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Precambrian Research xxx (2014) xxx–xxx

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review of volcanic-hosted massive sulfide (VHMS) mineralization inhe Archaean Yilgarn Craton, Western Australia: Tectonic,tratigraphic and geochemical associations�

.P. Hollisa,b,∗, C.J. Yeatsa, S. Wycheb, S.J. Barnesa, T.J. Ivanicb, S.M. Belfordc,.J. Davidsond, A.J. Roachee, M.T.D. Wingateb

CSIRO Earth Science and Resource Engineering, 26 Dick Perry Avenue, Kensington, Perth, Western Australia 6151, AustraliaGeological Survey Division, Department of Mines and Petroleum, East Perth, Western Australia 6004, AustraliaP.O. Box 1212, Fremantle 6959, AustraliaARC Centre for Excellence in Ore Deposits, School of Earth Sciences, University of Tasmania, 7001, AustraliaAngloGold Ashanti Australia Ltd, Level 13, 44 St. Georges Terrace, Perth, Western Australia 6000, Australia

r t i c l e i n f o

rticle history:eceived 31 March 2014eceived in revised form 30 October 2014ccepted 2 November 2014vailable online xxx

eywords:olcanic hosted massive sulfideHMSolcanogenic massive sulfideMSetrochemistryithogeochemistry

a b s t r a c t

The Archaean Yilgarn Craton of Western Australia represents a world-class metallogenic province, host-ing considerable resources of Au, Ni-sulfides and iron ore. Despite close geological similarities with thevolcanic-hosted massive sulfide (VHMS)-rich Superior Province of Canada, there is a strong disparity inthe number of discovered VHMS deposits between the two areas. This paper brings together recentlypublished U–Pb zircon geochronology and stratigraphic constraints from across the Yilgarn Craton, witha large number of existing whole rock geochemical datasets (881 samples from ∼125 localities). Recog-nized VHMS occurrences are placed in a detailed tectonic and stratigraphic framework. Temporal andgeochemical associations to mineralization are discussed. Areas of VHMS mineralization in the YilgarnCraton are preferentially associated with areas of thinned, juvenile crust as revealed through regional(Nd, Pb) isotope variations. The characteristics identified here for prospective host sequences are: largelybimodal volcanic complexes, synvolcanic faults, a spatial and temporal association to HFSE-enriched syn-volcanic intrusions, and the following geochemical signatures of felsic rocks. VHMS-bearing felsic rocksin the Youanmi Terrane and Eastern Goldfields are characterized by low Zr/Y, La/YbCN and Th/Yb ratios,high Sc/TiO2, Sc/V, HFSE and HREE contents, and flat HREE profiles similar to those of Abitibi greenstonebelt, Canada, and the Pilbara Craton of Western Australia. Chondrite-normalized REE profiles for felsicrocks overlying 2.82–2.80 Ga plume-related basalts and large igneous complexes of the Youanmi Terraneare flat. Other VHMS-bearing felsic rocks are characterized by slight LREE enrichment (La/SmCN < 3) andflattish HREE profiles. In the Youanmi Terrane four distinct periods of economic mineralization can berecognized: (i) >2.9 Ga (e.g. Golden Grove, Ravensthorpe), associated with early bimodal-mafic green-stone belts subjected to extension; (ii) c. 2815 Ma (e.g. Austin, Just Desserts, Youanmi), following a majorplume event and coeval with the emplacement of large igneous complexes across the northern YouanmiTerrane at shallow levels in the crust (Meeline and Boodanoo suites); (iii) 2760–2745 Ma (e.g. Hollandaire,Mt. Mulcahy) in areas of rift-related magmatism during the deposition of the Greensleeves Formation;(iv) c. 2725 Ma, in the Gum Creek greenstone belt associated with a second major plume event, broadly
coeval with the emplacement of high-level sills of the Yalgowra Suite. In the Eastern Goldfields Supert-errane, VHMS mineralization formed between c. 2700 and 2680 Ma (e.g. Teutonic Bore camp, Anaconda, Nimbus, Erayinia). All episodes of VHMS mineralization in the Yilgarn show strong temporal and spatial
Please cite this article in press as: Hollis, S.P., et al., A review

the Archaean Yilgarn Craton, Western Australia: Tectonic, stratigrhttp://dx.doi.org/10.1016/j.precamres.2014.11.002

associations to suites of HFSE-supersuite).

� This is a companion paper to “Submarine architecture of the Neoarchean Jaguar Voluminous extrusion”. Submitted to Precambrian Research by Belford S, Davidson GJ, M∗ Corresponding author at: CSIRO Earth Science and Resource Engineering, 26 Dick Perel.: +61 8 6436 8668.

E-mail address: [email protected] (S.P. Hollis).

ttp://dx.doi.org/10.1016/j.precamres.2014.11.002301-9268/© 2014 Elsevier B.V. All rights reserved.

of volcanic-hosted massive sulfide (VHMS) mineralization inaphic and geochemical associations. Precambrian Res. (2014),

enriched granitic intrusions (e.g. Eelya suite, Mt. Kenneth suite, Kookynie

© 2014 Elsevier B.V. All rights reserved.

HMS deposit, Western Australia, is a product of combined subtle extension andcPhie J and Large RR.ry Avenue, Kensington, Perth, Western Australia 6151, Australia.

dx.doi.org/10.1016/j.precamres.2014.11.002


http://www.sciencedirect.com/science/journal/03019268

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ontents

1. Introduction . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 002. Regional geology . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 00

2.1. Narryer and South West terranes . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 002.2. Youanmi Terrane . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 002.3. Eastern Goldfields Superterrane (EGS) . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 00

3. What is petrochemically prospective? . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 004. Geochemistry: methods . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 005. Geochemistry of felsic rocks in the Yilgarn craton . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 00

5.1. Areas associated with VHMS mineralization . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 005.2. Comparisons to the Abitibi subprovince. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 00

6. Tectonic-stratigraphic framework . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 006.1. Youanmi Terrane . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 006.2. Kalgoorlie and Kurnalpi terranes . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 006.3. Burtville and Yamarna terranes . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 006.4. South West Terrane . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 00

7. Conclusions . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 00Acknowledgements . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 00Appendix . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 00Appendix B. Supplementary data . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 00References . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 00

. Introduction

The Archaean Yilgarn Craton of Western Australia represents aorld-class metallogenic province, hosting considerable resources

f Ni-sulfides, Au and iron ore (Barnes, 2006; Blewett et al.,010a,b). Following the 1963 discovery of the giant Kidd Creeku–Zn deposit in Canada, the Archaean Yilgarn and Pilbara cratonsf Western Australia were actively targeted for volcanic-hostedassive sulfide (VHMS) mineralization throughout most the 1960s

nd 1970s (McConachy et al., 2004). The main exploration tech-ique was gossan searching (Butt, 2004) coupled with geophysics.ne substantial find was made at Gossan Hill in 1971 (Golden Groveamp; Ashley et al., 1988), and a smaller but higher grade find wasade in 1976 at Teutonic Bore in the Eastern Goldfields Superter-

ane (Hallberg and Thompson, 1985) (Fig. 1; Table 1). By the early980s, the general lack of success and an increasing gold price saw

change in focus and VHMS mineralization effectively dropped offhe exploration agenda in Western Australia for the next 25 yearsYeats, 2007). By 2004 only six significant base metal deposits hadeen brought into production out of all VHMS deposits hosted inroterozoic and Archaean rocks of Western Australia – two of whichere principally mined for Au (McConachy et al., 2004). Perhapsnsurprisingly, there has been much discussion about whether theilgarn Craton is intrinsically impoverished in VHMS mineraliza-ion or is simply underexplored (e.g. Witt et al., 1996; Ferguson,999; Brown et al., 2002; McConachy et al., 2004; Yeats, 2007;earncombe, 2010; Huston et al., 2014).

Historically there have been several major hindrances to VHMSxploration in the Yilgarn Craton, which is characterized by aaucity of outcrop, deep weathering and high strain (McConachyt al., 2004). Saline groundwaters have tended to overwhelmlectro-magnetic (EM) responses (Phillips, 2004), which combinedith deep weathering, conductive overburden and intercalated

lack shale horizons in prospective sequences, has meant feweposits have been discovered using such techniques. Electromag-etics is the principle exploration tool for VHMS mineralization

n Canada, and has only recently proven successful in the Yilgarn

meant deep weathering often hindered exploration efforts. Recentdevelopments in these fields and renewed exploration activitysince the early 2000s has led to a number of new discoveries, includ-ing further successes at Golden Grove, Nimbus and Manindi, andnew resources at Jaguar, Bentley, Austin, Just Desserts, Kundip andHollandaire (Fig. 1; Table 1). VHMS mineralization has also beenidentified at sites across the Yilgarn Craton, such as at The Cup,Erayinia (King) and Copper Bore (Fig. 1).

This paper brings together recently published U–Pb zircongeochronology and stratigraphic constraints from across theYilgarn Craton, with a large number of existing whole rock geo-chemical datasets (881 samples from ∼125 localities). RecognizedVHMS occurrences are placed in a detailed tectonic and strati-graphic framework. Temporal and geochemical associations tomineralization are discussed, including a temporal and spatial asso-ciation to geochemically HFSE-enriched granitic intrusive rocks inboth the Youanmi Terrane and Eastern Goldfields.

2. Regional geology

Through a combination of airborne magnetic surveys, detailedfollow up mapping, greatly expanded geochronology and isotopeterrane delineation, our understanding of the geology of the YilgarnCraton has improved considerably in recent years (e.g. Championand Sheraton, 1997; Cassidy et al., 2006; Champion and Cassidy,2007; Czarnota et al., 2010; Ivanic et al., 2010; Pawley et al., 2012;Van Kranendonk et al., 2013; Mole et al., 2014). The Yilgarn Cra-ton has historically been divided into a series of terranes basedon distinct lithological associations, geochemistry and ages of vol-canism (Gee et al., 1981; Myers, 1990; Cassidy et al., 2006). Thewestern half of the Yilgarn Craton comprises the Narryer, SouthWest and Youanmi terranes (Fig. 1). East of the Ida Fault, the EasternGoldfields Superterrane (EGS) can be divided into the Kalgoor-lie, Kurnalpi, Burtville and Yamarna terranes (Pawley et al., 2012;Fig. 1). Terranes are further divided into domains, all of which arebounded by an interconnected system of faults.



raton (e.g. Jaguar deposit: Ellis, 2004). Although deep weather-ng in Australia increases the economics of some deposits (e.g.imbus: McConachy et al., 2004; Hollandaire: Hayman et al.,

ubmitted for publication), a poor understanding of regolith pro-esses until recent decades (reviewed in Anand and Butt, 2010) has

Competing models for the formation of the Yilgarn Craton vari-


ably invoke Archaean subduction, arc and/or plume magmatism,and the accretion of allochtonous terranes (discussed in Czarnotaet al., 2010; Barnes et al., 2012; Van Kranendonk et al., 2013). Debateprimarily concerns whether subduction is required to explain the


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Table 1VHMS resources in the Youanmi Terrane and Eastern Goldfields Superterrane, Yilgarn Craton.

Terrane Domain Age (Ma) Deposit Year of discovery Mt Cu (%) Zn (%) Pb (%) Ag (g/t) Au (g/t) Resource reference

Youanmi Murchison ca. 2960–2930

[Golden Grove Camp]

Gossan Hill 1971 15.9 2.6 1.5 0.2 21 0.6 Gawlinski (2004); McConachy et al. (2004); MMG (2011);*pre-mining reservesScuddles 1979 10.5* 1.2 11.7 0.8 89 1.1

Amity 1999 1.91 15.1 1.4 93 2.00.25 10

Hougoumont 1999 0.56 21.5 7.5 305 6.21.49 14.6 2.1 89 2.0

Catalpa 1999 0.63 15.5 1.6 185 2.7Ethel 2000 0.45 20.7 2.5 5.8Xantho 2003 0.4 11.9Cambewarra 2003 0.14 13.3Gossan Valley/Felix 1971–1972/1979 1.5 7.9 10 0.9

1.3 2.3 14 0.3ca. 2930 Mt Gibson 1975 25.9 1.94 McConachy et al. (2004)ca. 2746 Hollandaire 2011 2.8 1.6 5 0.4 Inferred resource. Silver Lake Resources (2013a)ca. 2718 Austin (Quinns) 2008 1.48 1.02 1.39 3.31 0.24 Maiden resource. Silver Swan (2012)ca. 2814 Manindi (Freddie Well) 1972 1.35 0.25 6.04 3.4 0.25 JORC resource. Metals Australia Ltd. (2012)ca. 2815? Mt. Mulcahy Historic 0.25* 3.77 2.75 Marston (1979); *assuming a minimum true thickness of

1.52m and cut off of 2.5%Cu

Youanmi Southern Cross ca. 2813 Just Desserts 2007–2008? 1.07 1.82 0.8 JORC resource. Empire Resources (2012)ca. 2950 Kundip – 8.94 0.3 2.3 2.7 Silver Lake Resources (2013b)

Kurnalpi Gindalbie ca. 2690[Teutonic Bore Camp]

Teutonic Bore 1976 1.68* 3.5 10.7 140 *Production to end-1984 (Ellis, 2004); **Pre-miningreserve (Jabriu Metals 2006); ***Pre-mining resource(indicated and inferred) (Jabriu Metals, 2010)

Jaguar 2002 1.60** 3.1 11.3 0.7 115Bentley 2008 3.05*** 2.0 9.8 0.6 139 0.7

Murrin ca. 2700 Anaconda Historic Historic Cu production (4595t) Marston (1979)

Kalgoorlie Boorara ca. 2700? Nimbus 1993 4.88 1.33 79 0.29 Resource as of 25th July 2013. (MacPhersons, 2014)

Adapted from McConachy et al. (2004).


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Fig. 1. Major subdivisions of the Yilgarn Craton, Western Australia, showing the distribution of greenstone belts and base metal occurrences (excluding those associatedwith Ni mineralization). Significant VHMS resources, greenstone belts (green) and base metal occurrences discussed in the text are labelled. Terrane and domain boundaries( th thet 0.asp( to the

ehpemVEEE2giicKiaTbr

solid black lines) are modified after Cassidy et al. (2006) and Barley et al. (2008), wihe GSWA mineral occurrence database MINEDEX (http://www.dmp.wa.gov.au/397For interpretation of the references to color in figure legend, the reader is referred

volution of the EGS and which of the various terranes and domainsave a common history. While a number of workers favour bothlume and subduction processes (Czarnota et al., 2010; Hustont al., 2014), others highlight the problem of scale as plume mag-atism is expected to overwhelm subduction (Barnes et al., 2012;an Kranendonk et al., 2013; Barnes and Van Kranendonk, 2014).vidence for a common history between the Youanmi Terrane andGS, includes: (i) contemporaneous plume magmatism across theGS and Youanmi Terrane from at least c. 2.82 Ga (Ivanic et al.,010; Barnes et al., 2012); (iii) contemporaneous and voluminousranitic magmatism across the whole craton prior to the tim-ng of inferred accretion (Czarnota et al., 2010); (iv) simultaneousnferred ‘subduction-related’ magmatism across the whole of theraton inconsistent with the geometry of modern arc systems (Vanranendonk et al., 2013); and (v) stratigraphic and isotopic similar-

ties between the Kalgoorlie and Yamarna terranes, and Youanmi



nd Burtville terranes (Pawley et al., 2012; Mole et al., 2014).he issue remains highly contentious and the two models wille discussed further in Section 2.3 (Eastern Goldfields Superter-ane).

VHMS prospective Gindalbie domain labelled (G). Base metal occurrences are fromx). The box shows the location of Fig. 3. GB, greenstone belt; MB, metamorphic belt.

web version of the article.)

2.1. Narryer and South West terranes

The Narryer and South West terranes of the western YilgarnCraton are dominated by granite and granitic gneiss with minorsupracrustal greenstone inliers (Fig. 1). The c. 3.7 Ga Manfred Com-plex (a dismembered layered igneous complex) and MeeberrieGneiss (a sequence of felsic intrusive rocks) represent the old-est sequences of the Narryer Terrane (Wyche et al., 2013). Bothwere intruded by felsic magmas (c. 3.3 Ga; e.g. Dugel and Euradagneisses) and deformed and metamorphosed between amphibo-lite and granulite facies prior to the deposition of supracrustal rocks(e.g. Jack Hills greenstone belt) (Wyche et al., 2013). Early Archaeangneisses of the Narryer Terrane may represent an allochthon thrustover 3.0–2.9 Ga granitic crust of the Youanmi Terrane (Wyche et al.,2013).

The South West Terrane comprises strongly deformed, high-


grade granite-gneiss, metasedimentary and metaigneous rocksintruded by 2750–2620 Ma granites and pegmatites (Mole et al.,2012). Supracrustal successions range in age from 3200 to 3010 Main the Chittering, Jimperding and Balingup(?) metamorphic belts


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nd the Wongan Hills greenstone belt, to 2715–2675 Ma in the Sad-leback and Moranup greenstone belts (e.g. Pidgeon and Wilde,990; Mole et al., 2012; Fig. 1).

.2. Youanmi Terrane

It is now clear through regional mapping, SHRIMP and isotopeata (e.g. Van Kranendonk et al., 2013) that the Murchison Domainnd northern part of the Southern Cross Domain (Fig. 1) largelyhare a common history and were not brought together by anccretionary event (Ivanic et al., 2010; Wyche et al., 2013). Isotopetudies reveal a long process of crustal formation and rework-ng in the Youanmi Terrane (Champion and Cassidy, 2007; Ivanict al., 2012; Wyche et al., 2012; Mole et al., 2014). Detrital zirconsn quartzites and xenocrystic zircons from intrusive and extru-ive rocks date back to >4.0 Ga (Nelson, 1997; Wyche, 2007). Vanranendonk et al. (2013) recently presented a revised stratigra-hy for the long-lived, autochthonous Murchison Domain (Fig. 2),hich is likely comparable to the northern part of the South-

rn Cross Domain. Early supracrustal sequences in the Murchisonhich formed prior to 2.9 Ga are locally preserved in the Yalgoo-

ingleton (c. 2.96–2.93 Ga: Wang, 1998), Weld Range (c. 2.97 Ga:ingate et al., 2008), Tallering (c. 2.94 Ga) and Twin Peaks (c. 3.0 Ga:

idgeon and Wilde, 1990) greenstone belts. All of these green-tone belts contain VHMS mineralization. In the Southern Crossomain, supracrustal sequences of similar age (i.e. >2.9 Ga) occur

n the Ravensthorpe (c. 3.0–2.95 Ga: Witt, 1999), Koolyanobbingc. 3.0 Ga: Angerer et al., 2013), Marda-Diemals (c. 3.0 Ga?: Chent al., 2003), Forrestania (c. 2.9 Ga?: Perring et al., 1996), Southernross (c. 2.93–2.91 Ga?: Mueller and McNaughton, 2000) and Lake

ohnston (c. 2.92–<2.78 Ga: Romano et al., 2013) greenstone belts.Following an extended depositional hiatus across the Youanmi

errane (≤110 Myr), the unconformably overlying 2825–2805 Maorie Group was deposited (Van Kranendonk et al., 2013; Fig. 2).xposed predominantly across the northern parts of the Murchi-on Domain, the Norie Group records a major mantle meltingvent at c. 2.82 Ga which resulted in the emplacement of largeafic–ultramafic layered intrusions (Ivanic et al., 2010) and the

ruption of the Murrouli Basalt Formation (Watkins and Hickman,990; Van Kranendonk et al., 2013). This significant mantle melt-

ng event, possibly plume-related (Ivanic et al., 2010, 2012; Nebelt al., 2013), may have resulted in the partial breakup of the proto-ilgarn Craton, with E-W extension marked by younger Nd isotopeodel ages (Fig. 3; Czarnota et al., 2010; Huston et al., 2014). These

reas of thinned, juvenile crust (e.g. Cue Zone; Fig. 3) have beeninked to subsequent episodes of VHMS mineralization across theilgarn Craton (Huston et al., 2005, 2014). The Murrouli Basaltormation comprises a c. 4 km thick sequence of interbedded Ti-ich, Al-depleted komatiites and komatiitic volcaniclastic rocksverlain by tholeiitic basalts (Barley et al., 2000). Conformablyverlying rocks of the c. 500 m thick Yaloginda Formation are dom-nated by felsic volcanic and volcaniclastic sedimentary rocks andnterbedded units of ferruginous shale and/or BIF (Van Kranendonkt al., 2013; Fig. 2). Felsic volcanic rocks coeval with the Yalogindaormation also overlie the large 2.82 Ga layered intrusions (e.g.indimurra and Narndee igneous complexes) as the Kantie Mur-

ana Volcanics Member. Both the Yaloginda Formation and Kantieurdana Volcanics Member host significant VHMS mineralization

round Quinns, Narndee, Windimurra and Youanmi (Fig. 4).The 2800–2730 Ma Polelle Group (?dis)conformably overlies the

orie Group and consists of the following formations (Fig. 2): (i)oodardy – characterized by a thin (100 m thick) unit of basal



uartzite and BIF; (ii) Meekatharra – comprising a 2.5 km thickequence of tholeiitic basalt, komatiitic basalt, komatiite and thinnterflow 2800–2760 Ma felsic volcaniclastic sedimentary rocks;iii) Greensleeves – dominated by a ≤5 km thick, 2760–2740 Ma,

PRESSsearch xxx (2014) xxx–xxx 5

VHMS-bearing andesitic to rhyolitic volcanic and volcaniclasticrocks; and (iv) Wilgie Mia – characterized by interbedded BIF,shale and felsic volcaniclastic rocks (Van Kranendonk et al., 2013).Subduction affinity magmatism during the Greensleeves Forma-tion, coupled with the postulated existence of boninites, may berelated to convergence between the Narryer and Youanmi terranes(Wyman and Kerrich, 2012). A second (less-significant) unconfor-mity separates the Polelle Group from the overlying 2735–2700 MaGlen Group (Fig. 2), which includes the: (i) Ryansville Formation –dominated by clastic sedimentary rocks; and (ii) Wattagee Forma-tion – characterized by komatiitic basalt and subordinate rhyolite.The deposition of the Wattagee Formation was coeval with theemplacement of widespread, thick and differentiated sills of theYalgowra Suite (Figs. 2 and 4), predominantly hosted in the olderGreensleeves Formation (Ivanic et al., 2010; Wyche et al., 2013) andkomatiitic volcanism in the EGS (Section 2.3; Fig. 5).

In the northern part of the Southern Cross Domain, simi-lar greenstone sequences have been recognized to those of theMurchison Domain. In the Marda-Diemals greenstone belt a lowerVHMS-bearing greenstone sequence proposed to be c. 3.0 Ga inage (Chen et al., 2003) is unconformably overlain by the calc-alkaline (and possibly subduction related: Morris and Kirkland,2014) c. 2730 Ma Marda Complex and the clastic Diemals Forma-tion. Recent U–Pb zircon geochronology on an intrusive gabbro (c.2.8 Ga: Wingate et al., 2011b) from the lower greenstone sequencesuggest it may be may equivalent to mafic rocks which intrudethe Norie Group at this time (Fig. 2), implying the Murchison andnorthern part of the Southern Cross Domains shared a common his-tory prior to 2.8 Ga (Riganti et al., 2010). Similar assemblages to thelower greenstone sequence also occur in the Booylgoo Range green-stone belt of unknown age (Wyche et al., 2013). Further north inthe Southern Cross Domain, the c. 2722 Ma Gum Creek greenstonebelt (Bodorkos et al., 2006) is characterized by VHMS-bearing felsicvolcanic/volcaniclastic rocks, clastic sedimentary rocks and abun-dant graphitic shale (e.g. The Cup, Bevan: Fig. 1). Granitic rocksconstrained to c. 2800 Ma (Wingate and Bodorkos, 2007b) intrudethe northern end of the Gum Creek greenstone belt, indicating anolder age for part of the local stratigraphy.

2.3. Eastern Goldfields Superterrane (EGS)

In the Eastern Goldfields Superterrane at least four distinctperiods of volcanism are preserved: (i) at c. 2940 Ma in the Kalgoor-lie and Burtville terranes; (ii) a fragmentary record from c. 2810 Main the northern Kalgoorlie, Kurnalpi and Burtville terranes (Wiluna,Laverton and Duketon domains respectively); (iii) at c. 2760 Ma inthe Burtville Terrane (Merolia Domain); and (iv) a more consistentrecord from c. 2715 Ma in all terranes (Fig. 4; Czarnota et al., 2010).Although local stratigraphy has been established for a number ofgreenstone belts of the EGS, a detailed regional stratigraphy hasonly been described for the southern part of the Kalgoorlie Terrane(Fig. 5). This consists of a lower 2710–2692 Ma mafic–ultramaficsuccession (Beresford et al., 2005; ‘Kambalda Sequence’: Fig. 5)succeeded by the 2690–2660 Ma ‘Kalgoorlie Sequence’ (Krapezand Hand, 2008). The latter is characterized by a >3 km thickpackage of volcaniclastic rocks, felsic volcanic rocks, mafic intru-sive complexes with minor mafic volcanic rocks (Squire et al.,2010).

The mafic–ultramafic succession is related to a major plumeevent in the Yilgarn Craton at 2.72 Ga, broadly contemporane-ous with komatiitic magmatism in the Wattagee Formation ofthe Youanmi Terrane and the emplacement of the Yalgowra Suite


(Fig. 2). The occurrence of geochemically similar komatiites andbasalts at the same relative stratigraphic position across the Kalgo-orlie and Kurnalpi terranes of the EGS between 2705 and 2690 Masuggest the eastern Yilgarn Craton was assembled by 2705 Ma




Fig. 2. Stratigraphic scheme for the Murchison Domain within the Youanmi Terrane, divided into three main columns for supracrustal rocks, granitic rocks andultramafic–mafic intrusive rocks (Van Kranendonk et al., 2013). Granitic suites which display HFSE-enriched geochemical characteristics are highlighted. Areas associ-ated with the four main periods of VHMS mineralization in the Youanmi Terrane (as indicated by grey bars) include: 1 – Golden Grove, Ravensthorpe, Twin Peaks, Tallering,Weld Range; 2 – Copper Bore, Just Desserts, Quinns (Austin), Pincher Well, Narndee, Manindi, Chunderloo, Windimurra, Copper Hills, Barrambie; 3 – Hollandaire, Mt. Mulcahy,Emily Well, Chesterfield/Jillewarra, Abbotts; 4 – Gum Creek greenstone belt (The Cup, Bevan, Eds Bore); Wattagee Well(?), Marda Complex(?). (A)–(I) represent U–Pb zirconages for HFSE-enriched granitic rocks: (A) Mount Gibson monzogranite (Yeats et al., 1996); (B) Courlbarloo tonalite (AMIRA P482: Fletcher and McNaughton, 2002); (C) PeterWell biotite granite (Wingate et al., 2010b); (D) Eelya granitoid (Wang ANU unpublished cited by Fletcher and McNaughton, 2002); (E) Peter Well monzogranite (Wang,1998); (F) Peter Well granodiorite (Wang, 1998); (G) Keygo granophyric granodiorite (Fletcher and McNaughton, 2002); (H) Butcher Bird granophyre (Nelson, 2001a); (I)Montague monzogranite (Wang et al., 1998); (J) Damperwah granite (Wiedenbeck and Watkins, 1993); (K) Coolamen hornblende-biotite granite (Fletcher and McNaughton,2 ocks:

M athlee2

(tKTflYnd

KltTar(crcah

002). (L)–(R) represent U–Pb geochronology ages for ultramafic–mafic intrusive rurroulli dolerite (Wang, 1998); (O) Fleece Pool gabbro (Ivanic et al., 2010); (P) K

000); (R) Waladah gabbro (Ivanic et al., 2010).

Barnes et al., 2012). Plume-related komatiitic cumulate bodies ofhe Kalgoorlie Terrane host world-class Ni resources such as Mt.eith and Black Swan (Barnes, 2006; Barnes and Fiorentini, 2012).hese cumulate bodies are interpreted as the products of high-ux komatiite volcanism focused along the eastern margin of theouanmi Terrane. Thin, sparsely distributed komatiites of the Kur-alpi Terrane most likely represent thin flows or ponded lava lakesistal to the main source of volcanism (Barnes et al., 2012).

Between 2692 and 2680 Ma volcanic centres in the westernurnalpi Terrane (Gindalbie Domain: Fig. 1) are associated with

argely bimodal (basalt-rhyolite) volcanic and associated sedimen-ary rocks, although some contain significant volumes of andesites.hese rocks have been attributed by some workers as forming inrc-rift environments (see following) and are broadly contempo-aneous with the early Black Flag Group of the Kalgoorlie TerraneFig. 5). VHMS mineralization in the central EGS is closely asso-iated with HFSE-enriched felsic volcanic rocks, with significant



esources occurring in close proximity to geochemically similar andoeval large granitic complexes (Fig. 6; see Section 6.2). Late domingnd extension associated with the emplacement of a widespreadigh-Ca tonalite-trondjhemite-granodiorite (TTG) suite produced

(L) Gabanintha gabbro (Wang, 1998); (M) Narndee gabbro (Ivanic et al., 2010); (N)n Valley gabbro (Liu et al., 2002); (Q) Dalgaranga dolerite (Pidgeon and Hallberg,

the late clastic basins of the Yilgarn Craton (Wyche et al., 2013;Fig. 5).

Regarding tectonic setting, as stated previously there is stilldebate on whether subduction is required to explain the evolu-tion of the EGS. A number of workers have invoked subductionprocesses to explain the petrogenesis of >2.72 Ga intermediate andfelsic rocks of the Kurnalpi and Kalgoorlie terranes (e.g. Brown et al.,2002; Barley et al., 2008; Czarnota et al., 2010; Belford et al., inpreparation). Following early extension at c. 2810 Ma along theeastern margin of the Youanmi Terrane, Czarnota et al. (2010)suggested that west dipping subduction was initiated between2715 Ma and 2690 Ma. This resulted in arc volcanism in the KurnalpiTerrane and back-arc extension in the Kalgoorlie Terrane. However,recent work (Barnes et al., 2012; Barnes and Van Kranendonk, 2014)has suggested that plume magmatism (combined with magma-mixing and crustal contamination) can produce all the observedgeochemical characteristics for mafic, intermediate and felsic rocks


in the EGS. Although the back-arc setting fits with the location ofVHMS mineralization in the Gindalbie Domain around TeutonicBore (Fig. 3), it is worth pointing out that VHMS mineralization mayalso form in other tectonic settings associated with extension and



S.P. Hollis et al. / Precambrian Research xxx (2014) xxx–xxx 7

Fig. 3. Regional Nd and Pb isotope variations of the Yilgarn Craton. (a) Nd-depleted mantle model (NdDM) age map of the northern Yilgarn Craton (after Champion and Cassidy,2007; Czarnota et al., 2010). Terrane boundaries (white dashed lines) and base metal localities are identical to those shown in Fig. 1. (b) Nd2DM map of Huston et al. (2014)for the central Kalgoorlie and Kurnalpi terranes–box of Fig. 4a. (c) � map of Huston et al. (2014) for the central Kalgoorlie and Kurnalpi terranes. � represents 238U/204Pbintegrated to the present, with values calculated from galena and altaite Pb isotope data from VHMS and lode Au deposits of the EGS (described in Huston et al., 2005, 2014).Variations in � can be caused by fractionation of U and Pb in the source region and/or mixing between isotopically distinct reservoirs (such as an evolved crustal sourceand juvenile mantle sources). Juvenile Pb isotope characteristics (low �) at Teutonic Bore correspond to a narrow, linear zone of younger granite T2DM model ages (Fig. 3b).This was interpreted as a zone of extension by Huston et al. (2005, 2014), characterized by more juvenille basement. This zone of extension is consistent with mafic rocksat Teutonic Bore and Jaguar which resemble modern back-arc basin basalts (BABB) (e.g. Belford et al., submitted for publication) and melting of basalt at low pressure tof e heatm

hittN

rYc2hauctaNc2

orm FIII-affinity (or A-type) felsic rocks of the Gindalbie Domain. High temperaturineralization.

igh heat flow. Regardless of whether subduction was involved, Ndsotope data clearly indicates VHMS mineralization occurred alonghe margins of rift-zone (either back-arc or intra-cratonic) charac-erized by juvenile Pb isotope signatures (low �: <8.3) and youngerdDM ages (see Fig. 3; Huston et al., 2014).

Recent work by Pawley et al. (2012) has detailed the stratig-aphy of the Burtville and Yamarna terranes of the easternmostilgarn Craton (Supplementary Fig. 1). Four main episodes ofrustal growth were recognized at 2970–2910 Ma, 2815–2800 Ma,775–2735 Ma and 2715–2630 Ma. Whereas the Burtville Terraneas affinities with the Youanmi Terrane, the Yamarna Terrane hasffinities with the Kalgoorlie Terrane (Fig. 5; Supplementary Fig-re). Pawley et al. (2012) suggested extension and thinning at. 2720 Ma led to the separation of the Burtville and Youanmierranes (also discussed in Mole et al., 2014), although this is



gain controversial. Xenocrystic zircons (>2.72 Ga) and >3000 Mad model ages in granites and volcanics also suggest that olderrust remains beneath the juvenile terranes of the EGS (Mole et al.,014).

flow associated with extension and crustal (and mantle) melting facilitated VHMS

3. What is petrochemically prospective?

In the last 25 years, major advances have been made inpetrochemical (Lesher et al., 1986; Lentz, 1998; Wyman, 2000;Piercey et al., 2001; Hart et al., 2004; Piercey, 2011) and lithogeo-chemical VHMS exploration (e.g. element mobility, hyperspectrallogging and mapping). This is partly due to the routine applicationand increasingly low costs of multi-element ICP-MS geochem-istry, which has allowed exploration companies to plan drillingcampaigns based on the identification of VHMS favourable hostsequences and hydrothermal assemblages. VHMS deposits formin volcanic successions due to focused heat flow associated withhydrothermal convection, which is the result of tectonic extension,mantle depressurization and the formation of high temperaturemelts (Galley, 1993, 2003; Franklin et al., 2005; Galley et al., 2007).


Ultimately, petrochemical assemblages of mafic and felsic rocksindicative of an extensional tectonic setting and high temperatureheat flow at shallow crustal levels are desired (Lesher et al., 1986;Hart et al., 2004; Piercey, 2011).




F rn par(

fCtfip2afiRtiGtrabp(e

ig. 4. Distribution of mafic suites and HFSE-enriched granitic rocks in the northestars) as in Fig. 1.

Lesher et al. (1986) first proposed a threefold division of VHMS-ertile versus barren felsic rocks from the Superior Province ofanada (FI–FIIIb type). This scheme was subsequently appliedo Proterozoic and Phanerozoic deposits worldwide, and modi-ed to include FIV affinity felsic rocks common to post-Archaeanrimitive arcs (Barrie et al., 1993; Lentz, 1998; Piercey et al.,001; Hart et al., 2004). FI affinity felsic rocks are typically calc-lkaline (i.e. high Zr/Y, La/Yb, Th/Yb), with relatively low higheld strength element (HFSE) concentrations and strongly light-EE (LREE) enriched chondrite-normalized REE profiles relative tohe heavy-REE (HREE). This petrochemically unfavourable suite isndicative of deep melting and therefore reduced crustal heat flux.eochemical characteristics are due to the retention of Sc, Y and

he HREE by garnet (and to a lesser extent amphibole) in the sourceegion. The FII suite represents an intermediate stage between FInd FIII affinity felsic rocks. FIII affinity felsic rocks are characterized



y low Zr/Y and La/Yb, flat and tholeiitic chondrite-normalized REEatterns, and elevated HFSE contents (especially Y, Zr > 200 ppm)Piercey, 2011). In Archaean environments VHMS deposits are pref-rentially associated with FIII (and to a lesser extent FII) affinity

t of the Youanmi Terrane (after Ivanic et al., 2010, 2012). Base metal occurrences

rhyolites. These rocks are interpreted to have formed within riftsequences from high-temperature melts (T > 900 ◦C) at shallowto mid-crustal depths during extension (Piercey, 2011). Rhyolitesassociated with continental rifts or continental back-arc rifts oftendisplay extreme HFSE concentrations and higher REE contents (Leatet al., 1986; McConnell et al., 1991; Dusel-Bacon et al., 2012). TheFIV suite of Hart et al. (2004) is of little interest here as theserocks are predominantly restricted to post-Archaean primitive-arcsequences (Piercey, 2011).

Although the above scheme is broadly applicable to most VHMS-hosting felsic rocks worldwide, there are a number of importantexceptions: (i) post-Archaean deposits associated with continen-tal crust; and (ii) Au-rich VHMS deposits. It is well establishedthat rhyolites associated with the post-Archaean VHMS-rich Fin-layson Lake, Que River, Kuroko and Mount Windsor regions candisplay elevated Zr/Y and La/YbCN ratios and FI affinities (Ohmoto


and Skinner, 1983; Piercey et al., 2001, 2008). As noted by Pierceyet al. (2008), although such rocks can display ‘petrochemicallyunfavourable’ high Zr/Y and La/YbCN ratios, they often retain thecommon HFSE and REE enrichment typical of VHMS-hosting felsic




Fig. 5. Stratigraphic scheme for the Eastern Goldfields Superterrane (Czarnota et al., 2010). U–Pb geochronology ages for HFSE-enriched granitic rocks from Champion andC amyaT

rwataec

Lstt

assidy (2002); also Cassidy and Champion (2002). Localities: BW, Bore Well; J, JeedB, Teutonic Bore; WW, Welcome Well.

ocks worldwide. As the Lesher et al. (1986) classification schemeas initially conceived for use in Archaean environments, which

re dominated by basaltic substrate, it has its limitations in Pro-erozoic and Phanerozoic terranes. In these instances, high La/YbCNnd Zr/Y ratios not only reflect the depth of melting but also thefficiency of melting HFSE and REE enriched accessory phases ofontinental crust (discussed in Piercey et al., 2008).

In their recent review of Au-rich VHMS deposits, Mercier-



angevin et al. (2011) noted that most deposits occur at specifictratigraphic positions and volcanic settings, which differ fromhe Cu–Zn deposits in these districts. It has been suggested thathe Au-rich LaRonde deposit formed closer to the subduction

; LB, Liberty Bore; M, Melita; MM, Murrin Murrin (i.e. Anaconda); SW, Spring Well;

zone, associated with the rifting of thicker crust than the typi-cal Cu–Zn Noranda-type VHMS deposits (Mercier-Langevin et al.,2007). Again, partial melting of (or contamination by) continen-tal crust during the genesis of felsic rocks will lead to highLa/Yb and Zr/Y ratios. The hybrid characteristics of Au-rich VHMSdeposits towards epithermal-style mineralization are consistentwith their formation at shallower water depths, further fromthe back-arc spreading centre (Mercier-Langevin et al., 2011).


No Au-rich VHMS deposits have been identified in the YilgarnCraton, although the Ag-rich Nimbus deposit (Fig. 1) has manycharacteristics of a shallow water and low temperature VHMSdeposit.




F terranC

4

gnbiRdguirVHi(d(icm

ig. 6. Distribution of HFSE-enriched granitic rocks in the Eastern Goldfields Superassidy and Champion (2002).

. Geochemistry: methods

To investigate the geochemistry of felsic rocks across the Yil-arn Craton whole rock geochemical data was compiled from aumber of datasets (listed in the Appendix). This is complimentedy new Geological Survey of Western Australia (GSWA) geochem-

stry from the EGS (Anxiety Bore, Kookynie, Teutonic Bore andocky Dam) and Gum Creek greenstone belt (Montague Grano-iorite). All geochemical analyses were divided into lithologicalroupings based on original sample descriptions. Those classified asltramafic, mafic, granite-gneiss, banded iron formation and sed-

mentary from sample descriptions were removed. Intermediateocks were retained due to their occurrence around a number ofHMS deposits (e.g. Golden Grove, Teutonic Bore camp, Mt. Gibson,ollandaire; see discussion). Mafic associations to VHMS mineral-

zation will be discussed elsewhere. The database presented hereSupplementary Information) includes 881 samples from interme-iate and felsic rocks from ∼125 localities across the Yilgarn Craton



Fig. 7). As the datasets included herein were produced using var-ous techniques, over several decades, from different laboratories,areful consideration was given to detection limits. Historically,ost trace element data would have been obtained by XRF analysis,

e. Supersuite divisions and U–Pb ages are from Champion and Cassidy (2002); also

which has significantly poorer detection limits than modern ICP-MS analysis (e.g. REE, Th, Nb, Ta, Hf). It was clear that for a number ofthe published datasets, results below detection had been set to spe-cific values (e.g. 0.5× detection limits). To maintain a high degree ofquality in the retained database results below 1.5× XRF trace ele-ment detection limits were removed. Cut off values predominantlyaffected ultramafic and mafic rocks which are not of interest here.The only exception for the above rule was for the REE, which wereretained if the analysis included the HREE and was obtained byICP-MS in recent years; or displayed relatively smooth chondrite-normalized profiles. Ta and Hf data were also retained, although noratios were calculated using these elements. Major element datawere recalculated to 100% excluding LOI, S, CO2 and H2O+. Trace-elements were recalculated using the same corrections to maintainelement ratios. Iron is reported as Fe2O3T calculated from FeO andFe2O3 values after the method of Grunsky (2013).

Following the subdivision of samples into lithology groupingsbased on rock descriptions and the removal of questionable low


concentration data, samples were geochemically classified usinga number of standard published diagrams. This was primarily tocheck if samples had been correctly described in the first instance.Due to the extensive metamorphism and hydrothermal alteration


ING ModelP

ian Re

atSavomae(h(vat((xrfifibtred

aBivaai(hcc(haClwacw

5

ti2d2(1lJAatea



cross the Yilgarn Craton, elements easily mobilized by hydro-hermal fluids should be avoided for classification purposes (e.g.iO2, K2O, CaO, Na2O, MgO, Sr, Ba: MacLean, 1990). Silicificationnd sericitisation is a common feature of hydrothermally alteredolcanic rocks and consequently the Total Alkali–Silica diagram isf limited use (e.g. Fig. 8a), showing considerable scatter for inter-ediate and felsic rocks. Large mass gains of SiO2 are not always

pparent in analytical data due to the effects of closure. Immobilelement classifications using bivariate plots that do not use ratiose.g. Th-Co diagram of Hastie et al., 2007) are also not suitable forydrothermally altered rocks subjected to significant mass changeMacLean, 1990). A more appropriate method for classifying alteredolcanic rocks is using immobile element ratios, such as Zr/TiO2nd Nb/Y (Pearce, 1996). From comparison between rock descrip-ions and the Pearce (1996) diagram, there is some scatter for maficnot shown) and felsic rocks towards intermediate Zr/TiO2 ratiosFig. 8b). This may be due a combination of five possible causes: (i)enocrystic zircons may lead to uncharacteristically high Zr/TiO2atios; (ii) the samples may have not been correctly named in therst instance; (iii) the data fall within the ‘noise’/error of the classi-cation diagram; (iv) the HFSE were not strictly immobile; and (v)asalts classify as intermediate compositions because their man-le sources were modified by subduction melts with high Zr/TiO2atios (see Pearce, 1996). However, considering the original errorllipses of Pearce (1996) the majority of the felsic and intermediateata plot in the appropriate fields (Fig. 8b and c).

After samples were classified into rock types their magmaticffinity was investigated using the schemes of MacLean andarrett (1993); modified by Barrett and MacLean (1994). Tholei-

tic volcanic rocks are distinguished from calc-alkaline affinityolcanic rocks using Zr/Y, Th/Yb and La/Yb ratios. Traditionalpproaches using the AMF diagram (Irvine and Baragar, 1971)re not appropriate due to element mobility. Although the orig-nal MacLean and Barrett (1993) scheme was recently refinedRoss and Bédard, 2009), we have retained the original valueserein. The Ross and Bédard (2009) classification scheme wasonstructed using minimal felsic rocks (<4% were rhyolitic) andonsequently offers little discrimination for different felsic suitesFI–FIV) of interest for VHMS deposits. The term transitional is usederein to refer to geochemical characteristics between tholeiiticnd calc-alkaline magmas, not subalkaline and alkaline magmas.hondrite-normalized La/Sm, Dy/Yb and La/Yb ratios were calcu-

ated using values from McDonough and Sun (1995). For sampleshich lacked grid-coordinates (Whitford and Ashley, 1992; Yeats

nd Groves, 1998; Sharpe and Gemmell, 2001) prospect/depositoordinates from the GSWA mineral occurrence database MINEDEXere used.

. Geochemistry of felsic rocks in the Yilgarn craton

Few studies have been published detailing the style and set-ing of individual VHMS deposits of the Yilgarn Craton (reviewedn Barley, 1992; Large, 1992; Ferguson, 1999; McConachy et al.,004; Yeats, 2007). Geochemical studies on the host-sequences ofeposits are restricted to those at Gossan Hill (Sharpe and Gemmell,001), Scuddles (Whitford and Ashley, 1992); Mount GibsonYeats and Groves, 1998), Teutonic Bore (Hallberg and Thompson,985), Jaguar (Belford, 2010; Belford et al., in preparation), Hol-

andaire (Hayman et al., submitted for publication), Yuinmery (i.e.ust Desserts: Hassan, 2014) and Weld Range (Guilliamse, 2013).lthough high-quality geochemical data is available for felsic rocks



ssociated with these areas, the sample distribution elsewhere inhe Yilgarn Craton is patchy (Fig. 7). No data were found for sev-ral recent discoveries (e.g. Bentley, The Cup), and the Twin Peaksnd Tallering greenstone belts. The petrogenesis of intermediate


and felsic rocks from the Youanmi Terrane and EGS are discussedin detail by Van Kranendonk et al. (2013); also Wyman and Kerrich(2012), and Barnes and Van Kranendonk (2014) respectively, andis beyond the scope of this paper.

5.1. Areas associated with VHMS mineralization

The geochemistry of felsic and intermediate volcanic/volcaniclastic rocks of the Yilgarn Craton is presented in Figs. 9–13.Through comparisons to the VHMS-rich Abitibi greenstone beltof Canada (Lesher et al., 1986; Barrie et al., 1993) it is clear felsicrocks of the Yilgarn Craton display a similar, broad range of geo-chemical characteristics, ranging from unprospective (FI affinity)to highly-prospective (FIIIb affinity) (Figs. 9 and 10; MacLean andHoy, 1991; Mercier-Langevin et al., 2007; Gaboury and Pearson,2008). VHMS-bearing felsic rocks in the Yilgarn Craton (e.g. GoldenGrove, Jaguar, Hollandaire, Dalgaranga, Youanmi, Gum Creek) aresimilar to those of the VHMS-rich camps of the Abitibi greenstonebelt and the Pilbara Craton of Western Australia (Figs. 9 and 10;discussed below).

VHMS-associated (and prospective) felsic rocks are character-ized by:

• high SiO2 in unaltered rocks,• tholeiitic to transitional Zr/Y and La/Yb values and FII to domi-

nantly FIII characteristics (Figs. 9, 10 and 13),• flattish REE profiles (La/SmCN < 3; Dy/YbCN ratios ∼1;

Figs. 11 and 12),• high HFSE (Y, Nb, Zr, Sc) concentrations (Fig. 10),• high Sc/TiO2 and Sc/V (Fig. 9),• low V and Th/Yb (Th/Yb < 2 and Th > 5 ppm; Fig. 13).

The high HFSE and HREE concentrations allow VHMS-bearing/prospective units to be distinguished from VHMS-barren/unprospective felsic rocks using ratios (e.g. Zr/Y, Sc/TiO2)and absolute concentrations (e.g. A-type affinities). Felsic rocksassociated with VHMS mineralization and those which dis-play prospective geochemical characteristics are restricted tofour periods in the Youanmi Terrane: (i) >2.9 Ga greenstonebelts (e.g. Golden Grove, Weld Range, Ravensthorpe); (ii) c.2815 Ma Yaloginda Formation and Kantie Murdana VolcanicsMember (e.g. Quinns/Austin, Narndee, Windimurra,); (iii) c.2750 Ma Greensleeves Formation (e.g. Hollandaire, Chesterfield,Dalgaranga); and (iv) c. 2725 Ma Gum Creek greenstone belt(Figs. 2 and 10). Felsic rocks which lack VHMS mineralization anddisplay unprospective geochemical signatures (i.e. steep, TTG-likeREE profiles) have also been recognized from each of these periodsexcept those which formed at c. 2815 Ma (e.g. Figs. 10 and 11).These rocks are equivalent to the TTG and TTG-high Gd/Yb groups ofBarnes and Van Kranendonk (2014), and are considered unprospec-tive for mineralization.

Chondrite-normalized REE profiles for VHMS-associated c.2815 Ma felsic rocks of the Youanmi Terrane (i.e. Yaloginda For-mation and Kantie Murdana Volcanics Member) are flat (Fig. 11d).Other VHMS-bearing units are characterized by slight LREE enrich-ment (La/SmCN < 3) and flat HREE profiles (Dy/YbCN ratios ∼1or less) (e.g. Figs. 11 and 12). HREE concentrations (e.g. YbCN)are higher in VHMS-associated felsic rocks than unprospectiveunits (Figs. 9 and 10). In some instances, Dy/YbCN values <1 andslight LREE-enrichment (La/SmCN < 3) produce weakly U-shapedchondrite-normalized REE profiles (e.g. Golden Grove Formation:


Fig. 11a). For the REE, the best discrimination is provided byDy/YbCN ratios, as HREE profiles are typically flat and Yb concen-trations are often higher in VHMS associated felsic rocks. La/YbCNratios of felsic rocks associated with VHMS mineralization are also




Fig. 7. Sample localities for felsic and intermediate rocks included in this study from the (a) western Yilgarn (i.e. South West and Youanmi terranes) and (b) Eastern GoldfieldsS

lH

f

uperterrane.



ower than unprospective units (due to LREE-enrichment over theREE).

Clear geochemical distinctions are also apparent betweenootwall felsic rocks and andesitic to felsic rocks in the hanging


wall of deposits where detailed studies have been carried out(Golden Grove: Whitford and Ashley, 1992; Sharpe and Gemmell,2001; Guilliamse, 2013; Mount Gibson: Yeats and Groves, 1998;Jaguar: Belford, 2010; Belford et al., submitted for publication).




Fig. 8. Whole rock geochemistry for samples included in this study. (a) Total Alkali – Silica diagram for intermediate (open circles) and felsic (filled circles) rocks. (b andc) Pearce (1996) immobile-element discrimination diagram for intermediate (b) and felsic (c) rocks. Probability ellipses of Pearce (1996) for various rock types are shown.These ellipses represent 10% probability contours – that is 10% of samples from that group (e.g. basaltic andesite) will plot outside the respective contour. The majority oft 100 pp

Acpfvrub(awp1Soih

he samples herein plot within the correct ellipses apart from rocks with high Cr (>

similar situation was noted in the Pilbara Craton by Vearn-ombe and Kerrich (1999); Figs. 9 and 12i. In stark contrast toetrochemically prospective footwall sequences, hanging wallelsic rocks represent a return to ‘normal’ (i.e. non rift-related)olcanism with steep REE profiles. These hanging wall felsicocks have geochemical characteristics typical of unprospectivenits worldwide (i.e. FI to FII affinities) and are characterizedy significantly higher Zr/Y, Th/Yb, La/YbCN and Dy/YbCN ratiosi.e. calc-alkaline characteristics), and lower Sc/TiO2, Sc/V, HFSEnd HREE contents (Fig. 9). In the Golden Grove camp hangingall felsics at Scuddles (Fig. 14) contain both petrochemicallyrospective and unprospective signatures (Whitford and Ashley,992; Fig. 11b). Prospective signatures in the hanging wall of the



cuddles deposit are restricted to quartz-porphyritic ash flow tuffsf Scuddles Formation Member 2 (Fig. 14). However, this membern turn forms the footwall to Zn mineralization at Hougomontigher in the Golden Grove stratigraphy (Gawlinski, 2004; Fig. 14).

m).

5.2. Comparisons to the Abitibi subprovince

In their classic review of volcanic rocks of the VHMS-rich AbitibiSubprovince, Canada, Barrie et al. (1993) identified five distinctgeochemical groups; three of which are associated with VHMSmineralization (Groups I–III). Group I, associated with >50% ofall VHMS deposits by tonnage, comprised ∼10% of the area ofvolcanic terranes and included volcanic sequences at Kamisko-tia, Matagami and Chibougamau. These areas are characterized bybimodal assemblages of tholeitiic basalt-basaltic andesite and highsilica rhyolite with high HFSE and HREE concentrations, FIIIb sig-natures, low LREE (La/YbCN 0.8–3) and pronounced negative Euanomalies on chondrite-normalized REE diagrams (Barrie et al.,


1993). Group II felsic rocks, host to approximately 30% of VHMSdeposits in the Abitibi, are characterized more transitional tholeiiticto calc-alkalic signatures, intermediate HFSE contents and higherREE ratios (La/YbCN 1–4; FIIIa affinity; Barrie et al., 1993). Group




Fig. 9. Tukey (box and whisker) plots for felsic rocks from the Yilgarn Craton, Pilbara Craton (data from Vearncombe and Kerrich, 1999) and VHMS-bearing camps of theAbitibi greenstone belt, Canada, containing >20 Mt of ore (data from MacLean and Hoy, 1991; Mercier-Langevin et al., 2007; Gaboury and Pearson, 2008). Felsic rocks fromthe Yilgarn Craton are sorted into the following groups: (1) areas with no base metal mineralization (e.g. Norseman, Kambalda, Ulrich Range), (2) areas with minor Cu–Znmineralization (e.g. Dalgaranga, Windimurra, Narndee, Chesterfield, Jungle Pool), (3) areas with significant VHMS resources (e.g. Teutonic Bore, Jaguar, Quinns, Golden Grove,H d thatI

Icsc1

ItF2smQadaEtpNs

fFsclMTtuCt2

ollandaire), and (4) areas where no base metal mineralization has been identifienterquartile range.

II rocks are limited to one deposit (Selbaie mine) and are petro-hemically less prospective (i.e. FII affinity). VHMS barren volcanicequences of Groups IV and V are characterized by low HFSEontents (i.e. FI affinity) and high REE ratios (La/YbCN 8–20 and2–62 respectively) (Barrie et al., 1993).

In the Youanmi Terrane, felsic rocks similar to VHMS-rich Group rhyolites of the Abitibi greenstone belt (e.g. FIIIb affinity Kamisko-ia felsics) are restricted to those which belong to the Yalogindaormation/Kantie Murdana Volcanics Member and formed at c.815 Ma. These units are underlain by large mafic–ultramaficequences and intrusive complexes related to 2.82 Ga plumeagmatism (discussed later). Rocks sampled of this age fromuinns (Austin), Copper Hills, Youanmi and Windimurra are char-cterized by high HREE and HFSE concentrations (Fig. 10), andisplay flat chondrite-normalized REE profiles (Fig. 11d). VHMS-ssociated felsic rocks analyzed from Golden Grove, Weld Range,mily Well, Jillewarra, Dalgaranga, Hollandaire and Gum Creek ofhe Youanmi Terrane display similar chondrite-normalized REErofiles to the Group II suite of the Abitibi greenstone belt (i.e.oranda, Misema: Fig. 11a–e), although the latter typically displays

lightly lower LREE enrichment.Immobile-element ratios highlight subtle differences between

elsic rocks of the Yilgarn Craton and Abitibi greenstone belt inigs. 9 and 13. Felsic rocks from both areas are characterized byimilar Zr/Y and La/YbCN ratios, although these range to signifi-antly higher values in the Yilgarn – particularly from areas whichack mineralization or only contain minor Cu–Zn mineralization.

ost felsic samples in the Yilgarn also display significantly higherh/Yb values than felsic rocks from the Abitibi greenstone belt. Onlyhe Au-rich LaRonde and Bousquet felsic rocks show similar val-



es to barren and weakly mineralized felsic rocks from the Yilgarnraton. This is consistent with the extended crustal recycling inhe Youanmi Terrane (Champion and Cassidy, 2007; Ivanic et al.,013; Wyche et al., 2013), and its more evolved nature compared

may VHMS prospective based on their geochemistry (e.g. Melita, Bore Well). IQR,

to Abitibi crust (Huston et al., 2005, 2014). The only areas in the Yil-garn Craton which have comparable Th/Yb ratios to the Cu–Zn richareas of Abitibi (e.g. Noranda, Matagami) are those with significantVHMS resources (Figs. 9 and 13b,d). This adds further weight tosuggestions of Huston et al. (2014) that the Yilgarn may be impov-erished in VHMS mineralization as only in the Cue Zone and aroundTeutonic Bore was the crust sufficiently juvenile.

As documented previously (e.g. Huston et al., 2005, 2014),known VHMS occurrences are relatively scarce in the Eastern Gold-fields Superterrane. The recognition of bimodal volcanism in theGindalbie Domain and tholeiitic felsic rocks was suggested to reflectthe increased prospectivity of this region. According to Brownet al. (2002), the Gindalbie Domain (Fig. 1) includes both VHMS-prospective, HFSE-enriched bimodal (basalt-rhyolite) complexes(e.g. at Melita and Teutonic Bore), and largely unprospective, calc-alkaline intermediate-silicic volcanic rocks (e.g. at Spring Well andJeedamya). Felsic volcanic complexes at Melita and Teutonic Borewere described as having elevated concentrations of SiO2, HFSEand Y (i.e. A-type, FIII characteristics), low Zr/Y and Th/Yb, andflat to slightly LREE-enriched REE profiles (with pronounced neg-ative Eu anomalies) (Witt et al., 1996; Brown et al., 2002; Barleyet al., 2008). Recent work by Belford (2010) has demonstrated theTeutonic Bore volcanic complex is not strictly bimodal due to thepresence of abundant andesites in the hanging wall and footwallof mineralization at Jaguar. Significant volumes of andesite alsooccur at Mount Gibson (Yeats and Groves, 1998) and Hollandaire(Hayman et al., submitted for publication) and The Cup (CSIROunpublished). The data presented here also suggest that both petro-chemically favourable felsic rocks and unprospective rocks occurat Spring Well and Melita (e.g. Figs. 10, 12b–c and 13), although


the former is characterized by slightly lower HREE concentrationsthan rocks from Jaguar. Some samples from Melita show similargeochemical signatures to Group I Abitibi felsics, although are char-acterized by slightly higher LREE enrichment (Fig. 10). Although




F ne ana .

moccpumeow

6

6

MUesi

ig. 10. Prospectivity of felsic rocks from the Abitibi greenstone belt, Youanmi Terrare the same scale with Zr/Y values indicated on the y-axis. Data sources as in Fig. 9

ajor exploration efforts were made around Melita in the 1970s,nly small sub-economic concentrations of sulphides were dis-overed (mostly pyrite, minor pyrrhotite, sphalerite, galena andhalcopyrite at Jungle Pool to the southeast) (Witt, 1994). Sam-les from south of the Jungle Pool base metal occurrence appearnprospective (e.g. low HFSE; FII affinity; not shown), thoughay not represent the same stratigraphic horizon. Limited trace-

lement data is available for these rocks. Detailed GSWA-led studiesn the Nimbus and Erayinia VHMS deposits of the EGS are under-ay.

. Tectonic-stratigraphic framework

.1. Youanmi Terrane

Using the stratigraphy of Van Kranendonk et al. (2013) for theurchison Domain (Fig. 2), and an extensive database of published



–Pb zircon ages from the Yilgarn Craton, we have recognized sev-ral episodes of VHMS mineralization in the Youanmi Terrane. Theynvolcanic nature of VHMS deposits means the timing of mineral-zation will be within error of dated footwall assemblages providing

d Eastern Goldfields Superterrane according to Lesher et al. (1986). All stacked plots

there has been no extended depositional hiatus lasting more thana few million years. Four distinct periods of VHMS mineralizationhave been recognized in the Youanmi Terrane at >2.9 Ga, 2815 Ma,2760–2745 Ma and 2722 Ma (Fig. 2). VHMS-exploration should befocused on tholeiitic and HFSE-enriched felsic rocks, closely associ-ated with mafic volcanic rocks and argillaceous sedimentary rocks(particularly graphitic shales).

Two areas that produced much of Western Australia’s Cu andZn ore (Golden Grove and Ravensthorpe) formed prior to 2.9 Ga. Inthe c. 2.96–2.93 Ga Golden Grove camp significant Cu–Zn resourcesoccur at Gossan Hill, Scuddles, at various depths between the twodeposits (e.g. Amity, Ethel), and at Gossan Valley-Felix (Table 1). The3.0–2.95 Ga Ravensthorpe Greenstone belt accounted for much ofWestern Australia’s historic Cu production (Marston, 1979). Cu–Auand Cu–Zn mineralization is primarily hosted in the AnnabelleVolcanics (2989 ± 11 Ma) within 2 km from the contact of thesynvolcanic Manyutup Tonalite (2965 ± 12 Ma and 2989 ± 7 Ma)


(Witt, 1999). Additional VHMS-style base metal mineralizationwhich formed prior to 2.9 Ga has been recognized at Weld Range(2969 ± 3 Ma: Wingate et al., 2008a; 2979 ± 3 Ma:Wingate et al.,2012c; also see Guilliamse, 2013), in the Tallering Greenstone belt




Fig. 11. Selected chondrite-normalized REE profiles for intermediate and felsic rocks of the Youanmi Terrane. Shading reflects least altered/mineralized felsic rocks fromt d heavg veral sA

(s(Gss

msTtsmbdtrtiFam(t2t

he Golden Grove Formation. Intermediate and felsic rocks are indicated by faint anreenstone belt (bold line in (a)) is from Barrie et al. (1993). The geochemistry of seMIRA).

2935 Ma ± 2 Ma: Pidgeon and Wilde, 1990), Twin Peaks Green-tone belt (c. 3014? Ma: Pidgeon and Wilde, 1990) and at Mt. Gibsonc. 2.93 Ga: Yeats et al., 1996). New GSWA field mapping aroundolden Grove and U–Pb geochronology aims to refine the >2.9 Gatratigraphy of the Yalgoo-Singleton greenstone belt and Murchi-on Domain as a whole.

Detailed stratigraphic work around Golden Grove has docu-ented the role of at least local extension and the presence of

ynvolcanic faults (Clifford, 1992; Sharpe and Gemmell, 2000).he VHMS-bearing Golden Grove Formation is characterized byhe products of distal explosive felsic volcanism, re-deposited byuccessive mass flow processes (Sharpe and Gemmell, 2000). Sixembers have been identified (Fig. 14) and the absence of mem-

ers GG2 and GG3 at Gossan Hill has been suggested to reflect a localepositional hiatus caused by uplift along syn-depositional struc-ures (Sharpe and Gemmell, 2000). The upper parts of the formationeflect a waning of sediment influx, with unit GG6 (which hostshe bulk of mineralization) representing ambient background sed-mentation (Sharpe and Gemmell, 2002). The overlying Scuddlesormation consists of quartz-feldspar phyric rhyodacite overlainnd intruded by feldspar-quartz phyric dacite. Dacite also intrudesembers GG4–GG6 of the underlying Golden Grove Formation



Fig. 14) and is interpreted to be an intrusive/extrusive dacite domehat overlies its discordant volcanic feeder (Sharpe and Gemmell,000). The contact between unit GG6 and the Scuddles Forma-ion therefore records the onset of proximal felsic volcanism in

y lines respectively. The average group II composition for felsic rocks of the Abitibiynvolcanic intrusive rocks are also shown (data from Ivanic et al., 2012, WACHEM,

the area and further geodynamic change in the basins evolution.The position of original synvolcanogenic structures at Gossan Hillare highlighted by the: (i) asymmetry of massive sulfides, massivemagnetite and stringer zones relative to the volcanic feeder for theScuddles Formation dacite; (ii) a decreasing thickness of massivesulfide, magnetite and stockwork southwards from discordant con-tact of the hanging wall dacite; and (iii) the widest variation in �34Soccur at the southern end of the Gossan Hill orebody (Sharpe andGemmell, 2000).

Following an extended depositional hiatus and a major plumeevent at c. 2.82 Ga (Ivanic et al., 2010), a second period of VHMSmineralization occurred in the Youanmi Terrane between c. 2818and 2813 Ma. In the c. 2825–2805 Norie Group, VHMS miner-alization occurs at Quinns (2817 ± 3 Ma: Wingate et al., 2011a),Just Desserts (c. 2813 Ma, discussed in Hassan, 2014) and Chun-derloo associated with petrochemically prospective felsic rocksof the Yaloginda Formation. The Yaloginda Formation is char-acterized by tholeiitic to transitional felsic rocks with flat REEprofiles and HFSE enrichment (Van Kranendonk et al., 2013;Figs. 10 and 11d). Geochemically similar felsic rocks also host sig-nificant VHMS mineralization overlying the large 2815–2800 Maigneous complexes of the central Youanmi Terrane (Boodanoo and


Meeline suites: Figs. 2 and 4) in the Kantie Murdana VolcanicsMember (Fig. 11d). Base metal occurrences have been identifiedin supracrustal sequences associated with all of these igneouscomplexes (Fig. 4): Narndee, Youanmi, Windimurra, Barrambie




Fig. 12. Selected chondrite-normalized REE profiles for felsic and intermediate volcanic rocks of the Eastern Goldfields Superterrane (a–g), HFSE-enriched granitic intrusionsnear Teutonic Bore (h), and VHMS-associated felsic rocks from the Pilbara Craton (i). Intermediate and felsic rocks are indicated by faint and heavy lines respectively. Shadingreflects petrochemically prospective felsic rocks from Jaguar (Belford et al., submitted for publication) and Teutonic Bore (CSIRO unpublished) as in (a). *Localities withTTG-like REE profiles shown in (g) include: Aphrodite, Bronzewing, Callipole, Coolgardie, E of Norseman, Ida Hill, Jundee, Kalgoorlie, Kanowna Belle, Lake Giles, Lake Violet,L l Belt,

ao2ettatitTMtetmfiPFsvfa

otus, Mt Ida, Mt. Monger, Murphy Hills, NW of Menzies, Spargoville, St Ives, Yanda

nd Lady Alma (Figs. 1 and 4). U–Pb zircon geochronologyn supracrustal sequences at Windimurra (2813 ± 3 Ma: Nelson,001b) and Youanmi (2814 ± 14 Ma: Nelson, 2002) are withinrror of the VHMS-bearing felsic rocks of the Yaloginda Forma-ion. Dating of an andesite from a greenstone belt adjacent tohe Narndee Igneous Complex, has yielded a similar but olderge (2818 ± 3 Ma: Wingate et al., 2012b), most likely represen-ative of the Norie Group host rocks into which the complexntruded at c. 2800 Ma. The Windimurra Igneous Complex has arue thickness of at least 6 km and covers an area of 2500 km2.his voluminous layered intrusion, along with other anhydrouseeline Suite intrusions such as Youanmi Igneous Complex is

hought to represent a major, high-temperature mantle meltingvent at c. 2815 Ma (Ivanic et al., 2010). Pyroxene geobarome-ry suggest the Windimurra Igneous Complex was emplaced at

id-crustal depth (≤400 MPa: Ahmat, 1986). Pressure estimatesrom the younger and smaller Narndee Igneous Complex indicatet was emplaced at 3–10 km depth (100–300 MPa: Scowen, 1991).etrochemical signatures (FII–FIII characteristics) of the Yalogindaormation felsic rocks which host VHMS mineralization are con-



istent with shallow-melting of tholeiitic mafic substrate withariable degrees of crustal contamination. Coeval HFSE-enrichedelsic intrusions around Narndee, Windimurra and Youanmi (Fig. 4)re represented by the Mt. Kenneth Suite (Figs. 2 and 4) and

Wallaby.

display similar geochemical characteristics to the Yaloginda For-mation and Kantie Murdana Volcanics Member (Ivanic et al., 2012)(see Fig. 11d).

It has been suggested by Ivanic et al. (2010) the largeultramafic–mafic intrusions of the Meeline and Boodanoo suiteswere emplaced across the northern Youanmi Terrane into a rift-zone marked by younger NdDM model ages (the ‘Cue Zone’ ofHuston et al., 2014; Fig. 3). Mole et al. (2014) recently presentedNd isotope evidence that pre-existing 3.7–3.5 Ga crust was initiallyrifted in the Cue Zone at c. 3.0 Ga, thinning the crust and extract-ing new material from the mantle. The authors linked this eventto the extraction of the Lake Johnston block (i.e. southern part ofthe Southern Cross Domain) and Burtville Terrane crust from themantle. A plume-event at this time is evident from 3.0 Ga SouthernCross Domain komatiites (references in Mole et al., 2014). Duringthe subsequent 2.82 Ga plume event, the Cue Zone was reactivatedand preexisting structural weaknesses provided sites for magma-tism to rise to relatively shallow crustal levels (Ivanic et al., 2010).The shallow emplacement of these large intrusions likely facilitatedhydrothermal circulation in the upper crust.


In the 2800–2735 Ma Polelle Group of the Murchison Domain,VHMS mineralization has been recognized in the GreensleevesFormation at Hollandaire (2.8 Mt at 1.6% Cu, 5 g/t Ag and 0.4 g/tAu), Mt. Mulcahy, Emily Well and in the Dalgaranga greenstone




F fields

o 2007;G

bfiAcpm(l2Hwb(fiCrai2a(Dt(

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ig. 13. Geochemistry of felsic rocks from the Youanmi Terrane and Eastern Goldutlines in (b) and (d) (data from MacLean and Hoy, 1991; Mercier-Langevin et al.,

rove.

elt. Minor base metal mineralization also occurs at Chester-eld, Abbotts, Cullculli and around Meekatharra (Figs. 1 and 4).reas of the Greensleeves Formation which contain petrochemi-ally prospective felsic rocks host Cu–Zn mineralization, whereasetrochemically unprospective areas are barren and record nor-al ‘subduction affinity’ magmatism characterized by steep

TTG-like) REE profiles and pronounced negative Nb anoma-ies (e.g. Wyman and Kerrich, 2012; Van Kranendonk et al.,013). U–Pb zircon geochronology from NW of Hollandaire (Eelyaill) has yielded an age of 2746 ± 4 Ma (Wingate et al., 2012a),ithin error of ages obtained from the Dalgaranga greenstone

elt (c. 2745 Ma: Pidgeon and Hallberg, 2000), Mt. Mulcahynearby intrusion – 2748 ± 5 Ma:Wingate et al., 2010a), Chester-eld (2747 ± 5 Ma:Wingate et al., 2012d), and Abbotts (north of theonroy occurrence – 2739 ± 10 Ma:Wingate et al., 2008b). Moreecently, an age of c. 2759 Ma has been obtained from drill coret Hollandaire (Hayman et al., submitted for publication), almostdentical to an age from volcanic succession near Emily Well (c.761: Pidgeon and Hallberg, 2000). Both TTG-like (Cullculli suite)nd HFSE-enriched (Eelya suite) felsic intrusions occur at this timeFig. 2). The Eelya Suite is most extensive around Hollandaire andalgaranga (Fig. 4) and displays similar geochemical characteris-

ics to VHMS-associated felsic rocks of the Greensleeves FormationIvanic et al., 2012) (see Fig. 11e).

Finally, VHMS mineralization in the 2735–2700 Ma Glen Group



ccurs in the Gum Creek greenstone belt (e.g. The Cup, Bevan,lind Bat, Eds Bore) associated with felsic volcanic rocks andraphitic/carbonaceous sedimentary rocks. Felsic volcanic rocksear the Bevan base metal occurrence have yielded an age of

Superterrane. VHMS-bearing areas of the Abitibi greenstone belt are indicated by Gaboury and Pearson, 2008). All green symbols not labelled in (a) are from Golden

2722 ± 6 Ma (Bodorkos et al., 2006). The emplacement of thickdifferentiated mafic–ultramafic sills of the Yalgowra Suite into shal-low levels of the crust at this time may have driven hydrothermalcirculation (Figs. 2 and 13). The cumulative thickness of the Yalgo-wra Suite is ∼1 km (Wyche et al., 2013); its age is constrained byU–Pb dates of 2735 ± 5 Ma, 2719 ± 6 Ma, and 2711 ± 2 Ma (Ivanicet al., 2010). The Montague granodiorite (2722 ± 7 Ma: Wang et al.,1998) is both spatially and temporally associated with VHMS min-eralization in the Gum Creek greenstone belt. Its geochemicalaffinity is similar to nearby felsic rocks (Fig. 11f) which includesboth unprospective (FI affinity) and prospective (FIII affinity) units(Figs. 10 and 11f).

6.2. Kalgoorlie and Kurnalpi terranes

Although there are a number of synvolcanic base metal occur-rences in the Eastern Goldfields Superterrane (e.g. Teutonic Borecamp, Jungle Pool, Nimbus, Anaconda, Erayinia), the timing of min-eralization at several of these localities is not well constrained. Inthe northern Gindalbie Domain significant VHMS mineralizationoccurred at c. 2690 Ma in the Teutonic Bore camp (2688 ± 4 Ma:Pidgeon and Wilde, 1990; 2692 ± 4 Ma: Nelson, 1995) and is associ-ated with felsic volcanic complexes and deep-marine, argillaceoussedimentary rocks (Belford, 2010; Belford et al., Submitted). Maficrocks with BABB-like geochemical characteristics stratigraphically


overly and intrude VHMS mineralization at Jaguar (e.g. Belford,2010), and host VHMS mineralization at Teutonic Bore. U–Pb zircongeochronology from the Jeedamya Complex and Melita Complex(Fig. 5) have produced similar, albeit slightly younger, ages of




Fig. 14. Stratigraphy of the Golden Grove area of the central Yalgoo-Singleton greenstone belt (after Sharpe and Gemmell, 2002). Massive sulfides and stringer mineralizationare shown in red, with the position of VHMS resources after Gawlinski (2004). A, Andesite; B, basalt; D, dacite; R, rhyolite; RD, Rhyodacite. (For interpretation of the referencest

2aaaW

tcaatiRRiY

i(

o color in figure legend, the reader is referred to the web version of the article.)

681 ± 4 Ma (Nelson, 1997) and 2683 ± 2.4 Ma (Brown et al., 2002)nd may constrain the timing of minor base metal mineralizationt Jungle Pool. A similar age has also been obtained from 4 kmlong strike of the Erayinia/King VHMS occurrence (2680 ± 5 Ma:ingate and Bodorkos, 2007a).Unlike VHMS-associated felsics at Teutonic Bore, at Anaconda

here is a close temporal and spatial association between felsic vol-anic rocks and spinifex-textured komatiitic flows. Together withn age of 2698 ± 5 Ma (Nelson, 2005), this suggests VHMS miner-lization at Anaconda is hosted within an older volcanic sequencehan those of the northern Gindalbie Domain (Fig. 5). Constrain-ng the timing of VHMS mineralization at Nimbus, Brilliant Well,ungine and Balaguindi requires additional U–Pb geochronology.egardless, VHMS mineralization in the Eastern Goldfields Terrane

s clearly younger than the last period of mineralization in the



ouanmi Terrane (c. 2722 Ma).Five clans of HFSE-enriched granitic rocks have been identified

n the Eastern Goldfields Superterrane by Cassidy and Champion2002) and Champion and Cassidy (2002) which have clear spatial

and temporal associations to areas of VHMS mineralization (Fig. 6),as in the Youanmi Terrane (Figs. 2 and 4). HFSE-enriched graniteswere characterized by a distinct geochemistry of high FeO, MgO,TiO2, Y and Zr, with low Rb, Pb, Sr and Al2O3, and the presenceof biotite and/or amphibole in quartz and feldspar rich rocks(Champion and Cassidy, 2002). Clans were defined on similarpetrographic and geochemical characteristics (see Cassidy andChampion, 2002), and may be subdivided into supersuites andsuites. U–Pb zircon age constraints are only available for a limitednumber of supersuites, summarized in Fig. 5. The Kookynie Clanincludes the Penzance Supersuite (exposed near the Jungle Poolbase metal occurrence), Kookynie Supersuite (exposed east ofTeutonic Bore) and the Boo Boo and Gearless intrusions of thenorthern Kalgoorlie Terrane (Fig. 6). U–Pb ages of c. 2680 Ma for theKookynie and Penzance supersuites (Fig. 5) are comparable to ages


obtained from Jeedamya, Melita, Erayinia and the timing of maficintrusive across the EGS (2680 ± 8 Ma; 2687 ± 5 Ma: references inIvanic et al., 2010). Geochemically, these intrusive rocks are similarto felsic rocks associated with VHMS mineralization at Teutonic


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ore (Fig. 12h). The Bullshead Supersuite exposed east of Teutonicore may also be of similar age as it has similar geochemicalharacteristics (Fig. 12h). The Satisfaction Supersuite is restrictedo the eastern side of the northern Kalgoorlie Terrane (Fig. 6) andhows a strong spatial relationship with contemporaneous (andn part co-genetic) felsic volcanic rocks (Champion and Cassidy,002). Between 70 and 130 km SW of Anaconda, the Outcampore Supersuite occurs as a linear belt of foliated granitic rocksnd dykes, internal to the greenstone sequences, ranging inomposition from biotite monzogranite to tonalite (Champion andassidy, 2002). Ages from c. 2719 to 2698 Ma are within error ofhe Minerie and Kurnalpi sequences of the EGS (Fig. 5) and U–Pbircon geochronology from Anaconda (2698 ± 5 Ma: Nelson, 2005).

.3. Burtville and Yamarna terranes

As previously discussed, the Burtville Terrane shares many fea-ures of the Youanmi Terrane (e.g. Pawley et al., 2012). Rocks ofimilar age to the first three periods of VHMS mineralization in theouanmi Terrane occur in the Burtville Terrane at: c. 2.97 Ga (Ulrichange greenstone belt), c. 2805 Ma (Duketon greenstone belt), c.775–2755 Ma (Laverton, Irwin Hills-Stella Range and Mount Vennreenstone belts) (Supplementary Fig. 1; Pawley et al., 2012). Sam-les herein although limited to three areas (Fig. 12f) display steepEE profiles and are generally considered unprospective for VHMSineralization. Although the Burtville Terrane is isotopically more

uvenille than the Youanmi Terrane (even moreso than the Cueone) and would therefore appear VHMS prospective, this simplyeflects its younger mantle extraction age (c. 3.0 Ga: Pawley et al.,012). No areas equivalent to the Cue Zone have been documented

n the Burtville Terrane, except some single point anomalies char-cterized by slightly younger NdDM ages (Fig. 3). These areas reflecthe introduction of juvenile material between 2940 and 2755 Ma,

ost likely at 2810–2750 Ma associated with c. 2.82 Ga plume mag-atism (e.g. Swincer Dolerite) (Mole et al., 2014). As the 2.82 Ga

lume event in the Youanmi Terrane was particularly favourable forHMS mineralization, felsic rocks in these areas may be prospec-

ive. As in the Youanmi Terrane, VHMS prospective felsic rocks maylso occur in close proximity to unprospective units in the >2.9 GaUlrich Range) and c. 2.76 Ga (Laverton, Irwin Hills-Stella Range,

ount Venn) greenstone belts. Additional geochemistry from thesereas is recommended.

Although data is limited for the Yamarna Terrane, Nd isotopenalyses suggest the crust was extracted from the mantle at c.950–2850 Ma (Mole et al., 2014). Felsic rocks included herein are

imited to samples from Mount Gill, which display similar geo-hemical characteristics to VHMS bearing rocks at Teutonic Borend Jaguar (Fig. 12a and f). U–Pb zircon geochronology constrainshe sequence to 2683 ± 5 Ma (Pawley et al., 2012), within errorf dated assemblages at Melita and Erayinia, and slightly youngerhan Teutonic Bore. This area is considered prospective for VHMS

ineralization.

.4. South West Terrane

Base metal mineralization in the South West Terrane isestricted to the older c. 3.0–3.2 Ga sequences, with the Balin-up Metamorphic Belt hosting the Wheatley deposit, the Wonganills Greenstone belt hosting the Mystery and associated baseetal occurrences, and the Jimperding Metamorphic Belt associ-

ted with minor intercepts of base metal mineralization at Ularringock, Southern Brook, Ablett, Chapman and Dasher (MINEDEX).



o base metal occurrences have been identified in the younger715–2675 Ma Saddleback and Moranup greenstone belts (Fig. 1).–Pb zircon geochronology on a ‘psammite’ in the footwall of

he minor Zn–Cu mineralization at Wheatley (GA sample ID

PRESSsearch xxx (2014) xxx–xxx

2004968001A) yielded a maximum depositional age of 2646 Ma,with a spread of ages from ∼2600 to 2700 Ma (Sircombe et al.,2007). The meaning of this age is not clear.

7. Conclusions

Using an extensive database of compiled whole-rock geochem-istry, and recently published U–Pb and stratigraphic constraints,recognized VHMS occurrences from across the Yilgarn Craton havebeen placed in a detailed tectono-stratigraphic framework. VHMSmineralization in the Yilgarn Craton is preferentially associatedwith areas of thinned, juvenile crust as revealed by Nd and Pbregional isotope variations (e.g. Huston et al., 2014). Prospectivehost sequences can be identified through the presence of: largelybimodal volcanic complexes (although andesites do occur), syn-volcanic faults, HFSE- and HREE-enriched synvolcanic intrusions,regional isotope variations indicative of rifting, and specific petro-chemical signatures.

In terms of petrochemical signatures, VHMS-bearing felsic rocksin the Youanmi Terrane and Eastern Goldfields are characterizedby low Zr/Y, La/Yb and Th/Yb ratios, high Sc/TiO2, HFSE and HREEcontents, and flat HREE profiles. Chondrite-normalized REE pro-files for felsic rocks overlying 2.82–2.80 Ga plume-related basaltsand large igneous complexes of the Youanmi Terrane are flat. OtherVHMS-bearing felsic rocks are characterized by slight LREE enrich-ment (La/SmCN < 3) and flat HREE profiles (Dy/YbCN ∼ 1 or less).

In the South West Terrane VHMS mineralization is preferen-tially associated with older c. 3.0–3.2 Ga greenstone sequences.In the Youanmi Terrane four distinct periods of economic min-eralization can be recognized: (i) >2.9 Ga, associated with earlybimodal-mafic greenstone belts (e.g. Golden Grove, Ravensthorpe,Twin Peaks) subjected to extension; (ii) c. 2815 Ma, following amajor plume event and coeval with the emplacement of largeigneous complexes across the northern Youanmi Terrane at shallowlevels in the crust (e.g. Austin, Youanmi, Narndee, Windimurra);(iii) 2760–2745 Ma, in areas of rift-related magmatism during thedeposition of the Greensleeves Formation (e.g. Hollandaire, Dalgar-anga, Mt. Mulcahy); (iv) c. 2725 Ma, in the Gum Creek Greenstonebelt (e.g. The Cup, Bevan) during a second major plume-event,coeval with the emplacement of high-level sills. Subsequently,VHMS-mineralization occurred in the Eastern Goldfields Supert-errane where it was also closely associated with HFSE-enrichedsynvolcanic intrusions. The mineralization is apparently restrictedto areas of juvenile crust and largely bimodal complexes whichformed between c. 2700 and 2680 Ma (e.g. Teutonic Bore, Erayinia,Nimbus).

More data is required in the South West, Burtville and Yamarnaterranes, and a number of greenstone belts of the Youanmi Ter-rane (e.g. Twin Peaks, Tallering) in order to clearly delineateregions of prospectivity and establish temporal, geochemical andstratigraphic associations to mineralization. Localized studies arerequired in order to establish volcanological settings for a numberof deposits and their controlling factors.

Acknowledgements

This work builds on the research of countless individuals, allof whom are gratefully acknowledged. The principal author issupported by the Exploration Incentive Scheme at the Geologi-cal Survey of Western Australia, funded by the Western AustralianGovernment Royalties for Regions Programme. Paul Duuring and


Derek Wyman are thanked for supplying data. Joana Parr, SandraRomano and John Walshe are thanked for their constructive com-ments. AMIRA P-763 data is included with the permission of StuartBrown. David Mole, Nicole Patison, Pat Hayman and Ray Cas are


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hanked for many thoughtful discussions on the geology of the Yil-arn Craton. Stefan Gawlinski is thanked for assistance with Fig. 14.W, TJI, MTDW publish with permission from the Executive Direc-or of the Geological Survey of Western Australia. Two anonymouseviewers and Editor Randall Parrish are thanked for their construc-ive comments which improved this paper.

ppendix.

Yilgarn Craton geochemistry sources included herein: AMIRA763; Brown et al. (2002), Barley et al. (2008), Belford (2010),elford et al. (submitted for publication), Duuring and Hagemann2013), Frost (1992), GSWA (2008, 2010a,b, 2011), Hallbergatabase, Hill et al. (1999), Morris and Witt (1997), Messenger2000), OZCHEM (Champion et al., 2013); Sharpe and Gemmell2001), Van Kranendonk et al. (2013), Vickery (2004), WACHEMGSWA, 2013), Whitford and Ashley (1992), Yeats and Groves1998) and Wyman and Kerrich (2012).

ppendix B. Supplementary data

Supplementary data associated with this article can be found,n the online version, at http://dx.doi.org/10.1016/j.precamres.014.11.002.

eferences

hmat, A.L., 1986. Petrology, Structure, Regional Geology and Age of the GabbroicWindimurra Complex. University of Western Australia, Western Australia.

nand, R.R., Butt, C.R.M., 2010. A guide for mineral exploration through the regolithin the Yilgarn Craton, Western Australia. Aust. J. Earth Sci. 57, 1015–1114.

ngerer, T., Kerrich, R., Hagemann, S.G., 2013. Geochemistry of a komatiitic,boninitic, and tholeiitic basalt association in the Mesoarchean Koolyanobbinggreenstone belt, Southern Cross Domain, Yilgarn Craton: implications for man-tle sources and geodynamic setting of banded iron formation. Precambrian Res.224, 110–128.

shley, P.M., Dudley, R.J., Lesh, R.H., Marr, J.M., Ryall, A.W., 1988. The Scuddles Cu–Znprospect, an Archean volcanogenic massive sulfide deposit, Golden Grove dis-trict, Western Australia. Econ. Geol. 83, 918–951.

arley, M.E., 1992. A review of Archean volcanic-hosted massive sulfide and sulfatemineralization in Western Australia. Econ. Geol. 87, 855–872.

arley, M.E., Kerrich, R., Reudavy, I., Xie, Q., 2000. Late Archaean Ti-rich, Al-depletedkomatiites and komatiitic volcaniclastic rocks from the Murchison Terrane inWestern Australia. Aust. J. Earth Sci. 47, 873–883.

arley, M.E., Brown, S.J.A., Krapez, B., Kositcin, N., 2008. Physical volcanology andgeochemistry of a Late Archaean volcanic arc: Kurnalpi and Gindalbie Ter-ranes, Eastern Goldfields Superterrane, Western Australia. Precambrian Res.161, 53–76.

arnes, S.J., 2006. Nickel Deposits of the Yilgarn Craton: Geology, Geochemistry,and Geophysics Applied to Exploration. Society of Economic Geologists, Specialpublication 13, 210 pages.

arnes, S.J., Fiorentini, M.L., 2012. Komatiite magmas and sulfide nickel deposits: acomparison of variably endowed Archean terranes. Econ. Geol. 107, 755–780.

arnes, S.J., Van Kranendonk, M.J., 2014. Archean andesites in the East Yilgarn Craton,Australia: products of plume/crust interaction? Lithos 6, 80–92.

arnes, S., Van Kranendonk, M.J., Sontag, I., 2012. Geochemistry and tectonic set-ting of basalts from the Eastern Goldfields Superterrane. Aust. J. Earth Sci. 59,707–735.

arrett, T.J., MacLean, W.H., 1994. Chemostratigraphy and hydrothermal alterationin exploration for VHMS deposits in greenstones and younger volcanic rocks.In: Lentz, D.R. (Ed.), Alteration and Alteration Processes associated with Ore-forming Systems. Geological Association of Canada, Short Course Notes, vol. 11,pp. 433–467.

arrie, C.T., Ludden, J.N., Green, T.H., 1993. Geochemistry of volcanic rocks associ-ated with Cu–Zn and Ni–Cu deposits in the Abitibi Subprovince. Econ. Geol. 88,1341–1358.

elford, S.M., 2010. Genetic and Chemical Characterisation of the Host Successionto the Archean Jaguar VHMS Deposit. University of Tasmania, pp. 258.

elford, S.M., Davidson, G.J., McPhie, J., Large, R.R., 2014. An Immature Back-arc Set-ting for the Teutonic Bore Volcanic Complex Statigrapy, Host to the ArcheanJaguar VHMS Deposit (in preparation).

elford, S.M., Davidson, G.J., McPhie, J., Large, R.R., 2014. Architecture of theNeoarchean Jaguar VHMS deposit, Western Australia: implications for prospec-



tivity and presence of depositional breaks. Precambrian Res. (submitted forpublication).

eresford, S., Stone, W.E., Cas, R., Lahaye, Y., Jane, M., 2005. Volcanological controls onthe localization of the komatiite-hosted Ni-Cu-(PGE) coronet deposit, Kambalda,western Australia. Econ. Geol. 100, 1457–1467.


Blewett, R.S., Czarnota, K., Henson, P.A., Champion, D.C., 2010a. Structural-eventframework for the eastern Yilgarn Craton, Western Australia, and its implica-tions for orogenic gold. Precambrian Res. 183, 203–229.

Blewett, R.S., Henson, P.A., Roy, I.G., Champion, D.C., Cassidy, K.F., 2010b. Scale-integrated architecture of a world-class gold mineral system: the Archaeaneastern Yilgarn Craton, Western Australia. Precambrian Res. 183, 230–250.

Bodorkos, S., Love, G.J., Nelson, D.R., Wingate, M.T.D., 2006. 179239: porphyriticmetadacite, Montague Well; Geochronology dataset 647. In: Compilation ofGeochronology Data, June 2006 Update. Western Australia Geological Survey.

Brown, S.J.A., Barley, M.E., Krapez, B., Cas, R.A.F., 2002. The Late Archaean Melitacomplex, Eastern Goldfields, western Australia: shallow submarine bimodalvolcanism in a rifted arc environment. J. Volcanol. Geotherm. Res. 115, 303–327.

Butt, C.R.M., 2004. Geochemical exploration for base metals in deeply weatheredterrane. In: McConachy, T.F., McInnes, B.I.A. (Eds.), Recent Exploration Successat Golden Grove. CSIRO, Western Australia, pp. 81–101.

Cassidy, K.F., Champion, D.C., 2002. Granitoids of the Southeastern Yilgarn Craton:Distribution, Geochronology, Geochemistry, Petrogenesis and Relationship toMineralisation, AMIRA P482/MERIWA M281-Yilgarn Granitoids., pp. 3.1–3.52.

Cassidy, K.F., Champion, D.C., Krapez, B., Barley, M.E., Brown, S.J.A., Blewett, R.S.,Groenewald, P.B., Tyler, I.M., 2006. A Revised Geological Framework for theYilgarn Craton, Western Australia.

Champion, D.C., Cassidy, K.F., 2002. Granites of the Northern Eastern Goldfields:their Distribution, Age, Geochemistry, Petrogenesis, Relationship with Miner-alisation, and Implications for Tectonic Environment, AMIRA P482/MERIWAM281-Yilgarn Granitoids., pp. 2.1–2.49.

Champion, D.C., Cassidy, K.F., 2007. An overview of the Yilgarn Craton and its crustalevolution. In: Proceedings of Geoconferences (WA) Inc. Kalgoorlie 07 Confer-ence, Geoscience Australia Record 2007/14, pp. 8–12.

Champion, D.C., Sheraton, J.W., 1997. Geochemistry and Nd isotope systematics ofArchaean granites of the Eastern Goldfields, Yilgarn Craton, Australia: implica-tions for crustal growth processes. Precambrian Res. 83, 109–132.

Champion, D.C., Budd, A.R., Wyborn, L.A.I., 2013. OZCHEM National Whole RockGeochemistry Database, http://www.ga.gov.au/meta/ANZCW0703011055.html

Chen, S.F., Riganti, A., Wyche, S., Greenfield, J.E., Nelson, D.R., 2003. Lithostratigra-phy and tectonic evolution of contrasting greenstone successions in the centralYilgarn Craton, Western Australia. Precambrian Res. 127, 249–266.

Clifford, B.A., 1992. Facies and Palaeoenvironment Analysis of the Archean Volcanic-Sedimentary Succession Hosting the Golden Grove Cu–Zn Massive SulfideDeposits. Monash University, Western Australia, pp. 343.

Czarnota, K., Champion, D.C., Goscombe, B., Blewett, R.S., Cassidy, K.F., Henson, P.A.,Groenewald, P.B., 2010. Geodynamics of the eastern Yilgarn Craton. PrecambrianRes. 183, 175–202.

Dusel-Bacon, C., Foley, N.K., Slack, J.F., Koenig, A.E., Oscarson, R.L., 2012. Peralkaline-and calc-alkaline-hosted volcanogenic massive sulfide deposits of the Donnifielddistrict, East-Central Alaska. Econ. Geol. 107, 1403–1432.

Duuring, P., Hagemann, S., 2013. Genesis of superimposed hypogene and supergeneFe orebodies in BIF at the Mafoonga deposit, Yilgarn Craton, Western Australia.Miner. Depos. 48, 371–395.

Ellis, P., 2004. Geology and mineralisation of the Jaguar copper–zinc deposit, West-ern Australia. In: McConachy, T.F., McInnes, B.I.A. (Eds.), Copper–zinc massivesulphide deposits in Western Australia. CSIRO, pp. 39–46.

Empire Resources, 2012. Annual Report for the year ended 30 June 2012, Availableat http://www.resourcesempire.com.au/annual report.htm

Ferguson, K.M., 1999. Lead, zinc and silver deposits of Western Australia. West. Aust.Geol. Surv. Miner. Resour. Bull. 15, 314.

Fletcher, I.R., McNaughton, N.J., 2002. Granitoid Geochronology: SHRIMP Zir-con and Titanite Data, AMIRA P482/MERIWA M281-Yilgarn Granitoids.,pp. 6.1–6.155.

Franklin, J.M., Gibson, H.L., Galley, A.G., Jonasson, I.R., 2005. Volcanogenic massivesulfide deposits. In: Hedenquist, J.W., Thompson, J.F.H., Goldfarb, R.J., Richards,J.P. (Eds.), Econ. Geol. 100th Anniversary Volume. Society of Economic Geolo-gists, Littleton, CO.

Frost, K.M., 1992. The Role of Ground Melting in the Genesis of Komatiite HostedNickel Sulphide Deposits at Kambalda and Widgiemooltha, Western Australia.University of Western Australia, Nedlands, Australia, pp. 185.

Gaboury, D., Pearson, V., 2008. Rhyolite geochemical signatures and association withvolcanogenic massive sulfide deposits: examples from the Abitibi Belt, Canada.Econ. Geol. 103, 1531–1562.

Galley, A.G., 1993. Semi-conformable alteration zones in volcanogenic massive sul-phide districts. J. Geochem. Explor. 48, 175–200.

Galley, A.G., 2003. Composite synvolcanic intrusions associated with PrecambrianVMS-related hydrothermal systems. Miner. Depos. 38, 443–473.

Galley, A.G., Hannington, M.D., Jonasson, I.R., 2007. Volcanogenic massive sulphidedeposits. In: Goodfellow, W.D. (Ed.), Mineral Deposits of Canada: A Synthe-sis of Major Deposit-types, District Metallogeny, the Evolution of GeologicalProvinces, and Exploration Methods. Geological Association of Canada, MineralDeposits Division, pp. 141–161.

Gawlinski, S., 2004. Recent exploration success at Golden Grove, Western Australia.In: McConachy, T.F., McInnes, B.I.A. (Eds.), Copper–zinc Massive SulphideDeposits in Western Australia. CSIRO, pp. 33–37.

Gee, R.D., Baxter, J.L., Wilde, S.A., Williams, I.R., 1981. Crustal Development in the


Archaen Yilgarn Block, Western Australia, vol. 7. Geological Society of Australia,pp. 43–56 (special publication).

Grunsky, E.C., 2013. Predicting Archaean Volcanogenic Massive Sulphide DepositPotential from Lithogeochemistry: Application to the Abitibi Greenstone Belt.Geochemistry: Exploration, Environment, Analysis Online First.


http://dx.doi.org/10.1016/j.precamres.2014.11.002

http://dx.doi.org/10.1016/j.precamres.2014.11.002

http://refhub.elsevier.com/S0301-9268(14)00377-5/sbref0005










































































































































































































































































































































































































































































































































































































http://www.ga.gov.au/meta/ANZCW0703011055.html









































































































































http://www.resourcesempire.com.au/annual_report.htm


























































































































































































































































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L

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M

M

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2 S.P. Hollis et al. / Precambr

SWA, 2008. Central Yilgarn, 2008 Update: Western Australia Geological Survey,1:100,000 Geological Information Series.

SWA, 2010a. East Yilgarn, 2010 Update: Geological Survey of Western Australia,1:100,000 Geological Information Series.

eological Survey of Western Australia, Record 2010/18, 119–122.SWA, 2011. Murchison, 2011 Update: Geological Survey of Western Australia,

1:100,000 Geological Information Series.SWA, 2013. WACHEM, http://geochem.dmp.wa.gov.au/geochem/uilliamse, J.N., 2013. Investigation into the Potential for Volcanic-Associated

Massive Sulphide Mineralisation at Weld Range using Golden Grove as a Com-parative Model. The University of Western Australia, pp. 109.

allberg, J.A., Thompson, J.F.H., 1985. Geologic setting of the teutonic bore, mas-sive sulfide deposit, Archean Yilgarn Block, Western Australia. Econ. Geol. 80,1953–1964.

art, T.R., Gibson, H.L., Lesher, C.M., 2004. Trace element geochemistry and petro-genesis of felsic volcanic rocks associated with volcanogenic massive Cu–Zn–Pbsulfide deposits. Econ. Geol. 99, 1003–1013.

assan, L.Y., 2014. The Yuinmery volcanogenic massive sulfide prospects: mineral-ization, metasomatism and geology. In: Geological Survey of Western Australia,Report 131, 65p.

astie, A.R., Kerr, A.C., Pearce, J.A., Mitchell, S.F., 2007. Classification of altered vol-canic island arc rocks using immobile trace elements: development of the Th-Codiscrimination diagram. J. Petrol. 48, 2341–2357.

ayman, P.C., Hull, S.E., Cas, R.A.F., Summerhayes, E., Amelin, Y., Ivanic, T., Price, D.,2014. A new period of volcanogenic massive sulphide formation in the Yilgarn:a volcanological study of the ∼2.76 Ma Hollandaire Au-rich VMS deposit, YilgarnCraton, Western Australia. Aust. J. Earth Sci. (submitted for publication).

ill, R.E.T., Barnes, S.J., Thordarson, T., Dowling, S.E., Mattox, T.N., 1999. The geol-ogy of the Black Swan Succession and associated nickel sulfide orebodies. In:Exploration and Mining Report 646R. CSIRO, Perth, 325 pp.

uston, D.L., Champion, D.C., Cassidy, K.F., 2005. Tectonic controls on the endow-ment of Archean cratons in VHMS deposits: evidence from Pb and Nd isotopes.In: Mao, J., Bierlein, F.P. (Eds.), Mineral Deposit Research: Meeting the GlobalChallenge. , pp. 15–18.

uston, D.L., Champion, D.C., Cassidy, K.F., 2014. Tectonic controls on the endow-ment of Neoarchean cratons in volcanic-hosted massive sulfide deposits:evidence from lead and neodynium isotopes. Econ. Geol. 109, 11–26.

rvine, T.N., Baragar, W.R.A., 1971. A guide to the chemical classification of the com-mon volcanic rocks. Can. J. Earth Sci. 8, 523–548.

vanic, T.J., Wingate, M.T.D., Kirkland, C.L., Van Kranendonk, M.J., Wyche, S., 2010.Age and significance of voluminous mafic–ultramafic magmatic events in theMurchison Domain, Yilgarn Craton. Aust. J. Earth Sci. 57, 597–614.

vanic, T.J., Van Kranendonk, M.J., Kirkland, C.L., Wyche, S., Wingate, M.T.D.,Belousova, E.A., 2012. Zircon Lu–Hf isotopes and granite geochemistry of theMurchison domain of the Yilgarn Craton: evidence for reworking of Eoarcheancrust during the Meso-Neoarchean. Lithos 148, 112–127.

vanic, T.J., Van Kranendonk, M.J., Kirkland, C.L., Wyche, S., Wingate, M.T.D.,Belousova, E.A., 2013. Juvenile Crust Formation and Recycling in the North-ern Murchison Domain, Yilgarn Craton: Evidence from Hf Isotopes and GraniteGeochemistry. Geological Survey of Western Australia, Report 120, pp. 34.

abriu Metals, 2006. Annual Report 2006.abriu Metals, 2010. ASX announcement. 23 November 2010. Bentley Resource

Upgrade.rapez, B., Hand, J.L., 2008. Late Archaean deep-marine volcaniclastic sedimenta-

tion in an arc-related basin: the Kalgoorlie sequence of the Eastern GoldfieldsSuperterrane, Yilgarn Craton, Western Australia. Precambrian Res. 161, 89–113.

arge, R.R., 1992. Australian volcanic-hosted massive sulfide deposits: features,styles, and genetic models. Econ. Geol. 87, 471–510.

eat, P.T., Jackson, S.E., Thorpe, R.S., Stillman, C.J., 1986. Geochemistry of bimodalbasalt-subalkaline/peralkaline rhyolite provinces within the southern BritishCaledonides. J. Geol. Soc. Lond. 143, 259–327.

entz, D.R., 1998. Petrogenetic evolution of felsic volcanic sequences associated withPhanerozoic volcanic-hosted massive sulfide systems: the role of extensionalgeodynamics. Ore Geol. Rev. 12, 289–327.

esher, C.M., Goodwin, A.M., Campbell, I.H., Gorton, M.P., 1986. Trace-element geo-chemistry of ore-associated and barren, felsic metavolcanic rocks in the Superiorprovince, Canada. Can. J. Earth Sci. 23, 222–237.

iu, S.F., Champion, D.C., Cassidy, K.F., 2002. Geology of the Sir Samuel 1:250,000Sheet Area, Western Australia. Geoscience Australia Record 2002/14.

acLean, W.H., 1990. Mass change calculations in altered rock series. Miner. Depos.23, 231–238.

acLean, W.H., Barrett, T., 1993. Lithogeochemical techniques using immobile ele-ments. J. Geochem. Explor. 48, 109–133.

acLean, W.H., Hoy, L.D., 1991. Geochemistry of hydrothermally altered rocks atthe Horne mine, Noranda, Quebec. Econ. Geol. 86, 506–528.

acPhersons, 2014. ASX announcement, 6th August 2014. Available athttp://www.mrpresources.com.au/announcements.php

etals Australia Ltd., 2012. http://www.metalsaustralia.com.au/manindi-zinc.phparston, R.J., 1979. Copper mineralization in Western Australia. Geol. Surv. West.

Aust. Miner. Resour. Bull. 13, 208.cConachy, T.F., McInnes, B.I.A., Carr, G.R., 2004. Is Western Australia intrinsically



impoverished in volcanogenic massive sulphide deposits, or under explored? In:McConachy, T.F., McInnes, B.I.A. (Eds.), Copper–zinc Massive Sulphide Depositsin Western Australia. CSIRO, pp. 15–32.

cConnell, B.J., Stillman, C.J., Hertogen, J., 1991. An Ordovician basalt to peralkalinerhyolite fractionation series from Avoca, Ireland. J. Geol. Soc. Lond. 148, 711–718.

PRESSsearch xxx (2014) xxx–xxx

McDonough, W.F., Sun, S.-S., 1995. The composition of the Earth. Chem. Geol. 120,223–254.

Mercier-Langevin, P., Dubé, B., Hannington, M.D., Richer-Laflèche, M., Gosselin, G.,2007. The LaRonde Penna Au-rich volcanogenic massive sulfide deposit, AbitibiGreenstone Belt, Quebec: Part II. Lithogeochemistry and paleotectonic setting.Econ. Geol. 102, 611–631.

Mercier-Langevin, P., Hannington, M.D., Dubé, B., Bécu, V., 2011. The gold content ofvolcanogenic massive sulfide deposits. Miner. Depos. 46, 509–539.

Messenger, P.R., 2000. Geochemistry of the Yandal belt metavolcanic rocks, EasternGoldfields Province, Western Australia. Aust. J. Earth Sci. 47, 1015–1028.

MMG, 2011. Annual Report 2011, Available at http://www.mmg.com/en/Investors-and-Media/Reports-and-Presentations/Annual-Reports.aspx

Mole, D.R., Fiorentini, M.L., Thébaud, N., McCuaig, T.C., Cassidy, K.C., Kirkland, C.L.,Wingate, M.T.D., Romano, S.S., Doublier, M.P., Belousova, E.A., 2012. Spatio-temporal constraints on lithospheric development in the southwest-centralYilgarn Craton, Western Australia. Aust. J. Earth Sci. 59, 625–656.

Mole, D.R., Fiorentini, M.L., Cassidy, K.F., Kirkland, C.L., Thebaud, N., McCuaig, T.C.,Doublier, M.P., Duuring, P., Romano, S.S., Maas, R., Belousova, E.A., Barnes, S.J.,Miller, J., 2014. Crustal evolution, intra-cratonic architecture and the metal-logeny of an Archaean craton. In: Jenkin, G.R.T., Lusty, P.A.J., Mcdonald, I., Smith,M.P., Boyce, A.J., Wilkinson, J.J. (Eds.), Ore Deposits in an Evolving Earth. Geolog-ical Society, London, p. 393 (special publication).

Morris, P.A., Kirkland, C.L., 2014. Melting of a subduction-modified mantle source:a case study from the Archean Marda Volcanic Complex, central Yilgarn Craton,Western Australia. Lithos 190–191, 403–419.

Morris, P.A., Witt, W.K., 1997. Geochemistry and tectonic setting of two con-trasting Archaean felsic volcanic associations in the Eastern Goldfields, WesternAustralia. Precambrian Res. 83, 83–107.

Mueller, A.G., McNaughton, N.J., 2000. U–Pb ages constraining batholith emplace-ment, contact metamorphism, and the formation of gold and W-Mo skarnsin the Southern Cross Area, Yilgarn Craton, Western Australia. Econ. Geol. 95,1231–1257.

Myers, J.S., 1990. Precambrian tectonic evolution of a part of Gondwana, southwest-ern Australia. Geology 18, 537–540.

Nebel, O., Arculus, R.J., Ivanic, T.J., Nebel-Jacobsen, Y.J., 2013. Lu–Hf isotopic mem-ory of plume-lithosphere interaction in the source of layered mafic intrusions,Windimurra Igneous Complex, Yilgarn Craton, Australia. Earth Planet. Sci. Lett.380, 151–161.

Nelson, D.R., 1995. 112159: Porphyritic Dacite, Royal Arthur; Geochronology Dataset488, Compilation of Geochronology Data, June 2006 Update. Western AustraliaGeological Society.

Nelson, D.R., 1997. Evolution of the Archaean granite-greenstone terranes of theEastern Goldfields, Western Australia: SHRIMP U–Pb zircon constraints. Pre-cambrian Res. 83, 57–81.

Nelson, D.R., 2001a. 168959: Porphyritic Granophyre, Butcher Bird No. 1 mine;Geochronology Dataset 193, Compilation of Geochronology Data, June 2006Update. Western Australia Geological Survey.

Nelson, D.R., 2001b. 169003: Vesicular Rhyolite, Carron Hill; Geochronology Record170. Geological Survey of Western Australia.

Nelson, D.R., 2002. 169067: Quartz-chlorite Schist, Pincher Well; GeochronologyRecord 105. Geological Survey of Western Australia.

Nelson, D.R., 2005. 127238: Felsic tuff, Anaconda Cu Mine; Geochronology Dataset577. Geological Survey of Western Australia.

Ohmoto, H., Skinner, B.J., 1983. The Kuroko and Related Volcanogenic Massive Sul-fide Deposits.

Pawley, M.J., Wingate, M.T.D., Kirkland, C.L., Wyche, S., Hall, C.E., Romano, S.S., Dou-blier, M.P., 2012. Adding pieces to the puzzle: episodic crustal growth and a newterrane in the northeast Yilgarn Craton, Western Australia. Aust. J. Earth Sci. 59,603–623.

Pearce, J.A., 1996. A user’s guide to basalt discrimination diagrams. In: Wyman, D.A.(Ed.), Trace Element Geochemistry of Volcanic Rocks: Applications for MassiveSulphide Exploration. Geological Association of Canada, pp. 79–113.

Perring, C.S., Barnes, S.J., Hill, R.E.T., 1996. Geochemistry of komatiites from For-restania, Southern Cross Province, Western Australia: evidence for crustalcontamination. Lithos 37, 181–197.

Phillips, G.N., 2004. Opportunities for a major copper-zinc province in the YilgarnCraton. In: McConachy, T.F., McInnes, B.I.A. (Eds.), Copper–zinc massive sulphidedeposits in Western Australia. CSIRO, pp. 1–6.

Pidgeon, R.T., Hallberg, J.A., 2000. Age relationships in supracrustal sequencesof the northern part of the Murchison terrane, Archaean Yilgarn Craton,Western Australia: a combined field and U–Pb study. Aust. J. Earth Sci. 47,153–165.

Pidgeon, R.T., Wilde, S.A., 1990. Distribution of 3.0 Ga and 2.7 Ga Volcanic Episodesin the Yilgarn Craton of Western Australia. Precambrian Res. 48, 309–325.

Piercey, S.J., 2011. The setting, style, and role of magmatism in the formation ofvolcanogenic massive sulphide deposits. Miner. Depos. 46, 449–471.

Piercey, S.J., Paradis, S., Murphy, D.C., Mortensen, J.K., 2001. Geochemistry and pale-otectonic setting of felsic volcanic rocks in the Finlayson Lake, volcanic-hostedmassive sulfide district, Yukon, Canada. Econ. Geol. 96, 1877–1905.

Piercey, S.J., Peter, J.M., Mortensen, J.K., Paradis, S., Murphy, D.C., Tucker, T.L., 2008.Petrology and U–Pb geochronology of footwall porphyritic rhyolites from the


Wolverine volcanogenic massive sulfide deposit, Yukon, Canada: implicationsfor the genesis of massive sulfide deposits in continental margin environments.Econ. Geol. 103, 5–33.

Riganti, A., Wyche, S., Wingate, M.T.D., Kirkland, C.L., Chen, S.F., 2010. Constraintson ages of greenstone magmatism in the northern part of the Southern Cross







































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Domain, Yilgarn Craton. In: Tyler, I.M., Knox-Robinson, C.M. (Eds.), Fifth Inter-national Archean Symposium Abstract.

omano, S.S., Thebaud, N.J.M., Mole, D.R., Wingate, M.T.D., Kirkland, C.L., Doublier,M.P., 2013. Geochronological constraints on nickel metallogeny in the Lake John-ston belt, Southern Cross Domain. Aust. J. Earth Sci. 61, 143–157.

oss, P.-S., Bédard, J.H., 2009. Magmatic affinity of modern and ancient subalkalinevolcanic rocks determined from trace-element discrimination diagrams. Can. J.Earth Sci. 46, 823–839.

cowen, P., 1991. The Geology and Geochemistry of the Narndee Intrusion. Aus-tralian National University, Canberra, Australia.

harpe, R., Gemmell, J.B., 2000. Sulfur isotope characteristics of the Archean Cu–ZnGossan Hill deposit, Western Australia. Miner. Depos. 35, 533–550.

harpe, R., Gemmell, J.B., 2001. Alteration characteristics of the Archean GoldenGrove Formation at the Gossan Hill deposit, Western Australia: induration asa focussing mechanism for mineralizing hydrothermal fluids. Econ. Geol. 96,1239–1262.

harpe, R., Gemmell, J.B., 2002. The Archean Cu–Zn magnetite-rich Gossan Hillvolcanic-hosted massive sulphide deposit, Western Australia: genesis of a mul-tistage hydrothermal system. Econ. Geol. 97, 517–539.

ilver Lake Resources, 2013a. ASX announcement, 22 May 2013. Available athttp://www.silverlakeresources.com.au/investors/asx-announcements

ilver Lake Resources, 2013b. Paydirt’s Gold Conference, Perth April 2012. Presen-tation, Available at http://www.silverlakeresources.com.au

ilver Swan, 2012. Annual Report 2013, Available at http://www.caravelminerals.com.au/investors–media/annual-reports/2014

ircombe, K.N., Cassidy, K.F., Champion, D.C., Tripp, G., 2007. Compilation of SHRIMPU–Pb Geochronological Data, Yilgarn Craton, Western Australia, 2004–2006.Geoscience Australia Record 2007/01.

quire, R.J., Allen, C.M., Cas, R.A.F., Campbell, I.H., Blewett, R.S., Enchain, A.A., 2010.Two cycles of voluminous pyroclastic volcanism and sedimentation related toepisodic granite emplacement during the late Archean: Eastern Yilgarn Craton,Western Australia. Precambrian Res. 183, 251–274.

an Kranendonk, M.J., Ivanic, T.J., Wingate, M.T.D., Kirkland, C.L., Wyche, S.,2013. Long-lived, autochthonous development of the Archean MurchisonDomain, and implications for Yilgarn Craton tectonics. Precambrian Res. 229,49–92.

earncombe, S., 2010. Yilgarn volcanogenic massive sulphides. In: Wyche, S. (Ed.),Yilgarn-Superior Workshop – Abstracts, Fifth International Archean Sympo-sium. Geological Survey of Western Australia, Record 2010/20. , pp. 47–50.

earncombe, S., Kerrich, R., 1999. Geochemistry and geodynamic setting of vol-canic and plutonic rocks associated with Early Archaean volcanogenic massivesulphide mineralization. Pilbara Craton. Precambrian Res. 98, 243–270.

ickery, N.M., (unpublished Ph.D. thesis) 2004. The Plutonic Gold Deposit, WesterAustralia: Geology and Geochemistry of an Archaean Orogenic Gold System.University of New England, Armadale, 497 pp.

ang, Q., 1998. Geochronology of the Granite-greenstone Terranes in the Murchi-son and Southern Cross Provinces of the Yilgarn Craton, Western Australia.Australian National University, Canberra, Australia, pp. 186.

ang, Q., Beeson, J., Campbell, I.H., 1998. Granite-greenstone zircon U–Pbgeochronology of the gum creek greenstone belt, southern cross province,Yilgarn Craton: tectonic implications, structure of the Australian continent. Geo-dynamics, vol. 26. American Geophysical Union, pp. 175–186.

atkins, K.P., Hickman, A.H., 1990. Geological evolution and mineralization ofthe Murchison Province, Western Australia. Geol. Surv. West. Aust. Bull. 137,267.

hitford, D.J., Ashley, P.M., 1992. The Scuddles volcanic-hosted massive sulfidedeposit, Western Australia: geochemistry of the host rocks and evaluation oflithogeochemistry for exploration. Econ. Geol. 87, 873–888.

iedenbeck, M., Watkins, K.P., 1993. A time scale for granitoid emplacement in theArchean Murchison Province, Western Australia, by single zircon geochronol-ogy. Precambrian Res. 61, 1–26.

ingate, M.T.D., Bodorkos, S., 2007a. 177919: Felsic Metavolcanic Rock, Urania



Prospect; Geochronology dataset 666. Compilation of Geochronology Data. Geo-logical Survey of Western Australia Geological Survey.

ingate, M.T.D., Bodorkos, S., 2007b. 177933: Hornblende Granodiorite, CamelBore; Geochronology Dataset 675, Compilation of Geochronology data. WesternAustralia Geological Survey.


Wingate, M.T.D., Bodorkos, S., Kirkland, C.L., 2008a. 184112: Metasandstone, RamWell; Geochronology Dataset 736, Compilation of Geochronology Data. Geolog-ical Survey of Western Australia.

Wingate, M.T.D., Bodorkos, S., Kirkland, C.L., 2008b. 185138: Felsic Volcanic Rock,Spriggs Bore; Geochronology Dataset 738. Compilation of geochronology Data.Geological Survey of Western Australia.

Wingate, M.T.D., Kirkland, C.L., Van Kranendonk, M.J., 2010a. 185920: Biotite-hornblende Metamonzogranite, Outcamp Bore. Geochronology Record 889.Geological Survey of Wester Australia.

Wingate, M.T.D., Kirkland, C.L., Van Kranendonk, M.J., 2010b. 185933: Biotite Grano-diorite, Eelya North Mine; Geochronology Record 894. Geological Survey ofWestern Australia.

Wingate, M.T.D., Kirkland, C.L., Compston, W., Wyche, S., 2011a. 185998: FelsicMetavolcaniclastic Rock, Dan Well; Geochronology Record 979. Geological Sur-vey of Western Australia, pp. 4.

Wingate, M.T.D., Kirkland, C.L., Riganti, A., Wyche, S., 2011b. 185990: Metagab-bro, Grass Flat Bore; Geochronology Record 868. Geological Survey of WesternAustralia, pp. 4.

Wingate, M.T.D., Kirkland, C.L., Chen, S.F., 2012a. 185932: Metarhyolite, Eelya Hill;Geochronology Record 1007. Geological Survey of Western Australia, pp. p4.

Wingate, M.T.D., Kirkland, C.L., Chen, S.F., 2012b. 193979: Meta-andesite,Tootawarra Well; Geochronology Record 1012. Geological Survey of WesternAustralia, pp. 4.

Wingate, M.T.D., Kirkland, C.L., Ivanic, T.J., 2012c. 193972: Metarhyolite Clast in Vol-caniclastic Breccia, Weld Range; Geochronology Record 1011. Geological Surveyof Western Australia, pp. 4.

Wingate, M.T.D., Kirkland, C.L., Wyche, S., 2012d. 183338: Metadacite, MingahRange; Geochronology Record 1074. Geological Survey of Western Australia,pp. 4.

Witt, W.K., 1994. Geology of the Melita 1: 100,000 Sheet, Western Australia. WesternAustralia Geological Survey Explanatory Notes.

Witt, W.K., 1999. The Archaean Ravensthorpe Terrane, Western Australia: synvol-canic Cu–Au mineralization in a deformed island arc complex. Precambrian Res.96, 143–181.

Witt, W.K., Morris, P.A., Wyche, S., Nelson, D.R., 1996. The Gindalbie Terrane as aTarget for VMS-style Mineralisation in the Eastern Goldfields Province of theYilgarn Craton. Technical Paper, Geological Survey of Western Australia, AnnualReview 1995–1996., pp. 41–57.

Wyche, S., 2007. Evidence of pre-3100 Ma crust in the Youanmi and SouthWest Terranes, and Eastern Goldfields Superterrane, of the Yilgarn Craton.In: Van Kranendonk, M.J., Smithies, R.H., Bennet, V. (Eds.), Earth’s Old-est Rocks, Developments in Precambrian Geology. Elsevier, Amsterdam, pp.113–124.

Wyche, S., Kirkland, C.L., Riganti, A., Pawley, M.J., Belousova, E.A., Wingate, M.T.D.,2012. Isotopic constraints on stratigraphy in the central and eastern YilgarnCraton, Western Australia. Aust. J. Earth Sci. 59, 657–670.

Wyche, S., Pawley, M.J., Chen, S.F., Ivanic, T.J., Zibra, I., Van Kranendonk, M.J., Spag-giari, C.V., Wingate, M.T.D., 2013. Geology of the northern Yilgarn Craton. In:Wyche, S., Ivanic, T.J., Zibra, I. (Eds.), Youanmi and Southern Carnarvon Seismicand Magnetotelluric (MT) Workshop. Geological Survey of Western Australia.Record 2013/6. , pp. 31–60.

Wyman, D.A., 2000. High-precision exploration geochemistry: applications for vol-canogenic massive sulfide deposits. Aust. J. Earth Sci. 47, 861–871.

Wyman, D.A., Kerrich, R., 2012. Geochemistry and isotopic characteristics ofYouanmi terrane volcanism: the role of mantle plumes and subduction tectonicsin the western Yilgarn Craton. Aust. J. Earth Sci. 59, 671–694.

Yeats, C.J., 2007. VHMS mineral systems in the Yilgarn – characteristics and explo-ration potential. In: Bierlein, F.P. (Ed.), Proceedings of Geoconferences (WA) Inc.Kalgoorlie 07 Conference. , pp. 65–69.

Yeats, C.J., Groves, D.I., 1998. The Archaean Mount Gibson gold deposits,Yilgarn Craton, Western Australia: products of combined synvol-canic and syntectonic alteration and mineralisation. Ore Geol. Rev. 13,


103–129.Yeats, C.J., McNaughton, N.J., Groves, D.I., 1996. SHRIMP U–Pb geochronological

constraints on Archaean volcanic-hosted massive sulphide and lode gold min-eralization at Mount Gibson, Yilgarn Craton, Western Australia. Econ. Geol. 91,1354–1371.
























































































































































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a review of volcanic-hosted massive sulfide (vhms) mineralization in the archaean yilgarn craton,...

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