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| | | Edmundian Orogeny D2e/M2e (CED2) | S Sheppard, SP Johnson, FJ Korhonen, and MTD Wingate | | | | | Event type | deformation: undivided | Parent event | | Child events | | Tectonic units affected | | Tectonic setting | orogen: intracratonic orogen | Metamorphic facies | | greenschist: chlorite | amphibolite: sillimanite |
| Metamorphic/tectonic features | schistose |
| | | Summary | The first pervasive deformation event attributed to the Edmundian Orogeny in the Gascoyne Province (D2e) reflects structural and metamorphic reworking within the Mutherbukin Zone between the Ti Tree and Chalba Shear Zones. Deformation and metamorphism resulted in the formation of a pervasive foliation, and locally, the growth of both garnet and staurolite porphyroblasts. These tectonic fabrics and metamorphic assemblages were previously interpreted to be related to the Paleoproterozoic Capricorn Orogeny (Williams et al., 1983; Williams, 1986; Culver, 2001; Varvell, 2001; Fitzsimons et al., 2004) or to the Paleoproterozoic Mangaroon Orogeny (Sheppard et al., 2005). However, SHRIMP U–Pb dating of monazite and xenotime aligned within the D2e fabric indicates that regional metamorphism and deformation occurred between c. 1030 and c. 990 Ma (Sheppard et al., 2007). | | | Distribution | Prograde metamorphic assemblages and tectonic fabrics related to the D2e event in the Gascoyne Province are developed in metasedimentary and meta-igneous rocks in the Nardoo Hills region on southern MOUNT PHILLIPS and adjacent northern YINNETHARRA. | | | Description | In the Nardoo Hills area along the northern edge of the Mutherbukin Zone, the first of the pervasive events attributed to the Edmundian Orogeny, D2e, produced a strong foliation associated with greenschist to amphibolite facies metamorphism (M2e:M1 of Williams et al., 1983; Culver, 2001; Varvell, 2001). This area preserves an M2e metamorphic gradient ranging from amphibolite facies in the south to lower greenschist facies in the north adjacent to the Ti Tree Syncline. Pelitic schist of the Leake Spring Metamorphics in the southern part of the Nardoo Hills area contains black staurolite and scattered dark red–brown garnet porphyroblasts, which are enclosed by a strong composite fabric (S1e/S2e) and locally have remnants of S1e in pressure shadows and inclusion tails. A prominent mineral lineation (L2e) is defined mainly by the alignment of 1–2 mm long staurolite crystals. Interlayered amphibolite is fine grained and compositionally homogeneous with a strong foliation and a weak mineral lineation.
The southern margin of the Mutherbukin Zone in the Nardoo Well area is marked by a distinctive, foliated marine quartzite (P_-POs-mtqs), the Spring Camp Formation of the Pooranoo Metamorphics. The quartzite has a strong planar foliation (S1e/S2e) dipping to the south-southwest at 30–40°, and a prominent lineation (L2e). The lineation is similar in orientation to the mineral lineation in the pelitic schists to the north, but the foliation dips more shallowly to the south approaching the southern margin of the Pooranoo Metamorphics. The latter unit is interpreted to be in sheared contact with leucocratic granites of the Moorarie Supersuite. Much of the Pooranoo Metamorphics in the Nardoo Hills area comprises biotite–quartz–muscovite schist and quartz–muscovite–biotite schist (P_-POb-mlsm) of the Biddenew Formation, in which the S1e/S2e schistosity is crumpled by a moderately to steeply north-dipping crenulation cleavage. In low-grade areas of the Nardoo belt, near the Ti Tree Syncline, the Pooranoo Metamorphics are typically fine-grained rocks comprising mainly slate and phyllite. The rocks have a pervasive cleavage (S3e), which is axial planar to kilometre-scale folds in the Pooranoo and Leake Spring Metamorphics, and broadly parallel to structures in low-grade Edmund Group rocks within the Ti Tree Syncline.
Sheared leucogranite of the Moorarie Supersuite (Stop B11d of Martin et al., 2007; Zone 50, MGA 408838E 7293140N) contains sparse porphyroclasts of K-feldspar up to 4 mm, and in some areas, pegmatite veins that are boudinaged and isoclinally folded (F2e). The foliation in the monzogranite dips moderately or steeply to the south, parallel to the S1e/S2e fabric in the Pooranoo Metamorphics farther to the north, and is folded about an isoclinal F3e fold. In the sheet-like monzogranite there is a trend of increasing grain size and decreasing strain to the south and west, away from the contact with the Pooranoo Metamorphics. The combination of the southward increase in metamorphic grade in the Pooranoo Metamorphics, the dominance of D2e structures in this zone, and the south to south-southwest dip of the foliation, suggests that the contact between the monzogranite and the Pooranoo Metamorphics was a zone of uplift during D2e.
Rocks of middle-amphibolite facies are abundant in the northern part of the Mutherbukin Zone and contain a staurolite–biotite–muscovite–quartz assemblage (e.g. GSWA 180911, 191977), or a staurolite–plagioclase–biotite–muscovite–quartz assemblage (e.g GSWA 180918). The schists also contain lesser amounts of apatite, tourmaline, Fe–Ti oxide minerals, chlorite, zircon, xenotime, monazite, and barite. The schists have a strong composite S1e/S2e fabric, which is defined by the alignment of quartz, muscovite, biotite, and Fe–Ti oxide minerals, and quartz-rich and mica-rich domains. The pelites all contain coarse porphyroblasts of biotite and staurolite that overprint S1e and are enclosed by S2e. The biotite contains abundant pleochroic haloes, produced by inclusions of zircon, monazite, and xenotime. One of the most distinctive assemblages in the Nardoo Hills area is a staurolite–garnet–biotite–muscovite(–andalusite) schist. Staurolite porphyroblasts (4–6 cm long) are not uncommon in the area to the north and northwest of Morrissey Hill on southern MOUNT PHILLIPS and northern YINNETHARRA. However, towards Reid Well on northeastern YINNETHARRA, the rocks become finer grained with fewer large staurolite and garnet porphyroblasts. Some of the staurolite–garnet–biotite–muscovite(–andalusite) schists contain two generations of staurolite: large porphyroblasts and smaller crystals that define a lineation. Staurolite porphyroblasts commonly overprint an S1e/S2e schistosity. Inclusion trails show that porphyroblast growth post-dated both an early S1e foliation and some rotation of that foliation near porphyroblast margins, suggesting that growth may be late synkinematic with S2e. Amphibolites are interleaved with the metasedimentary rocks.
Greenschist facies pelites contain the assemblages biotite–plagioclase–chlorite–muscovite–quartz (GSWA 191970) or muscovite–quartz–chlorite (GSWA 191975). The dominant foliation (S2e) is defined by parallel muscovite, chlorite, and Fe–Ti oxide minerals, and mica-rich and quartz-rich bands. The S2 fabric has undergone folding and the development of a weak crenulation cleavage (S3e). Samples also contain minor amounts of Fe–Ti oxide minerals, Fe oxide minerals, zircon, xenotime and apatite. Monazite is absent from greenschist facies samples, which is consistent with previous studies that have found that monazite appears at the staurolite isograd in prograde pelites (e.g. Smith and Barreiro, 1990; Kingsbury et al., 1993; Spear and Pyle, 2002; Wing et al., 2003).
The presence of andalusite and cordierite in amphibolite facies pelites in the Leake Spring Metamorphics and Pooranoo Metamorphics was used originally to infer high-temperature and low-pressure conditions within the belt (Williams et al., 1983; Williams, 1986). However, the subsequent identification of kyanite in amphibolite facies assemblages (kyanite–staurolite–biotite–quartz–muscovite [CV063] and kyanite–chlorite–plagioclase–biotite–quartz–muscovite [CV064] schists) from two localities in the Nardoo Hills belt was used to infer a Barrovian thermal regime (600–700°C and 8–9 kbar; Varvell, 2001; Varvell et al., 2003; Fitzsimons et al., 2004). Based on these estimates, it was argued that metamorphism involved burial to depths of 30 km and intense north-northwesterly to south-southeasterly shortening, during continent–continent collision (Fitzsimons et al., 2004).
We have re-examined thin sections from the two samples containing what was interpreted to be kyanite (CV063 and CV064; Fig. 12; Varvell, 2001). The comparatively low relief and low birefringence of the mineral in question, combined with its length-fast optical orientation, are indicative of andalusite (Deer et al., 1985). X-ray diffraction analysis of the same mineral in samples of the Morrissey Metamorphics (GSWA 46981) and Pooranoo Metamorphics (Y65; Trautman, 1992) 5 km along strike from, and 2.5 km north of, respectively, the reported kyanite-bearing samples (CV063 and CV064) confirms that the stable Al2SiO5 polymorph is andalusite (R Clarke, pers. comm., 2006, 2007). The widespread presence of andalusite and the absence of kyanite in these samples is consistent with earlier observations (e.g. Williams et al., 1983; Williams, 1986), and indicates that peak regional metamorphism reached temperatures of 500–550° C and pressures of 3–4 kbar.
On central southern PINK HILLS, metasedimentary rocks of the Edmund Group and mafic intrusives of the Narimbunna Dolerite have been metamorphosed and deformed in the lower to middle amphibolite facies, with the widespread production of andalusite and garnet porphyroblasts within pelitic lithologies. These rocks form part of a regional-scale tight to isoclinal syncline, presumably formed during either the D2e or D3e event. The presence of andalusite rather than staurolite, as is prominent within similar rocks in the Nardoo Hills area, suggests that M2e metamorphism peaked at slightly lower pressures and temperatures than those in the Nardoo Hills area. The dominant pelitic rocks contain abundant 1–10 mm long andalusite and 1–5 mm diameter garnet porphyroblasts set within a matrix of muscovite and quartz. The andalusite porphyroblasts commonly grow in random orientations within the main S2e foliation. The relation of garnet porphyroblasts to this fabric is more equivocal as they commonly overgrow this fabric, but are also locally wrapped by it. Associated dolerite sills contain an amphibolite facies assemblage of hornblende–plagioclase–epidote. Peak metamorphic conditions constrained by the andalusite–garnet bearing pelites is <550°C and <3 kbar. | | | | | | Geochronology | | | Edmundian Orogeny D2e/M2e | Maximum age | Minimum age | Age (Ma) | 1026 ± 12 | 995 ± 6 | Age | Mesoproterozoic | Neoproterozoic | Age data type | Isotopic | | References | | |
| Five samples of schist were collected from the Pooranoo and Leake Spring Metamorphics in the Nardoo Well area of the central Gascoyne Province (GSWA 180911, 180918, 191970, 191975, 191977) for SHRIMP U–Pb dating of monazite and xenotime in thin sections (Sheppard et al., 2007). Monazite is widespread in all three samples of the staurolite-bearing schists (GSWA 180918, 180911, 191977) where it typically occurs in the matrix as idioblastic crystals oriented parallel to the main fabric, S1e/S2e. Monazite crystals are also present as inclusions aligned with S1e in staurolite and biotite porphyroblasts that overprint the matrix. In places, monazite crystals contain inclusions of Fe–Ti oxide minerals, quartz, and muscovite that are aligned parallel to S1e/S2e, suggesting that monazite grew with these minerals during deformation. Xenotime crystals are found in all of the metapelitic schists (GSWA 180918, 180911, 191977) but are less abundant and smaller than monazite. Xenotime is typically subidioblastic and equant, although elongate crystals are aligned with S1e/S2e. Xenotime occurs in the matrix and as inclusions within large overprinting staurolite and biotite porphyroblasts.
The oldest and youngest dates obtained were 1026 ± 12 Ma (GSWA 180911, monazite) and 995 ± 6 Ma (GSWA 180918, xenotime) thus providing the maximum and minimum age constraints for D2e (Sheppard et al., 2007), respectively. Additional dates were: 1005 ± 10 Ma (GSWA 180918, monazite), 1004 ± 8 Ma (GSWA 191977, monazite), 998 ± 8 Ma (GSWA 191970, xenotime) (Sheppard et al., 2007).
In the central part of the Mutherbukin Zone on YINNETHARRA, small leucocratic melt pockets are widely developed in granitic rocks of the Durlacher and Moorarie Supersuites. Small leucocratic melt pockets (GSWA 185945) that cut the gneissic fabric in the Davey Well Granite were sampled for SHRIMP U–Pb zircon geochronology. Concentrically zoned zircon cores yield a concordia age of 1648 ± 6 Ma, interpreted as the age of magmatic crystallization of the monzogranite (Wingate et al., 2010). High-U rims with low Th/U ratios (≤0.05) yield a concordia age of 1000 ± 8 Ma, interpreted as the age of magmatic crystallization of the pegmatite (Wingate et al., 2010). This date also provides a minimum age for the gneissic fabric in the Davey Well Granite. This date is within the uncertainty of most of the U–Pb dates on monazite and xenotime in thin sections of the metasedimentary rocks. | | | Tectonic Setting | Some previous studies attributed the Edmundian Orogeny to far-field reactivation of the Capricorn Orogen during the break up of Rodinia (Powell et al., 1994) and the assembly of Gondwana (Fitzsimons, 2003). In contrast, Myers et al. (1996) suggested that the Edmundian Orogeny resulted from the collision of the North and West Australian Cratons between c. 1300 and c. 1100 Ma. However, dolerite sills dated at c. 1070 Ma (Wingate, 2002) that intrude the Edmund and Collier Groups are also deformed into easterly trending folds. More recent advances in understanding the amalgamation history of the Rodinia supercontinent indicate that the collision of the eastern margin of Australia with Laurentia occurred at c. 1000 Ma (Li et al., 2008 and references therein), a time coincident with the Edmundian Orogeny recorded here in the West Australian Craton. In most Rodinia reconstructions (i.e. Pisarevsky et al., 2003; Li et al,., 2008) the western margin of the West Australian Craton faces an open ocean, so if these configurations are correct, the Edmundian Orogeny must be a response to far-field plate stresses related to Rodinia assembly along the eastern margin of Australia. However, it is possible that the Edmundian Orogeny formed in response to plate collision/accretion along the western margin of the West Australian Craton and that current models of Rodinia are incomplete (Johnson, 2013). Uplift of the southern Capricorn Orogen between c. 950 and c. 850 Ma (Occhipinti, 2004, 2007) has been linked to collision of the Kalahari Craton with the western margin of Australia along the Pinjarra Orogen (Occhipinti, 2004). The Northampton and Mullingarra Inliers in the Pinjarra Orogen are interpreted to be allochthonous terranes, derived from the Albany Fraser Belt (Ksienzyk et al., 2007, 2012) that were metamorphosed at granulite and amphibolite facies, respectively at c. 1080 Ma, and intruded by granites at c. 1070 Ma. The inliers were thought to have been emplaced in their present position relative to the Yilgarn Craton in the Neoproterozoic (Fitzsimons, 2003) although, because they contain undeformed dolerites of the Mundine Well Dolerite, emplacement must have occurred prior to dolerite intrusion at c. 755 Ma. The metamorphism in the central Gascoyne Province is a minimum of 40 Ma younger than that in the Northampton Inlier. However, a pegmatite from the Northampton Inlier has been dated at 989 ± 2 Ma (Bruguier et al., 1999), suggesting that there could be other tectonothermal events in the Pinjarra Orogen coeval with the metamorphism and magmatism dated here (see also Ksienzyk et al., 2007). A comparison of the age of detrital zircons from metasedimentary rocks of the Northampton Inlier with similar, possibly correlative packages from the Maud Belt of Antarctica, reveals different ages suggesting that the Kalahari Craton – West Australian Craton association may not be valid (Ksienzyk et al., 2007). | | | | References | Bruguier, O, Bosch, D, Pidgeon, RT, Byrne, DI and Harris, LB 1999, U-Pb chronology of the Northampton Complex, Western Australia - evidence for Grenvillian sedimentation, metamorphism and deformation and geodynamic implications: Contributions to Mineralogy and Petrology, v. 136, p. 258–272. | Culver, KE 2001, Structure, metamorphism and geochronology of the northern margin of the Gurun Gutta Granite, Central Gascoyne Complex, Western Australia: Curtin University of Technology, Perth, Western Australia, BSc (Hons) thesis (unpublished), 126p. | Deer, WA, Howie, RA and Zussman, J 1985, An introduction to the rock forming minerals: Longman Group Limited, Harlow, England, 528p. | Fitzsimons, ICW 2003, Proterozoic basement provinces of southern and southwestern Australia, and their correlation with Antarctica: Geological Society, London, Special Publications, v. 206, p. 93–130. | Fitzsimons, ICW, Varvell, CA and Culver, KE 2004, Kyanite-chlorite and staurolite-garnet schists of the Gascoyne Complex: Barrovian thermal gradients during Palaeoproterozoic orogenesis in Western Australia, in Dynamic Earth: past, present and future edited by McPhie, Jocelyn and McGoldrick, P: 17th Australian Geological Convention, Hobart, Tasmania, 2004/02/08: Geological Society of Australia, Sydney, New South Wales; GSA Abstracts no. 73, p. 157. | Johnson, SP 2013, The birth of supercontinents and the Proterozoic assembly of Western Australia: Geological Survey of Western Australia, Perth, Western Australia, 78p. View Reference | Kingsbury, JA, Miller, CF, Wooden, JL and Harrison, TM 1993, Monazite paragenesis and U-Pb systematics in rocks of the eastern Mojave Desert, California: Chemical Geology, v. 110, p. 147–167. | Ksienzyk, AK, Jacobs, J, Boger, SD, Kosler, J, Sircombe, KN and Whitehouse, MJ 2012, U-Pb ages of metamorphic monazite and zircon from the Northampton Complex: Evidence of two orogenic cycles in Western Australia: Precambrian Research, v. 198–199, p. 37–50. | Ksienzyk, AK, Jacobs, J, Kosler, J and Sircombe, KN 2007, A comparative provenance study of the late Mesoproterozoic Maud Belt (East Antarctica) and the Pinjarra Orogen (Western Australia): Implications for a possible Mesoproterozoic Kalahari-Western Australia connection, in Antarctica: a keystone in a changing world - online proceedings of the 10th international symposium on Antarctic earth sciences edited by Cooper, Alan and Raymond, C, Santa Barbara, California, USA, 26 August - 1 September 2007; USGS Open-File Report 2007–1047. | Li, ZX, Bogdanova, SV, Collins, AS, Davidson, A, Waele, B, Ernst, RE, Fitzsimons, ICW, Fuck, RA, Gladkochub, DP, Jacobs, J, Karlstrom, KE, Lu, S, Natapov, LM, Pease, V, Pisarevsky, SA, Thrane, K and Vernikovsky, V 2008, Assembly, configuration, and break-up history of Rodinia: A synthesis: Precambrian Research, v. 160, no. 1–2, p. 179–210, doi:10.1016/j.precamres.2007.04.021. | Martin, DMcB, Sheppard, S, Thorne, AM, Farrell, TR and Groenewald, PB 2007, Proterozoic geology of the western Capricorn Orogen — a field guide: Geological Survey of Western Australia, Record 2006/18, 43p. View Reference | Myers, JS, Shaw, RD and Tyler, IM 1996, Tectonic evolution of Proterozoic Australia: Tectonics, v. 15, p. 1431–1446. | Occhipinti, SA 2004, Tectonic evolution of the southern Capricorn Orogen, Western Australia: Curtin University of Technology, Perth, Western Australia, PhD thesis (unpublished), 220p. | Occhipinti, SA 2007, Neoproterozoic reworking in the Paleoproterozoic Capricorn Orogen: Evidence from ⁴⁰Ar/³⁹Ar ages: Geological Survey of Western Australia, Record 2007/10, 41p. View Reference | Pisarevsky, SA, Wingate, MTD, Powell, CMcA, Johnson, SP and Evans, DAD 2003, Models of Rodinia assembly and fragmentation: Geological Society, London, Special Publications, v. 206, no. 1, p. 35–55, doi:10.1144/GSL.SP.2003.206.01.04. | Powell, CMcA, Preiss, WV, Gatehouse, CG, Krapež, B and Li, ZX 1994, South Australian record of a Rodinian epicontinental basin and its mid-Neoproterozoic breakup (~700 Ma) to form the Palaeo-Pacific Ocean: Tectonophysics, v. 237, p. 113–140. | Sheppard, S, Occhipinti, SA and Nelson, DR 2005, Intracontinental reworking in the Capricorn Orogen, Western Australia: The 1680–1620 Ma Mangaroon orogeny: Australian Journal of Earth Sciences, v. 52, p. 443–460, doi:10.1080/08120090500134589. | Sheppard, S, Rasmussen, B, Muhling, JR, Farrell, TR and Fletcher, IR 2007, Grenvillian-aged orogenesis in the Palaeoproterozoic Gascoyne Complex, Western Australia: 1030–950 Ma reworking of the Proterozoic Capricorn Orogen: Journal of Metamorphic Geology, v. 25, p. 477–494. | Smith, HA and Barreiro, B 1990, Monazite U-Pb dating of staurolite grade metamorphism in pelitic schists: Contributions to Mineralogy and Petrology, v. 105, p. 602–615. | Spear, FS and Pyle, JM 2002, Apatite, monazite, and xenotime in metamorphic rocks, in Phosphates: geochemical, geobiological and materials importance edited by Kohn, MJ, Rakovan, J and Hughes, JM: Mineralogical Society of America, Washington D.C., USA, Reviews in Mineralogy and Geochemistry vol. 48, no. 1, p. 293–335. | Trautman, RL 1992, The mineralogy of the rare-element pegmatites of the Yinnetharra pegmatite belt, Gascoyne Province, Western Australia: The University of Western Australia, Perth, Western Australia, BSc (Hons) thesis (unpublished). | Varvell, CA 2001, Age, structure and metamorphism of a section of the Morrissey Metamorphic Suite, Central Gascoyne Complex, Western Australia: Curtin University of Technology, Perth, Western Australia, BSc (Hons) thesis (unpublished), 209p. | Varvell, CA, Culver, KE and Fitzsimons, ICW 2003, Structure, metamorphism and SHRIMP U-Pb geochronology of the central Gascoyne Complex, Western Australia, in Abstracts edited by Reddy, S, Fitzsimons, ICW and Collins, AS, Kalbarri, Western Australia: Geological Society of Australia; SGTSG Field Meeting, p. 56. | Williams, SJ 1986, Geology of the Gascoyne Province, Western Australia: Geological Survey of Western Australia, Report 15, 85p. View Reference | Williams, SJ, Williams, IR, Chin, RJ, Muhling, PC and Hocking, RM (compilers) 1983, Mount Phillips, Western Australia: Geological Survey of Western Australia, 1:250 000 Geological Series Explanatory Notes, 29p. View Reference | Wingate, MTD 2002, Age and palaeomagnetism of dolerite sills of the Bangemall Supergroup on the Edmund 1:250 000 sheet, Western Australia: Geological Survey of Western Australia, Record 2002/4, 48p. View Reference | Wingate, MTD, Kirkland, CL, Sheppard, S and Johnson, SP 2010, 185945.1: pegmatite lenses in metamonzogranite, Yinnetharra Homestead; Geochronology Record 901: Geological Survey of Western Australia, <www.dmpe.wa.gov.au/geochron>. View Reference | Wing, BA, Ferry, JM and Harrison, TM 2003, Prograde destruction and formation of monazite and allanite during contact and regional metamorphism of pelites: Petrology and geochronology: Contributions to Mineralogy and Petrology, v. 145, p. 228–250. |
| | | | Recommended reference for this publication | Sheppard, S, Johnson, SP, Korhonen, FJ and Wingate, MTD 2022, Edmundian Orogeny D2e/M2e (CED2): Geological Survey of Western Australia, WA Geology Online, Explanatory Notes extract, viewed 05 August 2025. <www.dmp.wa.gov.au/ens> |
| | | This page was last modified on 09 March 2022. | | | | | Grid references in this publication refer to the Geocentric Datum of Australia 1994 (GDA94). Locations mentioned in the text are referenced using Map Grid Australia (MGA) coordinates, Zones 49 to 52. All locations are quoted to at least the nearest 100 m. Capitalized names in text refer to standard 1:100 000 map sheets, unless otherwise indicated. WAROX is GSWA’s field observation and sample database. WAROX site IDs have the format ‘ABCXXXnnnnnnSS’, where ABC = geologist username, XXX = project or map code, nnnnnn = 6 digit site number, and SS = optional alphabetic suffix (maximum 2 characters). All isotopic dates are based on U–Pb analysis of zircon and quoted with 95% uncertainties, unless stated otherwise. U–Pb measurements of GSWA samples were conducted using a sensitive high-resolution ion microprobe (SHRIMP) in the John de Laeter Centre at Curtin University, Perth, Western Australia. Digital data related to WA Geology Online, including geochronology and digital geology, are available online at the Department’s Data and Software Centre and may be viewed in map context at GeoVIEW.WA. | | | Further details of geological publications and maps produced by the Geological Survey of Western Australia are available from: Information Centre Department of Mines, Industry Regulation and Safety 100 Plain Street EAST PERTH, WA 6004 Telephone: +61 8 9222 3459 Facsimile: +61 8 9222 3444 |
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