marker at -320 feet. Thus 220 feet from Blue Marker to top of R-5 oil shale. Data from MS-29, •'•}-, 32, 56 and A-66 all indicate distance from Blue Marker to top R-5 oil shale averages about U 220 feet.

Surmjiary Notes: distant brown cliff is one continuous stratigraphic unit with R-7 oil shale and Wavy Bedded ;•»$, Tuff both above it; near brown cliff at light blue dot is different stratigraphic unit

<=> associated with R-5 oil shale; MS-46 near Mt. Bartles has the vertical distance from Blue <=> Marker to top of R-5 oil shale as 180 feet. The Geology Map shows the trace of the R-5 fO °il shale from Mt. Bartles to Photo 1 to Photo 2; the two brown cliffs are stratigraphically <J3 separated by almost 100 vertical feet as determined by marker beds.

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Photo 2. R-5 Oil Shale Eafet of Mount Bartles.

View is looking southeast. Paper shale texture of R-5 oil shale is well-illustrated in these excellent exposures associated with brown cliffs east of Mount Bartles. Photo location is shown on Geology Map. The main axis of the Mt. Bartles-Bruin Point flexure extends from Range Creek (left of upper red dot and out of view) into the valley located immediately to the right of this photo.

yellow dot: above tall TV tower near U.S.G.S. Bruin. orange dot: above lunch spot located at flat drill pad area of drill hole GN-8. Blue Marker is located

about 50-100 feet downslope on all sides of this flat drill pad area, left red dot: lower portion of R-5 oil shale located immediately above brown outcrops of nonbituminous

iron-stained siltstones. These cliff outcrops contain multiple horizons of abundant molds of incomplete mudcracks and thin interbedded olive gray shales. The lower portion of R-5 oil shale is located about 200 feet above the Blue Marker,

upper red dot: above R-5 oil shale outcrops near viewpoint overlooking proposed site of mine dump and above collar of A-42 drill hole. See Geology Map.

note: gamma ray well logs of R-7 oil shale and R-5 oil shale show distinctly different patterns. The . 20 foot thick R-7 oil shale interval is characterized by three nearly equal prongs that from peak to peak have a positive to almost infinite slope. The 20 foot thick R-5 oil shale interval is characterized by three unequal prongs that from peak to peak have a negative slope.

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Photo 3. Outcrop of Wavy Bedded Tuff.

This photo is looking south at exposures of the Wavy Bedded Tuff which exist at the drill pad of Pan American-Nutter Corp. No. 1, located near coordinates 475,000 N and 2,337,500 E on the Geology Map and located in T14S, R14E, Section 1, SW/4. Here the Wavy Bedded Tuff is 24 inches thick with a color of very pale orange 10YR 8/2 to pale grayish orange 10YR 8/4. Light olive gray shales (5Y 5/2) of the Parachute Creek Member exist above and below this air fall tuff.

light blue dot: decomposed thumb size ash fragments, visible below dot are a characteristic feature of the Wavy Bedded Tuff (capitalized as represents formal U.S.G.S. nomenclature),

yellow dot: 1-5% fresh medium to coarse grained biotite exists in the lower 6-8" of this tuff. Biotite concentrates from this location yield a ^^Ar/^^K age date of 47.3±1.8 m.y. by Geochron Laboratories.

The Wavy Bedded Tuff exists 35 feet above the top of the R-7 oil shale (or Mahogany Ledge), see Figure 15. Identification of this tuff is the single most critical factor in the positive field identification of the R-7 oil shale.

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Photo 4. Mini Anticline in R-5 Oil Shale Northeast of Mount Bartles.

This photo was taken about 3500 feet northeast of Mount Bartles near coordinates 501,500 N and 2,315,000 E on the Geology Map and is located in T13S, R14E, Section 7, NE/4. This unique mini anticline strikes N70°W with the view looking S70°E. In the photo the left flank dips 40°NE while the right flank dips 25°SW. This small anticlinal structure is located about 600 feet from the main axis of the Mt. Bartles-Bruin Point flexure as shown on the Geology Map. A second less photogenic mini anticline is located about 300 feet from the location of the main axis of the flexure. These two mini anticlines are associated with the upper 10 feet of the 20 foot thick R-5 oil shale. The lower 10 feet of the R-5 oil shale is undisturbed and has a rectangular joint pattern highlighted with patches of grass in the joints. A local unobserved decollement surface exists within the middle portion of the R-5 oil shale.

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Photo 5. Drill Core Illustrating Type I Algal Kerogen.

The central white mass is 1.9" high and represents a distinct algal stromatolite of fresh water origin. The concentric growth layers were predominantly formed by blue-green algae. The dark brown laminations of the overlying oil shale are draped over the small domal growth of the algal stromatolite and show no evidence of slumping.

This photo is a unique example of Type I algal kerogen (i.e. kerogen derived from an algal source). During the 1988 drilling season about 4000 feet of core from the Parachute Creek Member was logged in detail. This photo is of the most diagnostic sample that illustrates the intimate relationship of algal growth adjacent to oil shale.

This NX drill core is ten inches high by two inches in diameter (actually 1.875" D) and comes from the three foot thick R-3 oil'shale in A-72 at a depth of 347 feet. The Blue Marker exists 71 feet below at a depth of 418 feet. The Blue Marker is at the base of the Parachute Creek Member of the Green River Formation.

Blue green algal stromatolites commonly form in shallow nearshore to intertidal environments under aerobic/oxygenated aquatic conditions. The kerogen probably formed from an algal ooze under anaerobic/nonoxygenated conditions. Today algal blooms result from rapid uncontrolled growth of blue green algae that rapidly depletes the local oxygen supplies. Did algal blooms occur during Parachute Creek time and help to form the oil shale in relatively shallow water under anaerobic conditions?

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Photo 6. Blue Marker in Core from Drill Hole CD-I.

Core footages read as a newspaper going from upper left at depth of 350 feet above upper green dot to lower right,at depth of 365 feet. Wooden blocks were placed by drillers at end of each 10 foot run. Core footages marked by Rob Roy.

'-is--above^yellow dot: start of 3 foot thick R-2 oil shale associated with Blue Marker. To right of yellow dot distorted

'?sT near vertical wiggles are slightly deformed worm burrows. above two blue dots: 'thin coal seams of Blue Marker. The coal seams at base of R-2 oil shale (outcrops as dinner

plate oil shale with fossil fish fragments) exist throughout the Sunnyside Tar Sand area and can be found in nearly all core holes and measured sections that cross this contact of the Parachute Creek Member and Garden Gulch Member. This specific coal horizon has been used as the reference point to establish elevations for the Structure Contour Map of the Blue Marker.

above lower green dot: fossil turtle bone fragments. above orange dot: stylolite formed by compaction of clay seam and late diagenetic processes above red dot: algal stromatolite with 2" relief and brown strip containing 2-3 wt% bitumen. 351-360.4: light gray to light olive gray shale with 1-2% pyrite visible from 357-358. 360.4-363.4: 3 foot R-2 oil shale. Oil shale content increases with intensity of brown color. Color code

from GSA Rock Color Chart.

very pale orange 10YR 8/2 very lean grade pale yellowish brown 10YR 6/2 lean grade (near 360.5) increasing intensity dark yellowish brown 10YR 4/2 moderate grade of brown color dusky yellowish brown 10YR 2/2 rich grade (near 361.6) -

363.4-363.6: 0.5-1.0 inch coal seams of Blue Marker. 363.6-364.2: local transgressive lag deposits. 364.2-365: gray shale, 1-2 wt% bituminous siltstone and nonbituminous to 2-3 wt% bituminous algal

limestone.

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Photo 7. Rich Tar Sands in Core from Drill Hole A-67.

Core footages read as two columns of a newspaper. Left column is from 447-476.5 feet, and right column is from 476.5-505.4 feet. Average tar sand content determined from soxhlet oil extractions by Core Laboratories

Environment of

deposition

proximal distributary mouth bar to. distributary channel

nearshore proximal distributary" mouth bar to distributary channel

The stratigraphic position of Zones 31 and 32 is seen on the A-67 strip log. Tar Zone 31 is 43.3 feet thick between depths of 439.2-480.5 feet with an average bitumen content of 21.74 gpt and a density of 2.126 grams/ Tar Zone 32 is 25 feet thick between depths of 491.3-516.3 feet with an average bitumen content of 21.88 gpt and a density of 2.176 grams/cc. Highlights of the detailed core descriptions include:

447-467.8 9-10 wt% bit fine grained sandstone with medium scale trough cross bedding. 467.8-468.6 an upper 2" algal stromatolite and a basal 3" swirled mass containing l/wt% bit siltstone. 468.6-475 8 wt% bit very fine grained sandstone. 475-476 lag deposit (or intraformational conglomerate=IFC)with nonbit shale and siltstone clasts (50%)

in matrix of 5 wt% bit fine grained sandstone (50%). 476-479.6 7-8 wt% bit fine grained to very fine grained sandstone. 479.6-480.5 bit siltstone-shale IFC with 1 inch coal seam at base. 480.5-481.4 almost white calcareous shale. 481.4-483 5 wt% bit limestone (micrite to wackestone). 483-491.3 greenish gray shale with weak bit siltstone interval near 490.7. 491.3-505.4 9-10 wt% bit fine grained to very fine grained sandstone. Bedding features masked by

bitumen.

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Footages - • > > - •

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439.2-450.5 450.5-460.5 460-5-470.5 470.5-480.5 480.5-491.3 491.3-501.3 501.3-511.3

Weight percent bitumen

8.6 9.9 9.9 7.9 1.0 9.6 8.8

Gallons per ton

20.6 ~ 23.8 23.7 19.0_ 2.3 23.1 ' 21.0 .

Tar zone

number

31

32

GEOGRAPHY OF THE COLORADO-WYOMING-UTAH AREA. Shows present topography, extent of the Green River Formation (shaded) and

the depositional basins of the Green River Formation (modified slightly from Bradley, 1931).

Van West, 1972

Figure 1. General Locat ion Map, Sunnyside Tar Sands (red d o t ) , Uinta Basin, Utah.

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EXPLANATION

MS-£7 - MEASURED SECTION LOCATION & NUMBER

A-71&,- 1988 DRILL SITE

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SCALE

FIGURE 3

LOCATION OF MT. BARTLES-BRUIN POINT SEGMENTED FLEXURE, MEASURED SECTIONS OF 1986-1988 AND DRILL SITES OF 1988.

SUNNYSIDE TAR SANDS AREA, CARBON COUNTY, UTAH

LEASEHOLD

• AMOCO gg| QNC

BLM g| SABINE

STATE • ENEBCOR

DATA! BLM, 1983, SUNNYSIDE EIS, MAP 1-4

SUNNYSIDE TAR SAND AREA BOUNDARY OF BLM

FIGURE 4 LEASEHOLD AND FEE OWNERSHIP MAP, SUNNYSIDE TAR SANDS, CARBON COUNTY, UTAH

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AMOCO FEE

COCA MINES FEE

GIBBS HEIRS FEE

• PRIVATE

§§ STATE OF UTAH

El BLM DATA: BLM, 1983, SUNNYSIDE EIS. MAP 1-4

•SUNNYSIDE TAR SAND AREA BOUNDARY OF BLM

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•c. FIGURE 5 SURFACE OWNERSHIP MAP, SUNNYSIDE TAR SANDS, CARBON COUNTY, UTAH

ENERGY RESOURCES MAP OF UTAH MAY 198 J

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Oil AND RATUftAL CAS

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GENERALIZED SEDIMENT TRANSPORT DIRECTION

FACIES

I:'"".'] ALLUVIAL FAN [ , ' ) ALLUVIAL PLAIN £ V • ) PALUDAL-LACUSTRINE

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GENERALIZED SEDIMENT TRANSPORT DIRECTION

ALLUVIAL FAN

ALLUVIAL PLAIN

FACIES

CD g=l

i i 32 KM

MARGINAL L A C U S T R I N E

OPEN LACUSTRINE

o OS

Early Paleocene paleogeography, Norlh Horn Formation, northeastern Utah.

Late Paleocene paleogeography, northeastern Uiah.

Bruhn, Picard and Deck (193 3)

Figure 7. Paleogeography of the Paleocene (66-58Ma), Northeast Utah.

-GENERALIZED SEDIMENT TRANSPORT DIRECTION

FACIES GENERALIZED SEDIMENT TRANSPORT DIRECTION 32 KM

ALLUVIAL FAN

I I ALLUVIAL PLAIN

112*

MARGINAL LACUSTRINE

OPEN LACUSTRINE

FACIES

| | ALLUVIAL PLAIN JOPEN LACUSTRINE ['-] MARGINAL LACUSTRINE

Middle Eocene paleogeography, Upper Parachute Creek, Green River Formation, norlheastern Utah.

Late Eocene paleogeography, northeastern Ulah.

Bruhn, Picard and Beck (1983)

Figure 8. Paleogeography of the Eocene (58-37Ma), Northeast Utah.

UINTA BASIN

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Duchesne Riyer

Fm

Uinta Fm

These formations are so similar that they cannot be separated in well logs.

U>

Evacuation Cr M

Parachute Cr M

Douglas Creelt M Renegade" Tong t lot Wasatch Fm

Willow Creek M

Wasatch (Colton) Fm

Flagstaff Lr North Horn Fm

Mesaverde Group

Mancos Shale

rrontiftr-Mowrv Fm: rronTier-MOwrv i-ms Dakota-Cedar Mtn F

Morrison Fm CItirrk r-m Entrada Ss Carmel Fm

Glen Canyon Group Chinle-Garta Fms

Moenkopi Fm

Weber-Park City Fms

undifferentiated Miss-renns limestones

Devonian undiff. Cambrian undiff.

"granite"

0-3000±

0-5000±

100-600

300-600 01 :m

0-1000

0-1200

0-500

0-300

3200-5000

Si 500-620

0-220

500-650 70-l50v=rr;

100-760 "OlSW

-830 0(SW) -1500 O-I60 0-200

Ttltodut (Titanotktrt)

Eoihippus Hyrocodon

Echinutfin/ j (turtle)

Epihippus

Uinlattwriwn Htrrachrui

oil ihalt Mahogany oil

thala bad

black thala mbr

Phenacodus Coryphodon

Hyrantherium iEahippui)

thint northaaftward

tfcickani north* oattward

north araa only

Nu49«) Si

All pra-Triauic wat arodad from tha Uncompar-ora block. Thin Pa. laoioic taction found on north-aatt tida of tub* turfaca Uncom-pahcjra uplift

W Y O M I N G

SALT h LAKE

CITY

Pteieni eroslonal edge of Uinta Basin Tertiary.,

PROVO i

ISOPACH MAP of DUCHESNE RIVER

and UINTA FORMATIONS

W Y O M I N G

_ SALT •-•LAKE

CITY

PROVO •

Present erosional edge of Uinta Basin Tertiary-

ISOPACH MAP

G R E E N R I V

F O R M A T I O

W Y O M I N G

SALT h LAKE

CITY

Present erostonal edge of Uinta Basin Teniary-

PROVOi

ISOPACH MAP of

WASATCH FORMATION

(Colton-Flagstaff-North Horn Fms)

Hintze, 1972

Figure 9. Stratigraphic Section and Isopach Maps of Uinta Basin.

01048

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Chart i l l u s t r a t i n g s t r a t l g r aph l c nomenclature and c o r r e l a t i o n of major Albian to middle Eocene rock un i t s from the Sanpete Valley of cen t ra l Utah to the Book Cl i f f s of eas tern Utah (modified from Fouch and o the r s , In p r e s s ) . V e r t i c a l l i n e through s t r a t a Indicates a change In s t r a t l g r a p h l c nomenclature.

Fouch, et al, 1983

Figure 10. Northeastern Utah Correlation Chart

39°

>io° modified from Van West, 1972 >09c

O

EXPLANATION

UINTA & YOUNGER FORMATIONS A-A- LINE OF SECTION

GREEN RIVER FORMATION NAMED TAR SAND AREAS

FIGURE 11

INDEX MAP OF THE UINTA AND PICEANCE CREEK BASINS

WEST NORTHWEST

A

EAST SOUTHEAST

A '

WESTERN UINTA BASIN - - EASTERN UINTA BASIN -

AREA OF SUNNYSIDE TAR SANDS PROJECTED 20 MILES DOWNUP TO SHOW ITS RELATIVE STRATIGRAPHC POSTION

•3

- I B 10.000

MODIFIED FROM McDONALD 1972

HORZ.

12X VERTICAL EXACCERATION

FIGURE 12

WEST TO EAST CROSS SECTION OF THE UINTA BASIN LOOKING NORTH

01051

LOOKING NORTHWEST SOUTHWEST NORTHEAST

O

Bruin Point

GREEN RIVER FORMATION

GARDEN GULCH

MEMBER

PARACHUTE CREEK

MEMBER

Shore or Green Shale

Facies

Lake or Gray Shale Facies

DOUGLAS CREEK

MEMBER

Asphalt Mine

Delta or Red Shale

Facies

TAR ZONE NUMBER

Base of Tar Sands Falls Downdip at ° U S SANDSTONE Average Rate of 30 Feet Per 1000 Feet

•IOOOO

300

-9700

-9400

-9IOO

— 8800

-8500

FIGURE 13 SCALE

Beds Dip at Average Rate of 120 Feet Pet 1000 Feet

IDEALIZED SECTION OF BRUIN POINT SUBDELTA SHOWING TAR ZONES AND DEPOSITIONAL ENVIRONMENTS

SOUTHWEST LOOKING NORTHWEST

NORTHEAST

ARCO Woter Tank

- 9 7 0 0

GREEN RIVER FORMATION

- 9 4 0 0

-9100

Delta or Red Shale Facies

- 8 8 0 0

r Bose of Tor Rises to Northwest at Averoge Rote of 25 Verticol Feet Per 1000 Horizontal Feet If

Bose of Tar Falls to Southeast at Average Rate of 35 Vertical Feet Per 1000 Horizontal Feet

- 8 5 0 0

0

L Oi 300

J*i I SCALE

FIGURE 14 IDEALIZED SECTION OF DRY CANYON SUBDELTA SHOWING TAR ZONES AND DEPOSITIONAL ENVIRONMENTS

APPROXIMATE FOOTAGE

INTERVALS BRIEF

DESCRIPTION STRATIGRAPHIC

MARKERS

U.S.G.S. OIL SHALE ZONATION

355

in in m I o o m

LLI

O Z <

T 35

I 20

90

20

•jr

50

19-23" BIOTITE-RICH TUFF WITH ERODED V'ASH FRAGMENTS

18-27'OIL SHALE, OUTCROPS AS SEPARATE DISTINCT DOUBLETS 10-40'BROWN CLIFF, ABUNDANT MOLDS OF MUDCRACKS IN LT BROWN SILTSTONES

II

.. 1 = 55

140

85

WAVY BEDDED TUFF 47.0+ 1.8 m.y.

MAHOGANY OIL SHALE

R-7

18-22'OIL SHALE, OUTCROPS AS SEPARATE DISTINCT DOUBLETS

R-5 OIL SHALE R-5

2 -5 'O IL SHALE 1-14" BIOTITE-RICH TUFF, CORE & RARE OUTCROP

1-2" INTERVAL OF VIVID GREEN MINERAL 2 -5 'O IL SHALE

LOWER TUFF 51.5+2.0 m.y.

R-4

R-3

2 - 7 ' OIL SHALE, OUTCROPS AS 1-2' DINNER PLATE OIL SHALE WITH 0.5" COAL SEAM 1-1.5'BELOW

BLUE MARKER BASE OF PARACHUTE

R-2

SCALE: 1" = 50' DATA BASE: DRILL CORE 1988

OUTCROPS 1986-1988

COMPILATION: W. CALKIN DATE: 2-15-89

FIGURE 15 STRATIGRAPHIC MARKERS IN THE PARACHUTE CREEK MEMBER, SUNNYSIDE TAR SANDS, CARBON COUNTY, UTAH

01054

2.0

DENSITY

g/cc

(IN AIR) J L

2.5 _ l

GAMMA RAY

API CORE

LITHOLOGY DEPTHS

WAVY BEDDED TUFF

i

UJ Z o N

Ul -i < X (/)

'

i

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tr 1t^

t

DC UJ

m UJ

S

UJ UJ oc o

UJ

=> X o < oc < a

FIGURE 16A WAVY BEDDED TUFF & MAHOGANY ZONE. A - 6 4 , WELL LOG & LITHOLOGY CORRELATIONS

01055

2.0 L_

DENSITY g/cc

W AIR) J L.

2.5 !

GAMMA RAY CORE

203 LITHQLOGY DEPTH

LT OLIVE GRAY SH

OIL SHALE LT OLIVE GRAY SH & VOLCANIC TUFF

OIL SHALE

*-R J

WAVY BEDDED TUFF L-M

M

PELLET IPC

OIL SHALE

NONBlTvfg SANDSTONE WITH MUSC. LAMINAE

OLIVE GRAY SH

MED GRAY TO

MED BLUISH GRAY SH

UJ ffi S w S.

MED GRAY TO

OLIVE GRAY SH

VL L-M LT OLIVE GRAY SH

DK YELLOWISH GRAY SH

M-R

L

ALGAL STROMATOLITIC LS

L-VL

RICH

LEAN

RICH mg 5 VTT% BIT SS *S 4 WT% BIT SS V*S3WT%SITSS

DK YELLOWISH GRAY SH mg NONBtT SS ig 1 WT% BIT

SILTSTONE

YELLOWISH GRAY TO GREENISH GRAY SH

_ l

o > < a o X < 5

'

i

w z o N K

3-* X 05

'

UJ Ui EC O

u i J -

X O < £C <

a

FIGURE 16B WAVY BEDDED TUFF & MAHOGANY ZONE, A - 7 1 , WELL LOG & LJTHOLOGY CORRELATIONS

AMOCO

Or tur ru-mr rm M i l l Mini m m w-u-n

CAMERON

— " 0 7 O T A •r m mr m

i m m miu IMII nun

CAMERON

• t.i.t. n IUU INITM: I I I I U •nSTWTMS CUT K II: U U W I M K U 1171

INOfX MAP LINE OF SECTION

MTC TOPS IM M S I OF IKN MALI ZOWS AUVTRAMLV DCPMCD tT ». «/T SMALC n u n IT u i t a . U U M . ITOKM

* MS$MC COM MTMVAL

•OTCAl SOU FEDERAL TRACT C - a

HIO BLANCO CO.. COLOHAOO

SW-Nf HISTOGRAM CROSS SECTION (APPHOX NOHMAL TO SOPACH STAKE}

01 IT» IT W J Ot t t lCHAI l

SW-NE oil-yield histogram cross section (in gal/ton), Federal Tract C-a.

Z i e m b a , 197 4

Figure 17. Oil Shale Zonation and Important Markers in the Green River Formation.

01057

THICKNESS, IN FEET

200

400

600

800 —

1000

1200

MAHOGANY LEDGE

OR ZONE

'B" GROOVE

R-6 ZONE <

1-5 ZONE <

R-5 ZONE <

L-4 ZONE

R-4 ZONE

L-3 ZONE

R-3 ZONE

1400

R-1 ZONE <

ORANGE ZONE IZone of low electrical

resistivity that includes the orange

marker)

<.• ••- '-: • • •:>

ii'-'-r ?v -' • £?•>• fc-'"

§§§ffjm Ifiw

--''.!':.>-;,";:;""" ^ ^ 5 ^ 1

"• /:V^>£':'' : >'*i V%^ •v--'-'-'!',-".'.v-.^"-<x'--'--^'''-'^1

1 r • ¥••• "

L \

• . -

1'. ?•'

: '

: •

r

* M

r . •

*

CS^MSm •:-'^7:M^

- • ^ ' • S ; ' ^

• • • ' • ' • - " - ' • • • - ' • ' • • • - '

^ • *

---*

• " N - J

^ „

«. - >-. i t . > .

•

•

•

. *

- " V ~i

.. *. . ^ ••. ?-^

<*, ~ * .. ~ c *

-J

. , , . :

.

' T. ^ -

> ^ -

.

. ;

r,'

-1 " * ^

r • » *

.

,

m

c v ; / ^ : ;

' "" —•~~i

- T y n n ^ i^Wg.-t^H

The uppermost and most widespread rich oil-shale zone in the Piceance and Uinta basins. The top of the saline aquifer is in the lower one-third of the Mahogany zone

Represents a major decrease in size of Lake Uinta just prior to the deposition of the Mahogany zone

Nahcolite and halite have been leached from this zone in most of the Piceance basin

Brecciated oil shales in this zone represent intervals where nahcolite and (or) halite beds have been leached. Bedded nahcolite and halite are preserved in small areas

One of the richest oil-shale zones in the Piceance basin. Also contains the greatest resou-ce of nahcolite of any zone. The uppermost significant content of dawsonite is found in this zone

Richest oil-shale zone in the center of the Piceance basin. Contains moderate amount of nahcolite and a large amount of dawsonite

Zone containing the greatest amount of dawsonite

Contains three of the most widespread, thick, dissemin­ated nahcolite zones in the basin

Lowest zone containing significant amounts of nahcolite and dawsonite

"Blue Marker", top of the Garden Gulch Member. Base of saline deposition

Rich oil shale in dominantly clay matrix

Clay-shale zone containing no oil shale

Donnel l , 19 87

Figure 18. Rich and Lean Oil Shale Zones in t h e Green Riv; Formation, Piceance Creek Basin , Colorado.

01058

Detailed measured section of the Oil-shale fades of Parachute Creek Member at Douglas Pass, Colorada

l ESTIMATED i OIL-SHALE

* „ 0 r S GRADE

I I I I I •LITHOLOGY 70 Mn

6 0 -

5 0 - .

4 0 -

2 0 -

10-

EXPLANATION

HH Oil Shale

| | Marlstone

• x Tuff

P Plant Debris

i Insect Fossils

UPPER

OIL-SHALE

ZONE

» Wavy Tuff

A GROOVE

MAHOGANY -False Marker

-Mahogany LEDGE Bed

f * Curly Tuff B GROOVE

= R-8

= R-7

Cole , 1985

Figure 19. D e t a i l of Mahogany Oi l Shale Terminology.

0105.Q

2.0 1 I

DENSITY g/ec

(IN AIR! 1 1

2-5 1 1

GAMMA RAY

API CORE

203 LITHOLOGY DEPTHS

n

m z o N m -J < z to _ l

o

to l

£t

< '

tr UJ

UJ

2

ui UJ cc o

Ui H

X o < DC < o.

FIGURE 20A R-5 OIL SHALE, CD-1 WELL LOG & LITHOLOGY CORRELATIONS

01060

2.0 l _

GAMMA RAY

API CORE

283 UTHGIOGY DEPTH

5 1 400

DENSITY

g/ce

(IN AIR; J L

2.5

425 ' I

MEDIUM OLiVE GRAY SHALE

LIGHT OLIVE GRAY SHALE

IU Z o N Ul < X

to I

L-VL OIL SH

IFC

L -VL OtL SH

FIGURE 20B R-5 OIL SHALE, A - 7 1 , WELL LOG & LITHOLOGY CORRELATIONS

01061

2.0 i i

DENSITY

g/cc {IN AIR)

L_ I 2.5

i i

GAMMA RAY

API 200 CORE

LITHOLOGY DEPTH

175

20G

225

CC m m S in

ill •z

o N Ui _1 < X <ft _l

o

tft t cc

UI •til 0C O

H

X o < GC < O.

FIGURE 20C R-5 OIL SHALE, A - 7 2 , WELL LOG & LITHOLOGY CORRELATIONS

01062

2.0 1 1

DENSITY

g/cc

UK Am) 25 1 !

GAMMA RAY

API CORE

203 LITHOLOGY DEPTH

GRAY SHALE

OIL SHALE

LT GRAY SH

1 WT% SIT vfg SS

OLIVE GRAY SHALE

1-2 WT% BIT fg SANDSTONE

OLIVE GRAY SHALE

OIL SHALE m-2) 0 5 - 1 " C O A L GRAY SHALE

MiCRtTE

LT GREENISH GRAY SHALE

3 6 3

* UJ UJ cr U £ C m UJ . Q3 3 2 x m O S < tr < a.

BLUE MARKER

MICRITE

LT GREENISH GRAY SH

I

o _s

O m 2! >s. UJ a a: <

UJ

J 40fi

FIGURE 21A BLUE MARKER, C D - 1 , WELL LOG & LITHOLOGY CORRELATIONS

\\ 1 0 fi 1 J i. v ^ O

2.0 l

GAMMA BAY

AP! CORE

203 UTHQLQGY DEPTH .;•*-—

**3

600

" • • * ! "

'Si

li­

sts ~ -

DENS1TY

g/cc

{IH A iR)

J L 2.5

650

LT OLIVE GRAY SHALE

6-8 WT% BIT fg SANDSTONE

LT OLIVE GRAY SHALE

Hi til oc o m

z> X o <

< a

tr UJ CQ

S

OIL SHALE (R-2) 1"COAL GRAY SHALE LSIFC GRAY SHALE BIOMICRITE

GREENISH GRAY SH

i -3WT%S)T SJLTSTONE

7-8 WT% BIT fg SANDSTONE (ZONE 2 t i

SH-LStFC

MICH! TE 80% SHALE 20% ALGAL STROMATOUTtC LS

GREENISH GRAY SHALE

618 BLUE

MARKER

X

o _J O UJ _ CQ

ty a EC < 0

UJ

01064 FIGURE 21B BLUE MARKER, A - 7 1 ,

WELL LOG & LITHOLOGY CORRELATIONS

.0 I 1

g/cc {IN AIR}

1 1 ,„ , J 25

J

GAMMA RAY

AH

- 400

CORE 280 LITHOLOGY

DEPTH

LT OLiVE GRAY SHALE

OIL SHALE <R-2)

OS"COAL

STYOLITE PALE ORANGE SHALE

MICR1TE

GREENISH GRAY TO GRAY SHALE

S1LTSTONE

2 WT% SIT fg SANDSTONE (ZONE 2t ;

MICRITE

GREENISH GRAY SHALE

418

* Ui Ui DC

o Ui H z> X

< CC < a.

BLI

CC Ui tn S m S

JE

X u - 1 3 a z w a cc < a

CC Ui

m 2 w 2

01065

FIGURE 21C BLUE MARKER, A - 7 2 , WELL LOG & LITHOLOGY CORRELATIONS

GRouPS GR or PS high water level Serra and Sulpice, 1975

« • . • . • . • • • • • • • • " ^

• • • • _ • • • • • • . . . • . • low water level

Barre al luvial* Channel sand

sea level

^^''•^"."•^.^••"""•'•'^tvr'.V.'-A'.^'iT.'.'r It .v. .'.••. .*.» •"

Zone J>ordiere du delta Delta front deposit

Cordon littoral Barrier bar

mmmmw* Sable transgressif Transgressive sand sur une discordance

ELECTROFACIES CLASSIFICATION SNAIE PERCENTAGE INCREASING

UPPER CONTACT OF SAND ABRUPT

CYLMDBI SHAPE • bad

SMOOTH SERRATED SMOOTH

BELL SHAPE* lining iimrf ugutnci

SERRATED

CONCAVE UNEAR CONVEX

FUNNEL SHAPE =emm

SMOOTH SERRATED

EGG SHAPE =qdt

SMOOTH SERRATED

Classification of electrofacies by shapes of log responses.

Serra, 1986

Figure 23. Well Log Shapes and Grain Size Distribution. 01067

Cylindrical

Clean, No Trend

150

aeolian, braided fluvial, carbonate shelf, reef, submarine canyon fill

Funnel Shaped

Abrupt Top Coarsening Upward

o 150

crevasse splay, distributary mouth bar, clastic strand plain, barrier island, shallow marine sheet sand­stone, carbonate shoaling-upward sequence, submarine fan lobe

Bell Shaped

Abrupt Base

Fining Upward

150

fluvial point bar, tidal point bar, deep sea channel, some transgressive shelf sands

Symmetrical

Rounded Base and Top

150

sandy offshore bar, some transgressive shelf sands, amalgamated CU and FU units

Irregular

Mixed Clean and Shaly, No Trend

150

fluvial floodplain, carbonate slope, clastic slope, canyon fill

The most common idealized gamma-ray (SP) log curve shapes and at least some of

the depositional settings in which they can originate. Several environments are listed under more than one curve, indicating they

are somewhat variable.

Cant, 1984 O

OO Figure 24. Well Log Shapes and Depositional Settings.

3 o

CO (U r r C i-< (u r r H-O 3

IX 1-1 H-M M

S4

O M (D

' f D M (D

<! (u r r H> O 3 CO

o M l

O o \-> \-> (U H

(U 3 IX

<r (U CO fD

o M l

(U M M

« CD M M

rx Co r r (u

H-3

M i (D (D r r

o OS CO

W t l C/3 C/3 > > H H

II II

cr" IX fu ro CO T3 (D it­

s' O Mi r r

O CO Cu r r r t O C X) H (U O r t Mi H« O X) 3 i-l

H -

^ 3 H- n • H-ro x) . (U - M

CT r t O (U r t i-l r t O CO S 0>

3 o rx M i CO

r t / -^ Co O H <J

(D CO i-l

CO CT"

3 C CX. i-l CO I X x - ' (D

3

el­

s' H> n !C

(U 3 CX

a H' 3 H-

a c s 1—• o

09 (U M CO

~-* r t O 3 *—'

£ C/3 > H

II

r t O r t CO •—

K> O O r t CO

09 <T>

p CO H-3

CO CO r t C i-l CO r t

ro IX

N o 3 ro CO

/ ^ 3 H' 3 H-0 C

s t—

o Mi (D

ro

w d > H

II II

r t , r t O O r t r t (U (u M M

Mi p. O ft) O T3 r t r t 0> p*

OQ ro (U M M

CO Co r t C i-l CO r t ro <x CO ro <x H-S ro 3 r t CO

r t Mi o O r t O Co r t | -

OQ ro

i—1

H-* rjo O l

a

I I I I I I I I I

r o t - 1 0 * C O v l O » U i * -

O K i O H N v l O O W H

H - ' N 3 L n L n N J N J N J ~ - J i - ' O O f - s J s J l O C O O U l O O U i U v l U i H O W ^ O

H W N) H H Ln M M v J v J O i v O M O O - P -C M » J > 0 v U N « ( » O

U I W K I V J H H O H I C t O U i M C O U i O O O O O U

V I—1 I—1 I—1 I—1 t-" I—•

I I H O H M V J O O N H O C X i O C l C 7 > l - ' l - ' l - ' ~ - J N 3 O O W U H O O O O O O N H

n n i i

U) r o

i—1

O Ln

o o o o

M ~-J r o Lo O

LO Ln O

+ V

LO Ln ~-J O O O

V • - V O Ln

o o c o

n i

Ln o o

Ln r o

i—1

>o +

•c~ Ln LO

V Ln O o

EC O M ro z o

n o

H c/: > H

s C/l

> H

O C/l

> H

W C/l

> H

c/: e § @ >-t

o

(—• > D

n H » r -

c? M ro

Table IB. Available Well Logs from 1988 Drill Logs

Hole No. TD Fluid Level G-D-C Res Sonic

CD-I CD-2 CD-3

500 500 1000

92 235 671

/ / /

/ / /

A-64 A-65

A-66 A-67 A-68 A-69 A-70 A-71 A-72

/ = log x = no

1179 1329

849 749 1236 1169 1099 1239 1009

log ail dimensions

dry to TD dry to stoppage @ 725

210 304 757 425 485 760

dry to void @ 612

in feet

V /

/ / V / / / /

X

X

X / / X

/ / X

X

X

/' X

/ X

X

X

X

01070

Table 2. Status of 1988 Drill Holes

Hole No.

CD-I

CD-2

CD-3

Total Depth

500

500

1000

Date Completed

9- 6-88

7-22-88

8-24-88

Surface Status Downhole Conditions

reclaimed, screw cap on 11! casing not visible

reclaimed, screw cap on 9' casing under rock reclaimed, screw cap on 10' casing not visible

full of hole plug*

full of hole plug

full of hole plug

Well Log Fluid Level

92

235

671

A-64

A-65

A-66

A-67

A-68

A-69

A-70

A-71

A-72

1179

1329

849

749

1236

1169

1099

1239

1009

7-22-88

7-14-88

7-24-88

8- 3-88

10- 4-88

8-18-88

9- 2-88

9-19-88

10- 5-88

reclaimed, visible screw cap** on 13' casing +3' extension reclaimed, screw cap on 10' casing not visible

reclaimed, screw cap on 19' casing not visible

reclaimed, screw cap on 18' casing under rock

reclaimed, screw cap on 10' casing not visible

reclaimed, screw cap on 18' casing not visible

reclaimed, screw cap on 20' casing not visible reclaimed, visible screw cap on 20' casing +3' extension reclaimed, visible screw cap on 10' casing +3' extension

open to 1165***

full to hole plug

full of hole plug

full of hole plug

full of hole plug

full of hole plug

full of hole plug

open to 1228

open to 612; 612-1009 unk

dry

dry to stoppage at 725

210

304

757

425

485

760

dry to 612; no well log beyond 612 as major void 617-626

* Hole Plug is a Baroid product of graded bentonite granules ** screw cap needs two 2-3 foot pipe wrenches for removal *** drill bit and 10 ft core barrel stuck in bottom of hole after dynamited off; all dynamite wire removed

note: 1. all well data in feet 2. all drill holes are NX size (2.98 inches diameter) with hole volume of 36.3 gal per 100 feet 3. all screw caps labelled with drill hole number, date of completion and location by quarter

section per BLM regulations

Table 3. Blue Marker Data Base

Drill Hole

A-2 A-4 A-5

A-8 A-9 A-ll A-12 A-14 A-15 A-16 A-17 A-18 A-19 A-20 A-21 A-22 A-23 A-24 A-25

A-26 A-27 A-28 A-29 A-30 A-4 2 A-60 A-63 A-64 A-65 A-66 A-67 A-68 A-69 A-71 A-72 CD-I CD-2 CD-3 BP-1A RCT-3A RCT-4 RCT-5 RCT-6 RCT-7 RCT-8 RCT-9 RCT-11 RCT-12 CNC-14A Gulf No. 1 Pan Am -NC No. 1 Shell No. 3

Collar Elevation

9627.7 9974.1

9403.4

9908.3 9810.7 10049.6 10101.8 9760.8 9943.1 10021.3 9781.0 10035.7 9893.6 9863.5 9821.7 9488.2 10034.0 9902.5 9564.6

9484.7 9977.4 9989.4 10036.1 10010.6 9960.0 9632.1 9822.7 9853.1 10104.0 8815.3 9718.3 9692.8 9690.6 9578.3 9490.9 8737.3 8858.2 9067.7 9822 9824 9746 9689 9772 9386 9548 9793 9411 9454 9916 8120

9310.7

9734

Blue Marker Depth

106 226

1(creek outcrop)

166 212 145 128 66 61 79 90 81 70 98 245 52 101 129 186 <a-45° 67 143 100 61 123 158 258 333 571 113 320 136 549 121 618 418 363 429 364 372 164 164 150 130 138 149 120 400 395 144 210

378

408

Blue Marker Elevation

9522 9748 9402

9742

9599 9905 9974 9695 9882 9942 9691 9955 9824 9766 9577 9436 9933 9774 9433 @130'E 9418 9834 9889 9975 9888 9802 9374 9460 9282 9991 8495 9582 9144 9570 8960 9073 8374 8429 8704 9450 9660 9582 9539 9642 9248 9399 9673 9011 9059 9772 7910

8933

9326 01072

s s s s s s s K w w w oi w tn I I I I I I I

s s s s CO CO c/i CO

I I I I

S S S K S CO CO CO CO CO 1 1 ( 1 1

C O C O C O C O C O C / J C O C / J

I I I I I I I I I I I I I I I I I I I I I I I I I I I I I 1 I I I O i ( - n ( - n ( - n ( - n ( - n l j i ( - n 4 > - 4 > - 4 > - U > U > O J O J O J O J U > N 5 N 5 N 3 i - - ' i - - ' i - - ' .C-i O 0 0 s l ( J \ U l W N O 0 0 v J ( J i v l W M J N H O l 0 0 0 v J a O l O

K>

1—• 1—' I—• O V O V O V O V O V O V O V O V O V O V O V O 0 C 0 0 V O V O 0 0 0 0 0 0 0 0 0 0 V O 0 0 V D O V O O H O \ ( n o o u u n O v n o w N U i o o t - H u u f - V I O » O \ H O O o H W i O W 0 C l n ^ H 0 0 H j > H O M W 0 0 v l U i M C D ( O 0 0 0 0 W t - l » J > 0 0 ( - n ( _ n K ) 4 > - . p - O C T > O a N O < - n O O O O O O O O ( - n ( - n v O O U > ( _ n O

C/J

n> o r t H-

o 3

M M (T>

< (U r t H -O

o

£ (0 Pi CO

c l-t ft)

n o i d

h-3 CD a* i—i (T>

O O 0 rt H-0 <T> a.

N w ^

U O i t ^ W O l N H H - ' . C - M M l - ' M M l - ' M h C N J N i l - " v j H 4 > - N J N f - ^ W C O m \ 0 0 ( ^ ^ H t > y 3 \ O v l p - W ( J i s l O i N ) O O j ; > v j o o ( o w v o > O N O N O » j s u i w o o a i u i ( y u i v i o o t ' O o u i M

I—' I—1

O v O ^ O O O O O O v O v O v O v O v O O O O O O O O O v O ^ J O O O O O O O O v O O O V O O v O v O O W H O I S 1 V J W V I V I 0 0 S I 0 0 O W V 0 N 0 0 H O N ^ O V I * - H 0 0 « ) 4 > - ( - ' ( - n O O J ( - ' O O O O C T > < - n O O J 4 > - ^ J O J ^ J ( _ n ^ - O J O O N 3 i - ' ^ J N 3 0 v O ( - • • ~ J U J V 0 ( - n O O - P - O . p - O v 0 a N l J i ^ J M . p - ( - n ^ - ( - n 0 0 ( _ n v 0 a N U i O 0 0

CO

Table 4. Lithology of Sunnyside Delta Complex and Its Two Subdeltas

Total Footage*

47,418 30,497 16,921

Average Thickness

189 634 266

1,089 Avg TD

Average Thickness

43 495 89 627 Avg TD

Delta or Subdelta

Sunnyside Delta Complex Bruin Point Subdelta Dry Canyon Subdelta

Bruin Point Subdelta (28 deep holes) Parachute Creek Mbr. (Lake) Garden Gulch Mbr. (Shore) Douglas Creek Mbr. (Delta)

Dry Canyon Subdelta (27 deep holes) Parachute Creek Mbr. (Lake) Garden Gulch Mbr. (Shore) Douglas Creek Mbr. (Delta)

% s s

33.1 30.7 37 .3

% SL

10.6 11.0 9.8

L i t h i

% SH :

47 .9 50.0 44 .1

ology .

% LS

6.8 6.7 7.1

%,,CG

1.5 1.5 1.7

% VOLC

TR TR TR

6.7 2 4 . 9 53.8

6 .3 10.4 14.4

83.7 52.5 27.9

2 .3 11.0

1.6

0.8 1.2 2 .3

8.6 40 .0 36.1

4 .8 9.5

14.9

84.7 40.6 44.2

0 .5 8.2 3.3

1.1 1.7 1.5

0.2

0.3

*base on 1980 -

1981 -1982 -1984 -1988 -

6 holes, 7268 ft (includes top 339 ft of A-1 and top 201 ft of A-4 drilled and logged pre-1980)

9 holes, 9208 ft (excludes 1003 ft shallow pilot mine holes and 585 ft angle hole) 18 holes, 11720 ft (excludes 580 ft shallow pilot mine holes) 10 holes, 7364 ft (excludes 450 ft shallow pilot mine holes) 12 holes, 11858 ft

Table 5. Rock Type Characteristics, Sunnyside Tar Sands

Bitumen Content Rock Type Common Color Fossils

significant: moderate to high

fine grained to very fine grained sandstone

dark gray to black very limited: garpike fish, log fragments and thin coal seams

significant: moderate to high

fine grained to very fine grained sandstone

dark gray to black very limited: ostra-cods, algal debris

significant: fine grained to dark gray to black moderate to high very fine grained

sandstone

limited: ostracods, biota trash, fish scales

moderate: low to moderate, streaky saturation

siltstone tan to brown to black

moderate: low to high

limestone white to black common: ostracods and algal stromatolites

negligible: on some shale fractures near tar zones

negligible: on some shale fractures near tar zones

negligible: on some shale fractures near tar zones

red to maroon to grayish red

mixed colored shale: olive drab, brown, red, purple, green

greenish gray

very limited: root­lets and plant debris

limited: associated algal stromatolites and ostracods

limited to common: fish scales, turtles bone fragments, associated ostracods and thick algal stromatolites

negligible: on some shale fractures

It. olive gray rare to limited: plant debris, small fish, associated very thin algal stromatolites (no ostracods)

Distinguishing Characteristics

channel scour, trough cross bedding, planar bedding, basal IFC's with shale and silt-stone clasts, 1-2% muscovite, subtle fining upward within sandstone sequence

trough cross bedding, planar cross bedding, current ripple lamina­tions with muscovite laminae, basal and internal IFC's with limestone clasts, dis­torted bedding, 2-3% muscovite, subtle fining upward within sandstone sequence

trough cross bedding, planar bedding

Environment Abbreviation of Deposition

distributary channel

DC

Member Occurrence

Tgd&Tgg

distributary mouth bar (proximal)

DMB Tgg&Tgd

beach or beach bar

B or BB all

micro-trough cross bedding, moderate bio-turbation, 1-2% muscovite

levee Tgg&Tgd

micrites to biomicrites nearshore and bay

NS & ID Tgg&Tgd

red shales, limited bioturbation

marsh Tgd

mixed colored laminated interdis-shales, moderate bio- tributary turbation bay

thick green shales, nearshore limited to moderate bioturbation, associa­ted thin limestones with fossils

ID

NS

Tgg

Tgg

It. olive gray shales, laminated to thinly bedded, oil shale with paper shale texture, deformed bioturbation

offshore OS Tgp

Table 6. Mean Composition of Bituminous Sandstones, Sunnyside Tar Sand

A A

u o

u o cu

e « u fa

2

o c

s V V

e c

Constituents

Monocrystalline Quartz Polycrystalline Quartz Orthoclase Microcline Plagioclase Rock Fragments (subtotal)

Mica Accessory Minerals Allochems (ostracods, oolites and carbonate fragments) (subtotal)

Calcite Dolomite

* Hematite

CU

A

I

Ti O >

CO

Pyrite Clay Matrix (subtotal)

Porosity Bitumen (subtotal)

Banks (1981)

X

311.2 ' .2:9 9.7

3.1 15.9

7.8 (70.6)

0 .5 0.4

0 .3 ( 1.2)

0 .8 2 .5 3.8 — . 0.4 0 .5

( 8.0)

4 .3 15.9

(20.2)

Remy (1984)

X

29.3 3.7

11.4

16.9 8.5

(69.8)

0.5 0.4

3.1 ( 4 .0)

1.2 2 .0 1.0 0.4 — 1.2

( 5.8)

17.2 3.2

(20.4)

Total 100.0 100.0

data: Banks (1981) 39 surface samples, bitumen not extracted Remy(1984) 20 core samples, bitumen extracted

compilation: W. Calkin, 1988

01076

Table 7. Core Sample and Well Log Correlations, Sunnyside Tar Sands

Lithology

Sandstone(bit) Sandstone(nonbit) Siltstone Limestone

Oil shale Shale: Gray

Green Mixed Red

Tuff

Unconformity

Gamma (API)

100±30 80±20 130±30 65±25

(peaks to 600) 60±20

70+25

140±20 170±20 100+20 150±50

single peaks of

.Typical Res

Density (gras/cc)

2.25±:05 2.25±.05 2.35±.05 2.45±.05

2.1 ±.10

2.45±.05

2.40±.05 2.40±.05 2.45±.05 UNK as all readings in air

ponses

Focused Electric

(ohm/meters)

1000-20,000 100-1000 100-2000 100-10,000

20-100

200±100 (expanded and serrated pattern) 90±20 60±20 50±10 UNK

Sonic (microsec/ft)

85±5 85±5 80±5 80±15

100

85±15

75±5 75±5 70±5 UNK

200-600 common

TABLE 8 and TABLE 9

DRILL CORE TAR ZONE DATA

EXPLANATION

GL CE TD 21T-21B GP-17 NC ND * THIN NP NA NONBIT WK MOD X BIT 5.6/13.

5 est 114 100M 24+

EOD DF DB B BB OS NS BAY L DMB DC

ground level color elevation total depth designated tar zone, top and bottom top picked by geophysics no core not drilled not a designated tar zone used in mine model less than 5 feet chick not present no analyses nonbituminous weak bitumen content moderate bitumen content

4 weighted average bitumen in wt%/gals per ton 5 wt% bit visual estimate continuous tar sands 114 feet thick multiple tar sands, cumulative thickness noted 24 feet of nonbituminous sandstone drilled; drill hole stopped before full thickness of zone was penetrated environment of deposition delta front distal bar beach beach-bar offshore nearshore interdistributary bay levee distributary mouth bar distributary channel

01078

DRILL CORE TAB ZONE DATA Bruin Point Subdelta Sunnyside Tar Sands

Drill Hole

No. 1 ui m 0\ <M <y, -H

U t-

No. 2

vO

s s Oi O*

U H

No. 3

_ O vO O <M

No. 4

<r r-i

o\ n o\ -*

U H

No. 5

m

S S 0\ TO

U H

No. 6 r- <M

O* —<

o\ «

U E-

No. 7

TO <M

S (N o\ ~-

U H

No. 8

TO m o — o\ — OA —

U H

No. 9

-i m

TO S

U H

No. 10

OA

o\ o\

U H

No. 11

o o ^

2 « U Q

Zone-*-Data-V

Elevation Depth Thickness X Bit EOD

Elevation Depth Thickness X Bit EOD

Elevation Depth Thickness X Bit EOD

Elevation Depth Thickness X Bit EOD

Elevation Depth Thickness X Bit EOD

Elevation Depth Thickness X Bit EOD

Elevation Depth Thickness X Bit EOD

Elevation Depth Thickness X Bit EOD

Elevation Depth Thickness X Bit EOD

I Elevation Depth Thickness X Bit EOD

Elevation Depth Thickness X Bit EOD

10T 10B

ERODED

ERODED

ERODED

ERODED

ERODED

ERODED

ERODED

ERODED

ERODED

ERODED

ERODED

11T 11B

9916-9899 69-86

17 8.4/19.9

BB

THIN

9966-9955 85-96

11 7.0/16.6

BB

THIN

ERODED

THIN

THIN

THIN

THIN

ERODED

THIN

21T 21B

9870-9851 115-134

19 6.0/14.1

BB

9471-9454 155-172

17 6.1/14.4

BB

9917-9907 134-144

10 8.8/20.9

BB

9698-9677 276-297

21 6.2/14.8

BB

9348-9301 55-102

47 5.5/13.1

DMB

9654-9605 263-312

49 5.8/13.6

DMB

THIN

THIN

9542-9527 269-284

15 7.4/17.4

BB

9471-9454 88-105 GP17 4.8/11.4

BB

THIN

22T 22B

9796-9773 189-212

23 7.2/17.0 DMB

9444-9434 182-192

10 7.1/16.7

BB

9880-9871 171-180

9 3.5/8.3

B

THIN

THIN

Combined with

Zone 21

9784-9733 204-255

51 5.0/12.1

DMB

THIN

THIN

9387-9373 172-186

14 4.7/13.8

BB

9838-9802 212-248

36 1.6/14.4 DMB

23T 23B

THIN

9338-9331 288-295

7 8.1/14.4

BB

9839-9830 212-221

9 4.2/9.8

BB

9618-9602 356-372

16 8.6/15.5

BB

9200-9185 203-218

15 3.3/8.0

B

9581-9540 336-377

41 6.6/15.3

DMB

THIN

NS

THIN

NS

THIN

NS

9339-9320 220-239

19 3.8/9.0

BB

9760-9740 290-310

20 7.2/17.0 DMB

25T 25B

9700-9678 285-307

22 5.2/12.8

NS

9285-9264 341-362

21 4.3/10.1

NS

9744-9732 307-319

12 5.9/13.9

NS

9521-9501 453-473

20 3.7/8.8

NS

9169-9144

234-259 25

'3.3/7.7 NS

9472-9459 445-458

13 4.3/10.1

NS

9599-9587 389-401

12 3.6/8.4

NS

9508-9496 400-412

12 3.5/8.3

NS

9370-9345 441-466

25 3.5/8.3

NS

9316-9304 243-255

12 1.3/3.2

NS

9678-9655 372-395

23 4.2/9.8

NS'

26T 26B

9665-9651 320-334

14 3.7/8.6

NS

9252-9248 374-378

4 3.4/8.1

NS

9721-9714 330-337

7 4.0/9.5

NS

9488-9472 486-502

16 1.7/4.0

NS

9126-9115 277-288

11 1.6/3.9

NS

9448-9430 469-487

18 3.8/9.1

NS

9566-9558 422-430

8 2.5/5.8

NS

9485-9469 423-439

16 1.1/2.6

NS

9334-9315 477-496

19 1.4/3.4

NS

9292-9276 267-283

16 0.9/2.1

NS

9642-9627 408-423

15 1.8/4.4

NS

31T 31B

9519-9493 466-492

26 7.5/17.6 DMB

9190-9159 436-467

31 7.1/16.7

DMB

9641-9594 410-457

47 6.8/16.0

DMB

9428-9399 546-575

29 8.9/21.0

DMB

9072-9026 331-377

46 1.4/3.4

L

9404-9364 513-553

40 7.0/16.3

DMB

9537-9446 451-542

77M 5.8/13.5

DMB

9445-9397 463-511

48 6.5/15.4

DMB

9266-9263 545-548

3 4.0/9.0

NS

9249-9216 310-343

33 3.1/8.7

DMB

9580-9564 470-486

16 6.0/14.2

DMB

33T 33B

9450-9425 535-560

25 7.2/16.9

DMB

9091-9078 535-548

13 8.9/20.8

BB

9528-9516 523-535

12 9.8/23.4

BB

9336-9313 638-661

23 7.2/17.0

DC

8955-8938 448-465

17 4.9/11.6

BB

9281-9272 635-644

9 7.5/17.5

BB

9381-9364 607-624

17 8.1/18.9

P:B

9344-9303 564-605

41 7.5/17.7

DC

9206-9201 605-610

5 5.8/13.6

BB

9149-9111 410-448

38 6.4/15.0

DMB

9450-9438 600-612

12 3.4/8.1

NS

35T 35B

9376-9320 609-665

56 7.8/18.4

DC

9019-8991 607-635

28 5.9/14.0

DC

9508-9471 543-580

37 8.0/19.1

DMB

9261-9236 713-738

25 7.1/16.8

DC

8898-8886 505-517

12 4.1/9.7

BB

9197-9085 720-832

112 8.1/18.9

DMB

9324-9316 664-672

8 9.2/21.5

BB

9280-9263 628-645

17 6.9/16.3

BB

9129-9118 682-693

11 8.2/19.3

BB

9064-9034 495-525

30 6.8/16.1

DC

9412-9395 638-655

17 8.9/21.0

BB

36T 36B

9287-9265 698-720

22 8.7/20.6

DC

8954-8895 672-731

59 3.1/7.4

DC

9440-9381 611-670

59 8.6/20.3

DMB

9210-9147 764-827

63 8.1/19.2

DMB

8831-8778 572-625

53 3.5/8.3

DC

9081-9060 836-857

21 6.9/16.0

DMB

9291-9224 697-764

67 7.6/17.8

DC

9197-9132 711-776

65 7.4/17.5

DC

9037-8929 774-822

48 8.5/20.1

DC

8994-8952 565-607

42 7.4/17.5

DC

9365-9293 685-757

72 5.2/12.4

DC

37T 37B

9245-9182 740-803

63 7.7/18.3

DC

8880-874 7 746-879 133M

3.4/8.1 DC

9443-9250 708-801

7 2M 7.3/17.2 BB&DC

9110-9016 864-958

94 8.7/20.5

DMB

8752-8660 651-743

92 3.7/8.8

DC

9081-8955 865-962

97 8.3/19.4

DMB

9204-9101 784-881

103M 6.7/15.6

DC

9101-8992 807-916

109 6.9/16.2

DC

8941-8843 870-968

98 6.7/15.9

DC

8905-8814 654-745

91 3.9/9.2

DC

9287-9220 763-830

67 6.4/15.1

DC

38T 38B

9163-9113 822-872

50 8.3/19.7

DC

8723-8697 903-929

26 2.8/6.7

DC

9154-9129 897-922

25 3.4/7.9

DC

8985-8933 989-1041

52 5.9/13.9

DC

8575-8562 828-840

12 NONBIT

DC

8897-8863 1019-1054

35 8.4/19.7

DC

9078-8993 910-995

85 5.6/13.0

DC

8984-8861 924-1047

100M 5.7/13.7

2DC's

8825-8745 986-1066

80 4.1/9.6

DC

8769-8755 790-804

14 4.7/11.1

DC

9188-9084 862-956

79M 7.0/16.6

DC

41T 41B

9013-8980 972-1005

33 8.0/18.9

DC

ND

9033-8966 1018-1085

67 6.9/16.4

DC

8829-8816 1145-1158

13 6.9/16.4

DC

ND

8798-8769 1119-1148

30 9.0/20.9

DC

8976-8962 1012-1026

14 8.9/20.8

BB

8834-8795 1074-1113

18M 0.1/0.2

BB'S

8720-8697 1091-1114

23 2.6/6.2

DC

8750-8683 809-876

67 3.9/9.3

DC

9065-9031 985-1019

34 2.4/5.6

L

42T 42B

8954-8921 1331-1064

33 7.7/18.1

DC

ND

8961-8934 1090-1117

27 6.4/15.2

DC

8771-8711 1203-1263

60 0.0/0.0

DC

ND

8744-8725 1073-1173

19 NONBIT

DC

8881-8799 1107-1189

82 7.1/16.5

DC

ND

8619-8539 1192-1272

80 4.0/9.3

DMB

ND

8916-8886 1134-1164

30 7.5/17.6

DC

43T 43B

8855-8803 1130-1182

32 6.2/14.7

DC

ND

8912-8891 1139-1160

21 4.1/9.8

DC

8685-8631 1289-1343

54 0.0/0.0

DC

ND

ND

8781-8756 1207-1232

25 NONBIT

DC

ND

ND

ND

8850-8821 1200-1229

29 6.7/15.9

DC

45T 45B

ND

ND

8813-8790 1238-1261

23 0.0/0.0

DC

8626-8586 1348-1338

40 0.0/0.0

DC

ND

ND

ND

ND

ND

ND

8770-8759 1280-1291

11 3.7/8.7

BB

Base of Tar

8788 1197

8697 929

8891 1160

8780 1194

8660 743

8769 1148

8800 1189

8805 1103

8539 1272

8680 879

8755 1295

01079

page 2 of 4

Drill Hole

No. 12

CJ CO

2 £ o -• U E-

No. 13

m a>

cj \o

U E-

No. 14

o t-

t^ o c* -

se No. 15

o O

c

No. 16

CM O

O "i

No. 17 -. lO

( o

No. 18 *0 CM

O N

o u o (J H

No. 19 sj m

CO C

U H

No. 20 sj O

CO —<

c* -.

O H

No. 21

CJ o

co —

U O (J H

No. 22

CO c^ CO c^ sj CO

u a

Zone-* Data +

Elevation Depth Thickness X Bit

EOD

Elevation Depth Thickness X Bit

EOD

Elevation Depth Thickness X Bit

EOD

Elevation Depth Thickness X Bit EOD

Elevation Depth Thickness X Bit

EOD

Elevation Depth Thickness X Bit

EOD

Elevation Depth Thickness X Bit EOD

Elevation Depth Thickness X Bit EOD

Elevation Depth Thickness X Bit EOD

Elevation Depth Thickness X Bit EOD

Elevation Depth Thickness X Bit EOD

10T 10B

ERODED

ERODED

ERODED

ERODED

ERODED

ERODED

ERODED

ERODED

ERODED

ERODED

ERODED

11T 11B

THIN

ERODED

THIN

THIN

THIN

9707-9700 74-81

7 NA DS

THIN

THIN

THIN

THIN

ERODED

21T 21B

9964-9945 138-157

19 7.1/16.9

BB

ERODED

THIN

9869-9858 74-85 11

8.3/19.7 DB

9935-9921 86-100

14 9.3/21.9

DB

9641-9612 140-169

29 5.8/13.8

DHB

9940-9929 96-107 11

7.8/18.4

BB

9811-9799 83-95

12 6.9/16.2

BB

9709-969] 155-173

18 6.4/15.0

BB

9526-9506 296-316

20 6.8/16.1

DMB

9404-9374 84-114

30 6.0/14.1

B

22T 22B

9908-9848 194-204

10 5.7/13.3

B

ERODED

THIN

9822-9812 121-131

10 7.0/16.6

BB

9887-9875 134-146

12 5.9/14.0

BB

THIN

9863-9854 173-182

9 4.5/10.8

B

9771-9753 123-141

18 6.7/15.8

BB

9634-9621 230-243

13 6.5/15.4

BB

THIN

9314-9251 174-237

63 5.4/12.6 DHB

23T 23B

9841-9833 261-269

8 5.5/12.9

BB

9181-9160 24-45 21

3.7/13.4

BB

THIN

NS

ND

THIN

NS

9559-9545 22-236

14 6.4/15.0

BB

9778-9768 256-268

10 5.3/12.5

BB

ND

ND

THIN

NS

Combined with

Zone 22

25T 25B

9749-9726 353-376

23 3.2/7.7

NS

9160-9148 45-57 12

2.0/6.9 NS

9467-9444 293-316

23 3.5/8.2

NS.

26T 26B

9715-9698 387-404

17 2.5/5.9

MS

9138-9130 67-75

8 1.4/3.4

NS

9431-9414 329-346

17 1.5/3.4

NS

31T 31B

9637-9594 465-508

43 6.1/14.4 DMB

9098-9065 107-140

33 7.8/18.5

DC

9376-9354 384-406

22 6.1/14.6

DC

SHALLOW PILOT MINE HOLE

9728-9704 293-317

24 4.2/9.9

NS

9462-9439 319-342

23 NA NS

ND

9696-9677 325-344

19 3.8/8.9

NS

9428-9409 353-372

19 NA NS

9605-9545 416-476

60 6.7/15.7 DMB

9361-9340 420-441

21 6.4/10.2 DMB

33T 33B

9568-9529 534-573

39 5.7/13.5 DMB

9002-8987 203-218

15 3.9/9.3

BB

9311-9297 449-463

14 4.8/11.3

L

9545-9503 476-540

66 5.8/14.0 DMB

THIN

BAY

SHALLOW PILOT MINE HOLE

SHALLOW PILOT MINE HOLE

SHALLOW PILOT MINE HOLE

9347-9323 475-499

24 3.7/8.7

NS

9200-9176 288-312

24 2.6/6.2

NS

9300-9293 522-529

7 NA NS

9152-9144 336-344

8 NA

NS

9249-9232 573-590

17 7.0/16.5

DMB

9105-9086 383-402

19 6.8/16.1 DMB

9202-9121 620-701

81 6.7/15.9 DMB

9000-8995 488-493

5 4.9/11.5

BB

35T 35B

9479-9473 623-629

6 2.8/6.6

NS

8890-8850 315-355

40 5.3/12.6

DC

9220-9170 540-590

50 7.1/16.8 DMB

9392-9372 629-649

20 5.0/11.9

DC

9197-9176 584-605

21 6.7/15.8 DMB

THIN

NS

8919-8893 569-595

26 5.5/12.9

DC

36T 36B

9428-9303 674-799 125

6.0/14.1 DMB

8890-8765 362-415

53 5.4/12.6

DC

9112-9094 648-666

18 6.0/14.1

DC

9336-9281 685-740

55 6.7/15.8 DMB

9113-9084 668-697

29 8.6/20.2 DMB

9017-8953 805-869

64 6.3/14.9

DMB

8853-8819 635-669

34 4.1/9.7

DMB

37T 37B

9272-9220 830-882

52 8.6/20.4 DMB

8740-8692 465-513

48 2.9/7.1

DC

9072-8977 688-783

95 7.6/17.8

DC

9255-9203 766-818

52 8.0/18.9

DMB

9071-8926 710-855 145

6.9/16.3 DC

8918-8809 904-1013

109 4.8/11.3

DC

8772-8727 716-761

45 2.8/6.6

DC

38T 38B

9188-9183 914-919

5 4.3/10.2

B

8682-8648 523-557

34 3.2/7.7

DC

8967-8838 793-922 129

4.7/11.0 DC

9173-9140 848-881

33 9.3/22.1

DC

8907-8837 874-956

82 4.1/9.7

DC

8792-8762 1030-1060

30 3.9/9.4

DC

8704-8667 784-821

37 3.4/8.0

DC

41T 41B

THIN

BAY

8610-8598 595-6C7

12 0.3/0.8

DC

8738-8727 1022-1033

11 1.5/3.5

BB

9034-9004 987-1017

30 7.5/17.7

DC

ND

8752-8707 1070-1115

45 4.7/11.2

DC

8636-8594 852-894

42 2.7/6.3

DC

42T 42B

9022-8941

1080-1161 81

7.8/16.6 DC

ND

8698-8683 1062-1077

15 0.2/0.6

DC

8994-8885 1027-1136

109 5.9/14.0 DMB

ND

8639-8632 1183-1190

7 0.4/1.0

B

ND

43T 43B

8922-8894 1180-1206

26 7.1/16.7

DC

ND

ND

8866-8826 1155-1195

40 6.3/14.9

DC

ND

ND

ND

45T 4 5B

8859-8834 1243-1268

25 0.4/1.0

DC

ND

ND

ND

SD

ND

STJ

/

Base of Tar

8877 1225

8648 557

8727 1033

8821 1200

8825 956

8707 1115

8594 894

llAOl

No. 23

£ £ g -UJ o

No. 24

^

E l e v a t i o n Depth T h i c k n e s s X flit EOD

E l e v a t i o n Depth T h l c l t n e s s X B i t

11B 21T 21B

N 9 9 2 0 - 9 9 0 8

22B 23T 23B 25T 25B 26T 26B 31T 31B 33T 33B 35T 35B 36T 36B 37T

D SliALLOU PILOT HINE MOLE

M T _ _ 4 1 B 42T 42B

10 4 . 6 / 1 0 . 9

BB

i n Compute i

9514-9496 9 4 6 5 - 9 4 4 2 9 3 1 7 - 9 3 0 7 9 2 6 8 - 9 2 4 5 9220-9172 9 1 2 9 - 9 0 3 0 8 9 7 5 - 8 9 2 0 389-407 4 3 8 - 4 6 1 5 8 6 - 5 9 6 6 3 5 - 6 5 8 6 8 3 - 7 3 1 7 7 4 - 8 7 3 9 2 8 - 9 8 3

18 23 10 23 4B 81M 55 N A 5 . 6 / 1 3 . 2 3 - 0 / 7 . 1 4 . 7 / 1 1 . 0 7 . 3 / 1 7 . 2 6 . 9 / 1 6 . 3 8 . 2 / 1 9 . 3

No. 26 E l e v a t i o c Dep th

£ 2 T h i c k n e s s £ < ° X B i t u Q EOD

S l f t na l E l e v a t i o ,

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9 4 7 4 - 9 4 6 2 349 -361

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9 1 2 7 - 9 1 0 1 505 -531

26 4 - 3 / 1 0 . 4

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E l e v a t i o n Depth T h i c k n e s s X B i t EOD

E l e v a t i o n Depth T h i c k n e s s X B i t EOD

E l e v a t i o n Dep th T h i c k n e s s X B i t EOD

E l e v a t i o n Depth T h i c k n e s s X B i t EOD

E l e v a t i o n Dep th T h i c k n e s s X B i t EOD

E l e v a t i o n Dep th T h i c k n e s s X B i t EOD

E l e v a t i o n Depth T h i c k n e s s X B i t 1.0D

E l e v a t i o n Depth T h i c k n e s s X B i t EOO

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10T 10B

9 5 6 0 - 9 5 5 0 2 9 3 - 3 0 3

10 8 . 0 / 1 8 . 2

BB

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8 7 5 6 - 8 7 4 8 59-67

8 5 . 6 / 1 4 . 0

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9384-9367 3 0 9 - 3 2 6

17 5 . 2 / 1 2 . 4

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9262-9257 316-321

5 6 . 2 / 1 5 . 0

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9 3 8 4 - 9 3 5 1 107-140

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33 3 . 5 / 8 . 5

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9 2 2 1 - 9 2 0 6 2 7 0 - 2 8 5

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9 2 1 7 - 9 2 0 3 6 3 6 - 6 5 0

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9 9 3 9 - 9 9 1 9 1 6 5 - 1 8 5

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32 5 . 2 / 1 2 . 4

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9 5 1 3 - 9 4 9 0 1 7 8 - 2 0 1

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22T 22B

HP

THIN

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18 7 . 8 / 1 8 . 6

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9 5 0 5 - 9 4 8 3 2 1 3 - 2 3 5

22 6 . 5 / 1 5 . 6

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9 0 1 1 - 8 9 9 1 6 8 2 - 7 0 2

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8 9 3 1 - 8 9 2 3 7 6 2 - 7 7 0

8 3 . 8 / 8 . 9

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9 4 3 5 - 9 4 0 2 2 5 6 - 2 8 9

33 7 . 1 / 1 7 . 0

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9 3 6 6 - 9 3 4 2 2 0 1 - 2 2 5

24 5 . 5 / 1 3 . 2

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30 7 . 9 / 1 9 . 0

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8 8 8 2 - 8 8 7 6 6 0 9 - 6 1 5

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9 0 4 3 - 9 0 1 8 8 1 0 - 8 3 5

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19 2 e s t

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9 3 5 9 - 9 3 3 6 359-382

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8 8 2 5 - 8 8 0 4 8 6 8 - 8 8 9

21 3 e s t

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9 3 4 2 - 9 3 1 8 3 4 9 - 3 7 3

24 5 e s t

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9 2 8 3 - 9 2 5 9 2 8 4 - 3 0 8

24 S e a t

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8 7 1 0 - 8 6 8 7 8 6 8 - 8 9 1

23 3 e s t

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26 2 e s t

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8 9 9 3 - 8 9 6 8 8 6 0 - 8 8 5

2 5H 3 c s t

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9 7 3 4 - 9 7 1 7 3 7 0 - 3 8 7

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8 2 4 1 - 8 2 1 9 5 7 4 - 5 9 6

22 2 e s t

NS

9 3 2 5 - 9 3 0 6 3 9 3 - 4 1 2

19 2 e s t

NS

8 7 9 1 - 8 7 7 2 9 0 2 - 9 2 1

19 3 e s t

NS

9 3 0 7 - 9 2 8 6 3 8 4 - 4 0 5

21 3 e a t

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9 2 4 8 - 9 2 3 0 3 1 8 - 3 3 7

18 2 e s t

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8 6 7 4 - 8 6 6 6 9 0 4 - 9 1 2

8 3 e s t

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8 7 9 0 - 8 7 7 1 7 0 1 - 7 2 0

19

NS

3 I T 318

8 9 3 7 - 8 9 2 2 9 1 6 - 9 3 1

15 9 . 1 / 2 1 . 8

BB

9 6 9 4 - 9 6 4 9 4 1 0 - 4 5 5

45 4 . 2 / 8 . 4

DMA

8 1 5 7 - 8 1 2 5 6 5 8 - 6 9 0

32 3 . 3 / 7 . 9

BB

9 2 7 9 - 9 2 3 8 4 3 9 - 4 8 0

41 9 . 0 / 2 1 . 7

DMB

8 7 3 7 - 8 7 1 4 9 5 6 - 9 7 9

23 6 . 4 / 1 5 . 4

DMB

9 2 7 5 - 9 2 3 0 4 1 6 - 4 6 1

4 5 6 . 3 / 1 5 . 0

DMB

9 2 1 0 - 9 1 7 2 3 5 7 - 3 9 5

38 6 . 4 / 1 5 . 3

DMB

8 6 3 9 - 8 5 9 8 9 3 9 - 9 8 0

41 5 . 1 / 1 2 . 2

DMB

8 7 3 2 - 8 7 0 6 7 5 9 - 7 8 5

26 7 . 5 / 1 8 . 0

B

32T 32B

NP

DMB

9 6 4 9 - 9 6 0 2 4 5 5 - 5 0 2

47 5 . 9 / 1 4 . 2

DMB

NP

9 2 2 7 - 9 2 0 2 4 9 1 - 5 1 6

25 9 . 1 / 2 1 . 9

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8 6 7 5 - 8 6 6 0 1 0 1 8 - 1 0 3 3

15 5 . 0 / 1 1 . 9

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9 1 9 7 - 9 1 7 7 4 9 4 - 5 1 4

20 7 . 5 / 1 8 . 0

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9 1 4 3 - 9 1 0 3 4 2 4 - 4 6 4

40 8 . 5 / 2 0 . 3

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8 5 5 3 - 8 5 4 5 1 0 2 0 - 1 0 3 3

13 6 . 8 / 1 6 . 3

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33T 33B

NP

BB

9 5 9 1 - 9 5 5 8 5 1 3 - 5 4 6

33 6 . 5 / 1 5 . 4

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8 0 2 3 - 8 0 1 2 7 9 2 - 8 0 3

11 3 . 2 / 7 . 7

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9 1 6 4 - 9 1 4 8 5 5 4 - 5 7 0

16 9 . 7 / 2 3 . 3

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8 6 2 1 - 8 6 1 6 1 0 7 2 - 1 0 7 7

5 5 . 5 / 1 3 . 1

9 1 4 2 - 9 1 2 7 5 4 9 - 5 6 4

15 / 1 6 . 6

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9 1 0 3 - 9 0 6 9 4 6 4 - 4 9 8

34 7 . 4 / 1 7 . 7

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8 4 5 4 - 8 4 4 2 1124-1136

12 4 . 9 / 1 1 . 7

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8 5 8 5 - B 5 6 8 9 0 6 - 9 2 3

17 4 . 0 / 9 . 7

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35T 35B

8 7 6 2 - 8 7 3 2 1 0 9 1 - 1 1 2 1

30 3 . 2 / 7 . 6

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9 5 2 2 - 9 4 6 6 5 8 2 - 6 3 8

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9 0 1 9 - 8 9 6 1 6 7 2 - 7 3 0

58 9 . 2 / 2 2 . 0

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9 0 1 9 - 8 9 8 4 5 4 8 - 5 8 3

35 6 . 4 / 1 5 . 4

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8 3 5 6 - 8 3 3 9 1 2 2 2 - 1 2 3 9

17 0 . 4 / 0 . 8

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8 5 5 3 - 8 5 2 3 9 3 8 - 9 6 8

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36T 36B

8 6 8 1 - 8 6 7 4 1172-1179

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53 5 . 3 / 1 2 . 5

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36 8 . 2 / 1 9 . 6

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15+ 0 . 1 / 0 . 3

8 9 6 1 - 8 B 9 0 7 3 0 - 8 0 1

71 9 . 5 / 2 2 . 8

DC

8 9 4 5 - 8 9 0 7 6 2 2 - 6 6 0

38 8 . 0 / 1 9 . 2

DC

ND

8 5 2 3 - 8 4 8 2 9 6 8 - 1 0 0 9

41 0 . 0 / 0 . 0

99T 99B

ND

9 3 7 7 - 9 3 1 1 7 2 7 - 7 9 3

66 6 . 1 / 1 4 . 7

BB

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a l s o Z-36 7 2 1 - 7 3 3

12 0 . 4 / 1 . 1

ND

MB 5 4 - 8 8 36 8 3 7 - 8 5 6

18 3 . 4 / 8 . 2

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UP

ND

ND

37T 378

ND

9 3 0 2 - 9 2 3 7 8 0 2 - 8 6 7

65 8 . 8 / 2 1 . 2

DH8

ND

NO

ND

8 8 0 2 - 8 7 9 0 8 8 4 - 9 0 1

12 4 . 0 / 9 . 6

DC

8 8 0 9 - 8 7 1 3 7 5 8 - 8 5 4

95M 2 . 7 / 6 . 5

OC

ND

ND

38T 38B

ND

9 1 7 7 - 9 1 5 6 9 2 7 - 9 4 8

21 9 . 0 / 2 1 . 6

8B

ND

ND

ND

8 7 6 8 - 8 7 2 0 9 2 3 - 9 7 1

48 3 . 8 / 9 . 0

DC

8706-8637 8 6 1 - 9 3 0

69 3 . 6 / 8 . 7

DC

HD

ND

41T 41B

ND

9 1 2 0 - 9 0 6 9 9 8 4 - 1 0 3 5

39H 5 . 5 / 1 3 . 2

BSDC

NO

ND

ND

8 6 7 3 - 8 6 3 9 1018-1052

34 3 . 5 / 8 . 3

DC

8 5 8 3 - 8 5 5 9 9 8 4 - 1 0 0 8

24 4 . 3 / 1 0 . 2

B

ND

ND

42T 42B

ND

9 0 2 7 - 8 9 1 7 1077-1187

90H 7 . 1 / 1 7 . 1

2 D C s

ND

ND

ND

8 5 9 7 - 8 5 6 8 1 0 9 4 - 1 1 2 3

29 3 . 7 / B . 8

DC

8 5 1 3 - 8 4 8 2 1 0 5 4 - 1 0 8 5

31 3 . 7 / 8 . 9

DC

ND

ND

43T 43B

ND

8 8 5 5 - 8 8 3 2 1 2 4 9 - 1 2 7 2

23 7 . 7 / 1 8 . 5

DC

ND

ND

ND

8 5 9 7 - 8 5 2 2 1 0 9 4 - 1 1 6 9

45M 3 . 7 / 8 . 9

DC

a l s o Z-42 1 0 8 5 - 1 0 9 9

14 0 . 1 / 0 . 1

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ND

p a g e 4 of

45T 45B

ND

8 7 9 9 - 8 7 7 5 1 3 0 5 - 1 3 2 9

24+ 0 . 1 / 0 . 3

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ND

ND

ND

ND

ND

ND

ND

Base c T a r

8732 1121

8832 1272

8012 8 0 3

9000 718

84 82 1211

•=8522 > 1 1 6 9

8482 1085

8393 1185

8523 968

Pan Am No. 1

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ss

i E l e v a t i o n Depth T h i c k n e s s X 8 1 t EOD

E l e v a t i o n Depth T h i c k n e s s X B i t EOD

E l e v a t i o n Depth T h i c k n e s s X B i t EOD

E l e v a t i o n Depth T h i c k n e s s

n e a r 55

9 7 1 1 - 9 6 9 5 111-127

16 5 . 6 / 1 3 . 5

OB

ERODED

ERODED

n e a r 240

THIN

9 6 4 1 - 9 6 1 8 4 8 - 7 1

23 3 . 7 / B . 8

DB

9 4 8 7 - 9 4 7 7 61 -71

10

8 9 1 9 - 8 8 9 1 3 9 2 - 4 2 0

28 NONBIT

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9 4 0 0 - 9 3 7 9 4 2 2 - 4 4 6

21 6 . 3 / 1 5 . 0

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9 4 8 3 - 9 4 3 7 2 0 6 - 2 5 2

46 5 . 2 / 1 2 . 5

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9 3 6 4 - 9 3 5 3 1 8 4 - 1 9 5

11

8 8 5 5 - 8 8 4 1 4 5 6 - 4 7 0

14 BIT

B

THIN

THIN

9 3 2 4 - 9 2 9 8 2 2 4 - 2 5 0

26

9 2 1 6 - 9 1 9 1 6 0 6 - 6 3 1

25 3 e s t

NS

9 1 6 8 - 9 1 4 5 6 5 4 - 6 7 7

23 2 e s t

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9 1 1 6 - 9 1 0 0 7 0 6 - 7 2 2

16 8 . 1 / 1 9 . 5

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8 4 1 8 - 8 3 9 7 8 9 3 - 9 1 4

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8 9 7 4 - 8 9 1 7 8 4 8 - 9 0 5

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8 3 5 4 - 8 3 0 7 9 5 7 - 1 0 0 4

47 NONBIT

8 8 7 3 - 8 8 1 9 9 4 9 - 1 0 0 3

54 4 . 3 / 1 0 . 2

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THIN

THIN

8 2 6 1 - 8 1 9 3 1050 -1118

54M NONBIT

DC

8 7 9 8 - 8 7 3 8 1024-1084

60 3 . 1 /7 .4 L+2DC's

8 1 8 1 - 8 1 4 1 1130-1170

40 NONBIT

OC

8 6 8 4 - 8 5 7 8 1138-1244

106 NONBIT

OC

3086-8029 1225-1282

57 NONBIT

DC

8 5 2 3 - 8 5 0 1 1299-1321

22 NONBIT

DC

8 0 0 1 - 7 9 7 3 1310 -1338

28 NONBIT

DC

ND

7 9 4 8 - 7 9 1 7 1363-1394

31 NONBIT

DC

ND

7 8 9 9 - 7 8 2 2 1 4 1 2 - 1 4 8 9

77 NONBIT

DC

ND

8372 939

8731 1091

1 0 . 9 / 2 6 . 0 NONBIT

9 1 7 2 - 9 1 4 9 913B-9117 9 1 0 5 - 9 0 4 8 3 7 6 - 3 9 9 4 1 0 - 4 3 1 4 4 3 - 5 0 0

HD 9108

ND 8787

2 . 5 / 6 . 0 4 . 7 / 1 1 . 1 i / 1 8 . 8 3 . 8 / 9 . 2

RCT-12 E l e v a t l o r ^ „ Depth 3 o T h i c k n e s s 01 - X B i t ™ S EOD

RCT-14 E l e v a t i o n « f> Depth -a — T h i c k n e s s

X B i t

C . n / 1 6 . 2 7 . 2 / 5 . 4 7 . 1 / 1 6 . 9 7 . 1 / 1 7 . J

9 4 2 9 - 9 3 6 6 6 3 - 1 2 6

48H 5 . 5 / 1 3 . 1

2 B ' E

9197-9157 295-335

40 4 . 9 / 1 1 . 7

DMB

9147-9106 345-386

41 7 . 4 / 1 7 . 8

DHB

TIITN 9064-8962 428-530

80M 6 . 8 / 1 6 . 4 DCSHB

8899-8843 593-649

56 3 . 5 / 8 . 4

DMB

8827-88D2 665-690

25 0 . 3 / 0 . 6

DC

KD ND

01082

DRILL CORE TAR ZONE DATA Dry Canyon Subdelta Sunnyside Tar Sands

page 1 of 4

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E l e v a t i o n D e p t h T h i c k n e s s X BIT EOD

E l e v a t i o n D e p t h T h i c k n e s s X BIT EOD

E l e v a t i o n D e p t h T h i c k n e s s ' X BIT EOD

E l e v a t i o n Dep th T h i c k n e s s X BIT EOD

E l e v a t i o n Dep th T h i c k n e s s X BIT EOD

E l e v a t i o n D e p t h T h i c k n e s s X BIT EOD

E l e v a t i o n Dep th T h i c k n e s s X BIT EOD

E l e v a t i o n Dep th T h i c k n e s s X BIT EOD

E l e v a t i o n

D e p t h T h i c k n e s s X BIT EOD

E l e v a t i o n D e p t h T h i c k n e s s X BIT EOD

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23T 23B

E r o d e d

9 2 9 7 - 9 2 8 9 1 0 1 - 1 0 9

8 1 . 7 / 4 . 1

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9 2 9 7 - 9 2 8 9 1 1 5 - 1 2 3

B NA BB

25T 25B 26T 26B

E r o d e d

E r o d e d

E r o

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E r o

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9 3 8 6 - 9 3 8 1 1 3 - 1 8

5 NONBIT

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9 2 8 1 - 9 2 6 0 1 1 7 - 1 3 8

21 1 . 5 / 3 . 5

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9 2 2 5 - 9 2 0 2 1 7 3 - 1 9 6

23 5 . 6 / 1 3 . 3

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d e d

d e d

d e d

d e d

9 3 5 0 - 9 3 4 3 4 9 - 5 6

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27 4 . 4 / 1 0 . 6

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20 3 . 5 / 8 . 3

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9 5 5 1 - 9 5 3 2 4 9 - 6 8

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9 6 3 2 - 9 6 1 1 2 0 - 4 1

21 4 . 2 / 1 0 . 2

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9 3 0 3 - 9 2 9 8 9 6 - 1 0 1

5 NA NS

THIN

NS

THIN

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33T 33B

9 4 7 0 - 9 4 5 2 1 3 0 - 1 4 8

18 7 . 1 / 1 7 . 1

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9 4 8 5 - 9 4 4 2 2 4 0 - 2 8 3

43 9 . 8 / 2 3 . 4

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9 5 8 2 - 9 5 5 3 7 0 - 9 9

29 5 . 0 / 1 2 . 0

DMB

THIN

BAY

92C0-9170 6 4 - 9 4

30 2 . 4 / 5 . 7

DMB

9 0 8 3 - 9 0 6 0 3 1 5 - 3 3 8

23 6 . 9 / 1 6 . 6

DMB

9 0 7 7 - 9 0 4 5 3 2 1 - 3 5 3

32 7 . 8 / 1 8 . 8

DMB

9 5 9 7 - 9 5 7 7 2 0 - 4 0

20 5 . 3 / 1 2 . 6

DMB

35T 35B

9 4 0 9 - 9 3 5 9 1 9 1 - 2 3 1

40 7 . 2 / 1 7 . 2

DMB

9 3 8 6 - 9 3 7 3 3 3 9 - 3 5 2

13 1 0 . 4 / 2 4 . 8

BB

9 5 0 4 - 9 4 7 1 8 - 2 9

2 1 7 . 5 / 1 8 . 0

CMB

9 5 4 8 - 9 5 1 8 2 4 - 5 4

30 5 . 7 / 1 3 . 6

DMB

9 5 0 3 - 9 4 4 8 1 4 9 - 2 0 4

55M 8 . 1 / 1 9 . 3 BB & DMB

9 2 0 3 - 9 1 7 4 1 9 6 - 2 2 5

29 5 . 2 / 1 2 . 5

DMB

THIN

NS

9 0 3 8 - 9 0 2 8 3 6 0 - 3 7 0

10 6 . 4 / 1 5 . 4

BB

9 0 2 4 - 9 0 1 6 3 7 4 - 3 8 2

8 7 . 2 / 1 7 . 3

BB

9 5 4 9 - 9 4 9 3 6 8 - 1 2 4

56 7 . 9 / 1 8 . 9

DMB

36T 36B

9 3 4 5 - 9 2 9 3 2 5 5 - 3 0 7

52 7 . 9 - 1 8 . 8

DMB

9 3 4 6 - 9 2 9 5 3 7 9 - 4 3 0

51 5 . 8 / 1 3 . 9

DMB

9 4 5 1 - 9 4 3 2 5 3 - 7 2

IS 5 . 0 / 1 2 . 1

[MB

9 4 8 3 - 9 4 3 5 8 9 - 1 3 7

48 4 . 9 / 1 1 . 7

DMB

9 5 4 9 - 9 5 3 0 1 0 - 3 9

29 8 . 5 / 2 0 . 4

DMB

9 4 2 5 - 9 3 7 1 2 2 7 - 2 8 1

54 6 . 9 / 1 6 . 6

DMB

9 1 3 9 - 9 1 1 3 2 6 0 - 2 8 6

26 7 . 3 / 1 7 . 4

DMB

9 0 3 3 - 8 9 9 3 2 3 1 - 2 7 1

40 8 . 3 / 1 9 . 7

DMB

8 9 5 0 - 8 9 2 5 4 4 8 - 4 7 3

25 5 . 4 / 1 2 . 9

DMB

8 9 5 1 - 8 9 1 3 4 4 7 - 4 8 5

38 5 . 0 / 1 1 . 9

DMB

9 4 6 1 - 9 4 2 3 1 5 6 - 1 8 9

23 5 . 6 / 1 3 . 5

DMB

99T 99B

9 2 6 5 - 9 2 2 5 3 3 5 - 3 7 5

2 5M 6 . 8 / 1 6 . 4

2 BBs

9 2 8 0 - 9 2 1 1 4 7 8 - 5 1 4

36 7 . 0 / 1 8 . 2

DMB

9 3 9 8 - 9 3 6 0 1 0 6 - 1 4 4

32M 6 . 1 / 1 4 . 7 BB S CMB

9 3 9 9 - 9 3 5 9 1 7 3 - 2 1 3

40 6 . 7 / 1 6 . 1

DMB

9 5 1 2 - 9 4 8 4 5 7 - 8 5

28 5 . 7 / 1 3 . 7

L

9 3 4 0 - 9 3 1 3 3 1 2 - 3 3 9

27 7 . 4 / 1 7 . 7

DMB

9 0 5 7 - 9 0 1 3 3 4 2 - 3 8 6

44 6 . 7 / 1 6 . 0

DMB

THIN

NS

8 8 8 8 - 8 8 4 9 5 1 0 - 5 4 9

39 6 . 6 / 1 5 . 7

DMB

8 8 5 9 - 8 8 3 9 5 3 9 - 5 5 9

20 8 . 7 / 2 0 . 8

DMB

9 3 9 7 - 9 3 4 8 2 2 0 - 2 6 9

49 7 . 4 / 1 7 . 7

DMB

37T 37B

9 1 9 3 - 9 1 1 9 4 0 7 - 4 8 1

74 6 . 1 / 1 4 . 7

DMB

9 1 9 5 - 9 1 1 7 5 3 0 - 6 0 8

78 7 . 7 / 1 8 . 5

DMB

9 3 3 9 - 9 3 1 5 1 6 5 - 1 8 9

24 9 . 1 / 2 1 . 7

CMB

9 3 3 3 - 9 2 5 0 2 3 9 - 3 2 2

83M 5 . 9 / 1 3 . 6

2 DMBs

9 4 1 2 - 9 3 4 7 1 5 7 - 2 2 2

65 7 . 8 / 1 8 . 8

DMB

9 2 9 7 - 9 2 4 7 3 5 5 - 4 0 5

50M 6 . 8 / 1 6 . 4 BB & DMB

8 9 7 9 - 8 9 2 1 4 2 0 - 4 7 8

58 2 . 8 / 6 . 7

DMB

8 9 1 9 - 8 9 0 9 3 4 5 - 3 5 5

10 2 . 8 / 6 . 6

BB

8 8 1 1 - 8 7 5 6 5 8 7 - 6 3 7

50 2 . 8 / 6 . 7

DMB

8 8 0 0 - 8 7 4 9 5 9 8 - 6 4 9

51 3 . 2 / 7 . 7

DMB

9 3 1 0 - 9 2 3 4 3 0 7 - 2 8 3

76M 7 . 4 / 1 7 . 7

DMB

38T 38B

9 2 0 8 - 8 9 8 9 5 4 5 - 5 5 9

14 N7VKK

BB

THIN

BAY

THIN

9 1 5 3 - 9 1 3 8 4 1 9 - 4 3 4

15 5 . 9 / 1 4 . 2

B

9 2 4 4 - 9 2 3 4 3 2 5 - 3 3 5

10 5 . 7 / 1 3 . 6

BB

9 1 6 7 - 9 1 3 7 4 8 4 - 5 1 5

30 2 . 7 / 6 . 6

L

8 8 4 6 - 8 8 2 5 5 5 3 - 5 7 4

21 0 . 1 / 0 . 2

DC

8 8 5 9 - 8 8 4 8 4 0 5 - 4 1 6

11 0 . 2 / 0 . 6

DC

8655-8645 7 4 3 - 7 5 3

10 0 . 1 / 0 . 1

DC

8 6 7 0 - 8 6 4 8 728-750

22 0 . 1 / 0 . 2

DC

THIN

NS

41T 41B

9 0 2 8 - 9 0 1 7 5 7 2 - 5 8 3

1 1 4 . 8 / 1 1 . 5

B

8 9 8 4 - 8 9 1 5 7 4 1 - 7 6 9

28 6 . 9 / 1 6 . 4

DC

9 1 7 0 - 9 1 1 7 3 3 4 - 3 8 7

53

3 . 7 / 8 . 9 CMB

9 1 1 2 - 9 0 8 7 4 6 0 - 4 8 5

25 4 . 1 / 9 . 9

DMB

9 2 0 9 - 9 1 3 4 3 6 0 - 4 3 5

75 4 . 5 / 1 0 . 8

DMB

9 0 5 7 - 9 0 0 2 5 9 5 - 6 5 0

55 4 . 8 / 1 1 . 5

DC

ND

ND

ND

ND

9 0 9 2 - 9 0 3 7 5 2 5 - 5 8 0

55 7 . 2 / 1 7 . 1

DC

42T 42B

9 0 0 0 - 8 9 8 9 6 0 0 - 6 1 1

1 1 3 . 2 / 7 . 6

B

8 9 5 2 - 8 8 9 9 7 7 3 - 8 2 6

53 2 . 7 / 6 . 5

DC

9 0 6 2 - 9 0 3 9 4 4 2 - 4 6 5

2 3

0 . 2 / 0 . 4 DC

9 0 7 7 - 9 0 3 4 4 9 5 - 5 3 8

43 3 . 6 / 8 . 7

CMB

9 1 0 2 - 9 0 2 1 4 6 7 - 5 4 8

81M 0 . 3 / 0 . 6

2 DCs

8 9 6 9 - 8 9 5 2 6 8 3 - 7 0 0

17 0 . 1 / 0 . 2

DC

ND

ND

ND

ND

8 9 8 8 - 8 9 5 5 6 2 9 - 6 6 2

33 0 . 1 / 0 . 3

DC

B a s e of T a r

8989 611

8899 826

9100 404

9034 538

' 9109

460

8 9 8 ' 665

8921 478

8890 373

8761 637

8749 649

9023 594

01083

Table 9 p a g e 2 ot 4

D r i l l Hole Da 23B 25T 25B 26T 26B 31T 31B 33T 33B 35T 35B 3 6 T 3 6 B 99T 99B 37T 37B 38T 38B 41T 41B 42T

Base 43T 43B of Tar

No. 41 E l e v a t i o n co ^r Depth ° [o T h i c k n e s s ^ X BIT S H EOD

9179-9167 129-141

12 WK/NA

NS

9143-9111 165-197

32 5 . 3 / 1 2 . 5 BB & NS

9017-9007 291-301

10 3 . 9 / 9 . 3

BB

8984-8948 324-360

36 5 . 8 / 1 3 . 9

DMB

8934-8897 374-411

37 6 . 8 / 1 6 . 2

DMB

8849-8812 459-495

36M 5.8/13.8 2 DMBs

8748-8736 560-572

12 0.4/0.9

L

8746 562

No. 43 Elevation -H r Depth m r Thickness w X BIT

E r o d e d 9267-9218 9159-9137 94-143 202-224 49 22

4.8/11.5 7.9/19.0 BB t. DMB DMB

9118-9055 243-306

63 3.1/7.5 2 DMBs

WK/NA L

8962-8926 399-435

36 0.1/0.2

DC

9055 306

No. 44 Elevation c-i o Depth ^r m Thickness ^ X BIT

E r o d e d 9473-9443 9378-9351 9330-9293 9283-9257 9156-9141 10-40 105-132 153-190 200-226 327-342

30 27 37 26 15 5 . 9 / 1 4 . 1 4 / 9 . 7 7 . 7 / 1 8 . 6 9 . 8 / 2 3 . 5 5 . 9 / 1 4 . 1

CMB BB DMB DMB BB

9108-9072 8999-8983 375-411 484-500

36 16 3 . 4 / 8 . 0 0 . 4 / 0 . 8

DMB DC

9072 411

No.45B E l e v a t i o n r~ *o Depth n *o Th icknes s * X BIT

9254-9235 83-102

19 WK/NA

NS

9190-9166 147-171

24 4.3/10.2

NS

9093-9074 244-263

19 6 . 0 / 1 4 . 4

DMB

9051-9020 281-317

36 7 . 8 / 1 8 . 8

DMB

8990-8964 347-373

26 8.2/19.5

DMB

8919-8881 418-456

38M 3.7/8.9 DMB & BB

8840-8807 497-530

33 4 . 4 / 1 0 . 6

DMB

8761-8711 576-626

50 1 . 1 / 2 . 5

DMB

ND ND ND 8730 607

No. 46 E l e v a t i o n o o Depth En £ Th ickness ^ X BIT u H EOD

E r o d e d 9565-9516 9475-9442 9410-9330 9234-9220 9192-9139 9083-9050 15-64 105-138 170-250 346-360 388-441 497-530 49 33 80M 14 53 33

3.5/8.3 7.7/18.4 6.4/15.4 4.4/10.6 6.0/14.3 0.1/0.2 DMB DMB DMB BB DMB DC

9139 441

No. 47 Elevation Depth

X BIT EOD

E r o d e d 9746-9721 9652-9625 9577-9528 9502-9449 9439-9375 9349-9321 9251-9239 9140-9013 55-105 149-176 224-267 299-352 362-426 452-480 550-562 661-788

50M 27 43 53 64 28 12 127 3 . 4 / 8 . 1 5 . 3 / 1 2 . 7 7 . 3 / 1 7 . 5 6 . 3 / 1 5 . 0 8 . 9 / 2 1 . 3 7 . 6 / 1 8 . 3 6 . 2 / 1 4 . 8 6 . 7 / 1 6 . 1 DMB S, BB DMB DMB DMB DMB DMB BB DMB

8985-8954 8 9 2 1 - 8 9 0 1 816-847 880 -900

31+ 20+ 2 . 8 / 6 . 8 0 . 1 / 0 . 2

DC DC

8963 838

No. 48 E l e v a t i o n i- o Depth £ ~ Th ickness

X BIT EOD a a

E r o d e d 9767-9728 9767-9728 9605-9577 9552-9515 9512-9477 9402-9323 9286-9266 9167-9132 9083-9067 10-49 75-117 172-200 225-262 265-300 375-454 491-511 610-645 694-710

39 42 28 37 35 79 20 35 16 7 . 5 / 1 8 . 0 4 . 5 / 1 0 . 8 9 . 2 / 2 2 . 0 3 . 4 / 8 . 0 8 . 7 / 2 0 . 8 7 . 2 / 1 7 . 3 2 . 8 / 6 . 8 7 . 2 / 1 7 . 1 0 . 3 / 0 . 7

DMB 2 BBS DMB DMB DMB DC DMB DC DC

ND 9133 644

No. 49 E l e v a t i o n m o Depth —i o

Thickness X BIT

E r o d e d 9565-9513 9485-9417 50-102 130-198 52 68

7.5/18.0 8.6/20.6 DMB DMB

9405-9378 9334-9304 210-237 281-311

27 19M 1 0 . 0 / 2 8 . 1 8 . 5 / 2 0 . 4

BB 2Bs

THIN 9 1 1 5 - 9 0 7 0 9031-9015 500-545 584-600

36M 16 7 . 1 / 1 6 . 9 N3NBIT

BAY DC i BB BB

9070 545

No. 50 E l e v a t i o n -i o Depth *o r~ Th ickness °; X BIT

No. 51 E l e v a t i o n o% o Depth *n *& Th ickness

E r o d e d

X BIT EOD

E r o d e d

9586-9573 45-58

13 7 . 8 / 1 8 . 8

B

9561-9541 70-90

20 8 . 4 / 2 0 . 1

BB

9549-9525 20-44

24 6 . 8 / 1 6 . 4

DMB

9496-9444 135-187

52 8 . 7 / 2 0 . 8

DMB

9507-9458 62-111

49 8 . 2 / 1 9 . 8

DMB

9432-9364 199-267

68 5 . 0 / 1 2 . 1

DMB

9426-9369 143-200

57 7 . 2 / 1 7 . 1

DMB

9354-9315 277-316

39 8 . 7 / 2 0 . 8

DMB

9358-9290 211-279

68 7 . 8 / 1 8 . 8

DMB

9283-9199 348-432

84 7 . 3 / 1 7 . 8

DC

9272-9226 297-343

46M 8 . 5 / 2 0 . 4

DC

9169-9156 462-475

13 7 . 0 / 1 6 . 7

B

9163-9084 406-485

79M 7 . 1 / 1 6 . 8

DMB

9070-8959 561-672

111 8 . 2 / 1 9 . 1

DMB

9054-8989 515-580

65 6 . 4 / 1 5 . 4

DMB

8937-8920 694-711

17 5 . 6 / 1 3 . 3

BB

8956-8909 613-660

47 1 . 3 / 3 . 0

DC

8903-8881 728-750

22 0 . 0 / 0 . 0

DC

ND

8920 711

8925 644

01084

Table 9 page 3 of 4

Drill Hole

No. 53

\C o

W Q U H

No. 54

O <N r-- r--

W Q CJ H

No. 55

00 00 r--

W O U H

No. 56

00 CT\ r--

M o U H

No. 57

in o

r--as W O u H

No. 58

( o r--

W Q U H

No. 59 (N O o o 00 -H CT\

W Q

No. 61 -<r -<r -3- m o>

W Q

No. 62 00 O r-- m -<r m

&• W Q U H

Zone-> Data +

Elevation Depth Thickness X BIT EOD

Elevation Depth Thickness X BIT EOD

Elevation Depth Thickness X BIT EOD

Elevation Depth Thickness X BIT EOD

Elevation Depth Thickness X BIT EOD

Elevation Depth Thickness x BIT EOD

Elevation Depth Thickness X BIT EOD

Elevation Depth Thickness X BIT EOD

Elevation Depth Thickness X BIT EOD

23T 23B 25T 25B 26T 26B 31T 31B 33T 33B 35T 35B 36T 36B 99T 99B 37T 37B 38T 383 AIT A1B 42T A2B A3I Base

A3B of Tar

Eroded 9188-9162 91A9-9130 138-16A 177-196

26 19M 2 . 1 / 5 . 0 WK/NA

NS NS

E r o d e d

E r o d e d

E r o d e d

E r o d e d

E r o d e d

E r o d e d

E r o d e d

E r o d e d

THIN

NS

THIN

NS

ND THIN THIN 8925-8873 8826-8789 87A9-8706 ND ND A01-A53 500-537 577-620

52 37 A3 7.8/18.7 A.2/10.2 1.2/2.9

NS NS DMB BB DC

9608-958A 95A7-9A97 9A69-9A06 9368-9355 9319-923A 9198-9173 9106-90A1 8991-8991

ND

99-123 2A

2.9/7.1 BB

160-210 38M

7.0/16.8 BB 4 B

238-301 63

8.5/20.5 DMB

339-352 13

7.9/18.9

388-A73 85

7.5/17.9 DMB

509-529 20

A. 8/11.5 Distal DMB

601-666 65

7.6/18.1 DMB

716-726 10+

0.0/0.0 DC

8721 605

9030 677

9760-9728 SHALLOW PILOT MINE HOLE 21-53 32

10.1/24.3 DMB

9759-97A3 SHALLOW PILOT MINE HOLE 22-38 16

5.2/12.5 BB

9783-9776 SHALLOW PILOT MINE HOLE 12-19 7

5.7/13.6

+• Zone 31 •+ 9769-9760 9738-9731 30-39 and 61-68 9 7

6.3/15.2 7.9/19.0 B BB

-i- Zone 31 •* 9762-9758 97A0-9730 A0-AA and 62-72 A 10

A.A/10.A 6.1/14.6 BB B

SHALLOW PILOT MINE HOLE

SHALLOW PILOT MINE HOLE

9A29-9400 55-8A 29

6.A/15.3 BB

9A56-9423 22-55 33

6.6/15.9 DMB

9335-9276 1A9-208

59 6.3/15.2

DMB

9362-9359 116-129

13 10.5/25.2

DC

9227-9188 257-296

39 5.5/13.3

DMB

9283-9269 195-209

1A 3.7/8.9

B

91A6-9126 338-358

20 5.0/12.0

BB

9251-9198 227-280

53 3.A/8.1

DC

906A-9016 A20-463 38M

2.3/5.5 2 DCs

9184-9137 294-341

47 1.8/4.4

DMB

8948-8940 536-544

8 0.1/0.2

DC

9054-9042 424-436

12 4.5/10.3

BB

ND

9008-8960 470-518

48 1.1/2.5

DMB

ND

ND

9016 468

8977 501

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AMOCO CORPORATION

July 20, 1989

G. I. Bresnick, MC 4903, Chicago V. G. Butler, RBOSC, Denver R. D. Kaplan, Naperville, H-4 R. L. Marcus, Denver APC D. J. Soderberg, Naperville, H-l R. W. Walker, MetroWest-SFD

Geologic Summary Report of the 1988 Exploration Program Sunnyside Tar Sands Project

Attached for your use is the final report (Vol. I, IIA, IIB, and III) on the 1988 geologic work performed last summer. The report, prepared by W. S. Calkin, our consulting geologist, includes measured section information on three additional sites in and outside of the conceptual mine area, and geologic interpretation of the twelve core holes completed in the 1988 drilling program.

Geologic interpretation of the resource confirms the distribution of tar sands is controlled by both structure and lithology. Structural control is associated with a northwest trending flexure which was first noted in 1986. Lithologic control is determined by porous and permeable sandstones deposited in the Sunnyside delta complex. Most significant in the exploration work is the identification and quantification of an area of very rich tar sands at South Knoll in the Amoco South (previously Mono Power) properties as noted in Drill hole A-67.

Geologic information has been utilized to update Sunnyside geologic model; this work is expected to be completed by August. A study to investigate alternative mining strategies to capitalize on the South Knoll will be addressed subsequently with completion of a mining study due in March, 1990.

P ; E ' 7 ? 7 P 9 ^ ' 0 0 9 3 1 Phone 717-2445 Metrowest-SFD Naperville

GET/amv/8902

Attachments

W. S. Calkin, w/o attachments R. D. Hall, Metrowest-SFD, w/o attachments E. G. Wollaston, Naperville, H-l, w/o attachments File: TS-25.6