Stratigraphic Revision of the Warrawoona and Gorge Creek Groups in the Kelly Greenstone Belt, Pilbara Craton, Western Australia by L

Technical papers

Stratigraphic revision of the Warrawoona and Gorge Creek Groups in the Kelly greenstone belt, Pilbara Craton, Western Australia by L. Bagas1

variable than previously thought (Van Kranendonk et al., 2002). The Abstract following review and reinterpret- ation of the stratigraphy of the Kelly Mapping in the Kelly greenstone belt in the eastern part of the East greenstone belt is based on mapping Pilbara Granite–Greenstone Terrane of the Pilbara Craton indicates that and geochronology resulting from the stratigraphy of the Warrawoona Group requires significant revision. the National Geoscience Mapping Four stratigraphic revisions are proposed. The Warrawoona Group now Accord (NGMA) projects on the includes the redefined Salgash Subgroup and the newly defined Kelly SPLIT ROCK * (Bagas and Van Subgroup. The felsic volcanic rocks of the c. 3325–3320 Ma Wyman Kranendonk, in prep.), MOUNT EDGAR Formation conformably overlie the Euro Basalt and are now included in (Williams and Bagas, in prep.), and the Warrawoona Group. The 3324 ± 4 Ma Kelly porphyry, previously NULLAGINE (Bagas, in prep.) 1:100 000 thought to be a felsic volcanic interbed in the Euro Basalt, is now sheet areas. recognized as intruding the Euro Basalt and is associated with the overlying Wyman Formation. The Charteris Basalt, previously included in the Gorge Creek Group, is now included with the Kelly Subgroup and it conformably overlies the Wyman Formation. The redefined East Pilbara Granite– Warrawoona Group is unconformably overlain by sedimentary rocks of Greenstone Terrane the c. 3308 Ma Budjan Creek Formation and dominantly clastic sedimentary rocks of the 3240–2940 Ma Gorge Creek Group (locally The EPGGT is characterized by large redefined to exclude the Charteris Basalt). ovoid granitoid complexes forming domes that are surrounded by KEYWORDS: Archaean, Pilbara Craton, stratigraphy, East Pilbara synformal greenstone belts or Granite–Greenstone Terrane, Kelly greenstone belt. unconformably overlain by volcanic and sedimentary rocks of the Fortescue Group (Fig. 2). The greenstone belts commonly dip at moderate to steep angles away from granitoid complexes, and are typically metamorphosed to greenschist facies, although higher grades are reached near the Introduction granite–greenstones of the Kelly complexes. greenstone belt form part of the The Archaean Pilbara Craton in c. 3655–2830 Ma East Pilbara Table 1 summarizes the former and the northwest of Western Granite–Greenstone Terrane current stratigraphic nomenclature Australia contains well-exposed (EPGGT) of the northern Pilbara of the EPGGT, and Table 2 shows granite–greenstones that are Craton (Hickman, 2001; Fig. 1). the geochronological data for the unconformably overlain by volcanic Kelly greenstone belt. and sedimentary rocks of the Hickman (1983, 1984) provided a c. 2770–2400 Ma Hamersley Basin, regional lithostratigraphic which around the Kelly greenstone interpretation of the EPGGT based belt are part of the 2770–2630 Ma on 1:250 000-scale reconnaissance Stratigraphy of the Kelly Fortescue Group (Trendall, 1990; geological mapping during the greenstone belt Thorne and Trendall, 2001). The 1970s. Subsequent investigations broadly confirmed the continuity The southern part of the Kelly 1 [email protected] between greenstone belts of the greenstone belt outcrops between * Capitalized names refer to standard 1:100 000 EPGGT, but have also shown that the Corunna Downs Granitoid map sheets. the greenstones are more laterally Complex (CDGC) to the west and

53 Geological Survey of Western Australia 2001–02 Annual Review

20° 117° 118° 119° 120° 121° INDIAN OCEAN ? ? 100 km

TERRANE

WEST PILBARA GRANITE–GREENSTONEZONE 21° MOUNT CENTRAL PILBARA TECTONIC EDGAR WPGGTMB GRANITOID TERRANE COMPLEX

MB EAST PILBARA GRANITE–GREENSTONE EPGGT Mosquito Creek Basin

22° Figure 2

LB132a 25.09.02

Mesoproterozoic–Phanerozoic rocks MB Mallina Basin LOCATION MAP

Hamersley Basin GGT Granite–greenstone terrane MAP AREA Terrane and/or tectonic zone boundary PILBARA Northern Pilbara Inlier CRATON

CAPRICORN OROGEN Mallina Basin

YILGARN Greenstone CRATON

PERTH Granitoid 500 km

Figure 1. Regional geological setting of the East Pilbara Granite–Greenstone Terrane

the Fortescue Group to the east, and were emplaced approximately with the Euro Basalt and Wyman the northeastern part of the belt lies contemporaneously with felsic Formation in the Kelly Subgroup between the McPhee Dome and the volcanic rocks of the Wyman of the Warrawoona Group. Mount Edgar Granitoid Complex Formation and the Budjan Creek (Fig. 2). In both areas the belt Formation (Bagas et al., 2002). Another change not shown in comprises dominantly greenschist- Table 1 is that the 3324 ± 4 Ma facies volcanic rocks of the Salgash Kelly porphyry, previously and Kelly Subgroups of the Warrawoona Group thought to be a correlative of the Warrawoona Group. The Following detailed mapping and Panorama Formation (Hickman, Warrawoona Group is unconform- geochronological studies in the Kelly 1983) or a felsic volcanic interbed in ably overlain by the dominantly greenstone belt, three major the Euro Basalt (McNaughton et al., sedimentary sequences of the stratigraphic revisions have been 1993), is now recognized as Budjan Creek Formation (Noldart made for the Warrawoona Group intruding the Euro Basalt and and Wyatt, 1962; Lipple, 1975), (Tables 1 and 2): associated with the overlying which in turn is unconformably • The Kelly greenstone belt is now Wyman Formation. overlain by the dominantly clastic subdivided into the redefined sedimentary rocks of the Gorge Salgash Subgroup and the newly Salgash Subgroup Creek Group (Noldart and Wyatt, defined Kelly Subgroup. 1962; Ryan and Kriewaldt, 1964; • The felsic volcanic rocks of the The Salgash Subgroup, which Hickman and Lipple, 1978; c. 3325–3320 Ma Wyman formerly included the Towers Hickman, 1983), and the Fortescue Formation conformably overlie Formation, Apex Basalt, Panorama Group (Bagas and Van Kranendonk, the Euro Basalt and are now Formation, and Euro Basalt in prep.; Table 2). included in the Warrawoona (Hickman 1990), now comprises the Group. Apex Basalt (not in the Kelly Granitoid rocks in the CDGC (Fig. 2) • The Charteris Basalt, which was greenstone belt), Panorama mostly range in age from about 3317 previously included in the Gorge Formation, and Strelley Pool Chert to 3307 Ma (Nelson, 2001, 2002), and Creek Group, is now included (Table 1).

54 Technical papers

Fortescue Group

MOUNT Gorge Creek Group Ultramafic rock EDGAR Corunna Downs Granitoid Complex Budjan Creek Formation Boobina Porphyry

Charteris Basalt C Wyman Formation Kelly Porphyry B Kelly

Subgroup Euro Basalt 21°30' Mount Edgar Granitoid Complex Strelley Pool Chert Panorama Formation 3433±2 Ma

Salgash Apex Basalt Subgroup Warrawoona Group Duffer Formation Talga Talga Subgroup 80 Spinaway Mine Anticline 5 60 D Point referred to in text 70 70 3324±4 Ma Geochronology site McPhee Way-up indicator, pillow structure Dome 15 Bedding, showing strike and dip Plunging anticline Plunging syncline 70 NULLAGINE 1: 100 000 map sheet 3317±2 Ma 65 3321±4 Ma Unconformity Copper Hills Fault c. 3346 Ma 3308±5 Ma Road

3325±3 Ma Track 3315±4 Ma

NULLAGINE Figure 2. Geology of the Kelly greenstone belt 50

35 The Panorama Formation (Lipple, previously interpreted as the 1975) consists of felsic Towers Formation (Hickman, volcaniclastic rocks, with 1983). The Strelley Pool Chert subordinate felsic lavas and chert. consists of silicified chert, 120°00' The formation outcrops in the sandstone, and intraformational northeastern part of the Kelly breccia. The chert commonly has Kellys greenstone belt and is intruded by pseudomorphs after barite and granitoid rocks of the CDGC. It gypsum, and wavy to domal 3324±4 Ma was previously interpreted as the laminates with local conical 15 c. 3470–3465 Ma Duffer Formation stromatolites. The base of the unit 50 (Hickman, 1983). Three samples of shows evidence of relict 3325±4 Ma SPLIT volcanic breccia from the topography and differential Cookindina ROCK formation at Sandy Creek were erosion of the underlying Syncline dated at 3433 ± 2 Ma (Nelson, Panorama Formation, with a A 2000), and 3428 ± 4 and 3427 ± corresponding pinching and 3323±3 Ma 2 Ma (Nelson, 2001). These dates swelling of the chert along strike are consistent with the age of the and the filling of palaeochannels in 40 D E Panorama Formation elsewhere in places (Williams and Bagas, in the EPGGT. prep.). 30 N The Strelley Pool Chert (Lowe, Deposition of the Strelley Pool 1983) is a discontinuous unit Chert reflects a hiatus in volcanism 15 conformably overlying the recognized over 220 km across the 5 km Panorama Formation in the EPGGT (Van Kranendonk et al., northeastern part of the Kelly 2002) and is thought to represent LB140 07.10.02 greenstone belt, and was the final hydrothermal phase of

55 Geological Survey of Western Australia 2001–02 Annual Review

Table 1. Stratigraphy of the East Pilbara Granite–Greentone Terrane. Units in the Kelly greenstone belt are here shown in bold, and the stratigraphic nomenclature for units outside of the belt is taken from Van Kranendonk et al. (2002)

Hickman (1990) This paper Lalla Rookh Sandstone De Grey Group De Grey Group Lalla Rookh Sandstone (s) Budjan Creek Formation

Pyramid Hill Formation (sh)

Honeyeater Basalt Honeyeater Basalt Cleaverville Formation Paddy Market Formation (sh, BIF) Corboy Formation Corboy Formation

Subgroup Pincunah Hill Formation Soanesville (sh, BIF) Gorge Creek Group Gorge Creek Group Subgroup Soanesville Charteris Basalt

Wyman Formation Kangaroo Caves Formation (f, an, c) Kunagunarrina Formation (u, b) Group Springs Sulphur Leilira Formation (ss, f) FF Golden Cockatoo Formation (ss, sh) Budjan Creek Formation (cong, ss, sh, f)

Charteris Basalt (b, f)

Wyman Formation (f, ss) Kelly

Euro Basalt Subgroup Euro Basalt (b, c)

Strelley Pool Chert (c, ss, cong)

Panorama Formation Panorama Formation (f) Salgash Salgash Subgroup Subgroup Apex Basalt Apex Basalt (b)

Towers Formation Towers Formation (c, b)

Duffer Formation Duffer Formation (f, an) Warrawoona Group Warrawoona Group Mount Ada Basalt Mount Ada Basalt (b)

McPhee Formation McPhee Formation (u, c, f)

Subgroup North Star Basalt North Star Basalt (b, u) Talga Subgroup Talga Dresser Formation (c, b)

Double Bar Formation (b)

Coucal Formation (f, c) Coonterunah Group Table Top Formation (b)

LB139 25.09.02

unconformity cong conglomerate

local unconformity ss sandstone

FFfault sh shale b basalt c chert

u ultramafic rock BIF banded iron-formation

an andesite f felsic volcanic rocks

56 Technical papers felsic volcanism associated with the In the Kelly greenstone belt the Euro Formation unconformably overlies deposition of the Panorama Basalt consists dominantly of the Salgash Subgroup 7 km Formation. Both formations are tholeiitic pillow basalt, with southwest of Budjan Creek interpreted to be genetically related subordinate interbedded pillowed, (Hickman, 1983). New mapping has (Van Kranendonk, 2000), whereas ocellar, and occasionally vesicular, established that the unconformity in the overlying ultramafic and mafic high-Mg basalt. The base of the this area is between the Euro Basalt rocks of the Euro Basalt mark the formation typically contains a unit of and the Budjan Creek Formation. beginning of a new volcanic phase. komatiite or komatiitic basalt up to Van Kranendonk et al. (2002) 500 m thick. The formation is also The Wyman Formation is about suggested that the Euro Basalt was interbedded with chert that is locally 1 km thick and consists of felsic tuff related to a separate mantle plume stromatolitic (Williams and Bagas, in interbedded with porphyritic than the one they interpreted to have prep.). The Euro Basalt has a rhyolite to rhyodacite, felsic produced the Salgash Subgroup. For stratigraphic thickness of about 4 km agglomerate and volcaniclastic this reason the Euro Basalt has been in the northeastern part of the Kelly sandstone, and fine-grained quartz separated from the Salgash greenstone belt. However, this is a sandstone. The formation has been Subgroup and included in the minimum thickness for the dated in three places in the Kelly overlying Kelly Subgroup (Bagas formation as its top is locally faulted greenstone belt with a conventional and Van Kranendonk, in prep.). out, and elsewhere in the belt its zircon age of 3325 ± 4 Ma (Thorpe base is intruded by granitoid rocks et al., 1992b; McNaughton et al., 1993), and sensitive high-resolution Kelly Subgroup of the CDGC. ion microprobe (SHRIMP) U–Pb The Kelly Subgroup conformably West of the Copper Hills mine, the zircon ages of 3323 ± 3 Ma (Nelson, overlies the Salgash Subgroup and Euro Basalt contains several bands 2001), and 3321 ± 4 Ma (Barley and consists of the Euro Basalt, Wyman of chert interbedded with minor Pickard, 1999). These ages are Formation, and Charteris Basalt. mafic and felsic tuff. Chert in the identical within analytical error to upper part of the formation contains the 3324 ± 4 Ma SHRIMP U–Pb After deposition of the Strelley Pool zircon populations of 3363 ± 6, zircon age for intrusive felsic rocks Chert, volcanism in the Kelly 3346 ± 6, and 3311 ± 9 Ma (Nelson, from the informally named Kelly greenstone belt resumed with 2001). The age of the youngest porphyry (McNaughton et al., 1993). deposition of high-Mg basaltic rocks population (6 of 22 zircons analysed) The porphyry has been shown to be and komatiite of the Euro Basalt. The is within the error margins of the an intrusive unit by Bagas and Van date at which this volcanism 3315 ± 4 Ma age of the Boobina Kranendonk (in prep.) rather than resumed is unknown, but probably Porphyry (Barley and Pickard, 1999), an extrusive unit as suggested by occurred at c. 3420–3410 Ma, which which intruded the Euro Basalt Hickman (1983) and McNaughton is the age of gold mineralization about 500 m to the south. The age of et al. (1993). These data confirm that (Thorpe et al., 1992a) and zircon the youngest zircon population is there is a synchronous relationship overgrowths (Zegers, 1996; Van therefore interpreted to represent between volcanism (Wyman Kranendonk, in prep.). The duration an overgrowth event associated Formation) and subvolcanic of volcanism is a major outstanding with porphyry intrusion (Bagas intrusions (Kelly porphyry) in the problem, but indications are that this and Van Kranendonk, in prep.). The Kelly greenstone belt. succession was deposited over an c. 3346 Ma age of the largest approximately 100 million-year population (14 of 22 samples) is The Charteris Basalt outcrops in the period from c. 3420 to 3325 Ma, the interpreted as the depositional age northeastern part of the Kelly younger limit being the age of the of the tuff, whereas the oldest greenstone belt, on the northwestern conformably overlying Wyman population is considered to be part of NULLAGINE and southwestern Formation in the southeastern part of xenocrystic. part of MOUNT EDGAR (Fig. 2), where the Kelly greenstone belt. it is between 500 and 2000 m thick The c. 3325 Ma Wyman Formation and consists mainly of pillowed conformably overlies the Euro Basalt high-Mg and tholeiitic basalt. The across a transitional zone of basalt lies conformably on the Table 2. Ages of units in and around the Kelly interbedded rhyolite and basalt that greenstone belt Wyman Formation (e.g. at point B is about 50 m thick (e.g. at point A on Fig. 2; Williams and Bagas, in on Fig. 2) and is now therefore prep.) and is unconformably included in the Warrawoona Group. overlain by clastic sedimentary rocks Unit Age (Ma) The Wyman Formation was of the 3240–2940 Ma Gorge Creek excluded from the Warrawoona Group (e.g. at point C on Fig. 2; Fortescue Group 2770–2630 Group by Hickman (1990) for two Williams and Bagas, in prep.). The Gorge Creek Group 3240–2940 reasons. Firstly, geochronological Charteris Basalt must therefore be Budjan Creek Formation 3308 ± 5 data available in the late 1980s Boobina Porphyry 3315 ± 4 aged between 3320 and 3240 Ma, Kelly porphyry 3324 ± 4 suggested that the contact between and has thus been reassigned from Warrawoona Group c. 3490–3320 the Wyman Formation and the unconformably overlying Gorge Kelly Subgroup underlying Euro Basalt represented Creek Group (Hickman, 1983; Charteris Basalt c. 3320 (inferred) a time break of about 125 million Lipple, 1975) to the top of the Wyman Formation c. 3325–3320 years. Recent geochronological data, Euro Basalt 3420–3325 Warrawoona Group (Table 1). Salgash Subgroup however, indicate that the upper Strelley Pool Chert c. 3425 (inferred) part of the Euro Basalt is about Rocks similar to the Charteris Basalt Panorama Formation 3433–3427 3346 Ma. Secondly, mapping in the within the Wyman Formation about 1970s suggested that the Wyman 50 km west of the Kelly greenstone

57 Geological Survey of Western Australia 2001–02 Annual Review belt in the Warrawoona area horizon, which extends to north of from the margin of the CDGC and (Hickman, in prep.) indicate that the the Copper Hills mine, and consists Mount Edgar Granitoid Complex. ultramafic and mafic volcanic rocks of lithic wacke, siltstone, minor of the Charteris Basalt do not conglomerate, crystal-lithic felsic tuff The unconformable relationships necessarily represent a new volcanic and agglomerate, and fine-grained between the c. 3325–3320 Ma cycle above the Kelly Subgroup. volcanogenic sandstone. Crystal- Wyman Formation of the lithic tuff from 1 km southeast of the Warrawoona Group and the Copper Hills mine (Fig. 2) was dated 3308 Ma Budjan Creek Formation, Budjan Creek Formation at 3308 ± 5 Ma (Nelson, 2001). This and between the Budjan Creek date provides a tight constraint on Formation and the c. 3235–2970 Ma The Budjan Creek Formation only the age of folding and faulting of the Gorge Creek Group have a number outcrops in the Kelly greenstone belt Warrawoona Group in the Kelly of implications. Several different where the upward-fining boulder greenstone belt. types of tectonic structures formed conglomerate at the base of the during the short period between formation unconformably overlies 3320 and 3308 Ma, and between 3308 the Warrawoona Group (e.g. at Gorge Creek Group and c. 3240 Ma (Bagas and Van point D on Fig. 2). The formation Kranendonk, in prep.). The first grades upward into interbedded The Gorge Creek Group overlies the period of deformation may be sandstone and siltstone, which are Budjan Creek Formation with a low- related to the development of the overlain across a low-angle angle unconformity on SPLIT ROCK, dome forming around the CDGC, unconformity by pebble disconformably overlies the and points to a discernible episode conglomerate at the base of the c. 3240 Ma Sulphur Springs Group of compression related to the Gorge Creek Group (e.g. at point E on adjoining NORTH SHAW and formation of the Spinaway Anticline, on Fig 2; Bagas and Van TAMBOURAH (Van Kranendonk and Cookindina Syncline, and the CDGC Kranendonk, in prep.). The lower Morant, 1998), and is unconformably (Fig. 2). The maximum age limit of unconformity with the Warrawoona overlain by the c. 2940 Ma De Grey the first event is slightly older than Group was previously equated with Group (Van Kranendonk et al., the granitic rocks near the eastern the one above the Gorge Creek 2002). The Gorge Creek Group is edge of the CDGC, which decrease Group (Lipple, 1975; Hickman, 1983; therefore between 3240 and 2940 Ma in age westward from 3317 ± 2 Ma Hickman, 1990), and the formation in age. (Barley and Pickard, 1999) to 3307 ± was correlated with the Lalla Rookh The Gorge Creek Group on eastern 4 Ma (Nelson, 2000). These limited Sandstone of the De Grey Group geochronological data indicate that SPLIT ROCK and southern MOUNT (Table 1). The unconformity above granitoid magmatism was the Budjan Creek Formation was not EDGAR is at least 750 m thick. Its basal unit consists of a lensoidal, synchronous with the older previously recognized and shows deformation event. that the formation cannot be upward-fining, clast- to matrix- supported, cobble to pebble correlated with the much younger The Budjan Creek Formation and conglomerate that probably De Grey Group. Gorge Creek Group dip at about 30° correlates lithologically with the away from the centre of the CDGC Corboy Formation (Table 1). The The thickness of the Budjan Creek in the same direction as limited conglomerate contains clasts of Formation varies along strike from palaeocurrents measured in the chert, felsic porphyry, and rare mafic about 1.5 km southeast of the Kelly formations (Bagas and Van volcanic rocks, which are identical to mine to about 500 m east of the Kranendonk, in prep.). This tilting rocks in the underlying Warrawoona Copper Hills mine. The basal part of away from the complex is indicative Group. The conglomerate is the formation southeast of the Kelly of its upward and outward growth conformably overlain by a mine is an approximately 1 km-thick after the earlier deformation event. succession of silicified and succession, starting with a boulder The Gorge Creek Group overlies the ferruginized shale, banded iron- conglomerate that fines upward into Budjan Creek Formation with a low- formation and grey and white a pebble conglomerate interbedded angle unconformity on the eastern layered chert, banded and with arkosic sandstone, and then side of SPLIT ROCK, indicating that ferruginous chert, black into siltstone and shale. The clasts in tilting was intermittent during the carbonaceous shale and minor the conglomerate consist deposition of these units. predominantly of vein quartz and siltstone, and thinly bedded banded chert with rare felsic volcanic rocks, iron-formation interbedded with and are consistent with derivation ferruginous chert. This succession is from a local Warrawoona Group lithologically similar to, and source. In addition, the arkosic probably correlates with, the Paddy composition of the sandstone and Market Formation (Table 1). the rare south- to southeast-trending palaeocurrent direction within the sandstone are consistent with the Discussion and conclusion derivation of at least part of the formation from the CDGC. The volcanic and volcaniclastic rocks of the Warrawoona Group in the The basal clastic unit of the Budjan Kelly greenstone belt are Creek Formation is conformably and unconformably overlain by sharply overlain by an successively younger groups with approximately 500 m-thick marker shallowing dips to the east away

58 Technical papers

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