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| | | | HM Howard, R Quentin de Gromard, RH Smithies, and PW Haines | | | | | Event type | tectonic: undivided | Parent event | _Top of Event list | Child events | | Tectonic units affected | | Tectonic setting | orogen: intracratonic orogen | Metamorphic facies | | epidote-amphibolite: garnet | prehnite-pumpellyite: undivided | amphibolite: green hornblende |
| Metamorphic/tectonic features | granofelsic; augen; layered; granoblastic |
| | | Summary | The Giles Event records the evolution of a failed intracontinental rift, the Ngaanyatjarra Rift. Deposition of volcano-sedimentary rocks began at c. 1085 Ma and continued until c. 1030 Ma. Large, layered, mafic–ultramafic intrusions of the Giles Suite were emplaced between c. 1078 and 1075 Ma, followed by gabbro of the West Hinckley Suite and co-mingled leucogranite (Warakurna Supersuite) that was synchronous with regional-scale, upright folding in a transpressional setting. Granitic rocks of the Warakurna Supersuite were generated intermittently throughout the event.
The main regional depocentre generated during rifting was the Bentley Basin, into which the Bentley Supergroup (P_-BE) was deposited. With the exception of the Tjauwata Group, which straddles the Northern Territory – Western Australia border, most of the sequence lies in Western Australia within the Blackstone and Talbot Sub-basins. The latter preserves large-volume, mantle-derived rhyolitic lavas and ignimbrites, with interleaved tholeiitic basalt flows and sedimentary intercalations. Many of the felsic volcanic units of the sub-basin can be traced laterally for over 90 km and have volumes that reflect ‘supervolcano’ class eruptions.
The Giles Event was not a simple single event; rather, it involved protracted magmatism and deformation throughout its history. Magmatism was more likely initiated by tectonic movement rather than by a mantle plume. | | | Distribution | The effects of the Giles Event are evident across the Musgrave Province. Units within the Walpa Pulka Zone, Tjuni Purlka Zone and Mumutjarra Zone are affected by the event. | | | Description | The 1085–1030 Ma Giles Event records the evolution of the long-lived, ultimately failed, intracontinental Ngaanyatjarra Rift (Evins et al., 2010). Aitken et al. (2013) identified two phases of rifting: an early rift stage (1085–1074 Ma) that is characterized by voluminous magmatism within the upper crust and relatively little tectonic deformation; and a late rift stage that is characterized by tectonic deformation, synchronous with the deposition of a thick pile of volcanic and sedimentary rocks (1074–1030 Ma). In this rift, magmatism was the dominant process and the overall crustal extension was very limited (Aitken at al., 2013).
The early rifting event began with deposition of volcano-sedimentary rocks into the Bentley Basin. The basal part of the sequence (Kunmarnara Group; P_-KR) extends for a distance of over 200 km along the rift-basin boundaries that widen to the west. Bimodal magmatism followed, producing large, layered, mafic–ultramafic intrusions, gabbro, granite, and an extensive volcano-sedimentary succession.
Between c. 1078 and 1075 Ma, more than a dozen giant, layered, mafic–ultramafic intrusions of the Giles Suite, a component of the Warakurna Supersuite (and Warakurna Large Igneous Province), were emplaced into the Musgrave Province at mid- to upper-crustal levels. The intrusions were generated from tholeiitic mafic magmas of variable composition which formed mafic and locally ultramafic cumulates, including wehrlite-, harzburgite- and websterite-rich bodies, intrusions dominated by olivine–gabbronorite, and those with a dominantly troctolitic composition (Maier et al., 2014). Many of the troctolitic intrusions, such as the Bell Rock, Blackstone and Jameson–Finlayson intrusions, lie on crustal scale faults and are tectonically dislocated portions of an originally contiguous body, named the Mantamaru intrusion (Maier et al., 2014). Steeply north-dipping faults are present along the southern margins of the Jameson and Blackstone intrusions and these are constrained by the younger granitic plutons that are not displaced by these faults.
Mutual contacts show that the c. 1075 Ma West Hinckley Suite, comprising massive gabbro and co-mingled leucogranite, subsequently intruded fully crystallized Giles intrusions (Howard et al., 2015). Magmatism at c. 1075 Ma may have been characterized by mafic and felsic magmas focused along coeval linear shear zones. This magmatism was synchronous with macroscopic, upright folding in a transpressional setting — events indicative of basin inversion (Evins et al., 2010).
Deposition of the Bentley Supergroup continued and the rocks extend from the west into the northern part of the province in the Northern Territory, where the sequence of volcanic, volcaniclastic, and clastic rocks within the footwall of the Woodroffe Thrust is defined as the Tjauwata Group (Close et al., 2003). The largest exposure of the Bentley Supergroup is in the Talbot Sub-basin, in the western part of the province. This sequence preserves large-volume, mantle-derived rhyolitic lavas and ignimbrites, with interleaved tholeiitic basalt flows and sedimentary intercalations. Many of the felsic volcanic units of the sub-basin can be traced laterally for over 90 km and have volumes that reflect ‘supervolcano’ class eruptions (Smithies et al., 2013).
In the Blackstone Sub-basin, rhyolite of the Tollu Group directly overlies the layered Blackstone intrusion of the Giles Suite. The rhyolite is the same age (c. 1075 Ma) and composition as leucogranite associated with the massive gabbro intrusions and was most likely derived from the same magma. This suggests that extensive and rapid uplift, erosion and exhumation of the layered Giles intrusions was immediately followed by felsic volcanism. Andesite in the upper part of the Tollu Group is the same age (c. 1068 Ma) and geochemical composition as ferrogabbro of the Alcurra Dolerite (Howard et al., 2009) and the gabbro host to significant orthomagmatic nickel–copper mineralization at Nebo–Babel (Seat, 2008).
The late rift phase of Aitken et al. (2013) involved large-scale folding of the Giles and West Hinckley Suites, and the overlying Tollu Group, between c. 1075 and 1064 Ma. This was followed by deformation that produced northeast-trending faults in the Barrow Range – Cavenagh Corridor. During the closing stages of the Ngaanyatjarra Rift, east-southeast-trending faults with dextral offsets developed and major fault boundaries were reactivated. This deformation was the mid- to upper-crustal expression of deeper movements on the Mundrabilla Shear Zone (Aitken et al., 2013).
The Giles Event has been attributed to the effects of a deep mantle plume (e.g. Zhao and McCulloch, 1993; Wingate et al., 2004). However, Smithies et al. (2015b) suggested the extreme thermal pre-history of the Musgrave Province led to the prolonged (>50 Ma) mantle-derived magmatism without producing a time-transgressive magma trace. These factors suggest magmatism was more likely initiated by tectonic movement rather than by a mantle plume. | | | | | | Geochronology | | | Giles Event | Maximum age | Minimum age | Age (Ma) | 1085 | 1030 | Age | Mesoproterozoic | Mesoproterozoic | Age data type | Inferred | | References | | Edgoose et al. (2004) | Edgoose et al. (2004) |
| | Smithies et al. (2007) | Wingate et al. (2015) | Wingate et al. (2017) |
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| Rocks formed during the Giles Event range in age from c. 1085 to 1030 Ma. The maximum age is based on the c. 1085 Ma regional maximum age of magmatic rocks of the Bentley Supergroup and Warakurna Supersuite (Edgoose et al., 2004; Evins et al., 2010), which must be nearly coeval with the onset of the Ngaanyatjarra Rift and deposition of the Kunmarnara Group.
The Giles Suite includes large layered intrusions dated at 1078–1075 Ma. A sample of Giles Suite layered rocks obtained from Mount Finlayson (on FINLAYSON) yielded a magmatic crystallization age of 1076 ± 7 Ma (GSWA 194762, Kirkland et al., 2011a), and Sun et al. (1996) obtained a date of 1078 ± 3 Ma from a granitic layer within the layered Bell Rock intrusion.
West Hinckley Suite gabbro ranges in age from c. 1078 to 1074 Ma and field relationships indicate that this massive gabbro post-dates emplacement of the layered intrusions. The emplacement age of the massive gabbro unit is constrained by the ages of the Giles Suite (maximum age c. 1078 Ma; Sun et al., 1996) and the granitic rocks that crosscut, are crosscut by, and are locally mingled with the gabbro. A co-mingled granitic dyke at Amy Giles Hill, yielded a date of 1074 ± 3 Ma (GSWA 174589, Bodorkos and Wingate, 2008), interpreted to be the minimum age for the suite. A syn-mylonitic leucogranite, dated at 1075 ± 3 Ma (GSWA 185509, Kirkland et al., 2008), occupies boudin necks in a northwest-trending mylonite. Seven granite samples, showing textural evidence of synchronous intrusion with gabbro, have been dated, together giving a weighted average crystallization age of 1075 ± 1 Ma for both granite and gabbro (Evins et al., 2010), with a potential range from c. 1078 to 1074 Ma. The ages obtained for the west Hinckley Suite define a very narrow time interval of concomitant intrusion of massive gabbro, multi-phase intrusion of leucogranites, felsic volcanism, macroscopic folding, and crustal-scale shearing (Smithies et al., 2009).
Granitic rocks of the Warakurna Supersuite intruded during several separate stages of the Giles Event at c. 1075, 1073, 1062, and 1030 Ma, with the full range of intrusive ages ranging between c. 1078 and 1030 Ma. In the Bell Rock area, there are c. 1075 Ma granitic rocks, in the Tollu and Talbot Sub-basin areas there is a middle phase of c. 1073 Ma granitic magmatism, in the northern part of the Tjuni Purlka Zone and in the Talbot Sub-basin is a phase of c. 1062 Ma granite, and in the Rawlinson Range area the youngest granitic phase is c. 1030 Ma (GSWA 208486, Wingate et al., 2017).
Age constraints for the Tollu Group are from two rhyolite samples from around Mount Jane in the east of the Blackstone Syncline. These yielded dates of 1073 ± 7 Ma (GSWA 191706, Coleman et al., 2010a) and 1071 ± 8 Ma (GSWA 191728, Coleman et al., 2010b).
In the Talbot Sub-basin, several samples from each of the volcano-sedimentary packages (Mount Palgrave, Kaarnka, Pussy Cat, Cassidy and Mission Groups) have been dated. However, all felsic igneous rocks of the Talbot Sub-basin include a large proportion of recycled cognate material (i.e. zircon antecrysts). Therefore, the most conservative age range for magmatic activity within the Talbot Sub-basin is probably between c. 1077 and 1047 Ma (Smithies et al., 2015a).
The Tjauwata Group, in the northern part of the west Musgrave region, ranges in age from c. 1085 to 1030 Ma. With the exception of the Karukali Quartzite and Mount Harris Basalt, in Western Australia, ages obtained from units of the Bentley Supergroup in the Rawlinson area are notably younger than those of the Talbot and Blackstone sub-basins. For example, the Wankari Volcanics of the Tjauwata Group yielded SHRIMP U–Pb zircon dates of 1041 ± 8 Ma (GSWA 201708, Lu et al., 2017b), 1043 ± 8 Ma (GSWA 201702, Lu et al., 2017a) and 1039 ± 7 (GSWA 208489, Lu et al., 2017c), interpreted as igneous crystallization ages. | | | Tectonic Setting | An intracontinental setting is indicated for the Musgrave Province for at least 150 Ma prior to the Giles Event, and this setting has persisted to the present (Evins et al., 2010). The sequence of events encompassed by the Giles Event describes a long-lived, failed intracontinental rift. Although initial studies related the Giles Event to the effects of a deep-mantle plume (Zhao and McCulloch, 1993; Wingate et al., 2004; Pirajno, 2007) the duration of related mantle-derived magmatism exceeds 50 Ma, and the entire history is recorded within the restricted area of the west Musgrave region, with no time-progressive spatial magmatic trend. It appears that the controls on this magmatism were long-lived and specifically attached to the lithosphere.
It has recently been proposed that the reasons for the Giles Event are entirely tectonic, relating primarily to a coincidence of two major factors — an extreme thermal pre-history of the region, and primarily sinistral strike-slip movement along translithospheric faults (Smithies et al., 2015a). The Giles Event can be viewed as the temporal continuation of a much longer history of greatly enhanced thermal gradients extending back at least to the beginning of the Musgrave Orogeny (c. 1220 Ma). Thermal modelling of this region suggests that temperatures at a depth of 20 km possibly exceeded 800°C throughout the Giles Event, consistent with geochronological evidence that zircon-saturated migmatites continued to form in the mid-crust for at least 120 Ma after the Musgrave Orogeny (Smithies et al., 2013). Such a steep, elevated thermal profile in the crust also suggests that lithospheric regrowth and thickening were retarded, so that the crustal thickness at the beginning of the Giles Event may not have differed significantly from that throughout the Musgrave Orogeny (i.e. ~35 km to the asthenosphere boundary).
Mantle-derived melts were a significant contributor to Pitjantjatjarra magmatism throughout the Musgrave Orogeny (Smithies et al., 2010; Kirkland et al., 2013) and continued as the (overwhelmingly) dominant component of magmas formed during the Giles Event. In this regard, it is possible that both the thermal state and the regional lithospheric architecture — thin crust locked between three cratonic masses — allowed for a prolonged mantle-melt enriched zone beneath the region. The Ngaanyatjarra Rift is truncated by a north-trending, translithospheric structure (the Mundrabilla Shear Zone), and the point of truncation coincides with the Talbot Sub-basin. Movement along this shear zone potentially had significant implications for the Mesoproterozoic evolution of central Australia (e.g. Aitken et al., 2013), including triggering the Giles Event. There was major sinistral strike-slip displacement along this shear zone during or after c. 1140 Ma granitic magmatism to the south of the Musgrave region (Kirkland et al., 2011b; Smithies et al., 2015a), but prior to the c. 1085 Ma beginning of the Giles Event. Significant displacement along this structure may have initiated the Giles Event by catastrophically destabilising the post-Musgrave Orogeny juvenile lithosphere. | | | | References | Aitken, ARA, Smithies, RH, Dentith, MC, Joly, A, Evans, S and Howard, HM 2013, Magmatism-dominated intracontinental rifting in the Mesoproterozoic: The Ngaanyatjarra Rift, central Australia: Gondwana Research, v. 24, no. 3–4, p. 886–901, doi:10.1016/j.gr.2012.10.003. | Bodorkos, S and Wingate, MTD 2008, 174589.1: quartz syenite dyke, Amy Giles Hill; Geochronology Record 715: Geological Survey of Western Australia, <www.dmpe.wa.gov.au/geochron>. View Reference | Close, DF, Edgoose, CJ and Scrimgeour, IR 2003, Hull and Bloods Range, Northern Territory: Northern Territory Geological Survey, 1:100 000 Geological Map Series Explanatory Notes, 46p. | Coleman, PM, Kirkland, CL, Wingate, MTD and Smithies, RH 2010a, 191728.1: rhyolite, Mount Jane; Geochronology Record 917: Geological Survey of Western Australia, <www.dmpe.wa.gov.au/geochron>. View Reference | Coleman, PM, Kirkland, CL, Wingate, MTD and Smithies, RH 2010b, 191706.1: mylonitic rhyolite, Mount Maria; Geochronology Record 915: Geological Survey of Western Australia, <www.dmpe.wa.gov.au/geochron>. View Reference | Edgoose, CJ, Scrimgeour, IR and Close, DF 2004, Geology of the Musgrave Block, Northern Territory: Northern Territory Geological Survey, Report 15, 46p. | Evins, PM, Smithies, RH, Howard, HM, Kirkland, CL, Wingate, MTD and Bodorkos, S 2010, Devil in the detail: the 1150–1000 Ma magmatic and structural evolution of the Ngaanyatjarra Rift, west Musgrave Province, central Australia: Precambrian Research, v. 183, p. 572–588. | Evins, PM, Smithies, RH, Howard, HM, Kirkland, CL, Wingate, MTD and Bodorkos, S 2010, Redefining the Giles Event within the setting of the 1120-1020 Ma Ngaanyatjarra Rift, west Musgrave Province, central Australia: Geological Survey of Western Australia, Record 2010/6, 36p. View Reference | Howard, HM, Smithies, RH, Kirkland, CL, Evins, PM and Wingate, MTD 2009, Age and geochemistry of the Alcurra Suite in the western Musgrave Province and implications for orthomagmatic Ni–Cu–PGE mineralization during the Giles Event: Geological Survey of Western Australia, Record 2009/16, 16p. View Reference | Howard, HM, Smithies, RH, Kirkland, CL and Quentin de Gromard, R 2015, The burning heart — the Musgrave Province, in GSWA 2015 extended abstracts: promoting the prospectivity of Western Australia: Geological Survey of Western Australia, Record 2015/2, p. 28–30. View Reference | Kirkland, CL, Smithies, RH, Woodhouse, AJ, Howard, HM, Wingate, MTD, Belousova, EA, Cliff, JB, Murphy, RC and Spaggiari, CV 2013, Constraints and deception in the isotopic record; the crustal evolution of the west Musgrave Province, central Australia: Gondwana Research, v. 23, no. 2, p. 759–781. | Kirkland, CL, Wingate, MTD and Bodorkos, S 2008, 185509.1: leucogranite, Mount Aloysius; Geochronology Record 725: Geological Survey of Western Australia, <www.dmpe.wa.gov.au/geochron>. View Reference | Kirkland, CL, Wingate, MTD and Smithies, RH 2011a, 194762.1: leucogabbro, Mount Finlayson; Geochronology Record 966: Geological Survey of Western Australia, <www.dmpe.wa.gov.au/geochron>. View Reference | Kirkland, CL, Wingate, MTD, Spaggiari, CV and Tyler, IM 2011b, 194773.1: granitic rock, Eucla No. 1 drillhole; Geochronology Record 1001: Geological Survey of Western Australia, <www.dmpe.wa.gov.au/geochron>. View Reference | Lu, Y, Wingate, MTD, Kirkland, CL, Howard, HM, Quentin de Gromard, R and Haines, PW 2017a, 201708.1: porphyritic rhyolite, Warilpra Creek; Geochronology Record 1403: Geological Survey of Western Australia, <www.dmpe.wa.gov.au/geochron>. View Reference | Lu, Y, Wingate, MTD, Kirkland, CL, Howard, HM, Quentin de Gromard, R and Haines, PW 2017b, 201702.1: porphyritic rhyolite, Kathleen Range; Geochronology Record 1402: Geological Survey of Western Australia, <www.dmpe.wa.gov.au/geochron>. View Reference | Lu, Y, Wingate, MTD, Quentin de Gromard, R, Howard, HM and Haines, PW 2017c, 208489.1: metarhyolite, Mount Deering; Geochronology Record 1407: Geological Survey of Western Australia, <www.dmpe.wa.gov.au/geochron>. View Reference | Maier, WD, Howard, HM, Smithies, RH, Yang, S, Barnes, S-J, O'Brien, H, Huhma, H and Gardoll, S 2014, Mafic-ultramafic intrusions of the Giles Event, Western Australia: Petrogenesis and prospectivity for magmatic ore deposits: Geological Survey of Western Australia, Report 134, 82p. View Reference | Pirajno, F 2007, Ancient to modern Earth: The role of mantle plumes in the making of continental crust, 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. 1037–1064. | Seat, Z 2008, Geology, petrology, mineral and whole-rock chemistry, stable and radiogenic isotope systematics and Ni-Cu-PGE mineralisation of the Nebo-Babel intrusion, west Musgrave, Western Australia: The University of Western Australia, Perth, Western Australia, PhD thesis (unpublished). | Smithies, RH, Howard, HM, Bodorkos, S, Evins, PM and Pirajno, F 2007, Timing and geochemistry of felsic magmatism in the west Musgrave Complex, in GSWA 2007 extended abstracts: promoting the prospectivity of Western Australia: Geological Survey of Western Australia, Record 2007/2, p. 5–6. View Reference | Smithies, RH, Howard, HM, Evins, PM, Kirkland, CL, Kelsey, DE, Hand, M, Wingate, MTD, Collins, AS, Belousova, E and Allchurch, S 2010, Geochemistry, geochronology, and petrogenesis of Mesoproterozoic felsic rocks in the west Musgrave Province, Central Australia, and implications for the Mesoproterozoic tectonic evolution of the region: Geological Survey of Western Australia, Report 106, 73p. View Reference | Smithies, RH, Howard, HM, Evins, PM, Kirkland, CL and Wingate, MTD 2009, New insights into the geological evolution of the west Musgrave Complex, in GSWA 2009 extended abstracts: promoting the prospectivity of Western Australia edited by Geological Survey of Western Australia: Geological Survey of Western Australia, Record 2009/2, p. 19–22. View Reference | Smithies, RH, Howard, HM, Kirkland, CL, Korhonen, FJ, Medlin, CC, Maier, WD, Quentin de Gromard, R and Wingate, MTD 2015a, Piggy-back supervolcanoes — long-lived, voluminous, juvenile rhyolite volcanism in Mesoproterozoic central Australia: Journal of Petrology, v. 56, no. 4, p. 735–763, doi:10.1093/petrology/egv015. | Smithies, RH, Howard, HM, Kirkland, CL, Werner, M, Medlin, CC, Wingate, MTD and Cliff, JB 2013, Geochemical evolution of rhyolites of the Talbot Sub-basin and associated felsic units of the Warakurna Supersuite: Geological Survey of Western Australia, Report 118, 74p. | Smithies, RH, Kirkland, CL, Korhonen, FJ, Aitken, ARA, Howard, HM, Maier, WD, Wingate, MTD, Quentin de Gromard, R and Gessner, K 2015b, The Mesoproterozoic thermal evolution of the Musgrave Province in central Australia - plume vs. the geological record: Gondwana Research, v. 27, no. 4, p. 1419–1429, doi:10.1016/j.gr.2013.12.014. | Sun, S-S, Sheraton, JW, Glikson, AY and Stewart, AJ 1996, A major magmatic event during 1050-1080 Ma in central Australia, and an emplacement age for the Giles Complex: AGSO Journal of Australian Geology & Geophysics, v. 24, p. 13–15. | Wingate, MTD, Kirkland, CL and Haines, PW 2015, 199408.1: sandstone, Dixon Range; Geochronology Record 1258: Geological Survey of Western Australia, <www.dmpe.wa.gov.au/geochron>. View Reference | Wingate, MTD, Lu, Y, Quentin de Gromard, R and Howard, HM 2017, 208486.1: migmatitic metasyenogranite, south of Mount Deering; Geochronology Record 1438: Geological Survey of Western Australia, <www.dmpe.wa.gov.au/geochron>. View Reference | Wingate, MTD, Pirajno, F and Morris, PA 2004, Warakurna large igneous province: A new Mesoproterozoic large igneous province in west-central Australia: Geology, v. 32, no. 2, p. 105–108. | Zhao, J and McCulloch, MT 1993, Sm-Nd mineral isochron ages of Late Proterozoic dyke swarms in Australia: Evidence for two distinctive events of mafic magmatism and crustal extension: Chemical Geology, v. 109, no. 1–4, p. 341–354. |
| | | | Recommended reference for this publication | Howard, HM, Quentin de Gromard, R, Smithies, RH and Haines, PW 2020, Giles Event (MGE): 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 29 January 2020. | | | | | 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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