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| | | | AH Hickman | | | | | Event type | deformation: undivided | Parent event | | Child events | | Tectonic units affected | | Tectonic setting | orogen: undivided | Metamorphic facies | | Metamorphic/tectonic features | faulted; cataclastic; folded; lineated; sheared |
| | | Summary | The 3325–3290 Ma Emu Pool Event was an event of deformation, granitic intrusion (3324–3290 Ma Emu Pool Supersuite), and felsic volcanism (3325–3315 Ma Wyman Formation) in the East Pilbara Terrane of the Pilbara Craton. The event took place during the evolution of a mantle plume that initially resulted in the widespread eruption of the c. 3350–3335 Ma Euro Basalt (komatiite, komatiitic basalt and tholeiite). The Euro Basalt, Wyman Formation and an overlying formation, the Charteris Basalt, make up the 6–10 km thick Kelly Group. In terms of the origin of the Emu Pool Event, an important observation is that while the Euro Basalt was erupted across the entire area of the East Pilbara Terrane, the Wyman Formation and Emu Pool Supersuite were restricted to the eastern half of the terrane. The western boundaries of these felsic units are abrupt and coincide with the Coongan – Warralong Fault Zone. This fault zone is interpreted to have originated as a c. 3325 Ma rift fault along the previously faulted western margins of the Muccan, Mount Edgar and Corunna Downs Domes (Hickman, 2021). These domes, and three others to the east, were tectonically and magmatically active during the Emu Pool Event, while all five domes to the west show no evidence of 3325–3290 Ma activity. The distribution of the Emu Pool Supersuite, restricted to the eastern domes, suggests crustal thickening in the eastern East Pilbara Terrane that influenced subsequent rifting of the crust farther to the west (3280–3176 Ma East Pilbara Terrane Rifting Event).
The first phase of deformation during the Emu Pool Event (PCE1) involved folding of the Euro Basalt prior to eruption of the Wyman Formation, resulting in local angular unconformities between the formations. PCE1 was followed by major diapiric uplift of the eastern domes at c. 3315 Ma that was accompanied by granitic intrusion and vertical shearing of granite–greenstone contacts (PCE2). Metamorphism during PCE2 reached amphibolite facies. | | | Distribution | The Emu Pool Event (Hickman and Van Kranendonk, 2008) was restricted to six granite–greenstone domes in the eastern half of the East Pilbara Terrane (Muccan, Mount Edgar, Corunna Downs, Warralong, McPhee and Yilgalong Domes) on MUCCAN, COONGAN, WARRAWAGINE, MARBLE BAR, MOUNT EDGAR, SPLIT ROCK, NULLAGINE, YILGALONG and EASTERN CREEK. The event included intrusion of the Emu Pool Supersuite and eruption of the genetically related Wyman Formation. The limited distribution of these felsic units was first documented by Van Kranendonk et al. (2004). | | | Description | The Paleoarchean crustal evolution of the 3530–3223 Ma East Pilbara Terrane took place through diapiric doming and sagduction (Hickman, 1975, 1981, 1983, 1984; Collins, 1989; Williams and Collins, 1990), also referred to as 'partial convective overturn' (Collins et al., 1998; Van Kranendonk, 1998 2000; Van Kranendonk et al., 2002, 2004b, 2006, 2007a,b; Hickman, 2004; Hickman and Van Kranendonk, 2004). The 3325–3290 Ma Emu Pool Event (PCE), which involved diapiric deformation, metamorphism, granitic intrusion (Emu Pool Supersuite) and felsic volcanism (Wyman Formation) occupied a relatively short stage in the 300 Ma tectonic history of the terrane.
The East Pilbara Terrane is composed of eleven granite–greenstone domes separated by vertical boundary faults (Van Kranendonk, 1998 Hickman, 2001; Van Kranendonk et al., 2002, 2006; Hickman and Van Kranendonk, 2004). Stratigraphic variations across the terrane reveal that the individual domes evolved at slightly different times and with different rates and magnitudes of uplift (Hickman, 1984, 2001, 2021; Hickman and Van Kranendonk, 2004). Consequently, the tectonic histories of the individual domes differ slightly with respect to the timing of events of deformation, metamorphism, and related granitic intrusion and volcanic activity. Doming was accompanied by granitic intrusion into the dome cores (Collins et al., 1998; Hickman and Van Kranendonk, 2004), so that the granite geochronology indicates the timing of the main diapiric uplift in any particular dome. An example of regional differences in the timing of doming is provided by geochronology on the Emu Pool Supersuite. Geochronology on this supersuite in the Mount Edgar and Corunna Downs Domes indicates that most granitic intrusion took place between 3320 and 3300 Ma (Collins et al., 1998; Van Kranendonk et al., 2002, 2006; Hickman, 2021). However, in the Yilgalong Dome (EASTERN CREEK and YILGALONG) the supersuite intruded between 3299 and 3290 Ma (Williams, 2007).
The Emu Pool Event interrupted the volcanic eruption of the 3350–3290 Ma Kelly Group. The almost entirely volcanic succession of this group was produced by a mantle plume event (Van Kranendonk et al., 2002, 2006, 2007a,b; Hickman, 2004; Smithies et al., 2005). The 6–10 km-thick stratigraphy of the Kelly Group consists of three formations, which in ascending stratigraphic order are: 1), the 3350–3335 Ma Euro Basalt composed of komatiite, komatiitic basalt, and tholeiitic basalt; 2), the 3325–3315 Ma Wyman Formation, mainly composed of rhyolite lava and volcaniclastic rocks; and 3), the 3325–3315 Ma Charteris Basalt of similar composition to the Euro Basalt, although with only rare komatiite. The succession from komatiite at the base of the Euro Basalt to rhyolite in the Wyman Formation is interpreted to represent a single ultramafic–mafic–felsic volcanic cycle (Hickman, 2011). In older volcanic cycles of the East Pilbara Terrane, such as those of the Coongan and Salgash Subgroups, the basaltic section is conformably overlain by andesite and dacite, with rhyolite being minor and mainly confined to the top of the cycle. Vertical geochemical trends in the older cycles indicate derivation of felsic magma by fractional crystallization of basaltic magma (Barley, 1993; Cullers et al., 1993; Smithies et al., 2007), but there is no evidence of this in the Wyman Formation. The geochemistry of the Wyman Formation indicates magma derived by partial melting of older felsic crust (Barley and Pickard, 1999; Champion and Smithies, 2007; Bagas et al., 2003; Van Kranendonk et al., 2007a,b, 2019). By contrast, the geochemistry of the Euro Basalt indicates derivation of magma through partial melting of the mantle (Van Kranendonk et al., 2002, 2004a,b, 2006, 2007a,b, 2010; Hickman and Van Kranendonk, 2004; Smithies et al., 2005).
Erupted before the Emu Pool Event, the Euro Basalt was deposited across the entire area of the East Pilbara Terrane, whereas the Wyman Formation and the Emu Pool Supersuite are restricted to greenstone successions east of the northerly to southerly trending Coongan – Warralong Fault Zone (Hickman, 2021). The observation that this major fault zone forms the western limits of both the Wyman Formation and the Emu Pool Supersuite suggests a direct relationship to the Emu Pool Event. The maximum age of the structure is c. 3335 Ma, because it cuts across the Euro Basalt. Its minimum age is more difficult to define because major faults zones were commonly re-activated during subsequent deformation events. However, 40Ar/39Ar hornblende cooling ages in the Coongan greenstone belt between c. 3197 Ma (Zegers, 1996) and c. 3240 Ma (Davids et al., 1997) place a minimum age on the structure. These ⁴⁰Ar/³⁹Ar ages are most likely related to metamorphism during the 3280–3176 Ma East Pilbara Terrane Rifting Event, in which case they do not directly date the Coongan – Warralong Fault Zone. It is likely that the fault zone originated during the Emu Pool Event and that it was a major northerly to southerly trending crustal fracture. Its formation was apparently related to the doming process, because it links the faulted western boundaries of the Muccan, Mount Edgar and Corunna Downs Domes (Hickman, 2021). With the possible exception of the Corunna Downs Dome, these domes existed prior to the Emu Pool Event and had faulted contacts with adjacent domes. If intrusion of the Emu Pool Supersuite commenced in the eastern half of the East Pilbara Terrane, these three domes might have been re-activated before domes farther to the west. Given this scenario, the faulted western margins of the domes might have merged into an east-side-up fault zone. Substantial uplift (>10 km) of the eastern half of the East Pilbara Terrane relative to the west might have resulted in a structural or thermal barrier along the Coongan – Warralong Fault Zone that impeded later granitic intrusion farther west.
Two phases of deformation are recognized during the Emu Pool Event, although due to regional variations in the tectonic histories of individual domes any summary is inevitably a generalization. The first phase of deformation (PCE1) involved local folding of the Euro Basalt prior to eruption of the Wyman Formation. PCE1 was the fifth phase of deformation (D5) in the northern Pilbara Craton (Hickman, 2021). Erosion of the folded strata prior to deposition of the Wyman Formation resulted in local unconformities. The Wyman Formation unconformably overlies the Euro Basalt in the McPhee greenstone belt (Barley and Pickard, 1999) and also in the western Warralong greenstone belt (Van Kranendonk, 2004). In the southeastern Kelly greenstone belt there is an angular discordance of 20–30º between the formations, suggesting an unconformity (Van Kranendonk et al., 2002), although Bagas (2003) disputed the unconformity, preferring an interpretation that rhyolite flows of the Wyman Formation were inclined when erupted.
PCE1 was followed by PCE2 involving major diapiric uplift of the domes between c. 3325 and c. 3290 Ma. In the Mount Edgar Dome, the main uplift took place at c. 3315 Ma (Collins et al., 1998), and was accompanied by granitic intrusion and vertical shearing of granite–greenstone contacts (D6 in the regional deformation history of the northern Pilbara Craton). Diapiric uplift was concentrated in the granitic cores of the domes, whereas greenstones between the granites sank deep into the crust by gravity-driven sagduction (Collins et al., 1998; Hamilton, 2007; Bedard et al., 2013; Thébaud and Rey, 2013). In some instances, sagduction took greenstones close to the base of the crust, resulting in high-grade metamorphism (François et al., 2014). It is uncertain to what extent sagduction of the greenstone succession and of granitic rocks close to granite–greenstone contacts led to partial melting and generation of new magmas that were transported to the upper crust. Some granitic cores, such as that of the Mount Edgar Dome show a patterned granite age zonation with the youngest granites in the centres of the domes and the oldest granites along granite–greenstone contacts (Hickman and Van Kranendonk, 2004). This suggests that diapirism involved progressive outward displacement of older granites towards greenstone contacts, eventually followed by their sagduction along with the oldest greenstones. | | | | | | Geochronology | | | Emu Pool Event | Maximum age | Minimum age | Age (Ma) | 3325 | 3290 | Age | Paleoarchean | Paleoarchean | Age data type | Inferred | | References | | |
| Geochronology relating to the Emu Pool Event has been obtained from the Emu Pool Supersuite and the Wyman Formation. The maximum age of the event is constrained by the youngest date on the Euro Basalt that was locally deformed by the first deformation of the event, PCE1. The undated Charteris Basalt, overlying the Wyman Formation, might represent the basal section of a later volcanic cycle (Hickman, 2011).
The minimum age of the Euro Basalt is indicated by a date of 3335 ± 7 Ma (GSWA 168999, Nelson, 2004) on detrital zircons in a thin quartzite unit within felsic volcaniclastic rocks in the southwestern Kelly greenstone belt. The maximum age of the Emu Pool Supersuite is constrained by a date of 3324 ± 4 Ma on the Boobina Porphyry (McNaughton et al., 1993). A date of 3324 ± 4 Ma was obtained on the Wilina Granodiorite (Collins et al., 1998), although analytical details were not provided. The c. 3324 Ma date accords well with the maximum age of the Wyman Formation at c. 3325 Ma, which is genetically related to the Emu Pool Supersuite. The minimum age of the supersuite is c. 3290 Ma, defined by the youngest date of 3290 ± 4 Ma (GSWA 169263, Nelson, 2005) obtained on the Elsie Creek Tonalite (A-EMel-mgtn) of the Yilgalong Granitic Complex (YILGALONG and EASTERN CREEK). The maximum depositional age of the Wyman Formation is well defined at c. 3325 Ma based on several dates on rhyolite (Thorpe et al., 1992; McNaughton et al., 1993). The minimum depositional age is provided by two dates of 3315 ± 3 Ma on rhyolite of the Wyman Formation (GSWA 144681, Nelson, 2002; sample 94003, Buick et al., 2002).
| | | Tectonic Setting | The Emu Pool Event took place within the intracontinental setting of the East Pilbara Terrane mid-way through its 3530 to 3220 Ma evolution as a continental volcanic plateau (Van Kranendonk et al., 2002; Hickman, 2004, 2012, 2021; Hickman and Van Kranendonk, 2004). The tectonic history of the plateau was dominated by diapiric doming and sagduction in response to a succession of mantle plumes. The plume responsible for the Emu Pool Event first impacted the terrane at c. 3350 Ma when it melted the Paleoarchean mantle to generate ultramafic and mafic magmas that erupted to deposit the 4 to 9 km-thick Euro Basalt in the lower part of the Kelly Group. The Euro Basalt was erupted across the entire East Pilbara Terrane, which, allowing for present partial concealment by Neoarchean formations, still has a preserved an area of at least 100 000 km². Strong stratigraphic and geochronological similarities between successions of the Pilbara and Kaapvaal Cratons at this time (Hickman, 2012, 2021) suggest that the Euro Basalt is equivalent to the volcanic part of the Kromberg Formation of the Onverwacht Group. In this case ultramafic and mafic volcanism from the plume is likely to have extended across up to 1 000 000 km² of the Pilbara–Kaapvaal continental crust (Hickman, 2021).
Volcanic eruption of the Kelly Group was interrupted by folding and uplift between 3335 and 3325 Ma, marking the beginning of the Emu Pool Event. In the Kaapvaal Craton, a rifting event followed final deposition of the Kromberg Formation at c. 3334 Ma (Byerly et al., 2019) and the Emu Pool Event also included faulting. One interpretation is that by c. 3325 Ma crustal extension above the mantle plume was affecting a very large area of continental crust. In the East Pilbara Terrane, crustal uplift took the form of diapiric doming with contemporaneous intrusion of granodiorite and monzogranite intrusions of the Emu Pool Supersuite. However, doming and granitic intrusion were restricted to the eastern half of the terrane, east of the Coongan – Warralong Fault Zone, which might have been a rift zone. An alternative interpretation of the Coongan – Warralong Fault Zone would be that it includes a large amount of strike-slip movement that juxtaposed an area of doming and granitic intrusion with an area lacking significant c. 3315 Ma doming or granitic intrusion. However, an objection to such major strike-slip movement during or after the Emu Pool Event is that there are no visible displacements of older units of the terrane, such as the Strelley Pool Formation, the Duffer Formation and the Talga Talga Subgroup.
Geochemical evidence that the Euro Basalt was derived by plume melting of mantle material, whereas the Emu Pool Supersuite and Wyman Formation were derived by melting of older felsic crust, indicates that the plume-related melting moved from the mantle to the crust at c. 3325 Ma. A very similar change took place during the subsequent mantle plume event that was responsible for eruption of the 3280–3235 Ma Sulphur Springs Group and intrusion of the Cleland Supersuite. That plume event resulted in rifting and continental breakup of the East Pilbara Terrane. The analogy suggests that the Coongan – Warralong Fault Zone probably represents a failed intracontinental rift, although it was different from plate tectonic rifting in that it involved displacements along the margins of diapiric domes. | | | | References | Bagas, L 2003, Stratigraphic revision of the Warrawoona and Gorge Creek Groups in the Kelly greenstone belt, Pilbara Craton, Western Australia, in Geological Survey of Western Australia annual review 2001–02 edited by Day, L and Reddy, DP: Geological Survey of Western Australia, Perth, p. 53–60. View Reference | Bagas, L, Smithies, RH and Champion, DC 2003, Geochemistry of the Corunna Downs Granitoid Complex, East Pilbara Granite-Greenstone Terrane, in Geological Survey of Western Australia annual review 2001–02 edited by Day, L and Reddy, DP: Geological Survey of Western Australia, Perth, p. 61–69. View Reference | Barley, ME 1993, Volcanic, sedimentary and tectonostratigraphic environments of the ~3.46 Ga Warrawoona Megasequence: A review: Precambrian Research, v. 60, no. 1–4, p. 47–67. | Barley, ME and Pickard, AL 1999, An extensive, crustally-derived, 3325 to 3310 Ma silicic volcanoplutonic suite in the eastern Pilbara Craton: Evidence from the Kelly Belt, McPhee Dome and Corunna Downs Batholith: Precambrian Research, v. 96, p. 41–62. | Bédard, JH, Harris, LB and Thurston, PC 2013, The hunting of the snArc: Precambrian Research, v. 229, p. 20–48. | Buick, R, Brauhart, CW, Morant, P, Thornett, JR, Maniw, JG, Archibald, NJ, Doepel, MG, Fletcher, IR, Pickard, AL, Smith, JB, Barley, ME, McNaughton, NJ and Groves, DI 2002, Geochronology and stratigraphic relationships of the Sulphur Springs Group and Strelley Granite: a temporally distinct igneous province in the Archean Pilbara Craton, Australia: Precambrian Research, v. 114, p. 87–120. | Byerly, GR, Lowe, DR and Heubeck, C 2019, Chapter 24 – Geologic evolution of the Barberton Greenstone Belt: A unique record of crustal development, surface processes, and early life 3.55–3.20 Ga, in Earth’s oldest rocks (2nd) edited by Van Kranendonk, MJ, Bennett, VC and Hoffmann, JE: Elsevier B.V., p. 569–613. | Champion, DC and Smithies, RH 2007, Geochemistry of Paleoarchean granites of the East Pilbara Terrane, Pilbara Craton, Western Australia: implications for early Archean crustal growth, in Earth's oldest rocks edited by Van Kranendonk, MJ, Bennett, VC and Smithies, RH: Elsevier B.V., Burlington, Massachusetts, USA, Developments in Precambrian Geology 15, p. 369–410. | Collins, WJ 1989, Polydiapirism of the Archean Mount Edgar batholith, Pilbara Block, Western Australia: Precambrian Research, v. 43, no. 1–2, p. 41–62. | Collins, WJ, Van Kranendonk, MJ and Teyssier, C 1998, Partial convective overturn of Archaean crust in the east Pilbara Craton, Western Australia: driving mechanisms and tectonic implications: Journal of Structural Geology, v. 20, no. 9–10, p. 1405–1424, doi:10.1016/S0191-8141(98)00073-X. | Cullers, RL, DiMarco, MJ, Lowe, DR and Stone, J 1993, Geochemistry of a silicified felsic volcanic suite from the early Archean Panorama Formation, Pilbara Block, Western Australia — an evaluation of depositional and post-depositional processes with special emphasis on the rare earth elements: Precambrian Research, v. 60, p. 99–116. | Davids, C, Wijbrans, JR and White, SH 1997, ⁴⁰Ar³⁹Ar laserprobe ages of metamorphic hornblendes from the Coongan Belt, Pilbara Western Australia: Precambrian Research, v. 83, no. 4, p. 221–242. | François, C, Philippot, P, Rey, PF and Rubatto, D 2014, Burial and exhumation during Archean sagduction in the east Pilbara granite–greenstone terrane: Earth and Planetary Science Letters, v. 396, p. 235–251. | Hamilton, WB 2007, Earth's first two billion years – the era of internally mobile crust, in 4-D framework of continental crust edited by Hatcher, RD, Carlson, MP, McBride, JH and Martinez Catalan, JR: Geological Society of America, Memoir 200, p. 233–296. | Hickman, AH 1975, Precambrian structural geology of part of the Pilbara Region, in Annual report for the year 1974: Geological Survey of Western Australia, p. 68–73. View Reference | Hickman, AH 1981, Crustal evolution of the Pilbara Block, in Archaean Geology: Second International Symposium, Perth 1980 edited by Glover, JE and Groves, DI: Geological Society of Australia, Special Publication 7, p. 57–69. | Hickman, AH 1983, Geology of the Pilbara Block and its environs: Geological Survey of Western Australia, Bulletin 127, 268p. View Reference | Hickman, AH 1984, Archaean diapirism in the Pilbara Block, Western Australia, in Precambrian tectonics illustrated edited by Kröner, A and Greiling, R: E. Schweizerbart'sche Verlagsbuchhandlung, Stuttgart, Germany Final report, p. 113–127. | Hickman, AH 2001, East Pilbara diapirism: New evidence from mapping, in GSWA 2001 extended abstracts: new geological data for WA explorers edited by Geological Survey of Western Australia: Geological Survey of Western Australia, Record 2001/5, p. 23–25. View Reference | Hickman, AH 2004, Two contrasting granite–greenstones terranes in the Pilbara Craton, Australia: Evidence for vertical and horizontal tectonic regimes prior to 2900 Ma: Precambrian Research, v. 131, p. 153–172. | Hickman, AH 2011, Pilbara Supergroup of the East Pilbara Terrane, Pilbara Craton: Updated lithostratigraphy and comments on the influence of vertical tectonics, in Geological Survey of Western Australia annual review 2009–10 edited by Bower, R and Johnston, J: Geological Survey of Western Australia, p. 50–59. | Hickman, AH 2012, Review of the Pilbara Craton and Fortescue Basin, Western Australia: Crustal evolution providing environments for early life: Island Arc, v. 21, p. 1–31. | Hickman, AH 2021, East Pilbara Craton: a record of one billion years in the growth of Archean continental crust: Geological Survey of Western Australia, Report 143, 187p. View Reference | Hickman, AH and Van Kranendonk, MJ 2004, Diapiric processes in the formation of Archaean continental crust, east Pilbara granite–greenstone terrane, Australia, in The Precambrian Earth: tempos and events edited by Eriksson, PG, Altermann, W, Nelson, DR, Mueller, WU and Catuneanu, O: Elsevier, Amsterdam, The Netherlands, Developments in Precambrian Geology 12, p. 54–75. | Hickman, AH and Van Kranendonk, MJ 2008, Archean crustal evolution and mineralization of the northern Pilbara Craton — a field guide: Geological Survey of Western Australia, Record 2008/13, 79p. View Reference | McNaughton, NJ, Compston, W and Barley, ME 1993, Constraints on the age of the Warrawoona Group, eastern Pilbara Block, Western Australia: Precambrian Research, v. 60, p. 69–98. | Nelson, DR 2002, 144681.1: agglomeratic rhyolite, Baroona Hill; Geochronology Record 273: Geological Survey of Western Australia, <www.dmpe.wa.gov.au/geochron>. View Reference | Nelson, DR 2004, 168999.1: quartzite, Pethernurrina Spring; Geochronology Record 59: Geological Survey of Western Australia, <www.dmpe.wa.gov.au/geochron>. View Reference | Nelson, DR 2005, 169263.1: tonalite gneiss, Bullyarrie Well; Geochronology Record 572: Geological Survey of Western Australia, <www.dmpe.wa.gov.au/geochron>. View Reference | Smithies, RH, Champion, DC, Van Kranendonk, MJ and Hickman, AH 2007, Geochemistry of volcanic rocks of the northern Pilbara Craton, Western Australia: Geological Survey of Western Australia, Report 104, 47p. View Reference | Smithies, RH, Van Kranendonk, MJ and Champion, DC 2005, It started with a plume — early Archaean basaltic proto-continental crust: Earth and Planetary Science Letters, v. 238, no. 3–4, p. 284–297. | Thébaud, N and Rey, PF 2013, Archean gravity-driven tectonics on hot and flooded continents: controls on long-lived hydrothermal systems away from continental margins: Precambrian Research, v. 229, p. 93–104. | Thorpe, R, Hickman, AH, Davis, D, Morton, JGG and Trendall, AF 1992, U–Pb zircon geochronology of Archaean felsic units in the Marble Bar region, Pilbara Craton, Western Australia: Precambrian Research, v. 56, p. 169–189. | Van Kranendonk, MJ 1998, Litho-tectonic and structural components of the North Shaw 1:100 000 sheet, Archaean Pilbara Craton, in Geological Survey of Western Australia annual review 1997–98 edited by Johnston, JF and Nowak, IR: Geological Survey of Western Australia, Perth, p. 63–70. View Reference | Van Kranendonk, MJ 2000, Geology of the North Shaw 1:100 000 sheet: Geological Survey of Western Australia, 1:100 000 Geological Series Explanatory Notes, 86p. View Reference | Van Kranendonk, MJ 2004, Geology of the Carlindie 1:100 000 sheet: Geological Survey of Western Australia, 1:100 000 Geological Series Explanatory Notes, 45p. View Reference | Van Kranendonk, MJ, Collins, WJ, Hickman, AH and Pawley, MJ 2004b, Critical tests of vertical vs horizontal tectonic models for the Archean East Pilbara granite–greenstone terrane, Pilbara Craton, Western Australia: Precambrian Research, v. 131, no. 3, p. 173–211. | Van Kranendonk, MJ, Hickman, AH, Smithies, RH and Champion, DC 2007a, Paleoarchean development of a continental nucleus: the East Pilbara Terrane of the Pilbara Craton, Western Australia, in Earth's oldest rocks edited by Van Kranendonk, MJ, Bennett, VC and Smithies, RH: Elsevier B.V., Burlington, Massachusetts, USA, Developments in Precambrian Geology 15, p. 307–337. | Van Kranendonk, MJ, Hickman, AH, Smithies, RH, Nelson, DN and Pike, G 2002, Geology and tectonic evolution of the Archaean North Pilbara terrain, Pilbara Craton, Western Australia: Economic Geology, v. 97, p. 695–732, doi:10.2113/gsecongeo.97.4.695. | Van Kranendonk, MJ, Hickman, AH, Smithies, RH, Williams, IR, Bagas, L and Farrell, TR 2006, Revised lithostratigraphy of Archean supracrustal and intrusive rocks in the northern Pilbara Craton, Western Australia: Geological Survey of Western Australia, Record 2006/15, 57p. View Reference | Van Kranendonk, MJ, Smithies, RH and Champion, DC 2019, Chapter 19 – Paleoarchean development of a continental nucleus: the East Pilbara Terrane of the Pilbara Craton, Western Australia, in Earth’s oldest rocks (2nd) edited by Van Kranendonk, MJ, Bennett, VC and Hoffmann, JE: Elsevier B.V., p. 437–462. | Van Kranendonk, MJ, Smithies, RH, Hickman, AH, Bagas, L, Williams, IR and Farrell, TR 2004a, Event stratigraphy applied to 700 million years of Archean crustal evolution, Pilbara Craton, Western Australia, in Geological Survey of Western Australia Annual Review 2003–04 edited by Geological Survey of Western Australia, Perth, Western Australia, p. 49–61. View Reference | Van Kranendonk, MJ, Smithies, RH, Hickman, AH and Champion, DC 2007b, Secular tectonic evolution of Archaean continental crust: Interplay between horizontal and vertical processes: Terra Nova, v. 19, p. 1–38. | Van Kranendonk, MJ, Smithies, RH, Hickman, AH, Wingate, MTD and Bodorkos, S 2010, Evidence for Mesoarchean (~3.2 Ga) rifting of the Pilbara Craton: The missing link in an early Precambrian Wilson cycle: Precambrian Research, v. 177, no. 1–2, p. 145–161, doi:10.1016/j.precamres.2009.11.007. | Williams, IR 2007, Geology of the Yilgalong 1:100 000 sheet: Geological Survey of Western Australia, 1:100 000 Geological Series Explanatory Notes, 45p. View Reference | Williams, IS and Collins, WJ 1990, Granite–greenstone terranes in the Pilbara Block, Australia, as coeval volcano-plutonic complexes: evidence from U–Pb zircon dating of the Mount Edgar batholith: Earth and Planetary Science Letters, v. 97, no. 1–2, p. 41–53, doi:10.1016/0012-821X(90)90097-H. | Zegers, TE 1996, Structural, kinematic, and metallogenic evolution of selected domains of the Pilbara granite–greenstone terrain: Geologica Ultraiectina, Utrecht University, Utrecht, the Netherlands, PhD thesis (unpublished), 208p. |
| | | | Recommended reference for this publication | Hickman, AH 2024, Emu Pool Event (PCE): 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 05 March 2024. | | | | | 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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