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EXPLANATORYNOTES
SHEET SG 51-9 INTERNATIONAL INDEX
DEPARTMENT OF MINERALS AND ENERGY
GEOLOGICAL SURVEY OF WESTERN AUSTRALIA
WILUNA
SECOND EDITION
1:250 000 SHEETWESTERN AUSTRALIA
Further details of geological publications and maps produced by theGeological Survey of Western Australia can be obtained by contacting:
Information CentreDepartment of Minerals and Energy100 Plain StreetEast Perth WA 6004Phone: (08) 9222 3459 Fax: (08) 9222 3444www.dme.wa.gov.au
FAR
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GOVERNMENT OFWESTERN AUSTRALIA
1:250 000 GEOLOGICAL SERIES
WILUNAWESTERN AUSTRALIASECOND EDITION
SHEET SH 51-9 INTERNATIONAL INDEX
by
T. R. FARRELL
Perth, Western Australia 2001
GEOLOGICAL SURVEY OF WESTERN AUSTRALIA
1:250 000 GEOLOGICAL SERIES — EXPLANATORY NOTES
MINISTER FOR STATE DEVELOPMENT; TOURISM;
SMALL BUSINESS; GOLDFIELDS–ESPERANCE
The Hon. Clive Brown MLA
DIRECTOR GENERAL
L. C. Ranford
DIRECTOR, GEOLOGICAL SURVEY OF WESTERN AUSTRALIA
Tim Griffin
Copy editor: D. P. Reddy
REFERENCEThe recommended reference for this publication is:FARRELL, T. R., 2001, Wiluna, W.A. (2nd edition): Western Australia Geological Survey,
1:250 000 Geological Series Explanatory Notes, 28p.
ISSN 0729–3720
National Library of Australia Card Number and
ISBN 0 7307 5683 1
Grid references in this publication refer to the Australian Geodetic Datum 1984 (AGD84)
Printed by Haymarket Bureau, Perth, Western Australia
Copies available from:
Information Centre
Department of Minerals and Energy
100 Plain Street
EAST PERTH, WESTERN AUSTRALIA 6004
Telephone: (08) 9222 3459 Facsimile: (08) 9222 3444
www.dme.wa.gov.au
iii
CONTENTS
INTRODUCTION ............................................................................................................... 1
Physiography, climate, and vegetation ........................................................................... 1
Previous investigations ................................................................................................... 3
Nomenclature .................................................................................................................. 4
REGIONAL GEOLOGICAL SETTING ............................................................................ 4
PRECAMBRIAN GEOLOGY ............................................................................................ 6
Agnew–Wiluna greenstone belt ...................................................................................... 7
Merrie greenstone belt .................................................................................................... 8
Yandal greenstone belt .................................................................................................... 8
Dingo Range greenstone belt .......................................................................................... 9
Mount Fisher greenstone belt ......................................................................................... 9
Archaean Yilgarn Craton .............................................................................................. 10
Ultramafic rocks (Au, Aup, Aus, Aut, Aux) ............................................................... 10
Fine-grained mafic rocks (Ab, Aba, Abf, Abg, Abip, Abm, Abs, Aby) ...................... 10Medium- to coarse-grained mafic rocks (Aog, Aogf, Aogo) .................................... 11
Felsic volcanic and volcaniclastic rocks (Af, Afp, Afdp, Afi, Afs, Aft) ...................... 12
Sedimentary rocks (As, Asc, Asd, Ash, Ass, Ac, Aci) ................................................ 12
Metamorphic rocks (Alqf ) ....................................................................................... 13
Quartzofeldspathic gneiss (Anq, Angb) .................................................................... 13
Granitoid rocks (Ag, Agm, Agg, Aga, Agd, Agmh, Agdq, Ags, Agmp, Agb,
Agf, Agnq, Agzq, Agz) .............................................................................................. 14
Quartz veins (q) ........................................................................................................ 15
Palaeoproterozoic mafic dykes (#d) ............................................................................. 15
Palaeoproterozoic Yerrida Basin .................................................................................. 15
Yerrida Group .......................................................................................................... 15
Windplain Subgroup ............................................................................................ 16
Juderina Formation (#Yj, #Yjf, #Yjb) .............................................................. 16
Johnson Cairn Formation (#Yc) ...................................................................... 16
Mooloogool Subgroup ......................................................................................... 16
Thaduna Formation (#Yt) ................................................................................ 16
Killara Formation (#Yk, #Ykd, #Ykc, #Ykb) .................................................... 16
Maraloou Formation (#Ym) ............................................................................. 17
Palaeoproterozoic Earaheedy Basin .............................................................................. 17
Earaheedy Group ...................................................................................................... 17
Yelma Formation (#Ey) ....................................................................................... 17
Frere Formation (#Ef ) ......................................................................................... 17
Windidda Formation (#Ed) ................................................................................. 18
Chiall Formation (#Ecw) ..................................................................................... 18
iv
Unassigned Proterozoic sedimentary rocks (#s) .......................................................... 18
Structure ........................................................................................................................ 18
Metamorphism .............................................................................................................. 19
PALAEOZOIC GUNBARREL BASIN ............................................................................ 20
Permian Paterson Formation (Pa) ................................................................................. 20
CAINOZOIC GEOLOGY ................................................................................................. 20
ECONOMIC GEOLOGY ................................................................................................. 21
Gold ............................................................................................................................... 21
Nickel ............................................................................................................................ 21
Uranium ........................................................................................................................ 22
REFERENCES .................................................................................................................. 23
APPENDIX
Gazetteer of localities ........................................................................................................ 28
FIGURES
1. Regional geological setting of WILUNA .......................................................................... 2
2. Physiography and simplified Cainozoic geology of WILUNA ........................................ 3
3. Simplified geological map of WILUNA ........................................................................... 5
4. Grey-scale image of total magnetic intensity for WILUNA ............................................. 8
TABLE
1. Summary of the geological history of WILUNA .............................................................. 6
1
Explanatory notes on the Wiluna1:250 000 geological sheet,Western Australia (second edition)
by T. R. Farrell
INTRODUCTION
The WILUNA* 1:250 000 geological sheet (SG 51-9) covers an area in the north EasternGoldfields Province (Fig. 1) bounded by latitudes 26°00'S and 27°00'S, and longitudes120°00'E and 121°30'E. The map is named after the town of Wiluna†, in the western partof the sheet area.
Access to WILUNA is via the Kalgoorlie–Meekatharra road, which services the town ofWiluna, or the Wongawol Road, which joins the Gunbarrel Highway at Carnegie on theSTANLEY sheet to the northeast. There are also graded roads connecting Wiluna to Sandstoneand the Yeelirrie, Barwidgee, Granite Peak, Cunyu, and Jundee homesteads (Fig. 2). Stationtracks and numerous mineral exploration grid lines provide good access to most areasunderlain by greenstones, but access is difficult to areas underlain by Archaean granitoidrocks or Proterozoic rocks due to the scarcity of tracks.
The sheet area is sparsely populated. The only permanent settlements are the town ofWiluna, small aboriginal communities at Kukabubba and Ngangganawili, mining campsfor the Wiluna and Jundee–Nimary gold mines, and the pastoral stations of Lake Way,Lake Violet, and Millrose.
PHYSIOGRAPHY, CLIMATE, AND VEGETATION
WILUNA is typically flat to undulating, ranging in altitude from about 490 m AustralianHeight Datum (AHD) around Lake Way in the southwest, to more than 600 m in the west.The main physiographic features on WILUNA are the playa lake systems of Lake Way inthe southwest and Lake Ward in the north, an unnamed easterly trending saline drainagein the southeast, and dissected plateaus of Proterozoic rocks in the northeast and central-west (Finlayson Range; Fig. 2). Mount Alice West, in the Finlayson Range, is the highestpoint in the area at 640 m AHD.
Areas underlain by greenstones are characterized by low strike-ridges of resistant rocks,subdued hills with rubbly outcrop and ferruginous debris, and broad valleys covered insheetwash and alluvium. Areas underlain by granitoid rocks are dominated by extensivesandplains, with scattered outcrops and small breakaways in areas of recent erosion.Proterozoic units in the west and northeast are gently dipping and typically form steep-sided plateau remnants. Prominent scarps in the Finlayson Range, north and west of Wilunatownship, have relative reliefs of up to about 50 m.
* Capitalized names refer to standard 1:250 000 map sheets, unless otherwise indicated.† Australian Map Grid (AMG) coordinates of localities on WILUNA mentioned in the text are listed in the
Appendix.
2
The climate of the area is semi-arid to arid, with an average annual rainfall of approximately254 mm*. The rainfall tends to be sporadic and varies markedly from year to year. Thesummers are hot, with maximum temperatures commonly in excess of 40°C, whereas thewinters are cool to mild with occasional frosts and an average maximum temperature inJuly of 19°C.
Most of Wiluna falls within the Murchison Region of the Eremaean Botanical Province(Beard, 1990), except for the area underlain by Proterozoic rocks in the northeastern corner,which lies in the Gascoyne Region. The following description of the vegetation on WILUNA
is mainly from Beard (1990).
The Murchison and Gascoyne Regions are dominated by mulga (Acacia aneura) country.Vegetation on areas of alluvium and sheetwash is characterized by low mulga woodlandwith a variety of small shrubs (mainly Cassia and Eremophila species), and various grassesand ephemeral herbs. Small trees (including Eucalyptus camaldolensis and Casurina obesa)grow adjacent to the larger watercourses. The vegetation on areas of outcrop is typifiedby mulga scrub, with other less abundant Acacia species, and a variety of shrubs (includingEremophila and Cassia). Spinifex (Triodia basedowii) grassland, with scattered trees
* Climate data from Commonwealth Bureau of Meteorology website, 2001.
Figure 1. Regional geological setting of WILUNA (modified from Myers and Hocking, 1998)
Wiluna
Laverton
Leonora
YILGARN
CRATON
EaraheedyBasin
YerridaBasin
BryahBasin
DUKETONSIR SAMUEL
LEONORA LAVERTON
WILUNA
100 km
Greenstone
Granitoid and quartzofeldspathic gneiss
Fault
Town
TRF45 22.03.01
123°120°
26°
27°
28°
121°30'
Phanerozoiccover
3
30 km
TRF46 22.03.01
Homestead
Community
Road
Playa deposits
Sandplain deposits
Colluvium and sheetwash
Calcrete
Duricrust
Archaean greenstone and associated elluvium
Kukabubba
Jundee
LakeVioletWiluna
NgangganawiliCommunity
LakeWay
Mine
Town
Archaean granitoid rock and associated elluvium
LakeWay
MillroseJundee–Nimary
Wiluna
Cunyu
Mt AliceWest
Mt Fisher
FINLAYSON
RA
NG
E
Proterozoic rocks Prominent hill
26°00'121°3
0'
120°0
0'
27°00'
LakeWard
Figure 2. Physiography and simplified Cainozoic geology of WILUNA
(mainly marble gum, Eucalyptus gongylocarpa) and small shrubs, is present in areas coveredby sandplains. Salt-tolerant plants, including saltbush (Atriplex species), bluebush(Maireana species), and samphire (Halosarcia species), grow in open, low-lying areas aroundlake systems.
PREVIOUS INVESTIGATIONS
Most of the early work on WILUNA focused on the gold deposits around the town of Wiluna(Blatchford, 1899; Gibson, 1908; Montgomery, 1909; Talbot, 1920; Edwards, 1953).
4
Sofoulis and Mabbut (1963) presented the first regional geological account of the area,and this was followed by the first edition map and Notes for WILUNA by Elias and Bunting(1981, 1982). Extensive hydrogeological work was also carried out in the area surroundingWiluna (Ellis, 1954; Chapman, 1962; Morgan, 1962; Brookfield, 1963; Sanders, 1973).
The WILUNA 1:250 000 sheet was remapped at 1:100 000 scale in the 1990s by theGeological Survey of Western Australia (GSWA) and the Australian Geological SurveyOrganisation (AGSO). Three 1:100 000 maps — LAKE VIOLET (Stewart and Bastrakova,1997), BALLIMORE (Blake and Whitaker, 1996a), and SANDALWOOD (Blake and Whitaker,1996b) — were published by AGSO. The remaining three 1:100 000 maps — MILLROSE
(Farrell and Wyche, 1997), CUNYU (Adamides et al., 1998), and WILUNA (Langford and Liu,1997) — were published by GSWA. Descriptions of the geology of the individual 1:100 000sheets are presented in Stewart (1997), Adamides et al. (1998), Farrell and Wyche (1999),Langford et al. (2000), and Whitaker et al. (2000).
Published works on the mine geology and gold mineralization at Wiluna includeMcGoldrick (1990), Hagemann et al. (1992), Kent and Hagemann (1996), and Chanter et al.(1998). The geology of the Matilda gold deposits, in the Coles mining centre south ofWiluna, is described by Morgan and El-Raghy (1990). Descriptions of the goldmineralization and geology of the Jundee–Nimary deposits are presented in Phillips et al.(1998a, 1998b) and Byass and MacLean (1998), and the setting of the deposits and controlson mineralization are discussed by Vearncombe (1998, 2000). The geology of the MountFisher gold mine, in the southeastern part of WILUNA, is described by Powell et al. (1990).
Nickel mineralization in ultramafic rocks at Honeymoon Well is detailed in Donaldson andBromley (1981), Gole and Hill (1990), and Gole et al. (1996). Aspects of the geology andvolcanology of the ultramafic rocks are also discussed by Hill et al. (1990, 1995).
Ferguson (1998) presented a compilation of the mineral occurrences on WILUNA. Briefdescriptions of aspects of the geology, exploration, and mineralization of various small partsof the area, mainly in the greenstone belts, can also be found in open-file statutory mineralexploration reports held in the Department of Minerals and Energy’s library in Perth.
NOMENCLATURE
All greenstones on WILUNA have undergone low- to medium-grade metamorphism.However, primary textures are preserved in many cases, and it is commonly possible toidentify the parent rock. In view of this, igneous or sedimentary terminology has been usedwherever possible. Metamorphic rock names have only been used in areas where the rockshave been extensively recrystallized and the protolith is no longer clear.
The nomenclature of the igneous rocks largely follows the recommendations of theInternational Union of Geological Sciences (Le Maitre et al., 1989). Komatiite refers toultramafic rocks with a platy olivine-spinifex texture (cf. Arndt and Nisbet, 1982), and high-Mg basalt refers to mafic volcanic rocks with varioles or relict pyroxene-spinifex texture.
REGIONAL GEOLOGICAL SETTING
WILUNA covers an area of Archaean granite–greenstone terrain on the northeastern marginof the Yilgarn Craton (Fig. 1), and small areas of the Palaeoproterozoic Yerrida (Occhipintiet al., 1997) and Earaheedy Basins (Pirajno, 1999; Fig. 3). The granite–greenstone terrainconsists of elongate belts of deformed and metamorphosed volcano-sedimentary rocks, and
5
30 km
TRF47 11.04.01
Earaheedy Group
Mafic dyke
Fault
EARAHEEDY BASIN
YIL
GA
RN
C
RA
TO
N
YIL
GA
RN
C
RA
TO
N
Yerrida Group
Syenite
Granitoid rock, mainly monzogranite
Interleaved foliated granitoid and mafic rocks
Quartzofeldspathic gneiss dominant
Chert and banded iron-formation
Metamorphosed felsic rock dominant
Porphyritic dacite; metamorphosed
Intermediate volcanic rock; metamorphosed
Metamorphosed mafic rock dominant
Metamorphosed ultramafic rock dominant
Hornblende quartz monzonite andminor quartz diorite
Granitoid rock and quartzofeldspathic gneissin various proportions
Layered sequence of quartzofeldspathic gneiss,monzogranite, and metamorphosed mafic rock
Mixed sequence of metamorphosedsedimentary and felsic rocks
YERRIDA BASIN
Metasedimentary rock dominantProterozoic sedimentary rock, unassigned
Merriebelt
Yandalbelt
Agnew–Wiluna
belt
DingoRange
beltMountFisher
belt
26°00' 12
1°3
0'
12
0°0
0'
27°00'
Wiluna
Wiluna
Erraw
alla
Fault
Cunyu
Jundee
Jundee–Nimary
LakeViolet
Millrose
Mt Fisher
Town
Homestead
Mine
Figure 3. Simplified geological map of WILUNA
large intervening areas of granitoid rock and gneiss, both of which belong to the EasternGoldfields Province (Gee et al., 1981; Griffin, 1990). The Yerrida Basin contains ac. 2.2 – 1.9 Ga volcano-sedimentary succession that lies unconformably on Yilgarn Cratonbasement. The Earaheedy Basin succession comprises deformed, c. 1.85 – 1.8 Ga, shallow-marine and fluviodeltaic sedimentary rocks that are unconformable on both the YilgarnCraton and Yerrida Basin (Pirajno, 1999; Jones et al., 2001).
6
The Precambrian rocks are overlain in the east by Phanerozoic sedimentary rocks of theGunbarrel Basin, (formerly part of the Officer Basin; Hocking, 1994), scattered outliers ofwhich are present in the northeastern corner of WILUNA. Much of the bedrock geology isobscured by Cainozoic regolith.
A summary of the geological history of WILUNA is presented in Table 1.
PRECAMBRIAN GEOLOGY
Greenstone belts in the north Eastern Goldfields Province contain a wide range of rocks,including chert, banded iron-formation (BIF), clastic sedimentary rocks, and ultramafic tofelsic volcanic and volcaniclastic rocks (Fig. 3). There are also local areas of conglomeratethat postdate the main greenstone sequences, and late felsic to intermediate dykes and plugs.The greenstones were deposited between c. 2750 and c. 2660 Ma (Kent and Hagemann,1996; Nelson, 1997a,b, 1998), and deformed and metamorphosed at grades ranging fromprehnite–pumpellyite to amphibolite facies (Binns et al., 1976).
Table 1. Summary of the geological history of WILUNA
Age (Ma) Tectonic event
c. 2750–2700 Deposition of early greenstone succession in Agnew–Wiluna belt (and other
greenstone belts?)
2747 ± 11(a) Intrusion of granitoid precursor to quartzofeldspathic gneiss; northern end of
Yandal belt
D1 deformation: tight to isoclinal folding in gneisses; foliation in early
greenstones
c. 2700–2690 Deposition of greenstones
c. 2685–2655 D2 deformation: strong foliation parallel to granite–greenstone contact;
main phase of granitoid intrusion
c. 2670–2655 Felsic to intermediate volcanism in Yandal belt
2658 ± 2(a) Intrusion of post-D2 granitoid dyke into gneiss at northern end of Yandal belt
c. 2650–2635(b) Late-stage granitoids; syenite to diorite and low-Ca monzogranite
c. 2640(b) D3 deformation: north to northwesterly trending shear zones and upright
folds
D4 deformation: kink folds and crenulations
c. 2400 Intrusion of Palaeoproterozoic mafic dykes
c. 2200–1900 Deposition of Yerrida Group in a rift-related basin
c. 1850–1800 Deposition of Earaheedy Group in a passive-margin setting
?c. 290 Deposition of Paterson Formation
SOURCES: (a) AGSO, OZCRON database
(b) Nelson (1997b, 1998)
7
There are few published studies on the structural geology of the north Eastern GoldfieldsProvince (e.g. Platt et al., 1978; Eisenlohr, 1989; Hammond and Nisbet, 1992; Farrell, 1997;Vearncombe, 1998), and interpretation of the structure has been hampered by the poorexposure in the region. The following summary of the structure is based on work carriedout during 1:100 000-scale mapping on the DUKETON, SIR SAMUEL, and WILUNA 1:250 000sheets.
Four regional Archaean deformation events (D1–D
4) have been recognized in the north
Eastern Goldfields Province (Hammond and Nisbet, 1992; Farrell, 1997; Wyche and Farrell,2000). Evidence of an early deformation is locally preserved in c. 2750–2700 Ma gneissesadjacent to greenstones (Farrell, 1997), but the nature of this event is unclear. The seconddeformation coincided with a period of extensive granitoid intrusion at c. 2685–2655 Ma,and was followed by a later phase of granitoid magmatism after c. 2650 Ma, including asuite of alkaline rocks (Smithies and Champion, 1999). The granitoid rocks range incomposition from diorite to granite, but monzogranite is by far the most abundant rocktype. The third deformation event occurred at c. 2640 Ma within a broadly east–westcompressional regime and resulted in the development of major, north to northwesterlytrending shear zones and the regional foliation trends. This event was followed by late-stage crenulation and kinking of all earlier structures. Numerous faults and fracture zonescut across all Archaean structures. The faults correspond to prominent aeromagneticlineaments, and many are intruded by Proterozoic mafic–ultramafic dykes (Hallberg, 1987)or quartz veins.
There are five greenstone belts on WILUNA — the Agnew–Wiluna, Merrie, Yandal, DingoRange, and Mount Fisher belts (Griffin, 1990; Fig. 3) — as well as small rafts of greenstoneswithin the granitoids. All greenstones in the region are poorly exposed, and much of theinterpreted geology is based on data obtained from mineral exploration drilling programs,and regional-scale (400 m line-spacing) aeromagnetic surveys (Fig. 4).
AGNEW–WILUNA GREENSTONE BELT
The Agnew–Wiluna belt (Fig. 3) in the western part of WILUNA contains a metamorphosedsequence of ultramafic, mafic, and felsic volcanic, and sedimentary rocks, as well as youngerconglomerate (Jones Creek Conglomerate). Ultramafic rocks host major nickel deposits atPerseverance, Six Mile, and Mount Keith (all on SIR SAMUEL), and Honeymoon Well onWILUNA. Large gold deposits are present at Wiluna and Agnew (on LEONORA).
The section of the Agnew–Wiluna belt exposed on WILUNA can be divided into easternand western domains separated by the Erawalla Fault (Fig. 3; Hagemann et al., 1992;Langford et al., 2000). Strongly deformed metasedimentary rocks adjacent to the ErawallaFault may be equivalent to the Jones Creek Conglomerate on SIR SAMUEL (Durney, 1972;Marston and Travis, 1976; Marston, 1978; Liu et al., 1998). In the eastern domain,Hagemann et al. (1992) described a westerly younging stratigraphy around the Wilunamining centre, and Gole and Hill (1990) described a westerly younging stratigraphy nearHoneymoon Well. A correlation between the successions at Wiluna and Honeymoon Wellwas proposed by Liu et al. (1995). In their stratigraphy, the lowest preserved unit, whichconsists of basalt and gabbro, is overlain by a unit dominated by basalt, including bothhigh-Mg and tholeiitic basalt. Felsic volcanic and sedimentary rocks, and a regionalultramafic unit (Liu et al., 1995), overlie the basalt. The uppermost unit consists ofsedimentary and felsic volcanic rocks.
There is no readily identifiable stratigraphy in the western domain because the mafic-dominated succession is poorly exposed and possibly repeated by folding. However, the
8
local presence of BIF and the absence of thick ultramafic units suggest that the sequenceis not the same as that east of the Erawalla Fault.
The age of the Agnew–Wiluna belt is poorly constrained. The only published sensitivehigh-resolution ion microprobe (SHRIMP) U–Pb zircon date from the northern part is2749 ± 7 Ma for a microdiorite dyke from the Wiluna mine (Kent and Hagemann, 1996).This age is supported by a SHRIMP U–Pb zircon date of 2720 ± 14 Ma for a felsic volcanicunit from near the Rockys Reward mine on SIR SAMUEL (Nelson, 1997b), and by aconventional U–Pb zircon date of 2795 ± 38 Ma for a granophyric differentiate from alayered gabbro near Yakabindie (on SIR SAMUEL; Cooper and Dong, 1983).
MERRIE GREENSTONE BELT
The southern tip of the Merrie greenstone belt extends onto the northwestern corner ofWILUNA, east of Cunyu Homestead. Exposure of this belt is poor, and the only outcropsare of extremely weathered mafic rock. On NABBERU, to the north, the Merrie greenstonebelt contains a metamorphosed succession of basalt, subordinate gabbro, and ultramaficrock, and local felsic and sedimentary rocks (Adamides, 2000).
YANDAL GREENSTONE BELT
The Yandal greenstone belt (Fig. 3) in the central part of WILUNA contains a large volumeof felsic volcanic and volcaniclastic rocks. Although there are a number of thin komatiite
Figure 4. Grey-scale image of total magnetic intensity for WILUNA (400 m line spacing, data fromAGSO and GSWA, 1994)
30 kmTRF48 26.02.01
12
0°0
0'
27°00'
26°00' 121
°30
'
9
and high-Mg basalt units, the Yandal belt does not have the thick units of ultramafic rockthat characterize the Agnew–Wiluna belt, and there is no known economic nickelmineralization.
The Yandal belt contains several major gold deposits (Jundee–Nimary on WILUNA
and Bronzewing, Mount McClure, and Darlot on SIR SAMUEL) and numeroussmaller deposits, and remains an area of significant gold exploration activity (Phillips et al.,1998a).
Poor exposure and a scarcity of younging indicators hinder determination of a detailedstratigraphy for the part of the Yandal greenstone belt on WILUNA (Fig. 3). In the northernhalf of the sheet, the belt bifurcates into two arms separated by an extensive area ofgranitoid rocks and gneiss. Outcrop mapping and examination of numerousmineral exploration drillholes (Stewart and Bastrakova, 1997; Farrell and Wyche, 1999)have allowed the western arm of the belt to be divided into three main lithologicalpackages:• an eastern sequence dominated by mafic and ultramafic rocks, with locally abundant
felsic volcanic and subvolcanic rocks (the Middle Greenstone Sequence of Phillips et al.,1998a);
• a thick central sequence of felsic volcanic and sedimentary rocks (the Upper GreenstoneSequence of Phillips et al., 1998a);
• a thin western sequence of mafic and ultramafic rocks, and prominent chert and BIF(the Lower Greenstone Sequence of Phillips et al., 1998a).
Pillow lava structures in high-Mg basalt in the mafic–ultramafic-dominated eastern sequenceindicate younging to the west. This is supported by sedimentary structures in drillcore fromthe Jundee gold mine.
There are few published geochronological data from the Yandal greenstone belt. In thesouthern part of the belt, on SIR SAMUEL, a SHRIMP U–Pb zircon age of 2690 ± 6 Ma wasdetermined for a porphyritic rhyolite from the Spring Well complex, and an age of2702 ± 5 Ma for porphyritic rhyolite from the Darlot mine (Nelson, 1997b). In the northernpart of the belt on WILUNA, a SHRIMP U–Pb zircon age of 2669 ± 10 Ma was obtainedfor a dacite porphyry from within the central sequence near Camel Bore (Nelson, 1998).Post-mineralization dykes at Jundee and Mount McClure have SHRIMP U–Pb zircon datesof 2668–2656 Ma (Yeats et al., 1999).
DINGO RANGE GREENSTONE BELT
The Dingo Range greenstone belt, which extends onto the southeastern corner of WILUNA
(Fig. 3) from SIR SAMUEL, contains a metamorphosed mafic–ultramafic sequence with thininterbeds of chert and BIF, and minor amounts of felsic and clastic sedimentary rocks. Thinunits of tremolite–chlorite schist and strongly deformed felsic rock are abundant. The partof the Dingo Range greenstone belt on WILUNA is almost completely obscured by regolith.The age of the Dingo Range greenstone belt is unknown.
MOUNT FISHER GREENSTONE BELT
The Mount Fisher greenstone belt is poorly exposed in the southeastern corner of WILUNA.Little is known about this belt, but it may be related to the Dingo Range greenstone belt.There are sparse weathered outcrops of mafic, ultramafic, and felsic rocks, as well as thinunits of chert. The age of the belt is unknown.
10
ARCHAEAN YILGARN CRATON
Ultramafic rocks (Au, Aup, Aus, Aut, Aux)
Ultramafic rocks are widely distributed through the Agnew–Wiluna and Yandal greenstonebelts on WILUNA. However, in most cases, the rocks are poorly exposed and much of thesurface exposure has been affected by deep weathering, resulting in the formation of adistinctive light-brown, siliceous caprock (Czu). Ultramafic rocks are typically in thin,laterally extensive units or lenticular bodies.
Ultramafic rocks on WILUNA have been separated into five units: undivided metamorphosedultramafic rock (Au), metamorphosed peridotite (Aup), serpentinite (Aus), talc–chlorite schist(Aut), and metamorphosed pyroxenite (Aux). Minor ultramafic rock types not shownseparately include tremolite–chlorite schist, talc–carbonate schist, and serpentinized dunite.
Undivided metamorphosed ultramafic rock (Au) is used mainly to describe fine-grained,deeply weathered, deformed, and locally altered ultramafic rocks where the original rocktype could not be positively identified. Serpentinized peridotite (Aup) is a fine- to medium-grained, granular, weakly foliated rock with well-preserved cumulate textures. Olivinecrystals are pseudomorphed by serpentine-group minerals. Fine-grained aggregates ofmagnetite, plus one or more of talc, tremolite, and chlorite, occupy the intercumulus areas,which were probably filled originally by pyroxene and magnetite. A minor associated rocktype is serpentinized dunite. Massive serpentinized ultramafic rock (Aus), lackingidentifiable primary textures, outcrops on the western edge of the Agnew–Wiluna belt nearBridal Well. Metamorphosed pyroxenite (Aux) forms a small body within granitoid rockson the western side of the Yandal belt, south of the Wongawol road.
There are patchy exposures of strongly deformed talc–chlorite(–carbonate) schist (Aut) inhigh-strain zones in all three greenstone belts, particularly near granite–greenstone contacts.The rock is soft, well foliated, typically fine grained, and contains finely intergrown talcand chlorite, as well as minor amounts of carbonate and finely dispersed opaque minerals(probably magnetite).
Fine-grained mafic rocks (Ab, Aba, Abf, Abg, Abip, Abm, Abs, Aby)
Metamorphosed mafic rocks are a major component of the greenstone sequences on WILUNA.
Undivided, metamorphosed mafic rock (Ab) is common throughout the Agnew–Wiluna,Yandal, and Dingo Range greenstone belts. The unit includes deeply weathered and veryfine grained mafic rocks, as well as subordinate interleaved metamorphosed gabbro andthin interbeds of metamorphosed sedimentary rock. It also includes some areas ofmetamorphosed tholeiitic basalt and plagioclase-phyric basalt that are too small to be shownseparately.
Amphibolite (Aba) is the dominant mafic rock type in areas of higher metamorphic grade,and is common in greenstone enclaves within granitoid rocks and in the greenstonesequences close to the granite–greenstone contacts. Amphibolite (Aba) consists mainly ofacicular hornblende and plagioclase, and is typically well foliated with a strong lineationdefined by the alignment of hornblende. In the Dingo Range belt, amphibolite is commonlyinterleaved with metamorphosed gabbro and tremolite schist. Amphibolite (Aba) is also aminor component of quartzofeldspathic gneiss (Anq), and mixed units containing gneisses(Angb, Agnq). In gneisses, the amphibolite is typically fine to medium grained and layeredon a scale of 5–30 mm, according to variations in the abundance of dark-green hornblendeand plagioclase. The rocks also contain subordinate pale-green clinopyroxene (?diopside)
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and quartz, plus accessory sphene, epidote, and iron oxides. There are lenses of amphibolite(Aba), up to 1 km long and 400 m wide, north of Deadwood Bore on the western edge ofWILUNA. These amphibolite bodies are interpreted as metamorphosed gabbro. The weakdeformation of the amphibolite lenses, and the presence of fine-grained margins andoffshoots into the surrounding strongly deformed granitoid rocks, suggests that they haveintruded the granitoids.
Strongly foliated metamorphosed mafic rock (Abf ) is common along the margins of theAgnew–Wiluna belt in the Coles Find* area. Also common in areas close to the granite–greenstone boundary is a mixed unit of strongly foliated mafic rock with abundantinterleaved, deformed granitoid rock (Abg).
Metamorphosed porphyritic basaltic andesite (Abip) is only encountered in explorationdrillholes in the northern part of the Yandal belt near Panakin Bore and in the Jundee area.The rock consists of albitized plagioclase phenocrysts set in a recrystallized matrix ofplagioclase and actinolite, with minor chlorite, biotite, and epidote.
Metamorphosed high-Mg basalt (Abm) includes basaltic volcanic rocks characterized bypyroxene-spinifex textures or varioles. The best exposure of high-Mg basalt is southeastof the Jundee–Nimary gold mine in the Yandal belt. Here, the rock has abundant variolesand a locally preserved relict pyroxene-spinifex texture, consisting of randomly orientedtremolite–actinolite pseudomorphs of igneous pyroxene set in a fine-grained matrix oftremolite–actinolite, chlorite, epidote, albite, and fine-grained opaque minerals. Locally,the rock contains pillow structures that indicate younging to the west (Farrell and Wyche,1999). The basalt is spatially associated with metamorphosed fine-grained gabbro.
Fine- to medium-grained, well-foliated, chlorite-rich mafic schist (Abs) is restricted to afew small outcrops in the Yandal belt north of Millrose Homestead, although it has alsobeen noted in drillholes in the Jundee area. The origin of this rock is unclear — it may bederived from mafic volcaniclastic rocks, high-Mg basalt, or ultramafic rocks.
Metamorphosed amygdaloidal basalt (Aby) is a minor mafic rock type in the Yandal belt.Amygdales are a common feature in the mafic volcanic rocks, but amygdaloidal basalt israrely in mappable units. The amygdales are up to 15 mm in size, and contain assemblagesof pale amphibole, subordinate albite, and minor amounts of epidote and sphene. The hostbasalt is typically fine grained and consists of quartz, plagioclase, epidote, and actinolite.
Medium- to coarse-grained mafic rocks (Aog, Aogf, Aogo)
Medium- to coarse-grained mafic rocks form intrusions or coarser intervals in mafic volcanicsuccessions. Metamorphosed gabbro (Aog) is common in all the greenstone belts on WILUNA,and also includes dolerite or microgabbro and areas of basalt with abundant gabbrointrusions. The primary minerals are pseudomorphed by metamorphic assemblages ofamphibole, plagioclase, and minor, fine-grained opaque minerals (?ilmenite), and localquartz. The rocks may be intergranular, granular, subophitic, or locally porphyritic. Stronglyfoliated metamorphosed gabbro (Aogf) is typical of areas adjacent to the granite–greenstonecontact, such as the Coles Find area.
Metamorphosed olivine gabbro (Aogo) is present in a small intrusive body near Twin TanksWell in the Yandal belt. The rock is fine to medium grained and undeformed, and containsclinopyroxene, plagioclase, a skeletal opaque mineral (?magnetite), and altered, anhedral
* Labelled as Coles mining centre on the 1:250 000 map sheet.
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?olivine up to 4 mm in size. The olivine is pseudomorphed by very fine fibrous chlorite,acicular tremolite, and fine-grained, granular epidote.
Felsic volcanic and volcaniclastic rocks (Af, Afp, Afdp, Afi, Afs, Aft)
Metamorphosed felsic rocks are common in the Yandal belt near Lake Violet Homestead,and in the northern end of the Agnew–Wiluna belt, but are only a minor component of theDingo Range belt. In most cases the felsic rocks are poorly exposed and affected by deepweathering.
Undivided metamorphosed felsic volcanic and volcaniclastic rocks (Af ) are typicallykaolinized and silicified. Relict quartz is common in hand specimen and assists in theidentification of the rocks. Deeply weathered felsic rocks have only been subdivided wherethey have a relict porphyritic texture (Afp).
Metamorphosed dacite porphyry (Afdp) is exposed in fresh, rubbly outcrops south of CamelBore in the Yandal belt (Farrell and Wyche, 1999). The rock is undeformed and seriatetextured to porphyritic. Plagioclase and quartz crystals, up to 16 mm in size, are set in afiner grained groundmass of quartz, plagioclase, and minor biotite, with metamorphic whitemica, chlorite, sphene, epidote, ?pumpellyite, and very fine iron oxides. The dacite porphyrycontains some scattered, irregular aggregates of chlorite and epidote, and clusters of?pumpellyite, which may be former amygdales. The rock has a SHRIMP U–Pb zircon dateof 2669 ± 10 Ma (Nelson, 1998).
Metamorphosed intermediate rocks (Afi) are a minor component of the greenstone sequencesin the Yandal belt. They range in composition from basaltic andesite to dacite. These rockstypically contain plagioclase phenocrysts (up to 6 mm), and altered mafic minerals in afine-grained groundmass of quartz and plagioclase, with small amounts of chlorite and ironoxides, and accessory zircon, apatite, and epidote. These rocks are interpreted to be dykesor shallow-level intrusions.
Strongly deformed felsic schist (Afs) is present in areas of higher metamorphic grade alongthe greenstone margins. The schist is typically well foliated and contains relict, partlyrecrystallized quartz grains in a foliated matrix of quartz, white mica, and plagioclase. Thenature of the protolith is unclear, but is thought to have been a felsic volcanic orvolcaniclastic rock.
Felsic tuff (Aft) in the Agnew–Wiluna belt includes eutaxitic tuff with euhedral relicts offeldspar pyroclasts up to 1 mm, and ignimbritic tuff with relict feldspar clasts and pumicelapilli up to 5 mm.
Sedimentary rocks (As, Asc, Asd, Ash, Ass, Ac, Aci)
Metamorphosed sedimentary rocks on WILUNA can be divided into two broad categoriesaccording to their composition and mode of deposition — metamorphosed clasticsedimentary rocks (As, Asc, Asd, Ash, Ass) and metamorphosed chemical sedimentary rocks(Ac, Aci).
Undivided metamorphosed clastic sedimentary rocks (As) are deeply weathered and poorlyexposed. They are a minor component of the greenstone sequences on WILUNA, and typicallyform thin units within volcanic successions, or more extensive units with a significantvolcaniclastic component. The sedimentary rocks are typically well foliated and difficultto classify due to deep weathering.
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Metamorphosed sandstones (Ass) in the Yandal belt are broadly felsic in composition,and contain subrounded to well-rounded clasts of quartz, plagioclase, and felsic rock, in afine-grained metamorphosed matrix. Metamorphosed polymictic conglomerate (Asc) is aminor component of the sedimentary successions in the Yandal belt near Strife Bore. Therock is weathered and contains large (up to 300 mm), well-rounded clasts of massive chert,felsic rock, and BIF in a fine-grained mafic matrix.
Metamorphosed fine-grained sedimentary rocks (Ash) include metashale and metasiltstone,and are poorly exposed and deeply weathered. Locally, they are thin bedded and, in freshdrillhole samples, consist of scattered, fine sand-sized clasts of quartz and plagioclase in avery fine grained matrix of metamorphic quartz, albite, white mica, and opaque minerals.Graphite-bearing varieties are present locally. Metamorphosed carbonate-rich sedimentaryrocks, dominantly metadolomite (Asd), outcrop in one area northwest of Abercromby Wellin the Agnew–Wiluna belt.
Metamorphosed chert (Ac) forms extensive strike ridges throughout the greenstonesequences, and is a minor but distinctive rock type that can be a useful local stratigraphicmarker. There is a range from finely layered chert through to green-grey and brown-greymassive chert. The layering is typically 1 to 30 mm thick, and defined by variations iniron oxide and silica content. Chert units commonly have well-developed mesoscale folding,and some are brecciated or cut by late-stage fractures.
Metamorphosed BIF (Aci) is restricted to the western side of the Yandal belt, and the westernside of the Agnew–Wiluna belt around Deep Bore. Rhythmic layering in the BIF is typicallyplanar and laterally continuous, and up to 4 mm thick. The layering comprises alternatingsilica-rich and iron-oxide-rich zones, and is locally magnetite bearing. On the western sideof the Yandal belt, the BIF is associated with a metamorphosed succession of ferruginouschert, clastic sedimentary rocks, and ultramafic rock.
Metamorphic rocks (Alqf )
Quartz–feldspar schist (Alqf ) is a strongly foliated felsic rock, probably derived from felsicvolcanic or volcaniclastic rocks. The rock is associated with felsic schist, adjacent to theErawalla Fault, east of Bridal Well.
Quartzofeldspathic gneiss (Anq, Angb)
Gneisses underlie large areas on WILUNA, but the rocks are poorly exposed, being coveredmainly by sandplain and Cainozoic sheetwash deposits. The quartzofeldspathic gneissesare multiply deformed and intruded by granitoids in many locations, and are older than alldated granitoid rocks. This is illustrated by a SHRIMP U–Pb zircon date of 2747 ± 11 Mafor a gneiss near the northern end of the Yandal belt (AGSO, OZCRON database), and therange of granitoid dates from 2658 to 2648 Ma (Nelson, 1998; AGSO, OZCRON database).
Quartzofeldspathic gneiss is present both as distinct, mappable units (Anq) and as acomponent of mixed units of granitoid rock and gneiss (Angb, Agnq, see Granitoid rocks).The rock commonly shows a diffuse layering defined by variations in grain size and modalmineralogy, and is multiply deformed. Locally, the gneiss contains two generations ofleucosomes and granitic veins. Early leucosomes are thin, rich in quartz, and parallel to arelict S
1 foliation. The leucosomes were folded during the D
2 event, and in high-strain zones
they are largely transposed in the S2 foliation. The first-generation leucosomes are cut by
a second generation of thicker, monzogranite leucosomes that are commonly subparallelto the S
2 foliation. Both the host gneiss and the early leucosomes are cut by an undeformed,
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porphyritic monzogranite dyke that has been dated at 2658 ± 2 Ma (AGSO, OZCRONdatabase).
A north-northwesterly trending belt in the central-northern part of WILUNA, at Amees Bore,contains a layered succession of quartzofeldspathic gneiss and metamorphosed hornblendemonzogranite, quartz monzonite, and mafic rock (Angb). The exposure is poor, butindividual layers appear to be less than 100 m thick. The monzogranite is a hornblende-bearing, fine- to medium-grained, well-foliated rock containing sparse clots of hornblendeup to 10 mm in diameter. There appears to be a gradation from hornblende monzograniteto hornblende-bearing quartz monzonite (Agzq, see Granitoid rocks). Numerous thin layers(less than 5 m thick) of mafic rock are also present. The main mafic rock type is a foliatedand lineated amphibolite (Aba, see Mafic rocks) with a crude layering defined by variationsin plagioclase content, and the alignment of thin, plagioclase-rich leucosomes. Epidotealteration of the succession is common and affects all rock types.
Granitoid rocks (Ag, Agm, Agg, Aga, Agd, Agmh, Agdq, Ags, Agmp, Agb, Agf, Agnq,Agzq, Agz)
Many areas of exposed granitoid rock are deeply weathered and have been mapped asundivided granitoid rock (Ag) if the primary mineralogy could not be ascertained. In areaswhere the rocks can be positively identified, biotite monzogranite (Agm) is by far thedominant rock type. Minor granitoid rocks types include granodiorite (Agg), fine-grainedaplitic granitoid (Aga), and dykes of diorite to quartz diorite (Agd). Hornblende-bearingmonzogranite (Agmh) and quartz diorite (Agdq) are only observed in drillhole samples. Abody of syenite (Ags) in the Yandal belt, west of Jundee Homestead, is not exposed, buthas been identified from exploration drillholes and aeromagnetic images.
Biotite monzogranite (Agm) is widespread on WILUNA. The rock is variously deformed andtypically fine to medium grained with local, sparsely porphyritic zones. The monzograniteconsists of quartz, plagioclase, K-feldspar, small amounts of biotite, opaque minerals, andaccessory epidote, allanite, sphene, and zircon. Porphyritic biotite monzogranite (Agmp)is present on the edge of the Yandal greenstone belt, near Millrose Homestead, and formsdykes in quartzofeldspathic gneiss east of Amees Bore.
Foliated granitoid rock with interleaved mafic rocks (Agb) outcrops along the eastern sideof the Agnew–Wiluna greenstone belt near Honeymoon Well. Aeromagnetic images suggestthat these rocks extend much farther north, in an area covered extensively by regolith. Themafic rocks typically form discontinuous layers or lenses in the granitoids, along with minoramounts of high-grade metasedimentary rock. Strongly deformed granitoid rock with minorquartzofeldspathic gneiss (Agf ) outcrops on the edge of the Agnew–Wiluna belt, nearHoneymoon Well, and north of Mount Wilkinson. Locally, the rock has biotite-richschlieren and a diffuse layering.
Over much of WILUNA, granitoid rocks are intimately associated with quartzofeldspathicgneiss and migmatite on a scale too small for the individual rock types to be shownseparately. Deep weathering and poor exposure also make it difficult to determine theproportions of each rock type, and so they are mapped as a mixed unit of granitoid rockand gneiss (Agnq). Granitoid rocks in this unit commonly have a diffuse layering andabundant biotite-rich schlieren.
There are several large bodies of quartz monzonite (Agzq) in the northern part of WILUNA.The quartz monzonite around Lake Ward is known only from mineral exploration drillholesand aeromagnetic data. The rock ranges in composition from monzogranite to quartz diorite
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and quartz monzonite. The dominant rock type is a weakly deformed, medium-grainedquartz monzonite containing equal proportions of plagioclase and K-feldspar, variousamounts of hornblende and clinopyroxene, and minor quartz and biotite. The quartzmonzonite east of Panakin Bore has been dated at 2664 ± 4 Ma (Nelson, 1999) on NABBERU,just north of WILUNA.
Quartz monzonite is also a component of the layered gneissic sequence near Lignan Welland at Amees Bore (Angb), where it appears to be in thin layers (less than 30 m thick).The monzonite in this sequence is a fine- to medium-grained rock containing K-feldspar,plagioclase, various amounts of quartz (5–20 vol.%), and minor sphene and myrmekite(after K-feldspar). Accessory minerals include iron oxides, apatite, epidote, and rare zircon.In contrast to the large bodies of quartz monzonite, the monzonite in the layered sequencedoes not contain clinopyroxene or biotite. Monzonite (Agz) has also been noted inexploration drillholes in parts of the Yandal belt.
Quartz veins (q)
Quartz veins (q) are ubiquitous on WILUNA, but in most cases are too small to be shown onthe map. Strongly deformed quartz veins are common in the greenstones. These veins aretypically subparallel to the regional foliation and boudinaged or folded. A younger set ofquartz veins, consisting of interlocking crystals of milky quartz and local iron oxides after?pyrite, cuts across the regional foliation trends and forms upstanding ridges in areas ofpoorly exposed granitoid rocks. These veins are typically east to northeasterly trending andparallel to linear magnetic features. Associated with these crosscutting quartz veins is aset of complex veins consisting of multiple generations of quartz veins, and variouslybrecciated and silicified wallrock.
PALAEOPROTEROZOIC MAFIC DYKES (#d)
Mafic dykes (#d) that cut across the granite–greenstone terrain on WILUNA belong to a suiteof Palaeoproterozoic mafic dykes found throughout the Yilgarn Craton (Hallberg, 1987).On WILUNA the dykes range in composition from gabbro to diorite or granophyric gabbro.They rarely outcrop, but are apparent on aeromagnetic images as distinct, linear anomalies(Fig. 4). Easterly trending mafic dykes outcrop between Granite Well and Terry Bore, eastof the town of Wiluna.
PALAEOPROTEROZOIC YERRIDA BASIN
Yerrida Group
Palaeoproterozoic sedimentary rocks of the 2.2 – 1.9 Ga Yerrida Group were deposited inthe Yerrida Basin, on the western border of WILUNA. The group has been divided into theWindplain and Mooloogool Subgroups (Occhipinti et al., 1997). The lowermost unit, theWindplain Subgroup, consists of sedimentary rocks deposited in fluvial and tidalenvironments in a continental sag basin (Occhipinti et al., 1997). The Mooloogool Subgroupcomprises basal turbidites and conglomerate, overlain by rift-related mafic volcanic andvolcaniclastic rocks, evaporites, and chemical sedimentary rocks.
On WILUNA the Windplain Subgroup is represented by the Juderina Formation, a siliciclasticunit with local stromatolitic carbonates and evaporites (Adamides et al., 1999; Langfordet al., 2000). The Mooloogool Subgroup is represented by the Killara Formation, which isa succession of subaqueous to subaerial lava flows and mafic sills, with local evaporitesand chemical sedimentary rocks (Adamides et al., 1999; Langford et al., 2000).
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Windplain Subgroup
Juderina Formation (#Yj, #Yjf, #Yjb)
The Juderina Formation (#Yj), at the base of the Yerrida Group, is a shallow-water sequenceof quartz sandstone with minor siltstone, chert breccia, and conglomerate. Two distinctivesubunits, the Finlayson and Bubble Well Members, have been recognized (Occhipinti et al.,1997). The formation outcrops around the margins of the Yerrida Basin, where it typicallyforms resistant ridges up to 60 m high.
The Finlayson Member (#Yjf ) is a unit of mature quartz sandstone and subordinate quartzsiltstone at the base of the Juderina Formation. The dominant rock type is an off-white,silica-cemented quartz sandstone with abundant ripple marks, and local brown diageneticspots. The sandstone is thin to thick bedded (a few centimetres to 1 m thick), and consistsof well-rounded quartz grains (0.2 – 0.5 mm in diameter) and minor detrital zircon,tourmaline, biotite, and rutile.
The Bubble Well Member (#Yjb; Gee and Grey, 1993) is a unit of chertified carbonateand evaporitic sedimentary rocks near the base of the Juderina Formation that is interpretedas a facies of the Juderina Formation (Adamides et al., 1999). The Bubble Well Memberhas both well-bedded and chaotic breccia facies. The unit typically consists of layers ofchert breccia, chert with a wavy microbial lamination, and chertified stromatolitic dolomite.An outcrop 2 km north of Top Kukabubba Well contains stromatolites of the speciesWilunella glengarrica (Grey, K., pers. comm. in Adamides et al., 1999).
Johnson Cairn Formation (#Yc)
The Johnson Cairn Formation (Occhipinti et al., 1997) is not exposed on WILUNA, but isinferred, from mapping on the GLENGARRY 1:100 000 sheet to the west, to underlie an areaon the western edge of WILUNA. In the type area, the formation consists of iron-rich shaleand minor carbonate.
Mooloogool Subgroup
Thaduna Formation (#Yt)
The Thaduna Formation (Occhipinti et al., 1997; originally named the ‘Thaduna Greywacke’by Gee, 1979) is not exposed on WILUNA, but is interpreted to underlie part of thenorthwestern edge of the sheet. The contact with the underlying Johnson Cairn Formationis inferred to be conformable (Bagas, 1998). The formation consists of lithic sandstoneand hematitic shale, and is interpreted as a proximal turbidite sequence (Occhipinti et al.,1997).
Killara Formation (#Yk, #Ykd, #Ykc, #Ykb)
The Killara Formation (#Yk; Occhipinti et al., 1997) consists mainly of dolerite and basalt,with local chertified microbial laminates near the top of the unit and is thought to be theresult of continental volcanism related to the rifting of the Yerrida Basin (Occhipinti et al.,1997). The Killara Formation interfingers with rocks of the Juderina and MaraloouFormations along the northeastern margin of the Yerrida Basin.
Dolerite sills belonging to the Killara Formation (#Ykd) have been preferentially intrudedalong siltstone layers at three different stratigraphic levels in the Juderina Formation
17
(Adamides et al., 1999). The dolerite consists of plagioclase, orthopyroxene, clinopyroxene(?augite), and magnetite, and has local interstitial granophyric intergrowths of quartz andfeldspar. The rock is microporphyritic in places.
Basalt of the Killara Formation (#Ykb) outcrops in an arcuate belt around the eastern edgeof the Yerrida Basin on WILUNA (Adamides et al., 1999). The basalt is fine grained andhas intergranular or intersertal textures. Microporphyritic varieties are developed in someareas. Clinopyroxene, plagioclase, and titanomagnetite, along with secondary chlorite,quartz, sphene, and prehnite, are the main constituents. There are thinner layers and chertyinterflow sedimentary rocks in the upper parts of the basalt.
The Bartle Member (#Ykc) is a thin, laterally discontinuous unit of chert, tuffaceous rocks,chertified sedimentary rocks, and thin lava flows (Occhipinti et al., 1997; Pirajno and Grey,1997). Deposition of the unit is interpreted to have occurred in a hot-spring environment(Pirajno and Grey, 1997). The unit consists largely of chert, and attains a maximumthickness of about 10 m. The chert is locally laminated, with cherty siltstone and ironstonein places. Bartle Member cherts locally contain silica pseudomorphs of rhomb-shapedcrystals (probably dolomite), globular iron-hydroxide structures, and spherulites ofchalcedonic silica (Adamides et al., 1999).
Maraloou Formation (#Ym)
The Maraloou Formation (Occhipinti et al., 1997) is not exposed on WILUNA, but has beeninferred to underlie part of the western edge of the area, based on mapping on theGLENGARRY 1:100 000 sheet. The Maraloou Formation consists of black shale, marl,dolostone, and minor chert.
PALAEOPROTEROZOIC EARAHEEDY BASIN
Earaheedy Group
Palaeoproterozoic rocks of the Earaheedy Group (Hall et al., 1977; Pirajno, 1999) areexposed in the northeastern corner of WILUNA. The four stratigraphically lowest formationsin the group are exposed in the sheet area, and the rocks are typically undeformed and dipgently to the northeast. The Earaheedy Group is interpreted to be a passive-marginsuccession deposited on the northern margin of the Yilgarn Craton at c. 1.85 – 1.8 Ga (Joneset al., 2000).
Yelma Formation (#Ey)
On WILUNA the Yelma Formation (#Ey) includes sandstone, shale, and minor conglomeratedeposited in shallow-marine and locally fluvial environments. The formation is only a fewmetres thick on WILUNA, but attains a maximum thickness of about 500 m on NABBERU tothe north (Hocking et al., 2000; Jones et al., 2000). Carbonate rocks that form part of theformation elsewhere (Hocking et al., 2000) are not present on WILUNA.
Frere Formation (#Ef)
The Frere Formation (#Ef ) consists of granular iron-formation (GIF), ferruginous siltstone,and shale, as well as minor BIF and chert. Granular iron-formation units consist of beds ofjasperoidal GIF, 50 to 200 mm thick, with intraclastic breccia and shale interbeds. IndividualGIF beds consist of iron oxides, peloids of microplaty hematite, chert, and jasper in a
18
chalcedonic or jasperoidal cement. Hematite is locally replaced by magnetite. The GIFunits probably formed on a continental shelf, where ferruginous peloids accreted in wave-and current-agitated, iron-rich, shallow waters (Beukes and Klein, 1992). Interbeddedferruginous shale and siltstone are parallel laminated with minor cross-laminations, andwere possibly deposited in a lagoonal environment.
Windidda Formation (#Ed)
The Windidda Formation (#Ed ) comprises limestone, shale, and minor jasper and GIF.The formation was probably deposited in a carbonate shelf with coastal lagoons. Recentmapping in the southeastern part of the Earaheedy Basin suggests that the WindiddaFormation is a correlative of the upper part of the Frere Formation, rather than an overlyingunit (Jones et al., 2000).
Chiall Formation (#Ecw)
On WILUNA the Chiall Formation is represented by the Wandiwarra Member (#Ecw;Hocking et al. 2000), which is a unit of siltstone and shale with subordinate sandstone thatoutcrops in the northeastern corner of the sheet area.
UNASSIGNED PROTEROZOIC SEDIMENTARY ROCKS (#s)
Proterozoic sedimentary rocks that have not formally been assigned to any stratigraphicunit outcrop at Mount Wilkinson, Mount Lawrence Wells, and near Scorpion Bore, eastof Wiluna town. The rocks at Mount Wilkinson and Mount Lawrence Wells consist of chertbreccia, quartz-vein breccia, siliceous arenite and conglomerate, cherty mudstone, andsilicified carbonates. These rocks are flat lying and undeformed, and partly overlain bysilcrete (Czz). They were correlated with the ‘Finlayson Sandstone’ (now the JuderinaFormation) by Elias and Bunting (1982), but have not been assigned to any stratigraphicunit in recent 1:100 000-scale mapping.
The unassigned sedimentary rocks east of the town of Wiluna consist of silicified quartz-rich arenite and conglomerate. They are restricted to several easterly trending ridges parallelto large quartz veins in the underlying granitoid rocks. Silicification of the sedimentaryrocks is considered to have occurred along fractures related to the formation of the quartzveins (Langford et al., 2000).
STRUCTURE
Four phases of Archaean deformation (D1–D
4) have been recognized in the north Eastern
Goldfields Province (Farrell, 1997; Wyche and Farrell, 2000) from regional 1:100 000-scale mapping carried out by GSWA and AGSO. The recognition of these structures isbased on overprinting relationships of outcrop-scale structures, interpretation of magneticimages, and correlation of structures in different parts of the area. All four phases ofdeformation are recognizable on WILUNA.
First-generation (D1) structures have largely been overprinted during later events, but relict
D1 fabrics are preserved in gneisses, and possibly in some greenstones. However, it is not
clear how the early structures in different parts of the area are related, or even if they aredue to the same event. Gneisses northeast of Turnup Bore, in the northwestern part ofWILUNA, commonly contain a composite S
1–S
2 fabric with rootless isoclinal folds of S
1
19
leucosomes. A SHRIMP U–Pb zircon age of 2747 ± 11 Ma (AGSO, OZCRON database)for a gneiss in this area constrains the timing of D
1 to c. 2750 Ma or later.
The second deformation (D2) coincided with peak metamorphism in the greenstones and
craton-wide granitic magmatism. The effects of D2 are recognized throughout the area, but
are most pronounced in high-strain zones in amphibolite-facies rocks adjacent to granite–greenstone contacts. This deformation may be equivalent to the early extension event (D
E)
of Hammond and Nisbet (1992).
The characteristic D2 structure is a steeply dipping foliation (S
2) subparallel to greenstone
margins. Layered cherts in the northern end of the Yandal belt contain a strong composite(S
0–S
2) fabric with abundant steeply plunging, tight to isoclinal, intrafolial folds (F
2). The
fold axes are typically subparallel to a prominent, steeply plunging, combined intersection– mineral lineation (L
2). Northeast of Turnup Bore, a 2747 ± 11 Ma gneiss contains F
2 folds
of S1 leucosomes. The gneiss is cut by an undeformed monzogranite dyke, parallel to S
2,
that has been dated at 2658 ± 2 Ma (AGSO, OZCRON database), indicating that D2 had
ceased by c. 2658 Ma.
The last major penetrative deformation event was largely responsible for shaping thepresent-day disposition of the greenstone belts. Strong east–west to east-northeast–west-southwest shortening produced large-scale, upright, and shallow to moderately plungingfolds, and north to northwesterly trending faults and shear zones (Fig. 3). Outcrop-scale F
3
folds are typically upright and open to tight with shallowly plunging axes that are subparallelto a fine mineral lineation (L
3).
The last recognized Archaean deformation in the region produced outcrop-scale kinks,crenulations, and quartz-filled tension-gash arrays. These features may be related to brittlefaults and fractures that form the high-angle conjugate structures described by Vearncombe(1998, 2000).
METAMORPHISM
All greenstones on WILUNA are metamorphosed. The greenstone belts show a distinctivemetamorphic zoning from amphibolite facies in areas close to granitoid contacts, togreenschist or prehnite–pumpellyite facies in the central parts of the belts. This type ofmetamorphic zonation is developed throughout the Eastern Goldfields Province (Binns et al.,1976), and is characteristic of Archaean granite–greenstone terrains worldwide (Condie,1981; Wilkins, 1997).
In the Agnew–Wiluna belt, the metamorphic conditions range from prehnite–pumpellyiteor lower greenschist facies in the centre of the belt (Hagemann et al., 1992) to amphibolitefacies in the south, near Coles Find and Honeymoon Well. At Wiluna the typical assemblagein mafic rocks is chlorite–epidote–quartz–plagioclase(–calcite). Hagemann et al. (1992) alsoreported the presence of pumpellyite in mafic rocks, but this is not diagnostic of prehnite–pumpellyite facies, as pumpellyite is also stable under lower greenschist-facies conditions.The absence of prehnite may be due to the presence of small amounts of CO
2 (indicated
by the presence of calcite), which is enough to suppress the formation of prehnite (Bucherand Frey, 1994).
In the Yandal belt, most of the greenstones are metamorphosed to lower greenschist (orprehnite–pumpellyite) facies. Amphibolite-facies rocks are restricted to narrow zones alonggranite–greenstone contacts. Mafic rocks in the centre of the belt contain the metamorphicassemblage chlorite–albite–epidote–actinolite, which is diagnostic of greenschist facies
20
(Bucher and Frey, 1994). Felsic rocks contain co-existing white mica – chlorite–albite(–epidote–pumpellyite), which indicates metamorphism at lower greenschist-faciesconditions (or lower).
In quartzofeldspathic gneisses, the assemblages are not diagnostic, but the presence ofCa-plagioclase is indicative of amphibolite-facies conditions (or higher). Additionally,the presence of clinopyroxene-bearing amphibolite lenses and localized partial meltingsuggest upper amphibolite-facies metamorphism and a peak temperature of more than650–700°C.
PALAEOZOIC GUNBARREL BASIN
PERMIAN PATERSON FORMATION (Pa)
Outliers of flat-lying, probable Permian sedimentary rock (Pa) are exposed in thenortheastern corner of WILUNA. These rocks are interpreted as part of the Paterson Formationon the basis of similarities with Permian rocks to the east (Lowry, 1971). The rocks consistof poorly sorted, medium- to coarse-grained sandstone, pebbly sandstone, and conglomerate.
CAINOZOIC GEOLOGY
Cainozoic regolith deposits, comprising residual indurated material exposed by erosion andyounger alluvial, eluvial, eolian, and lacustrine deposits, cover large areas on WILUNA.Individual regolith units have been mapped using field observations, aerial photography,and Landsat TM (Thematic Mapper) images.
The oldest regolith units typically form residual deposits on low hills and in breakaways,and are interpreted as remnants of the Tertiary weathering surface. These units includeferruginous duricrust and ferricrete (Czl), silcrete (Czz), and silica caprock over ultramaficrocks (Czu).
Proximal slope deposits, comprising rock debris, sand, and silt, lie on or adjacent to lowhills and on slopes beneath breakaways. They include colluvium (Czc), quartz-vein debris(Czcq), and ferruginous rock debris and ironstone rubble (Czf ). The latter unit forms bythe degradation of ferruginous duricrust, and is typically developed on low hills, and quartz-vein debris (Czcq) is typically associated with large quartz veins. Areas adjacent to outcropsof granitoid rock are commonly covered by deposits of coarse-grained quartz–feldspar sandwith various proportions of small fragments of granitoid rock (Czg).
Distal parts of the regolith are dominated by sheetwash (Cza) and sandplain deposits (Czs).Sheetwash deposits (Cza) are extensive adjacent to the main drainage systems and on themargins of sandplains. They consist of a thin layer of sand, silt, and clay over weatheredrock, and are gradational into sandplain deposits. Areas underlain by granitoid rocks arecovered by extensive sandplains (Czs) consisting of unconsolidated quartz sand and silt.Ridges of windblown sand are present locally.
The Lake Way drainage system in the southwest and the Lake Carnegie drainage in theeast contain a range of ephemeral lake deposits. Playa lakes (Czp) contain saline orgypsiferous evaporites, along with minor amounts of sand, silt, and clay. The playas areassociated with saline or gypsiferous dune deposits (Czd) that contain low, crescent-shapeddunes formed by wind action during dry periods. Extensive, low-lying areas containinghummocky deposits (Czb) of sand, silt, and clay, with small interspersed playas, claypans,
21
and patchy deposits of calcrete, surround the gypsiferous dune deposits. There are alsolarger deposits of calcrete (Czk) around the margins of the lake deposits.
Younger deposits of unconsolidated to semiconsolidated sandy alluvium and gravel (Qa),of probable Quaternary age lie along intermittently active fluvial channels and on adjacentfloodplains. These deposits grade laterally into sheetwash and may have undergone somedegree of eolian reworking. Lake and sheetwash deposits may also contain small claypans(Qac), consisting of thin deposits of silt and clay in shallow depressions that are filled withwater after heavy rainfall.
ECONOMIC GEOLOGY
Metallic mineral production from WILUNA is restricted to gold and accessory silver, withrecorded production to 30 June 2000 of about 161 882 kg of gold and 315 kg of silver.There are major deposits of nickel on WILUNA, although these have not yet been broughtinto production.
GOLD
WILUNA lies within the East Murchison Mineral Field, and includes five historic gold miningcentres — Wiluna in the southwest (Edwards, 1953; McGoldrick, 1990; Hagemann et al.,1992), and Coles Find (Morgan and El-Raghy, 1990), Kingston, Collavilla, and NewEngland in the south — as well as the disused Mount Fisher mine in the southeast (Powellet al., 1990), and the Jundee–Nimary mining operation in the central part (Byass andMacLean, 1998; Phillips et al., 1998b). Gold was discovered at Wiluna in 1896, and wasmined in three main periods (Chanter et al., 1998). Between 1896 and 1924, the gold wasextracted from near-surface reefs and relatively shallow workings into the oxidized zone(Gibson, 1908; Montgomery, 1909). Gold production fell when mining progressed belowthe oxidized zone and refractory, primary sulfide ore was encountered. The second mainperiod of mining occurred in the period 1926–1950, when sulfide flotation techniques wereused to treat the sulfide ore. Present-day mining operations commenced in 1984 (Chanteret al., 1998). Gold mineralization at Wiluna is in quartz–carbonate–fuchsite–sulfide veinsand breccia zones associated with late northerly to northeasterly trending faults (Hagemannet al., 1992). The mineralization has tentatively been dated at c. 2630 Ma, or later (Kentand Hagemann, 1996).
Gold mineralization was not discovered in the Jundee area until the mid-1980s. The Jundeeand Nimary deposits were discovered during drilling programs in 1990 and 1992respectively (Lewington, 1995; Wright and Herbison, 1995). Opencut mining commencedin 1995, and a total of 48.8 t of gold was produced from the Jundee–Nimary project until30 June 2000. The geology of the Jundee–Nimary goldfield is described in more detail inByass and Maclean (1998) and Phillips et al. (1998b). Gold mineralization is in variouslyoriented quartz–calcite–pyrite veins in late brittle structures (Phillips et al., 1998b), whichare cut by undeformed felsic dykes dated at 2656 ± 7 Ma (Yeats et al., 1999).
NICKEL
Nickel mineralization is developed in a thick, poorly exposed ultramafic unit at HoneymoonWell in the southwestern part of WILUNA (Donaldson and Bromley, 1981; Gole et al., 1996).The mineralization is known from extensive drilling and geophysical surveys. Nickel ispresent as disseminated sulfides in serpentinized olivine-rich cumulates, and as massivesulfides in spinifex-textured komatiite flows (Gole et al., 1996). Deposits have beenidentified at Hannibals, Harrier, Wedgetail, Corella, and Kingston, all in the southwestern
22
part of WILUNA, with resources (indicated and inferred) of sulfide and laterite mineralizationtotalling about 370 Mt at average grades of 0.8 – 0.9% Ni (Outokumpu Oyj, 2000). Minornickel mineralization is also developed in ultramafic rocks elsewhere on WILUNA (Ferguson,1998).
URANIUM
Uranium (carnotite) mineralization is developed in calcrete along two palaeodrainagesystems that discharge into Lake Way in the southwestern part of WILUNA. Three prospects— Hinkler Well, Centipede, and Lake Way — have been identified (Ferguson, 1998). Atthe Lake Way prospect, carnotite forms coatings on bedding planes of rock fragments inalluvial gravels, and on fractures in calcrete. The prospect contains a measured resourceestimated at 3.77 Mt of ore at 0.98 kg/t U
3O
8 (3695 t of contained metal; Ferguson, 1998).
23
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YEATS, C. J., McNAUGHTON, N. J., RUETTGAR, D., BATEMAN, R., GROVES, D. I., HARRIS,J. L., and KOHLER, E., 1999, Evidence for diachronous Archaean lode gold mineralization in theYilgarn Craton, Western Australia: a SHRIMP U–Pb study of intrusive rocks: Economic Geology,v. 94, p. 1259–1276.
28
Appendix
Gazetteer of localities
Locality AMG coordinatesEasting Northing
Abercromby Well 233000 7027400
Amees Bore 254100 7101900
Bridal Well (abd) 225600 7029300
Camel Bore 264700 7079600
Centipede U prospect 237600 7027400
Corella Ni prospect 240000 7022700
Cunyu Homestead (abd) 211400 7118400
Deadwood Bore 201900 7028200
Deep Bore (abd) 209200 7035900
Granite Well 261900 7046300
Hannibals Ni prospect 239800 7019400
Harrier Ni prospect 241500 7017000
Hinkler Well U prospect 220100 7024000
Honeymoon Well (abd) 243100 7022200
Jundee Homestead 265400 7083100
Jundee–Nimary gold mine 260000 7081000
Kingston Ni prospect 243400 7014700
Kukabubba community 223800 7084600
Lake Violet Homestead 267200 7062400
Lake Ward 271500 7088000
Lake Way Homestead 248300 7016800
Lake Way U prospect 237300 7043900
Lignan Well 293000 7100500
Matilda gold mine 222900 7037600
Millrose Homestead 295700 7078200
Mount Alice West 224700 7079200
Mount Fisher gold mine 349500 7029700
Mount Lawrence Wells 221800 7031900
Mount Wilkinson 218100 7032000
Ngangganawili community 231500 7050500
Panakin Bore 274300 7117000
Scorpion Bore 242000 7057100
Strife Bore (abd) 259000 7073700
Terry Bore 253300 7070200
Top Kukabubba Well 224900 7087600
Turnup Bore 254400 7097600
Twin Tanks Well (abd) 267100 7070300
Wedgetail Ni prospect 237000 7023700
Wiluna gold mine 225000 7051300
Wiluna town 223400 7055500
NOTE: abd: abandoned
Localities are specified by Australian Map Grid (AMG) coordinates, Zone 51, to
at least the nearest 100 m
BARROWISLAND
DAMPIER ROEBOURNE
1 2 3
5 6 7
ONSLOW YARRALOOLA PYRAMID
NINGALOO YANREY
12 9
EDMUND
14
MANDORA
NABBERU STANLEY
GUNANYA
MUNRO
LA GRANGE
BROOME
PENDER
McCLARTYHILLS
JOANNASPRING
SAHARA
RUNTON
MADLEY
HERBERT BROWNE
WARRI
MORRIS
URAL
PERCIVAL
DUMMER
CROSSLAND
CHARNLEY
QUOBBA MT PHILLIPS MTEGERTON
COLLIER
ROBINSONRANGESHARK
BAY-
EDEL
HOUTMANABROLHOS
DONGARA-
GERALDTON-
AJANA
YARINGABELELE
GLENGARRY
MURGOO
YALGOO KIRKALOCKA YOUANMI
SANDSTONE
KINGSTON ROBERT
12
7 8
43
13 14 15 16
10
6
2 4
MTELIZABETH
LANSDOWNE DIXONRANGE
MT RAMSAY GORDONDOWNS
HELENA
WILSON WEBB
RYAN MACDONALD
1
CAMBRIDGEGULF
ASHTON
MEDUSABANKS
MONTAGUESOUND
CAMDEN SOUNDPRINCE
12 10
16 13 14
5 6
9 10
5
9 10
14 15 16 13 14
42 3 4 3 4
8,
7 5 6 7 8
12 9 11 12 10 11
13 14 16
12 3 4
5,
COBB RAWLINSON
BENTLEY SCOTT
YOWALGA TALBOTCOOPER
SIRSAMUEL
THROSSELL WESTWOOD LENNIS WAIGEN
LEONORA LAVERTON RASON NEALE VERNON WANNA
5 6
12 9 10
13 15 16 13 14
1 2 3 4 1 2
1 2
PERENJORI NINGHAN BARLEE MENZIES
HILLRIVERMOORA BENCUBBIN
JACKSON
PERTH KELLER- SOUTHERNCROSSBERRIN
6 7 8 5
9 10 11 12
14 15 16
MINIGWAL PLUMRIDGE JUBILEE MASON
CUNDEELEESEEMORE LOONGANA
FORREST
ZANTHUS NARETHA MADURA EUCLA
7 8 5 6
11 12 9 10
15 16 13 14
PINJARRA CORRIGIN HYDEN LAKEJOHNSTON
NORSEMAN
COLLIE DUMBLE-YUNG
NEWDE-GATE
RAVENS-THORPE
ESPERANCE-
PEMBERTON- MT BREMERBAY
MONDRAINISLAND
IRWIN INLET
ALBANY
2 3 4 1 2
6 7 8 5
6,
12
10
BALLA-DONIA
CULVER BURN-ABBIE
NOONAERA
MALCOLM-CAPE ARID
3 4 1 2
SD 52
SE 52
SG 52SG 51
SH 52SH 50
SI 51SI 50
SG 49
LONDON-DERRY
114 o 120 o 126 o
32 o
28 o
24 o
20 o
16 o
5,9
15,
7, 11
DRYSDALE-
BARKER-
10, 14 11, 155, 9
BUSSELTON-
AUGUSTA
YAMPI
3
DERBY
7
LENNARDRIVER
8
BAH
12
NOONKAN-MTANDERSON
SE 51
11
SF 52
MT BANNER-MAN
13
CORNISH
1 2
LUCAS
14
BILLILUNA
STANSMORE
6
ANKETELL
2
PATERSONRANGE
6
DOWNSBALFOUR
9
MARBLEBAR
8
NULLAGINE
5
YARRIE
1
PORTHEDLAND-
ISLAND4
BEDOUT
TABLETOP
11
ROBERTSON
13
NEWMAN
16
TUREECREEK
15
WYLOO
10
MINILYA
16
WINNINGPOOL
KENNEDYRANGE
1
13
WOORAMEL
5
GLENBURGH
6
BULLEN
1
TRAINOR
2
PEAK HILL
8
CUE
15
WIDGIE-
14
BOOR-ABBIN
13
KAL-GOORLIE
9
MOOLTHA
SF 49
WESTERN AUSTRALIA
TRF44 22.03.01
REGENT-
-
11 12
ROY HILLMT BRUCE
SF 50
Second Edition
GEOLOGICAL MAPS
RUDALL
10
SF 51
SG 50BYRO
10
EDJUDINA
6 SH 51KURNALPI
10
LISSADELL
2
14
DUKETON
WILUNA
9
INDEX TO 1:250 000-SCALE
EXPLANATORYNOTES
SHEET SG 51-9 INTERNATIONAL INDEX
DEPARTMENT OF MINERALS AND ENERGY
GEOLOGICAL SURVEY OF WESTERN AUSTRALIA
WILUNA
SECOND EDITION
1:250 000 SHEETWESTERN AUSTRALIA
Further details of geological publications and maps produced by theGeological Survey of Western Australia can be obtained by contacting:
Information CentreDepartment of Minerals and Energy100 Plain StreetEast Perth WA 6004Phone: (08) 9222 3459 Fax: (08) 9222 3444www.dme.wa.gov.au
FAR
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GOVERNMENT OFWESTERN AUSTRALIA
1:250 000 GEOLOGICAL SERIES
LAKE
Gum
Cree
k
WARD
LindsayGordon
Lagoon
IvesCk
L A K E W A Y
PEAK
GRANITE
NgangganawiliAboriginalLand
WILUNA 2
MOUNT GREEN
MOUNT ALICE WEST
Yard
Yard
Yard
Jundee
Millrose
Lake Way
NgangganawiliCommunity
Ngangganawili
AboriginalLand
Kukabubba
Cunyu (disused)
Millrose
Lake Violet
LAKE
VIOLET
ROAD
JUNDEE MILLROSEROAD
MEEKATHARRA ROAD
WONGAWOL
ROAD
SANDS
TONE
WILUNA
ROAD
YEEL
IRRIE
ROAD
KALGOORLIE
CANN
ING
STOC
KRO
UTE
WILUNA
NORTHROAD
JUNDEEROAD
WILUNA
NORTH
ROAD
New Spring Homestead 27 km
ROAD
WILUNA
WONGAWOL
ROAD
GRANITE
PEAK
KALGOORLIEÊMEEKATHARRA ROAD
ROSE HILLS
TWIN HILLSYd
Jundee Mine Village
Yd
Yd
Mee
kath
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158
km
Yeelirrie Homestead 37 km
Old
Gid
gee
Hom
este
ad 1
05 k
m
Yakabindie Homestead 68 km
(abd)(abd)
Millgool Outcamp
Millbillillie
Wiluna
546 m
546 m
538 m
549 m
571 m
579 m
592 m
574 m
617 m
640 m
604 m
541 m
525 m
500 m
610 m
555 m
509 m
553 m
609 m
588 m
WILUNA 25
WILUNA 27
NMF129
WILUNA 26
WILUNA 16
WILUNA 15
WILUNA 5
WILUNA 4
NMF130
G 53-12
G 53-10
G 53-6
G 53-4
G 53-5
NMF 131
G 53-8
BARE GRANITE HILL
PROMINENT HILL
WILUNA 1
WILUNA 11
WILUNA 14
WILUNA 3
WELLS
Exploration CampHoneymoon Well
Barwidgee Homestead 5 km
Granite Peak Homestead 42 km
Yelm
a Ho
mes
tead
41
km
Wonganoo Homestead 21 km
Yd
MOUNTALICE
MOUNT WAY
LAWRENCEMOUNT
MOUNT WILKINSON
MOUNT FISHER
MOUNT CLEAVER
Yard
Yard
Yard
Yard
Yard
Yard
Yard
Yard
Yard
Yard
Yard
Yard
Yard
Yard
Yard
Yard
Yard
YardYard
Yard
Yard
Yard
Yard
Yard
Yard
Yard
YardYard
Yard
Yard
F I N
L A
Y S
O N
R A N
G E
P
B
Jundee Soak
SwampDuck
T
T
T
LAKE WAY
Ts
W
W
W (abd)
No 1 W
Dingo W
L A K E
LAKEURAMURDAH
V I O L E T
B
B (abd)
W
The Bore (abd)
W
Sk
B
W
T
(abd)
(PD)
2A Tank (PD)Old Cunyu WellHomestead Bore
Spinifex Bore
McMeakin Bore
No 4 Bore
No 3 Bore (abd)
Fyfe Well
Jungarra Soak
Jungarra Bore
No 2 Well
Top Kukabubba WellDingo Rockhole
Calcalong Rockhole
Bendys Bore
Mudjon Bore
Optimist Bore
Kukabubba No 2 Bore
Little Kukabubba Well (abd)
Taylor Bore (abd)
Cork Bore (abd)
Bucktin Well (abd)
Quadrios Bore (abd)
Della Bore (abd)
Ross Well (abd)
Phyllis Well
Goosie Bore (abd)
No 1 Bore
No 2 Bore (abd)
North Pool
Chantra Billie Bore
Camp Well
Baldy Well (abd)
Town WellsShed No 1 Bore
Shed No 1 Bore
Shed No 2 Bore
Shed No 3 BoreClinchs Bore
Shannons Dam Bore (abd)Scorpion Bore (abd)
Harvey Bore (abd)
Spinifex Bore (abd)
Morrissey Well Beau Bore (abd) Carry On Bore
Uramurdah Well (abd)
Warren Bore (abd) Sandhill Bore (abd)
Coolibah Bore (abd)
Camel Soak Sandhill Bore
Gladsome Bore
Tall Bore
Prospector Well
Abercromby Well
Salt Bore
Hinkler Well
Tullock Well (abd)
Honeymoon Well (abd)
Butcher Well
Kingston WellScotty Well
North Bore
Lake Way Well
Cross Road Bore
Middle Bore
Centipede BoreJust It BoreTony Bore
Reserve WellDawson Well
White Well
Deadwood Bore
Atkins Well (abd) Bridal Well (abd)
Deep Well (abd)Deep Bore (abd)
Little Diorite Well (abd)
Lanagan Bore (abd)
Critch Bore (PD)
Ward 1 Well (abd) Gold Tooth Well (abd)
Old Govt Well (abd)
Trennaman Well (abd)
Freshwater Well (abd)
Red Hill Well (abd)
Old Yard Well (abd)
Railway Well (abd)
Hayes Well (abd)Vincent Bore
Bubble Well (PD)
Jeffries Bore (abd) Cocksparrow Well (abd)
No 1 Well (abd)
No 48 Well Moonbria Well
No 47 Well
Parson Well
Corktree Well
Gunally WellBasset Well
Duffer Well
Irving Well (abd) Limestone Well (abd)
Conglomerate Bore
Mitchell Well
Scaddan Well
Leeman Well
Taffy Bore
MacNamara WellToohey Well
Sailor Jack Well
No 30 Bore
No 28 Bore
No 29 Bore
No 27 Bore
No 13 BoreNo 26 Bore
No 17 Bore
McKay Bore
Gabbagundi Bore
North East Bore
Orphan Well No 2 Bore
Bowman Well (abd)
Rennie Well
Sandalwood Bore
Kingsley Well
Slav Well
No 16 Bore
Kalamunda Bore
New Trial Well
Little Well
Rinaldi Well
South Homestead WellBuglio Well
25 Mile Bore
Double Hole Well (abd)
West Guy Well
Guy Well
21 Mile Well
Granite Well
Breakaway BoreGranite Well
Ironstone Well
Woolshed Well
Ram WellVause Well
Munn Well
Marconi Well (abd)Deep Well
Two Flats Well
Mahood Well
Roto Well
Pumpkin Well
The Strip Well
Spinifex Well
Bitter Well
Pope Well Daulby Well Lupton WellKenden Well
Old Shaft Well
14 Mile Well
Double Barrel Well
Outcamp Well
8 Mile Well
Dingbat Well
Coolup Bore
Kooyong WellTragedy Well (abd)
Pommy Well
Destiny Well Longreach Well
Shady Well
Rocky WellOutcamp Well
Melrose Well
Mandilla Well
Granite Well Paddy Well
Biddy Well
Sam Well (abd)
Bullock Well
Spinifex Well
May Queen Well
Herbert Bore
Boomer Bore
Emu Bore
New Bore
Towser Bore
Supply Well
Mona Vale Well
East Well
Black Cat Well
Divine Bore
Porcupine WellSandy Bore
Panakin Bore
4 Mile Bore
Bundle Well (abd) Mistake BoreAlex Well
Kerry Lyn Bore
George BoreMizina Well
Hughes BoreAmees Bore
Turnup Bore
Dingo Bore
Quartz Bore
Lignan Well
Knob Bore
Pizzetti Well
Jackys BoreBogada Bore
Bejinks Bore
Terry Bore
Strife Bore (abd)
Nimarry Bore
Option Bore
Camel Bore
Mundy Bore
Christmas Bore Snake Well
Old Camp Bore
Boas Bore
Bloodwood Bore
Depot Bore
McHugh WellSoak Creek Well
Lockhart Well
Emu Bore
Two Hills Bore
Quartz Well
Lucky Bore
Harry Hill Well
Gum Well (abd)
Ronnie Bore (abd)
Twin Tanks Well (abd)O'Keefe Well
Oasis Bore (abd)
Boundary Bore
Dingo Bore
Fergy Bore
Oxby BoreHegarty Bore
Sardine Bore (abd)
Jink Bore (abd)
New Market Bore Camel Well Thomas Bore
North Well
Bartlett Bore (abd)
Worthy Bore (abd)
Squeeky Bore (abd)
Johnson Bore
New Bore
Christmas Creek Well
Gravel Bore
Octopus Bore (abd)Desert Bore
Quartz Bore
Tommy Bore
Deep Well
Porcupine Bore
King BoreSpinifex Bore
Fyfe Bore
Running Waters BoreCorner Well
Lorna Glen Well
Karrah Bore
No 5 Bore
No 1 BoreNo 3 Bore No 2 Bore
No 4 Well (abd)
No 10 Well
No 2 Well
No 4 Bore
No 9 Well
No 1 Well84 Bore
65 Well (abd)
Two Hills Well (abd)
Plover Bore
WellMurphy
WH
S
Norms Bore
Spring
Bore (abd)
Bore
Bore (abd)Bore
Bore
Bore
MorphettWell
Well
Hadji Bore
Bore
Well (abd)
Well
WaterholeWaterhole
Soak
TipperaryWell
Springs
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Mount Fisher
Empire Laterites
Corboys Find
Bills Find
Sims Find
New Golden Way Slav Well
Herbert Well
Flushing Meadow
May QueenRewardIves Find
WILUNA
COLES
KINGSTON
COLLAVILLA
NEW ENGLAND
E A S T M U R C H I S O N M I N E R A L F I E L D
W I L U N A D I S T R I C T
M U R C H I S O N M. F.
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Happy Jack
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15
22
PRODUCT OF THE NATIONAL
GEOSCIENCE MAPPING ACCORD
2 3
10
Kilometres
0 20 30 40 50
SCALE 1:1000 000
10
Kilometres
0 20 30 40 50
SCALE 1:1000 000
0 5 10 15 20 25 305000
Metres KilometresTRANSVERSE MERCATOR PROJECTION
VERTICAL DATUM: AUSTRALIAN HEIGHT DATUM
SCALE 1:Ý250Ý000
Grid lines indicate 20Ý000 metre interval of the Australian Map Grid Zone 51
HORIZONTAL DATUM: AUSTRALIAN GEODETIC DATUM 1984
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Alluvium _ clay, silt, sand, and gravel; in channels and on floodplainsClay and silt in claypans
Ephemeral lake and dune deposits _ clay, silt, and sand; in drainage basins adjacent to playa lakesDune deposits _ sand, silt, clay, gypsum, and carbonate; in low dunes adjacent to playa lakesPlaya deposits _ saline and gypsiferous evaporites, clay, and sand in playa lakes
Sheetwash deposits _ clay, silt, and sand in extensive fans; commonly ferruginousSandplain deposits _ unconsolidated sand and minor silt; includes stabilized dunes
Colluvium _ silt, sand, and rock debris as slope deposits and proximal sheetwash; includes ironstone fragmentsQuartz vein rubble and debris
Ferruginous rubble _ degraded lateritic duricrust, and ferruginous debrisSand over granitoid rock _ quartzofeldspathic sand
CalcreteLateritic duricrustSilica caprock over ultramafic rockSilcrete
sandstone, pebbly siltstone, and conglomerate
Conglomerate, quartz-rich sandstone, arkosic sandstone, and microbial laminates; commonly silicified and brecciated
siltstone and shale, and subordinate sandstone
limestone and shale
granular iron-formation, ferruginous siltstone, and shale; minor banded iron-formation and chert
sandstone, shale, and minor conglomerate
undivided mafic intrusive and extrusive rocks (simplified geology only)
chertified microbial laminates with barite and anhydrite nodules
Medium- to coarse-grained dolerite dykes and sills
Aphyric tholeiitic basalt
quartz sandstone; local siltstone, chert breccia, and conglomerate
stromatolitic chert and chert breccia; minor dolomite
quartz arenite and subordinate siltstone; planar-bedded or cross-stratified; commonly ripple-marked
Mafic dyke
Quartz vein
Syenite (simplified geology and subsurface)Monzonite (subsurface only)
Granitoid rock, undividedFine-grained granitoid rockFoliated granitoid rock with interleaved mafic rockDiorite and quartz dioriteQuartz diorite and quartz monzodiorite (subsurface only)Foliated granitoid rockGranodioriteBiotite monzograniteHornblende monzogranite (subsurface only)Porphyritic biotite monzogranite
Granitoid rock and quartzofeldspathic gneiss; minor calcÊsilicate gneiss and mafic gneissHornblende quartz monzonite; minor quartz diorite
Interlayered quartzofeldspathic gneiss, monzonite, and metamorphosed mafic rockQuartzofeldspathic gneiss, commonly with diffuse layering
QuartzÊfeldspar schist
Metamorphosed sedimentary rock, undivided; includes minor felsic volcaniclastic rockPolymictic conglomerate; metamorphosedDolomite; metamorphosedShale, and minor siltstone and sandstone; metamorphosedSandstone and minor siltstone; metamorphosed
Chert and banded chert; metamorphosedBanded iron-formation; metamorphosed
Metamorphosed felsic rock, undividedPorphyritic dacite; metamorphosedIntermediate volcanic rock; metamorphosedPorphyritic felsic rock; metamorphosedFelsic schistFelsic tuff; metamorphosed
MetagabbroStrongly foliated gabbro; metamorphosed
Olivine gabbro; metamorphosed
Metamorphosed fine- to medium-grained mafic rock, undivided; includes some metagabbroAmphibolite; generally fine- to medium-grainedStrongly foliated metamorphosed mafic rockStrongly foliated metamorphosed mafic rock interleaved with minor foliated granitoid rockPorphyritic basaltic andesite; metamorphosed (subsurface only)High-Mg basalt; commonly with pyroxene-spinifex and variolitic textures; metamorphosedMafic schist; chlorite-rich schist, probably after high-Mg basaltAmygdaloidal basalt; metamorphosed
Metamorphosed ultramafic rock, undividedPeridotite; metamorphosedSerpentinized ultramafic rockTalcÊchlorite(Êcarbonate) schistPyroxenite; metamorphosed
Bubble Well Member:
FRERE FORMATION:
WINDIDDA FORMATION:
YELMA FORMATION:
KILLARA FORMATION:
Bartle Member:
JUDERINA FORMATION:
Finlayson Member:
Geological boundary
exposed....................................................................................
concealed, interpreted from aeromagnetic data...................
Fault or shear zone
exposed....................................................................................
concealed, interpreted from aeromagnetic data...................
Bedding, showing strike and dip
Way-up indicator
pillow structure........................................................................
sedimentary structure.............................................................
inclined.....................................................................................
vertical......................................................................................
inclined.....................................................................................
horizontal..................................................................................
Mining area
Mineral occurrence
Nickel........................................................................................
Uranium....................................................................................
concealed.................................................................................
Metamorphic foliation, showing strike and dip
Joint, fracture, or vein, showing strike and dip
inclined.....................................................................................
vertical......................................................................................
prominent trend, unspecified.................................................
fracture pattern in granitoid rock...........................................
S-vergence...............................................................................
Mineral lineation, showing trend and plunge
tailings, mullock.......................................................................
inclined.....................................................................................
vertical......................................................................................
horizontal.................................................................................
Airphoto lineament
Small-scale fold axis, showing trend and plunge
trend of bedding.....................................................................
Archaean deformation
Structural symbols are labelled according to the sequence
DÛ, Dç..........................................................................
concealed.................................................................................
of local deformation events, where known
Strongly foliated rock............................................................................
Aeromagnetic lineament.......................................................................
Formed road..........................................................................................
Track.......................................................................................................
Railway, abandoned..............................................................................
Powerline................................................................................................
Landing ground.....................................................................................
Homestead.............................................................................................
Building..................................................................................................
Yard........................................................................................................
Microwave repeater station..................................................................
Horizontal control; minor......................................................................
Breakaway..............................................................................................
Sand dune..............................................................................................
Soak........................................................................................................
Spring......................................................................................................
Waterhole................................................................................................
Well.........................................................................................................
Pipeline...................................................................................................
Position doubtful....................................................................................
Abandoned.............................................................................................
Tank........................................................................................................
Windpump..............................................................................................
Bore.........................................................................................................
Mineral field boundary...........................................................................
Mining centre..........................................................................................
Mine (gold, unless otherwise indicated)..............................................
Major opencut........................................................................................
Opencut..................................................................................................
Treatment plant......................................................................................
made ground............................................................................
Mineral exploration drillhole, showing subsurface data.....................
Prospect ................................................................................................
crenulation, showing trend and plunge of axis, inclined.....
Intersection lineation, showing trend and plunge, inclined...............
unspecified...............................................................................
Watercourse with ephemeral pool, rockhole, soak,
spring or waterhole...................................................................
QUAT
ERNA
RY
CAIN
OZOI
C
PHAN
EROZ
OIC
PALA
EOZO
IC
PERM
IAN
Eara
heed
y Gro
up
Moo
loog
ool S
ubgr
oup
Win
dpla
in S
ubgr
oup
Yerri
da G
roup
PALA
EOPR
OTER
OZOI
C
PROT
EROZ
OIC
ARCH
AEAN
EARA
HEED
Y BA
SIN
YERR
IDA
BASI
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ON
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N
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y Gr
oup
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roup
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Windp
lain S
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120^00À26^00À
15À
30À
45À
27^00À120^00À 30À 121^00À 121^30À
27^00À
45À
30À
15À
15À 30À 45À 121^00À121^30À15À
26^00À
15À15À 45À
GEOLOGICAL SURVEY OF WESTERN AUSTRALIA SHEET SG 51-9000 GEOLOGICAL SERIESAUSTRALIA 1:250
REFERENCE
JAMINDI
2647
THREE RIVERS
2747
MARYMIA
2847
FAIRBAIRN
2947
METHWIN
3047
RHODES
3147
MUDAN
3247
GLENAYLE
3347
KAHRBAN
3447
2642
2643
2644
2645
2646
2742
2743
2744
2745
2746
2842
2843
2844
2845
2846
2942
2943
2944
2945
2946
3042
3043
3044
3045
3046
3142
3143
3144
3145
3146
3242
3243
3244
3245
3246
3342
3343
3344
3345
3346
3442
3443
3444
3445
3446
WOODLEY
NOWTHANNA
GABANINTHA
GLENGARRY
BRYAH
SANDSTONE
YAGANOO
MOOLOOGOOL
DOOLGUNNA
MONTAGU
MEREWETHER
THADUNA
YEELIRRIE
WILUNA
CUNYU
MERRIE
MILLROSE
NABBERU
DARLOT
WANGGANNOO
SANDALWOOD
BALLIMORE
BANJAWARN
TATE
YELMA
WONGAWOL
EARAHEEDY
DUKETON
URAREY
COLLURABBIE
WINDIDDA CARNEGIE
COONABILDIE
MOUNT KEITH DE LA POER
COSMO NEWBERYSIR SAMUELDEPOT SPRINGSLAKE MASON
YOUNO DOWNS
MOUNT BARTLE
LEE STEEREGRANITE PEAK
VON TREUERLAKE VIOLET
PEAK HILL
SG 50-8
NABBERU
SG 51-5
STANLEY
SG 51-6
KINGSTON
SG 51-10
WILUNA
SG 51-9
GLENGARRY
SG 50-12
SANDSTONE
SG 50-16
SIR SAMUEL
SG 51-13
DUKETON
SG 51-14
Edited by N. Tetlaw and G. Loan
Cartography by D. Ladbrook and B. Williams
Topography from the Department of Land Administration Sheet SG 51-9with modifications from geological field survey
Published by the Geological Survey of Western Australia. Copies available fromthe Information Centre, Department of Minerals and Energy, 100 Plain Street,
East Perth, WA, 6004. Phone (08) 9222 3459, Fax (08) 9222 3444
This map is also available in digital form
Printed by the Sands Print Group, Western Australia
The recommended reference for this map is:FARRELL, T. R., 1999, Wiluna, W.A. Sheet SG 51-9 (2nd edition):Western Australia Geological Survey, 1:250000 Geological Series
Compiled by T. R. Farrell 1997
Geology after GSWA and AGSO maps (see sheet index)
15
70
35
80
39
75
SIMPLIFIED GEOLOGYSIMPLIFIED REGOLITH
N.T.
W.A.
S.A.
Qld
N.S.W.
A.C.T.
Vic.
Tas.
SHEET INDEX
Western Australia 1999
The lines indicate magnetic declination, 1995
+ means declination is east and correction must be
added to compass bearing to give true bearing
- means declination is west and correction must be
subtracted from compass bearing to give true bearing
Annual change is 1À easterly
NATURAL SCALE
Mafic dyke; dashes indicate concealed by younger rock
Quartz vein
SyeniteHornblende quartz monzonite and minor quartz diorite
Granitoid rock, mainly monzograniteInterleaved foliated granitoid and mafic rocks
Granitoid rock and quartzofeldspathic gneiss in various proportions
Layered sequence of quartzofeldspathic gneiss, monzogranite,and metamorphosed mafic rock
Quartzofeldspathic gneiss dominant
Metasedimentary rock dominantMixed sequence of metamorphosed sedimentary and felsic rocksChert and layered chert; metamorphosedBanded iron-formation; metamorphosed
Metamorphosed felsic rock dominantPorphyritic dacite; metamorphosedIntermediate volcanic rock; metamorphosed
Metamorphosed mafic rock dominant
Metagabbro
Metamorphosed ultramafic rock dominant
Paterson Formation
Proterozoic sedimentary rock, unassigned
Chiall Formation, Wandiwarra Member
Windidda Formation
Frere Formation
Yelma Formation
Maraloou Formation
Killara Formation
Bartle Member
Medium- to coarse-grained dolerite dykes and sills
Aphyric tholeiitic basalt
Thaduna Formation
Johnson Cairn Formation
Juderina Formation
Bubble Well Member
Finlayson Member
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Playa deposits
Sandplain depositsColluvium and sheetwash deposits
CalcreteDuricrust
Permian sedimentary rock
Proterozoic rock
Archaean granitoid rock and associated eluvium
Archaean greenstone and associated eluvium
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Published 1:100000 maps used in compilation
See current GSWA map catalogue for full range of published products
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PATERSON FORMATION:
SYMBOLS
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SHEET SG 51-9
SECOND EDITION 1999
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GEOLO
G IC A L SURVEY
WE
ST
E R N A U S T RA
LIA
GEOLOGICAL SURVEY OF
WESTERN AUSTRALIA
DAVID BLIGHT, DIRECTOR
DEPARTMENT OF MINERALS
AND ENERGY
L. C. RANFORD, DIRECTOR GENERAL
GOVERNMENT OF WESTERN AUSTRALIA
HON. NORMAN MOORE, M.L.C.
MINISTER FOR MINES
D
A
E
B
C