NORTHERN TERRITORY GEOLOGICAL SURVEY Geological Survey Record 2001-003 - electronic pre-release

Igneous rocks of the Tanami Region

Alison A. Dean

1 NORTHERN TERRITORY DEPARTMENT OF MINES AND ENERGY MINISTER: Hon Daryl Manzie, MLA SECRETARY: Peter Blake NORTHERN TERRITORY GEOLOGICAL SURVEY DIRECTOR: Dr R Dennis Gee

Bibliographic reference: Dean AA 2001. Igneous rocks of the Tanami Region - Northern Territory Geological Survey Record GS 2001-0003

ISSN 1443-1149; Geological Survey Record GS 2001-0003 ISBN 0 7245 7008 X

Keywords: Tanami 1:250 000 SE 52-15; The Granites 1:250 000 SF52-03; Archaean; Palaeoproterozoic; igneous petrology; mafic; felsic; dolerite; granite; intrusives; extrusives; petrogenesis; geophysics; geochemistry

This report may be obtained from: Department of Mines and Energy (DME) NT Geological Survey 3rd Floor, Centrepoint Building Smith Street Mall DARWIN NT 0800 or from the NTGS web site:http://www.dme.nt.gov.au/ntgs

Cover photograph

Granite Outcrop, Frederick Suite, MACFARLANE, AMG 504632-778659

ACKNOWLEDGEMENTS The author thanks Chris Field, Max Heckenberg and Liam McNally for their assistance and company during fieldwork. We thank the staff of Normandy NFM, Otter Gold, Anglo Gold, Tanami Gold and Glengarry Resources for their on going support of the Tanami Project.

Authorship

© Copyright in this information is vested in the Crown. The Government of the Northern Territory retains ownership of the intellectual property rights. No reproduction of this information, or any part of the information is permitted in any form except as the user may be licensed to produce by the Minister for Mines and Energy for the Northern Territory. All rights are reserved to the Crown.

2 Preface This publication represents the preliminary interpretations of petrographical and geochemical data from the Tanami Region by the Northern Territory Geological Survey (NTGS). The intention is to disseminate new information and ideas as quickly as possible to help stimulate the generation of new exploration models. Readers are advised that interpretations may change as new information becomes available.

It is intended that after further editing and interpretation, the material contained in this Record will be incorporated, along with companion Records on structure and srtatigraphy, into a comprehensive bulletin on the geology and mineralisation of the Tanami Region.

Disclaimer This information is provided on the understanding that the user agrees to release and indemnify the Northern Territory, the Commonwealth of Australia, companies who supplied and acquired the data, and their employees, agents and contractors, in respect of all liability for actions, claims, costs, expenses, loss, damage or injury, which may be suffered by them, or any other persons, arising from the users use of the data, or as a consequence of any unlawful or negligent act or omission of the user.

3 ABSTRACT

Grantoids comprise a large percentage (~60%) of the Tanami Region. They are predominantly biotite (± hornblende) monzogranite and granodiorite, with minor syenogranite, quartz syenite, monzonite, tonalite and quartz diorite. Grantoids are distinguished on macro, meso and microscopic features and are subdivisible into the following: Coomarie Supersuite, comprising three suites: • Coomarie Suite, non-magnetic, metaluminous, oxidized and reduced, biotite monzogranite. • Inningarra Suite, moderately magnetic, foliated, metaluminous or weakly peraluminous, oxidized and reduced biotite monzogranite and granodiorite. • The Granites Suite, non to moderately magnetic, metaluminous, oxidized and reduced, biotite monzogranite and granodiorite. • numerous unassigned minor felsic stocks and dykes.

Defined also are: • Frederick Suite, non-magnetic to highly magnetic, metaluminous, reduced to weakly oxidized, biotite hornblende monzogranite and granodiorite. • Winnecke Suite, non-magnetic to moderately magnetic, metaluminous, reduced to highly oxidized, hornblende biotite monzogranite, granodiorite and dacite. • Borefield Road Suite, moderately to highly magnetic, metaluminous, hornblende - biotite monzogranite to gabbro. Suites display predominantly calc-alkaline character and are metaluminous to weakly peraluminous (>1.1ASI). Peraluminous and peralkaline analyses are variably differentiated or metasomatized.

Two genetic groups are discerned on trace element abundances: • Sr, Ti, Nb, and P depleted, Y undepleted or slightly undepleted – infer residual plagioclase, ilmenite, rutile, and apatite, with variable hornblende content in the source area. • Sr undepleted, Ti, Nb, P and Y depleted - infer residual hornblende, garnet, ilmenite, rutile, and apatite in the source area. This implies partial melting of protoliths at increasing depth with time.

Three overlapping events of granitoid magmatism are recognised: an early 1830-1820 Ma event (Winnecke Suite), an 1820-1810 Ma event (Coomarie Supersuite, Inningarra Suite), and a later 1810- 1790 Ma period (The Granites Suite, Frederick Suite). Granite chemistry is equivocal with regard to tectonic setting. Distinctive chemical signatures defining suites suggest variable depths for partial melting and variable protolith compositions.

Intermittent felsic volcanism concurrent with sedimentation is indicated by interbedded rhyolitic lava and ash-fall tuff. Mafic plutonism and volcanism was syn and post kinematic, and prior to or synchronous with granite intrusion.

Tanami Region mafic rocks can be classified as subalkaline tholeiitic and exhibit a broad range in Mg # (26-71). Two groups are defined from stratigraphic petrographic and geochemical features: • Dead Bullock Soak Dolerite - intruded into Tanami Group, continental flood basalt chemistry, MgO wt% 6-7, LREE enriched, weak Eu anomaly. • Mount Charles Formation Basalt - extruded within Mount Charles Formation, distinctive low-K chemistry, similar to continental rift tholeiite.

In the absence of evidence to the contrary and based on regional stratigraphy, this study supports the findings of previous authors that Tanami Group dolerite and associated mafic rocks intruded into developing basins during initial extension, and Mount Charles basalt and metamorphosed equivalents were extruded during a subsequent rifting event.

4 CONTENTS

ABSTRACT

INTRODUCTION 9

REGIONAL SETTING

ARCHAEAN ...... 8 PALAEOPROTEROZOIC...... 9 FELSIC ROCKS PETROGRAPHIC FEATURES ...... 10 GENERAL GEOCHEMICAL FEATURES...... 14 GENERAL FEATURES OF GRANITOIDS...... 21 COOMARIE SUITE...... 24 Coomarie Dome Intrusives...... 25 Frankenia Monzogranite...... 26 Talbot South Monzogranite...... 26 MacFarlane Granodiorite...... 27 Browns Range Dome Intrusives ...... 27 INNINGARRA SUITE...... 29 Muriel Range Intrusives...... 30 Grimwade Ridge Intrusives...... 31 Murdoch Cliffs Intrusives...... 31 Officer Hill Intrusives...... 32 Bunkers Tonalite ...... 33 Watertower Tonalite...... 33 THE GRANITES SUITE ...... 34 The Granites Monzogranite...... 35 Ptilotus Granodiorite ...... 35 Twin Bonanza Porphyry...... 36 UNASSIGNED FELSIC INTRUSIVES ...... 36 Hurricane Dacite Dyke ...... 37 Pargee Rhyolite Dyke...... 38 FREDERICK SUITE ...... 39 Pipeline Granodiorite ...... 41 Mavericks Monzogranite...... 42 Apertawonga Monzogranite...... 43 Inspiration Peak Monzogranite...... 43 MacFarlane Peak Monzogranites...... 44 Walnut Granodiorite ...... 46 Nora Range Monzogranite ...... 46 Slatey Creek and Lewis Granites (WA - NT)...... 47 WINNECKE SUITE (PGW, PLWA, PN)...... 47 Winnecke Monzogranite...... 49 Nanny Goat Volcanics and Mount Winnecke Group...... 51 FELSIC VOLCANIC ROCKS ...... 54 Mavericks Volcanics ...... 55 MacFarlane Volcanics ...... 55 MAFIC ROCKS

CHEMICAL AND MODAL CLASSIFICATION ...... 57 GENERAL PETROGRAPHIC AND GEOCHEMICAL FEATURES ...... 57 MAFIC PLUTONIC ROCKS...... 59 Ptilotus And The Granites Dolerites ...... 59 Dead Bullock Soak dolerite...... 60 Borefield Road Suite (Pgb)...... 62

5 MAFIC VOLCANIC ROCKS ...... 64 Mount Charles Formation basalt (Pcb) ...... 64 Nanny Goat Volcanics basalt (Pn4)...... 66 DISCUSSION OF PETROGENSIS

GRANITE PROTOLITHS...... 67 MAFIC SOURCES...... 70 TECTONIC SETTING ...... 71 MINERALIZATION

FELSIC MAGMATISM AND MINERALIZATION ...... 74 MINERALIZATION ASSOCIATED WITH FELSIC MAGMATISM ...... 75 CONCLUSIONS...... 77

LIST OF TABLES

TABLE 1 PETROGRAPHIC FEATURES OF GRANITE SUITES FROM THE TANAMI

REGION 7

TABLE 2 MEASURED FE2+ VALUES PLUS CALCULATED FE3+/( FE3++ FE2+)12

TABLE 3 ASSAY RESULTS FOR NTGS DRILLING PROGRAM (PPB) 77

TABLE 4 ELEMENT ABUNDANCES FOR OFFICER HILL INTRUSIVES 78

LIST OF REFERENCES AND APPENDICES NOT INCLUDED IN THIS ELECTRONIC PRE-RELEASE

APPENDIX 1 SAMPLE LIST, COORDINATES AND LOCALITY MAP

APPENDIX 2 NOMENCLATURE, ABBREVIATIONS AND ACRONYMS, PETROGRAPHIC DESCRIPTIONS

APPENDIX 3 GEOCHEMICAL ANALYSES

6 INTRODUCTION

Igneous rocks, particularly granitoids, comprise a substantial part of the Tanami Region. This study focuses primarily on new petrographical and geochemical data of igneous rocks and complements recently released stratigraphic and structural records on the Tanami Region by the Northern Territory Geological Survey (NTGS) [Hendrickx, 2000 #1056; Vandenberg, 2001 #834].

The prime objective of this study is to petrographically and geochemically define the character of the igneous rocks of the Tanami Region. Current work will also define the character of igneous rocks in adjacent map sheets in order to understand relationships between the Tanami Region and adjoining basement terranes.

Despite limited exposure, observations and sampling were carried out on igneous outcrops in conjunction with regional re-mapping of the Tanami Region at 1:100 000 and 1:250 000 scales. This report is supported by basement geology maps defining concealed igneous bodies, interpreted from detailed aeromagnetic and gravity surveys undertaken by NTGS and exploration companies [Hendrickx, 2000 #1056; Slater, 2000 #1071; Slater, 2000 #1070; Slater, 2000 #1072; Slater, 2000 #1073].

Diamond drill core and drill logs, made available by exploration companies (Otter Gold, Normandy NFM and Anglo Gold) were systematically collected and used where suitable, adding substantially to samples from outcrop. Data were also obtained from the AGSO database OZROC. Brief descriptions and geochemical analyses for unweathered samples from previous geological programs (AGSO and others) have been included with this work. Some thin sections from early BMR (Bureau of Mineral Resources) work were provided by AGSO to aid this study. New precise radiometric U-Pb ages used in this report were acquired by JB Smith under a joint AGSO – NTGS program using SHRIMP 1 at The Australian National University. These ages are reported in Smith (2001).

The scarcity of fresh granite outcrop and the presence of numerous intrusive bodies under surficial cover, interpreted from geophysical imagery, necessitated a drilling program to provide fresh samples for geochronology and geochemistry. Eleven holes were RAB drilled to a depth of about 80m, then diamond cored for about 10m to provide fresh samples. Several samples described in this report are still in the process of geochronological analysis. To sample more remote areas of the Tanami Region a helicopter was used. All suitable material was cut for thin section petrography and prepared for whole-rock geochemistry at the NTGS facilities in Alice Springs. Over 300 thin sections from igneous rocks have been examined in detail. Description sheets for each sample can be found in Appendix 2. Geochemical analyses were carried out at AMDEL laboratories in Adelaide, or at AGSO laboratories in Canberra, if geochronology was undertaken.

7 Mapping, sampling and drilling programs were undertaken in the early seventies by BMR to determine the geology of the Tanami Region [Blake, 1972a #1034; Blake, 1972b #1035; Blake, 1973 #1036; Blake, 1974 #1037; Blake, 1979 #1039; Blake, 1975 #1038]. Numerous exposed and subsurface, mafic and felsic units were named and described ([Blake, 1972a #1034; Blake, 1972b #1035; Blake, 1973 #1036; Blake, 1974 #1037; Blake, 1979 #1039; Blake, 1975 #1038]. These works contain detailed descriptions of most areas and form the basic foundation of the current work.

Various research theses have been undertaken in the Tanami over the past two decades, but with limited attention on the igneous rocks. The most significant is Tunks (1996) on the Tanami Gold Mine, which contains petrology on granite and basalt, and Garnaut (1995) on mafic rocks. Subsequent works used early BMR and exploration data to summarise igneous characteristics [Wyborn, 1988 #1089; Wyborn, 1996 #1090]. Mining operators in the Tanami have large collections of drillcore plus petrographic and geochemical descriptions in company reports.

REGIONAL SETTING

The Tanami Region is located 600 kms north-northwest of Alice Springs. Its contact relationships with the adjacent basement terranes of the Halls Creek Orogen to the northwest, Pine Creek Orogen to the northeast, the Tennant Inlier to the east and the Arunta to the southeast are obscured by later cover sequences. Geophysical imaging suggests a continuation of the Halls Creek Orogen into the Tanami Region, but a major discontinuity, possibly a crustal scale a shear zone may exist between basement terranes to the southeast.

The following summary represents a synopsis of salient points pertinent to this report from recently published stratigraphical and structural reports. For detailed information on stratigraphy and structure the author is directed to the relevant report [Hendrickx, 2000 #1056; Vandenberg, 2001 #834].

ARCHAEAN

The oldest rocks are part of a late Archaean (2600-2500 Ma) basement which probably was quite extensive [Page, 1995 #1067; Page, 1996 #1068]. Archaean basement predominantly comprises orthogneiss which outcrops at two separate localities. The Billabong Complex, (2514 ± 3 Ma) situated southeast of The Granites Gold Mine in GRANITES occurs as a fault bounded sliver of orthogneiss (2504 ± 4 Ma) and leucogranite (2510 ± 22 Ma), plus minor metasedimentary rocks along the southern margin of the Browns Range Dome in MALLEE [Page, 1995 #1067; Page, 1996 #1068] The Browns Range Metamorphics is described by Hendrickx, 2000 #1056.

8 PALAEOPROTEROZOIC

The basal Palaeoproterozoic sequence (MacFarlane Peak Group) is dominated by mafic volcanic and volcaniclastic rocks, with minor clastics and calcsilicates [Hendrickx, 2000 #1056]. This sequence is interpreted as an extensional early rift stage between 1910-1880 Ma. Thick clastic sediments (Tanami Group) overlie MacFarlane Peak Group, and are thought to represent a passive margin sequence. The lower Tanami Group is characterised by carbonaceous siltstone with minor BIF and calcsilicates (Dead Bullock Formation), characteristic of deposition in a deep water reducing environment. The upper Tanami Group is a thick sequence of turbiditic sedimentary sandstone and siltstone (Killi Killi Formation) [Hendrickx, 2000 #1056]. MacFarlane Peak and Tanami Group rocks are intruded by dolerite which predates initial deformation in the Tanami Region.

Figure 1 Regional map of the North Australian Craton, indicating the study area (The Granites and Tanami 1:250,000 sheet locations), plus spatial and temporal relationships with surrounding Precambrian terranes (modified from [Hendrickx, 2000 #1056])

9 Deformation between 1845-1840 Ma (in this report called the Tanami Event) was accompanied by greenschist to amphibolite grade metamorphism. This was followed by local extension basins which filled with shallow marine sediments in the west (Pargee Sandstone) and basalt and turbiditic sediments in the east (Mount Charles Formation). Granite intrusion and volcanism occurred about 1830-1790 Ma prior to, during and post dating deformation. The Birrindudu Group, a 2 km thick platform sequence dominated by quartz arenite with minor carbonate, was deposited after intrusion of the Granites Suite

(1795Ma) [Hendrickx, 2000 #1056]. The Muriel Range Sandstone to the south in INNINGARRA, represents a lateral correlative of the Lewis Range and Munyu Sandstones. The Neoproterozoic Redcliff Pound Group in the Tanami Region is part of a thick sequence of predominantly sublithic and quartz arenite in a shallow marine setting [Blake, 1979 #1039].

FELSIC ROCKS

Felsic rocks of the Tanami Region have initially been classified according to geophysical characteristics.

Differentiation of an igneous body can cause considerable increase in SiO2 content with respect to overall elemental content, therefore this division was considered provisional only. Geochronology (if available), spatial distribution, field association, petrographic features and geochemical analyses allow refinement of the initial gross subdivisions. Where age has been ascertained, this determines the order of description of suites from oldest to youngest.in this Record.

PETROGRAPHIC FEATURES

The extent of extrusives and intrusives is illustrated on the modified geophysical interpretation map (Figure 2). Sample localities are listed and plotted in Appendix 1. Petrography was carried out on all samples collected and is detailed in Appendix 2. A condensed version listing salient petrographic and geochemical features of individual suites can be found in Table 1. Samples, too weathered for geochemistry still provide information on modal character and texture.

10 TABLE 1 PETROGRAPHIC AND GEOCHEMICAL FEATURES OF GRANITE SUITES FROM TANAMI REGION

Suites Magnetic ASI Type Mineralogy Trace elements Textures Other Character Coomarie variable metaluminous I S biotite Sr depleted fine to coarse K, Na, Ca Suite generally non- to weakly hornblende Y undepleted grained, metasomatism magnetic to peraluminous magnetite/ negative Nb Ti equigranular to high U weakly magnetic ilmenite P porphyritic, differentiated ±±± magmatic to reduced to submagmatic strongly foliation oxidized The Granites variable metaluminous I biotite Sr depleted fine to medium, high U, Suite generally magnetite/ Y undepleted equigranular to differentiated moderately ilmenite negative Nb Ti porphyritic, reduced to magnetic P ±±± magmatic to weakly submagmatic oxidized foliation

Inningarra variable metaluminous I S biotite Sr depleted fine to coarse Sn-W-Ta Suite generally non- to strongly muscovite Y undepleted grained, greisen, magnetic to peraluminous magnetite/ negative Nb Ti equigranular to highly weakly magnetic ilmenite P porphyritic, differentiated ±±± magmatic to reduced to post magmatic oxidized foliation Frederick highly magnetic metaluminous I biotite Sr undepleted fine to coarse visible Suite and non- hornblende Y undepleted grained, sulphides, magnetic ilmenite to depleted equigranular to megacrystic negative Nb Ti megacrystic, kspar, P ±±± magmatic reduced to foliation weakly oxidized Winnecke magnetic and metaluminous I S biotite Sr depleted fine to coarse cosanguinous Suite non-magnetic to weakly hornblende Y undepleted grained, volcanics, peraluminous pyroxene negative Nb Ti granophyric to reduced to to peralkaline magnetite P equigranular, strongly ±±± magmatic oxidized foliation

11 Figure 2 Distribution of granite and associated volcanic rocks of the Tanami Region and spatial relationship to known Au mineralization and identified major structural elements (modified from Hendrickx et al 2000.

12 Recent precise U-Pb zircon ages obtained from granite and felsic volcanics suggest three overlapping periods of felsic magmatism (± maficvolcanism): between 1830-1820 Ma, 1820-1810 Ma and 1810-1790 Ma. N.B. Geochronology from this region is still imcomplete, and numerous intrusives inferred from geophysical interpretation are yet to be dated. Many samples collected are at various stages in the SHRIMP process.

Point counting (average of 1000 points, dependent on grainsize) for the majority of granites provides classification according to IUGS recommendations. Modal information has been plotted on the Quartz - Alkali Feldspar - Plagioclase ternary diagram (Figure 3a). Modal analyses compare favourably with normative data (Figure 3b).

Figure 3a Quartz-Alkalies-Plagioclase ternary diagram plotting modal data, illustrating predominantly monzogranitic and granodioritic character of felsic igneous rocks of the Tanami Region (Le Maitre 1989).

Figure3b Normative Quartz-Orthoclase-Plagioclase ternary diagram to compare chemical data with modal data (Le Maitre 1989).

13 However, a shift toward the Or and Q apex is noted for some samples (tonalite becomes granodiorite) as biotite is not accounted for in the CIPW norm (Figure 3b). A shift toward the Pl apex is also noted in this case - the result of albite in perthitic alkali feldspar being recorded as plagioclase.

Rock types (including un-analysed samples) range from leucocratic to melanocratic granitoids that cover a broad range of compositions, from tonalite to alkali feldspar granite, quartz diorite to quartz syenite, and diorite to syenite. Overall monzogranite and granodiorite predominate. Textures range from coarse to fine grained, granophyric to graphic, megacrystic, seriate porphyritic to equigranular and aphyric. Foliation, where present is defined by feldspar, mica and hornblende alignment and mica and quartz recrystallisation. Subgrain development and grain boundary migration of quartz around grain margins with elongation into quartz ribbons is taken to indicate synchronous or post-crystallisation deformation.

Granites generally record a subsolvus history, with the formation of two distinct feldspars. However, several intrusives (Winnecke Granophyre - Winnecke Suite, and Muriel Range Granite - Inningarra Suite) and minor intrusives (stocks, dykes and sills - Coomarie Suite), record a change to hypersolvus conditions with formation of granophyric intergrowths and miarolitic cavities, indicative of sub-volcanic intrusion.

GENERAL GEOCHEMICAL FEATURES

Previously unpublished whole rock analyses of Tanami samples are presented in Appendix 3. Felsic rocks range between 53.9 wt% to 83.10 wt%. Most concentrate at about 70% SiO2. Values under 60 wt% SiO2 represent comagmatic mafic microgranular enclaves and dykes. Samples displaying hydrothermal alteration from petrographic observation were excluded from chemical analysis. Samples over 79% SiO2 were deemed silica flushed and unsuitable for the purposes of this study. Petrography indicates late to post magmatic modification is generally minimal. Igenous textures predominate and recrystallisation is concentrated around grain boundaries where it is often associated with the development of secondary sericite, muscovite, epidote, chlorite and calcite (Table A4) [in appendix 2]

The total alkalis versus SiO2 diagram illustrates the subalkaline to moderately calcalkaline character. The clustering of points also supports the predominantly dacitic to rhyolitic classification of volcanic rocks from the Winnecke Suite (Figure 4).

14 Figure 4 Total alkalis versus silica diagram illustrating subalkaline character and supports predominantly rhyodacitic classification of felsic volcanics (Irvine & Baragar, 1971; Le Bas et al., 1986).

The Aluminium Saturation Index (ASI), defined as the molar ratio Al2O3/CaO + K2O + Na2O indicates the degree to which it is saturated in aluminium (Zen 1986). Indices indicate the majority have metaluminous to weakly peraluminous compositions. Samples with an ASI >1.0 represent fractionated members of metaluminous suites (Coomarie Supersuite, Winnecke Suite). Some samples (Coomarie Suite) have been affected by pervasive alkali metasomatism (Figure 5). Samples that plot within the peralkaline field are from the Winnecke Suite and Inningarra Suite and illustrate anorogenic character, discussed later in this Record.

Figure 5 Alumina Saturation Indicies for the felsic rocks of the Tanami Region illustrating predominantly metaluminous character (after Zen 1986).

15 Fe2O3 and FeO values illustrate the mixed nature of granitoids with respect to oxidation. Granites plot from reduced to strongly oxidised, the majority being weakly oxidised (Figure 6). All suites contain both oxidised and reduced components. The majority of Fe2+ analyses come from the AGSO database OZROC. However, new whole rock Fe2+ data were obtained on fresh granite by the NTGS drilling program and are also presented in Table 2. Although Fe2+ data are insufficient and relate only to Coomari and Frederick suites, the data indicates values between 0.3 and 0.4, which is comparable with data for magnetite bearing I-type granites of the Lachlan Fold Belt (Whalen & Chappell 1988).

Figure 6 Redox diagram for Tanami Region felsic intrusives, FeOT (Total iron as Fe2+ ) vs Fe2O3/Fe2O3+FeO (Fe3+/(Fe3++ Fe2+) (after (Champion & Heinemann 1994))

Table 2 Measured values for whole rock Fe2+ and calculated Fe3+/(Fe3++ Fe2+) Sample Numbers Fe3+ Fe2+ Fe3+/(Fe3++ Fe2+) TAN99DDH1R1 1.7 2.1 0.46 TAN99DDH2R1 1.5 2.4 0.39 TAN99DDH3R1 1.7 3.0 0.37 TAN99DDH5R1 1.8 1.9 0.49 TAN99DDH6R1 0.8 1.7 0.32 TAN99DDH7R1 0.6 0.9 0.41 TAN99DDH15R1 0.7 1.2 0.39 TAN99DDH20R1 0.6 1.1 0.39 TAN99DDH21R1 1.1 1.3 0.46 TAN99DDH23R1 1.0 1.1 0.48 TAN99DDH28R1 1.2 2.1 0.36 TAN99AD372R1 0.9 1.4 0.41

Th/U indicate considerable U loss in some granites, probably associated with alteration or weathering. However, most samples plot around average crustal value of 0.4 (Figure 7).

16 Figure 7 Th/U versus SiO2 plot for Tanami Region felsic rocks

REE and primordial mantle-normalised spider diagrams indicate all felsic intrusives and extrusives are LREE enriched with a moderate to strong niobium anomaly. Strontium and yttrium are either depleted or undepleted and these values are used to distinguish suites. In a plot used primarily to define A-type anorogenic granites, samples plot outside the fractionated and ordinary granite (I- S-type) fields due to the generally high values for HFS elements, particularly yttrium (Figure 8).

Figure 8 10000*Ga/Al versus Zr+Nb+Ce+Y for Tanami samples illustrating high values for HFS elements (Eby 1990)

Most suites display some degree of differentiation even where the silica range is narrow. The most fractionated are Winnecke Suite intrusives, some of Inningarra Suite (Officer Hill Alkali Feldspar Granite and Muriel Range Monzogranite) and Twin Bonanza porphyry (The Granites Suite). These suites also display varying degrees of alteration.

17 Figure 9 Rb-Ba-Sr ternary diagram illustrating fractionated character of some suites using incompatible elements (after El Bouseily & El Sokkary 1975)

Suites generate linear to curvilinear geochemical trends on Harker diagrams (Figures10a to 10n) with varying degrees of scatter. Features attributable to individual suites will be discussed in following paragraphs. In general more mobile elements (K, Na, Rb, Sr) display a higher degree of scatter than those considered immobile (Ti, Al, Zr, Nd). Compare within suites Figures 10a, b, i, j with Figures 10f, g, l, m.

18 19 Figure 10 Harker diagrams illustrating major element and trace element behaviour in intrusives of the Tanami Region (a) TiO2, (b) Al2O3, (c) FeOT, (d) MgO, (e) CaO, (f) Na2O, (g) K2O, (h) Nb, (i) Zr, (j) Nd, (k) Y, (l) Sr, (m) Ba, (n) Rb

20 GENERAL FEATURES OF GRANITOIDS

Granites are a predominate component of the Tanami Region, as they are in most Australian Proterozoic orogenic terranes. The Palaeoproterozoic suites intrude Tanami Group, Mount Charles Group and Pargee Sandstone. Plutons are both discrete and multiple, zoned and unzoned, magnetic and non-magnetic. More mafic compositions, while generally absent in outcrop, are indicated by mafic microgranular enclaves and intermediate to gabbroic dykes and stocks in drillcore. Granites (sensu lato) are syn- orogenic to post orogenic. Foliation, where present, is defined by preferred orientation of crystals, plastic deformation of quartz (subgrain development and grain boundary migration leading to elongation parallel to foliation), and development of discrete deformation zones (Figure 11a). Foliation is interpreted to be magmatic through to solid state, developed as a result of both flow during emplacement and regional deformation during crystallization.

Figure 11a The development of discrete deformation zones (shears) within a biotite hornblende micro-quartz diorite (TAN99MH708R1, PTILOTUS, AMG 634677-7727907, XPL-FOV 8.0 mm)

21 Figure 11b Foliated granitic dyke, recrystallized biotite, quartz and alkali feldspar enveloping resistant plagioclase crystals (TAN99AD80R1, GRANITES, AMG 636183-772876, PPL-FOV 8mm)

Metamorphic grade increases around granite intrusions. Metasedimentary rocks become schistose, micaceous and spotted with biotite, muscovite, anadulsite (often retrogressed) and garnet, (Figure 12). At Apertawonga (AMG 556890-7762014) and MacFarlanes (AMG 549362-7755491) porphyroblasts of acicular andalusite were noted (mm to 4 x 1cm) with distinctive chiastolitic graphitic inclusions Contact aureole rock forms a resistant ridge that defines the intrusion shape in outcrop and in geophysical imaging. Contact aureoles are rarely more than 100m in width, indicating intrusion at upper crustal levels. Tourmaline and fluorite in granitoids and surrounding metasedimentary rocks indicate volatile rich fluids associated with intrusion.

Metasomatism has resulted in a variety of alteration products depending on fluid composition. Epidote, hornblende and titanite assemblages are associated with calcium metasomatism. Sericitization, albitization, kaolinization and corresponding leaching of elements are associated with alkali metasomatism. Potassic alteration occurred during late stage crystallization when temperatures were high. Subsequent alteration occurred during weak hydrothermal activity as temperature decreased.

22 Figure 12 Retrogressed andalusite porphyroblast in thermally metamorphosed Killi Killi Formation surrounding the Pipeline Monzogranite (PARGEE, AMG 506741-7813875) (XPL-FOV 8.0 mm)

To facillitate discussion, the felsic intrusive bodies are grouped into one broadly encompassing supersuite, the Coomarie Supersuite, comprising three similar yet distinct suites, Coomarie Suite, Inningarra Suite and The Granites Suite. In addition, there are unassigned minor intrusives (predominantly felsic dykes); plus two separate suites, the Winnecke Suite and Frederick Suite. Divisions were initially based on geophysical and macroscopic features, but have subsequently been divided according to petrographic and geochemical features. The remainder of this section describes distinctive features of individual suites.

The Coomarie Supersuite comprises non-magnetic to moderately magnetic, individual and composite plutons. Silica content varies between 53.90 wt % and, in altered samples, up to 83.10 wt %. The ASI indicates predominantly metaluminous character, peraluminosity increasing with alkali metasomatism. Alteration is variable, but predominantly potassic. They plot along a calc-alkaline trend on an AFM diagram (Figure 13). However, several intrusives exhibit post crystallization Fe enrichment attributable to weathering, which pushes values into the tholeiitic field.

23 Figure 13 Alkalis (Na2O+K2O) vs FeO*(FeO=FeO+0.8999Fe2O3) vs MgO (AFM) ternary diagram showing whole-rock compositions for Coomarie Supersuite intrusives (after [Irvine, 1971 #637]

The supersuite is Sr depleted and Y undepleted, has negative Nb, Ti and P anomalies, and elevated HFS elements. Granitoids are LREE enriched, with flat to slightly enriched HREE patterns. There is weak to strong differentiation within suites. Three individual suites are distinguished, Coomarie, Inningarrra and The Granites Suites.

COOMARIE SUITE

Intrusives of this suite were first described from geophysical features, particularly the large low non- magnetic anomalies within the large Browns Range Dome and Coomarie Dome, plus the irregularly shaped Frankenia Dome. These are distinctive features of TANAMI and The GRANITES, sheets. This suite has been extended to include felsic intrusives with low to moderate magnetic signatures in

MACFARLANE, TANAMI, GRANITES and PTILOTUS. Outcrop is deeply weathered and fresh material is obtained by drilling.

Silica for Coomarie Suite varies between 53.90 to 78.10 wt% (Appendix 3). However, only mafic microgranular enclaves and associated dykes and sills have values below 65 wt%. ASIs indicate intrusives are metaluminous to peraluminous (samples with ASI >1.2 have undergone varying degrees of calcic - sodic - potassic alteration) (Figure 5). The suite comprises fine to coarse grained, equigranular, granophyric to porphyritic, weakly foliated to massive muscovite-biotite syenogranite; leucocratic to

24 biotite monzogranite; leucocratic to biotite-hornblende granodiorite; leucocratic biotite tonalite, and biotite-quartz monzodiorite, with biotite micromonzogranite and microtonalite dykes, and microgranular enclaves. The dominant opaque mineral is magnetite (± ilmenite). Mafic microgranular and enclaves (tonalitic quartz diorite or trachyandesitic composition) and associated minor intrusives (basalt, gabbro diorite and serpentinized ultramafic) are common.

Primary mineral and normative assemblages indicate granitoids are predominantly I-type [Chappell, 1974 #264; White, 1977 #942], and display both oxidized and reduced character (Figure 6). Members display LREE enrichment, positive or no Eu anomaly, and flat to slightly enriched HREE (Figure 14a). Harker diagrams show TiO2, P2O5, Ba, Nb, and Sr all decrease, while Na2O, K2O, Rb and LREE increase with increasing SiO2 (Figure 10, Figure 14b). Sulphide mineralization was noted in the proximal aureole of TAN99DDH3.

Figure 14 Trace element abundances for least fractionated members of the Coomarie Suite (a) Chondrite normalized REE diagram [McDonough, 1992 #860](b) Multi-element primordial mantle normalized diagram [McDonough, 1995 #465]

Coomarie Dome Intrusives

(TAN99AD363R1-DDH3-AGSO#99496219, TAN99AD364R1-DDH5, TAN99AD365R1-DDH6)

Coomarie Dome is a broad elevated structural feature northwest of Tanami Mine, covered by Cainozoic sediments and encircled by low strike ridges of Gardiner Sandstone. BMR drilling during the 1970s found the dome to comprise pink medium grained two-mica leucocratic intrusives, minor mafic intrusives and extrusives, plus contact metamorphosed sedimentary sequences [Blake, 1974 #1037; Blake, 1979 #1039].

Geophysical images indicate a composite pluton [Slater, 2000 #1108]. NTGS drilling identified at least three previously undescribed felsic bodies. Modal analyses identified fine to coarse grained equigranular biotite monzogranite, granodiorite and tonalite (Figure 15). A magmatic foliation, defined by alignment of plagioclase and ferromagnesian minerals, is weakly developed. U/Pb zircon dating of core from TAN99DDH3 indicated crystallization at 1815 ± 4 Ma. Weathering extends 40 to 80 metres below the present surface. The highly micaceous nature of material within the weathered zone may indicate

25 greisenization of granite and country rock. Weathered granite is pervasively kaolinized and quartz veining is prolific.

Figure 15 Photomicrograph of TAN99DDH3R1, note igneous textures, abundant apatite and biotite (TANAMI, AMG 544939-7817879, PPL-FOV 8mm)

Frankenia Monzogranite (TAN99AD366R1-DDH7-AGSO#99496220)

Geophysical images in the Frankenia Dome also indicate a complex pluton [Slater, 2000 #1108]. Because of the lack of outcrop, a central position was targeted for drilling. The core recovered dark pink, fine to medium grained equigranular muscovite-biotite monzogranite to quartz monzonite. Incipient magmatic foliation is defined by alignment of biotite. Sericitization and saussuritization of feldspars, and presence of muscovite are considered secondary alteration products. Thin pegmatite veins cut the monzogranite in various orientations. Quartz infilled miarolitic cavities indicate the pluton intruded to shallow crustal level. U/Pb zircon dating of TAN99DDH7 indicates crystallization at 1805 ± 6 Ma.

Talbot South Monzogranite (TAN99AD367R1-DDH15-AGSO#99496224)

Geophysical images in the Talbot South area indicate several irregularly shaped plutonic bodies cut by numerous faults [Slater, 2000 #1108]. NTGS drilling in this area recovered pink medium to coarse grained equigranular biotite monzogranite that has been pervasively sericitized to depths of 100m. Chloritization of ferromagnesian phases has occurred along fine (cm – mm) shears within the granite. A

26 weak magmatic foliation is defined by alignment of biotite. U/Pb zircon dating for this pluton is in the final stages.

MacFarlane Granodiorite (TAN99MH707-AGSO#99496209)

Magnetic data and surface mapping indicate this granodiorite intrudes MacFarlane Peak Group southwest of Tanami Mine. Drilling indicates a foliated, pink to grey, fine to medium grained, hornblende-biotite granodiorite. This granodiorite provided a well-constrained U/Pb zircon date of 1809 ± 8 Ma that is taken as the crystallization age. Deformation was magmatic to subsolidus, and is defined by alignment of ferromagnesian phases and recrystallized quartz-feldspar zones. The pluton is cut by narrow (>0.5cm) undeformed aplitic veins.

Browns Range Dome Intrusives (AGSO#88495015, AGSO#88495018A, AGSO#88495016B)

Interpretation of magnetic data from Browns Range Dome in MALLEE indicates three magnetic domains. The largest, an area of low magnetic response, is similar to that displayed by granite in Coomarie Dome and Frankenia Dome. Field mapping noted several textural variants that were not sampled, including leuco-monzogranite with pervasive magmatic fabric that crosscuts fine grained foliated biotite monzogranite, and is in turn cut by undeformed pegmatite (Figure 16). U/Pb zircon dating from an outcropping granite from a high magnetic response zone in the southwestern corner of the area provided ages of 1805 ± 7 Ma and 1796 ± 7 Ma. This granite is porphyritic to megacrystic biotite monzogranite, previously correlated with The Granites Granites, but here placed with the Coomarie Suite which includes The Granites Granites.

27 Figure 16 Crosscutting relationships between Browns Range Dome intrusives, a foliated fine grained granitoid is cut by a leucocratic microgranitic aplite which in turn is cut by a undeformed pegmatite (MALLEE, AMG 000000-0000000)

A mingled granitoid and diorite was noted in BREADEN (Figure 17). At this locality fine to medium grained equigranular granite interfingers with a fine grained aphyric diorite. No chill margins were noted indicating both bodies were at elevated temperatures during mingling. The mafic intrusive weathers with pseudo-pillows, characteristic of diorite in this region. Both intrusives contain a tectonic foliation (60→120°) defined by pervasive cleavage and preferred mineral alignment.

28 Figure 17 Intermingled mafic/felsic intrusives (BREADEN, AMG 501171-7896463)

INNINGARRA SUITE

Inningarra intrusives have variable magnetic signatures, ranging from low to high, which make identification of individual plutons difficult where multiple intrusion has occurred. Initially defined by textural and spatial association, this suite now includes intrusives from INNINGARRA, MACFARLANE,

FRANKENIA, PTILOTUS and GRANITES. Outcrop varies from extremely weathered fault smeared patches to reasonably fresh, well jointed tors.

Silica content ranges from 64.30 wt% (hornblende-biotite tonalite) to 76.8 wt% (leucocratic monzogranite)(Appendix 3). Greissenized granite from Officer Hill displays elevated silica between 77.50 wt% and 83.10 wt%. Alumina saturation indices indicate metaluminous to weakly peraluminous character (Figure 5). Peraluminous samples are highly differentiated. Primary mineral and normative assemblages indicate predominantly I-type character. However, muscovite bearing differentiates could be S-type [White, 1977 #942].

29 The suite comprises fine to coarse grained, equigranular, granophyric, strongly foliated to massive, muscovite alkali-feldspar granite, together with muscovite syenogranite, leucocratic to biotite-hornblende monzogranite, leucocratic, biotite-hornblende granodiorite, and leucocratic, muscovite, hornblende biotite tonalite. Opaque minerals, where present are a magnetite-ilmenite mixture, commonly altered to haematite or titanite. Mafic microgranular enclaves and associated mafic intrusives are rare. Ferrous iron content indicates this suite is generally oxidized, although the least fractionated samples are reduced (Figure 6).

Inningarra Suite displaysLREE enrichment (increasing with silica content), negative to no Eu anomaly, slight MREE enrichment, with flat to slightly enriched HREE (Figure 18a). Chemistry indicates moderate Sr depletion and Y undepltion (Figure 18b). Harker diagrams indicate TiO2, FeOT, CaO, MgO and Sr all decrease, while Na2O, K2O, and Rb increase with increasing SiO2 (Figure 10). Mineralization was recorded in greissenized outcrop (TAN99AD289R1, AMG 567837-7706810).

Figure 18 Trace element abundances for the least differentiated Inningarra Suit Intrusives (a) Chondrite normalized REE diagram [McDonough, 1992 #860](b) Multi-element primordial mantle normalized diagram [McDonough, 1995#465}

Muriel Range Intrusives (TAN99AD104R1, TAN99AD258R1, TAN99AD259R1, TAN99AD261R1, TAN99AD268R3, TAN99AD269R1, TAN99AD270R1, TAN99AD277R1/R2)

Muriel Range intrusives comprise predominantly fine to medium grained equigranular to foliated biotite monzogranite, biotite-muscovite granodiorite and biotite-muscovite tonalite. Foliation is the result of magmatic flow but may be tectonically induced near major faults. Sheared outcrop was seen in fault contact with Muriel Range Sandstone to the south, and Dead Bullock Formation to the north. Drill chips to the north of Muriel Range indicate intrusion into Tanami Group, which is thermaly metamorphosed to micaceous schist.

30 Figure 19 Muriel Range Monzogranite outcrop, note central smeared schlieren (TAN99AD277R1, INNINGARRA, AMG 557450-7710301)

Grimwade Ridge Intrusives (TAN99AD118R1, TAN99AD120R1)

In this area, weathered granite interfingers with Tanami Group, forming low-lying isolated hills and hummocks. Cross cutting relationships noted in the field indicate several intermingled intrusive phases. Thin section indicates predominantly fine grained equigranular biotite monzogranite with minor leucocratic micro-monzogranitic dykes.

Murdoch Cliffs Intrusives (TAN99AD310R1, TAN99AD311R1)

Granite outcrop in the Murdoch Cliffs area 100 m northwest of Muriel Range Sandstone fault scarps in INNINGARRA forms raised margins around several large salt pans. Outcrop at this locality represents the most southerly outcrop of granite on TANAMI. Weathering precludes chemical analysis. The granite is a well jointed, foliated, medium to fine grained hornblende - biotite monzogranite to granodiorite. Foliation is defined by preferred alignment of ferromagnesian minerals and quartz ribbon development indicating submagmatic deformation in the solid state.

31 Figure 20 Well jointed intrusive outcrop, Murdoch Cliffs area (TAN99AD310R1, INNINGARRA, AMG 584159-7708048)

Officer Hill Intrusives (TAN99AD286R1, TAN99AD289R1/R2, TAN99AD290R1/R2, TAN99AD291R1, TAN99AD298R1)

This composite zoned intrusive body to the south of Officer Hill in INNINGARRA, comprises medium grained biotite monzogranite to leuco-monzogranite, and coarse to medium grained muscovite syenogranite and alkali feldspar granite. Greissenization of the most differentiated intrusive phase has occurred with associated mineralization (see later section). Pyrite replaces some ferromagnesian phases, and opaques are commonly oxidized to hematite. Thick (1m wide) tourmaline pegmatites are common throughout the outcrop.

32 Figure 21 Greisenized granitic outcrop, Officer Hill area (INNINGARRA AMG 567837 to 568013 - 7706810 to 7706670)

Bunkers Tonalite (TAN99AD80R1, TAN99AD124R3/R4, TAN99MH708-AGSO#99496210)

This granitoid intrudes and thermally metamorphoses Killi Killi Formation in Bunkers opencut near The Granites Gold Mine (AMG 641373-7725952). It is described from outcrop and drillcore as medium to coarse grained equigranular biotite granodiorite and hornblende-biotite tonalite. Tonalite displays pervasive magmatic foliation defined by alignment of ferromagnesian phases and incipient deformation of quartz. Localized strain results in intense deformation and chloritization along well developed shear zones (see Figures 11a and b). A U/Pb zircon date of 1815 ± 4 Ma is inferred as the crystallization age. Tonalite is crosscut by undeformed aplite dykes, inferred to be distal apophyses of the Granites Monzogranite, part of The Granites Suite.

Watertower Tonalite (TAN99AD114R1-AGSO#99496213)

This non-magnetic intrusive is expressed as isolated, relatively fresh boulders, unearthed during construction of a pipeline along Watertower Road (AMG 648327-7729490. It is medium to coarse grained equigranular hornblende-biotite tonalite, with pervasive foliation defined by alignment of biotite and hornblende and weak elongation of quartz indicating magmatic to submagmatic deformation. The previously obtained 1840 ± 11 Ma age [Cooper, 1997 #804] correlates well with inherited populations

33 recorded for the most recent U/Pb zircon data, which gives a younger age of 1821 ± 4 Ma for crystallization.

THE GRANITES SUITE

The Granites Suite was invoked to classify spatially associated intrusives in GRANITES and has been expanded to include intrusives from MACFARLANE, PTILOTUS and INNINGARRA. Apart from The Granites Monzogranite, TAN99AD330R1, which outcrops as well jointed tors south of The Granites Gold Mine (AMG 643157-7724822), all other intrusives are identified from drillcore. Intrusives display low to moderate magnetic signatures.

Silica content varies between 65.90 wt% (biotite tonalitic enclave) and 73.00 wt% (biotite monzogranite) (Appendix 3). ASI indicates metaluminous I-type character, which is supported by primary mineral and normative assemblages (Figure 5)[Chappell, 1974 #264; White, 1977 #942]. One strongly peraluminous sample displayed pervasive alkali metasomatism. Apart from this predominantly medium grained biotite monzogranites, the suite also includes fine to coarse grained, equigranular to porphyritic (megacrystic), foliated to massive, leucocratic monzogranite, and biotite granodiorite. Spatially associated aplitic dykes have also been included with this suite. These display characteristics indicative of contaminated residual fluids ( tourmalinized garnet muscovite micro-syenogranite TAN99AD344R1). Mafic microgranular enclaves are common and have biotite tonalite composition (TAN99AD353R3).

The intrusives of this suite generally straddle the oxidized - reduced boundary with Fe3+/(Fe3++ Fe2+) values ~ 0.3 – 0.4 (Figure 6). The Granites Suite displays LREE enrichment, negative Eu anomaly, MREE enrichment, with flat HREE (Figure 22a). Similar to other Coomarie Supersuite intrusives, The Granite Suite is Sr depleted and Y undepleted (Figure 22b). Harker diagrams indicate relatively elevated Nb, Zr, Nd and the hydrothermally altered nature of Twin Bonanza Porphyry (TAN99AD352, TAN99AD353) (Figure 10). The small number of unaltered samples make it difficult to determine trends within this suite. However, with increasing silica, there seems to be an increase in LREE, K2O and

Rb, and a decrease in TiO2, MgO and FeOT (Figure 10).

Figure 22 Trace element abundances for least fractionated members of The Granites Suite (a) Chondrite normalized REE diagram [McDonough, 1992 #860](b) Multi-element primordial mantle normalized diagram [McDonough, 1995 #465]

34 The Granites Monzogranite (TAN99AD330R1)

This subcircular intrusion with a moderate magnetic response has a diameter of 4 km and is slightly elongated in an east-west direction (possibly indicating north-south flattening). It is predominantly medium grained variably porphyritic biotite monzogranite, with minor aplitic syenogranitic apophyses. Foliation, where present, is due to magmatic flow. Crystallization for this intrusive is 1795 ± 5 Ma.

Figure 23 The Granites Granite outcrop from the Tanami Road (AMG 643157-7724822)

Ptilotus Granodiorite (TAN99MH705R1-AGSO99496207)

This foliated coarse grained weakly porphyritic biotite granodiorite was sampled by drilling a weakly magnetic pluton identified from aeromagnetic imagery. The granodiorite intrudes Dead Bullock Formation and has a strongly zoned foliation indicative of magmatic solid-state deformation. Pervasive green-pink colouration is due to epidote and chlorite alteration. U/Pb zircon dating provides an 1805 ± 5 Ma age, similar to that obtained for other intrusives of this suite.

35 Figure 24 Photomicrograph of Ptilotus Monzogranite, note zoned plagioclase with sericitized core (top left), recrystallization along shear zone (bottom left to top right) and patch perthite in alkali feldspar (bottom right) (TAN99MH705R1, AMG 617604-7754844, XPL-FOV 8mm)

Twin Bonanza Porphyry (TAN99MH706R1-99496208, TAN99AD350R1, TAN99AD351R1, TAN99AD352, TAN99AD353)

The small intrusive known as Twin Bonanza prospect is located 57 kms west-southwest of Tanami Mine. Drillcore samples indicate coarse grained equigranular biotite monzogranite, with large, euhedral, perthitic alkali feldspar megacrysts. The intrusive has undergone pervasive sericitization and saussuritization and is cut by numerous epidote-chlorite veins. Gold mineralization was detected along small quartz filled fractures. The U/Pb zircon age of this intrusive (1802 ± 8 Ma), places it within error of the previously obtained age of 1787 ± 5Ma [Cooper, 1997 #804].

UNASSIGNED FELSIC INTRUSIVES

Minor intrusives in the Tanami Region include numerous porphyritic aplitic and microgranitic dykes and sills. These crosscut dominant structural fabrics at The Granites and Tanami mine areas, and are believed coeval and possibly cosanguinous with younger intrusive plutons previously discussed (The Granites Suite, The Coomarie Suite). Petrography indicates these minor intrusives are pervasively altered. Both silica and potassium values are high (SiO2 between 70.00 and 77.19 wt %; K2O between 3 and 4 wt %), with corresponding low CaO and Na2O. Least differentiated samples indicate LREE enrichment, no Eu anomaly, and flat HREE pattern (Figure 25a). As with Coomarie Supersuite, these intrusives display

36 strong Sr depletion, with Y undepleted or enriched (Figure 25b). Porphyritic quartz syenite has been described from outcrop and drillcore in MACFARLANE (TAN99MH682R1, AMG 536703-7751247) and is also included here.

Figure 25 Trace element abundances for the least fractionated unassigned felsic dykes (a) Chondrite normalized REE diagram [McDonough, 1992 #860](b) Multi-element primordial mantle normalized diagram [McDonough, 1995 #465]

Hurricane Dacite Dyke (TAN99AD1R1)

This cream coloured aphanitic to porphyritic dacite dyke, cuts folded Mt Charles Formation in Hurricane opencut, Tanami Gold Mine. The dyke displays well developed chill margins 10-15 cms wide and is 3-4 metres thick (Figure 26a). Phenocrysts comprise recrystallized embayed quartz, ferromagnesian phases replaced by pyrite, and altered euhedral feldspar set in a sericitized felsitic matrix. Phenocrysts displaying alignment with dyke margins indicate magmatic flow during emplacement (Figure 26b).

37 Figure 26a Dacite dyke cutting folded Tanami Group, Hurricane Pit (TAN99ADR1, TANAMI, AMG 576011-7793857)

Figure 26b Dacite dyke detail showing flow alignment of altered feldspar phenocrysts, Hurricane Pit (TAN99AD1R1, TANAMI, AMG 576011-7793857)

Pargee Rhyolite (TAN99MH551R1- AGSO99496206, TAN99AD250R1/R2)

This 30-50 cm wide rhyolite sill, with pervasive fracture cleavage, has been folded with Pargee Sandstone in PARGEE, approximately 50 kms west-southwest of Tanami Mine (Figure 27). The rhyolite is fine grained, porphyritic with altered feldspar and minor embayed quartz crystals in a sericitized matrix. To the north (AMG 523050-7782195) the sill becomes a dyke that cuts stratigraphy. This rock was sampled for U/Pb zircon dating and two inherited populations were identified (2500-2200 Ma and ~1860 Ma) from a small number of recovered zircons.

38 Figure 27 Pargee Rhyolite sill/dyke (TAN99AD250R1, PARGEE , AMG 523085-7782195)

FREDERICK SUITE

The Frederick Suite comprises granite plutons with a distinctive moderate to highly magnetic character and low gravity response, that form ellipsoidal bodies in the far western part of PARGEE and

MACFARLANE. Non-magnetic responses and breaks in the magnetic image are interpreted as jointing and faults. Several small well defined elliptical plutons with non magnetic character in MACFARLANE,

INNINGARRA and FRANKENIA have been included within this suite. Intrusives immediately west of the WA - NT border have similar geophysical signature to those described within the Frederick Suite. Drill sampling by BMR and ESSO during the 1970s also indicates a similar petrographic character [Blake, 1973 #5].

Within this suite silica varies from 63.30 wt% (quartz syenite) to 71.60 wt% (biotite monzogranite)

(Appendix 3). Values of 57.40 and 78.20 wt% SiO2 were obtained for a dioritic mafic microgranular enclave and an altered aplitic dyke respectively. Intrusives are metaluminous and considered I-type, based on primary mineral and normative assemblages (Figure 5) [Chappell, 1974 #264; White, 1977 #942]. This suite plots along a calcalkaline trend on an AFM diagram (Figure 28). This suite is predominantly reduced, but some of the differentiated members have an oxidized character (Figure 6).

39 Figure 28 Alkalis (Na2O+K2O) vs FeO*(FeO=FeO+0.8999Fe2O3) vs MgO (AFM) ternary diagram showing whole-rock compositions for the Frederick Suite (after [Irvine, 1971 #637])

Plutons comprise undeformed (excluding magmatic fabrics), medium to coarse grained, equigranular, granophyric to porphyritic, leucocratic quartz syenite, syenogranite, biotite-hornblende monzogranite, and hornblende-biotite granodiorite. Hornblende-biotite tonalite, biotite-hornblende microdioritic enclaves, and leucocratic aplitic and pegmatitic dykes are common. High sodic content has pushed perthitic alkali feldspar megacrystic biotite-hornblende monzogranite into the trondhjemite field of diagrams that use normative anorthite-albite-orthoclase values.(Figure 29).

Figure 29 Normative orthoclase-anorthite-albite ternary diagram (after [Barker, 1979 #1032])

40 This suite displays LREE enrichment, positive Eu anomaly, and flat HREE (Figure 30a). It has undepleted Sr and depleted to undepleted Y character, with strong Nb and weak Ti and P negative anomalies (Figure 30b).

Figure 30 Trace element abundances for Frederick Suite Intrusives (least fractionated) (a) Chondrite normalized REE diagram [McDonough, 1992 #860](b) Multi-element primordial mantle normalized diagram [McDonough, 1995 #465]

Abundant microgranular mafic enclaves noted in outcrop and core have a different geochemical signature. They represent disseminated mingled mafic magmas that have mechanically mixed with the host granite. Alteration (sulphides in calcite-epidote-chlorite veins and fine quartz veins) was noted disseminated in cored plutons and is discussed later.

Pipeline Granodiorite (TAN99AD361R1/R2/R3-TAN99DDH1R1/R2/R3)

This non-outcropping intrusive forms a large ellipsoidal, highly, magnetic northwest striking pluton

(18kms long and 9kms wide) in PARGEE (AMG 510588-7799989). Non-magnetic linear responses within the pluton reflect pervasive fractures and faults. The northern and eastern margins of the granite are intensely magnetic. The granite has a low gravity response of -270 µms-2. Drillcore obtained by NTGS drilling indicate medium grained, equigranular biotite - hornblende granodiorite with abundant biotite - hornblende tonalite, and dioritic mafic microgranular enclaves (Figure 31). The pluton is surrounded by thermally metamorphosed andalusite bearing Killi Killi Formation. A variable magmatic foliation is defined by alignment of plagioclase, biotite and hornblende. U/Pb zircon analysis of this intrusive is in progress

41 Figure 31 Photomicrograph of Pipeline Monzogranite illustrating igneous texture, note prismatic apatite enclosed in hornblende and euhedral hornblende (TAN99AD361-TAN99DDH1, MACFARLANE, AMG 510588-7799989, PPL-FOV 8mm)

Mavericks Monzogranite (TAN99AD362R1/R2-TAN99DDH2R1/R2-AGSO#99496221)

This granitoid, which straddles the boundary between MACFARLANE and PARGEE and the WA border (AMG 505529-7786509) is defined by an ellipsoidal highly magnetic shape. It outcrops intermittently over several kilometres as weathered, well jointed low-lying hills. The pluton has dimensions of 7 x 5 km and is slightly less magnetic and not as dense (-µ240 ms-2) as Pipeline Granodiorite, possibly indicating it is not as thick.

Sampled by part of NTGS drilling this rock is equigranular hornblende-biotite monzogranite and granodiorite. Outcrop and drillcore display pervasive magmatic foliation defined by alignment of ferromagnesian minerals, feldspars and abundant ellipsoidal mafic microgranular enclaves (Figure 32). Oblique quartz veins, measured in drillcore, are cut by fine vertical quartz veins laced with sulphides (pyrite-pyrrhotite-arsenopyrite?). Sulphides are also visible as disseminated blebs within granitoid. Both mafic microgranular enclaves and schistose metasedimentary enclaves were noted in outcrop. Mafic microgranular enclaves sampled from drill core have variable quartz content, with little or no alkali feldspar, and high concentrations of hornblende and biotite (up to 60%), and can be modally classified as tonalitic and dioritic (Figure 32). A crystallization age of 1801 ± 4 Ma was obtained by U/Pb zircon dating.

42 Figure 32 Photomicrograph of Mavericks Monzogranite, illustrating hornblende biotite monzogranite/enclave margin, note titanite (centre) and euhedral hornblende (centre right) (TAN99AD362-TAN99DDH2, MACFARLANE, AMG 505539-7786509, PPL-FOV 8mm)

Apertawonga Monzogranite (TAN99AD370R1-TAN99DDH23R1)

This non-magnetic poorly defined pluton outcrops poorly to the south of Tanami Mine (AMG 556501). It is hornblende biotite monzogranite with strong to weak magmatic foliation defined by aligned feldspar, biotite and hornblende. Outcrop is dominated by silica rich aplitic and pegmatitic dykes and quartz veins. The monzogranite intrudes Tanami Group, forming an andalusite-sulphide rich hornfelsic aureole. U/P6 zircon dating of this granitoid is in progress.

Inspiration Peak Monzogranite (TAN99AD371R1A/B-TAN99DDH28R1)

This intrusion is a small semi-circular pluton with a non-magnetic signature, surrounded by strongly magnetic thermally metamorphosed Dead Bullock Formation which defines the pluton dimensions. This granitoid does not outcrop and was sampled by drilling. The granitoid is undeformed coarse to medium grained biotite monzogranite (Figure 33). Drillcore is cut with numerous randomly oriented quartz veins, aplitic and pegmatitic dykes. Zircon dating of this granitoid is in progress.

43 Figure 33 Photomicrograph of Inspiration Peak Monzogranite illustrating igneous texture, note crosshatch twinning indicating microcline inversion, sutured quartz margins, subhedral partially sericitized plagioclase and biotite (TAN99AD371-TAN99DDH28, FRANKENIA, AMG 601692- 7738217, XPL-FOV8mm)

MacFarlane Peak Monzogranites (TAN99AD368R1-TAN99DDH20R1, TAN99AD369R1-TAN99DDH21R1)

These intrusives form non-magnetic small elliptical plutons with well defined magnetic aureoles in

MACFARLANE (AMG 535385/534800-7759208/7751850). In drillcore they range in composition from medium grained megacrystic biotite monzogranite to equigranular biotite monzogranite. Large (>3cm) perthitic alkali feldspar megacrysts display resorbed irregular margins mantled by oligoclase (rapakivi texture) (Figure 34a and b). Generally plutons are undeformed. However, alignment of feldspar phenocrysts and ferromagnesian minerals defines a magmatic foliation near pluton margins, which is ascribed to flow during emplacement. Zircon dating of this granitoid is in progress.

44 Figure 34a MacFarlane Peak monzogranite outcrop illustrating megacrystic character and rapakivi texture (TAN99AD369-TAN99DDH21, MacFarlane AMG 534800-7751850)

Figure 34b Resorbed perthitic alkali feldspar megacryst margin with sericitized plagioclase overgrowth (rapakivi texture), note zoned plagioclase in top left quadrant and euhedral hornblende with prominent cleavage (bottom centre)(TAN99AD369-TAN99DDH21, MACFARLANE, AMG 534800-7751850, XPL-FOV 8mm)

45 Walnut Granodiorite (TAN99AD123R1-AGSO#99496216)

This intrusive has a moderate magnetic signature and outcrops as abundant fresh tors southeast of Dead Bullock Soak, in the Grimwade Ridge area (AMG 628848-7707509). Modally the intrusive is variably porphyritic, medium grained, equigranular, hornblende - biotite granodiorite. Numerous leucocratic aplitic and pegmatitic dykes crosscut the outcrop. The localized alignment of alkali feldspar phenocrysts and ferromagnesian minerals is attributed to flow during emplacement. A sample is currently undergoing U/Pb zircon analysis.

Nora Range Monzogranite (TAN99AD174R1, TAN99AD175R1)

This highly magnetic intrusive outcrops in west MACFARLANE (AMG 509427-7756531), and has previously been described as part of the composite Lewis Granite which outcrops extensively west of the WA - NT border [Blake, 1973 #1036]. Despite deep and pervasive weathering, the granite can still be identified as foliated (magmatic), coarse to medium grained, equigranular, biotite monzogranite unconformably overlain by Gardiner Sandstone (Figure 35a and b).

Figure 35a Nora Range Monzogranite (TAN99AD175, MACFARLANE, AMG 509427-7756531)

46 Figure 35b Nora Range Monzogranite overlain by Gardiner Sandstone ( TAN99AD174, MACFARLANE, AMG 509459-7756584)

Slatey Creek and Lewis Granites (WA - NT) (TAN99AD372R1)

These highly magnetic granites have been previously described [Blake, 1973 #1036; Blake, 1979 #1039]. A sample of the Orion Granodiorite (TAN99AD372R1, AMG (84) 441757-7813666), part of the composite Lewis Granite, was analysed along with the previously described rocks of the Frederick Suite to compare similarities. This fine to medium grained equigranular biotite granodiorite resembles Nora Range, Mavericks and Pipeline Monzogranites, with comparable mesoscopic features, geophysical character, textures and modal analyses. The analysis for Orion Granodiorite is included in all Frederick Suite plots.

WINNECKE SUITE (PGW, PLWA, PN)

Multiple intrusives with magnetic and non-magnetic character identified from geophysics are interpreted as members of the Winnecke Suite, which includes the extensively outcropping Winnecke Granodiorite and Granophyre [Traves, 1955 #1080], in the north of TANAMI extending south into WILSONS CREEK. Outcrop varies from highly weathered to unweathered spheroidal tors. This suite also includes extrusives of Mount Winnecke Group, Nanny Goat Volcanics and coeval bimodal volcanics. SiO2 varies between

69.70 wt% and 76.80wt% (Appendix 3). Volcanics exhibit silicification (SiO2 up to 88.70 wt% in one sample). Mafic volcanics range between 50.10 wt% and 63.50 wt% SiO2. Intrusives are predominantly

47 metaluminous, with one altered peraluminous and peralkaline example (Figure 5). Based on primary mineral and normative assemblages, this suite is I-type [Chappell, 1974 #264; White, 1977 #942]. Winnecke Suite intrusives and extrusives (felsic and mafic) plot with a tholeiitic trend on an AFM diagram (Figure 36).

Figure 36 Alkalis (Na2O+K2O) vs FeO*(FeO=FeO+0.8999Fe2O3) vs MgO (AFM) ternary diagram showing whole-rock compositions for the Winnecke Suite (after [Irvine, 1971 #637])

Felsic members of this suite range from reduced to strongly oxidized (Figure 6), and are modally classified as fine to coarse grained equigranular, porphyritic, granophyric, hornblende-biotite syenogranite, biotite monzogranite and hornblende-biotite granodiorite. Magnetite is the common opaque mineral, with minor ilmenite. Felsic volcanics include porphyritic to aphyric dacite and rhyolite. Porphyritic variants, both intrusive and extrusive, comprise embayed β-quartz and euhedral plagioclase set in finer grained, equigranular, often recrystallised mixture of quartz, alkali feldspar and plagioclase.

This suite is Sr, Ba, Ti, and P depleted and Y undepleted, with LREE enrichment, a negative Eu anomaly, and flat but elevated HREE (Figure 37a and b).

48 Figure 37 Trace element abundances for Winnecke Suite Intrusives (least fractionated) (a) Chondrite normalized REE diagram [McDonough, 1992 #860](b) Multi-element primordial mantle normalized diagram [McDonough, 1995 #465]

The small number of analysed samples make it difficult to determine elemental trends in Harker diagrams. However, analyses display relatively high HFS abundances, and with increasing silica content felsic intrusives and extrusives display decreasing TiO2, FeOT, MgO, CaO and Nb, and increasing Na2O (Figure 10).

Winnecke Monzogranite (TAN99AD243R1-AGSO#99496214)

This sample was obtained from outcrops of spheroidal boulders, low hillocks and well-jointed tors in BIRRINDUDU (AMG 631951-7901189). At this locality the monzogranite outcrops as undeformed, medium to coarse grained, equigranular, granophyric hornblende granodiorite (Figure 38a and b). Miarolitic cavities infilled with quartz chlorite epidote and (rarely) zeolite are common. Mafic microgranular enclaves are present and outcrop is cut by several generations of aplitic dykes.

Winnecke Suite granitoids visibly intrude Mount Winnecke Group volcanics [Blake, 1972a #1034; Blake, 1972b #1035; Blake, 1979 #1039]. Features such as miarolitic cavities, porphyritic character and geochemical affinity show Winnecke intrusives were emplaced at shallow levels and are subvolcanic correlatives of Mount Winnecke volcanics. It is difficult to distinguish thick porphyritic lavas from intrusives in the absence of outcrop.

49 Figure 38a Winnecke Monzogranite outcrop (TAN99AD243, AMG 631951-7901189)

Figure 38b Winnecke Monzogranite illustrating textural character (TAN99AD243, AMG 631951- 7901189)

50 Recent U/Pb dating provided 1825 ± 5 Ma for crystallization of this intrusive body which is older, but within error of previous ages [Blake, 1979 #1039]. This date also correlates well with ages of the Mount Winnecke and Nanny Goat Volcanics (1824 ± 5 Ma and 1816 ± 7 Ma respectively).

Figure 39 Granophyric textured variant, Winnecke intrusives (TAN99AD241R3, AMG 633902- 7897208, XPL-FOV 8mm)

Nanny Goat Volcanics and Mount Winnecke Group (eg TAN99AD51R1/R2/R3/R4, TAN99AD157R1, TAN99AD169R1, TAN99AD239R1, TAN99AD240R1, TAN99ADMH45R1, TAN99MH73R1, TAN99MH177R1)

Previously separated, these volcanic assemblages are grouped within this report because of similar petrographic, chemical and temporal features. Nanny Goat Volcanics extend south into WILSONS CREEK from postulated volcanic sources to the north in BIRRINDUDU [Blake, 1972a #1034; Blake, 1972b #1035; Blake, 1979 #1039]. As discussed in Hendrickx et al (2000), Nanny Goat Volcanics outcrop extensively west and east of Lajumanu Road in WILSON CREEK, consistant of several distinct volcanic units. Volcaniclastic sandstone at AMG 612692-7870505 previously part of Supplejack Sandstone are included in Nanny Goat Volcanics owing to similar composition and structure.

Rock types include porphyritic quartzo-feldspathic ignimbrite (Pn1), which has a conventional U/Pb age of 1816 ± 7Ma [Page, 1995 #1067. This is possibly gradational into porphyritic feldspathic ignimbrite (Pn2) to the west of Lajamanu Road (between AMG 612420-7887125 and 610785-7887400) however, contact relationships are obscured. Rhyolite lava (Pn3) could be crystal or lithic ash. Weathered textures are difficult to decipher. Rhyolite is porphyritic (1-15% phenocrysts) with some samples displaying flow

51 banding and autobrecciation. Rhyolite gives a conventional U/Pb age of 1800 ± 13 Ma [Page, 1995 #1067]. Intermingled, generally aphyric amygdaloidal basalt (Pn4) will be dealt with further in this section.

Composition is consistently rhyolitic to dacitic. Porphyritic character is ubiquitous but variable (between 1 and 50% phenocrysts). Phenocryst content is predominantly quartz, with felspar in varying amounts (ratios of 2:1 to 5:1 (Pn1) to 1:10 (Pn2) have been recorded). Quartz is generally β-form and can be embayed or fragmental, with minor dynamic recrystallization, involving subgrain development and grain boundary migration (Figure 40). Feldspar is subhedral to euhedral and variably sericitized. Albite twins, indicative of sodic plagioclase remain. Ferromagnesian minerals are generally haematite, pyrite, chlorite, or sericite pseudomorphs after biotite, amphibole and (rarely) pyroxene. Lithic clasts are common and comprise volcanic, granophyric, granitic and country rock clasts. The matrix comprises a devitrified felsitic mixture of feldspar and quartz, exhibiting mineral alignment which defines magmatic flow. Devitrification and alteration generally masks original textures. However, squashed pumice, eutaxitic texture and glass shards indicate ignimbritic origin for some volcanics (Figure 41).

Figure 40 βββ-quartz habit and haematite pseudomorph after biotite in fine grained felsitic matrix (TAN99AD163, AMG 611166-7887307, XPL-FOV8mm)

Contacts between felsic and mafic volcanics indicate complex mingling relationships. Aphyric basalt interfingers with porphyritic dacite and at one locality is brecciated within a dacitic lithic rich matrix indicating possible remobilization of the dacite-rhyolite host (Figure 42a and b).

52 Figure 41 Devitrified squashed pumice and crystal fragments (TAN99AD51R1, AMG 612540- 7882304)

Figure 42(a) Interfingering dacite and basalt (TAN99AD167, AMG 612492-7882131)

53 Figure 42b Brecciated basaltic clasts in felsic lithic rich matrix (TAN99MH177, TAN99AD157, AMG 613993-7887316)

Well jointed, massive Mount Winnecke Group volcanics (Plwa) outcrop extensively to the southeast in BIRRINDUDU, extending south into TANAMI (AMG 638452-7897856) where they are faulted to the west against Winnecke Suite granite [Hendrickx, 2000 #1056]. Volcanics are predominantly weakly magnetic, porphyritic dacite and rhyolite. Phenocrysts (10 –25%) comprise sericitized feldspar (alkali feldspar and plagioclase), chlorite pseudomorphs after pyroxene, magnetite, minor anhedral angular or embayed quartz, and iron oxides. The matrix comprises fine grained, devitrified mixture of plagioclase, alkali feldspar and quartz. Textures give no clue to deposition and these rocks which could be thick lava, pyroclastics or hypabyssal intrusive. A U/Pb zircon date of 1824 ± 5 Ma is considered to be the crystallization age [Page, 1995 #1067].

FELSIC VOLCANIC ROCKS

Numerous interbedded felsic volcanics occur within Tanami Group and overlying stratigraphic units [Blake, 1972a #1034; Blake, 1972b #1035; Blake, 1973 #1036; Blake, 1974 #1037; Blake, 1975 #1038; Blake, 1979 #1039; Hendrickx, 2000 #1056]. However, pervasive alteration, particularly of thin tuffaceous beds, makes identification difficult.

54 Mavericks Volcanics (TAN99AD26R1/R2/R3)

Thick 1-2m feldspathic rich interbedded units are folded with Killi Killi Formation in the Mavericks area

(MACFARLANE, AMG 507688-7790463). These extrusives comprise fine to medium grained feldspar laths with zones of anhedral recrystallized quartz and quartz-alkali feldspar intergrowths. Occasional clusters of weathered feldspar phenocrysts (1%) also occur. REE patterns are irregular showing both flat and enriched LREE patterns, a slight positive Eu anomaly, with flat HREE pattern (Figure 43a). The primordial mantle-normalized diagram reflects depletion in mobile elements with negative anomalies for 3+ Pb, Ba, K, Na, Sr, and P (Figure 43b). With SiO2 content ~65 wt%, Fe2O3T (total iron as Fe ) values >10 wt%, and a marked lack of alkalis, these could represent more mafic extrusives that have undergone iron enrichment and silicification.

Figure 43 Trace element abundances for interbedded volcanics in the Mavericks area (a) Chondrite normalized REE diagram [McDonough, 1992 #860](b) Multi-element primordial mantle normalized diagram [McDonough, 1995 #465]

MacFarlane Volcanics (TAN99AD321R1, TAN99AD322R1)

These porphyritic quartzo-feldspathic dacite and rhyolite extrusives form discrete units 0.5 - 2m thick, interbedded with MacFarlane Peak Group siltstone and sandstone in MACFARLANE (AMG 538190- 7751554). Phenocrysts (10%) are predominantly sericitized plagioclase with minor weathered ferromagnesian minerals. The matrix comprises plagioclase, alkali feldspar, and minor quartz. Foliation defined by alignment of phenocrysts and matrix minerals, is the result of compaction during lithification. It is inferred to have been originally deposited as subaerial ash fall tuff.

55 Nora Range Porphyry (TAN99MH468R1-AGSO#99496218, TAN99AD177R1)

This volcanic porphyry is spatially associated with outcropping Nora Range Monzogranite and Killi Killi

Group in MACFARLANE (AMG 509223-7756443), and has been included with the later. It is difficult to determine whether the rock is a sill, dyke or lava flow. Phenocrysts comprise about 25% of this rock being predominantly alkali feldspar, with plagioclase, embayed β-quartz and altered ferromagnesian minerals. Euhedral to subhedral forms indicate pseudomorphs after pyroxene and biotite. The matrix is a mixture of feldspar and quartz.

Figure 44 Trace element abundances for Nora Range volcanic porphyry (a) Chondrite normalized REE diagram [McDonough, 1992 #860](b) Multi-element primordial mantle normalized diagram [McDonough, 1995 #465]

Trace elements display enriched LREE and slight negative Eu anomaly, with flat HREE when normalized to chondritic abundances (Figure 44a). The multi-element primordial mantlenormalized diagram shows negative anomalies for Ba, Nb, Sr, Ti and P (Figure 43b). SiO2 content is 70.0 wt% and the rock plots as rhyolite in all classification diagrams. U/Pb zircon dating is in progress.

MAFIC ROCKS

Mafic rocks are found within most stratigraphic levels, and from a mineral prospective viewpoint, provide a potential source for base metals. Geophysical interpretation indicates mafic rocks are ubiquitous [Slater, 2000 #1070; Slater, 2000 #1071; Slater, 2000 #1072; Slater, 2000 #1073; Slater, 2000 #1108]. The mafic rocks of the Tanami region can be divided into plutonic and volcanic associations. Sample localities of the rocks discussed are listed and plotted in Appendix 1. Literature and company data is utilised where applicable. As with felsic rocks, petrographic analysis was carried out on all mafic samples. A tabulation of detailed information can be found in Appendix 2.

56 CHEMICAL AND MODAL CLASSIFICATION

Modally, mafic rocks are peridotite, pyroxenite, gabbro, norite, dolerite, amphibolite, basalt, diorite and quartz diorite. Contact relationships identify intrusive dykes, sills, plutons, stocks, extrusive lava (subaerial and subaqueous) and breccia.

Chemical methods are used to classify mafic rocks because the aphyric nature precludes modal classification. Using total alkalis versus silica, samples plot from picro-basalt through to dacite (Figure 45). High silica samples represent differentiation from more mafic compositions and, in some instances, silicification.

Figure 45 Total alkalis versus silica (TAS) diagram illustrating character of Tanami region mafic rocks (after [Le Bas, 1986 #772])

GENERAL PETROGRAPHIC AND GEOCHEMICAL FEATURES

Textures range from coarse to fine grained, aphyric, vesicular, amygdaloidal and glomeroporphyritic. Foliation is defined by alignment of hornblende and plagioclase. Amphibolites are thermally metamorphosed basalt within contact aureoles. Where there is strong anisotropy, shearing may have instigated recrystallization and resultant mineral elongation. Igneous textures predominate, however petrography indicates some calcic alteration and silicification. Uralitization is common, replacing primary pyroxene and hornblende. Previously unpublished whole rock analyses for mafic rocks from the Tanami Region are presented in Appendix 3.

Most samples display iron-enrichment, plotting within the tholeiitic field on an AFM diagram (Figure 46). Mg# (100(Mg2+/(Mg2+ + Fe2+) (total iron recast as Fe2+), a measure of differentiation within mafic magmas, varies between 26 and 71 for unaltered samples, indicating direct mantle derivation. CIPW

57 normative values indicate saturation with normative diopside, hypersthene and olivine. Quartz normative samples are altered and have low MgO wt % (<5 wt%). All samples plot in the subalkaline field in the Ne-Or-Q ternary diagram using normative values (Figure 47).

Figure 46 Alkalis (Na2O+K2O) vs FeO*(FeO=FeO+0.8999Fe2O3) vs MgO (AFM) ternary diagram showing whole-rock compositions for mafic rocks of the Tanami Region (after [Irvine, 1971 #637])

Fgure 47 Ne–Or–Q ternary diagram using normative values to determine alkalinity (after [Irvine, 1971 #637])

58 MAFIC PLUTONIC ROCKS

Mafic intrusives include dolerite dykes, mafic microgranular dioritic or tonalitic enclaves in granitoids, and small isolated stocks in TANAMI and THE GRANITES. However, numerous unexposed mafic intrusives are indicated by geophysics [Slater, 2000 #1070; Slater, 2000 #1071; Slater, 2000 #1072; Slater, 2000 #1073; Slater, 2000 #1108. With the presence of dolerite hosted mineralization in the Talbot South area, these should be exploration targets. Monzodioritic bodies have been reported from drillcore in the western part of THE GRANITES and TANAMI [Blake, 1979 #1039]. Gabbro has been encountered in drill core from the Coomarie Dome and Frankenia Dome (Blake, 1974 #35). Gabbro has also been recorded cutting granite across the border in WEBB [Blake, 1973 #1036]. Metaperidotite, dunite and metapyroxenite have been described from outcrops along the souhwestern margin of Coomarie

Dome in PARGEE (J Waters, D Powers (NFM) pers com), and diorite intermingles with granite in

BREADEN.

Timing of mafic intrusion is inferred from stratigraphic relationships to have occurred prior to and during major Tanami deformation at about 1840 Ma. [Hendrickx, 2000 #1056; Vandenberg, 2001 #834]. Intermingling indicates some magmatism was coeval with granite intrusion, between 1830 – 1790 Ma. Radiometric dating of differentiated dolerite (U/Pb SHRIMP on baddeleyite) may constrain some events.

Ptilotus and The Granites Dolerites (TAN99AD74R1, TAN99AD342R1, TAN99AD347R1, TAN99MH709R1-AGSO#99496215)

Dolerite sills are exposed in pit walls at The Granites, where they intrude Killi Killi Group. They weather to distinct large greenish purple spheroidal forms (GRANITES, AMG 661256-7748650). Intrusives at this locality are predominantly fine to coarse grained dolerite sills. They crosscut major fold structures but are deformed by later shearing and faulting [Hendrickx, 2000 #1056]. Primary assemblages comprise clinopyroxene (uralitized to actinolitic hornblende), plagioclase and magnetite. Ferromagnesian minerals display ophitic texture, poikilitically enclosing all other minerals. Plagioclase (An 35-90%) is variably sericitized with evidence of minor albitization. Amphibolite is totally recrystallized, displaying pervasive foliation defined by mineral alignment, and no orignial igneous texture remains. Mineral assemblages comprise hornblende, plagioclase, biotite and magnetite, with minor quartz.

Silica varies between 45.08 wt% and 54.90 wt% (Appendix 3). One foliated dyke containing 67.40 wt%

SiO2 is intermediate. Mg#, varies between 20 and 71. Amphibolite has lowest Mg # and appears differentiated relative to dolerite. Dolerite exhibits LREE enriched REE pattern, with negative or no Eu anomaly and relatively flat HREE pattern (Figure 48a). They are moderately to strongly Sr and P depleted and Y undepleted (Figures 48b).

59 Figure 48 Trace element abundances for The Granites dolerite and amphibolite (a) Chondrite normalized REE diagram [McDonough, 1992 #860](b) Multi-element primordial mantle normalized diagram [McDonough, 1995 #465]

Dead Bullock Soak dolerite (TAN99AD332R1, TAN99AD333R1/R2, TAN99AD334R1/R2, TAN99AD335R1, TAN99AD336R1/R3, TAN99AD337R1, TAN99AD339R1, TAN99AD340R1, TAN99AD342R1/R2/R3)

At Dead Bullock Soak dolerite sills (locally named End it all Dolerite and Coora Dolerite, [Smith, 1998 #1075] are affected by the main Tanami deformation and can be up to 200m thick [Hendrickx, 2000 #1056; Vandenberg, 2001 #834]. They vary from fine to coarse grained and are foliated, equigranular, porphyritic, poikilitic dolerite to quartz diorite. Primary minerals are plagioclase (An 60-85%), clinopyroxene, hornblende and magnetite. Foliation is defined by mineral alignment. Alteration invloves uralitization and saussuritization with minor albitization (Figure 49). Previous studies also identify potassium rich assemblages with affinities to shoshonitic lamprophyres at both Dead Bullock Soak and The Granites [Garnaut, 1995 #1114].

Silica content is between 45.20 wt% and 58.90 wt% (Appendix 3). Samples with lower values have undergone marked calcic metasomatism. Mg# varies between 28 and 71 (average 54). Thick dolerite sills can be differentiated internally and grade from dolerite to quartz diorite. Trace element normalized diagrams distinguish the two groups (Figures 50, 51a and b). Coora dolerite displays flat REE with positive to no Eu anomaly (Figure 50a), Sr, Nb and Y undepletion with negative P anomaly (Figure 50b). End it all dolerite exhibits LREE and MREE enrichment, with a slight to no negative Eu anomaly and flat HREE pattern (Figure 51a). It also displays Sr, P, Ti, Nb and K negative anomalies relative to primitive mantle and is enriched in U and Th relative to Coora dolerite(Figure 51b).

60 Figure 49 Uralitized pyroxene and hornblende in Coora dolerite (TAN99AD342, MACFARLANE, AMG 597408-7729164, XPL-FOV 8mm)

Figure 50 Trace element abundances for Coora dolerite, Dead Bullock Soak (a) Chondrite normalized REE diagram [McDonough, 1992 #860](b) Multi-element primordial mantle normalized diagram [McDonough, 1995 #465]

61 Figure 51 Trace element abundances for End it all dolerite, Dead Bullock Soak (a) Chondrite normalized REE diagram [McDonough, 1992 #860](b) Multi-element primordial mantle normalized diagram [McDonough, 1995 #465]

Borefield Road Suite (Pgb)

The Borefield Road Complex is a circular composite intrusion 6km in diameter, situated 4kms north - northeast of The Granites (GRANITES, AMG 643844-7730358). The complex does not outcrop and is known only from drill core and high magnetic response. It has a moderate Bouguer gravity response of -190 to -250 µms-2. The highest part of the anomaly is positioned on the southwestern portion of the granite. Simli+ar geophysically interpreted circular bodies in PTILOTUS and INNINGARRA are correlatives of the Borefield Road Complex (Figure 2)[Slater, 2000 #1073; Slater, 2000 #1108].

Silica varies between 45.10 wt% and 52.70 wt % (Appendix 3). Mg# is between 40-52 (average 47), indicating little differentiation. This suite does not show iron enrichment on AFM but has a calc-alkaline character (Figure 46). Rock types include pyroxenite, augite norite, pyroxene-hornblende-biotite diorite/gabbro, biotite-clinopyroxene-hornblende diorite/gabbro, porphyritic microdiorite, and hornblende-biotite tonalite and granodiorite. Primary minerals include plagioclase (An 20-55%), biotite, hornblende, clinopyroxene and magnetite. Biotite forms large anhedral pools which poikilitically enclose other minerals (Figure 52). Hornblende appears primary and secondary, often uralitizing clinopyroxene (augite). Magnetite is abundant (up to 10 wt%), explaining the high magnetic signature. Apatite and zircon form abundant prismatic inclusions in biotite, which is reflected in high P and Zr (Figure 53b)(Appendix 3). The suite displays medium to coarse grained, cummulate and subophitic textures. Alteration includes uralitization, minor serictization, and locally potassic metasomatism. Metasedimentary xenoliths were noted in drillcore.

62 Figure 52 Poikilitic texture, anhedral biotite enclosing plagioclase, hornblende, abundant apatite and zircon (GRANITES, AMG 643844-7730358, PPL-FOV 8mm)

Figure 53 Trace element abundances for Borefield Road intrusives (a) Chondrite normalized REE diagram [McDonough, 1992 #860](b) Multi-element primordial mantle normalized diagram [McDonough, 1995 #465]

This suite displays LREE enrichment, which increases with increasing SiO2, indicative of calc-alkaline character and crustal assimilation (Figure 53a). Intrusives have positive or no Eu anomaly, flat HREE (Figure 53a), depleted K, Nb, and Sr, and are Y and Ti undepleted (Figure 53b).

63 MAFIC VOLCANIC ROCKS

Extrusive mafic rocks are inferred from magnetic signature throughout the Tanami Region [Slater, 2000 #1070; Slater, 2000 #1071; Slater, 2000 #1072; Slater, 2000 #1073; Slater, 2000 #1108]. Overlying Palaeozoic Antrim Plateau Volcanics tend to mask signals from older volcanics.

Mount Charles Formation basalt (Pcb)

(TAN99AD1R2, TAN99AD4R2, TAN99AD229R1, TAN99AD230R1, TAN99AD328R1, TAN99AD329R1-AGSO#99496212)

The three basaltic lithofacies within Mount Charles Formation - massive, brecciated basalt, and pillow basalt [Tunks, 1996 #1081] - all exhibit similar petrographic and chemical features. Massive basalt forms 20m thick units in sharp contact with adjacent sediments [Tunks, 1996 #1081]. Brecciated basalt is interpreted as autobrecciation along the margins of massive flows [Tunks, 1996 #1081]. Pillows with fine grained chill margins, are associated with massive basalt in several Tanami Mine pits, indicating shallow subaqueous extrusion (Figure 54). The basalt-sediment contact is recognised as the locus for deformation and hydrothermal fluid flow [Hendrickx, 2000 #1056; Vandenberg, 2001 #834].

Basalt is fine to very fine grained and equigranular to weakly porphyritic. Primary minerals comprise variably albitised plagioclase laths (An ~60%), interstitial augite, and fine grained magnetite (Figure 55). Smaller phenocrysts comprise pseudomorphs of chlorite after pyroxene or olivine and occasional euhedral magnetite. The matrix is a devitrified mixture of chlorite and epidote. Amygdales are common, filled with calcite, chlorite and quartz.

Figure 54 Pillow lavas in Mount Charles Formation, pillow shape indicates folded Tanami Group is younging upwards at this locality (TAN99AD4, AMG 571797-7787735)

64 Figure 55 Typical aphyric basalt with sericitized plagioclase laths, chloritized pyroxene/olivine (TAN99AD4, AMG 571797-7787735, PPL-FOV 8mm)

SiO2 varies between 41.60 and 57.90 wt%, with Mg# between 37 and 55 (Appendix 3). Some alteration is indicated by high LOI values. Least altered samples are low-K tholeiite (K2O <~ 0.2 wt%) (see later for further discussion). Basalt exhibits LREE enrichment with no Eu anomaly and relatively flat HREE pattern (Figure 56a). Least altered samples exhibit flat primordial mantle normalized patterns, with moderate Sr and P depletion (Figure 56b).

Figure 56 Trace element abundances for Mount Charles Formation basalts (a) Chondrite normalized REE diagram [McDonough, 1992 #860](b) Multi-element primordial mantle normalized diagram [McDonough, 1995 #465]

Highly magnetic bands with associated high Bouger responses in the Tanami mine area are interpreted as basalt interbedded and deformed with turbiditic sequences [Hendrickx, 2000 #1056]. Individual flows

65 can be traced for several kilometres. Extensive fine to medium grained, foliated amphibolite also outcrops at Officer Hill and MacFarlanes Peak, where it represents basalt thermally metamorphosed by nearby granite (AMG 538063-7752243 and 566953-7710916 respectively). These amphibolites are similar chemically to Tanami Mine basalts.

Nanny Goat Volcanics basalt (Pn4) (TAN99AD52R2/R3/R4, TAN99AD54R1, TAN99AD57R1/R2/R3, TAN99AD64R1/R2/R3, TAN99AD144R1, TAN99AD153R1, TAN99AD159R2, TAN99AD168R1, TAN99AD325R1/R2, TAN99AJC36R1)

Basalt of the Nanny Goat Volcanics outcrops in the Crusade exploration area in WILSONS CREEK, and based on geophysical interpretation, is inferred to extend north into BIRRINDUDU [Slater, 2000 #1070]. Rock types include fine grained, foliated, aphyric to weakly porphyritic, amygdaloidal basalt and basaltic andesite and sub-ophitic textured dolerite (Figure 57). Primary minerals are variably sericitised plagioclase laths (An 55%), pyroxene and olivine (replaced by chlorite and haematite). The matrix is chlorite, epidote, magnetite and ilmenite. The contact with rhyolitic lava at Crusade Hill (AMG 612975- 7883170) and to the south (AMG 612630-7882190) is complex. Brecciated basalt intruded as dykes or sills into lithified rhyolite which appears to have locally remobilized. The contact hosts gold mineralization at these localities [Hendrickx 2000 # 1056] Silica content varies between 50.10 and 63.50 wt%, with Mg # between 26-45 (Appendix 3), indicating a relatively evolved character for Nanny Goat Volcanic basalts.

Figure 57 Irregular amygdale infilled with calcite and quartz in fine grained basalt (TAN99AD64, AMG 612783-7883150, XPL-FOV 8mm)

66 DISCUSSION OF PETROGENESIS

This section examines the data presented, and infers possible petrogenesis for felsic and mafic igneous rocks of the Tanami Region. Both mafic and felsic rocks cover a broad range in silica composition, which could indicate a variety of protoliths, differentiation processes, and alteration styles (Figure 57).

Felsic rocks range between 65 and 75 wt% SiO2 (mean =69), mafic rocks range between 45 and 55 wt%

SiO2 (mean = 49).

Figure 58 Histograms displaying silica content for (a) mafic rocks and (b) felsic rocks of the Tanami Region

GRANITE PROTOLITHS

Granitoids are derived from partial melts of variable compositions, and subsequently change by various differentiation processes. The oxidized character (Fe3+/(Fe3++ Fe2+) = 0.4) indicates that Coomarie and Frederick suites, at least, are crustally derived [Wones, 1989 #1116]. The metaluminous nature of all analysed granitoid samples (ASI >1.1), and increasing ASI with SiO2 content, supports classification as I- type. They are derived from an igneous infracrustal source that has not undergone weathering at the Earth surface [Chappell, 1974 #264; Chappell, 1988 #689]. The presence of hornblende with titanite, magnetite, apatite and zircon, also support I-type classification [White, 1977 #942; Whalen, 1988 #1088].

A comparison of Na20 and K20 for samples with a silica range between 60 and 75 wt%, indicates that many intrusives from all suites have values that fall outside the field defined for the 1880-1840 Ma granite suite recognized by Wyborn et al (1988). Least differentiated members of suites represent parental partial melts which are likely to retain characteristics that identify the nature of protoliths.

67 Proposed parental partial melt compositions for each suite, based on least differentiated, unaltered analyses are as follows:

Coomarie Suite – 62.30 wt% SiO2, biotite granodiorite/tonalite;

Inningarra Suite – 65.76 wt% SiO2, biotite-hornblende tonalite;

The Granites Suite – 67.12 wt% SiO2, biotite-granodiorite;

Frederick Suite – 65.00 wt% SiO2, biotite-hornblende granodiorite/tonalite; and

Winnecke Suite – 69.70 wt% SiO2, hornblende-biotite granodiorite.

The combined features of the least fractionated members of Coomarie, Inningarra, and The Granites suites, provide the characteristics closest to parent melt for the Coomarie Supersuite which is hornblende- biotite tonalite.

Figure 59 K2O versus Na2O for Tanami granitoids - marked field corresponds to that for Proterozoic granites (after [Wyborn, 1988 #1089])

Relatively low Rb and high Sr support this proposition, and further indicate granitoids do not represent differentiated products from an unexposed tonalite or diorite. The absence of significant tonalite and diorite outcrops in the Tanami Region does not preclude its presence. The almost ubiquitous presence of mafic microgranular enclaves and associated minor mafic intrusives (basalt, gabbro, diorite and serpentinized ultramafic), coincident with felsic intrusion, indicates mafic material at depth during time of intrusion. This provides a potential mantle derived source for felsic intrusives, and if they are not direct derivatives, then there is potential for hybridization.

Isotopic analysis (Sm/Nd), currently in progress should clarify crustal-mantle relationships further. Most granitoids investigated show only localized ductile strain and have obviously been emplaced late in the deformation history of the Tanami Region [Hendrickx, 2000 #1056; Vandenberg, 2001 #834].

68 Geochronology to date, indicates intrusion occurred between 1830 to 1790 Ma, which is later than the main phase of the Barramundi Orogeny. The 1801 ± 4 Ma age for the Mavericks Granite and the generally undeformed nature of Frederick Suite (excluding magmatic fabrics) indicate this suite occurred quite late in the orogenic history of the Tanami Region. Abundant pegmatitic and aplitic dykes which represent late residual fluid phases of the granitoids, cross cut the main structural elements, further showing the minor intrusives coincided with post-tectonic intrusive phases (The Granites Suite and Frederick Suite).

Intrusion into cogenetic volcanic piles at shallow crustal levels and bimodal character of magmas suggest Winnecke suite may be associated with caldera type volcanism (see Figure 31 [Hendrickx, 2000 #1056]). A subaqueous environment is inferred due to the close association between felsic lava and subaqueous sedimentary rocks [Blake, 1975 #1038]. Timing of volcanism and intrusion (1825 -1815 Ma), has no direct equivalents in the Tanami region. However, widespread felsic volcanism and granite intrusion occurred throughout the North Australian Craton during this period (1830-1800 Ma). Pervasive but variable sericitization and saussuritisation of granites indicates hydrothermal alteration. Notably, the most altered samples occur in the Tanami mine and Winnecke areas.

Chondrite and mantle-normalized trace-element diagrams indicate two contrasting granitoid groups:

• Sr, Ti, Nb, P depleted, Y undepleted or slightly depleted, with negative to no Eu anomaly; and • Sr undepleted, Ti, Nb, P and Y depleted, with positive to no Eu anomaly.

This distinction has been regarded previously as indicating source inheritance [Tarney, 1987 #1142; Wyborn, 1988 #1089]. Negative Y anomalies have been interpreted to indicate residual garnet in the source region [Wyborn, 1992 #14; Wyborn, 1996 #1090]. However, REE are partitioned by hornblende and garnet similarly in equilibrated silicic magmas, and a negative Y anomaly could reflect presence of hornblende or garnet [Barker, 1979 #1032; Martin, 1986 #1118]. Negative Ti and Nb anomalies, present in all analysed granitoid samples, indicate a residual titaniferous phase, which will have a marked effect of LREE and MREE in equilibrated melts [Green, 1986 #1122, Green, 1987 #1121]. Negative P anomalies infer the presence of residual apatite. Sr depletion infers plagioclase is present in the source [Tarney, 1987 #1142]. The trace element chemistry implies partial melting occurred at different depths. Sr depleted, Y undepleted granitoids with residual plagioclase were generated at more shallow levels in the crust than the Sr undepleted, Y depleted garnet-hornblende residual granitoids, possibly sourcing different protoliths in response to different stimuli.

69 Subsequent magmatic and subsolidus processes can progressively modify the chemical and mineralogical features of the primary assemblages, obscuring evidence of protolith determination. Commonly invoked magmatic differentiation processes that account for compositional variation within suites include: • Hybridization – mixing of granite magma with material from a different source will generate a compositional spectrum either by magma mixing or crustal assimilation. Hybridization will generate a linear trend on variation diagrams; • Fractional crystallization – continuous removal of crystals from a crystallizing liquid resulting in residual liquids and solid rich cumulates will generate an exponential curve on variation diagrams; • Restite unmixing – progressive separation of residual solids and the melt [White, 1977 #942; Chappell, 1987 #918]. Unmixing of the two components allow the protolith to be constrained and generates linear trends on variation diagrams [White, 1977 #942; Chappell, 1987 #918].

Inningarra Suite exhibits a marked curve in compatible versus incompatible plots indicating fractional crystallization has influenced composition of the suite. The scatter on most variation diagrams suggests fractional crystallization or crustal contamination may have played a part in evolution of most granitoid suites. Approximately linear trends indicate either hybridization or restite unmixing. Least evolved granites lack evidence of restitic minerals, and distinctly calcic cores within zoned plagioclase are absent [Chappell, 1987 #918]. Mafic microgranular enclaves which support the restite unmixing model, display features indicative of magma mixing (igneous texture, quartz ocelli and acicular apatite, [Vernon, 1983 #301]). Monzogranite of the Frederick Suite also displays rapakivi texture, in some cases indicative of magma mixing [Stimac, 1992 #680; Andersson, 1994 #1130]. Detailed trace element modelling, isotopic analysis, and comparison with experimental data will allow tighter constraint of differentiation processes and protolith characteristics. Tanami granitoids are similar in character to those of the Halls Creek Orogen (1835-1805 Ma)#[Blake, 1998 #1040; Sheppard, 1999 #671].

70 MAFIC SOURCES

Mafic rocks are subalkaline to tholeiitic and exhibit a broad range in Mg # (26-71) (Figure 60).

Figure 60 Aluminium versus normative An% to determine character of mafic magmas (after [Irvine, 1971 #637])

Two dolerite samples from Browns Range and Borefield Road Suite display characteristics transitional from tholeiite to calc-alkaline (Figure 60). Dolerite generally exhibits features typical of continental flood basalt, MgO wt% about 7, significant LREE enrichment, and weak negative Eu anomaly [Thompson, 1983 #871; MacDougall, 1988 #1135]. Mount Charles basalt exhibits less LREE enrichment, more elevated HREE and distinctively low K in unaltered samples, and are considered low-K tholeiite [MacDougall, 1988 #1135].

There is no chronological control on mafic rocks. However stratigraphic and structural relationships indicate they pre-date and post-date the main deformation event (1845-1840 Ma), and are in some T instances synchronous with granite intrusion (1825-1790 Ma). Nd model ages ( NdDM) obtained from limited isotopic work in this area indicate separation from the mantle about 2.6Ga [Garnaut, 1995 #1114]. 87 86 Dolerite and diorite generally retain primitive Sr/ Sr and εNd T signatures (0.7026 and 1.0 respectively). Petrographic similarities allow correlation with Woodward Dolerite in the Halls Creek Orogen, and Zamu Dolerite in the Pine Creek Orogen [Needham, 1988 #1066; Blake, 1998 #1040](see Figure 2 [Hendrickx, 2000 #1056]).

TECTONIC SETTING

Two tectonic models have been proposed for the Australian Proterozoic:

1. Australia was cratonised by the early Proterozoic and crust was added by vertical accretion [Etheridge, 1987 #1053]. Evidence used in support of this hypothesis includes similar post Archaean tectonstratigraphic histories, compositionally uniform felsic magmatism, plus few rocks with

71 intermediate compositions or ocean crust affinity [Etheridge, 1987 #1053; Etheridge, 1990 #1054; Wyborn, 1988 #1089; Wyborn, 1992 #14]. Intracontinental tectonics were driven by plate tectonics which, because of thick continental lithosphere, allowed compressional and extensional stress to propagate further into continental interiors than in the Phanerozoic [Solomon, 1994 #1134; Etheridge, 1994 #1055]. Extension with accompanying basin development and mafic volcanism culminated with the Barramundi Orogeny (1870-1850 Ma), and extensive I-type felsic plutonism and volcanism of uniform character [Etheridge, 1987 #1053; Wyborn, 1987 #1136; Wyborn 1988 #1089; Etheridge, 1994 #1055]. The presence of a high velocity seismic layer underneath Australian Proterozoic infers major underplating, which consequently provides source material for voluminous granite production [Finlayson, 1987 #1145; Drummond, 1982 #1137; Drummond, 1988 #1144; Wyborn, 1992 #18]. The Barramundi Orogeny was followed by further extension, characterised by basin development with basal bimodal volcanics and quartz-rich clastics [Rutland, 1976 #535; Rutland, 1990 #1138].

2. By 1800 Ma three major cratons are thought to have developed from numerous Archaean nuclei, with final amalgamation of the Australian continent occurring between 1300 and 1000 Ma [Myers, 1990 #771; Myers, 1996 #770]. Each craton records individual orogenic events, and amalgamation caused repeated tectonism along southern margin of Northern Australian Craton [Myers, 1996 #770]. Evidence in support of this hypothesis includes the presence of igneous rocks with oceanic affinities [Tyler, 1990 #1141], possible oceanic crust and development of foreland basins associated with several orogens [Myers, 1990 #771; Myers, 1994 #1140; Myers, 1996 #770; Cooney, 1995 #1139], and inferred subduction with associated mineralisation [Solomon, 1994 #1134].

Granite chemistry is often equivocal with regard to tectonic setting. Winnecke Suite and Coomarie Supersuite display chemistries indicative of shallow crustal melts (<45 kms). The bimodal nature of Winnecke Suite volcanics implies intrusion or extrusion within an extensional tectonic regime [McPhie, #1143]. The distinctive chemistry of Frederick Suite intrusives implies a deeper level for partial melting, variable protolith composition, and a thickening of the continental crust (>45 kms) by the time of intrusion at around (1800 Ma).

The abundance of Sr depleted, Y undepleted intrusives in the Tanami Region is in accord with the underplating model previously proposed [Etheridge, 1987 #1053; Etheridge, 1994 #1055; Wyborn, 1987 #1136]. However, geochronology indicates that partial melting and felsic intrusion and volcanism occurred at a much later stage (1830-1790 Ma). The later Frederick Suite also indicates a change in intrusive style perhaps reflecting changes in protolith and tectonic regime. Tectonic discrimination diagrams using immobile elements (Ti, Zr, Nb, Y, REE), constrained by known tectonic setting, have been applied to Tanami samples [Pearce, 1973 #1112; Pearce, 1984 #505] (Figures 61and 62).

72 Figure 61 Discrimination diagram to determine tectonic setting, Rb versus Y + Nb for felsic rocks (after [Pearce, 1984 #422])

Samples plot predominantly in the volcanic arc field, with scatter into the syn-collision and within-plate settings (Figure 61). On the Ti-Zr-Y diagram, mafic samples cluster in oceanic floor (B), and calc- alkaline (B/C) fields, with scatter into the within-plate field (Figure 62). This reflects the calcalkaline signature of Borefield Suite mafics and the low-K tholeiite character of Mount Charles basalt [Pearce, 1973 #1112]. There is also marked separation between dolerite from Dead Bullock Soak and the End it all Dolerite, which displays more evolved character (Figure 62).

In the absence of evidence to the contrary and based on regional stratigraphy, this study supports the findings of previous authors that Tanami Group dolerite sills intruded into developing basins during initial extension and represent equivalents of intrusive continental flood basalt [Etheridge, 1987 #1053]. Mount Charles basalt and metamorphosed equivalents formed subsequently during the Leichardt rifting event (1810-1740Ma?) and represent continental rift tholeiite [Etheridge, 1994 #1055; Tunks, 1996 #1081].

73 Figure 62 Discrimination ternary diagram to determine tectonic setting for mafic rocks, Zr-Ti/100- Y*3 (after [Pearce, 1973 #1112])

MINERALIZATION

FELSIC MAGMATISM AND MINERALIZATION

The sheer volume of felsic magmatism inevitably places economic ore deposits in close proximity to felsic intrusives. Within the focus of this report this spatial association of felsic intrusions with gold is examined with regard to consanguinity and genetic control. Mineralization associated with granitoids forms two categories:

• granophile type deposits; and • porphyry type deposits.

Granophile deposits are rich in Be, B, Li, P, F, Cl, CO3, Sn, W, U, and Mo [Strong, 1988 #1123]. Granophile deposits usually concentrate near granitoid contacts and zone outwards into country rock from Sn, W, As, U into U, Ni, Co, Cu, Pb, Zn, Ag, Au to Fe and Sb sulphides. Deposits are generally hosted by muscovite leucogranite, with a strong correlation between deposit characteristics and depth of emplacement – for example greisen formation between 6-12 km depth [Strong, 1988 #1123]. Water content is the most important compositional variable, controlling the physical and chemical behaviour of felsic melts [Burnham, 1979 #190].

In H2O saturated conditions partial melts occur deeper in the crust and granophile elements concentrate in residual liquids, lowering the viscosity and crystallization temperature, prolonging differentiation and allowing intrusion to shallower levels [Strong, 1988 #1123].

74 In H2O undersaturated conditions partial melting results in intermediate amphibole-biotite compositions, shallower intrusion and, if circulating groundwater is present, porphyry type deposits. Porphyry type deposits are associated with Cu, Cu and Mo, Cu and Au mineralisation. Deposits are usually large tonnages and low grade. There are recorded occurrences of Proterozoic deposits of this type, but diagnostic features are masked by metamorphism and subsequent alteration [Kirkham, 1972 #1146; Gaál, 1979 #1147]. Intrusives are usually differentiated and of intermediate compostion. They intrude to shallow depths (often subvolcanic) in various tectonic settings [Sangster, 1979 #1148].

Two end members are considered: • Orthomagmatic – 95% of hydrothermal fluids are derived from the crystallising magma; • Convective – majority (~95%) of fluids are derived from ground water (meteoric, connate or seawater). The wide spectrum of characteristics displayed by Cu porphyry deposits reflects numerous variables and stages in the evolution of a porphyry hydrothermal system. Generally magmas are emplaced between 1 - 2 kms depth. There are distinctive alteration zones ranging from potassic, phyllic (sericite dominated), through to propylitic (chlorite dominated), and there is associated brecciation indicating release of volatiles [McMillan, 1988 #1124].

MINERALIZATION ASSOCIATED WITH FELSIC MAGMATISM

Tanami felsic intrusives do not exhibit strong signatures of mineralization of either of the above styles, particularly the reduced, unfractionated and unaltered samples. However, possible hosts include the subvolcanic Winnecke Suite and Twin Bonanza porphyry of The Granites Suite, which have potassic, phyllic and propylitic alteration features associated normally with porphyry type deposits. The Inningarra Suite has greisenization and anomalously high Sn and W abundances

Assay results from the NTGS drilling programme indicate anomalous Au and Pt associated with two granite suites, Coomarie and Frederick Suites, plus a basalt overlying granite in TAN99DDH3. The basalt is assigned to the Tanami Group, but could also be associated with ultramafic intrusives (AMG 595600-7805800). Pyrite-pyrrhotite-arsenopyrite mineralization was noted in Mavericks granite core (TAN99AD362-TAN99DDH2 - AMG 505529-7786509) associated with small mafic clots disseminated throughout granite, and as blebs along quartz veinlets. In the Frankenia Monzogranite sulphides occur (TAN99AD366-TAN99DDH7 - AMG 586504-7778075) as disseminated cubic crystals, and in association with adjacent thermally metamorphosed sedimentary rock (TAN99AD363-TAN99DDH3 - AMG 544939-7817879). Assay results are listed in Table 3. Full analyses are listed in Appendix 3.

75 Sample # Classification Ru Rh Pd Ir Os Pt Au

TAN99DDH1R1 Frederick Suite 2<1<5<1<23<1

TAN99DDH2R1 Frederick Suite 3 <1<5<1<2<1<1

TAN99DDH2R2 Frederick Suite 4<1<5<1<22<1

TAN99DDH3R1 Coomarie Suite 2 <1<5<1<2<1<1

TAN99DDH3R5 Tanami Group ( basalt) 5<110<1<2156

TAN99DDH5R1 Coomarie Suite 4 <1<5<1<25 6

TAN99DDH6R1 Coomarie Suite 7<15<1<23<1

TAN99DDH7R1 Coomarie Suite 5 <1<5<1<26 6

TAN99DDH15R1 Coomarie Suite 7 <1<5<1<24 7

TAN99DDH20R1 Frederick Suite 7 <1 5 <1 <2 5 6

TAN99DDH21R1 Frederick Suite 4 <1<5<1<22 6

TAN99DDH23R1 Frederick Suite 5 <1 5 <1 <2 12 <1

TAN99DDH28R1 Frederick Suite 4 <1<5<1<2<15

Table 3 Assay results for NTGS drilling programme (in ppb)

Officer hill intrusives, to the southwest of Dead Bullock Soak Officer (TAN99AD286R1, TAN99AD290R1/R2; TAN99AD298R1), exhibit significant Sn, Ta, W. This peraluminous (S-type) granite exhibits extreme differentiation with greisenization expressed as muscovite rich pods of quartz, ± cassiterite, fluorite and tourmaline. (TAN99AD289R1/R2, TAN99AD291R1) (Figure 63). Elemental concentrations are displayed in Table 4. Similar Sn-Ta-W mineralization has been recorded in the Halls

Creek Orogen (San Sou Monzogranite), and in the northern Arunta (Anningie Tin Field in MOUNT PEAKE and Wolfram Hill in MOUNT DOREEN).

Figure 63 a and b REE chondrite-normalized and multi-element primordial mantle normalized diagram for Officer Hill intrusives and greisenized granite illustrating extreme fractionation and altered signature.

76 Figure 64 Greisenized granite (TAN99AD289R1, INNINGARRA, AMG 567837-7706810, FOV 8 mm)

Sample # Sn W Ta Nb Ga Zn Rb

TAN99AD289R1 270 80 46 89 57 190 3800

TAN99AD289R2 230 57 21 50 29 73 1800

TAN99AD290R1 21 380 8 56 32 21 800

TAN99AD291R1 105 1000 7 50 26 93 1350

Table 4 Officer Hill intrusives and greisenized granite indicating significant element abundances (ppm)

CONCLUSIONS

While the majority of Tanami Region granites display characteristics that indicate it unlikely they will host significant mineralization, this study indicates several potentially economic possibilities. Alteration haloes and associated trace element signatures may indicate potential for porphyry and granophile styles. Current NTGS investigations into the nature, source and timing of quartz veining and Au mineralisation should clarify mineralization relationships in the Tanami Region. Fluid inclusion, oxygen and Re-Os isotope studies of the fluids and associated granite intrusives will provide information in the near future. Results indicate a magmatic component to the mineralized fluids. Felsic intrusives provide magmatic fluids and the thermal environment to drive hydrothermal systems. Timing is a significant factor in mineralisation potential of granites. Current information indicates the younger intrusives of the area may have been important in this respect, particularly those of the Frederick and Granites suites. It is also

77 likely that granite plutons have acted as massive buttresses that influenced stress fields, and allowed gold to deposit in late structures in low-presure zones around plutons.

78 Appendix 1 Sample list and locality map

Table A1 Sample numbers, locality, brief description and AMG coordinates (datum 66) Sample No Locality Description Easting Northing TAN99AD1R1 Tanami Mine felsic intrusive 576011 7793857 TAN99AD1R2 Tanami Mine mafic intrusive 576011 7793857 TAN99AD4R1 Tanami Mine metasediment 571797 7787735 TAN99AD4R2 Tanami Mine mafic extrusive 571797 7787735 TAN99AD4R3 Tanami Mine felsic intrusive 571797 7787735 TAN99AD8R1 Apertawonga contact aureole 556890 7762014 TAN99AD12R1 Pendragon conglomerate 537355 7794289 TAN99AD17R1 Apertawonga felsic intrusive 556548 7762086 TAN99AD26R1 Mavericks intermediate volcanic 507688 7790463 TAN99AD26R2 Mavericks intermediate volcanic 507688 7790463 TAN99AD26R3 Mavericks intermediate volcanic 507688 7790463 TAN99AD30R1 Mavericks intermediate volcanic 506460 7789764 TAN99AD31R1 Mavericks contact aureole 506355 7786878 TAN99AD31R2 Mavericks contact aureole 506355 7786878 TAN99AD34R1 Mavericks contact aureole 506438 7786741 TAN99AD48R1 Tanamai tuffaceous mudstone 518605 7799597 TAN99AD49R1 Mount Frederick contact aureole 506741 7813875 TAN99AD50R1 Mount Frederick conglomerate 505869 7812177 TAN99AD51R1 Crusade felsic extrusive 612540 7882304 TAN99AD51R2 Crusade felsic extrusive 612540 7882304 TAN99AD51R3 Crusade felsic extrusive 612540 7882304 TAN99AD51R4 Crusade felsic extrusive 612540 7882304 TAN99AD52R1 Crusade felsic extrusive 612543 7882241 TAN99AD52R2 Crusade mafic extrusive 612543 7882241 TAN99AD52R3 Crusade mafic extrusive 612543 7882241 TAN99AD52R4 Crusade mafic extrusive 612543 7882241 TAN99AD54R1 Crusade mafic extrusive 612986 7883197 TAN99AD57R1 Crusade intermediate volcanic 615142 7883901 TAN99AD57R2 Crusade intermediate volcanic 615142 7883901 TAN99AD57R3 Crusade intermediate volcanic 615142 7883901 TAN99AD58R1 Winnecke felsic intrusive 621429 7909839 TAN99AD58R2 Winnecke felsic intrusive 621429 7909839 TAN99AD58R3 Winnecke quartzite 621429 7909839 TAN99AD59R1 Winnecke felsic extrusive 629002 7925651 TAN99AD61R1 Winnecke tuffaceous mudstone 633182 7931993 TAN99AD61R2 Winnecke tuffaceous mudstone 633182 7931993 TAN99AD62R1 Galifrey felsic intrusive 560698 7769956 TAN99AD62R2 Galifrey felsic intrusive 560698 7769956 TAN99AD62R3 Galifrey mafic extrusive 560698 7769956 TAN99AD63R1 Tanami Mine mafic extrusive 564266 7771024 TAN99AD63R2 Tanami Mine mafic extrusive 564266 7771024 TAN99AD63R3 Tanami Mine mafic extrusive 564266 7771024 TAN99AD63R4 Tanami Mine mafic extrusive 564266 7771024 TAN99AD64R1 Crusade mafic extrusive 612783 7883150 TAN99AD64R2 Crusade mafic extrusive 612783 7883150 TAN99AD64R3 Crusade mafic extrusive 612783 7883150 TAN99AD64R4 Crusade mafic extrusive 612783 7883150 TAN99AD65R1 Pendragon mafic extrusive 541820 7791571 TAN99AD65R2 Pendragon mafic extrusive 541820 7791571 TAN99AD65R3 Pendragon mafic extrusive 541820 7791571 TAN99AD66R1 Galifrey felsic intrusive 562370 7768801 TAN99AD66R2 Galifrey felsic intrusive 562370 7768801 TAN99AD66R3 Galifrey felsic intrusive 562370 7768801 TAN99AD66R4 Galifrey felsic intrusive 562370 7768801 TAN99AD66R5 Galifrey felsic intrusive 562370 7768801 TAN99AD67R1 Apertawonga felsic intrusive 562190 7757800 TAN99AD68R1 Tanami Mine felsic intrusive 571172 7784722 TAN99AD72R1 The Granites felsic intrusive 634982 7728235 A1 Sample No Locality Description Easting Northing TAN99AD72R2 The Granites metasediment 634982 7728235 TAN99AD74R1 The Granites amphibolite 634817 7728202 TAN99AD74R2 The Granites amphibolite 634817 7728202 TAN99AD80R1 The Granites mafic intrusive 636183 7728761 TAN99AD81R1 Dead Bullock Soak mafic intrusive 597903 7730308 TAN99AD81R2 Dead Bullock Soak mafic intrusive 597903 7730308 TAN99AD88R1 Dead Bullock Soak mafic intrusive 597894 7730510 TAN99AD88R2 Dead Bullock Soak mafic intrusive 597894 7730510 TAN99AD89R1 Grimwade Ridge quartzite 625532 7710221 TAN99AD91R1 Grimwade Ridge siltstone 624225 7710281 TAN99AD104R1 Muriel Range felsic intrusive 553648 7711486 TAN99AD109R1 Officer Hill amphibolite 567115 7710758 TAN99AD109R2 Officer Hill amphibolite 567115 7710758 TAN99AD109R3 Officer Hill amphibolite 567115 7710758 TAN99AD110R1 Officer Hill amphibolite 566953 7710916 TAN99AD114R1 The Granites felsic intrusive 648327 7729490 TAN99AD115R1 Inningara felsic intrusive 595203 7713977 TAN99AD115R2 Inningara felsic intrusive 595203 7713977 TAN99AD115R3 Inningara felsic intrusive 595203 7713977 TAN99AD115R4 Inningara felsic intrusive 595203 7713977 TAN99AD118R1 The Granites felsic intrusive 615382 7709252 TAN99AD120R1 Grimwade Ridge felsic intrusive 624712 7708748 TAN99AD121R1 Grimwade Ridge felsic intrusive 626269 7707492 TAN99AD122R1 Grimwade Ridge felsic intrusive 627798 7707338 TAN99AD122R2 Grimwade Ridge felsic intrusive 627798 7707338 TAN99AD123R1 Grimwade Ridge felsic intrusive 628848 7707509 TAN99AD124R1 The Granites felsic intrusive 641373 7725952 TAN99AD124R2 The Granites felsic intrusive 641373 7725952 TAN99AD124R3 The Granites felsic intrusive 641373 7725952 TAN99AD124R4 The Granites felsic intrusive 641373 7725952 TAN99AD129R1 Rabbit Flat amphibolite 611925 7771559 TAN99AD130R1 Rabbit Flat quartzite 611986 7771493 TAN99AD131R1 Rabbit Flat mafic extrusive 611474 7771533 TAN99AD142R1 Crusade felsic extrusive 612657 7870634 TAN99AD144R1 Crusade mafic extrusive 612352 7888154 TAN99AD144R2 Crusade mafic extrusive 612352 7888154 TAN99AD148R1 Winnecke felsic intrusive 621551 7910115 TAN99AD149R1 Winnecke felsic intrusive 621681 7910288 TAN99AD149R2 Winnecke felsic intrusive 621681 7910288 TAN99AD149R3 Winnecke felsic intrusive 621681 7910288 TAN99AD150R1 Crusade felsic extrusive 613335 7887396 TAN99AD151R1 Crusade felsic extrusive 613301 7887484 TAN99AD153R1 Crusade felsic extrusive 613397 7887414 TAN99AD154R1 Crusade felsic extrusive 613410 7887311 TAN99AD156R1 Crusade felsic extrusive 613794 7887301 TAN99AD157R1 Crusade bimodal volcanic 613993 7887316 TAN99AD158R1 Crusade mafic extrusive 613960 7887311 TAN99AD158R2 Crusade mafic extrusive 613960 7887311 TAN99AD159R1 Crusade felsic extrusive 612399 7887092 TAN99AD159R2 Crusade felsic extrusive 612399 7887092 TAN99AD159R3 Crusade felsic extrusive 612399 7887092 TAN99AD161R1 Crusade felsic extrusive 611734 7887352 TAN99AD163R1 Crusade felsic extrusive 611166 7887307 TAN99AD166R1 Crusade felsic extrusive 613005 7883209 TAN99AD166R2 Crusade mafic extrusive 613005 7883209 TAN99AD166R3 Crusade felsic extrusive 613005 7883209 TAN99AD168R1 Crusade mafic extrusive 612492 7882131 TAN99AD169R1 Crusade felsic extrusive 612554 7882150 TAN99AD170R1 Wilsons felsic intrusive 505234 7769711 TAN99AD174R1 Wilsons conglomerate 509459 7756584 TAN99AD177R1 Wilsons felsic intrusive 509206 7756447 TAN99AD179R1 Wilsons amphibolite 538063 7752243 A2 Sample No Locality Description Easting Northing TAN99AD180R1 Wilsons calcsilicate 538150 7751681 TAN99AD182R1 Wilsons felsic intrusive 544643 7751839 TAN99AD184R1 Wilsons felsic intrusive 544699 7751855 TAN99AD185R1 MacFarlane felsic intrusive 545090 7751682 TAN99AD185R2 MacFarlane felsic intrusive 545090 7751682 TAN99AD186R1 MacFarlane felsic intrusive 546078 7751861 TAN99AD187R1 MacFarlane felsic intrusive 546447 7752282 TAN99AD194R1 MacFarlane felsic intrusive 547640 7756394 TAN99AD196R1 MacFarlane metasediment 549451 7755619 TAN99AD228R1 Tanami Mine felsic intrusive 588608 7805595 TAN99AD229R1 Tanami Mine mafic extrusive 591029 7806236 TAN99AD230R1 Tanami Mine mafic extrusive 590979 7806245 TAN99AD231R1 Ptilotus felsic intrusive 596799 7810787 TAN99AD232R1 Ptilotus felsic intrusive 602996 7811372 TAN99AD233R1 Ptilotus intermediate intrusive 602874 7811390 TAN99AD234R1 Ptilotus felsic intrusive 631868 7823273 TAN99AD234R2 Ptilotus felsic intrusive 631868 7823273 TAN99AD234R3 Ptilotus felsic intrusive 631868 7823273 TAN99AD235R1 Ptilotus mafic intrusive 631830 7823366 TAN99AD235R2 Ptilotus mafic intrusive 631830 7823366 TAN99AD236R1 Ptilotus felsic intrusive 649648 7779000 TAN99AD236R2 Ptilotus felsic intrusive 649648 7779000 TAN99AD237R1 Winnecke felsic intrusive 642108 7896349 TAN99AD237R2 Winnecke metasediment 642108 7896349 TAN99AD239R1 Winnecke mafic extrusive 638452 7897856 TAN99AD240R1 Winnecke mafic extrusive 636334 7895937 TAN99AD241R1 Winnecke felsic intrusive 633902 7897208 TAN99AD241R2 Winnecke felsic intrusive 633902 7897208 TAN99AD241R3 Winnecke felsic intrusive 633902 7897208 TAN99AD243R1 Winnecke felsic intrusive 631951 7901189 TAN99AD247R1 MacFarlane felsic intrusive 514064 7750986 TAN99AD247R2 MacFarlane quartz conglomerate 514064 7750986 TAN99AD247R3 MacFarlane quartz conglomerate 514064 7750986 TAN99AD250R1 MacFarlane felsic intrusive 523042 7782361 TAN99AD250R2 MacFarlane felsic intrusive 523042 7782361 TAN99AD250R3 MacFarlane felsic intrusive 523042 7782361 TAN99AD251R1 MacFarlane felsic intrusive 523085 7782356 TAN99AD251R2 MacFarlane felsic intrusive 523085 7782356 TAN99AD255R1 Muriel Range micaceous siltstone 557212 7712283 TAN99AD258R1 Muriel Range felsic intrusive 553684 7711575 TAN99AD259R1 Muriel Range felsic intrusive 553696 7711505 TAN99AD260R1 Muriel Range sandstone 552462 7710645 TAN99AD261R1 Muriel Range felsic intrusive 553161 7706470 TAN99AD266R1 Muriel Range felsic intrusive 554555 7705591 TAN99AD267R1 Muriel Range vein quartz 557851 7705397 TAN99AD268R1 Muriel Range feldspathic sandstone 557953 7706158 TAN99AD268R2 Muriel Range feldspathic sandstone 557953 7706158 TAN99AD268R3 Muriel Range feldspathic sandstone 557953 7706158 TAN99AD269R1 Muriel Range felsic intrusive 557958 7706221 TAN99AD270R1 Muriel Range felsic intrusive 557938 7705793 TAN99AD274R1 Muriel Range felsic intrusive 558636 7705711 TAN99AD275R1 Muriel Range calcrete 557320 7708716 TAN99AD276R1 Muriel Range sandstone 557450 7709301 TAN99AD277R1 Muriel Range felsic intrusive 557450 7710301 TAN99AD277R2 Muriel Range felsic intrusive 557450 7710301 TAN99AD278R1 Officer Hill amphibolite 566878 7710504 TAN99AD279R1 Officer Hill amphibolite 566983 7710555 TAN99AD280R1 Officer Hill amphibolite 566953 7710554 TAN99AD281R1 Officer Hill amphibolite 566680 7710784 TAN99AD286R1 Officer Hill felsic intrusive 570281 7710222 TAN99AD288R1 Officer Hill folded siltstone 568283 7710216 TAN99AD289R1 Officer Hill felsic intrusive 567837 7706810 A3 Sample No Locality Description Easting Northing TAN99AD289R2 Officer Hill felsic intrusive 567837 7706810 TAN99AD290R1 Officer Hill felsic intrusive 567548 7706759 TAN99AD290R2 Officer Hill felsic intrusive 567548 7706759 TAN99AD291R1 Officer Hill felsic intrusive 568013 7706670 TAN99AD292R1 Officer Hill sandstone 567908 7705290 TAN99AD293R1 Officer Hill sandstone 567511 7705170 TAN99AD296R1 Officer Hill felsic intrusive 566780 7707290 TAN99AD298R1 Officer Hill felsic intrusive 566799 7708527 TAN99AD300R1 Officer Hill spotted phyllite/shale 566521 7710224 TAN99AD301R1 Officer Hill siltstone 566021 7710416 TAN99AD305R1 Officer Hill folded siltstone 567112 7710022 TAN99AD309R1 Officer Hill amphibolite 567822 7710465 TAN99AD310R1 Murdoch Cliffs felsic intrusive 584159 7708048 TAN99AD310R2 Murdoch Cliffs felsic intrusive 584159 7708048 TAN99AD311R1 Murdoch Cliffs felsic intrusive 584019 7707912 TAN99AD313R1 Dead Bullock Soak folded chert 592292 7720725 TAN99AD319R1 MacFarlanes amphibolite 537340 7751207 TAN99AD321R1 MacFarlanes felsic volcanic 538190 7751554 TAN99AD322R1 MacFarlanes felsic volcanic 538206 7751569 TAN99AD323R1 MacFarlanes felsic volcanic 538219 7752008 TAN99AD324R1 Crusade felsic volcanic 613379 7887266 TAN99AD324R2 Crusade felsic volcanic 613379 7887266 TAN99AD324R3 Crusade felsic volcanic 613379 7887266 TAN99AD325R1 Crusade mafic extrusive 614021 7887299 TAN99AD325R2 Crusade mafic extrusive 614021 7887299 TAN99AD325R3 Crusade mafic extrusive 614021 7887299 TAN99AD326R1 Crusade felsic volcanic 612988 7883157 TAN99AD327R1 Crusade felsic volcanic 612504 7882206 TAN99AD328R1 Tanami mafic intrusive 572148 7787948 TAN99AD329R1 Tanami mafic intrusive 571797 7787740 TAN99AD330R1 The Granites felsic intrusive 643157 7724822 TAN99AD331R1 Borefield Road mafic intrusive 643844 7730358 TAN99AD331R2 Borefield Road mafic intrusive 643844 7730358 TAN99AD331R3 Borefield Road mafic intrusive 643844 7730358 TAN99AD331R4 Borefield Road mafic intrusive 643844 7730358 TAN99AD331R5 Borefield Road mafic intrusive 643844 7730358 TAN99AD331R6 Borefield Road mafic intrusive 643844 7730358 TAN99AD331R7 Borefield Road mafic intrusive 643844 7730358 TAN99AD331R8 Borefield Road mafic intrusive 643844 7730358 TAN99AD331R9 Borefield Road mafic intrusive 643844 7730358 TAN99AD331R10 Borefield Road mafic intrusive 643844 7730358 TAN99AD331R11 Borefield Road mafic intrusive 643844 7730358 TAN99AD331R12 Borefield Road mafic intrusive 643844 7730358 TAN99AD332R1 Dead Bullock Soak mafic intrusive 596622 7729340 TAN99AD333R1 Dead Bullock Soak mafic intrusive 596941 7729286 TAN99AD333R2 Dead Bullock Soak mafic intrusive 596941 7729286 TAN99AD334R1 Dead Bullock Soak mafic intrusive 596657 7729639 TAN99AD334R2 Dead Bullock Soak mafic intrusive 596657 7729639 TAN99AD335R1 Dead Bullock Soak mafic intrusive 596680 7729661 TAN99AD336R1 Dead Bullock Soak mafic intrusive 596679 7729658 TAN99AD336R2 Dead Bullock Soak mafic intrusive 596679 7729658 TAN99AD336R3 Dead Bullock Soak mafic intrusive 596679 7729658 TAN99AD336R4 Dead Bullock Soak mafic intrusive 596679 7729658 TAN99AD336R5 Dead Bullock Soak mafic intrusive 596679 7729658 TAN99AD337R1 Dead Bullock Soak mafic intrusive 596835 7729460 TAN99AD338R1 Dead Bullock Soak mafic intrusive 596815 7729464 TAN99AD339R1 Dead Bullock Soak mafic intrusive 597404 7729930 TAN99AD340R1 Dead Bullock Soak mafic intrusive 596927 7729359 TAN99AD341R1 Dead Bullock Soak mafic intrusive 597412 7729803 TAN99AD342R1 Dead Bullock Soak mafic intrusive 597408 7729164 TAN99AD342R2 Dead Bullock Soak mafic intrusive 597408 7729164 TAN99AD342R3 Dead Bullock Soak mafic intrusive 597408 7729164 A4 Sample No Locality Description Easting Northing TAN99AD343R1 The Granites mafic intrusive 661256 7748650 TAN99AD344R1 The Granites felsic intrusive 641481 7725877 TAN99AD345R1 The Granites felsic intrusive 634677 7727907 TAN99AD346R1 Officer Hill mafic intrusive 570306 7711280 TAN99AD347R1 East Ptilotus mafic intrusive 627988 7753967 TAN99AD348R1 MacFarlane mafic intrusive 602856 7756536 TAN99AD349R1 MacFarlane mafic intrusive 603093 7756356 TAN99AD350R1 MacFarlane felsic intrusive 514300 7772550 TAN99AD351R1 MacFarlane felsic intrusive 514360 7772450 TAN99AD352R1 MacFarlane felsic intrusive 514451 7772431 TAN99AD353R1 MacFarlane felsic intrusive 514371 7772322 TAN99AD353R2 MacFarlane felsic intrusive 514371 7772322 TAN99AD353R3 MacFarlane felsic intrusive 514371 7772322 TAN99AD354R1 MacFarlane felsic intrusive 534822 7751855 TAN99AD354R2 MacFarlane felsic intrusive 534822 7751855 TAN99AD355R1 MacFarlane metasediment 512095 7778071 TAN99AD360R1 Mavericks felsic intrusive 505180 7786486 TAN99AD360R2 Mavericks felsic intrusive 505180 7786486 TAN99AD361R1(DDH1) Mount Frederick felsic intrusive 510588 7799989 TAN99AD361R2 (DDH1) Mount Frederick felsic intrusive 510588 7799989 TAN99AD361R3(DDH1) Mount Frederick felsic intrusive 510588 7799989 TAN99AD362R1(DDH2) Mavericks felsic intrusive 505529 7786509 TAN99AD362R2(DDH2) Mavericks felsic intrusive 505529 7786509 TAN99AD363R1(DDH3) Coomarie Dome felsic intrusive 544939 7817879 TAN99AD363R2(DDH3) Coomarie Dome felsic intrusive 544939 7817879 TAN99AD363R3(DDH3) Coomarie Dome metasediment 544939 7817879 TAN99AD363R4A(DDH3) Coomarie Dome metasediment/dyke 544939 7817879 TAN99AD363R4B(DDH3) Coomarie Dome metasediment/dyke 544939 7817879 TAN99AD363R5(DDH3) Coomarie Dome mafic extrusive 544939 7817879 TAN99AD363R6(DDH3) Coomarie Dome epidote/metasediment 544939 7817879 TAN99AD364R1(DDH5) Coomarie Dome felsic intrusive 558522 7803574 TAN99AD365R1(DDH6) Coomarie Dome felsic intrusive 545991 7809375 TAN99AD365R2(DDH6) Coomarie Dome felsic intrusive 545991 7809375 TAN99AD366R1(DDH7) Frankenia felsic intrusive 586504 7778075 TAN99AD367R1(DDH15) Talbot South felsic intrusive 600350 7811145 TAN99AD368R1A(DDH20) MacFarlane felsic intrusive 535385 7759208 TAN99AD368R1B(DDH20) MacFarlane felsic intrusive 535385 7759208 TAN99AD369R1A(DDH21) MacFarlane felsic intrusive 534800 7751850 TAN99AD369R1B(DDH21) MacFarlane felsic intrusive 534800 7751850 TAN99AD369R1C(DDH21) MacFarlane felsic intrusive 534800 7751850 TAN99AD370R1A(DDH23) Apertawonga felsic intrusive 556501 7761950 TAN99AD370R1B(DDH23) Apertawonga felsic intrusive 556501 7761950 TAN99AD371R1A(DDH28) Dead Bullock Soak felsic intrusive 601692 7738217 TAN99AD371R1B(DDH28) Dead Bullock Soak felsic intrusive 601692 7738217 TAN99AD372R1 Western Australia felsic intrusive 441757 7813666 TAN99MH45R1 Wilsons Creek felsic extrusive 612096 7882362 TAN99MH73R1 Wilsons Creek felsic extrusive 612605 7870721 TAN99MH118R1 MacFarlane metasediment 519827 7780847 TAN99MH136R1 MacFarlane felsic intrusive 523049 7782437 TAN99MH177R1 Wilsons Creek bimodal volcanics 612973 7883172 TAN99MH296R1 Wilsons Creek felsic extrusive 613300 7887450 TAN99MH299R1 Wilsons Creek felsic extrusive 613152 7887363 TAN99MH407R1 Mt Solitaire felsic intrusive 659171 7721696 TAN99MH410R3 Frankenia felsic intrusive 601257 7748656 TAN99MH412R1 Mt Solitaire mafic intrusive 661189 7748582 TAN99MH412R2 Mt Solitaire mafic intrusive 661189 7748582 TAN99MH414R1 East Ptilotus felsic intrusive 627677 7754268 TAN99MH419R1 The Granites felsic intrusive 641260 7725890 TAN99MH420R1 The Granites metasediment 641260 7725890 TAN99MH422R1 The Granites felsic intrusive 634677 7727907 TAN99MH423R1 The Granites felsic intrusive 634677 7727907 TAN99MH434R1 Ptilotus mafic extrusive 612052 7771370 A5 Sample No Locality Description Easting Northing TAN99MH435R1 Ptilotus mafic extrusive 612140 7771499 TAN99MH436R1 Ptilotus mafic extrusive 612179 7771482 TAN99MH437R1 Ptilotus mafic extrusive 612230 7771010 TAN99MH438R1 Ptilotus mafic extrusive 612235 7771115 TAN99MH449R1 Supplejack felsic extrusive 612692 7870565 TAN99MH454R1 Wilsons Creek felsic extrusive 611864 7887220 TAN99MH458R1 Wilsons Creek felsic extrusive 610354 7887807 TAN99MH468R1 Nora Range felsic extrusive 509223 7756443 TAN99MH489R1 MacFarlanes contact aureole 547304 7755534 TAN99MH528R1 Tanami felsic intrusive 602907 7811401 TAN99MH537R1 Wilsons Creek felsic intrusive 634122 7896854 TAN99MH543R1 Wilsons Creek felsic intrusive 624954 7894529 TAN99MH543R1A Wilsons Creek felsic intrusive 624954 7894529 TAN99MH551R1 Tanami felsic extrusive 523085 7782356 TAN99MH605R1 MacFarlane contact aureole 551932 7769640 TAN99MH656R1 MacFarlane felsic intrusive 524635 7777884 TAN99MH669R1 MacFarlane felsic intrusive 538263 7751878 TAN99MH670R1 MacFarlane felsic intrusive 538197 7752035 TAN99MH675R1 MacFarlane mafic extrusive 537129 7751318 TAN99MH676R1 MacFarlane mafic extrusive 537100 7751325 TAN99MH678R1 MacFarlane amphibolite 537180 7751279 TAN99MH679R1 MacFarlane amphibolite 537345 7751253 TAN99MH682R1 MacFarlane felsic extrusive 536703 7751247 TAN99MH682R2 MacFarlane felsic extrusive 536703 7751247 TAN99MH705R1 Ptilotus felsic intrusive 617604 7754844 TAN99MH706R1 MacFarlane felsic intrusive 514455 7775459 TAN99MH707R1 MacFarlane felsic intrusive 545017 7756720 TAN99MH708R1 The Granites felsic intrusive 641260 7725890 TAN99MH709R1 East Ptilotus mafic intrusive 628000 7754176 TAN99MH710R1 Tanami Mine felsic intrusive 575007 7792859 TAN99MH711R1 Tanami felsic intrusive 561402 7767444 TAN99MH712R1 Tanami Mine felsic intrusive 565763 7767770 TAN99MH713R1 Crusade felsic intrusive 612744 7883161 TAN99MH714R1 Galifrey felsic intrusive 560765 7769809 TAN99MH715R1 Browns Range felsic intrusive 512869 7901836 TAN99MH716R1 Browns Range felsic intrusive 504869 7898836 TAN99MH717R1 Browns Range felsic intrusive 519869 7901836 TAN99AJC36R1 Crusade mafic extrusive 612520 7881578 TAN99AJC78R1A Crusade mafic extrusive 612478 7882153 TAN99AJC85R1 Birindudu felsic extrusive 629000 7929000 TAN99AJC86R1 Birindudu volcanogenic sandstone 635777 7937845 TAN99AJC87R1 Birindudu tuffaceous siltstone 633182 7931993 TAN99AJC107R1A North Tanami felsic intrusive 559811 7884423 TAN99AJC112R1 North Tanami felsic intrusive 559887 7884431

All samples have been entered into an Access database which will be added to the AGSO OZROC database, forming part of the Tanami GIS package.

A6

Figure A1 Sample localities projected on a 1:500,000 total magnetic map of the Tanami Region

(this is available to download in MapInfo with detailed sample data under MapInfo folder in ReportFigures/Appendices folder on CD)

A7 Appendix 3 Whole Rock Analyses

Whole rock analyses were obtained from Amdel laboratories for NTGS samples. The AGSO OZROC database provided additional Tanami Region samples. Traces records the sum of all trace elements after conversion to oxides. Total is the sum of all components with the exception of F and S.

Geochronology samples were analysed for whole rock geochemistry at AGSO laboratories in Canberra – for many of these the analysis is still pending.

Core samples for drillhole data (prefix TAN99DDH) are held at the Alice Springs Core Library. To access consult the NTGS Alice Springs core store.

A278 Table A5 Whole rock analyses for the Tanami Region Coomarie Supersuite Inningarra Suite Muriel Officer Hill Range Sample TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 Number AD104R1 AD258R1 AD269R1 AD270R1 AD277R1 AD289R1 AD289R2 AD290R1 AD291R1 wt% SiO2 75.10 71.40 71.20 70.90 76.00 47.70 79.60 77.50 83.10 TiO2 0.06 0.40 0.05 0.03 0.12 0.07 0.04 0.03 0.03 Al2O3 12.40 13.30 14.90 12.90 13.20 31.20 9.93 12.90 8.95 Fe2O3T 0.97 3.30 0.82 0.73 1.06 6.15 2.31 0.76 2.39 MnO <0.01 0.02 0.00 0.00 0.04 0.60 0.20 0.04 0.24 MgO 0.12 0.12 0.18 0.17 0.20 0.11 0.14 0.11 0.02 CaO 0.07 0.29 0.98 0.45 1.00 0.17 0.22 0.32 0.05 Na2O 0.13 0.16 5.27 2.63 3.11 0.23 0.10 3.75 0.08 K2O 6.28 5.13 5.19 7.30 4.98 10.50 3.69 4.35 3.25 P2O5 0.02 0.07 0.01 0.01 0.06 0.01 0.04 0.01 0.05 LOI 4.39 5.01 1.21 4.65 0.60 4.06 1.78 0.81 1.51 ppm Be <2 2 7 2 3 11 4 4 4 Sc <5 6 0 0 <5 12 4 <5 <5 V 8 12 5 4 6 0 2 <2 <2 Cr 6 4 0 0 <2 0 0 <2 <2 Co 42 2 1 1 39 1 1 58 43 Ni 4 6 3 2 <2 0 0 <2 <2 Cu 9 13 7 11 3 1 7 7 3 Zn 12 25 9 8 27 190 73 21 93 Ga 16 23 24 15 18 57 29 32 26 As n.d. 0 0 1 n.d. 2 2 n.d. n.d. Se <0.5 0 0 0 1 0 0 <0.5 <0.5 Rb 310 390 470 250 200 3700 1200 800 1350 Sr 78 77 65 105 130 31 17 13 15 Y 12 43 11 9 10 9 17 39 26 Zr 70 600 160 39 86 36 51 50 50 Nb 8 22 35 8 9 89 50 56 50 Mo 0 0 0 1 <0.1 1 4 0 1 Ag <0.1 1 1 0 0 0 0 1 0 Cd <0.1 0 0 0 0 0 0 <0.1 <0.1 In <0.05 0 0 0 <0.05 0 0 0 0 Sn n.d. 18 9 4 n.d. 270 67 21 105 Sb <0.5 0 0 0 <0.5 0 0 <0.5 <0.5 Te <0.2 0 0 0 <0.2 0 0 <0.2 <0.2 Cs 6 4 5 8 3 89 24 14 34 Ba 600 1600 160 460 310 85 80 60 30 La 13 145 4 11 25 1 2 15 1 Ce 20 270 4 19 38 4 7 33 4 Pr 3 30 1 2 6 0 1 4 1 Nd 11 100 3 8 19 1 2 15 4 Sm 2 17 1 2 3 0 1 5 2 Eu 1 3 0 1 1 0 0 0 0 Gd 1 12 1 2 2 1 1 4 2 Tb 0 1 0 0 0 0 0 1 0 Dy 2 8 2 2 2 2 3 9 5 Ho 0 1 0 0 0 0 1 2 1 Er 1 4 2 1 1 1 3 5 3 Tm 0 1 0 0 0 0 1 1 1 Yb 2 5 3 1 1 2 5 7 5 Lu 0 1 1 0 0 0 1 1 1 Hf 2 12 10 3 3 5 4 4 3 Ta <2 2 8 2 <2 46 21 8 7 W n.d. 1 0 0 n.d. 80 57 380 1000 Ru ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Rh ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pd ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ir ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Os ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pt ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Au ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Tl 2 3 2 2 1 17 6 3 5 Pb 24 21 31 45 40 20 11 22 450 Bi 0 0 3 0 <0.1 2 58 4 0 Th 27 30 15 24 28 18 21 25 21 U 3 8 2 5 10 8 11 14 9 Traces 0.13 0.35 0.11 0.11 0.10 0.48 0.18 0.17 0.34 Totals 99.66 99.55 99.91 99.87 100.47 101.28 98.23 100.75 100.00

A279

Grimwade The East Ridge Granites Ptilotus Sample TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 Number AD120R1 AD121R1 AD124R4 AD114R1a AD114R1b MH708R1 AD233R1 MH438R1 99496213 99496210 wt% SiO2 76.80 64.60 70.50 65.76 64.30 67.75 75.80 72.10 TiO2 0.21 1.86 0.36 0.68 0.74 0.46 0.45 0.86 Al2O3 11.50 15.70 14.00 15.18 16.10 15.28 13.60 6.75 Fe2O3T 0.92 5.36 3.34 5.89 6.63 4.25 2.11 8.21 MnO 0.00 0.04 0.08 0.08 0.08 0.07 <0.01 0.10 MgO 0.24 1.44 0.98 1.74 1.86 1.45 0.41 2.11 CaO 0.25 0.35 0.11 4.01 4.14 3.20 0.09 7.36 Na2O 0.09 0.06 0.10 3.15 3.37 3.51 0.07 0.29 K2O 0.96 1.73 2.53 2.71 2.83 2.55 2.22 0.25 P2O5 0.02 0.18 0.03 0.19 0.17 0.14 0.04 0.10 LOI 5.20 7.85 7.79 0.87 0.53 1.36 5.81 0.92 ppm Be 0 4 3 2 2 2 <2 <2 Sc 3 12 5 16 10 9 5 20 V 13 89 35 71 67 54 51 105 Cr 10 58 12 30 19 23 11 26 Co 1 11 43 n.d. 13 n.d. 37 150 Ni 3 31 17 22 18 17 8 47 Cu 5 25 38 26 35 14 16 81 Zn 7 110 155 71 79 77 54 135 Ga 9 25 22 20 23 18 19 17 As 0 2 n.d. n.d. 1 n.d. n.d. n.d. Se 0 0 <0.5 n.d. 0 n.d. <0.5 <0.5 Rb 38 700 160 113 115 117 125 <1 Sr 150 220 28 232 270 280 41 51 Y 9 47 32 26 22 15 13 14 Zr 120 280 150 223 210 172 280 93 Nb 8 23 13 11 14 10 13 9 Mo 0 1 0 1 1 0 0 <0.1 Ag 0 1 0 n.d. 1 n.d. 0 <0.1 Cd 0 0 0 n.d. 0 n.d. <0.1 <0.1 In 0 0 <0.05 n.d. 0 n.d. <0.05 0 Sn 0 0 n.d. n.d. 5 n.d. n.d. n.d. Sb 0 0 <0.5 0 0 0 <0.5 <0.5 Te 0 0 <0.2 n.d. 0 n.d. <0.2 <0.2 Cs 2 11 13 6 6 11 10 0 Ba 4450 2100 550 659 650 835 1050 55 La 14 195 58 52 58 51 41 5 Ce 19 220 64 97 96 90 74 12 Pr 2 33 12 10 11 9 11 2 Nd 8 120 43 36 37 30 36 8 Sm 3 21 8 6 7 5 8 3 Eu 1 6 2 1 2 1 1 1 Gd 1 16 6 6 6 4 4 3 Tb 0 2 1 1 1 1 1 0 Dy 1 11 6 5 4 3 3 3 Ho 0 2 1 1 1 1 0 1 Er 1 4 3 3 2 1 1 2 Tm 0 1 0 n.d. 0 n.d. 0 0 Yb 1 4 3 2 2 1 1 2 Lu 0 1 0 0 0 0 0 0 Hf 4 6 4 n.d. 7 n.d. 6 3 Ta 0 2 <2 1 0 1 <2 3 W 0 2 n.d. n.d. 1 n.d. n.d. n.d. Ru ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Rh ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pd ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ir ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Os ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pt ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Au ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Tl 0 5 1 n.d. 1 n.d. 2 <0.1 Pb 6 36 28 18 17 24 25 2 Bi 0 0 0 0 0 0 0 0 Th 7 18 17 15 16 16 29 1 U 1 21 7 3 3 3 6 1 Traces 0.49 0.45 0.15 0.18 0.18 0.19 0.20 0.09 Totals 96.68 99.62 99.97 100.44 100.93 100.21 100.80 99.13

A280 Table A5 cont.

Coomarie Suite Coomarie Frankenia Talbot Dome South Sample TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 Number DDH3R1 DDH3R3 DDH3R4 DDH3R5 DDH5R1 DDH6R1 DDH7R1 MH410R3 DDH15R1 AD363R1 AD363R3 AD363R4 AD363R5 AD364R1 AD365R1 AD366R1 AD367R1 wt% SiO2 62.30 53.90 70.20 52.70 63.20 70.40 73.00 71.80 73.10 TiO2 0.57 2.29 0.60 1.17 0.54 0.28 0.19 0.03 0.21 Al2O3 17.40 18.40 17.20 14.20 16.20 14.60 14.40 14.80 13.20 Fe2O3T 5.06 20.70 4.50 12.80 5.18 2.30 1.79 1.15 2.18 MnO 0.03 0.08 0.01 0.20 0.03 0.02 0.03 0.06 0.03 MgO 1.96 2.62 1.18 6.16 3.66 1.82 0.69 0.22 1.01 CaO 3.44 1.59 2.86 8.82 0.68 0.58 1.12 1.54 0.30 Na2O 3.73 0.69 2.34 2.85 1.84 1.75 4.17 4.08 2.64 K2O 2.99 1.10 1.53 0.66 4.30 6.14 3.89 3.77 5.45 P2O5 0.29 0.10 0.07 0.09 0.10 0.06 0.03 0.06 0.03 LOI 2.04 0.25 0.20 0.65 4.50 2.20 0.35 2.22 1.26 ppm Be 1 1 2 1 2 2 2 3 2 Sc 15 42 4 30 10 <5 <5 <5 <5 V 60 300 105 250 69 26 12 <2 9 Cr 21 105 16 79 41 3 3 <2 <2 Co 14 44 15 51 18 4 3 88 3 Ni 30 87 34 110 39 4 5 <2 2 Cu 26 145 9 105 7 12 9 22 4 Zn 98 140 68 130 66 40 45 32 31 Ga 30 24 26 22 21 20 22 33 19 As <0.5 0 1 <0.5 1 <0.5 <0.5 n.d. 2 Se <0.5 0 0 <0.5 <0.5 2 1 <0.5 2 Rb 79 35 42 8 100 165 170 340 145 Sr 440 91 280 210 150 105 175 8 77 Y 11 30 4 25 9 7 8 12 11 Zr 150 200 160 94 115 135 120 9 165 Nb 7 15 6 8 8 8 11 25 8 Mo 0 0 0 0 0 0 0 2 1 Ag 0 1 1 0 <0.1 0 0 1 0 Cd 0 0 0 0 <0.1 <0.1 <0.1 <0.1 <0.1 In <0.05 0 0 0 <0.05 <0.05 <0.05 <0.05 <0.05 Sn n.d. 3 0 n.d. n.d. n.d. n.d. n.d. n.d. Sb <0.5 0 0 <0.5 <0.5 <0.5 <0.5 <0.5 <0.5 Te <0.2 0 0 <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 Cs 2 2 2 0 6 5 4 10 2 Ba 480 90 155 145 420 500 440 60 650 La 58 21 36 12 23 32 28 4 57 Ce 96 39 66 22 38 50 45 9 99 Pr 10 6 9 3 4 5 4 1 10 Nd 35 22 34 13 15 15 15 6 32 Sm 7 6 6 4 3 4 3 2 6 Eu 2 2 2 1 1 1 1 0 2 Gd 3 6 3 2 1 1 1 2 3 Tb 0 1 0 0 0 0 0 0 0 Dy 2 7 1 3 1 1 1 2 2 Ho 0 1 0 1 0 0 0 0 0 Er 1 3 1 2 1 0 0 1 1 Tm 0 1 0 0 0 0 0 0 0 Yb 1 4 1 2 1 1 1 2 1 Lu 0 1 0 0 0 0 0 0 0 Hf 5 5 5 4 4 3 3 3 3 Ta <2 0 0 <2 <2 <2 <2 20 <2 W 1 2 1 1 1 3 1 n.d. 1 Ru ppb 2 n.d. n.d. 5 4 7 5 n.d. 7 Rh ppb <1 n.d. n.d. <1 <1 <1 <1 n.d. <1 Pd ppb <5 n.d. n.d. 10 <5 5 <5 n.d. <5 Ir ppb <1 n.d. n.d. <1 <1 <1 <1 n.d. <1 Os ppb <2 n.d. n.d. <2 <2 <2 <2 n.d. <2 Pt ppb <1 n.d. n.d. 15 5 3 6 n.d. 4 Au ppb <1 n.d. n.d. 6 6 <1 6 n.d. 7 Tl 0 0 0 <0.1 0 1 1 1 1 Pb 20 5 16 5 6 14 27 8 28 Bi <0.1 3 1 <0.1 <0.1 0 0 1 1 Th 20 7 21 4 11 18 17 8 25 U 2 1 1 1 1 4 5 11 5 Traces 0.17 0.15 0.11 0.14 0.12 0.12 0.12 0.07 0.14 Totals 99.98 101.87 100.80 100.44 100.35 100.27 99.77 99.80 99.55

A281

Satellite Titania Mac- Granite Farlane Sample TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 Number AJC107R1 AJC112R1 AD348R1 AD349R1 AD185R1 AD185R2 AD350R1 AD351R1 MH682R1 wt% SiO2 70.80 73.80 78.10 56.80 66.60 73.60 68.00 65.50 68.00 TiO2 0.58 0.12 0.38 0.94 0.47 0.04 0.45 0.41 0.42 Al2O3 15.90 14.40 10.60 14.60 15.70 14.70 14.80 14.40 15.70 Fe2O3T 3.19 2.49 1.71 9.35 3.77 0.54 2.73 3.47 3.56 MnO 0.01 0.00 <0.01 0.07 0.05 0.01 0.03 0.04 0.05 MgO 0.35 0.12 1.70 3.81 1.95 0.16 1.37 1.41 1.51 CaO 0.21 0.24 0.18 2.53 3.53 0.80 1.06 1.67 2.72 Na2O 0.04 0.06 0.08 0.91 4.37 4.27 0.09 3.26 4.31 K2O 0.85 1.09 3.28 3.86 2.65 4.89 4.94 5.02 1.56 P2O5 0.04 0.02 0.11 0.14 0.18 0.03 0.15 0.16 0.14 LOI 7.17 6.07 3.46 6.46 0.98 0.65 5.36 4.03 1.49 ppm Be 0 0 <2 3 2 <2 9 7 2 Sc 8 5 10 20 10 <5 5 <5 5 V 34 32 45 160 56 4 41 34 59 Cr 5 5 15 46 21 <2 10 10 9 Co 4 2 37 25 68 37 40 22 42 Ni 10 6 11 16 23 4 15 9 11 Cu 30 19 4 78 24 9 600 170 1050 Zn 49 20 11 200 59 12 72 26 130 Ga 21 20 18 26 24 22 26 21 20 As 3 0 n.d. n.d. n.d. n.d. n.d. n.d. n.d. Se 0 0 2 2 <0.5 <0.5 3 1 <0.5 Rb 46 33 93 77 90 135 410 270 52 Sr 25 14 10 82 700 420 77 360 470 Y 13 3 13 25 8 4 20 23 5 Zr 310 38 200 120 200 46 380 390 125 Nb 8 7 12 13 7 5 28 32 6 Mo 0 0 16 2 0 0 2 26 1 Ag 1 0 0 0 <0.1 <0.1 2 1 1 Cd 0 0 <0.1 1 <0.1 <0.1 1 0 0 In 0 0 <0.05 0 <0.05 <0.05 0 <0.05 <0.05 Sn 3 0 n.d. n.d. n.d. n.d. n.d. n.d. n.d. Sb 0 0 1 1 <0.5 <0.5 380 9 <0.5 Te 0 0 <0.2 <0.2 <0.2 <0.2 1 <0.2 <0.2 Cs 2 1 2 1 2 2 9 6 4 Ba 185 195 330 340 900 1150 750 700 650 La 51 11 39 31 58 8 78 130 13 Ce 72 10 67 51 79 9 155 210 32 Pr 8 1 10 8 11 2 22 26 3 Nd 25 3 32 29 36 6 73 86 10 Sm 4 1 6 6 6 2 11 12 2 Eu 1 0 1 1 2 1 2 2 1 Gd 3 0 4 5 3 1 6 7 1 Tb 0 0 0 1 0 0 1 1 0 Dy 3 0 2 4 2 1 4 4 1 Ho 0 0 0 1 0 0 1 1 0 Er 2 0 1 2 1 0 2 2 1 Tm 0 0 0 0 0 0 0 0 0 Yb 2 0 1 2 1 0 2 2 1 Lu 0 0 0 0 0 0 0 0 0 Hf 7 3 4 3 4 2 12 12 3 Ta 0 0 <2 <2 <2 <2 6 6 <2 W 0 1 n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ru ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Rh ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pd ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ir ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Os ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pt ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Au ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Tl 0 0 1 0 1 1 3 1 0 Pb 21 6 3 77 23 36 15 68 15 Bi 0 0 1 <0.1 <0.1 <0.1 12 4 0 Th 27 13 19 11 18 4 83 99 9 U 2 1 5 3 2 2 26 18 2 Traces 0.10 0.04 0.10 0.15 0.24 0.19 0.34 0.28 0.27 Totals 99.24 98.45 99.70 99.62 100.49 99.88 99.32 99.65 99.73

A282 Table A5 cont.

The Granites Suite Tanami The Twin Intrusives Granites Bonanza Sample TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 Number MH707R1 AD4R3a AD4R3b MH551R1 AD330R1 AD352R1 AD353R1 AD353R2 99496209 99496206 wt% SiO2 64.94 70.00 71.20 76.19 73.00 65.90 69.00 67.00 TiO2 0.55 0.52 0.51 1.17 0.31 0.46 0.42 0.43 Al2O3 15.09 16.60 16.70 10.80 13.60 14.80 15.30 14.50 Fe2O3T 4.39 2.05 2.16 4.72 2.47 3.44 2.66 3.49 MnO 0.06 <0.01 0.01 0.00 0.05 0.05 0.03 0.03 MgO 2.71 0.74 0.75 0.68 0.49 1.67 1.16 1.17 CaO 3.96 0.11 0.13 0.02 1.79 1.67 0.97 1.56 Na2O 3.77 0.24 0.24 0.04 3.17 3.62 0.09 3.56 K2O 3.39 4.38 4.19 3.73 4.54 5.11 5.17 4.95 P2O5 0.31 0.04 0.03 0.04 0.11 0.18 0.16 0.16 LOI 0.75 4.85 3.85 2.37 0.66 3.17 3.94 2.41 ppm Be 2 <2 <2 2 3 9 10 10 Sc 12 15 10 28 <5 5 <5 <5 V 71 68 73 220 17 39 36 37 Cr 91 29 21 486 3 13 11 10 Co n.d. 12 25 n.d. 62 45 39 43 Ni 56 20 21 47 2 12 11 11 Cu 47 110 115 7 6 51 420 230 Zn 60 34 27 18 57 31 33 37 Ga 19 28 28 15 24 24 25 24 As n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Se n.d. <0.5 <0.5 n.d. <0.5 <0.5 1 <0.5 Rb 108 125 125 164 195 260 430 290 Sr 697 24 22 29 155 390 58 400 Y 11 12 12 15 25 20 21 22 Zr 206 185 135 183 210 390 350 370 Nb 7 8 7 9 18 30 31 32 Mo 0 0 0 5 0 10 46 75 Ag n.d. 0 <0.1 n.d. 0 1 1 1 Cd n.d. <0.1 <0.1 n.d. <0.1 <0.1 0 0 In n.d. <0.05 0 n.d. <0.05 <0.05 0 <0.05 Sn n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Sb 0 3 3 15 <0.5 4 15 3 Te n.d. <0.2 <0.2 n.d. <0.2 <0.2 <0.2 <0.2 Cs 3 7 6 5 6 6 10 11 Ba 1332 550 550 1593 600 950 650 700 La 69 21 23 33 55 140 145 160 Ce 131 36 38 63 91 220 230 240 Pr 14 5 5 7 12 26 28 29 Nd 48 18 17 23 40 81 84 93 Sm 7 4 4 4 7 12 12 13 Eu 2 1 1 1 1 2 2 3 Gd 4 2 3 3 5 7 7 8 Tb 1 0 0 1 1 1 1 1 Dy 2 2 2 3 4 4 4 4 Ho 0 0 0 1 1 1 1 1 Er 1 1 1 2 2 2 2 2 Tm n.d. 0 0 n.d. 0 0 0 0 Yb 1 1 1 2 2 2 2 2 Lu 0 0 0 0 0 0 0 0 Hf n.d. 5 3 n.d. 5 12 13 13 Ta 1 2 <2 1 <2 6 7 5 W n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ru ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Rh ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pd ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ir ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Os ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pt ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Au ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Tl n.d. 1 0 n.d. 1 2 3 2 Pb 32 3 1 6 38 24 41 56 Bi 0 <0.1 <0.1 0 <0.1 1 2 2 Th 18 11 10 11 24 91 94 98 U 4 2 2 4 5 18 22 20 Traces 0.32 0.13 0.13 0.34 0.17 0.29 0.29 0.31 Totals 100.24 99.66 99.90 100.10 100.35 100.36 99.19 99.56

A283

Frederick Suite East Mount Mavericks MacFarlane Apertawonga Ptilotus Frederick Sample TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 Number MH705R1 MH706R1 DDH1R1 DDH2R1 DDH2R2 DDH20R1 DDH21R1 DDH23R1 AD17R1 99496207 99496208 AD361R1 AD362R1 AD362R2 AD368R1 AD369R1 AD370R1 wt% SiO2 68.91 67.12 65.10 65.00 57.40 71.60 68.40 69.30 78.20 TiO2 0.47 0.43 0.53 0.58 0.90 0.25 0.39 0.35 0.06 Al2O3 14.47 14.85 15.90 15.40 15.40 15.20 14.40 15.80 11.50 Fe2O3T 4.28 3.51 5.08 4.45 7.24 1.98 3.22 2.92 0.61 MnO 0.06 0.03 0.09 0.08 0.16 0.03 0.06 0.04 <0.01 MgO 1.40 1.07 2.14 1.92 4.02 0.73 1.93 1.39 0.04 CaO 1.07 1.66 3.58 3.56 5.75 1.83 2.64 2.19 0.09 Na2O 3.55 3.65 3.34 3.65 3.73 4.46 4.11 4.55 0.11 K2O 3.85 5.16 3.71 4.22 3.36 3.53 4.19 3.01 3.87 P2O5 0.12 0.17 0.20 0.24 0.46 0.04 0.25 0.09 0.01 LOI 1.89 0.69 1.05 1.15 0.81 0.44 0.54 0.48 4.80 ppm Be 2 9 3 3 4 2 5 2 <2 Sc 13 5 10 10 15 <5 <5 5 <5 V 47 43 75 65 120 23 49 39 5 Cr 12 24 21 19 47 5 32 9 <2 Co n.d. n.d. 14 12 23 5 11 8 36 Ni 12 17 23 23 66 12 38 16 12 Cu 15 223 19 21 30 9 11 8 9 Zn 58 104 78 86 125 49 57 51 13 Ga 19 19 23 23 27 22 23 22 24 As n.d. n.d. 2 2 <0.5 2 5 1 n.d. Se n.d. n.d. <0.5 <0.5 <0.5 1 <0.5 <0.5 <0.5 Rb 141 287 150 155 140 125 170 100 200 Sr 144 413 600 800 700 410 850 550 41 Y 28 21 14 20 29 4 11 5 4 Zr 196 331 130 195 240 105 220 130 45 Nb 12 28 9 14 16 7 11 7 10 Mo 1 19 1 1 1 0 1 0 0 Ag n.d. n.d. 0 0 0 0 0 0 <0.1 Cd n.d. n.d. <0.1 <0.1 <0.1 <0.1 <0.1 <0.1 <0.1 In n.d. n.d. <0.05 <0.05 0 <0.05 <0.05 <0.05 <0.05 Sn n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Sb 0 12 1 <0.5 <0.5 <0.5 <0.5 <0.5 <0.5 Te n.d. n.d. <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 Cs 3 13 7 4 4 6 6 4 6 Ba 1066 776 1200 1450 1250 700 1500 700 1600 La 42 104 46 74 91 26 70 24 5 Ce 84 201 75 125 155 39 110 44 7 Pr 9 21 7 14 18 4 12 4 1 Nd 28 69 24 48 67 13 40 15 3 Sm 5 10 6 10 13 4 10 4 1 Eu 1 2 2 3 3 1 4 2 1 Gd 5 6 2 4 6 1 3 1 1 Tb 1 1 0 0 1 0 0 0 0 Dy 5 3 2 3 4 1 2 1 1 Ho 1 1 0 1 1 0 0 0 0 Er 3 2 1 1 2 0 1 0 1 Tm n.d. n.d. 0 0 0 0 0 0 0 Yb 2 2 1 1 2 0 1 0 1 Lu 0 0 0 0 0 0 0 0 0 Hf n.d. n.d. 8 6 7 3 3 3 3 Ta 1 3 2 2 2 <2 <2 <2 <2 W n.d. n.d. 1 4 1 0 1 0 n.d. Ru ppb n.d. n.d. 2 3 4 7 4 5 n.d. Rh ppb n.d. n.d. <1 <1 <1 <1 <1 <1 n.d. Pd ppb n.d. n.d. <5 <5 <5 5 <5 5 n.d. Ir ppb n.d. n.d. <1 <1 <1 <1 <1 <1 n.d. Os ppb n.d. n.d. <2 <2 <2 <2 <2 <2 n.d. Pt ppb n.d. n.d. 3 <1 2 5 2 12 n.d. Au ppb n.d. n.d. <1 <1 <1 6 6 <1 n.d. Tl n.d. n.d. 1 1 1 1 2 1 1 Pb 15 122 23 24 23 33 55 22 33 Bi 0 6 0 <0.1 <0.1 0 1 0 0 Th 15 78 11 28 24 15 34 13 25 U 3 21 6 8 5 4 12 3 2 Traces 0.21 0.24 0.26 0.33 0.33 0.17 0.34 0.18 0.21 Totals 100.28 98.58 100.98 100.57 99.56 100.26 100.46 100.30 99.50

A284 Table A5 cont.

Winnecke Suite Galifrey Inspiration Grimwade Winnecke Mount Nanny Goat Peak Ridge Intrusives Winnecke Sample TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 Number AD62R1 AD66R1 DDH28R1 AD123R1 AD243R1A AD243R1B AD59R1 AD239R1 AD51R2 AD371R1 99496214 wt% SiO2 65.00 63.30 67.90 71.10 70.67 69.70 70.80 70.70 88.70 TiO2 0.33 0.36 0.43 0.18 0.48 0.49 0.44 0.42 0.16 Al2O3 13.90 14.30 15.80 13.90 12.91 13.20 12.70 12.60 5.77 Fe2O3T 2.97 3.20 3.41 1.95 4.69 4.98 3.88 3.78 1.46 MnO 0.05 0.04 0.05 0.03 0.10 0.09 0.05 0.05 <0.01 MgO 1.62 1.80 1.44 0.36 0.50 0.49 0.54 0.61 0.18 CaO 2.83 3.04 2.39 2.12 1.48 1.61 1.45 0.50 0.09 Na2O 3.71 3.89 4.35 3.74 2.59 2.69 2.32 2.29 0.02 K2O 2.28 2.17 3.07 3.74 5.29 5.25 5.31 5.84 1.52 P2O5 0.09 0.08 0.07 0.06 0.11 0.10 0.16 0.15 0.04 LOI 6.80 6.89 1.32 0.75 1.22 0.85 2.11 2.52 2.12 ppm Be <2 2 2 2 4 3 4 3 <2 Sc 5 10 5 0 12 7 10 10 <5 V 45 56 45 10 11 12 16 15 9 Cr 16 20 8 0 2 4 4 3 3 Co 18 22 9 3 n.d. 4 24 32 11 Ni 20 27 15 3 11 3 3 3 <2 Cu 5 12 25 1 18 11 6 4 5 Zn 15 51 65 37 159 185 125 80 14 Ga 24 23 23 18 21 25 19 22 11 As n.d. n.d. 1 1 n.d. 4 n.d. n.d. n.d. Se <0.5 1 <0.5 0 n.d. 0 <0.5 1 <0.05 Rb 64 63 91 120 305 310 310 330 100 Sr 250 350 380 180 79 92 85 82 9 Y 9 6 9 5 86 78 43 47 19 Zr 120 110 130 140 405 370 240 240 110 Nb 6 6 8 9 23 24 17 16 8 Mo 0 1 1 0 1 1 2 0 <0.1 Ag <0.1 <0.1 0 0 n.d. 1 1 0 <0.1 Cd <0.1 <0.1 <0.1 0 n.d. 0 0 <0.1 <0.1 In <0.05 <0.05 <0.05 0 n.d. 0 <0.05 <0.05 <0.05 Sn n.d. n.d. n.d. 0 n.d. 5 n.d. n.d. n.d. Sb 2 2 <0.5 0 2 2 1 2 1 Te <0.2 <0.2 <0.2 0 n.d. 0 <0.2 <0.2 <0.2 Cs 1 1 4 2 17 14 11 11 5 Ba 380 420 650 600 803 850 700 750 120 La 19 19 30 17 77 89 56 54 12 Ce 29 28 46 28 159 160 92 82 21 Pr 4 4 5 3 18 19 12 12 3 Nd 16 15 16 11 66 70 43 45 10 Sm 3 3 4 2 13 15 10 10 3 Eu 1 1 2 1 2 3 2 1 0 Gd 2 2 1 1 14 14 8 8 2 Tb 0 0 0 0 3 2 1 1 0 Dy 2 1 1 1 14 14 8 8 3 Ho 0 0 0 0 3 3 1 2 1 Er 1 1 1 1 8 8 4 5 2 Tm 0 0 0 0 n.d. 1 1 1 0 Yb 1 1 1 1 8 9 4 4 2 Lu 0 0 0 0 1 1 1 1 0 Hf 3 2 2 4 n.d. 10 6 5 3 Ta <2 <2 <2 0 3 3 3 <2 <2 W n.d. n.d. 0 0 n.d. 2 n.d. n.d. n.d. Ru ppb n.d. n.d. 4 n.d. n.d. n.d. n.d. n.d. n.d. Rh ppb n.d. n.d. <1 n.d. n.d. n.d. n.d. n.d. n.d. Pd ppb n.d. n.d. <5 n.d. n.d. n.d. n.d. n.d. n.d. Ir ppb n.d. n.d. <1 n.d. n.d. n.d. n.d. n.d. n.d. Os ppb n.d. n.d. <2 n.d. n.d. n.d. n.d. n.d. n.d. Pt ppb n.d. n.d. <1 n.d. n.d. n.d. n.d. n.d. n.d. Au ppb n.d. n.d. 5 n.d. n.d. n.d. n.d. n.d. n.d. Tl 0 0 1 1 n.d. 2 1 2 0 Pb 4 7 16 27 48 46 22 12 3 Bi <0.1 <0.1 0 0 0 0 1 0 0 Th 9 8 12 11 35 34 23 32 14 U 3 3 5 4 9 8 8 8 2 Traces 0.11 0.13 0.16 0.12 0.23 0.25 0.19 0.19 0.05 Totals 99.68 99.20 100.39 98.05 100.27 99.70 99.95 99.65 100.11

A285

Felsic Volcanics Mavericks

Sample TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 Number AD52R1 AD52R4 AD54R1 AD64R3 AD144R1 AD168R1a AD168R1b AD26R1 AD26R3 wt% SiO2 76.80 50.10 63.50 52.00 59.40 74.40 74.60 64.30 65.90 TiO2 0.24 2.65 2.23 2.55 0.82 1.22 1.24 1.40 1.63 Al2O3 11.80 12.30 11.80 12.00 14.70 12.50 12.50 13.70 12.90 Fe2O3T 3.26 14.90 14.30 15.30 11.40 4.88 4.95 10.90 10.90 MnO <0.01 0.14 <0.01 0.07 0.18 <0.01 <0.01 <0.01 <0.01 MgO 0.20 2.71 0.20 6.45 2.44 0.19 0.20 0.08 0.06 CaO 0.15 5.48 0.08 1.90 0.93 0.06 0.06 0.12 0.09 Na2O 0.07 1.96 0.05 0.04 1.98 0.07 0.08 0.03 0.03 K2O 3.83 1.63 1.71 1.60 2.66 2.12 2.11 0.32 0.17 P2O5 0.05 0.38 0.09 0.35 0.35 0.02 0.01 0.05 0.02 LOI 2.45 7.11 5.86 7.13 4.20 3.82 4.21 8.55 7.90 ppm Be 3 3 3 2 3 2 <2 <2 <2 Sc 10 25 25 25 20 30 30 30 25 V 11 220 110 145 <2 185 180 300 340 Cr 3 4 <2 4 3 78 78 53 45 Co 15 53 9 36 50 13 10 7 12 Ni <2 14 6 11 <2 17 17 48 37 Cu 4 36 14 3 5 8 7 69 105 Zn 23 175 23 125 195 39 40 100 41 Ga 24 33 30 30 37 17 16 24 28 As n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Se <0.5 <0.5 <0.5 1 <0.5 <0.5 1 <0.5 <0.5 Rb 175 58 67 65 79 105 105 14 4 Sr 43 180 130 11 61 28 28 11 6 Y 31 48 35 41 55 13 14 7 7 Zr 230 270 260 260 650 84 82 90 99 Nb 16 20 20 18 32 6 6 9 10 Mo 0 2 0 0 0 <0.1 <0.1 0 0 Ag 0 0 <0.1 <0.1 1 <0.1 <0.1 <0.1 <0.1 Cd <0.1 0 <0.1 <0.1 <0.1 <0.1 <0.1 <0.1 <0.1 In 0 0 0 0 0 0 0 0 0 Sn n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Sb 8 3 3 3 <0.5 12 13 1 2 Te <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 Cs 7 6 8 3 7 8 8 1 1 Ba 650 480 460 155 650 390 400 95 95 La 71 38 82 35 54 15 17 25 2 Ce 110 64 105 59 93 33 33 19 4 Pr 17 11 18 10 15 4 4 4 1 Nd 58 42 60 39 60 13 15 12 5 Sm 11 10 10 9 14 3 3 2 2 Eu 2 3 2 2 3 1 1 1 1 Gd 7 8 7 8 12 3 3 2 1 Tb 1 1 1 1 2 0 0 0 0 Dy 6 9 7 8 10 2 3 2 1 Ho 1 2 1 1 2 0 0 0 0 Er 3 5 4 4 6 2 2 1 1 Tm 1 1 1 1 1 0 0 0 0 Yb 3 5 4 4 7 2 2 1 1 Lu 1 1 1 1 1 0 0 0 0 Hf 6 6 6 6 12 3 3 3 3 Ta <2 <2 <2 <2 <2 <2 <2 <2 <2 W n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ru ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Rh ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pd ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ir ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Os ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pt ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Au ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Tl 1 0 0 0 0 0 0 0 <0.1 Pb 10 11 12 6 6 3 2 46 22 Bi 0 <0.1 0 <0.1 <0.1 0 0 0 1 Th 27 13 12 11 15 1 1 1 2 U 4 3 2 2 3 2 2 1 1 Traces 0.16 0.19 0.15 0.11 0.22 0.11 0.11 0.10 0.09 Totals 99.01 99.55 99.97 99.50 99.28 99.39 100.07 99.55 99.69

A286 Table A5 cont. Mafic Intrusives Borefield Road Suite Nora Range Borefield Road Sample TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 Number MH468R1 AD331R1 AD331R2 AD331R3 AD331R4 AD331R5 AD331R7 AD331R8 AD331R10 wt% SiO2 71.50 51.80 45.10 52.70 45.50 51.70 47.40 47.60 47.40 TiO2 0.26 0.93 1.28 0.84 1.20 0.79 1.43 1.31 1.50 Al2O3 13.50 14.60 16.40 18.00 16.40 16.40 15.10 15.30 15.20 Fe2O3T 2.53 12.60 14.10 10.00 14.40 10.60 12.80 12.20 12.40 MnO 0.05 0.17 0.20 0.11 0.19 0.17 0.16 0.16 0.15 MgO 0.33 6.01 5.15 3.84 5.08 6.07 6.18 6.00 6.31 CaO 1.32 8.79 9.60 7.49 9.71 8.24 9.07 8.90 9.03 Na2O 3.27 2.13 2.72 3.03 2.69 2.59 2.31 2.42 2.27 K2O 5.94 1.42 1.78 1.93 1.26 1.48 2.17 2.09 2.14 P2O5 0.06 0.42 1.56 0.42 1.49 0.38 0.98 0.86 0.85 LOI 1.03 1.02 1.18 1.13 0.90 0.77 1.36 2.38 1.92 ppm Be 3 3 3 3 2 2 3 2 2 Sc 3 35 25 20 25 25 25 25 30 V 13 220 260 195 260 190 230 210 210 Cr 3 110 8 45 9 110 52 48 48 Co 3 63 53 42 60 55 72 60 64 Ni 3 66 18 41 21 72 45 41 41 Cu 1 66 135 72 175 53 65 53 53 Zn 45 140 155 91 145 140 160 135 165 Ga 22 23 25 24 25 24 28 26 26 As 3 n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Se 0 <0.5 <0.5 2 1 <0.5 2 <0.5 2 Rb 270 50 63 78 31 47 76 76 76 Sr 105 340 1500 650 1200 750 1050 1050 950 Y 23 28 36 21 33 16 28 25 27 Zr 165 200 95 130 64 88 90 84 105 Nb 18 9 12 9 9 10 11 11 12 Mo 0 2 0 1 1 1 1 1 1 Ag 0 0 0 <0.1 <0.1 <0.1 0 0 0 Cd 0 0 0 0 0 0 0 0 0 In 0 0 0 <0.05 0 0 0 0 0 Sn 4 n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Sb 0 <0.5 <0.5 <0.5 <0.5 <0.5 <0.5 <0.5 <0.5 Te 0 <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 Cs 2 10 6 12 4 2 5 6 4 Ba 470 650 2650 850 1100 850 2100 1950 2000 La 63 69 210 82 160 73 110 100 91 Ce 105 120 350 120 280 115 190 170 160 Pr 12 16 52 18 41 15 27 26 24 Nd 41 54 190 61 155 54 100 96 91 Sm 7 9 29 9 24 9 17 16 16 Eu 1 2 7 3 5 3 4 4 4 Gd 5 7 17 6 14 5 10 9 10 Tb 1 1 2 1 2 1 1 1 1 Dy 4 5 8 4 8 3 6 6 6 Ho 1 1 1 1 1 1 1 1 1 Er 2 3 3 2 4 2 3 2 3 Tm 0 0 1 0 0 0 0 0 0 Yb 2 3 3 2 3 1 2 2 2 Lu 0 0 0 0 0 0 0 0 0 Hf 6 4 3 3 2 3 2 3 3 Ta 0 <2 <2 <2 <2 <2 <2 <2 <2 W 0 n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ru ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Rh ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pd ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ir ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Os ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pt ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Au ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Tl 2 0 0 1 0 0 0 0 0 Pb 31 12 17 18 12 14 15 21 17 Bi 0 0 0 0 <0.1 <0.1 0 0 0 Th 50 10 13 12 7 13 12 9 10 U 12 2 2 2 1 1 2 2 2 Traces 0.15 0.23 0.60 0.26 0.39 0.27 0.45 0.43 0.43 Totals 99.94 100.12 99.67 99.75 99.21 99.46 99.41 99.65 99.60

A287

Dead Bullock Soak

Sample TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 Number AD331R11 AD81R1 AD332R1a AD332R1b AD333R1 AD333R2 AD334R1 AD335R1 AD336R1 wt% SiO2 47.30 49.70 50.90 50.50 48.00 48.70 58.90 50.10 37.70 TiO2 1.43 0.63 0.89 0.88 0.66 0.71 0.52 0.97 1.76 Al2O3 15.30 14.30 11.30 11.30 15.90 14.30 14.20 13.70 13.60 Fe2O3T 12.70 10.80 10.60 10.50 11.70 12.90 6.29 11.20 22.10 MnO 0.16 0.18 0.14 0.14 0.17 0.19 0.07 0.15 0.23 MgO 6.39 8.53 8.81 8.74 7.61 7.73 5.58 6.04 4.44 CaO 9.32 10.80 8.69 8.45 9.87 9.69 6.48 7.46 11.10 Na2O 2.19 1.86 1.44 1.28 1.85 1.77 3.16 2.34 0.55 K2O 1.93 0.89 1.67 1.95 0.71 0.65 1.51 2.21 1.55 P2O5 0.87 0.06 0.54 0.54 0.07 0.07 0.28 0.45 0.04 LOI 1.27 1.72 3.94 4.54 3.03 3.01 2.02 4.58 6.40 ppm Be 3 <2 3 4 <2 <2 3 3 3 Sc 30 45 30 30 35 40 20 30 45 V 210 220 190 180 220 250 110 230 320 Cr 46 190 330 320 87 110 165 140 360 Co 50 59 45 41 60 72 40 44 66 Ni 43 135 76 74 145 140 135 81 230 Cu 50 72 56 59 89 175 3 28 165 Zn 145 71 175 175 105 135 73 105 185 Ga 22 19 16 15 16 20 19 21 26 As n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Se 3 <0.5 <0.5 <0.5 1 2 <0.5 <0.5 2 Rb 68 28 66 79 27 19 35 71 34 Sr 1050 120 460 430 130 140 400 550 59 Y 22 17 19 18 14 19 14 24 27 Zr 87 31 210 210 30 36 175 180 105 Nb 11 5 12 11 5 5 11 11 10 Mo 1 1 <0.1 <0.1 0 0 0 0 0 Ag 0 <0.1 0 0 <0.1 <0.1 0 0 0 Cd 0 0 0 0 0 0 0 0 0 In 0 <0.05 <0.05 0 <0.05 0 0 0 0 Sn n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Sb <0.5 1 <0.5 <0.5 <0.5 1 <0.5 <0.5 <0.5 Te <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 1 Cs 3 4 4 7 1 1 1 3 1 Ba 1900 80 1200 1250 55 90 270 1250 280 La 85 4 95 95 5 6 58 53 12 Ce 145 8 145 145 8 13 93 97 25 Pr 23 2 19 19 2 2 12 14 4 Nd 85 8 71 70 8 8 43 50 15 Sm 15 2 13 13 2 2 7 10 4 Eu 4 1 3 3 1 1 2 2 1 Gd 9 2 8 8 2 2 5 7 4 Tb 1 0 1 1 0 0 1 1 1 Dy 5 3 5 5 3 3 3 5 5 Ho 1 1 1 1 0 1 0 1 1 Er 2 2 2 2 2 2 1 2 2 Tm 0 0 0 0 0 0 0 0 0 Yb 2 2 2 2 2 2 1 2 3 Lu 0 0 0 0 0 0 0 0 0 Hf 3 1 5 6 <1 1 3 3 2 Ta <2 <2 2 2 <2 <2 <2 <2 <2 W n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ru ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Rh ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pd ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ir ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Os ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pt ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Au ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Tl 0 0 0 0 <0.1 0 0 1 0 Pb 12 13 28 28 4 4 27 38 7 Bi <0.1 0 0 0 <0.1 <0.1 <0.1 0 <0.1 Th 9 2 25 26 1 2 30 20 2 U 1 1 9 9 0 1 8 5 0 Traces 0.41 0.11 0.33 0.33 0.11 0.13 0.18 0.31 0.20 Totals 99.27 99.58 99.25 99.15 99.67 99.85 99.18 99.50 99.67

A288 Table A5 cont.

Sample TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 Number AD336R3 AD337R1 AD339R1 AD340R1 AD341R1 AD342R1 AD342R2 AD342R3 AD343 R1 wt% SiO2 49.20 49.30 48.70 31.80 50.20 50.30 47.60 37.70 54.40 TiO2 0.91 0.67 0.65 1.02 0.79 0.68 2.31 1.41 0.63 Al2O3 12.90 11.20 15.30 10.70 14.40 11.40 8.26 12.50 14.20 Fe2O3T 11.30 9.57 11.90 9.14 12.80 9.96 9.55 18.40 8.75 MnO 0.17 0.13 0.17 0.36 0.20 0.14 0.14 0.24 0.14 MgO 8.24 11.60 7.76 2.18 6.52 10.80 12.40 4.43 8.54 CaO 8.57 8.76 10.00 27.30 9.34 9.16 8.22 16.40 7.71 Na2O 1.70 1.31 1.77 0.23 2.17 1.47 0.11 0.98 1.70 K2O 2.46 3.15 0.70 0.42 1.00 1.63 4.58 0.61 1.57 P2O5 0.47 0.53 0.06 0.12 0.08 0.56 2.86 0.16 0.12 LOI 3.42 2.90 2.71 16.20 1.88 3.11 2.76 6.68 1.33 ppm Be 4 5 2 3 <2 4 7 2 2 Sc 35 30 35 30 45 30 25 40 25 V 240 190 220 195 280 190 155 320 150 Cr 310 500 97 135 66 470 330 175 290 Co 56 60 71 47 64 57 52 76 55 Ni 135 250 155 105 67 250 350 200 160 Cu 55 30 150 41 130 3 84 47 16 Zn 82 88 87 63 105 79 110 140 80 Ga 20 17 17 22 20 16 16 25 20 As n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Se 1 <0.5 1 1 2 <0.5 2 2 <0.5 Rb 90 110 25 3 31 49 230 <1 64 Sr 500 360 135 190 210 400 650 130 155 Y 25 21 15 39 20 22 47 24 18 Zr 190 240 32 64 40 260 180 90 100 Nb 12 15 3 9 6 15 50 9 9 Mo 0 0 0 1 0 2 0 3 1 Ag 0 0 <0.1 <0.1 <0.1 0 0 0 <0.1 Cd 0 0 0 0 0 0 0 0 <0.1 In 0 0 0 0 0 0 0 0 <0.05 Sn n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Sb <0.5 <0.5 <0.5 1 2 <0.5 <0.5 <0.5 <0.5 Te <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 1 <0.2 <0.2 Cs 4 3 2 <0.1 0 2 6 0 9 Ba 1400 1600 45 20 170 850 2200 65 280 La 53 68 4 18 5 71 400 24 21 Ce 94 115 7 35 9 125 700 41 37 Pr 13 16 1 5 2 17 100 7 5 Nd 50 59 7 22 8 62 370 27 18 Sm 10 12 2 6 3 12 58 6 4 Eu 3 3 1 2 1 3 13 2 1 Gd 7 7 2 6 3 8 32 5 3 Tb 1 1 0 1 0 1 3 1 0 Dy 5 4 3 6 3 5 13 5 3 Ho 1 1 1 1 1 1 2 1 1 Er 2 2 1 3 2 2 4 3 2 Tm 0 0 0 1 0 0 0 0 0 Yb 2 2 2 3 2 2 3 2 2 Lu 0 0 0 1 0 0 0 0 0 Hf 4 5 1 1 1 5 28 3 2 Ta <2 <2 <2 <2 <2 <2 3 <2 <2 W n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ru ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Rh ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pd ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ir ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Os ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pt ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Au ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Tl 1 1 <0.1 1 0 0 1 <0.1 1 Pb 18 19 2 15 3 30 95 20 10 Bi 0 0 <0.1 1 <0.1 <0.1 1 0 <0.1 Th 25 34 1 4 1 37 48 2 8 U 6 8 0 1 0 9 7 0 2 Traces 0.35 0.39 0.11 0.11 0.13 0.31 0.80 0.15 0.16 Totals 99.68 99.50 99.83 99.58 99.51 99.51 99.59 99.66 99.25

A289

The East Granites Ptilotus Sample TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 Number AD344R1 AD345R1 AD346R1 AD347R1 AD74R1 AD80R1 MH412R1 MH412R2 MH414R1 wt% SiO2 73.80 70.50 48.40 45.20 49.80 67.40 54.90 53.10 52.20 TiO2 0.04 0.31 0.60 3.57 0.69 0.49 1.20 0.63 1.30 Al2O3 14.30 14.30 13.00 11.70 14.50 15.10 17.40 14.80 13.00 Fe2O3T 1.18 2.98 10.40 18.90 10.60 4.19 13.90 8.88 14.30 MnO 0.12 0.05 0.18 0.24 0.17 0.05 0.06 0.17 0.18 MgO 0.20 1.02 8.04 4.12 7.47 1.69 3.38 8.04 2.21 CaO 0.48 2.22 9.15 7.86 10.20 2.68 0.34 7.72 4.02 Na2O 3.96 3.47 2.14 2.61 2.05 2.77 2.20 1.80 3.02 K2O 4.10 3.41 1.00 1.11 1.06 2.13 3.26 1.76 2.13 P2O5 0.18 0.08 0.17 0.79 0.07 0.13 0.09 0.11 0.55 LOI 0.77 0.89 6.19 3.25 2.81 2.64 2.75 1.85 6.67 ppm Be 4 3 2 2 <2 2 3 3 4 Sc <5 5 45 30 45 10 30 25 20 V <2 32 260 210 220 56 190 155 13 Cr <2 7 210 5 175 16 155 200 3 Co 38 50 49 57 47 23 61 58 66 Ni 3 7 50 11 84 26 125 135 <2 Cu 4 10 28 82 81 22 115 29 14 Zn 37 53 71 165 83 240 150 80 220 Ga 18 22 16 29 18 25 30 20 39 As n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Se 1 2 1 2 1 1 1 <0.5 <0.5 Rb 410 125 34 17 39 77 80 65 41 Sr 25 240 300 360 155 195 32 160 330 Y 8 15 20 36 16 15 9 17 51 Zr 31 140 50 310 34 175 135 97 600 Nb 10 13 6 29 5 12 14 9 44 Mo 0 1 0 2 0 0 0 1 3 Ag 0 0 <0.1 1 <0.1 0 0 <0.1 1 Cd 0 0 <0.1 0 0 0 <0.1 <0.1 0 In <0.05 <0.05 0 0 0 <0.05 0 <0.05 0 Sn n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Sb <0.5 <0.5 1 1 1 <0.5 <0.5 <0.5 <0.5 Te <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 Cs 33 6 3 1 1 3 15 7 5 Ba 55 800 450 410 65 550 600 360 950 La 3 45 14 41 3 29 32 18 74 Ce 6 69 23 78 7 41 49 34 125 Pr 1 8 4 12 2 7 7 4 19 Nd 4 27 16 51 7 23 25 16 79 Sm 1 5 4 11 2 4 5 3 17 Eu 0 1 1 4 1 1 1 1 5 Gd 1 3 3 10 2 3 4 3 13 Tb 0 0 0 1 0 0 0 0 2 Dy 1 2 4 8 3 3 2 3 11 Ho 0 0 1 1 1 0 0 1 2 Er 1 1 2 4 2 1 1 2 5 Tm 0 0 0 1 0 0 0 0 1 Yb 1 1 2 3 2 1 1 2 5 Lu 0 0 0 0 0 0 0 0 1 Hf 2 3 1 5 2 4 4 3 13 Ta 4 2 <2 3 <2 <2 4 2 6 W n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ru ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Rh ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pd ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ir ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Os ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pt ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Au ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Tl 2 1 0 <0.1 <0.1 0 0 0 0 Pb 19 29 9 7 3 17 6 12 66 Bi 0 <0.1 0 <0.1 <0.1 0 0 <0.1 <0.1 Th 4 17 4 5 1 14 11 7 10 U 17 6 1 1 0 3 2 2 3 Traces 0.07 0.17 0.17 0.20 0.11 0.16 0.19 0.15 0.29 Totals 99.20 99.40 99.43 99.55 99.53 99.42 99.67 99.01 99.87

A290 Table A5 cont. Mafic Extrusives

Officer Hill Rabbit Flat Tanami Mine Sample TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 Number MH709R1 AD109R3 AD110R1a AD110R1b AD129R1 AD131R1 AD4R2 AD63R1a AD63R1b 99496215 wt% SiO2 45.08 51.50 44.50 43.20 51.10 50.20 47.30 42.30 57.90 TiO2 3.88 0.80 3.72 3.77 1.67 1.24 1.70 1.86 0.53 Al2O3 12.67 12.30 11.60 11.60 11.80 12.40 12.40 11.60 15.00 Fe2O3T 18.60 14.80 16.50 17.00 14.30 15.00 16.90 17.60 5.13 MnO 0.22 0.22 0.23 0.23 0.14 0.22 0.23 0.24 0.13 MgO 4.17 5.55 6.94 7.18 3.32 5.47 5.42 5.44 3.21 CaO 6.50 9.69 11.50 11.30 14.40 9.97 7.18 6.62 3.93 Na2O 2.24 2.51 0.56 0.54 0.18 2.73 3.59 1.54 3.49 K2O 1.80 0.31 0.73 0.77 0.13 0.18 0.15 0.62 2.05 P2O5 0.65 0.10 0.70 0.74 0.17 0.12 0.19 0.21 0.14 LOI 5.04 1.69 2.33 3.46 2.21 1.79 4.50 11.80 8.51 ppm Be 1 <2 5 5 <2 <2 3 3 <2 Sc 27 50 25 25 35 40 40 30 10 V 252 300 250 250 290 340 410 330 83 Cr -1 38 75 69 54 26 62 26 75 Co n.d. 60 56 55 62 72 56 58 21 Ni 43 62 91 84 61 59 63 61 68 Cu 58 115 26 26 105 105 290 230 46 Zn 155 130 350 380 92 115 280 240 50 Ga 25 18 29 30 38 19 21 20 24 As n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Se n.d. 1 1 <0.5 1 <0.5 2 1 <0.5 Rb 55 <1 22 25 <1 <1 <1 8 55 Sr 280 145 88 88 170 105 130 85 200 Y 39 33 31 34 33 27 34 21 17 Zr 281 50 430 440 130 91 135 155 155 Nb 27 6 59 60 11 10 9 10 8 Mo 2 0 2 2 1 0 0 1 3 Ag n.d. <0.1 2 2 <0.1 <0.1 0 0 <0.1 Cd n.d. 0 0 0 <0.1 <0.1 0 0 0 In n.d. <0.05 0 0 0 0 0 0 <0.05 Sn n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Sb 1 <0.5 <0.5 <0.5 <0.5 <0.5 <0.5 1 1 Te n.d. <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 Cs 4 0 1 1 0 <0.1 0 1 1 Ba 620 95 250 320 130 95 45 85 320 La 38 2 59 62 13 8 15 17 40 Ce 82 6 115 120 23 15 26 32 58 Pr 11 1 16 17 4 3 4 5 9 Nd 44 7 61 66 19 14 20 22 31 Sm 9 3 13 14 6 4 6 6 5 Eu 3 1 4 5 2 1 2 2 1 Gd 9 3 11 12 6 4 6 5 4 Tb 1 1 1 1 1 1 1 1 0 Dy 7 6 8 9 6 5 7 4 3 Ho 1 1 1 1 1 1 1 1 0 Er 4 4 3 3 3 3 4 2 1 Tm n.d. 1 0 0 1 0 1 0 0 Yb 3 4 2 2 3 3 4 3 1 Lu 0 1 0 0 0 0 1 0 0 Hf n.d. 2 9 9 4 2 4 5 3 Ta 2 <2 6 6 <2 <2 <2 <2 <2 W n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ru ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Rh ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pd ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ir ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Os ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pt ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Au ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Tl n.d. <0.1 <0.1 <0.1 <0.1 <0.1 <0.1 <0.1 0 Pb 5 5 4 4 8 3 4 4 9 Bi 0 <0.1 <0.1 0 <0.1 <0.1 <0.1 <0.1 <0.1 Th 5 1 5 5 2 2 2 2 17 U 1 0 1 1 1 0 1 1 4 Traces 0.19 0.11 0.21 0.22 0.13 0.12 0.17 0.15 0.13 Totals 101.04 99.58 99.52 100.01 99.55 99.44 99.73 99.98 100.15

A291

Mac- Ptilotus Farlane Sample TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 TAN99 Number AD63R4 AD68R1 AD230R1 AD65R1 MH676R1 MH682R2 MH679R1 MH437R1a MH 437R1b wt% SiO2 41.60 53.40 47.10 43.50 48.40 47.70 49.60 60.10 52.20 TiO2 1.08 0.91 1.64 0.84 0.78 0.84 0.62 1.73 2.14 Al2O3 12.80 13.40 13.20 11.80 14.20 14.70 14.20 10.20 12.00 Fe2O3T 13.70 7.30 15.80 7.99 11.50 11.70 10.30 13.20 15.40 MnO 0.17 0.10 0.19 0.22 0.20 0.25 0.17 0.17 0.21 MgO 6.61 5.33 7.11 5.67 7.82 8.57 8.70 3.97 4.64 CaO 6.35 5.85 6.74 9.28 12.00 11.00 12.40 5.56 6.71 Na2O 0.60 2.63 3.21 0.24 1.15 1.39 1.66 2.96 3.52 K2O 1.32 1.85 0.13 2.66 0.41 0.81 0.28 0.21 0.22 P2O5 0.10 0.25 0.16 0.07 0.07 0.07 0.06 0.24 0.30 LOI 15.20 8.72 3.63 17.55 2.52 2.17 1.01 0.61 2.10 ppm Be <2 2 <2 <2 2 <2 3 2 4 Sc 35 20 40 35 45 45 40 25 30 V 250 125 340 240 230 240 185 260 220 Cr 150 100 74 48 200 210 290 32 33 Co 67 37 63 49 51 50 56 49 49 Ni 200 92 95 66 120 125 145 54 61 Cu 170 45 150 220 11 210 54 135 125 Zn 105 92 130 47 165 210 150 240 280 Ga 23 24 20 20 16 15 15 16 18 As n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Se 1 <0.5 1 1 <0.5 <0.5 <0.5 <0.5 <0.5 Rb 28 44 <1 62 10 31 <1 <1 <1 Sr 80 210 98 73 180 160 130 46 51 Y 11 17 26 17 16 16 19 33 44 Zr 90 175 105 54 37 40 67 185 230 Nb 8 7 8 5 5 5 8 13 15 Mo 1 0 0 0 0 0 0 0 0 Ag <0.1 <0.1 <0.1 <0.1 <0.1 <0.1 0 0 0 Cd 0 <0.1 <0.1 0 0 0 0 <0.1 0 In 0 <0.05 0 <0.05 0 0 0 0 0 Sn n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Sb 1 <0.5 <0.5 1 <0.5 <0.5 <0.5 <0.5 <0.5 Te <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 <0.2 Cs 2 1 0 2 1 3 0 <0.1 0 Ba 80 300 20 130 35 180 300 70 65 La 8 43 5 5 4 7 10 6 14 Ce 15 66 11 9 10 12 15 11 19 Pr 3 10 3 2 2 2 3 2 3 Nd 13 36 13 10 7 7 12 12 16 Sm 3 7 4 3 2 2 3 5 6 Eu 1 2 1 1 1 1 1 1 2 Gd 2 4 5 3 2 2 3 6 7 Tb 0 1 1 0 0 0 1 1 1 Dy 2 3 5 3 3 3 4 7 8 Ho 0 1 1 1 1 1 1 1 1 Er 1 2 3 2 2 2 2 3 5 Tm 0 0 0 0 0 0 0 1 1 Yb 1 2 3 2 2 2 2 4 5 Lu 0 0 0 0 0 0 0 1 1 Hf 3 4 3 2 2 2 2 5 5 Ta <2 <2 <2 <2 <2 <2 <2 <2 <2 W n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ru ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Rh ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pd ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Ir ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Os ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Pt ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Au ppb n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. Tl <0.1 0 <0.1 0 <0.1 <0.1 <0.1 <0.1 <0.1 Pb 2 5 2 3 3 7 1 2 3 Bi <0.1 <0.1 <0.1 <0.1 1 <0.1 <0.1 <0.1 0 Th 2 20 0 1 0 0 1 2 2 U 1 4 0 0 0 0 0 1 1 Traces 0.14 0.15 0.12 0.11 0.12 0.16 0.15 0.12 0.13 Totals 99.67 99.89 99.03 99.93 99.16 99.36 99.15 99.07 99.57

A292