Detrital Zircon Analysis of Permian Victoria Group Sandstones, Transantarctic Mountains, Antarctica

Home , Beacon Supergroup, Cape Denison, Ellsworth Mountains, Fremouw Formation, Gangamopteris, Geology of Antarctica

THESIS

Presented in Partial Fulfillment of the Requirements for the Degree Master of Science in the Graduate School of The Ohio State University

Samuel Hulett

Graduate Program in Geological Sciences

The Ohio State University

2012

Master's Examination Committee:

David Elliot, Advisor

Matt Saltzman

Larry Krissek

Samuel Hulett

2012

Abstract

The Beacon Supergroup in the central Transantarctic Mountains, the Gondwana sequence of Antarctica, comprises Devonian (inferred) and Permian-Triassic strata. The latter were deposited in an intracratonic basin which evolved into a foreland basin in mid Permian time. Sedimentary petrology and paleocurrent data indicate that this basin had two major detrital sources, a cratonic source and a volcaniclastic source that characterizes the upper

Buckley Formation and younger Triassic beds. In order to investigate the sedimentary provenance further, detrital zircons have been examined from both flanks of the basin. At

Clarkson Peak, samples were collected from the lower (quartzose) and upper

(volcaniclastic) Buckley Formation. At Mt. Bowers the complete Permian section, from pre-glacial to upper Buckley strata, was collected. Results show varied zircon age provenance, reflecting multiple source regions. In all pre-upper Buckley samples the major zircon provenance is in the 650-480 Ma age range, corresponding to overlapping

Ross and Pan African orogenic events, with a subsidiary province of “Grenville age”,

~1000 Ma. These age range variations reflect the influence of multiple sub-provinces.

There are also minor contributions from older Proterozoic sources, including a ~1500 Ma source that waned in Fairchild time and is nearly absent in the Buckley Formation. These older Proterozoic zircons were likely sourced from the coast of East Antarctica. A major shift in paleoflow directions between the lower and upper Buckley at both localities is accompanied by a significant input of Permian-age igneous zircons, documenting contemporaneous magmatism and flooding of the basin with detritus from an active magmatic arc. There is also a minor input of ~370 Ma grains which were most likely sourced from Devonian granitoids in West Antarctica.

Dedication

This document is dedicated to my parents, for all their help and encouragement when I

needed it most.

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Acknowledgments

I would like to extend a special thanks to: David Elliot, for his patience and help; the pilots of Petroleum Helicopters Incorporated for their invaluable assistance in getting to

field sites and the National Science Foundation for funding this project.

Vita

May 2006 ...... Licking Valley High School

May 2010……………………………………B.S Earth Sciences, Ohio State University

September 2010 to present…………Graduate Research Assistant, Ohio State Univeristy

Fields of Study

Major Field: Geological Sciences

Table of Contents Copyright ...... i Abstract ...... ii Dedication ...... iii Acknowledgments...... iv Vita ...... v Table of Contents ...... vi List Of Figures ...... viii List of Tables ...... xiii Chapter 1: Introduction ...... 1 Exposures in East Antarctica ...... 3 Exposures in West Antarctica...... 6 1.2 Geologic History ...... 7 Geologic History of East Antarctica ...... 7 Geologic History of West Antarctica ...... 11 1.3 The Transantarctic Mountains ...... 13 Stratigraphy of the Transantarctic Mountains ...... 13 Previous Provenance Studies in the TAM ...... 19 Previous Detrital Zircon Studies in the TAM ...... 19 Chapter 2: The Central Transantarctic Mountains ...... 22 2.1 Stratigraphy in the Central Transantarctic Mountains ...... 22 The Alexandra Formation ...... 22 The Pagoda Formation...... 27 The Mackellar Formation ...... 27 The Fairchild Formation ...... 28 The lower Buckley Formation ...... 28 The upper Buckley Formation ...... 29

Triassic strata ...... 29 2.2 Areas Specific to This Study ...... 30 Bunker Cwm (Lat: 83.17°S Long: 164.00°E) ...... 30 Clarkson Peak (Lat: 83°19’S Long: 164°34’E) ...... 31 Tillite Glacier ( Lat: 83°51’S Long: 166° 0’E) ...... 31 Mt. Weeks (Lat: 83°33’S Long: 160°54’E) ...... 33 Mt. Bowers (Lat: 85° 0’S Long: 164° 5’E) ...... 34 Mt. Achernar (Lat: 84°12’S Long: 160°56’E) ...... 37 Chapter 3: Methods ...... 39 3.1 Field Methods ...... 39 3.2 Laboratory methods...... 39 Chapter 4: Petrography ...... 41 Chapter 5: Results ...... 42 11-4-3 (lower Buckley Formation, Clarkson Peak) ...... 42 11-4-10 (upper Buckley Formation, Clarkson Peak) ...... 44 11-5-2 (Pre-Pagoda Sandstone, Mt Bowers) ...... 44 11-9-2 (Pagoda Formation, Mt Weeks)...... 49 11-5-8 (Fairchild Formation, Mt Bowers)...... 49 11-5-15 (lower Buckley Formation, Mt Bowers)...... 52 11-5-22 (upper Buckley Formation, Mt Bowers)...... 52 Chapter 5: Discussion ...... 59 5.1: >2500 Ma (Archean) ...... 59 5.2: 1300-2500 Ma ( Early Mesoproterozoic and Paleoproterozoic) ...... 61 5.3: 1000-1300 Ma (late Mesoproterozoic)...... 64 5.4: 480-650 Ma (Cambro-Ordovician to Neoproterozoic) ...... 66 5.5: 460 Ma (Ordovician) ...... 69 5.6: 260 Ma (Late Permian) ...... 70 Chapter 6: Conclusions ...... 74 References ...... 78 Appendix A: Raw Data and Concordia Plots ...... 83 Appendix B: Thin Section Descriptions ...... 97

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List Of Figures

Figure 1. Map of Antarctica with relevant places labeled. Grey shaded areas are major outcrops, black dots are smaller outcrops...... 2

Figure 2. Subglacial topography map of Antarctica. Modified from the British Antarctic Survey BEDMAP Project (Bedmap Consortium, 2000)...... 4

Figure 3. Map of Antarctica with possible subglacial extent of bedrock provinces. A: Mawson Craton. B: Wilkes Province C: Maud Province. D:Rayner Province . E: Albany- Fraser-Wilkes Orogen. F: Pinjarra Orogen (3 possible extents) G: East African Orogen H: Ross Orogen. I: Ross Province. J: Amundsen Province. East Antarctic provinces and terminology from Fitzsimons (2003), West Antarctic provinces and terminology from Pankhurst et al. (1998)...... 5

Figure 4. Paleogeographic reconstruction of Antarctica during the Permian. A: Mawson Craton. B: Albany-Fraser-Wilkes Orogen. C: Pinjarra Orogen (3 possible extents). D: East African Orogen. E: Ross Orogen. F: Ross Province. G: Amundsen Province. East Gondwana reco nstruction modified from Elliot and Fanning 2008, with provinces and terminology from Pankhurst et al. (1998)...... 8

Figure 5. Correlation diagram for the Transantarctic Mountains and Ellsworth Mountains. All formations are sedimentary, except for the Admiralty Intrusives and the Kirkpatrick Basalt. Modified from Collinson et al. (1994) to include Devonian rocks. Devonian formations from Barrett et al. (1986). Timescale according to Cohen et al., 2012. Parallel hachures represent a time break. Epochs are as follows: Permian; Cisuralian, Guadalupian, Lopingian. Triassic; Lower, Middle, Upper...... 14

Figure 6. Simplified stratigraphic column for the central Transantarctic Mountains. Modified from Elliot and Fanning (2008)...... 23

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Figure 7. Map of the Beardmore Glacier region with major field localities labeled. Arrow indicates mean paleocurrent direction for the inboard flank of the basin. Modified from Elliot and Fanning (2008)...... 24

Figure 8. Combined and simplified stratigraphic column for Mt Bowers and Mt Weeks. Pagoda Formation section taken from Mt Weeks, all other formations from Mt Bowers.25

Figure 9. Simplified stratigraphic column for Clarkson Peak...... 26

Figure 10. a: Sample location 11-4-3, the lower Buckley Formation, Clarkson Peak. Slope-forming sandstones directly overlying a dolerite sill, followed by shale stretching into the background. b: Sample location 11-9-2, the Pagoda Formation, Mt Weeks. Diamictite (darker) overlain by alternating conglomerate and parallel bedded sandstone. White line marks the lower contact of the diamictite. Ice axe (1m) for scale. Picture credits: David Elliot ...... 32

Figure 11. a: Sample location 11-5-8, Fairchild Formation, Mt Bowers. First sandstone bluff marking the Mackellar-Fairchild contact. Overlain by slope-forming sandstones. b: Sample location 11-5-15, the lower Buckley Formation, Mt Bowers. Channel sandstone following a mudstone/fine-grained sandstone interval. White line represents the channel bottom. Color variations above channel are due to weathering differences. Picture credits: David Elliot ...... 36

Figure 12. Zircon textures represented in this study; all interpretations are consistent with Corfu et al. (2003). A: 12.1- Elongate, euhedral, well-zoned igneous zircon, fractured. From sample 11-5-22, upper Buckley Formation. B: 45.1- Equant, euhedral, well-zoned igneous zircon, slightly rounded. From sample 11-4-3, lower Buckley Formation. C: 52.1- Sector zoned, subhedral igneous grain, slightly abraded. From sample 11-5-2, pre- Pagoda sandstone. D: 6.1- Grain with unmeasurable rim, most likely a very late stage of crystallization. From sample 11-4-3, lower Buckley Formation. E: 48.1- Poorly zoned, amorphous metamorphic grain, well rounded. From sample 11-5-2, pre-Pagoda sandstone. F: 1.1- Poorly zoned metamorphic grain with a prominent core. Core also shows sector zoning. From sample 11-4-3, lower Buckley Formation...... 43

Figure 13. Detrital zircon age-probability histogram and representative CL image for sample 11-4-3, lower Buckley Formation, Clarkson Peak. Grain 61.1 shows igneous zonation, and 58.1 has a core...... 45

Figure 14. Detrital zircon age-probability histogram focused on Neoproterozoic- Ordovician time for sample 11-4-3, lower Buckley Formation, Clarkson Peak...... 46

Figure 15. Detrital zircon age-probability histogram and representative CL image for sample 11-4-10, upper Buckley Formation, Clarkson Peak. Grains 42.1, 44.1 and 45.1 are euhedral and show igneous zonation...... 47

Figure 16. Detrital zircon age-probability histogram focused on the Permian Period for sample 11-4-10, upper Buckley Formation, Clarkson Peak...... 48

Figure 17. Detrital zircon age-probability histogram and representative CL image for sample 11-5-2, pre-Pagoda sandstone, Mt Bowers. Grain 40.1 shows igneous zonation. Grain 38 sampled both the rim and the core of the grain. The rim is late Neoproterozoic in age (1548 Ma) and the core is late Mesoproterozoic in age (1076 Ma)...... 50

Figure 18. Detrital zircon age-probability histogram and representative CL image for sample 11-9-2, Pagoda Formation, Mt Weeks. Grain 1.1 lacks zonation, indicating metamorphic origin. Grain 4.1 is euhedral and shows igneous zonation...... 51

Figure 19. Detrital zircon age-probability histogram and representative CL image for sample 11-5-8, Fairchild Formation, Mt Bowers. Grains 54.1 and 57.1 suggest metamorphic origin...... 53

Figure 20. Detrital zircon age-probability histogram focused on Neoproterozoic- Ordovician time for sample 11-5-8, Fairchild Formation, Mt Bowers...... 54

Figure 21. Detrital zircon age-probability histogram and representative CL image for sample 11-5-15, lower Buckley Formation, Mt Bowers. Grain 8.1 shows sector zoning. Both the rim and core were analyzed in grain 12, and their ages are 556 Ma and 521 Ma respectively. The younger core is most likely due to lead loss from the core before rim crystallization...... 55

Figure 22. Detrital zircon age-probability histogram focused on Neoproterozoic- Ordovician time for sample 11-5-15, lower Buckley Formation, Mt Bowers...... 56

Figure 23. Detrital zircon age-probability histogram and representative CL image for sample 11-5-22, upper Buckley Formation, Mt Bowers. Grains 40.1,41.1, 45.1 and 46.1 are all euhedral and show igneous zonation...... 57

Figure 24. Detrital zircon age-probability histogram focused on the Permian Period for sample 11-5-22, upper Buckley Formation, Mt Bowers...... 58

Figure 25. Map of Antarctica with Archean Provinces circled. Ages from Tingey (1991)...... 60

Figure 26. Map of Antarctica with Meso- and Paleoproterozoic provinces circled. Ages from Fitzsimons (2003)...... 62

Figure 27. Map of Antarctica with “Grenville age” provinces circled. Names of provinces and ages taken from Fitzsimons (2000)...... 65

Figure 28. Map of Antarctica with Ross/Pan-African provinces labeled. Dates for the Transantarctic Mountains from Stump (1995). Dates for Queen Maud Land from Jacobs et al. (1998). Dates for Enderby Land and Wilkes Land from Tingey (1991)...... 67

Figure 29. Map of Antarctica illustrating the shift from older to younger detrital zircon ages from south to north. Analyses from south to north: Elliot and Fanning (2008), this study, Goodge and Fanning (2010) ...... 71

Figure 30. Map of Antarctica with Permian rocks in the Amundsen Province labeled. Dates from Pankhurst et al. (1998), Mukasa and Dalziel, (2000), Pankhurst et al. (1993) and Millar et al. (2002)...... 72

Figure 31. Compiled data from the inboard flank of the basin. Approximate percentages derived from data in Appendix A. Zircons dated outside the listed age ranges represent a minor component of the analyses and are ignored from these percentages...... 76

Figure 32. Compiled data from the outboard flank of the basin. Approximate percentages derived from data in Appendix A. Zircons dated outside the listed age ranges represent a minor component of the analyses and are ignored from these percentages...... 77

Figure 33. Tera-Wasserburg plot for sample 11-4-3, lower Buckley Formation, Clarkson Peak...... 84

Figure 34. Tera-Wasserburg plot for sample 11-4-10, upper Buckley Formation, Clarkson Peak...... 86

Figure 35. Tera-Wasserburg plot for sample 11-5-2, pre-Pagoda sandstone, Mt Bowers.88

Figure 36. Tera-Wasserburg plot for sample 11-9-2, Pagoda Formation, Mt Weeks...... 90

Figure 37. Tera-Wasserburg plot for sample 11-5-8, Fairchild Formation, Mt Bowers. . 92

Figure 38. Tera-Wasserburg plot for sample 11-5-15, lower Buckley Formation, Mt Bowers...... 94

Figure 39. Tera-Wasserburg plot for sample 11-5-22, upper Buckley Formation, Mt Bowers...... 96

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List of Tables

Table 1: 11-4-3 (lower Buckley Formation) ...... 83

Table 2: 11-4-10 (upper Buckley Formation) ...... 85

Table 3: 11-5-2 (pre-Pagoda sandstone) ...... 87

Table 4: 11-9-2 (Pagoda Formation)...... 89

Table 5: 11-5-8 (Fairchild Formation) ...... 91

Table 6: 11-5-15 (lower Buckley Formation) ...... 93

Table 7: 11-5-22 (upper Buckley Formation) ...... 95

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Chapter 1: Introduction

The geology of Antarctica is known through very limited outcrops and geophysical data (Fig. 1). Because ice covers 98% of the continent’s surface, most exposures occur in the coastal regions and the Transantarctic Mountains (Bentley, 1991).

Outcrop geology of the continent provides the only ground truth but subglacial geology must also be established in order to develop a proper understanding of the regional and continental scale geology. However, due to remoteness and cost, subglacial geology cannot be determined through conventional methods such as drilling for rock core. Thus, more indirect methods are needed in order to assess the subglacial geology.

This study seeks to establish the provenance ages for the Permian strata of the

Victoria Group in the Beardmore Glacier region of the central Transantarctic Mountains by use of detrital zircon U-Th-Pb dating. By understanding these source regions, it will be possible to infer connections with both known outcrops and subglacial geology. This technique has been used on sandstones since the mid-1960’s in order to determine the provenance of sandstones and understand crustal evolution (Davis et al., 2003). It has been used recently to understand inputs into a range of sedimentary basins throughout time (Amato and Mack, 2012; Dinis et al., 2012; Schmidt et al., 2012) and even provide evidence for continental linkages (Duan et al., 2012).

Figure 1. Map of Antarctica with relevant places labeled. Grey shaded areas are major outcrops, black dots are smaller outcrops.

1.1: Exposures in Antarctica Radar sounding has shown that Antarctica is divided into two major geographic regions, known as East and West Antarctica (Fig. 2) (Bentley, 1991). When adjusted for isostatic depression by the ice cover, the subglacial floor of East Antarctica is mostly above sea level, and four distinct topographic regions have been identified: the

Gamburtsev Subglacial Mountains that rise to over 3000m; a subglacial trough lying below the Amery Ice Shelf and Lambert Glacier; and two extensive basins separated by highlands in the Australian quadrant. In contrast, the subglacial floor in West Antarctica is mostly below sea level, even when corrected for isostatic depression (Bentley,

1991).The bedrock topography is dominated by the expression of the West Antarctic Rift

System, a depression that crosses central West Antarctica known as the Byrd Subglacial

Basin. There are also significant topographic highs with exposed rock in West Antarctica, such as the Ellsworth Mountains, parts of Marie Byrd Land and the Antarctic Peninsula.

Exposures in East Antarctica

Coastal exposures of East Antarctica consist of metamorphic and igneous rocks of

Precambrian age, comprising the East Antarctic Craton (Fig. 3). These Precambrian rocks include schists, gneisses and other high-grade metamorphic rocks, as well as widely distributed granitoids. The only inland exposure of the cratonic basement is in the Miller

Range of the Transantarctic Mountains. The Miller Range rocks, the Nimrod Group, are amphibolite facies gneisses having an Archean protolith (Goodge and Fanning, 1999).

The Nimrod Group also shows evidence of having been reworked both during

Figure 2. Subglacial topography map of Antarctica. Modified from the British Antarctic Survey BEDMAP Project (Bedmap Consortium, 2000).

Paleoproterozoic metamorphism and again during the Cambrian Ross Orogeny. Based on coastal exposures and formerly adjacent Gondwana continents, provinces of Pan African

(~650-540 Ma), so-called ‘Grenville’ (~1000 Ma), Proterozoic and Archean age are inferred to be present (Fitzsimons, 2003). Archean basement rocks are scattered in the coastal exposures of Antarctica, such as Queen Maud Land, the Windmill Islands and

Enderby Land. A Proterozoic province of approximately 1700 Ma age in the Australian quadrant of Antarctica is correlated with the Mawson Craton exposed in southern

Australia (Fig. 3, area A). This craton is inferred to extend into the interior flank of the

Transantarctic Mountains. ‘Grenville age’ provinces exist in three places in East

Antarctica: the ‘Wilkes Province’(Fig. 3, area B)., including the Bunger Hills and

Windmill Islands, the ‘Rayner Province’(Fig. 3, area C)., including the area west of the

Amery Ice Shelf in Enderby Land and the ‘Maud Province’(Fig. 3, area D), including the

Littlewood Nunataks and the Shackleton Range. Aeromagnetic studies also provide evidence for multiple lithologic provinces which have been linked to outcrop geology in the Transantarctic Mountains (Studinger et al., 2006, Goodge and Finn, 2010). These data indicate different subglacial provinces in south Victoria Land, the Miller Range of the central Transantarctic Mountains and the South Pole sector of the Transantarctic

Mountains.

Exposures in West Antarctica West Antarctica has much more varied outcrop geology than East Antarctica. The oldest known rocks in West Antarctica are Proterozoic granodiorite gneisses and granitic sheets found in the Haag Nunataks east of the Ellsworth Mountains (Fig. 3) (Tingey,

1991). Elsewhere in West Antarctica rocks of that age are assumed to underlie the

exposed Cambrian through Permian sequence of sedimentary and minor volcanic rock in the Ellsworth Mountains (Laird, 1991). The Antarctic Peninsula has outcrops of lightly metamorphosed upper Paleozoic turbidite sequences and some older basement gneisses and migmatites, but is dominated by Mesozoic and younger volcanic rocks and volcaniclastic sequences (Millar et al., 2002). In Marie Byrd Land the oldest outcrops are of metagreywackes, with late Ordovician-Silurian metamorphic ages, known as the

Swanson Group (Adams et al., 1995). Trace fossil evidence gives a probable depositional age in the late Cambrian or early Ordovician period (Bradshaw et al, 1983). Most outcrops in Marie Byrd Land are formed of Paleozoic and Mesozoic igneous and metamorphic rocks, some of which are covered by Cenozoic volcanic rocks. Isotopic and geochemical study of the igneous rocks of the area suggests division of Marie Byrd Land into two major groups (Fig. 3) (Pankhurst et al., 1998): the Ross Province (Fig. 3, area F), which contains the Swanson Group, is defined by Devonian granitoid intrusions that extend into North Victoria Land and New Zealand; and the outboard Amundsen Province

(Fig. 3, area G), defined by the presence of Permian-Triassic granitoids that crop out both in Marie Byrd Land and Thurston Island, and which also contains minor Ordovician-

Silurian granitoids.

1.2 Geologic History

Geologic History of East Antarctica Many events have shaped the rocks and the landscape of East Antarctica. Antarctica was part of the supercontinent of Gondwana which reached its final assembly at about 570-

550 Ma (Meert, 2003) (Fig. 4). East Antarctica was the center of a group of five continents, the others being Australia, India, South America and Africa. These regions

Figure 4. Paleogeographic reconstruction of Antarctica during the Permian. A: Mawson Craton. B: Albany-Fraser-Wilkes Orogen. C: Pinjarra Orogen (3 possible extents). D: East African Orogen. E: Ross Orogen. F: Ross Province. G: Amundsen Province. East Gondwana reconstruction modified from Elliot and Fanning 2008, with provinces and terminology from Pankhurst et al. (1998).

have been tied to Antarctica by petrologic similarities, paleomagnetic data, stratigraphy, geochronology and the ‘rewinding’ of ocean-floor magnetic anomalies (Vilas and

Valencio, 1970; Audley-Charles, 1983; Fitzsimons, 2000). Evidence of important events in the history of East Antarctica can be inferred by the examination of geologic provinces that connect Antarctica with its neighboring Gondwana continents. In Terre Adélie-King

George V Land, basement lithologies and zircon geochronology have established correlations with the Australian Kimban Orogeny at approximately 1700 Ma, tying the limited coastal outcrops with the Mawson Craton of Australia (Fig. 4, area A)

(Fitzsimons, 2003). Evidence of this orogen continues into the central Transantarctic

Mountains, where it is observed in the Miller Range. In the west Australian segment of

Antarctica an event known as the Albany-Fraser-Wilkes Orogen is defined by two stages of tectonism, one at 1350-1260 Ma and the other at 1210-1140 Ma (Fig. 4, area B).

Evidence for this event is seen in the Windmill Islands and the Bunger Hills, and the western limit of the orogen is the Darling Fault Zone, a structural boundary later reactivated during Gondwana breakup. The Darling Fault zone also forms the eastern limit of the Pinjarra Orogen (Fig. 4, area C). The Pinjarra Orogen is defined by the presence of two tectonic episodes, one at ~1080 Ma and the other at ~550 Ma, and is observed in the Prydz Bay-Amery Glacier area. This orogenic belt likely extends into the interior of East Antarctica, but it is not known exactly what path it takes beneath the glacial cover. West of Prydz Bay is the Rayner Complex, a “Grenville age” province inferred to be related to the Eastern Ghats mobile belt of India (Fitzsimons, 2000). The

African quadrant of East Antarctica records the 650-540 Ma Pan-African Orogen (Fig. 4, area D) (Jacobs et al, 1998). This East African extension of the Pan-African Orogeny is

seen in outcrop throughout Queen Maud Land, and is inferred to continue westward towards the Weddell Sea under ice cover.

The history of the present-day Transantarctic Mountains region of East

Antarctica was characterized by episodes of compressional tectonics, notably the Nimrod and Ross orogenies. The Nimrod orogeny is known from the rocks of the Nimrod Group, found in the Miller and Geologists ranges of the Transantarctic Mountains (Goodge and

Fanning, 1999). Nimrod Group rocks indicate major deep-crustal metamorphism and magmatism at ~1730-1720 Ma. Very little is known about the Nimrod orogeny because of significant overprinting by the Ross orogeny. The Ross events, occurring from 550-

~480 Ma, involved folding of upper Neoproterozoic-lower Paleozoic sedimentary rocks, metamorphism and intrusion of granitoids along the Paleo-Pacific margin of East

Antarctica (Fig. 4, area E) (Stump, 1995).

Denudation following the Ross orogeny created the Kukri Erosion Surface, a relatively flat surface on which Devonian sediment was deposited. Further denudation created the Maya Erosion Surface, inferred to have great relief due to the discontinuous nature of the strata deposited on it (Isbell et al., 1999). Following the creation of the

Maya erosion surface, Permian glaciation created ice-scoured basins and morphological features, and deposited tills in many parts of the Transantarctic Mountains. Fluvial sedimentation dominated the Transantarctic Mountains region during post-glacial

Permian and Triassic time. Extension during early Jurassic time, related to the breakup of

Gondwana, is inferred from the presence of the Ferrar Group dolerite sills and basaltic flows which intrude and overlie the Beacon sedimentary rocks. Although the reasons for uplift of the Transantarctic Mountains are the subject of current debate (Bialas et al.,

2007; van Wijk et al., 2008), the mountain range is known to consist of deeply incised and uplifted fault blocks.

Geologic History of West Antarctica All paleogeographic reconstructions of West Antarctica during Gondwana time have some issues reconciling crustal blocks, geology and space issues (Fig. 4). West

Antarctica consists of four small crustal blocks: Marie Byrd Land, the Ellsworth and

Whitmore mountains, Thurston Island and the Antarctic Peninsula. The positions of these crustal blocks are known to have changed since Gondwana time based on structural trends and paleomagnetic data. In particular, the Ellsworth-Whitmore and Thurston

Island crustal blocks are known to be displaced and to have undergone rotation (Grunow et al., 1991). In the Ellsworth Mountains, structural trends of Gondwanide age are rotated

90º counterclockwise from their original position. By using paleomagnetic measurements, Grunow et al. (1987) found that this rotation must have occurred between

230 and 175 Ma. Paleomagnetic data also show that Thurston Island underwent 90º of counterclockwise rotation before 175 Ma (Grunow et al., 1991). Paleomagnetic data cannot constrain the movements of all of the crustal blocks in West Antarctica due to the lack of rotation in the blocks. However, terrane belts that are continuous from New

Zealand to the Antarctic Peninsula provide critical constraints on the positions of these blocks (Pankhurst et al., 1998; Vaughan and Storey, 2000).

The innermost and oldest of these terrane belts is known as the Ross Province in

Marie Byrd Land and the Eastern Domain in the Antarctic Peninsula (Fig. 4, area F)

(Vaughan and Storey, 2000). Inherited zircons in Late Paleozoic-Mesozoic granites, migmatites and gneisses suggest that Mesoproterozoic sources underlie this terrane

(Mukasa & Dalziel, 2000). The oldest exposed rocks in this province are Ordovician turbidites of the Swanson Group from Marie Byrd Land, suggesting a submarine fan depositional setting (Bradshaw et al., 1983). These were intruded by plutons of the Ford

Granodiorite at around 375 Ma, an event also recognized at Target Hill in the Antarctic

Peninsula (Millar et al., 2002). Similarly, a suite of granitoids emplaced between 340-320

Ma is also recognized in both Marie Byrd Land and the Antarctic Peninsula (Pankhurst et al., 1998). Later igneous events in the Eastern Domain included the emplacement of the

Ellsworth Land Volcanic Group, which is a suite of Gondwana breakup volcanic rocks, and Mid-Cretaceous arc plutonic rocks (Hunter et al., 2006).

Outboard of the Ross Province/Eastern Domain is what is termed, in Marie Byrd

Land, the Amundsen Province, and in the Antarctic Peninsula, the Central Domain (Fig.

4, area G). These are magmatic arc terranes linked by timing and rock type emplaced.

The Amundsen Province is defined by the presence of Permo-Triassic granitoids. This

Permian-Triassic arc is related to a fold-thrust belt recognized in deformed upper Permian sedimentary rocks in the Ellsworth and Pensacola mountains (Collinson et al., 1994). The basin created during this event extended from the Ellsworth Mountains to the central

Transantarctic Mountains. Vaughan and Storey (2000) recognized three distinct later episodes of granitoid emplacement in the Central Domain and Amundsen Province: one in the late Triassic Period, one in the mid-Jurassic Period and another in the late Jurassic- early Cretaceous period. Smaller terranes have been identified within the Central Domain in the Antarctic Peninsula, including a more mafic eastern terrane and more granitic western terrane (Ferraccioli et al., 1995). The outermost terrane, known as the Western

Domain in the Antarctic Peninsula, has no equivalent in Marie Byrd Land. It is an

accretionary terrane composed of upper Carboniferous to upper Cretaceous rocks.

Accretionary complexes of similar age are developed in southern South America and

New Zealand (Vaughan and Storey, 2000).

1.3 The Transantarctic Mountains

Stratigraphy of the Transantarctic Mountains

The Transantarctic Mountains are an excellent target for study of the subglacial geology of Antarctica because of their position on the border between East and West

Antarctica. During Gondwana time, the Transantarctic Mountains were the site of sedimentary basins which received sediments from both East and West Antarctica. These basins were described extensively by, and all information in this section comes from,

Collinson et al. (1994) unless otherwise noted. Devonian to Triassic strata (Fig. 5) in the

Transantarctic Mountains overlie Neoproterozoic to Cambrian metamorphosed sedimentary and volcanic strata which were intruded by granitoid batholiths related to the

Cambrian Ross Orogeny. Denudation following the Ross orogeny formed the Kukri

Erosion Surface, a relatively flat surface on which Devonian rocks were deposited (Isbell et al., 1999).

Devonian The Devonian rocks generally consist of thick sequences of quartzose sandstones, identified as Devonian by the presence of fossils. In north Victoria Land there are no

Devonian sedimentary rocks, the only rocks of similar age being the Admiralty Intrusive

Suite. In south Victoria Land, the Devonian sequence consists of sandstone, siltstone and mudstone dated by palynomorph and fish faunas. Trace fossil assemblages as well as

changing depositional styles suggest that the depositional environment transitioned from shallow marine to alluvial halfway through the section.

In the central Transantarctic Mountains, the Devonian sequence is an up-to-three hundred meter thick quartzose sandstone that rests unconformably on metasedimentary and volcanic rocks and in the Beardmore Glacier region is known as the Alexandra

Formation. The Alexandra Formation is devoid of diagnostic fossils; in the Ohio Range, however, the correlative Devonian Horlick Formation contains early Devonian shelly fossils. Paleocurrents and trace fossils suggest that the Alexandra Formation was deposited in a shallow coastal environment.

In the Pensacola Mountains, the Neptune Group and the Dover Sandstone comprise a 3,000 m thick sequence representing alluvial fan to shallow marine settings, with some late Devonian plant fossils identified from a correlated but isolated outcrop.

In the Ellsworth Mountains, located just outboard of the Transantarctic Mountains during Gondwana time, the upper portion of the 3,200 m thick Crashsite Quartzite is

Devonian in age. The thickness and lithology suggest a continental shelf setting along the

Paleo-Pacific margin of Gondwana.

Permian The Devonian quartzose sandstones are overlain by Permian glacial rocks deposited on a subglacial surface known as the Maya Erosion Surface. The Maya Erosion

Surface had great relief, inferred from the discontinuous nature of the glacial rocks in the area (Isbell et al., 1999; Isbell et al., 2008). Glaciation during the Permian was originally thought to have been the result of an ice sheet that covered large portions of Gondwana,

however recent research has shown glaciations during this time to have been less extensive than previously inferred (Isbell et al., 2008).

In Victoria Land, scattered glacial deposits known as the Darwin and Metschel tillites are attributed to glacio-marine deposition (Isbell et al., 2008). Along basin margins, subglacial deposits interfinger with glacio-marine deposits.

In the central Transantarctic Mountains the Pagoda and Scott Glacier formations comprise the Permian glacial sequence. Cyclical sequences are inferred to show glacial advance and retreat. The Buckeye Formation in the Ohio Range is considered a glacial and glacio-marine deposit, due to the presence of striated surfaces attributed to grounded ice and stratified diamictite and mudstone suggesting glacio-marine deposition during retreat.

The glacial sequence in the Pensacola Mountains is a 1,200 m thick sequence of diamictite, lenticular sandstone and interbedded mudstone known as the Gale Mudstone.

Due to the thickness and the presence of interbedded mudstone layers, the Gale is also considered a glacio-marine sequence. In the Ellsworth Mountains, the Whiteout

Conglomerate is a 1,000 m thick glacio-marine diamictite sequence with abundant dropstones.

The early Permian glacial sequence is overlain by a succession of post-glacial shales and mudstones. The post-glacial shales pinch out toward the north, being absent in

Victoria Land. In the central Transantarctic Mountains the sequence of post-glacial shales and fine sandstones is called the Mackellar Formation. High carbon to sulfur ratios and low trace-fossil diversity suggest fresh or slightly brackish water deposition; however, in the Ohio Range the Discovery Ridge Formation is interpreted as being marine. The

Mackellar Formation in the Beardmore Glacier region has a gradational contact with an overlying thick quartzose sandstone unit known as the Fairchild Formation. The Fairchild

Formation loses its identity toward the Ohio Range but is equivalent to the lower Mount

Glossopteris Formation. This lateral change in character is interpreted as the depositional system transitioning from a lacustrine environment into a deltaic system.

In the Ellsworth Mountains the lower Polarstar Formation consists of black shale, siltstone and fine-grained volcaniclastic sandstone. Rare ichnofossils suggest a marine environment of deposition.

Overlying the post-glacial sequences are coal-bearing strata containing a

Gangamopteris-Glossopteris flora. The widespread deposition of coal is attributed to warming and revegetation following the end of continental glaciation. In north Victoria

Land the Takrouna Formation coarsens gradually to the east, containing thick basal conglomerates with clasts derived from local granitic basement. Westward, the Takrouna

Formation become finer-grained and more carbonaceous and is interpreted to contain meandering stream facies. In south Victoria Land the Weller Coal Measures are composed of fining upward cycles of trough cross-bedded medium to fine-grained sandstones, mudstones and coal. The formation coarsens upward and toward the flanks of the basin. In south Victoria Land, Triassic sandstones directly overlie the Weller Coal

Measures. Although it is not observed, a similar stratigraphic relationship is inferred for the Takrouna Formation in northern Victoria Land

In the central Transantarctic Mountains, the lower Buckley Formation is a cyclical sequence of sheetlike quartzose sandstone, some carbonaceous shale, and minor coal.

This part of the formation is interpreted to represent braided streams and flood plain

deposits. Up-section, the Buckley Formation becomes a series of medium- to coarse- grained volcaniclastic sandstones, with fine-grained sandstone, mudstone, and common coal. In the Ohio Range, the Mount Glossopteris Formation sequences begin with lenticular rounded quartz-pebble conglomerates overlain by coal measures, followed by sequences of volcaniclastic sandstones very similar to the upper Buckley.

In the Ellsworth Mountains, the upper part of the Polarstar Formation is dominated by fining-upward cycles of medium to fine-grained volcaniclastic sandstones interpreted as a transition from prodeltaic to deltaic deposits.

Triassic In Victoria Land, the Feather Conglomerate occurs above a paleosol in some places, indicating a hiatus in the rock record. The Feather Conglomerate is a 175- to 250 m thick set of braided stream deposits composed of cross-bedded pebbly sandstone. This is overlain by the Triassic Lashly Formation, composed of fining upward sequences of sandstone and siltstone. In north Victoria Land, the Takrouna Formation is inferred to be overlain by the Section Peak Formation, a cross-bedded pebbly sandstone.

In the central Transantarctic Mountains, the Buckley Formation is overlain by

Triassic flood plain deposits known as the Fremouw and Falla formations. The base of the Fremouw Formation is quarztose, but the formation becomes increasingly volcaniclastic upward. The Falla Formation is comprised of fining upward cycles of coarse- to fine-grained sandstone overlain by sandstone, siltstone, carbonaceous shale and occasional thin coal seams. Overlying the Falla Formation is the Jurassic Hanson

Formation. The Hanson Formation consists of tuffs, tuffaceous sandstones, arkosic sandstones and minor lapillistones.

Previous Provenance Studies in the TAM Sedimentological studies of the Permian-Triassic strata in north Victoria Land have yielded a fairly simple provenance record (Collinson et al., 1986). During Permian time the depositional basin was formed in a complex graben feature situated almost completely within cratonic rocks. Because of this setting, the sediment transported into the basin was almost entirely of cratonic provenance. It was not until Triassic time that there was an influx of volcaniclastic sediment, relating to the volcanic arc in West

Antarctica.

The provenance of sedimentary rocks in south Victoria Land (Barrett and Kohn,

1975) is different from that in north Victoria Land. During Taylor Group deposition most of the sediment in southern Victoria Land was derived from the southwest, the area of the

East Antarctic Craton. However during the Permian and Triassic the dominant source area was to the northwest, the area of the present-day Ross Sea. Between the lower and upper parts of the Feather Conglomerate, there is a 90º paleocurrent shift, considered to be related to the Permo-Triassic paleocurrent reversal in the Beardmore Glacier area.

In their study and description of the Beacon rocks in the central Transantarctic

Mountains, Barrett et al. (1986) found evidence for two different sediment sources based on mineralogy and paleocurrent directions. The first is a granitic source presumed to have originated from the craton, dominant through much of the Permian succession. The second is a volcaniclastic source interpreted to be from a contemporaneous volcanic arc in West Antarctica. Accompanying this change in provenance is a ~180º shift in mean paleocurrent directions.

Previous Detrital Zircon Studies in the TAM

There have been few detrital zircon studies in the Transantarctic Mountains. The most relevant of these is the study conducted by Elliot and Fanning (2008) in the

Shackleton Glacier region of the central Transantarctic Mountains. The study sampled two sandstones from the Permian Buckley Formation and one from the Triassic Fremouw

Formation. In the investigation, evidence was found for multiple detrital zircon sources during Permian-Triassic time. These include sources of igneous Permian zircons derived from a late Permian arc, sources of Devonian age inferred to be derived from the Ford

Granodiorite, as well as Neoproterozoic and Cambrian grains attributed to the overlapping Ross and Pan-African orogenies. The influx of Permian igneous zircons into the upper Permian sandstones was interpreted as sedimentation from the active margin overwhelming the foreland basin which was previously dominated by a cratonic provenance.

Wysoczanski et al. (1997) analyzed rocks from the Devonian Junction sandstone in South Victoria Land, as well as some from the Takaka Terrane in New Zealand. Only

50 zircon grains from the Beacon were analyzed, however some major components were determined. The most abundant detrital zircon age in their Beacon sample is between

450-600 Ma, indicating a Ross/Pan-African source. The study also reported minor peaks at 1100 Ma and between 1500 and 1600 Ma.

The third of the detrital zircon studies in the Transantarctic Mountains was conducted by Wysoczanski et al. (2003). This study investigated rhyolitic and tuffaceous clasts from the Devonian Sperm Bluff Conglomerate of south Victoria Land. Due to chemical alteration, clasts could not be correlated with any nearby volcanic and plutonic provinces with any certainty. However, zircon geochronology yielded Ordovician ages

for the clasts, consistent with plutonic and hypabyssal rocks from the nearby McMurdo

Dry Valleys. This supports the hypothesis that the clasts were locally sourced as opposed to the more exotic sources proposed previously.

The fourth detrital zircon study in the Transantarctic Mountains was conducted in north Victoria Land by Goodge and Fanning (2010). Samples of the Permian Takrouna

Formation and the Triassic-Jurassic Section Peak Formation were dated. Results show samples dominated by Pan-African and Grenville age components, but with some significant differences. For example, the Ross age part of the Jurassic Section Peak sample is dominated by early Ross (560 Ma) material whereas the Permian Takrouna sample skews much younger (460 Ma). This suggests that the zircons in these samples were derived from erosion of separate Ross-age magmatic sources.

Chapter 2: The Central Transantarctic Mountains

The central Transantarctic Mountains are of particular use in the study of subglacial geology during Gondwana time because of the overall completeness of the Permian-

Triassic Beacon sequence and its position between East and West Antarctica. The general stratigraphy and exposure of the area has been described extensively by Barrett et al.

(1986), and in the Buckley Island region by Young and Ryburn (1968) (Fig. 6). Field areas specific to this study will be described in this work (Figs. 7, 8 and 9). Paleocurrent data will be given whenever applicable.

2.1 Stratigraphy in the Central Transantarctic Mountains

The Alexandra Formation The Alexandra Formation, of presumed Devonian age, is relatively thin in this area, as compared with the correlative strata in the Pensacola Mountains or south Victoria

Land. The Alexandra Formation ranges from 0-300 m thick in the region and unconformably overlies lightly metamorphosed igneous and sedimentary basement. The formation thins and disappears westward, where the Pagoda Formation lies directly upon basement rocks. This thinning is attributed to erosion by Permian ice cutting a grooved and polished surface on basement rocks. The lower contact of the Alexandra Formation with the Goldie Formation is mostly obscured by rubble, but is best observed at

Turnabout Ridge. The formation is composed almost entirely of white, medium- to coarse-grained well-sorted sandstones with some cross bedding. Paleocurrent

Figure 6. Simplified stratigraphic column for the central Transantarctic Mountains. Modified from Elliot and Fanning (2008).

Figure 8. Combined and simplified stratigraphic column for Mt Bowers and Mt Weeks. Pagoda Formation section taken from Mt Weeks, all other formations from Mt Bowers.

Figure 9. Simplified stratigraphic column for Clarkson Peak.

measurements (Barrett et al., 1986) were taken using cross bedding, channel structures and parting lineations. Although highly variable, the overall trend shows flow to the south and east.

The Pagoda Formation The Pagoda Formation is a glacial deposit ranging from 0-300 m in thickness.

These lateral variations have been attributed to infilling of glacial valleys. The Pagoda

Formation is described as a tillite which is an unbedded and very poorly sorted sandstone with dispersed pebbles and cobbles. Clast types are varied and include major basement rock types of the Transantarctic Mountains region. Grains are mostly quartzose and well rounded, presumably derived from the underlying Alexandra Formation. Water and ice movement directions were determined by Barrett et al. (1986) using channel orientations, cross-bedding, parting lineations and cross lamination. These measurements generally show flow to the east. Directions of ice flow in the Pagoda Formation follow this trend toward the east as determined by Lindsay (1970).

The Mackellar Formation The Mackellar Formation in the Beardmore region is a widely distributed series of carbonaceous shales and fine-grained sandstones, and is up to 140m thick at Buckley

Island. Local variation in formation thickness is considerable, with no discernible regional trend. The formation consists of alternating beds of dark grey shale and very fine grained white sandstone. Sandstone pods in scours are laterally discontinuous, most persisting for less than 10m. Some sequences are arranged in fining-upward cycles up to

18m thick. Paleocurrent directions in the Mackellar Formation were determined by

Barrett et al. (1986) using directional ripple marks, cross-bedding in sandstones and

parting lineations. Overall trends show consistent paleocurrents to the southeast. In this study paleocurrent directions were determined using ripple marks and cross-bedding only, but a similar flow direction was measured.

The Fairchild Formation The Fairchild Formation in this region is a widespread, white to light brown, cross-bedded, fine- to medium-grained sandstone up to 200m thick. The formation thins to the east from the Moore Mountains to the northern Queen Alexandra Range. Some pebbles are observed in the formation, and are increasingly more abundant toward the northwest. All clasts are well rounded, suggesting mostly fluvial transport. Paleocurrent measurements in the Fairchild Formation were determined using cross-bedding and parting lineations (Barrett et al., 1986). Paleocurrents are consistently oriented to the southeast throughout the Fairchild Formation.

The lower Buckley Formation In the central Transantarctic Mountains, the Buckley Formation is divided into two informal members based upon petrology. The lower Buckley Formation is a sequence of quartzose sandstones and shales with minor carbonaceous shales and coal beds. The transition from the Fairchild Formation to the lower Buckley Formation is generally marked by a laterally continuous quartz pebble conglomerate. Sandstone beds are up to 50m thick, separated by 10-15m of carbonaceous shale and sometimes a few centimeters of coal. The sandstones are white, quartzose, medium- to coarse-grained and contain well-rounded grains. The lower Buckley Formation contains the terrestrial plant fossil Glossopteris, establishing a Permian age for the Buckley Formation. Paleocurrent

directions in the lower Buckley Formation, from ripples and cross-beds, indicate flow to the south-southeast.

The upper Buckley Formation The upper Buckley Formation is distinguished from the lower Buckley Formation by the change from quartzose sandstone to volcaniclastic sandstone and an increased proportion of coal. The ratio of mudstone to sandstone becomes greater in the upper

Buckley Formation, and sandstone bluffs are less common. These sequences become cyclical, with a sandstone bluff giving way to progressively finer sandstones and carbonaceous shale, commonly topped by a coal bed. Sandstone bluffs are 10-15m tall and the sandstones tend to be highly pustular due to zeolite replacement in the rock. The fossil assemblages are the same as in the lower Buckley Formation, mostly Glossopteris and some flattened, coalified logs and stems. One other key difference between the upper

Buckley Formation and the lower Buckley Formation is the paleocurrent shift that accompanies the mineralogical change in the sandstones. Paleocurrents shift to the north in the upper Buckley Formation, as determined by measuring ripple marks and cross- bedding (Barrett et al., 1986).

Triassic strata The Fremouw Formation is a cyclical sequence of volcaniclastic sandstone and mudstone that disconformably overlies the Buckley Formation. The Fremouw Formation ranges from 80 to over 620 m thick, with the total thickness estimated at up to 800 m.

The lower part of the formation is known for its vertebrate fossils, whereas the upper part has plant fossils such as tree trunks and Dicroidium. Paleocurrents are similar to those in the upper Buckley Formation, with flow to the northwest. The Falla Formation (redefined

by Elliot, 1996) is an approximately 280 m thick sequence of sandstone and shale, with the upper contact defined by the appearance of tuffaceous beds. The formation thins away from the type section at Mount Falla and exposures are limited mainly to the central and southern Queen Alexandra Range. Paleocurrents continue a northwesterly trend, consistent with the Fremouw and upper Buckley formations.

2.2 Areas Specific to This Study

Bunker Cwm (Lat: 83.17°S Long: 164.00°E) The Alexandra Formation observed at Bunker Cwm is a white, fine-grained, quartzose sandstone interbedded with pebbly conglomeratic layers. The formation at this locality also contains some grey micaceous siltstone layers with sandy lenses. The lower contact of the Alexandra is below the ground surface and the upper contact is obscured by rubble. The observed thickness is approximately 20 m.

The Pagoda Formation was not observed at this locality. It is possible a thin sequence is obscured by rubble, or alternatively that it is absent. In either case, there must have been a paleotopographic high.

The Mackellar Formation at Bunker Cwm consists of alternating beds of shale, mudstone and fine sandstone with common ripple marks, both directional and interference. Sandstone beds are approximately 10-30 cm thick, whereas shale and mudstone layers are >10 m thick. Due to a large-scale post-depositional slump fold complex, total thickness is difficult to estimate due to the contorted nature of the formation at this locality, but it is estimated to be ~50 m. The upper contact with the

Fairchild Formation is abrupt, with a white sandstone bluff directly overlying shale beds.

The Fairchild Formation at this locality consists of 5-10 m thick white sandstone bluffs separated by 10-15 m of mudstone. Sandstones are white and quartzose with common black lithics and some biotite. Only the lower 30 m of the Fairchild Formation was examined at this locality; however the thickness is considerably greater than 30 m.

Clarkson Peak (Lat: 83°19’S Long: 164°34’E) The lower Buckley Formation at Clarkson Peak (Fig. 10a) is a white, cross- bedded, medium-grained sandstone with an abundance of concretionary bodies, most likely due to proximity to the dolerite sill that underlies it. There is a much smaller proportion of carbonaceous beds in the section at Clarkson Peak than might be expected for the lower Buckley Formation. The total thickness of the lower Buckley Formation at

Clarkson Peak is 300m.

The upper Buckley Formation at Clarkson Peak consists of mostly carbonaceous shales with some white sandstone bluffs. Sandstones are fine-grained, pustular and mostly volcaniclastic with some sparse visible feldspar. Total thickness of the upper

Buckley Formation at Clarkson Peak is approximately 100m.

Tillite Glacier ( Lat: 83°51’S Long: 166° 0’E) The Alexandra Formation at this locality consists of coarse-grained quartzose sandstone with some yellow alteration, as well as minor cross bedding, with cross beds measuring ~50 cm thick. The lower contact is obscured, and the upper contact with the

Pagoda Formation is abrupt. The Alexandra Formation thickness at this locality is approximately 10 m.

The Pagoda Formation at the Tillite Glacier locality is dominated by diamictite with boulder-sized clasts of conglomerate, granite, gneiss and paragneiss, and pebble-

sized clasts of limestone and shale. Some sandstone bodies are also observed. This is overlain by a thick slope-forming section of dark gray shale before grading into the overlying Mackellar Formation. The Mackellar Formation was not examined at this locality. The total thickness of the Pagoda Formation at Tillite Glacier is ~75 m.

The Fairchild Formation was examined at a separate locality across the glacier.

Only the upper 15m were examined and consist of medium- to fine-grained sandstones separated by mudstone intervals. Sandstones are ~3 m thick and mudstone layers are 7-8 m thick.

The lower Buckley Formation at Tillite Glacier is distinguished from the Fairchild

Formation by the first occurrence of a quartz pebble conglomerate found in lenticular channels. Only the lower 21 m were examined at this locality. The formation is mostly made of thin, grey, rippled sandstones with some carbonaceous particles, and interbedded with carbonaceous shales. These are topped by more quartz pebble conglomerates.

Mt. Weeks (Lat: 83°33’S Long: 160°54’E) At the Mt Weeks locality, the Pagoda Formation (Fig. 10b) consists of green diamictite interfingered with pebble conglomerates and sandy lenses. This is overlain by finely laminated sandstone with conglomeratic lenses and more diamictite. Pebble conglomerates are found in scours in the diamictite. The matrix is mostly quartz with common garnet and feldspar. Clasts are mostly granite, with some quartzite and nonresistant diamictite clasts. The lower contact is obscured by rubble at this locality and the upper contact with the Mackellar Formation is marked by a gradational change from tillite to grey shale.

At Mt Weeks, the Mackellar Formation is over 100m thick and consists of rippled shales and fine sandstones. Sandstones are quartz-rich with minor garnet and muscovite, and beds measure approximately 30-40 cm thick. The upper contact with the Fairchild

Formation is marked by an abrupt change in lithology from shale to highly resistant sandstone.

The Fairchild Formation consists of a series of medium- to fine-grained sandstones separated by mudstone intervals. Sandstones are ~5 m thick while mudstone intervals are 7-8 m thick. The total Fairchild Formation thickness is approximately 150 m.

At Mt Weeks, the lower Buckley Formation is separated from the Fairchild

Formation by a quartz pebble conglomerate bed. The lower Buckley Formation consists of white sandstone bluffs separated by carbonaceous shales. The sandstones, medium- grained and well rounded, are quartzose with minor muscovite, garnet and biotite. The lower Buckley Formation is reportedly over 100 m thick at this locality, however, in this study only the lower 40 m were observed.

Mt. Bowers (Lat: 85° 0’S Long: 164° 5’E) Young and Ryburn (1968) reported the presence of the Alexandra Formation in their Mt. Bowers section. However, upon further investigation, this unit is thought to be sufficiently distinct from the Alexandra to be recognized as a different sandstone unit.

The weathering pattern of the sandstone and the color of the rock indicate a diagenetic history and petrology distinct from the Alexandra Formation. This pre-Pagoda sandstone itself is white to pale green in color and medium- to coarse-grained. The sandstone consists mostly of quartz with some rare black lithic fragments, and carries common

concretions. The unit is unfossiliferous, and with no formation to correlate with there can be no age determination apart from being pre-Pagoda in age. The lower contact was not observed due to the presence of thick dolerite sills, whereas the upper contact with the

Mackellar Formation is abrupt, changing from sandstone to shale. The Pagoda Formation is absent at this locality.

At Mt Bowers, the Mackellar Formation is 135m thick and dominated by slope- forming shale with small beds of resistant sandstone 25-30cm thick. Some resistant beds have channel forms and are scoured slightly into the underlying shale. Lower shale sections contain iceberg keel marks and some pebble-sized dropstones. Some trace fossils and dewatering structures are also present in the shales. The upper contact of the

Mackellar Formation is marked by an abrupt change from slope-forming shale to thick sandstone bluffs.

The Fairchild Formation at Mt Bowers (Fig 11a) consists of bluffs of fine-grained sandstone separated by thin mudstone layers. Sandstone layers, up to 10 m thick, have channel forms and contain micaceous layers. Total thickness of the Fairchild Formation at this locality is approximately 100 m.

At Mt Bowers, the lower Buckley Formation (Fig 11b) is in direct contact with the Fairchild Formation, but lacks the quartz-pebble conglomerate marking the boundary between these two formations observed elsewhere. Instead, the boundary is assumed to be the first occurrence of non-resistant carbonaceous shale overlying a Fairchild

Formation sandstone bluff. The lower Buckley Formation at this locality includes large debris flow packets with rip-up breccia in large channels. Internally laminated and

rippled medium- to fine-grained quartzose sandstones form large bluffs. Moving upsection, the formation becomes more shale rich with sandstone bluffs becoming thinner but slightly more abundant. The upper sandstones take two forms: coarser grained, more micaceous bluff-formers with channeling and thinner, fine-grained slope formers with low-wavelength rippling. The contact with the upper Buckley Formation is gradational, with the boundary being marked as the first appearance of volcaniclastic sandstone. The total thickness of the lower Buckley Formation at Mt Bowers is 300m.

The upper Buckley Formation at Mt Bowers consists of three brown-pink sandstone bluffs separated by thick carbonaceous shale sequences and topped by coal seams. Shales contain common Glossopteris and some carbonized wood. Sandstones are pustular and pink in color, suggesting replacement of volcaniclastic grains by zeolite.

Some sandstones also contain carbonized wood and iron-rich concretions. Low angle cross-bedding is common in sandstones. Rippling is seen in shales, but not well defined enough for paleocurrent measurement.

Mt. Achernar (Lat: 84°12’S Long: 160°56’E) At Mt Achernar, only the transition between the lower and upper Buckley

Formation was examined. The lower Buckley Formation at this locality consists mostly of slope-forming greenish sandstone and fine-grained sandstone sets containing carbonaceous debris together with 10-15m white resistant sandstone cliffs. Sandstones are medium- to coarse-grained, well-rounded and quartz-rich.

The upper Buckley Formation at Mt Achernar consists of white sandstone bluffs separated by green mudstones and parallel laminated fine-grained sandstones. Sandstones

are white and pustular, indicating the replacement of volcanic grains by zeolite.

Sandstone bluffs are cross-bedded, with slight rippling on fine-grained layers.

Chapter 3: Methods 3.1 Field Methods

Samples of the sedimentary rocks of the Victoria Group were collected during the

2010/2011 Antarctic field season. Wherever possible, samples were selected on the basis of similar grain size in order to enhance recovery of usable zircon and to ensure no bias on the basis of grain size. Rocks collected were described and stratigraphic sections were measured for each site in order to give proper context to the samples. In some cases paleocurrents of the associated sandstone were measured and recorded.

3.2 Laboratory methods

Upon returning from the field, sandstone samples were thin sectioned and described. Samples were then selected based on locality, grain size, and mineralogy to be sent for zircon analysis. Samples selected were sent to the Research School of Earth

Sciences, Australian National University, Canberra, Australia, for analysis on the Super

High Resolution Ion Microprobe (SHRIMP) under the direction of C. Mark Fanning.

There, zircons were extracted using standard methods: crushing, washing, heavy liquid

(specific gravity: 2.96 and 3.3) separation, and paramagnetic separation. These zircons were then mounted in epoxy together with Temora reference zircons, sectioned approximately in half and then polished. From these mounts, reflected (RL) and transmitted (TL) light micrographs were produced as well as cathodoluminescence (CL)

images. CL images were used to examine the internal zonation of the grains in order to be sure that the ~20µm SHRIMP spot was wholly within one age component, ideally the youngest. RL and TL images were used to determine the presence of cracks and irregularities in the grains that were undetectable in the CL images. The U-Th-Pb analyses of the zircon grains were made using SHRIMP. For each sample, zircons were analyzed sequentially and randomly until a total of at least 70 grains had been reached.

Each analysis consisted of four scans through the mass range with the Temora reference zircon analyzed for every five unknown zircon grains. SHRIMP analytical methods followed Williams (1998 and references therein). The data have been reduced using the

SQUID Excel Macro of Ludwig (2001). U/Pb ratios have been normalized relative to a value of 0.0668 for the Temora reference zircon, equivalent to an age of 417 Ma (see

Black et al., 2003). Uncertainties given for individual analyses (ratios and ages) are at the one sigma level and are listed in the table footnotes.

Tera and Wasserburg (1972) concordia plots, probability density plots with stacked histograms and weighted mean 206Pb/238U age calculations were carried out using

ISOPLOT/EX (Ludwig, 2003). The “Mixture Modeling” algorithm of Sambridge and

Compston (1994), via ISOPLOT/EX, was used to un-mix statistical age populations or groupings; from these groups weighted mean 206Pb/238U ages were calculated and the uncertainties are reported as 95% confidence limits. Common lead was corrected for in two ways: for grains >800 Ma, the 204Pb/206Pb ratio was measured in order to make the correction and for grains <800 Ma or low in U or Pb, the207 Pb correction method was used.

Chapter 4: Petrography

Thin sections can be split into two broad groups based on petrology. The first is quartzose sandstone containing plagioclase and K-feldspar. These contain well-rounded to subrounded quartz, feldspar, biotite and/or muscovite, and trace sphene, garnet, and zircon. They contain little to no lithic fragments and have a phyllosilicate cement. There is common replacement of feldspar grains by zeolite, possibly laumontite. The second is sandstone containing common igneous lithic fragments. These sandstones contain a smaller proportion of quartz, plagioclase and K-feldspar. Possible igneous lithic fragments include: porphyritic volcanic fragments with pilotaxitic texture arising from alignment of feldspar laths; tuffaceous fragments showing wavy foliations; porphyritic volcanic fragments with microphenocrysts of feldspar in a fine groundmass of quartz and feldspar; aphanitic volcanic fragments, consisting of very fine grained crystalline matrix; and glass shards. These sandstones contain traces of biotite, sphene and zircon, and lack muscovite. They are commonly cemented with phyllosilicate. There is also common zeolite replacement of feldspar. For more detailed descriptions of individual thin sections, refer to Appendix B.

Chapter 5: Results

Results will be presented in stratigraphic order according to which flank of the basin the sample came from, starting on the West Antarctic flank. See Fig. 12 for examples and descriptions of zircon textures and Figs. 8 and 9 for stratigraphic columns.

All measured data and Tera-Wasserburg plots are in Appendix A. All measured zircons are between 50 and 100 µm. Some grains are euhedral, showing tetragonal crystal shape.

Most are subhedral to rounded due to abrasion and fracturing. Zonation in grains occurs in two types: oscillatory zoning, with concentric or nearly concentric zones and sector zoning, with the grain divided into 4 ‘sectors’. Some grains lack zonation, indicating a metamorphic origin. Some grains contain one or more distinct cores, which are relict zircon grains surrounded by zircon crystallized during subsequent magmatic or metamorphic events. Zircon analyses were conducted on the outermost measurable zone in order to capture the latest episode of crystallization in the zircon’s history. Some grains contain rims that are too small to fit the SHRIMP spot, making them unmeasurable.

Grains were rejected if the SHRIMP spot would intersect a fracture, due to the possibility of lead loss in fractures. This process favors intact grains with fewer fractures and larger grains with zones that are easier to measure.

11-4-3 (lower Buckley Formation, Clarkson Peak)

Zircons in this sample are equant to elongate and generally well rounded, or are fragments of rounded grains. Most measured grains show well developed zonation, but

large numbers show unmeasurable rims. Some grains are amalgamated into a single crystal. The most prominent zircon age-probability peak is late Neoproterozoic with a main peak at 565 Ma and a weak shoulder at 540 Ma (Figs. 13 and 14). Two grains comprise a very weak and small probability peak at ~450 Ma. There are some small but relatively significant older zircon age-probability peaks at approximately 925 Ma and approximately 2665 Ma, as well as scattered grains of other ages.

11-4-10 (upper Buckley Formation, Clarkson Peak)

Zircons in this sample are equant to elongate and generally euhedral or fragments of such grains. Most measured grains show clear, sharp zonation associated with igneous grains, although a few grains show no internal zonation consistent with metamorphic grains. The predominant zircon age peak in this sample is late Permian in age with the principal peak at 260 Ma (Fig. 15, 16). There is a minor low probability three-grain peak of late Devonian age (~358 Ma). There is also a broad late Neoproterozoic to Cambrian zircon age distribution with a zircon age-probability peak at approximately 550 Ma.

There are scattered Proterozoic and Archean grains, with a minor grouping of zircons centered at approximately 1100 Ma.

11-5-2 (Pre-Pagoda Sandstone, Mt Bowers)

Zircons in this sample are generally very stubby in appearance and equant to elongate, or fragments of such grains. A few grains show rounded euhedral crystal forms, but most are well rounded or broken. The majority of measured grains have metamorphic affinities, with amorphous or poorly defined zonation. Some scattered grains also show

565 Ma

2665 Ma 925 Ma

Figure 13. Detrital zircon age-probability histogram and representative CL image for sample 11-4-3, lower Buckley Formation, Clarkson Peak. Grain 61.1 shows igneous zonation, and 58.1 has a core.

565 Ma

450 Ma

Figure 14. Detrital zircon age-probability histogram focused on Neoproterozoic- Ordovician time for sample 11-4-3, lower Buckley Formation, Clarkson Peak.

260 Ma

540 Ma

260 Ma

Figure 16. Detrital zircon age-probability histogram focused on the Permian Period for sample 11-4-10, upper Buckley Formation, Clarkson Peak.

sector zoning, indicating an igneous origin. The dominant zircon age-probability peak in this sample is 577 Ma in age (Fig. 17). There is a minor grouping of zircons at approximately 1050 Ma, associated with a low zircon age-probability peak. There is also a broad scattering of grains from 1900 Ma to 2200 Ma, but no definitive zircon age- probability peak. A minor zircon age-probability peak occurs at approximately 2705 Ma, as well as scattered older Archean grains.

11-9-2 (Pagoda Formation, Mt Weeks)

Measured zircons in this sample are mostly equant, with few elongate grains.

Most are very well rounded with some scattered nearly euhedral grains. The majority of the grains show metamorphic affinities; however there are a few grains that show distinct zonation, indicating an igneous origin. Some grains show sector zoning, indicating igneous origin. The dominant zircon age-probability peak in this sample is 580 Ma with a very soft shoulder at 570 Ma and a few grains younger than 550 Ma (Fig. 18). There are multiple minor zircon age-probability peaks in the Proterozoic, at 1080 Ma, 1150 Ma, and 1430 Ma. There is also a smattering of single grains from approximately 1800 Ma to

2250 Ma, and scattered Archean grains.

11-5-8 (Fairchild Formation, Mt Bowers)

Zircons in this sample are mostly equant with a few broken elongate grains. Most measured grains are very well rounded with some scattered nearly euhedral grains. Most grains show distinct igneous zonation; some have amorphous zonation. Some grains show sector zoning indicating igneous origin. The major Neoproterozoic to Cambrian

577 Ma 577 Ma wysoczawysocza nsky

1050 Ma

1575 Ma 2705 Ma

580 Ma 577 Ma wysoczawysocza nsky

580Ma

wysoczan sky

1150 Ma

wysoczan 1430 Ma sky wysoczans ky

grouping of grains contains three zircon age-probability peaks: one at 580 Ma, one at 550

Ma and a relatively minor one at 528 Ma (Figs. 19 and 20). There is also a scattering of

Proterozoic and Archean grains. These include clusters at 990-1250 Ma, 1300-1500 Ma and 1800-2250 Ma.

11-5-15 (lower Buckley Formation, Mt Bowers)

Zircon grains are mostly equant with some scattered fragments of elongate grains.

Grain shapes are split between rounded and euhedral. Most grains have amorphous metamorphic-type zonation, but most euhedral grains have sharp igneous zonation. A few grains have sector zoning, indicating igneous origin. The dominant Neoproterozoic-

Cambrian grain grouping contains three zircon age-probability peaks, one at 575 Ma, one at 525 Ma with a soft shoulder at 540 Ma and a relatively minor one at 460 Ma (Fig. 21 and 22). There are a few scattered older grains and a minor zircon age-probability peak at around 2750 Ma.

11-5-22 (upper Buckley Formation, Mt Bowers)

Zircon grains in this sample are mostly elongate or fragments of such grains. Measured grains are mostly euhedral, some showing rounding on corners. Most grains show sharp igneous zonation, with some showing more poorly defined metamorphic zonation. The dominant zircon age-probability peak in this sample is at 260 Ma (Figs. 23 and 24). There is also a small cluster of grains at 500-600 Ma with a minor zircon age-probability peak.

The sample also contains some scattered older grains.

550 Ma 577 Ma wysoczawysocza nsky

1850 Ma 990 Ma wysoczan 2705 Ma wysocza sky nsky wysoczans ky

Figure 19. Detrital zircon age-probability histogram and representative CL image for sample 11-5-8, Fairchild Formation, Mt Bowers. Grains 54.1 and 57.1 suggest metamorphic origin.

550 Ma 580 Ma wysocza nsky wysocza nsky 528 Ma 577 Ma wysoczawysocza nsky

Figure 20. Detrital zircon age-probability histogram focused on Neoproterozoic- Ordovician time for sample 11-5-8, Fairchild Formation, Mt Bowers.

460 Ma

wysocz 525 Ma ansky 577 Ma wysoczawysocza nsky

2750 Ma

wysoczans ky

525 Ma

wysocza nsky 575 Ma 577 Ma wysoczawysocza 460 Ma nsky

wysocza nsky

Figure 22. Detrital zircon age-probability histogram focused on Neoproterozoic- Ordovician time for sample 11-5-15, lower Buckley Formation, Mt Bowers.

260 Ma 577 Ma wysoczawysocza nsky

Figure 24. Detrital zircon age-probability histogram focused on the Permian Period for sample 11-5-22, upper Buckley Formation, Mt Bowers.

Chapter 5: Discussion

Interpretations of the data presented will be discussed in chronological order of major detrital zircon age groupings. This is an attempt to look at overall trends in zircon age distributions as opposed to trends within a formation or specific flank of the basin.

5.1: >2500 Ma (Archean)

In most samples there are scattered Archean grains, however sandstones in the pre-Pagoda sandstone, the Fairchild Formation and both of the lower Buckley Formation samples all have minor age-probability peaks >2500 Ma. These 3-5 grain probability peaks each occur at ~2750 Ma. The major known outcrop source for Archean-age material is in Enderby Land (Fig. 25). More specifically, the grains can be linked to

2700-2800 Ma rocks outcropping along the Mawson Escarpment and the Prince Charles

Mountains. Some isolated outcrops of similar age exist elsewhere, but are less likely to have been major sources of Archean grains. The possibility of recycling also cannot be discounted when considering the presence of these grains in the Transantarctic

Mountains. Zircons may have been eroded from their original source rock, then deposited. Later, these grains may have been re-eroded from a sand, lithified sandstone or a meta-sandstone (schist or paragneiss) and deposited directly into the Permian basin or re-deposited one or more times before finally being eroded and deposited in the Permian sedimentary basin. Enderby Land is over 2000 km from the study area in the

Figure 25. Map of Antarctica with Archean Provinces circled. Ages from Tingey (1991).

Transantarctic Mountains, making the likelihood of direct transport from the source region very low. It is much more probable that these grains were recycled from a pre-

Permian sedimentary source.

Minor probability peaks of similar age are seen in the Fremouw Formation sample reported by Elliot and Fanning (2008). Studies in the Transantarctic Mountains by

Goodge and Fanning (2010) and Wysoczanski et al. (2003) did not record any significant input of Archean grains, however Goodge and Fanning (2010) also sampled sediment cores off the coast of King George V Land and found a major Archean input. That study attributed the input to minor Archean outcrops near Cape Denison. However, as a source for the sediment in this study, it suffers similar distance issues as the Enderby Land source with the added problem of being a single outcrop without any known greater extent.

5.2: 1300-2500 Ma ( Early Mesoproterozoic and Paleoproterozoic)

Various Meso- and Paleoproterozoic age-probability peaks occur in the analyses of the pre-Buckley samples. Outcrops of Mawson Craton rocks including the 1700 Ma rocks in the Miller Range and 1300-1700 Ma rocks in Terre Adélie/King George V Land are the most likely source for the grains present in these samples (Fig. 26). The actual distributions of ages are fairly spread out, suggesting multiple Proterozoic-age sources contributed to sediment being deposited in the basin during the Permian Period. Once again, the possibility of sedimentary recycling cannot be discounted. Although there is a local source for Proterozoic sediment in the Miller Range, its limited exposure makes it

Figure 26. Map of Antarctica with Meso- and Paleoproterozoic provinces circled. Ages from Fitzsimons (2003)

unlikely to have been the sole source of material. Aeromagnetic data reported by Goodge and Finn (2010) suggest that the subglacial extent of the Mawson rocks inboard is less than 50 Km, although it is unknown how extensive the aeromagnetic province is parallel to the Transantarctic Mountains. Assuming the belt of Mawson rock runs parallel to the study area, the narrow belt described by Goodge and Finn (2010) still seems an unlikely source for the Proterozoic zircons due to the likelihood of sediment covering the belt. As the basin filled with sediment, the sediment began to obscure sources from the middle of the basin, moving outward over time. Therefore a narrow belt closer to the middle of the basin, including the study area, is likely to become obscured during early stages of sedimentation. Further, if there were an exposed source of purely Mawson Craton zircon so close to the study area, there would have been a much greater input into the system than is seen in these samples.

It is worth noting that probability peaks of this age only show up in one previous provenance study in the Transantarctic Mountains. The Devonian Junction Sandstone in the Darwin Glacier area of South Victoria Land (Wysoczanski et al. 1997), contains a minor peak of 1400-1700 Ma age that may be related to that observed in this study. This finding points to a possible recycling of grains from the Devonian rocks underlying the

Victoria Group. The lack of this Mawson Craton component in other studies could be attributed to different sampling locations along the Transantarctic Mountains, temporal separation between different formations sampled or a source that was not active during the deposition of those samples. For the Elliot and Fanning (2008) samples the most likely explanation for the absence of this zircon age group is temporal rather than spatial separation, as their study area in the Shackleton Glacier area was close to the Beardmore

Glacier area of this study. They sampled rocks from the Buckley Formation, which were deposited after the Meso- and Paleoproterozoic source had been eroded away or buried.

Further, the sediment sources for their Buckley samples were in West Antarctica. For the other two studies, the geographic separation of the study areas most likely accounts for the differences in probability profiles

5.3: 1000-1300 Ma (late Mesoproterozoic)

The minor 1000-1300 Ma probability peaks in most of the samples reflect a so- called “Grenville age” source. Fitzsimons (2000) described three possible “Grenville age” sources along the edges of East Antarctica: the Wilkes Province with an age range of 1130-1330 Ma and exposed near the Darling Fault Zone; the Maud Province with an age range of 1030-1090 Ma and exposed in Queen Maud Land and the Shackleton

Range; and the Rayner Province with an age range of 900-990 Ma, exposed in Enderby

Land (Fig. 27). Based on the age ranges represented in our samples, the Wilkes Province is the most likely source for the “Grenville age” zircon grains. However, the limited number of grains make this determination uncertain at best.

As with all of the Proterozoic and Archean zircon grains, the possibility of sedimentary recycling must be considered, especially with the lack of a proximal “Grenville age” outcrop. The source began to die out in Fairchild time, and was nearly completely gone in

Buckley time, suggesting a source being eroded away, covered by subsequent sedimentation or being excluded by erosional processes, such as shifting river systems bypassing strata containing zircon grains of ‘Grenville’ age. Once again, the possible source for recycled grains is the Devonian sedimentary rocks underlying the Permian

Figure 27. Map of Antarctica with “Grenville age” provinces circled. Names of provinces and ages taken from Fitzsimons (2000).

sequence, a possibility bolstered by the findings of Wysoczanski et al. (1997). Their study of the Devonian Junction Sandstone in the Darwin Glacier region yielded minor zircon age-probability peaks in the 1000-1200 Ma range, matching relatively well with the zircon age-probability peaks in the samples described in this study. Assuming the

Devonian rocks which underlie the Permian sequence were the source of “Grenville age” zircon grains, each possibility must be considered equally likely. Due to the nature of the basin, the Devonian sediments probably lapped on to the craton, thinning toward the East

Antarctic flank of the basin. This makes it very possible that sediments or rocks on the edges of the basin could have been completely eroded away, but are still present near the center of the extant basin where they were much thicker. As the basin filled with sediment, the Devonian rocks could have been covered, thus cutting off the supply of

“Grenville age” zircons to the later formations.

5.4: 480-650 Ma (Cambro-Ordovician to Neoproterozoic)

The major component of all the pre-upper Buckley samples is zircon age- probability peaks with an age range of 480-650 Ma, pointing to a Ross/Pan-African age source. Most of the probability peaks in pre-Buckley samples are 550-650 Ma, a Pan-

African distribution; however the Buckley Formation has a major Ross source at 480-

560 Ma. Possible sources of Pan-African age sediment are scattered along coastal regions of East Antarctica with the major known source in Queen Maud Land, where the rocks are part of the East African Orogen (Fig. 28). However, there are no known outcrops of Pan-African age anywhere near the field area, suggesting three possibilities: an obscured subglacial Pan-African source; very long distance transport from the edges

of East Antarctica, or an earlier stage of Ross magmatism than is recognized currently.

The first two options are essentially end-member possibilities. Sediment could have been transported from a major Mississippi- or Amazon-like river system directly from the coastal regions of East Antarctica in one end member; in the other there is an unexposed

Pan-African source directly outside of the field area, presumably from the extension of aPan-African belt into the interior of East Antarctica. However, the process of recycling allows for movement of the Pan-African source closer to or farther from the

Transantarctic Mountains. There is no evidence for a single major river system that would have carried zircon from the coastal regions to the Transantarctic Mountains; however this does not reduce the possibility of multi-cycle transport through multiple sedimentary systems. However with such a strong, undiluted Pan-African signal the possibility of multiple stages of transport seems less likely. The best candidate for a Pan-

African age belt extending into the interior of East Antarctica is the East African Orogen exposed in Queen Maud Land. However, there are no indications that this belt extends past the Shackleton Range. Alternatively, a possible explanation for the 550-650 zircon age-probability peaks is that the Ross magmatic event began earlier than recognized so far, and that the rocks of the Ross Orogen extend inboard under the present-day East

Antarctic Ice Sheet.

The more conventional Ross Orogen probability peaks between 480 and 560 Ma are seen primarily in the lower Buckley Formation, although there is a trend toward younger Ross ages upsection at Mt Bowers. The Ross source is presumably local; however this creates its own problems. The Gondwana sequence is deposited directly on top of the rocks of the Ross Orogen, meaning that the currently exposed Ross Orogen

could not be the source of sediment for the lower Buckley sandstones. Therefore it is suggested that the Ross Orogen must extend inboard subglacially. The very minor

Ross/Pan-African probability peak in the upper Buckley Formation on the West Antarctic flank of the basin also suggests that there is a Ross/Pan-African source in West

Antarctica, possibly extending the Ross Orogen outboard as well.

These patterns are consistent throughout the detrital zircon studies in the

Transantarctic Mountains, with a major Ross/Pan-African source dominant until the late

Permian. Differences between analyzed samples can be accounted for by spatial and temporal differences in rocks collected.

5.5: 460 Ma (Ordovician)

There is a very minor input of Ordovician zircon in the lower Buckley Formation samples with an approximate 460 Ma age. There are very few known Ordovician source regions in the area, the most likely province being the Vanda Dikes in the Dry Valleys. However, the Vanda Dikes have a fairly well constrained youngest age of about 480 Ma

(Encarnación and Grunow, 1996), making them unsuitable as a source for the Ordovician material without invoking a later stage of magmatism. This leaves two possibilities, either a late stage of Ross magmatism or an unexposed source of Ordovician material. Because the age range is so close to the younger limits of the Ross Orogen, a late stage of Ross magmatism seems the most likely way to explain this minor Ordovician input.

Sources of this age are seen much more prominently in Goodge and Fanning

(2010). One of the major sources in the Takrouna Formation sample that they analyzed is approximately 470 Ma. This could be a link between the conventional youngest Ross

magmatism and the middle Ordovician input seen in the analyses presented in this study.

In Elliot and Fanning (2008), there is a major source of 480 Ma material, considered part of the youngest part of the Ross Orogen. This creates a trend from south to north in the

Transantarctic Mountains: the youngest Ross age zircons become progressively younger northward (Fig. 29). This suggests that perhaps the youngest Ross plutonic rocks are most prevalent in the northern part of the Transantarctic Mountains.

5.6: 260 Ma (Late Permian) The major probability peak in the upper Buckley Formation is at 260 Ma, or late Permian time. The transition from the lower to upper Buckley Formation comes with a change from quartzose sandstone to volcaniclastic sandstone. There is also a major paleocurrent reversal which began in upper Buckley time, indicating a tectonic shift affecting the basin. This tectonic shift is most likely related to the inception of the Permo-Triassic arc along the active margin in West Antarctica (Fig. 30). The paleocurrent reversal, along with the volcaniclastic input of late Permian sediment, suggests that the arc was the primary source of sediment for the upper Buckley Formation. This input is seen on both flanks of the basin, suggesting that inputs from the late Permian arc overwhelmed the basin. As the basin filled with sediment, arc-derived material traveled across the basin, lapping onto the East Antarctic flank.

This major Permian input is also described in Elliot and Fanning (2008). The upper Buckley Formation samples in their study have much the same 260 Ma peak, with a soft shoulder at 245 Ma. Goodge and Fanning (2010) do not report this arc material until the Jurassic Section Peak Formation. This suggests that the arc material did not reach all parts of the Transantarctic Mountains at once, instead showing that it became

Figure 30. Map of Antarctica with Permian rocks in the Amundsen Province labeled. Dates from Pankhurst et al. (1998), Mukasa and Dalziel, (2000), Pankhurst et al. (1993) and Millar et al. (2002).

dominant earlier in the southern and central Transantarctic Mountains and progressed into northern Victoria Land at a later time. This is consistent with the conclusions of

Collinson et al. (1994) based upon sandstone petrology.

Chapter 6: Conclusions

The main finding of this study is that detrital zircons in the Permian sandstones of the Beardmore Glacier region indicate multiple source regions supplied sediment into the

Permian basin (Figures 31 and 32). Specific conclusions can be summed up in this way:

• Minor sources of Proterozoic and Archean (>2500 Ma) age have been documented. These were most likely recycled from a sedimentary source on the East

Antarctic flank of the sedimentary basin, possibly from the Devonian sedimentary sequence which underlies the Permo-Triassic rocks.

• The minor “Grenville age” (1000-1300 Ma) sediment source dies out in Buckley time. The “Grenville age” zircons are also likely to have been recycled.

• The dominant Pan-African (550-650 Ma) age material suggests either a local Pan-

African source or very long distance transport. Alternatively, the material could have been derived from an unexposed Neoproterozoic source, possibly related to an early stage of the Ross Orogen.

• The Ross-age (480-560 Ma) material in the pre-upper Buckley sedimentary rocks suggests that the rocks of the Ross Orogen extend inboard of the active margin under the present-day East Antarctic Ice Sheet.

• The volcaniclastic sediment in the upper Buckley Formation is related to the contemporaneous late Permian (~260 Ma) arc in West Antarctica. A Ross-age source in

the upper Buckley Formation suggests the Ross Orogen extends outboard of the active margin into West Antarctica as well.

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Appendix A: Raw Data and Concordia Plots

Table 1: 11-4-3 (lower Buckley Formation)

Table xyz. Summary of SHRIMP U-Pb zircon results for sample 11-4-3, Lower Buckley, Clarkson Peak.

Total Ratios Radiogenic Ratios Age (Ma) preferred Age (Ma) Total Ratios Radiogenic Ratios 206 204 238 207 206 207 207 206 207 238 207 206 207 207 Grain. U Th Th/U Pb* Pb/ f206 U/ Pb/ Pb/ Pb/ Pb/ Pb/ Pb/ % Grain. % U/ Pb/ Pb/ Pb/ Pb/ spot (ppm) (ppm) (ppm) 206Pb % 206Pb ± 206Pb ± 238U ± 235U ± 206Pb ± r 238U ± 206Pb ± Disc spot ± Disc 206Pb ± 206Pb ± 238U ± 235U ± 206Pb ± r

1.1 36 82 2.28 3.0 0.001896 1.95 10.377 0.188 0.0753 0.0022 0.0945 0.0018 582 10 25.1 452 5 13.740 0.146 0.0574 0.0004 0.0727 0.0008 2.1 209 254 1.22 74.4 0.000118 0.17 2.411 0.028 0.2040 0.0013 0.4141 0.0049 11.563 0.157 0.2025 0.0014 0.869 2234 22 2847 11 22 51.1 469 8 13.091 0.228 0.0665 0.0020 0.0754 0.0013 3.1 1612 41 0.03 128.9 0.000028 0.09 10.747 0.111 0.0599 0.0003 0.0930 0.0010 573 6 36.1 513 9 11.957 0.218 0.0653 0.0028 0.0828 0.0016 4.1 180 541 3.00 14.6 0.000702 0.36 10.614 0.136 0.0623 0.0010 0.0939 0.0012 578 7 55.1 525 8 11.779 0.174 0.0581 0.0013 0.0849 0.0013 5.1 76 30 0.40 6.1 0.000410 0.72 10.751 0.166 0.0650 0.0015 0.0923 0.0015 569 9 30.1 528 8 11.628 0.177 0.0634 0.0014 0.0854 0.0013 6.1 174 73 0.42 23.1 0.000198 0.34 6.466 0.081 0.0733 0.0014 0.1541 0.0019 1.498 0.042 0.0705 0.0018 0.444 924 11 943 52 2 54.1 532 11 11.563 0.235 0.0630 0.0023 0.0860 0.0018 7.1 183 104 0.57 13.9 0.000364 0.27 11.273 0.144 0.0607 0.0010 0.0885 0.0012 546 7 39.1 533 8 11.577 0.168 0.0599 0.0013 0.0862 0.0013 8.1 53 50 0.94 4.3 0.001057 1.05 10.664 0.193 0.0677 0.0019 0.0928 0.0017 572 10 38.1 534 9 11.530 0.201 0.0618 0.0017 0.0863 0.0015 9.1 144 25 0.17 16.5 0.000243 <0.01 7.459 0.098 0.0660 0.0053 0.1341 0.0020 811 11 46.1 538 6 11.464 0.129 0.0603 0.0006 0.0870 0.0010 10.1 179 82 0.46 14.7 0.000239 0.20 10.492 0.136 0.0612 0.0010 0.0951 0.0013 586 7 45.1 544 6 11.336 0.137 0.0596 0.0008 0.0881 0.0011 11.1 73 47 0.64 20.0 0.000256 0.40 3.148 0.046 0.1688 0.0015 0.3164 0.0047 7.223 0.133 0.1656 0.0018 0.800 1772 23 2513 19 29 61.1 546 7 11.294 0.147 0.0604 0.0010 0.0883 0.0012 12.1 57 23 0.41 4.6 - 0.47 10.547 0.185 0.0632 0.0017 0.0944 0.0017 581 10 7.1 546 7 11.273 0.144 0.0607 0.0010 0.0885 0.0012 13.1 89 85 0.95 31.4 0.000492 0.73 2.446 0.034 0.1870 0.0013 0.4058 0.0056 10.121 0.178 0.1809 0.0019 0.790 2196 26 2661 18 17 26.1 552 8 11.155 0.160 0.0601 0.0013 0.0895 0.0013 14.1 176 88 0.50 81.7 0.000012 0.02 1.853 0.023 0.1847 0.0008 0.5397 0.0066 13.734 0.177 0.1846 0.0008 0.944 2782 27 2694 7 -3 48.1 557 7 11.075 0.134 0.0592 0.0008 0.0902 0.0011 15.1 219 102 0.47 17.4 0.000078 0.06 10.801 0.134 0.0596 0.0010 0.0925 0.0012 571 7 22.1 558 6 10.995 0.115 0.0629 0.0004 0.0905 0.0010 16.1 122 58 0.47 36.8 0.000063 0.10 2.860 0.037 0.1186 0.0024 0.3493 0.0045 5.672 0.141 0.1178 0.0025 0.520 1931 22 1923 38 0 31.1 558 8 11.002 0.151 0.0623 0.0011 0.0905 0.0013 17.1 241 62 0.26 29.0 0.000126 0.22 7.132 0.085 0.0739 0.0011 0.1399 0.0017 1.391 0.032 0.0721 0.0014 0.527 844 10 989 39 15 47.1 563 6 10.946 0.119 0.0604 0.0005 0.0912 0.0010 18.1 1033 354 0.34 85.1 0.000035 <0.01 10.432 0.110 0.0594 0.0004 0.0959 0.0010 590 6 59.1 564 9 10.883 0.183 0.0625 0.0016 0.0915 0.0016 19.1 236 161 0.68 19.4 0.000156 0.07 10.431 0.129 0.0602 0.0008 0.0958 0.0012 590 7 62.1 565 6 10.912 0.121 0.0599 0.0006 0.0915 0.0010 20.1 535 34 0.06 43.3 0.000062 0.01 10.605 0.118 0.0595 0.0006 0.0943 0.0011 581 6 41.1 565 9 10.907 0.170 0.0595 0.0014 0.0916 0.0015 21.1 36 21 0.59 6.6 - <0.01 4.717 0.088 0.1232 0.0029 0.2120 0.0040 3.601 0.108 0.1232 0.0029 0.623 1239 21 2003 42 38 56.1 565 6 10.895 0.122 0.0599 0.0006 0.0917 0.0010 22.1 1211 114 0.09 94.6 0.000119 0.51 10.995 0.115 0.0629 0.0004 0.0905 0.0010 558 6 5.1 569 9 10.751 0.166 0.0650 0.0015 0.0923 0.0015 23.1 604 34 0.06 50.4 0.000061 <0.01 10.289 0.113 0.0597 0.0007 0.0972 0.0011 598 6 15.1 571 7 10.801 0.134 0.0596 0.0010 0.0925 0.0012 24.1 57 26 0.46 6.6 0.000368 0.64 7.541 0.129 0.0739 0.0016 0.1318 0.0023 798 13 69.1 571 7 10.775 0.137 0.0614 0.0009 0.0926 0.0012 25.1 1063 1122 1.05 66.5 0.000069 0.17 13.740 0.146 0.0574 0.0004 0.0727 0.0008 452 5 8.1 572 10 10.664 0.193 0.0677 0.0019 0.0928 0.0017 26.1 116 364 3.14 8.9 0.000411 0.19 11.155 0.160 0.0601 0.0013 0.0895 0.0013 552 8 37.1 573 7 10.737 0.138 0.0612 0.0011 0.0929 0.0012 27.1 475 83 0.18 177.3 - <0.01 2.303 0.025 0.1817 0.0005 0.4342 0.0047 10.876 0.122 0.1817 0.0005 0.966 2325 21 2668 5 13 3.1 573 6 10.747 0.111 0.0599 0.0003 0.0930 0.0010 28.1 113 156 1.38 9.5 0.000334 0.28 10.230 0.146 0.0622 0.0012 0.0975 0.0014 600 8 50.1 574 6 10.735 0.114 0.0590 0.0004 0.0932 0.0010 29.1 640 258 0.40 55.6 - 0.12 9.899 0.108 0.0614 0.0005 0.1009 0.0011 620 7 4.1 578 7 10.614 0.136 0.0623 0.0010 0.0939 0.0012 30.1 91 78 0.86 6.7 - 0.67 11.628 0.177 0.0634 0.0014 0.0854 0.0013 528 8 63.1 579 12 10.506 0.230 0.0695 0.0025 0.0940 0.0021 31.1 134 135 1.01 10.5 0.000058 0.43 11.002 0.151 0.0623 0.0011 0.0905 0.0013 558 8 20.1 581 6 10.605 0.118 0.0595 0.0006 0.0943 0.0011 32.1 338 383 1.13 145.1 0.000010 0.01 2.002 0.022 0.1869 0.0006 0.4994 0.0056 12.859 0.151 0.1867 0.0006 0.959 2611 24 2714 5 4 12.1 581 10 10.547 0.185 0.0632 0.0017 0.0944 0.0017 33.1 174 28 0.16 38.1 0.000098 0.16 3.933 0.049 0.1697 0.0011 0.2538 0.0031 5.896 0.084 0.1685 0.0012 0.869 1458 16 2542 12 43 1.1 582 10 10.377 0.188 0.0753 0.0022 0.0945 0.0018 34.1 5 1 0.13 0.6 0.002371 <0.01 6.965 0.374 0.0303 0.0019 0.1503 0.0084 903 47 44.1 586 7 10.507 0.124 0.0603 0.0008 0.0951 0.0011 35.1 64 25 0.39 8.7 0.000337 0.58 6.258 0.101 0.0776 0.0014 0.1589 0.0026 1.595 0.064 0.0728 0.0027 0.407 951 14 1008 75 6 10.1 586 7 10.492 0.136 0.0612 0.0010 0.0951 0.0013 36.1 56 35 0.61 4.1 0.000278 0.95 11.957 0.218 0.0653 0.0028 0.0828 0.0016 513 9 58.1 590 6 10.438 0.116 0.0598 0.0006 0.0958 0.0011 37.1 186 105 0.57 14.9 0.000232 0.25 10.737 0.138 0.0612 0.0011 0.0929 0.0012 573 7 19.1 590 7 10.431 0.129 0.0602 0.0008 0.0958 0.0012 38.1 65 92 1.43 4.8 0.000751 0.46 11.530 0.201 0.0618 0.0017 0.0863 0.0015 534 9 18.1 590 6 10.432 0.110 0.0594 0.0004 0.0959 0.0010 39.1 117 53 0.46 8.7 0.000218 0.22 11.577 0.168 0.0599 0.0013 0.0862 0.0013 533 8 23.1 598 6 10.289 0.113 0.0597 0.0007 0.0972 0.0011 40.1 115 30 0.26 15.6 - <0.01 6.316 0.085 0.0693 0.0010 0.1584 0.0021 1.519 0.030 0.0696 0.0010 0.690 948 12 916 29 -4 28.1 600 8 10.230 0.146 0.0622 0.0012 0.0975 0.0014 41.1 84 31 0.37 6.6 0.000686 0.06 10.907 0.170 0.0595 0.0014 0.0916 0.0015 565 9 57.1 602 30 9.528 0.472 0.1147 0.0119 0.0979 0.0052 42.1 215 45 0.21 40.1 0.000168 0.28 4.596 0.055 0.1545 0.0011 0.2170 0.0026 4.556 0.066 0.1523 0.0012 0.827 1266 14 2372 14 47 29.1 620 7 9.899 0.108 0.0614 0.0005 0.1009 0.0011 43.1 181 107 0.59 71.9 0.000037 0.05 2.162 0.026 0.1822 0.0008 0.4623 0.0056 11.582 0.151 0.1817 0.0008 0.934 2450 25 2669 8 8 49.1 630 8 9.542 0.117 0.0778 0.0009 0.1026 0.0013 44.1 292 119 0.41 23.9 0.000124 0.09 10.507 0.124 0.0603 0.0008 0.0951 0.0011 586 7 60.1 651 8 9.409 0.113 0.0619 0.0010 0.1062 0.0013 45.1 278 84 0.30 21.1 0.000086 0.14 11.336 0.137 0.0596 0.0008 0.0881 0.0011 544 6 70.1 665 8 9.173 0.113 0.0642 0.0008 0.1087 0.0014 46.1 480 289 0.60 36.0 0.000097 0.26 11.464 0.129 0.0603 0.0006 0.0870 0.0010 538 6 24.1 798 13 7.541 0.129 0.0739 0.0016 0.1318 0.0023 47.1 771 69 0.09 60.5 0.000022 0.18 10.946 0.119 0.0604 0.0005 0.0912 0.0010 563 6 9.1 811 11 7.459 0.098 0.0660 0.0053 0.1341 0.0020 48.1 315 88 0.28 24.5 0.000113 0.06 11.075 0.134 0.0592 0.0008 0.0902 0.0011 557 7 17.1 844 10 15 7.132 0.085 0.0739 0.0011 0.1399 0.0017 1.391 0.032 0.0721 0.0014 0.527 49.1 256 21 0.08 23.0 0.000056 2.08 9.542 0.117 0.0778 0.0009 0.1026 0.0013 630 8 34.1 903 47 6.965 0.374 0.0303 0.0019 0.1503 0.0084 50.1 994 132 0.13 79.6 0.000001 <0.01 10.735 0.114 0.0590 0.0004 0.0932 0.0010 574 6 6.1 924 11 2 6.466 0.081 0.0733 0.0014 0.1541 0.0019 1.498 0.042 0.0705 0.0018 0.444 51.1 98 311 3.17 6.4 0.000655 1.24 13.091 0.228 0.0665 0.0020 0.0754 0.0013 469 8 40.1 948 12 -4 6.316 0.085 0.0693 0.0010 0.1584 0.0021 1.519 0.030 0.0696 0.0010 0.690 52.1 820 53 0.07 85.2 - <0.01 8.271 0.090 0.0717 0.0007 0.1209 0.0013 1.195 0.018 0.0717 0.0007 0.730 736 8 977 21 25 35.1 951 14 6 6.258 0.101 0.0776 0.0014 0.1589 0.0026 1.595 0.064 0.0728 0.0027 0.407 53.1 215 81 0.38 59.0 0.000281 0.44 3.136 0.045 0.1562 0.0017 0.3175 0.0046 6.681 0.144 0.1526 0.0024 0.674 1777 23 2376 27 25 52.1 977 21 25 8.271 0.090 0.0717 0.0007 0.1209 0.0013 1.195 0.018 0.0717 0.0007 0.730 54.1 46 22 0.48 3.4 0.001018 0.60 11.563 0.235 0.0630 0.0023 0.0860 0.0018 532 11 66.1 1060 12 2 5.698 0.062 0.0747 0.0005 0.1755 0.0019 1.808 0.022 0.0747 0.0005 0.873 55.1 124 66 0.53 9.0 0.000135 0.02 11.779 0.174 0.0581 0.0013 0.0849 0.0013 525 8 65.1 1117 26 12 6.064 0.081 0.0769 0.0010 0.1649 0.0022 1.747 0.032 0.0768 0.0010 0.720 56.1 452 14 0.03 35.7 0.000082 0.12 10.895 0.122 0.0599 0.0006 0.0917 0.0010 565 6 68.1 1814 10 5 3.256 0.035 0.1124 0.0005 0.3065 0.0033 4.687 0.057 0.1109 0.0006 0.898 57.1 6 3 0.61 0.5 - 6.69 9.528 0.472 0.1147 0.0119 0.0979 0.0052 602 30 64.1 1822 27 7 3.335 0.045 0.1129 0.0010 0.2994 0.0040 4.596 0.093 0.1113 0.0017 0.668 58.1 491 172 0.35 40.4 0.000122 0.03 10.438 0.116 0.0598 0.0006 0.0958 0.0011 590 6 16.1 1931 22 0 2.860 0.037 0.1186 0.0024 0.3493 0.0045 5.672 0.141 0.1178 0.0025 0.520 59.1 66 47 0.71 5.2 0.000165 0.44 10.883 0.183 0.0625 0.0016 0.0915 0.0016 564 9 21.1 2003 42 38 4.717 0.088 0.1232 0.0029 0.2120 0.0040 3.601 0.108 0.1232 0.0029 0.623 60.1 238 181 0.76 21.7 0.000237 0.07 9.409 0.113 0.0619 0.0010 0.1062 0.0013 651 8 42.1 2372 14 47 4.596 0.055 0.1545 0.0011 0.2170 0.0026 4.556 0.066 0.1523 0.0012 0.827 61.1 214 86 0.40 16.3 0.000398 0.24 11.294 0.147 0.0604 0.0010 0.0883 0.0012 546 7 53.1 2376 27 25 3.136 0.045 0.1562 0.0017 0.3175 0.0046 6.681 0.144 0.1526 0.0024 0.674 62.1 528 211 0.40 41.6 0.000058 0.12 10.912 0.121 0.0599 0.0006 0.0915 0.0010 565 6 11.1 2513 19 29 3.148 0.046 0.1688 0.0015 0.3164 0.0047 7.223 0.133 0.1656 0.0018 0.800 63.1 31 18 0.56 2.6 - 1.24 10.506 0.230 0.0695 0.0025 0.0940 0.0021 579 12 33.1 2542 12 43 3.933 0.049 0.1697 0.0011 0.2538 0.0031 5.896 0.084 0.1685 0.0012 0.869 64.1 105 202 1.93 27.1 0.000112 0.18 3.335 0.045 0.1129 0.0010 0.2994 0.0040 4.596 0.093 0.1113 0.0017 0.668 1688 20 1822 27 7 13.1 2661 18 17 2.446 0.034 0.1870 0.0013 0.4058 0.0056 10.121 0.178 0.1809 0.0019 0.790 65.1 125 52 0.41 17.8 0.000003 0.01 6.064 0.081 0.0769 0.0010 0.1649 0.0022 1.747 0.032 0.0768 0.0010 0.720 984 12 1117 26 12 27.1 2668 5 13 2.303 0.025 0.1817 0.0005 0.4342 0.0047 10.876 0.122 0.1817 0.0005 0.966 66.1 535 337 0.63 80.7 - <0.01 5.698 0.062 0.0747 0.0005 0.1755 0.0019 1.808 0.022 0.0747 0.0005 0.873 1042 10 1060 12 2 43.1 2669 8 8 2.162 0.026 0.1822 0.0008 0.4623 0.0056 11.582 0.151 0.1817 0.0008 0.934 67.1 71 35 0.49 31.6 0.000085 0.12 1.932 0.028 0.1888 0.0020 0.5171 0.0076 13.384 0.249 0.1877 0.0022 0.786 2687 32 2722 19 1 14.1 2694 7 -3 1.853 0.023 0.1847 0.0008 0.5397 0.0066 13.734 0.177 0.1846 0.0008 0.944 68.1 463 153 0.33 122.1 0.000113 0.18 3.256 0.035 0.1124 0.0005 0.3065 0.0033 4.687 0.057 0.1109 0.0006 0.898 1724 16 1814 10 5 32.1 2714 5 4 2.002 0.022 0.1869 0.0006 0.4994 0.0056 12.859 0.151 0.1867 0.0006 0.959 69.1 194 65 0.34 15.4 - 0.28 10.775 0.137 0.0614 0.0009 0.0926 0.0012 571 7 67.1 2722 19 1 1.932 0.028 0.1888 0.0020 0.5171 0.0076 13.384 0.249 0.1877 0.0022 0.786 70.1 222 35 0.16 20.8 0.000084 0.30 9.173 0.113 0.0642 0.0008 0.1087 0.0014 665 8 2.1 2847 11 22 2.411 0.028 0.2040 0.0013 0.4141 0.0049 11.563 0.157 0.2025 0.0014 0.869

Notes : 1. Uncertainties given at the one s level. Notes : 2. Error in Temora reference zircon calibration w as 0.84% for the analytical session. ( not included in above errors but required w hen comparing 206Pb/238U data from different mounts).

206 3. f 206 % denotes the percentage of Pb that is common Pb. 4. For areas older than ~800 Ma correction for common Pb made using the measured 204Pb/206Pb ratio. 5. For areas younger than ~800 Ma correction for common Pb made using the measured 238U/206Pb and 207Pb/206Pb ratios 83

Figure 33. Tera-Wasserburg plot for sample 11-4-3, lower Buckley Formation, Clarkson Peak.

Table 2: 11-4-10 (upper Buckley Formation)

Table xyz. Summary of SHRIMP U-Pb zircon results for sample 11-4-10, Upper Buckley, Clarkson Peak.

Total Ratios Radiogenic Ratios Age (Ma) preferred Age (Ma) Total Ratios Radiogenic Ratios 206 204 238 207 206 207 207 206 207 238 207 207 206 207 Grain. U Th Th/U Pb* Pb/ f206 U/ Pb/ Pb/ Pb/ Pb/ Pb/ Pb/ % Grain. % U/ Pb/ Pb/ Pb/ Pb/ spot (ppm) (ppm) (ppm) 206Pb % 206Pb ± 206Pb ± 238U ± 235U ± 206Pb ± r 238U ± 206Pb ± Disc spot ± Disc 206Pb ± 206Pb ± 235U ± 238U ± r 206Pb ±

1.1 169 1 0.01 12.9 0.000015 0.02 11.310 0.145 0.0586 0.0009 0.0884 0.0012 546 7 16.1 244 4 25.757 0.406 0.0560 0.0017 0.0386 0.0006 2.1 936 576 0.62 67.3 0.000140 0.27 11.947 0.127 0.0598 0.0004 0.0835 0.0009 517 5 20.1 247 3 25.296 0.286 0.0609 0.0023 0.0390 0.0005 3.1 262 161 0.61 9.4 0.000382 0.29 24.005 0.308 0.0538 0.0011 0.0415 0.0005 262 3 21.1 251 4 25.014 0.389 0.0580 0.0016 0.0396 0.0006 4.1 84 43 0.51 10.1 0.000263 0.46 7.137 0.104 0.0715 0.0012 0.1395 0.0020 1.303 0.039 0.0677 0.0018 0.487 842 12 861 55 2 30.1 251 3 25.138 0.276 0.0534 0.0006 0.0397 0.0004 5.1 436 276 0.63 15.1 0.000203 0.48 24.824 0.293 0.0551 0.0009 0.0401 0.0005 253 3 14.1 251 3 25.128 0.276 0.0520 0.0006 0.0398 0.0004 6.1 375 174 0.46 13.1 0.000186 0.26 24.516 0.300 0.0534 0.0009 0.0407 0.0005 257 3 11.1 252 3 25.055 0.294 0.0536 0.0008 0.0398 0.0005 7.1 533 263 0.49 78.5 0.000042 0.07 5.841 0.063 0.0742 0.0004 0.1711 0.0019 1.736 0.023 0.0736 0.0005 0.825 1018 10 1030 15 1 5.1 253 3 24.824 0.293 0.0551 0.0009 0.0401 0.0005 8.1 466 148 0.32 23.5 0.000248 0.46 17.009 0.193 0.0576 0.0007 0.0585 0.0007 367 4 9.1 256 3 24.646 0.275 0.0526 0.0006 0.0405 0.0005 9.1 715 238 0.33 24.9 0.000129 0.15 24.646 0.275 0.0526 0.0006 0.0405 0.0005 256 3 6.1 257 3 24.516 0.300 0.0534 0.0009 0.0407 0.0005 10.1 580 366 0.63 20.7 0.000248 0.52 24.057 0.273 0.0556 0.0007 0.0414 0.0005 261 3 44.1 257 3 24.524 0.287 0.0523 0.0008 0.0407 0.0005 11.1 456 307 0.67 15.6 0.000092 0.30 25.055 0.294 0.0536 0.0008 0.0398 0.0005 252 3 32.1 259 3 24.413 0.279 0.0519 0.0007 0.0409 0.0005 12.1 248 144 0.58 12.4 0.000531 0.65 17.227 0.218 0.0590 0.0013 0.0577 0.0007 361 5 63.1 259 3 24.364 0.275 0.0522 0.0007 0.0410 0.0005 13.1 619 260 0.42 22.0 0.000122 0.02 24.208 0.273 0.0516 0.0007 0.0413 0.0005 261 3 41.1 260 3 24.242 0.264 0.0524 0.0006 0.0412 0.0005 14.1 878 369 0.42 30.0 0.000046 0.10 25.128 0.276 0.0520 0.0006 0.0398 0.0004 251 3 42.1 260 3 24.179 0.279 0.0540 0.0008 0.0412 0.0005 15.1 384 46 0.12 101.3 0.000018 0.03 3.252 0.037 0.1138 0.0009 0.3074 0.0035 4.813 0.067 0.1136 0.0009 0.811 1728 17 1857 15 7 13.1 261 3 24.208 0.273 0.0516 0.0007 0.0413 0.0005 16.1 107 147 1.37 3.6 0.000754 0.61 25.757 0.406 0.0560 0.0017 0.0386 0.0006 244 4 46.1 261 3 24.148 0.274 0.0534 0.0007 0.0413 0.0005 17.1 316 143 0.45 11.6 0.000061 0.29 23.292 0.287 0.0540 0.0009 0.0428 0.0005 270 3 64.1 261 3 24.073 0.272 0.0558 0.0007 0.0413 0.0005 18.1 66 40 0.60 2.5 0.002343 3.70 22.501 0.424 0.0813 0.0029 0.0428 0.0008 270 5 10.1 261 3 24.057 0.273 0.0556 0.0007 0.0414 0.0005 20.1 760 281 0.37 25.8 0.000900 1.22 25.296 0.286 0.0609 0.0023 0.0390 0.0005 247 3 24.1 262 5 24.014 0.421 0.0547 0.0020 0.0415 0.0007 21.1 127 108 0.85 4.4 0.001027 0.85 25.014 0.389 0.0580 0.0016 0.0396 0.0006 251 4 3.1 262 3 24.005 0.308 0.0538 0.0011 0.0415 0.0005 22.1 319 2 0.01 28.8 0.000126 1.08 9.508 0.109 0.0698 0.0007 0.1040 0.0012 638 7 39.1 263 3 24.025 0.273 0.0520 0.0007 0.0416 0.0005 23.1 179 102 0.57 26.1 0.000055 0.09 5.891 0.072 0.0732 0.0007 0.1696 0.0021 1.694 0.029 0.0724 0.0008 0.724 1010 11 998 24 -1 27.1 263 3 23.849 0.288 0.0578 0.0009 0.0416 0.0005 24.1 74 55 0.75 2.6 0.000956 0.41 24.014 0.421 0.0547 0.0020 0.0415 0.0007 262 5 40.1 263 4 24.013 0.388 0.0516 0.0016 0.0416 0.0007 25.1 101 73 0.73 35.1 0.000058 0.09 2.462 0.033 0.1366 0.0009 0.4058 0.0054 7.598 0.115 0.1358 0.0010 0.878 2196 25 2174 13 -1 65.1 263 3 23.946 0.273 0.0533 0.0007 0.0417 0.0005 26.1 679 280 0.41 24.3 0.000047 <0.01 23.995 0.268 0.0513 0.0007 0.0417 0.0005 263 3 26.1 263 3 23.995 0.268 0.0513 0.0007 0.0417 0.0005 27.1 345 175 0.51 12.4 0.000623 0.79 23.849 0.288 0.0578 0.0009 0.0416 0.0005 263 3 34.1 265 3 23.855 0.306 0.0504 0.0010 0.0420 0.0005 28.1 128 73 0.57 15.8 - <0.01 6.962 0.091 0.0680 0.0009 0.1436 0.0019 1.347 0.025 0.0680 0.0009 0.705 865 11 868 27 0 36.1 267 3 23.611 0.291 0.0513 0.0009 0.0424 0.0005 29.1 167 45 0.27 13.2 0.000091 0.16 10.807 0.138 0.0604 0.0009 0.0924 0.0012 570 7 62.1 268 4 23.587 0.329 0.0518 0.0013 0.0424 0.0006 30.1 833 579 0.69 28.5 0.000071 0.27 25.138 0.276 0.0534 0.0006 0.0397 0.0004 251 3 18.1 270 5 22.501 0.424 0.0813 0.0029 0.0428 0.0008 31.1 157 33 0.21 12.3 0.000122 0.03 10.992 0.142 0.0591 0.0009 0.0909 0.0012 561 7 17.1 270 3 23.292 0.287 0.0540 0.0009 0.0428 0.0005 32.1 513 185 0.36 18.1 0.000043 0.07 24.413 0.279 0.0519 0.0007 0.0409 0.0005 259 3 61.1 271 3 23.245 0.260 0.0530 0.0008 0.0429 0.0005 33.1 194 46 0.24 30.8 0.000050 0.08 5.389 0.065 0.0757 0.0007 0.1854 0.0022 1.916 0.031 0.0749 0.0008 0.746 1096 12 1067 22 -3 45.1 290 4 21.779 0.296 0.0515 0.0009 0.0460 0.0006 34.1 244 102 0.42 8.8 0.000020 <0.01 23.855 0.306 0.0504 0.0010 0.0420 0.0005 265 3 50.1 356 4 17.588 0.212 0.0541 0.0008 0.0568 0.0007 35.1 161 90 0.56 23.6 0.000090 0.15 5.852 0.072 0.0773 0.0014 0.1706 0.0021 1.789 0.040 0.0761 0.0014 0.544 1016 12 1097 38 7 68.1 360 5 17.373 0.239 0.0545 0.0012 0.0575 0.0008 36.1 299 144 0.48 10.9 0.000183 <0.01 23.611 0.291 0.0513 0.0009 0.0424 0.0005 267 3 12.1 361 5 17.227 0.218 0.0590 0.0013 0.0577 0.0007 37.1 929 479 0.52 67.1 0.000123 0.10 11.907 0.126 0.0585 0.0004 0.0839 0.0009 519 5 8.1 367 4 17.009 0.193 0.0576 0.0007 0.0585 0.0007 38.1 78 233 3.01 6.3 0.000156 <0.01 10.574 0.161 0.0587 0.0013 0.0947 0.0015 583 9 70.1 475 6 13.063 0.156 0.0575 0.0007 0.0765 0.0009 39.1 560 250 0.45 20.0 0.000000 0.07 24.025 0.273 0.0520 0.0007 0.0416 0.0005 263 3 2.1 517 5 11.947 0.127 0.0598 0.0004 0.0835 0.0009 40.1 118 69 0.58 4.2 0.000522 0.01 24.013 0.388 0.0516 0.0016 0.0416 0.0007 263 4 37.1 519 5 11.907 0.126 0.0585 0.0004 0.0839 0.0009 41.1 802 392 0.49 28.4 0.000079 0.12 24.242 0.264 0.0524 0.0006 0.0412 0.0005 260 3 69.1 522 7 11.831 0.172 0.0590 0.0012 0.0844 0.0013 42.1 480 252 0.53 17.1 0.000020 0.33 24.179 0.279 0.0540 0.0008 0.0412 0.0005 260 3 47.1 528 6 11.690 0.127 0.0593 0.0005 0.0854 0.0009 43.1 288 118 0.41 25.0 0.000239 0.28 9.912 0.116 0.0627 0.0010 0.1006 0.0012 618 7 48.1 529 6 11.686 0.132 0.0583 0.0006 0.0855 0.0010 44.1 388 180 0.46 13.6 0.000304 0.11 24.524 0.287 0.0523 0.0008 0.0407 0.0005 257 3 59.1 539 7 11.542 0.141 0.0524 0.0023 0.0873 0.0011 45.1 406 157 0.39 16.0 0.000218 <0.01 21.779 0.296 0.0515 0.0009 0.0460 0.0006 290 4 1.1 546 7 11.310 0.145 0.0586 0.0009 0.0884 0.0012 46.1 522 424 0.81 18.6 0.000078 0.25 24.148 0.274 0.0534 0.0007 0.0413 0.0005 261 3 49.1 547 6 11.260 0.128 0.0614 0.0006 0.0885 0.0010 47.1 601 283 0.47 44.2 0.000012 0.16 11.690 0.127 0.0593 0.0005 0.0854 0.0009 528 6 66.1 549 8 11.215 0.158 0.0612 0.0012 0.0889 0.0013 48.1 439 170 0.39 32.3 0.000068 0.03 11.686 0.132 0.0583 0.0006 0.0855 0.0010 529 6 60.1 552 6 11.172 0.132 0.0599 0.0007 0.0894 0.0011 49.1 432 104 0.24 32.9 0.000270 0.36 11.260 0.128 0.0614 0.0006 0.0885 0.0010 547 6 58.1 553 6 11.149 0.131 0.0597 0.0007 0.0896 0.0011 50.1 296 122 0.41 14.5 0.000170 0.05 17.588 0.212 0.0541 0.0008 0.0568 0.0007 356 4 55.1 555 6 11.107 0.125 0.0591 0.0006 0.0900 0.0010 51.1 640 109 0.17 59.6 0.000021 0.19 9.231 0.099 0.0632 0.0004 0.1081 0.0012 662 7 31.1 561 7 10.992 0.142 0.0591 0.0009 0.0909 0.0012 52.1 310 165 0.53 43.6 0.000117 0.20 6.108 0.069 0.0783 0.0019 0.1634 0.0018 1.728 0.048 0.0767 0.0019 0.407 976 10 1113 50 12 67.1 565 6 10.927 0.127 0.0586 0.0007 0.0916 0.0011 53.1 345 155 0.45 28.8 0.000046 <0.01 10.294 0.116 0.0578 0.0006 0.0974 0.0011 599 7 56.1 566 16 11.107 0.125 0.0434 0.0220 0.0918 0.0027 54.1 262 188 0.72 46.1 0.000022 0.04 4.887 0.056 0.0793 0.0009 0.2046 0.0023 2.227 0.038 0.0790 0.0010 0.676 1200 13 1171 25 -2 29.1 570 7 10.807 0.138 0.0604 0.0009 0.0924 0.0012 55.1 440 66 0.15 34.0 - 0.05 11.107 0.125 0.0591 0.0006 0.0900 0.0010 555 6 38.1 583 9 10.574 0.161 0.0587 0.0013 0.0947 0.0015 56.1 58 40 0.68 4.5 0.000380 <0.01 11.107 0.125 0.0434 0.0220 0.0918 0.0027 566 16 53.1 599 7 10.294 0.116 0.0578 0.0006 0.0974 0.0011 57.1 115 71 0.62 16.7 0.000177 0.30 5.901 0.080 0.0767 0.0009 0.1690 0.0023 1.729 0.040 0.0742 0.0014 0.586 1006 13 1048 38 4 43.1 618 7 9.912 0.116 0.0627 0.0010 0.1006 0.0012 58.1 292 142 0.48 22.5 0.000084 0.13 11.149 0.131 0.0597 0.0007 0.0896 0.0011 553 6 22.1 638 7 9.508 0.109 0.0698 0.0007 0.1040 0.0012 59.1 221 124 0.56 16.5 0.000130 <0.01 11.542 0.141 0.0524 0.0023 0.0873 0.0011 539 7 51.1 662 7 9.231 0.099 0.0632 0.0004 0.1081 0.0012 60.1 288 94 0.33 22.2 0.000073 0.16 11.172 0.132 0.0599 0.0007 0.0894 0.0011 552 6 4.1 842 12 2 7.137 0.104 0.0715 0.0012 1.303 0.039 0.1395 0.0020 0.487 0.0677 0.0018 61.1 693 311 0.45 25.6 0.000255 0.17 23.245 0.260 0.0530 0.0008 0.0429 0.0005 271 3 28.1 865 11 0 6.962 0.091 0.0680 0.0009 1.347 0.025 0.1436 0.0019 0.705 0.0680 0.0009 62.1 177 93 0.53 6.4 - 0.02 23.587 0.329 0.0518 0.0013 0.0424 0.0006 268 4 23.1 1010 11 -1 5.891 0.072 0.0732 0.0007 1.694 0.029 0.1696 0.0021 0.724 0.0724 0.0008 63.1 624 334 0.53 22.0 0.000173 0.10 24.364 0.275 0.0522 0.0007 0.0410 0.0005 259 3 7.1 1030 15 1 5.841 0.063 0.0742 0.0004 1.736 0.023 0.1711 0.0019 0.825 0.0736 0.0005 64.1 614 296 0.48 21.9 0.000276 0.54 24.073 0.272 0.0558 0.0007 0.0413 0.0005 261 3 57.1 1048 38 4 5.901 0.080 0.0767 0.0009 1.729 0.040 0.1690 0.0023 0.586 0.0742 0.0014 65.1 606 255 0.42 21.7 0.000088 0.22 23.946 0.273 0.0533 0.0007 0.0417 0.0005 263 3 33.1 1096 12 -3 5.389 0.065 0.0757 0.0007 1.916 0.031 0.1854 0.0022 0.746 0.0749 0.0008 66.1 112 40 0.35 8.6 0.000263 0.34 11.215 0.158 0.0612 0.0012 0.0889 0.0013 549 8 35.1 1097 38 7 5.852 0.072 0.0773 0.0014 1.789 0.040 0.1706 0.0021 0.544 0.0761 0.0014 67.1 314 196 0.62 24.7 - <0.01 10.927 0.127 0.0586 0.0007 0.0916 0.0011 565 6 52.1 1113 50 12 6.108 0.069 0.0783 0.0019 1.728 0.048 0.1634 0.0018 0.407 0.0767 0.0019 68.1 166 55 0.33 8.2 0.000066 0.09 17.373 0.239 0.0545 0.0012 0.0575 0.0008 360 5 54.1 1200 13 -2 4.887 0.056 0.0793 0.0009 2.227 0.038 0.2046 0.0023 0.676 0.0790 0.0010 69.1 109 40 0.37 7.9 0.000212 0.15 11.831 0.172 0.0590 0.0012 0.0844 0.0013 522 7 15.1 1857 15 7 3.252 0.037 0.1138 0.0009 4.813 0.067 0.3074 0.0035 0.811 0.1136 0.0009 70.1 289 238 0.82 19.0 0.000040 0.11 13.063 0.156 0.0575 0.0007 0.0765 0.0009 475 6 25.1 2174 13 -1 2.462 0.033 0.1366 0.0009 7.598 0.115 0.4058 0.0054 0.878 0.1358 0.0010

Notes : 1. Uncertainties given at the one s level. Notes : 2. Error in Temora reference zircon calibration w as 0.59%, 0.92% & 0.54% for the analytical sessions. ( not included in above errors but required w hen comparing 206Pb/238U data from different mounts).

Figure 34. Tera-Wasserburg plot for sample 11-4-10, upper Buckley Formation, Clarkson Peak.

Table 3: 11-5-2 (pre-Pagoda sandstone)

Table xyz. Summary of SHRIMP U-Pb zircon results for sample 11-5-2, Pre-Pagoda sandstone, Mt. Bowers.

1.1 149 49 0.33 22.4 0.000121 0.20 5.727 0.074 0.0769 0.0009 0.1742 0.0023 1.806 0.052 0.0752 0.0019 0.456 1035 12 1073 51 4 31.1 504 5 12.291 0.136 0.0583 0.0006 0.0813 0.0009 2.1 304 222 0.73 26.1 - <0.01 10.009 0.117 0.0598 0.0007 0.1000 0.0012 614 7 4.1 524 9 11.742 0.208 0.0617 0.0022 0.0848 0.0015 3.1 75 48 0.64 9.4 0.000711 1.23 6.875 0.103 0.0723 0.0013 0.1440 0.0025 1.276 0.088 0.0642 0.0037 0.713 867 14 750 122 -16 24.1 525 6 10.760 0.132 0.1286 0.0013 0.0849 0.0011 4.1 54 33 0.60 4.0 0.000374 0.48 11.742 0.208 0.0617 0.0022 0.0848 0.0015 524 9 60.1 545 7 11.315 0.150 0.0605 0.0010 0.0882 0.0012 5.1 302 169 0.56 25.3 0.000163 0.23 10.244 0.119 0.0617 0.0007 0.0974 0.0012 599 7 38.1 546 6 11.202 0.124 0.0666 0.0006 0.0884 0.0010 6.1 90 110 1.22 13.7 0.000277 0.47 5.623 0.081 0.0783 0.0012 0.1770 0.0026 1.815 0.058 0.0744 0.0021 0.456 1051 14 1051 58 0 32.1 548 6 11.147 0.125 0.0680 0.0007 0.0887 0.0010 7.1 347 273 0.79 27.7 0.000160 0.37 10.777 0.125 0.0621 0.0007 0.0925 0.0011 570 6 27.1 549 6 11.233 0.126 0.0604 0.0006 0.0888 0.0010 8.1 70 45 0.65 28.9 0.000109 0.15 2.080 0.031 0.1765 0.0014 0.4800 0.0072 11.593 0.200 0.1752 0.0015 0.873 2527 31 2608 14 3 41.1 560 6 11.017 0.126 0.0585 0.0006 0.0908 0.0011 9.1 140 91 0.65 11.7 0.000356 0.52 10.274 0.139 0.0640 0.0011 0.0968 0.0013 596 8 56.1 562 9 10.943 0.183 0.0615 0.0017 0.0911 0.0016 10.1 519 690 1.33 179.9 0.000014 0.02 2.478 0.027 0.1335 0.0012 0.4051 0.0052 7.655 0.245 0.1371 0.0030 0.866 2192 24 2190 38 0 13.1 565 6 10.878 0.116 0.0626 0.0005 0.0915 0.0010 11.1 31 18 0.58 10.0 - <0.01 2.695 0.051 0.1268 0.0017 0.3715 0.0070 6.555 0.156 0.1280 0.0019 0.791 2036 33 2070 26 2 68.1 565 6 10.937 0.115 0.0574 0.0004 0.0916 0.0010 12.1 922 100 0.11 77.9 0.000048 0.06 10.165 0.107 0.0605 0.0004 0.0983 0.0011 605 6 53.1 569 6 10.842 0.123 0.0592 0.0006 0.0922 0.0011 13.1 874 157 0.18 69.0 0.000130 0.44 10.878 0.116 0.0626 0.0005 0.0915 0.0010 565 6 7.1 570 6 10.777 0.125 0.0621 0.0007 0.0925 0.0011 14.1 678 26 0.04 279.4 0.000015 0.02 2.085 0.022 0.1880 0.0013 0.4794 0.0050 12.418 0.158 0.1879 0.0013 0.828 2525 22 2724 12 7 15.1 572 8 10.699 0.154 0.0646 0.0013 0.0928 0.0014 15.1 109 81 0.74 8.8 0.000206 0.67 10.699 0.154 0.0646 0.0013 0.0928 0.0014 572 8 70.1 575 7 10.726 0.131 0.0592 0.0008 0.0932 0.0012 16.1 527 228 0.43 44.8 0.000035 0.05 10.120 0.111 0.0605 0.0005 0.0988 0.0011 607 7 48.1 575 8 10.714 0.145 0.0597 0.0011 0.0933 0.0013 17.1 544 182 0.33 96.5 0.000021 0.04 4.848 0.052 0.0798 0.0004 0.2062 0.0022 2.259 0.028 0.0795 0.0005 0.876 1209 12 1184 12 -2 35.1 576 6 10.632 0.120 0.0644 0.0006 0.0935 0.0011 18.1 67 37 0.56 30.9 0.000095 0.13 1.862 0.027 0.1866 0.0012 0.5363 0.0078 13.711 0.221 0.1854 0.0013 0.900 2768 33 2702 12 -2 23.1 577 6 10.652 0.121 0.0607 0.0006 0.0937 0.0011 19.1 145 111 0.77 22.6 0.000053 0.09 5.509 0.071 0.0722 0.0028 0.1814 0.0024 1.787 0.076 0.0715 0.0029 0.307 1074 13 971 82 -11 22.1 578 7 10.662 0.136 0.0597 0.0009 0.0937 0.0012 20.1 153 86 0.56 25.8 0.000059 0.10 5.088 0.064 0.0740 0.0021 0.1965 0.0027 1.992 0.092 0.0735 0.0029 0.635 1156 15 1029 79 -12 44.1 580 6 10.624 0.113 0.0596 0.0004 0.0941 0.0010 21.1 213 105 0.49 24.7 0.000042 0.07 7.415 0.091 0.0697 0.0008 0.1344 0.0018 1.233 0.046 0.0666 0.0019 0.760 813 10 825 59 1 67.1 581 7 10.584 0.123 0.0609 0.0009 0.0943 0.0011 22.1 177 187 1.05 14.3 0.000434 0.05 10.662 0.136 0.0597 0.0009 0.0937 0.0012 578 7 43.1 585 6 10.537 0.111 0.0593 0.0005 0.0949 0.0010 23.1 385 143 0.37 31.1 0.000009 0.17 10.652 0.121 0.0607 0.0006 0.0937 0.0011 577 6 62.1 586 7 10.504 0.122 0.0600 0.0007 0.0951 0.0011 24.1 242 190 0.78 19.3 0.004800 8.69 10.760 0.132 0.1286 0.0013 0.0849 0.0011 525 6 28.1 586 7 10.505 0.121 0.0600 0.0007 0.0951 0.0011 25.1 196 125 0.64 17.3 0.000076 1.14 9.711 0.124 0.0699 0.0010 0.1018 0.0013 625 8 64.1 588 10 10.504 0.181 0.0571 0.0016 0.0955 0.0017 26.1 205 141 0.69 85.6 0.000001 <0.01 2.060 0.024 0.1865 0.0008 0.4855 0.0057 12.482 0.156 0.1865 0.0008 0.946 2551 25 2711 7 6 69.1 589 6 10.461 0.112 0.0591 0.0007 0.0956 0.0010 27.1 441 147 0.33 33.7 0.000234 0.23 11.233 0.126 0.0604 0.0006 0.0888 0.0010 549 6 46.1 592 8 10.423 0.135 0.0576 0.0009 0.0962 0.0013 28.1 349 150 0.43 28.5 0.000044 0.05 10.505 0.121 0.0600 0.0007 0.0951 0.0011 586 7 9.1 596 8 10.274 0.139 0.0640 0.0011 0.0968 0.0013 29.1 566 327 0.58 166.3 0.000020 0.03 2.924 0.031 0.1241 0.0004 0.3418 0.0036 5.837 0.065 0.1238 0.0004 0.951 1896 18 2012 6 6 5.1 599 7 10.244 0.119 0.0617 0.0007 0.0974 0.0012 30.1 463 251 0.54 39.5 0.000095 <0.01 10.070 0.112 0.0600 0.0006 0.0993 0.0011 610 7 65.1 602 8 10.224 0.136 0.0586 0.0010 0.0980 0.0013 31.1 418 139 0.33 29.2 0.000069 0.12 12.291 0.136 0.0583 0.0006 0.0813 0.0009 504 5 12.1 605 6 10.165 0.107 0.0605 0.0004 0.0983 0.0011 32.1 371 171 0.46 28.6 0.000628 1.17 11.147 0.125 0.0680 0.0007 0.0887 0.0010 548 6 66.1 606 7 10.162 0.121 0.0589 0.0007 0.0985 0.0012 33.1 300 70 0.23 79.8 0.000031 0.05 3.233 0.036 0.1195 0.0005 0.3092 0.0034 5.076 0.062 0.1191 0.0006 0.913 1737 17 1942 9 11 16.1 607 7 10.120 0.111 0.0605 0.0005 0.0988 0.0011 34.1 194 117 0.60 56.4 0.000013 0.02 2.949 0.034 0.1146 0.0006 0.3390 0.0039 5.350 0.069 0.1145 0.0007 0.898 1882 19 1871 10 -1 50.1 610 8 10.040 0.140 0.0631 0.0011 0.0993 0.0014 35.1 349 223 0.64 28.2 0.000299 0.64 10.632 0.120 0.0644 0.0006 0.0935 0.0011 576 6 30.1 610 7 10.070 0.112 0.0600 0.0006 0.0993 0.0011 36.1 190 12 0.06 88.4 0.000008 0.01 1.851 0.021 0.2286 0.0008 0.5403 0.0062 17.022 0.206 0.2285 0.0008 0.957 2785 26 3042 6 8 57.1 611 8 10.076 0.143 0.0581 0.0011 0.0995 0.0014 37.1 344 242 0.70 89.5 0.000016 0.03 3.301 0.036 0.1164 0.0008 0.3029 0.0033 4.854 0.063 0.1162 0.0008 0.851 1706 16 1899 12 10 2.1 614 7 10.009 0.117 0.0598 0.0007 0.1000 0.0012 38.1 413 77 0.19 31.7 0.000512 1.01 11.202 0.124 0.0666 0.0006 0.0884 0.0010 546 6 25.1 625 8 9.711 0.124 0.0699 0.0010 0.1018 0.0013 38.2 336 167 0.50 52.0 0.000052 0.09 5.562 0.062 0.0760 0.0005 0.1796 0.0020 1.865 0.026 0.0753 0.0006 0.797 1065 11 1076 17 1 42.1 627 8 9.766 0.131 0.0620 0.0011 0.1022 0.0014 39.1 72 67 0.94 22.6 0.000087 0.13 2.737 0.038 0.1340 0.0014 0.3649 0.0050 6.683 0.123 0.1328 0.0016 0.751 2005 24 2136 21 6 54.1 650 7 9.230 0.105 0.0778 0.0013 0.1062 0.0012 40.1 116 55 0.47 33.1 0.000045 0.07 3.027 0.037 0.1347 0.0009 0.3302 0.0041 6.107 0.088 0.1342 0.0010 0.859 1839 20 2153 13 15 21.1 813 10 1 7.415 0.091 0.0697 0.0008 1.233 0.046 0.1344 0.0018 0.760 0.0666 0.0019 41.1 328 72 0.22 25.6 0.000018 <0.01 11.017 0.126 0.0585 0.0006 0.0908 0.0011 560 6 3.1 867 14 -16 6.875 0.103 0.0723 0.0013 1.276 0.088 0.1440 0.0025 0.713 0.0642 0.0037 42.1 125 54 0.43 11.0 - 0.17 9.766 0.131 0.0620 0.0011 0.1022 0.0014 627 8 1.1 1035 12 4 5.727 0.074 0.0769 0.0009 1.806 0.052 0.1742 0.0023 0.456 0.0752 0.0019 43.1 877 257 0.29 71.5 0.000049 <0.01 10.537 0.111 0.0593 0.0005 0.0949 0.0010 585 6 6.1 1051 14 0 5.623 0.081 0.0783 0.0012 1.815 0.058 0.1770 0.0026 0.456 0.0744 0.0021 44.1 722 121 0.17 58.4 - 0.03 10.624 0.113 0.0596 0.0004 0.0941 0.0010 580 6 63.1 1058 37 8 6.155 0.068 0.0746 0.0014 1.671 0.036 0.1625 0.0018 0.521 0.0746 0.0014 45.1 265 136 0.51 98.5 0.000055 0.08 2.312 0.026 0.1455 0.0006 0.4322 0.0049 8.629 0.104 0.1448 0.0006 0.933 2316 22 2285 7 -1 59.1 1073 18 1 5.504 0.089 0.0782 0.0014 1.884 0.121 0.1811 0.0034 0.764 0.0755 0.0039 46.1 156 109 0.70 12.8 - <0.01 10.423 0.135 0.0576 0.0009 0.0962 0.0013 592 8 19.1 1074 13 -11 5.509 0.071 0.0722 0.0028 1.787 0.076 0.1814 0.0024 0.307 0.0715 0.0029 47.1 64 42 0.66 31.7 0.000153 0.20 1.727 0.024 0.2518 0.0014 0.5779 0.0082 19.931 0.306 0.2501 0.0015 0.922 2940 33 3186 9 8 38.2 1076 17 1 5.562 0.062 0.0760 0.0005 1.865 0.026 0.1796 0.0020 0.797 0.0753 0.0006 48.1 124 112 0.90 9.9 0.000191 0.06 10.714 0.145 0.0597 0.0011 0.0933 0.0013 575 8 20.1 1156 15 -12 5.088 0.064 0.0740 0.0021 1.992 0.092 0.1965 0.0027 0.635 0.0735 0.0029 49.1 89 53 0.60 34.1 0.000048 0.07 2.237 0.030 0.1804 0.0011 0.4468 0.0059 11.077 0.163 0.1798 0.0011 0.901 2381 26 2651 11 10 52.1 1200 14 2 4.880 0.063 0.0820 0.0009 2.287 0.046 0.2047 0.0027 0.644 0.0811 0.0012 50.1 107 108 1.01 9.2 0.000160 0.35 10.040 0.140 0.0631 0.0011 0.0993 0.0014 610 8 17.1 1209 12 -2 4.848 0.052 0.0798 0.0004 2.259 0.028 0.2062 0.0022 0.876 0.0795 0.0005 51.1 248 100 0.40 58.4 - <0.01 3.654 0.041 0.0980 0.0006 0.2738 0.0031 3.714 0.048 0.0984 0.0006 0.878 1560 16 1594 12 2 55.1 1570 9 -2 3.546 0.037 0.0974 0.0005 3.777 0.043 0.2820 0.0029 0.906 0.0972 0.0005 52.1 113 176 1.56 19.8 0.000069 0.11 4.880 0.063 0.0820 0.0009 0.2047 0.0027 2.287 0.046 0.0811 0.0012 0.644 1200 14 1223 30 2 58.1 1591 10 2 3.640 0.041 0.0980 0.0005 3.723 0.047 0.2748 0.0031 0.895 0.0982 0.0005 53.1 340 103 0.30 26.9 0.000058 0.01 10.842 0.123 0.0592 0.0006 0.0922 0.0011 569 6 51.1 1594 12 2 3.654 0.041 0.0980 0.0006 3.714 0.048 0.2738 0.0031 0.878 0.0984 0.0006 54.1 333 81 0.24 30.9 0.000148 2.00 9.230 0.105 0.0778 0.0013 0.1062 0.0012 650 7 34.1 1871 10 -1 2.949 0.034 0.1146 0.0006 5.350 0.069 0.3390 0.0039 0.898 0.1145 0.0007 55.1 938 73 0.08 227.2 0.000016 0.03 3.546 0.037 0.0974 0.0005 0.2820 0.0029 3.777 0.043 0.0972 0.0005 0.906 1601 15 1570 9 -2 37.1 1899 12 10 3.301 0.036 0.1164 0.0008 4.854 0.063 0.3029 0.0033 0.851 0.1162 0.0008 56.1 53 66 1.24 4.2 0.000555 0.32 10.943 0.183 0.0615 0.0017 0.0911 0.0016 562 9 33.1 1942 9 11 3.233 0.036 0.1195 0.0005 5.076 0.062 0.3092 0.0034 0.913 0.1191 0.0006 57.1 96 195 2.03 8.2 - <0.01 10.076 0.143 0.0581 0.0011 0.0995 0.0014 611 8 29.1 2012 6 6 2.924 0.031 0.1241 0.0004 5.837 0.065 0.3418 0.0036 0.951 0.1238 0.0004 58.1 294 141 0.48 69.4 - <0.01 3.640 0.041 0.0980 0.0005 0.2748 0.0031 3.723 0.047 0.0982 0.0005 0.895 1565 16 1591 10 2 11.1 2070 26 2 2.695 0.051 0.1268 0.0017 6.555 0.156 0.3715 0.0070 0.791 0.1280 0.0019 59.1 49 38 0.79 7.6 0.000611 1.03 5.504 0.089 0.0782 0.0014 0.1811 0.0034 1.884 0.121 0.0755 0.0039 0.764 1073 18 1081 103 1 39.1 2136 21 6 2.737 0.038 0.1340 0.0014 6.683 0.123 0.3649 0.0050 0.751 0.1328 0.0016 60.1 135 6 0.05 10.2 0.000214 0.25 11.315 0.150 0.0605 0.0010 0.0882 0.0012 545 7 40.1 2153 13 15 3.027 0.037 0.1347 0.0009 6.107 0.088 0.3302 0.0041 0.859 0.1342 0.0010 61.1 167 129 0.77 72.6 0.000011 0.01 1.978 0.023 0.1893 0.0008 0.5055 0.0060 13.186 0.165 0.1892 0.0008 0.942 2638 26 2735 7 4 10.1 2192 24 0 2.478 0.027 0.1335 0.0012 7.655 0.245 0.4051 0.0052 0.866 0.1371 0.0030 62.1 307 149 0.49 25.1 0.000065 0.07 10.504 0.122 0.0600 0.0007 0.0951 0.0011 586 7 45.1 2285 7 -1 2.312 0.026 0.1455 0.0006 8.629 0.104 0.4322 0.0049 0.933 0.1448 0.0006 63.1 377 232 0.62 52.6 0.000003 0.01 6.155 0.068 0.0746 0.0014 0.1625 0.0018 1.671 0.036 0.0746 0.0014 0.521 970 10 1058 37 8 8.1 2608 14 3 2.080 0.031 0.1765 0.0014 11.593 0.200 0.4800 0.0072 0.873 0.1752 0.0015 64.1 52 11 0.20 4.3 - <0.01 10.504 0.181 0.0571 0.0016 0.0955 0.0017 588 10 49.1 2651 11 10 2.237 0.030 0.1804 0.0011 11.077 0.163 0.4468 0.0059 0.901 0.1798 0.0011 65.1 130 67 0.52 10.9 0.000130 <0.01 10.224 0.136 0.0586 0.0010 0.0980 0.0013 602 8 18.1 2702 12 -2 1.862 0.027 0.1866 0.0012 13.711 0.221 0.5363 0.0078 0.900 0.1854 0.0013 66.1 222 66 0.30 18.8 - <0.01 10.162 0.121 0.0589 0.0007 0.0985 0.0012 606 7 26.1 2711 7 6 2.060 0.024 0.1865 0.0008 12.482 0.156 0.4855 0.0057 0.946 0.1865 0.0008 67.1 275 93 0.34 22.3 0.000022 0.19 10.584 0.123 0.0609 0.0009 0.0943 0.0011 581 7 14.1 2724 12 7 2.085 0.022 0.1880 0.0013 12.418 0.158 0.4794 0.0050 0.828 0.1879 0.0013 68.1 998 5 0.01 78.4 0.000024 <0.01 10.937 0.115 0.0574 0.0004 0.0916 0.0010 565 6 61.1 2735 7 4 1.978 0.023 0.1893 0.0008 13.186 0.165 0.5055 0.0060 0.942 0.1892 0.0008 69.1 692 179 0.26 56.8 0.000040 <0.01 10.461 0.112 0.0591 0.0007 0.0956 0.0010 589 6 36.1 3042 6 8 1.851 0.021 0.2286 0.0008 17.022 0.206 0.5403 0.0062 0.957 0.2285 0.0008 70.1 211 18 0.09 16.9 0.000113 <0.01 10.726 0.131 0.0592 0.0008 0.0932 0.0012 575 7 47.1 3186 9 8 1.727 0.024 0.2518 0.0014 19.931 0.306 0.5779 0.0082 0.922 0.2501 0.0015

Notes : 1. Uncertainties given at the one s level. Notes : 2. Error in Temora reference zircon calibration w as 0.84% & 0.39% for the analytical sessions. ( not included in above errors but required w hen comparing 206Pb/238U data from different mounts).

Figure 35. Tera-Wasserburg plot for sample 11-5-2, pre-Pagoda sandstone, Mt Bowers.

Table 4: 11-9-2 (Pagoda Formation)

Table xyz. Summary of SHRIMP U-Pb zircon results for sample 11-9-2, Pagoda sandstone, Mt. Weeks.

1.1 69 157 2.27 5.3 0.000264 0.60 11.255 0.193 0.0633 0.0029 0.0883 0.0016 546 9 31.1 253 8 24.205 0.766 0.0768 0.0061 0.0400 0.0013 2.1 107 70 0.66 22.4 - <0.01 4.090 0.057 0.0964 0.0011 0.2445 0.0034 3.248 0.059 0.0964 0.0011 0.771 1410 18 1555 22 9 53.1 509 6 12.131 0.145 0.0594 0.0008 0.0822 0.0010 3.1 29 69 2.38 4.8 - <0.01 5.240 0.112 0.0857 0.0020 0.1908 0.0041 2.256 0.071 0.0857 0.0020 0.681 1126 22 1332 44 15 54.1 517 6 11.908 0.148 0.0618 0.0011 0.0835 0.0011 4.1 250 258 1.03 41.7 0.000036 0.06 5.147 0.061 0.0817 0.0007 0.1942 0.0023 2.175 0.033 0.0812 0.0007 0.795 1144 12 1227 18 7 48.1 523 6 11.824 0.130 0.0591 0.0005 0.0844 0.0009 5.1 251 162 0.65 53.5 0.000425 0.69 4.033 0.051 0.0967 0.0017 0.2462 0.0031 3.080 0.091 0.0907 0.0024 0.429 1419 16 1441 51 2 49.1 539 6 11.454 0.133 0.0591 0.0007 0.0872 0.0010 6.1 131 86 0.65 27.5 0.000259 0.42 4.109 0.055 0.0936 0.0009 0.2424 0.0033 3.008 0.064 0.0900 0.0015 0.636 1399 17 1426 31 2 1.1 546 9 11.255 0.193 0.0633 0.0029 0.0883 0.0016 7.1 219 211 0.97 41.0 0.006188 10.39 4.581 0.056 0.1648 0.0011 0.1956 0.0026 2.077 0.136 0.0770 0.0049 0.203 1152 14 1122 128 -3 37.1 552 6 11.174 0.133 0.0593 0.0007 0.0894 0.0011 8.1 278 350 1.26 21.8 0.000010 0.08 10.964 0.133 0.0595 0.0008 0.0911 0.0011 562 7 42.1 557 7 11.063 0.135 0.0605 0.0008 0.0902 0.0011 9.1 257 91 0.36 44.6 0.000065 0.11 4.937 0.058 0.0903 0.0007 0.2023 0.0024 2.494 0.036 0.0894 0.0008 0.809 1188 13 1413 16 16 25.1 560 8 10.989 0.157 0.0617 0.0012 0.0907 0.0013 10.1 324 74 0.23 31.5 - 0.02 8.836 0.104 0.0626 0.0007 0.1132 0.0014 691 8 8.1 562 7 10.964 0.133 0.0595 0.0008 0.0911 0.0011 11.1 282 169 0.60 23.0 0.000066 0.06 10.554 0.127 0.0600 0.0008 0.0947 0.0012 583 7 62.1 565 6 10.911 0.124 0.0599 0.0006 0.0915 0.0011 12.1 41 60 1.45 9.7 0.000305 0.49 3.641 0.069 0.0973 0.0016 0.2733 0.0052 3.509 0.116 0.0931 0.0025 0.573 1558 26 1490 51 -5 29.1 568 6 10.835 0.117 0.0605 0.0011 0.0921 0.0010 13.1 177 92 0.52 53.0 0.000009 0.01 2.867 0.036 0.1203 0.0008 0.3487 0.0043 5.778 0.081 0.1202 0.0008 0.883 1928 21 1959 12 2 69.1 568 7 10.834 0.142 0.0600 0.0010 0.0922 0.0012 14.1 86 113 1.32 14.6 - <0.01 5.070 0.077 0.0814 0.0011 0.1973 0.0030 2.218 0.045 0.0815 0.0011 0.739 1161 16 1235 27 6 70.1 572 9 10.734 0.179 0.0625 0.0016 0.0928 0.0016 15.1 67 54 0.81 13.0 0.000160 0.26 4.407 0.070 0.0910 0.0013 0.2263 0.0036 2.770 0.066 0.0888 0.0016 0.666 1315 19 1399 34 6 16.1 576 9 10.691 0.175 0.0600 0.0015 0.0934 0.0016 16.1 77 314 4.06 6.2 0.000022 0.09 10.691 0.175 0.0600 0.0015 0.0934 0.0016 576 9 40.1 580 7 10.614 0.125 0.0599 0.0007 0.0941 0.0011 17.1 326 138 0.42 50.6 0.000040 0.07 5.531 0.064 0.0786 0.0006 0.1807 0.0021 1.945 0.027 0.0781 0.0006 0.818 1071 11 1149 16 7 57.1 580 7 10.576 0.139 0.0626 0.0010 0.0942 0.0013 18.1 100 12 0.12 12.1 0.000199 0.35 7.141 0.104 0.0705 0.0027 0.1396 0.0020 1.301 0.061 0.0676 0.0030 0.312 842 12 857 93 2 47.1 581 8 10.579 0.140 0.0615 0.0011 0.0943 0.0013 19.1 153 83 0.54 12.6 0.000216 0.07 10.468 0.141 0.0601 0.0010 0.0955 0.0013 588 8 11.1 583 7 10.554 0.127 0.0600 0.0008 0.0947 0.0012 20.1 107 53 0.49 8.7 0.000114 <0.01 10.526 0.155 0.0583 0.0012 0.0951 0.0014 586 8 34.1 584 7 10.534 0.130 0.0606 0.0008 0.0948 0.0012 21.1 31 7 0.21 4.0 0.000730 1.26 6.669 0.148 0.0802 0.0024 0.1481 0.0034 1.424 0.113 0.0697 0.0053 0.288 890 19 920 156 3 56.1 584 9 10.527 0.157 0.0609 0.0013 0.0948 0.0014 22.1 490 499 1.02 87.3 0.000059 0.10 4.822 0.058 0.0928 0.0006 0.2072 0.0025 2.627 0.037 0.0920 0.0007 0.862 1214 13 1467 14 17 20.1 586 8 10.526 0.155 0.0583 0.0012 0.0951 0.0014 23.1 333 56 0.17 130.2 0.000041 0.06 2.195 0.024 0.1461 0.0005 0.4553 0.0051 9.136 0.107 0.1455 0.0005 0.950 2419 22 2294 6 -5 19.1 588 8 10.468 0.141 0.0601 0.0010 0.0955 0.0013 24.1 321 234 0.73 47.9 0.000086 0.15 5.756 0.066 0.0769 0.0006 0.1735 0.0020 1.810 0.027 0.0757 0.0007 0.765 1031 11 1087 19 5 52.1 597 7 10.289 0.121 0.0607 0.0007 0.0971 0.0012 25.1 125 232 1.86 9.7 0.000461 0.36 10.989 0.157 0.0617 0.0012 0.0907 0.0013 560 8 44.1 600 7 10.244 0.117 0.0609 0.0006 0.0975 0.0011 26.1 46 20 0.44 10.6 0.000310 0.50 3.750 0.065 0.0971 0.0015 0.2653 0.0046 3.394 0.101 0.0928 0.0022 0.583 1517 23 1483 46 -2 38.1 611 7 10.047 0.119 0.0610 0.0007 0.0994 0.0012 27.1 244 48 0.20 49.2 0.000033 0.05 4.260 0.050 0.0864 0.0006 0.2346 0.0028 2.782 0.040 0.0860 0.0007 0.833 1359 15 1338 15 -2 10.1 691 8 8.836 0.104 0.0626 0.0007 0.1132 0.0014 28.1 284 82 0.29 124.0 0.000004 0.01 1.966 0.023 0.2178 0.0015 0.5086 0.0058 15.270 0.203 0.2177 0.0015 0.863 2651 25 2964 11 11 64.1 702 9 8.690 0.114 0.0631 0.0009 0.1150 0.0016 29.1 803 55 0.07 63.6 0.000012 0.18 10.835 0.117 0.0605 0.0011 0.0921 0.0010 568 6 18.1 842 12 2 7.141 0.104 0.0705 0.0027 1.301 0.061 0.1396 0.0020 0.312 0.0676 0.0030 30.1 150 112 0.74 39.8 0.000055 0.09 3.242 0.041 0.1100 0.0015 0.3082 0.0039 4.643 0.087 0.1093 0.0015 0.672 1732 19 1787 25 3 21.1 890 19 3 6.669 0.148 0.0802 0.0024 1.424 0.113 0.1481 0.0034 0.288 0.0697 0.0053 31.1 26 18 0.69 0.9 0.002979 3.19 24.205 0.766 0.0768 0.0061 0.0400 0.0013 253 8 67.1 1066 20 18 6.843 0.080 0.0755 0.0006 1.508 0.023 0.1460 0.0017 0.763 0.0749 0.0007 32.1 111 141 1.27 18.9 0.001554 2.61 5.044 0.071 0.0932 0.0052 0.1948 0.0035 2.112 0.221 0.0786 0.0074 0.642 1147 19 1163 186 1 68.1 1067 24 20 7.075 0.086 0.0758 0.0008 1.459 0.025 0.1412 0.0017 0.722 0.0749 0.0009 33.1 745 166 0.22 251.1 0.000012 0.02 2.548 0.027 0.1331 0.0006 0.3924 0.0041 7.195 0.082 0.1330 0.0006 0.925 2134 19 2138 8 0 24.1 1087 19 5 5.756 0.066 0.0769 0.0006 1.810 0.027 0.1735 0.0020 0.765 0.0757 0.0007 34.1 243 104 0.43 19.8 0.000181 0.14 10.534 0.130 0.0606 0.0008 0.0948 0.0012 584 7 55.1 1089 24 8 5.949 0.064 0.0763 0.0009 1.755 0.028 0.1680 0.0018 0.672 0.0758 0.0009 35.1 58 38 0.66 12.0 0.000079 0.13 4.165 0.068 0.0917 0.0013 0.2398 0.0039 2.995 0.070 0.0906 0.0015 0.701 1386 20 1438 32 4 63.1 1118 32 2 5.409 0.074 0.0781 0.0010 1.957 0.041 0.1846 0.0025 0.647 0.0769 0.0012 36.1 286 195 0.68 47.2 0.000006 0.01 5.203 0.061 0.0789 0.0006 0.1922 0.0022 2.088 0.030 0.0788 0.0006 0.824 1133 12 1167 16 3 32.1 1147 19 1 5.044 0.071 0.0932 0.0052 2.112 0.221 0.1948 0.0035 0.642 0.0786 0.0074 37.1 306 296 0.97 23.6 0.000088 0.09 11.174 0.133 0.0593 0.0007 0.0894 0.0011 552 6 17.1 1149 16 7 5.531 0.064 0.0786 0.0006 1.945 0.027 0.1807 0.0021 0.818 0.0781 0.0006 38.1 313 181 0.58 26.7 0.000091 0.09 10.047 0.119 0.0610 0.0007 0.0994 0.0012 611 7 7.1 1152 14 -3 4.581 0.056 0.1648 0.0011 2.077 0.136 0.1956 0.0026 0.203 0.0770 0.0049 39.1 335 242 0.72 59.6 0.000073 0.12 4.825 0.056 0.1098 0.0007 0.2070 0.0024 3.106 0.042 0.1088 0.0008 0.856 1213 13 1780 13 32 36.1 1167 16 3 5.203 0.061 0.0789 0.0006 2.088 0.030 0.1922 0.0022 0.824 0.0788 0.0006 40.1 319 165 0.52 25.8 0.000076 0.07 10.614 0.125 0.0599 0.0007 0.0941 0.0011 580 7 41.1 1173 12 0 4.994 0.058 0.0818 0.0006 2.169 0.040 0.1995 0.0023 0.627 0.0788 0.0011 41.1 259 181 0.70 44.5 0.000212 0.36 4.994 0.058 0.0818 0.0006 0.1995 0.0023 2.169 0.040 0.0788 0.0011 0.627 1173 12 1168 29 0 9.1 1188 13 16 4.937 0.058 0.0903 0.0007 2.494 0.036 0.2023 0.0024 0.809 0.0894 0.0008 42.1 255 206 0.81 19.8 0.000084 0.21 11.063 0.135 0.0605 0.0008 0.0902 0.0011 557 7 61.1 1196 15 8 5.353 0.062 0.0803 0.0006 2.058 0.028 0.1867 0.0021 0.835 0.0799 0.0006 43.1 218 15 0.07 55.1 - <0.01 3.407 0.041 0.1308 0.0007 0.2935 0.0035 5.301 0.070 0.1310 0.0007 0.902 1659 17 2111 10 21 46.1 1205 18 4 5.087 0.058 0.0815 0.0006 2.174 0.032 0.1963 0.0023 0.775 0.0803 0.0008 44.1 410 158 0.39 34.4 0.000086 0.12 10.244 0.117 0.0609 0.0006 0.0975 0.0011 600 7 4.1 1227 18 7 5.147 0.061 0.0817 0.0007 2.175 0.033 0.1942 0.0023 0.795 0.0812 0.0007 45.1 216 77 0.35 44.2 0.000564 0.93 4.208 0.051 0.0976 0.0009 0.2354 0.0029 2.912 0.075 0.2354 0.0029 0.476 1363 15 1420 43 4 14.1 1235 27 6 5.070 0.077 0.0814 0.0011 2.218 0.045 0.1973 0.0030 0.739 0.0815 0.0011 46.1 290 158 0.55 49.0 0.000083 0.14 5.087 0.058 0.0815 0.0006 0.1963 0.0023 2.174 0.032 0.0803 0.0008 0.775 1155 12 1205 18 4 3.1 1332 44 15 5.240 0.112 0.0857 0.0020 2.256 0.071 0.1908 0.0041 0.681 0.0857 0.0020 47.1 153 114 0.75 12.4 0.000061 0.26 10.579 0.140 0.0615 0.0011 0.0943 0.0013 581 8 27.1 1338 15 -2 4.260 0.050 0.0864 0.0006 2.782 0.040 0.2346 0.0028 0.833 0.0860 0.0007 48.1 616 182 0.30 44.7 0.000061 0.16 11.824 0.130 0.0591 0.0005 0.0844 0.0009 523 6 15.1 1399 34 6 4.407 0.070 0.0910 0.0013 2.770 0.066 0.2263 0.0036 0.666 0.0888 0.0016 49.1 357 47 0.13 26.8 0.000121 0.10 11.454 0.133 0.0591 0.0007 0.0872 0.0010 539 6 45.1 1420 43 4 4.208 0.051 0.0976 0.0009 2.912 0.075 0.2354 0.0029 0.476 0.2354 0.0029 50.1 199 136 0.68 56.3 0.000035 0.05 3.037 0.037 0.1288 0.0007 0.3291 0.0040 5.825 0.078 0.1284 0.0007 0.902 1834 19 2076 10 12 6.1 1426 31 2 4.109 0.055 0.0936 0.0009 3.008 0.064 0.2424 0.0033 0.636 0.0900 0.0015 51.1 418 65 0.16 137.9 0.000026 0.04 2.606 0.029 0.1391 0.0005 0.3835 0.0042 7.336 0.085 0.1387 0.0005 0.953 2093 20 2212 6 5 35.1 1438 32 4 4.165 0.068 0.0917 0.0013 2.995 0.070 0.2398 0.0039 0.701 0.0906 0.0015 52.1 290 15 0.05 24.2 0.000065 0.10 10.289 0.121 0.0607 0.0007 0.0971 0.0012 597 7 5.1 1441 51 2 4.033 0.051 0.0967 0.0017 3.080 0.091 0.2462 0.0031 0.429 0.0907 0.0024 53.1 274 1 0.00 19.4 0.000141 0.24 12.131 0.145 0.0594 0.0008 0.0822 0.0010 509 6 22.1 1467 14 17 4.822 0.058 0.0928 0.0006 2.627 0.037 0.2072 0.0025 0.862 0.0920 0.0007 54.1 223 106 0.48 16.1 0.000070 0.51 11.908 0.148 0.0618 0.0011 0.0835 0.0011 517 6 26.1 1483 46 -2 3.750 0.065 0.0971 0.0015 3.394 0.101 0.2653 0.0046 0.583 0.0928 0.0022 55.1 579 72 0.12 83.6 0.000038 0.07 5.949 0.064 0.0763 0.0009 0.1680 0.0018 1.755 0.028 0.0758 0.0009 0.672 1001 10 1089 24 8 12.1 1490 51 -5 3.641 0.069 0.0973 0.0016 3.509 0.116 0.2733 0.0052 0.573 0.0931 0.0025 56.1 89 101 1.13 7.3 - 0.18 10.527 0.157 0.0609 0.0013 0.0948 0.0014 584 9 2.1 1555 22 9 4.090 0.057 0.0964 0.0011 3.248 0.059 0.2445 0.0034 0.771 0.0964 0.0011 57.1 158 547 3.47 12.8 0.000233 0.39 10.576 0.139 0.0626 0.0010 0.0942 0.0013 580 7 39.1 1780 13 32 4.825 0.056 0.1098 0.0007 3.106 0.042 0.2070 0.0024 0.856 0.1088 0.0008 58.1 730 261 0.36 359.5 0.000005 0.01 1.745 0.018 0.2300 0.0004 0.5731 0.0060 18.166 0.194 0.2299 0.0004 0.986 2920 25 3051 3 4 30.1 1787 25 3 3.242 0.041 0.1100 0.0015 4.643 0.087 0.3082 0.0039 0.672 0.1093 0.0015 59.1 93 91 0.97 24.3 0.000047 0.07 3.294 0.046 0.1273 0.0012 0.3034 0.0042 5.299 0.091 0.1267 0.0013 0.813 1708 21 2052 18 17 65.1 1835 17 1 3.069 0.042 0.1127 0.0009 5.038 0.085 0.3257 0.0045 0.822 0.1122 0.0011 60.1 260 247 0.95 67.2 0.000010 0.02 3.329 0.039 0.1129 0.0006 0.3004 0.0035 4.670 0.060 0.1128 0.0006 0.907 1693 17 1844 10 8 60.1 1844 10 8 3.329 0.039 0.1129 0.0006 4.670 0.060 0.3004 0.0035 0.907 0.1128 0.0006 61.1 300 97 0.32 48.2 0.000025 0.04 5.353 0.062 0.0803 0.0006 0.1867 0.0021 2.058 0.028 0.0799 0.0006 0.835 1104 12 1196 15 8 13.1 1959 12 2 2.867 0.036 0.1203 0.0008 5.778 0.081 0.3487 0.0043 0.883 0.1202 0.0008 62.1 401 467 1.16 31.6 0.000050 0.12 10.911 0.124 0.0599 0.0006 0.0915 0.0011 565 6 59.1 2052 18 17 3.294 0.046 0.1273 0.0012 5.299 0.091 0.3034 0.0042 0.813 0.1267 0.0013 63.1 114 55 0.48 18.1 0.000086 0.14 5.409 0.074 0.0781 0.0010 0.1846 0.0025 1.957 0.041 0.0769 0.0012 0.647 1092 14 1118 32 2 50.1 2076 10 12 3.037 0.037 0.1288 0.0007 5.825 0.078 0.3291 0.0040 0.902 0.1284 0.0007 64.1 141 50 0.36 13.9 - 0.04 8.690 0.114 0.0631 0.0009 0.1150 0.0016 702 9 43.1 2111 10 21 3.407 0.041 0.1308 0.0007 5.301 0.070 0.2935 0.0035 0.902 0.1310 0.0007 65.1 97 77 0.79 27.2 0.000037 0.06 3.069 0.042 0.1127 0.0009 0.3257 0.0045 5.038 0.085 0.1122 0.0011 0.822 1817 22 1835 17 1 33.1 2138 8 0 2.548 0.027 0.1331 0.0006 7.195 0.082 0.3924 0.0041 0.925 0.1330 0.0006 66.1 67 43 0.65 35.5 - <0.01 1.617 0.024 0.2503 0.0015 0.6185 0.0092 21.348 0.341 0.2503 0.0015 0.927 3104 36 3187 9 3 51.1 2212 6 5 2.606 0.029 0.1391 0.0005 7.336 0.085 0.3835 0.0042 0.953 0.1387 0.0005 67.1 268 113 0.42 33.6 0.000045 0.08 6.843 0.080 0.0755 0.0006 0.1460 0.0017 1.508 0.023 0.0749 0.0007 0.763 879 10 1066 20 18 23.1 2294 6 -5 2.195 0.024 0.1461 0.0005 9.136 0.107 0.4553 0.0051 0.950 0.1455 0.0005 68.1 197 10 0.05 23.9 0.000064 0.11 7.075 0.086 0.0758 0.0008 0.1412 0.0017 1.459 0.025 0.0749 0.0009 0.722 851 10 1067 24 20 28.1 2964 11 11 1.966 0.023 0.2178 0.0015 15.270 0.203 0.5086 0.0058 0.863 0.2177 0.0015 69.1 152 89 0.58 12.1 - 0.12 10.834 0.142 0.0600 0.0010 0.0922 0.0012 568 7 58.1 3051 3 4 1.745 0.018 0.2300 0.0004 18.166 0.194 0.5731 0.0060 0.986 0.2299 0.0004 70.1 68 50 0.74 5.4 0.000304 0.41 10.734 0.179 0.0625 0.0016 0.0928 0.0016 572 9 66.1 3187 9 3 1.617 0.024 0.2503 0.0015 21.348 0.341 0.6185 0.0092 0.927 0.2503 0.0015

Notes : 1. Uncertainties given at the one s level. Notes : 2. Error in Temora reference zircon calibration w as 0.51% for the analytical session. ( not included in above errors but required w hen comparing 206Pb/238U data from different mounts).

Figure 36. Tera-Wasserburg plot for sample 11-9-2, Pagoda Formation, Mt Weeks.

Table 5: 11-5-8 (Fairchild Formation)

Table xyz. Summary of SHRIMP U-Pb zircon results for sample 11-5-8, Fairchild, Mt. Bowers.

1.1 107 133 1.24 8.3 0.000217 0.31 11.121 0.154 0.0612 0.0012 0.0896 0.0013 553 8 54.1 468 7 13.238 0.189 0.0587 0.0013 0.0753 0.0011 2.1 280 171 0.61 22.0 0.000077 0.08 10.921 0.128 0.0596 0.0007 0.0915 0.0011 564 6 57.1 509 5 12.126 0.129 0.0609 0.0005 0.0821 0.0009 3.1 603 93 0.16 167.4 0.000604 0.94 3.094 0.033 0.1282 0.0016 0.3202 0.0034 5.304 0.094 0.1201 0.0017 0.594 1791 17 1958 26 9 53.1 514 7 12.017 0.162 0.0603 0.0011 0.0829 0.0011 4.1 48 96 2.01 4.0 0.000571 0.75 10.280 0.183 0.0659 0.0018 0.0965 0.0018 594 10 70.1 522 6 11.272 0.116 0.0971 0.0037 0.0844 0.0010 5.1 506 24 0.05 174.9 0.000060 0.09 2.485 0.026 0.1446 0.0007 0.4020 0.0043 7.973 0.095 0.1438 0.0008 0.895 2178 20 2274 9 4 55.1 523 7 11.306 0.136 0.0939 0.0055 0.0845 0.0012 6.1 545 163 0.30 87.2 0.000005 0.01 5.373 0.058 0.0517 0.0139 0.1882 0.0026 1.592 0.407 0.0613 0.0154 0.335 1112 14 651 540 -71 10.1 530 6 11.658 0.127 0.0581 0.0005 0.0858 0.0010 7.1 199 52 0.26 15.1 - 0.03 11.330 0.140 0.0586 0.0009 0.0882 0.0011 545 7 42.1 531 5 11.660 0.120 0.0573 0.0003 0.0858 0.0009 8.1 503 86 0.17 54.0 0.000168 1.38 7.994 0.088 0.0757 0.0005 0.1234 0.0014 750 8 58.1 533 6 11.585 0.137 0.0586 0.0008 0.0863 0.0010 9.1 1068 545 0.51 82.2 0.000194 0.44 11.154 0.116 0.0621 0.0004 0.0893 0.0009 551 6 50.1 539 6 11.364 0.126 0.0662 0.0022 0.0871 0.0010 10.1 498 180 0.36 36.7 0.000075 0.02 11.658 0.127 0.0581 0.0005 0.0858 0.0010 530 6 7.1 545 7 11.330 0.140 0.0586 0.0009 0.0882 0.0011 11.1 308 123 0.40 132.9 0.000011 0.02 1.991 0.022 0.1959 0.0006 0.5021 0.0055 13.555 0.155 0.1958 0.0006 0.963 2623 24 2791 5 6 45.1 547 6 11.288 0.127 0.0584 0.0006 0.0886 0.0010 12.1 157 136 0.86 12.4 - 0.18 10.875 0.139 0.0605 0.0010 0.0918 0.0012 566 7 9.1 551 6 11.154 0.116 0.0621 0.0004 0.0893 0.0009 13.1 601 251 0.42 94.2 0.000016 0.03 5.483 0.058 0.0759 0.0012 0.1823 0.0019 1.903 0.037 0.0757 0.0012 0.555 1080 11 1087 32 1 52.1 553 7 11.131 0.134 0.0609 0.0008 0.0896 0.0011 14.1 400 95 0.24 32.6 0.000075 0.13 10.558 0.119 0.0605 0.0006 0.0946 0.0011 583 6 1.1 553 8 11.121 0.154 0.0612 0.0012 0.0896 0.0013 15.1 1727 522 0.30 721.5 0.000862 1.21 2.057 0.021 0.1967 0.0002 0.4803 0.0049 12.327 0.131 0.1861 0.0006 0.956 2529 21 2708 5 7 49.1 555 6 11.133 0.130 0.0578 0.0007 0.0899 0.0011 16.1 374 107 0.29 53.4 0.000353 0.60 6.020 0.067 0.0757 0.0015 0.1652 0.0019 1.616 0.051 0.0710 0.0019 0.603 986 11 957 53 -3 21.1 556 6 11.059 0.120 0.0613 0.0010 0.0901 0.0010 17.1 1335 321 0.24 201.3 0.003422 5.85 5.697 0.059 0.1246 0.0014 0.1653 0.0017 1.730 0.053 0.0759 0.0022 0.342 986 10 1093 57 10 23.1 558 6 11.051 0.130 0.0589 0.0007 0.0905 0.0011 18.1 539 146 0.27 118.9 0.000018 0.03 3.897 0.041 0.1139 0.0004 0.2566 0.0027 4.020 0.046 0.1136 0.0005 0.926 1472 14 1858 8 21 20.1 560 6 10.972 0.114 0.0626 0.0007 0.0907 0.0010 19.1 344 150 0.44 29.0 0.000125 0.07 10.165 0.115 0.0606 0.0006 0.0983 0.0011 604 7 2.1 564 6 10.921 0.128 0.0596 0.0007 0.0915 0.0011 20.1 1482 131 0.09 116.1 0.000156 0.47 10.972 0.114 0.0626 0.0007 0.0907 0.0010 560 6 12.1 566 7 10.875 0.139 0.0605 0.0010 0.0918 0.0012 21.1 600 343 0.57 46.6 0.000196 0.31 11.059 0.120 0.0613 0.0010 0.0901 0.0010 556 6 37.1 571 9 10.771 0.179 0.0605 0.0016 0.0927 0.0016 22.1 866 10 0.01 69.6 0.000052 <0.01 10.686 0.113 0.0591 0.0004 0.0936 0.0010 577 6 59.1 572 7 10.763 0.128 0.0598 0.0008 0.0928 0.0011 23.1 295 118 0.40 22.9 0.000035 0.01 11.051 0.130 0.0589 0.0007 0.0905 0.0011 558 6 22.1 577 6 10.686 0.113 0.0591 0.0004 0.0936 0.0010 24.1 325 213 0.65 52.1 0.000043 0.07 5.353 0.061 0.0761 0.0006 0.1867 0.0021 1.944 0.029 0.0755 0.0007 0.760 1103 11 1083 19 -2 60.1 579 6 10.653 0.111 0.0586 0.0003 0.0940 0.0010 25.1 186 203 1.09 15.3 0.000123 0.02 10.471 0.131 0.0597 0.0009 0.0955 0.0012 588 7 29.1 581 6 10.591 0.117 0.0600 0.0005 0.0943 0.0011 26.1 138 104 0.76 12.5 0.000136 1.81 9.503 0.126 0.0756 0.0016 0.1033 0.0014 634 8 61.1 581 7 10.580 0.124 0.0604 0.0007 0.0944 0.0011 27.1 717 276 0.39 168.3 0.000939 1.51 3.662 0.038 0.1321 0.0006 0.2690 0.0029 4.429 0.074 0.1194 0.0016 0.633 1535 15 1948 23 21 14.1 583 6 10.558 0.119 0.0605 0.0006 0.0946 0.0011 28.1 194 89 0.46 27.0 0.000057 0.10 6.167 0.074 0.0930 0.0026 0.1620 0.0019 2.060 0.063 0.0922 0.0026 0.390 968 11 1472 54 34 25.1 588 7 10.471 0.131 0.0597 0.0009 0.0955 0.0012 29.1 436 72 0.16 35.4 0.000181 0.08 10.591 0.117 0.0600 0.0005 0.0943 0.0011 581 6 47.1 590 8 10.459 0.151 0.0579 0.0012 0.0958 0.0014 30.1 137 95 0.69 11.6 0.000044 <0.01 10.176 0.140 0.0595 0.0011 0.0983 0.0014 605 8 68.1 590 7 10.431 0.121 0.0593 0.0007 0.0959 0.0011 31.1 129 97 0.75 23.1 0.000030 0.05 4.783 0.061 0.0787 0.0008 0.2090 0.0027 2.255 0.038 0.0783 0.0009 0.752 1223 14 1153 22 -6 39.1 591 8 10.318 0.137 0.0673 0.0024 0.0960 0.0013 32.1 145 87 0.60 16.2 0.000049 <0.01 7.680 0.096 0.0637 0.0008 0.1305 0.0017 791 10 4.1 594 10 10.280 0.183 0.0659 0.0018 0.0965 0.0018 33.1 913 759 0.83 117.2 0.001221 2.11 6.696 0.070 0.0846 0.0045 0.1462 0.0016 1.351 0.104 0.0670 0.0051 0.140 880 9 839 159 -5 35.1 603 8 10.188 0.133 0.0605 0.0010 0.0981 0.0013 34.1 697 133 0.19 58.7 - <0.01 10.193 0.110 0.0593 0.0005 0.0982 0.0011 604 6 34.1 604 6 10.193 0.110 0.0593 0.0005 0.0982 0.0011 35.1 162 356 2.21 13.6 0.000080 0.06 10.188 0.133 0.0605 0.0010 0.0981 0.0013 603 8 19.1 604 7 10.165 0.115 0.0606 0.0006 0.0983 0.0011 36.1 107 110 1.03 31.8 0.000017 0.03 2.906 0.037 0.1143 0.0008 0.3440 0.0044 5.411 0.081 0.1141 0.0009 0.862 1906 21 1866 14 -2 30.1 605 8 10.176 0.140 0.0595 0.0011 0.0983 0.0014 37.1 56 70 1.25 4.4 0.000247 0.17 10.771 0.179 0.0605 0.0016 0.0927 0.0016 571 9 48.1 613 8 10.019 0.133 0.0601 0.0010 0.0998 0.0014 38.1 234 119 0.51 57.9 - <0.01 3.479 0.040 0.1853 0.0019 0.2875 0.0033 7.350 0.115 0.1854 0.0019 0.743 1629 17 2702 17 40 65.1 616 10 9.970 0.164 0.0606 0.0015 0.1003 0.0017 39.1 129 77 0.59 10.8 0.000555 0.93 10.318 0.137 0.0673 0.0024 0.0960 0.0013 591 8 64.1 623 7 9.847 0.120 0.0607 0.0008 0.1015 0.0013 40.1 198 167 0.84 33.5 0.000035 0.06 5.083 0.060 0.0909 0.0021 0.1966 0.0023 2.452 0.065 0.0904 0.0021 0.450 1157 13 1435 45 19 26.1 634 8 9.503 0.126 0.0756 0.0016 0.1033 0.0014 41.1 357 57 0.16 32.3 0.000050 0.06 9.514 0.108 0.0616 0.0006 0.1051 0.0012 644 7 69.1 641 7 9.566 0.115 0.0616 0.0008 0.1045 0.0013 42.1 1883 24 0.01 138.7 0.000018 <0.01 11.660 0.120 0.0573 0.0003 0.0858 0.0009 531 5 41.1 644 7 9.514 0.108 0.0616 0.0006 0.1051 0.0012 43.1 211 100 0.48 32.9 0.000018 0.03 5.494 0.064 0.0799 0.0007 0.1820 0.0021 1.998 0.030 0.0797 0.0007 0.792 1078 12 1188 18 9 62.1 669 10 9.151 0.142 0.0611 0.0014 0.1094 0.0017 44.1 317 206 0.65 70.2 0.009220 15.27 3.873 0.042 0.2642 0.0497 0.2188 0.0169 4.334 2.604 0.1437 0.0856 0.128 1275 89 2272 1027 44 56.1 735 8 15 7.987 0.084 0.0965 0.0005 1.130 0.060 0.1208 0.0013 0.226 0.0679 0.0033 45.1 375 244 0.65 28.5 0.000061 <0.01 11.288 0.127 0.0584 0.0006 0.0886 0.0010 547 6 8.1 750 8 7.994 0.088 0.0757 0.0005 0.1234 0.0014 46.1 445 71 0.16 58.0 0.000022 0.04 6.593 0.072 0.0746 0.0005 0.1516 0.0017 1.550 0.020 0.0743 0.0005 0.833 910 9 1050 15 13 32.1 791 10 7.680 0.096 0.0637 0.0008 0.1305 0.0017 47.1 92 462 5.00 7.6 0.000217 <0.01 10.459 0.151 0.0579 0.0012 0.0958 0.0014 590 8 33.1 880 9 -5 6.696 0.070 0.0846 0.0045 1.351 0.104 0.1462 0.0016 0.140 0.0670 0.0051 48.1 136 97 0.71 11.7 0.000167 <0.01 10.019 0.133 0.0601 0.0010 0.0998 0.0014 613 8 16.1 986 11 -3 6.020 0.067 0.0757 0.0015 1.616 0.051 0.1652 0.0019 0.603 0.0710 0.0019 49.1 297 200 0.67 22.9 - <0.01 11.133 0.130 0.0578 0.0007 0.0899 0.0011 555 6 17.1 986 10 10 5.697 0.059 0.1246 0.0014 1.730 0.053 0.1653 0.0017 0.342 0.0759 0.0022 50.1 437 121 0.28 33.0 0.000471 0.97 11.364 0.126 0.0662 0.0022 0.0871 0.0010 539 6 67.1 1030 11 -62 5.787 0.065 0.0586 0.0075 1.456 0.183 0.1733 0.0020 0.126 0.0609 0.0076 51.1 819 49 0.06 190.3 0.000022 0.03 3.699 0.039 0.1161 0.0004 0.2702 0.0028 4.320 0.050 0.1159 0.0004 0.953 1542 14 1893 6 19 46.1 1050 15 13 6.593 0.072 0.0746 0.0005 1.550 0.020 0.1516 0.0017 0.833 0.0743 0.0005 52.1 235 98 0.42 18.2 - 0.29 11.131 0.134 0.0609 0.0008 0.0896 0.0011 553 7 13.1 1080 11 1 5.483 0.058 0.0759 0.0012 1.903 0.037 0.1823 0.0019 0.555 0.0757 0.0012 53.1 129 195 1.51 9.2 0.000096 0.33 12.017 0.162 0.0603 0.0011 0.0829 0.0011 514 7 24.1 1103 11 -2 5.353 0.061 0.0761 0.0006 1.944 0.029 0.1867 0.0021 0.760 0.0755 0.0007 54.1 114 109 0.95 7.4 - 0.28 13.238 0.189 0.0587 0.0013 0.0753 0.0011 468 7 6.1 1112 14 -71 5.373 0.058 0.0517 0.0139 1.592 0.407 0.1882 0.0026 0.335 0.0613 0.0154 55.1 262 189 0.72 19.9 0.002597 4.43 11.306 0.136 0.0939 0.0055 0.0845 0.0012 523 7 66.1 1167 13 -4 5.038 0.059 0.0770 0.0007 2.110 0.030 0.1985 0.0023 0.809 0.0770 0.0007 56.1 785 83 0.11 84.4 0.001987 3.48 7.987 0.084 0.0965 0.0005 0.1208 0.0013 1.130 0.060 0.0679 0.0033 0.226 735 8 867 99 15 43.1 1188 18 9 5.494 0.064 0.0799 0.0007 1.998 0.030 0.1820 0.0021 0.792 0.0797 0.0007 57.1 909 165 0.18 64.4 0.000001 0.43 12.126 0.129 0.0609 0.0005 0.0821 0.0009 509 5 31.1 1223 14 -6 4.783 0.061 0.0787 0.0008 2.255 0.038 0.2090 0.0027 0.752 0.0783 0.0009 58.1 258 302 1.17 19.2 - 0.06 11.585 0.137 0.0586 0.0008 0.0863 0.0010 533 6 44.1 1275 89 44 3.873 0.042 0.2642 0.0497 4.334 2.604 0.2188 0.0169 0.128 0.1437 0.0856 59.1 230 489 2.13 18.3 0.000021 0.09 10.763 0.128 0.0598 0.0008 0.0928 0.0011 572 7 40.1 1435 45 19 5.083 0.060 0.0909 0.0021 2.452 0.065 0.1966 0.0023 0.450 0.0904 0.0021 60.1 1212 665 0.55 97.7 0.000038 -0.09 10.653 0.111 0.0586 0.0003 0.0940 0.0010 579 6 28.1 1472 54 34 6.167 0.074 0.0930 0.0026 2.060 0.063 0.1620 0.0019 0.390 0.0922 0.0026 61.1 243 294 1.21 19.8 - 0.13 10.580 0.124 0.0604 0.0007 0.0944 0.0011 581 7 18.1 1858 8 21 3.897 0.041 0.1139 0.0004 4.020 0.046 0.2566 0.0027 0.926 0.1136 0.0005 62.1 77 138 1.79 7.2 0.000174 -0.09 9.151 0.142 0.0611 0.0014 0.1094 0.0017 669 10 36.1 1866 14 -2 2.906 0.037 0.1143 0.0008 5.411 0.081 0.3440 0.0044 0.862 0.1141 0.0009 63.1 127 83 0.66 43.5 0.000019 0.03 2.504 0.031 0.1360 0.0008 0.3992 0.0049 7.470 0.100 0.1358 0.0008 0.895 2165 23 2174 11 0 51.1 1893 6 19 3.699 0.039 0.1161 0.0004 4.320 0.050 0.2702 0.0028 0.953 0.1159 0.0004 64.1 189 181 0.96 16.5 - 0.02 9.847 0.120 0.0607 0.0008 0.1015 0.0013 623 7 27.1 1948 23 21 3.662 0.038 0.1321 0.0006 4.429 0.074 0.2690 0.0029 0.633 0.1194 0.0016 65.1 56 91 1.62 4.8 0.000315 0.03 9.970 0.164 0.0606 0.0015 0.1003 0.0017 616 10 3.1 1958 26 9 3.094 0.033 0.1282 0.0016 5.304 0.094 0.3202 0.0034 0.594 0.1201 0.0017 66.1 194 112 0.58 33.0 - 0.00 5.038 0.059 0.0770 0.0007 0.1985 0.0023 2.110 0.030 0.0770 0.0007 0.809 1167 13 1121 17 -4 63.1 2174 11 0 2.504 0.031 0.1360 0.0008 7.470 0.100 0.3992 0.0049 0.895 0.1358 0.0008 67.1 312 34 0.11 46.3 0.000033 0.06 5.787 0.065 0.0586 0.0075 0.1733 0.0020 1.456 0.183 0.0609 0.0076 0.126 1030 11 637 268 -62 5.1 2274 9 4 2.485 0.026 0.1446 0.0007 7.973 0.095 0.4020 0.0043 0.895 0.1438 0.0008 68.1 270 142 0.52 22.3 - -0.04 10.431 0.121 0.0593 0.0007 0.0959 0.0011 590 7 38.1 2702 17 40 3.479 0.040 0.1853 0.0019 7.350 0.115 0.2875 0.0033 0.743 0.1854 0.0019 69.1 209 234 1.12 18.8 0.000069 0.06 9.566 0.115 0.0616 0.0008 0.1045 0.0013 641 7 15.1 2708 5 7 2.057 0.021 0.1967 0.0002 12.327 0.131 0.4803 0.0049 0.956 0.1861 0.0006 70.1 1474 266 0.18 112.4 0.002657 4.83 11.272 0.116 0.0971 0.0037 0.0844 0.0010 522 6 11.1 2791 5 6 1.991 0.022 0.1959 0.0006 13.555 0.155 0.5021 0.0055 0.963 0.1958 0.0006

Notes : 1. Uncertainties given at the one s level. Notes : 2. Error in Temora reference zircon calibration w as 0.39% & 0.77% for the analytical sessions. ( not included in above errors but required w hen comparing 206Pb/238U data from different mounts).

Figure 37. Tera-Wasserburg plot for sample 11-5-8, Fairchild Formation, Mt Bowers.

Table 6: 11-5-15 (lower Buckley Formation)

Table xyz. Summary of SHRIMP U-Pb zircon results for sample 11-5-15, Lower Buckley, Mt. Bowers.

1.1 53 65 1.23 3.8 0.000297 0.31 12.017 0.216 0.0601 0.0018 0.0830 0.0015 514 9 49.1 204 4 16.976 0.177 0.4137 0.0024 0.0321 0.0006 2.1 136 91 0.67 10.1 0.000107 0.19 11.618 0.157 0.0596 0.0011 0.0859 0.0012 531 7 40.1 416 5 14.959 0.165 0.0575 0.0006 0.0666 0.0007 3.1 206 78 0.38 16.4 - 0.29 10.767 0.132 0.0615 0.0009 0.0926 0.0012 571 7 59.1 457 10 13.556 0.286 0.0596 0.0024 0.0735 0.0016 4.1 752 88 0.12 60.3 0.000025 0.11 10.706 0.114 0.0601 0.0004 0.0933 0.0010 575 6 53.1 458 10 13.530 0.282 0.0588 0.0037 0.0737 0.0016 5.1 148 117 0.79 56.1 0.000004 0.01 2.265 0.027 0.1522 0.0044 0.4415 0.0053 9.264 0.290 0.1522 0.0044 0.384 2357 24 2371 49 1 21.1 461 6 13.441 0.174 0.0595 0.0015 0.0741 0.0010 6.1 408 117 0.29 33.3 0.000038 0.19 10.519 0.117 0.0610 0.0008 0.0949 0.0011 584 6 44.1 465 6 13.300 0.162 0.0600 0.0009 0.0748 0.0009 7.1 398 65 0.16 31.6 - 0.05 10.796 0.121 0.0595 0.0006 0.0926 0.0011 571 6 11.1 469 8 13.173 0.224 0.0605 0.0018 0.0755 0.0013 8.1 64 48 0.75 4.8 0.000034 <0.01 11.540 0.189 0.0568 0.0016 0.0868 0.0015 537 9 39.1 484 5 12.781 0.143 0.0591 0.0006 0.0780 0.0009 9.1 17 19 1.11 1.2 0.002001 0.93 12.220 0.337 0.0649 0.0033 0.0811 0.0023 503 14 64.1 492 6 12.589 0.150 0.0584 0.0008 0.0793 0.0010 10.1 218 112 0.51 81.3 0.000015 0.02 2.301 0.027 0.1832 0.0011 0.4345 0.0050 10.968 0.145 0.1831 0.0011 0.880 2326 23 2681 10 13 20.1 498 8 12.391 0.193 0.0608 0.0015 0.0803 0.0013 11.1 67 33 0.50 4.4 0.000390 0.51 13.173 0.224 0.0605 0.0018 0.0755 0.0013 469 8 9.1 503 14 12.220 0.337 0.0649 0.0033 0.0811 0.0023 12.1 48 48 0.99 3.7 0.000026 0.14 11.085 0.200 0.0599 0.0018 0.0901 0.0017 556 10 26.1 511 6 12.115 0.138 0.0585 0.0007 0.0824 0.0010 12.2 490 45 0.09 35.5 0.000008 0.28 11.851 0.132 0.0601 0.0006 0.0841 0.0010 521 6 1.1 514 9 12.017 0.216 0.0601 0.0018 0.0830 0.0015 13.1 429 377 0.88 32.8 0.000025 0.01 11.238 0.125 0.0586 0.0006 0.0890 0.0010 549 6 12.2 521 6 11.851 0.132 0.0601 0.0006 0.0841 0.0010 14.1 676 57 0.08 54.6 0.000010 0.10 10.634 0.114 0.0601 0.0005 0.0939 0.0010 579 6 28.1 522 6 11.829 0.135 0.0597 0.0007 0.0843 0.0010 15.1 189 90 0.48 69.1 0.000022 0.03 2.355 0.028 0.1821 0.0015 0.4245 0.0050 10.644 0.154 0.1818 0.0015 0.810 2281 22 2670 14 15 56.1 524 6 11.787 0.140 0.0599 0.0009 0.0846 0.0010 16.1 239 169 0.71 19.2 0.000082 0.18 10.684 0.127 0.0607 0.0015 0.0934 0.0011 576 7 43.1 524 6 11.777 0.133 0.0598 0.0007 0.0847 0.0010 17.1 1449 116 0.08 115.7 0.000008 0.10 10.755 0.111 0.0600 0.0003 0.0929 0.0010 573 6 45.1 526 6 11.737 0.134 0.0596 0.0007 0.0850 0.0010 18.1 294 120 0.41 24.4 0.000038 0.15 10.356 0.120 0.0610 0.0007 0.0964 0.0011 593 7 52.1 527 6 11.732 0.131 0.0587 0.0006 0.0852 0.0010 19.1 255 154 0.60 50.5 0.000074 0.12 4.336 0.050 0.0989 0.0007 0.2304 0.0026 3.107 0.043 0.0978 0.0008 0.822 1336 14 1583 15 16 30.1 528 6 11.674 0.137 0.0602 0.0008 0.0854 0.0010 20.1 84 88 1.05 5.8 - 0.45 12.391 0.193 0.0608 0.0015 0.0803 0.0013 498 8 24.1 528 7 11.670 0.159 0.0604 0.0011 0.0854 0.0012 21.1 187 412 2.20 12.0 - 0.40 13.441 0.174 0.0595 0.0015 0.0741 0.0010 461 6 2.1 531 7 11.618 0.157 0.0596 0.0011 0.0859 0.0012 22.1 716 364 0.51 94.3 0.003337 5.77 6.522 0.069 0.1250 0.0016 0.1445 0.0016 1.546 0.055 0.0776 0.0026 0.304 870 9 1137 68 23 31.1 534 9 11.547 0.195 0.0597 0.0017 0.0864 0.0015 23.1 397 49 0.12 48.8 - <0.01 6.978 0.077 0.0716 0.0015 0.1433 0.0016 1.418 0.033 0.0718 0.0015 0.470 863 9 979 42 12 46.1 535 7 11.554 0.158 0.0576 0.0016 0.0866 0.0012 24.1 122 28 0.23 9.0 0.000056 0.30 11.670 0.159 0.0604 0.0011 0.0854 0.0012 528 7 63.1 536 6 11.546 0.140 0.0580 0.0010 0.0866 0.0011 25.1 395 154 0.39 93.7 0.000004 0.01 3.620 0.039 0.1200 0.0006 0.2762 0.0030 4.567 0.054 0.1199 0.0006 0.915 1572 15 1955 9 20 8.1 537 9 11.540 0.189 0.0568 0.0016 0.0868 0.0015 26.1 375 143 0.38 26.6 0.000057 0.12 12.115 0.138 0.0585 0.0007 0.0824 0.0010 511 6 70.1 537 8 11.463 0.177 0.0622 0.0015 0.0868 0.0014 27.1 128 54 0.42 47.6 - <0.01 2.309 0.029 0.1974 0.0011 0.4330 0.0053 11.789 0.159 0.1974 0.0011 0.917 2319 24 2805 9 17 55.1 542 7 11.378 0.151 0.0595 0.0010 0.0878 0.0012 28.1 334 69 0.20 24.3 - 0.23 11.829 0.135 0.0597 0.0007 0.0843 0.0010 522 6 29.1 543 6 11.356 0.126 0.0601 0.0006 0.0879 0.0010 29.1 442 201 0.45 33.5 - 0.21 11.356 0.126 0.0601 0.0006 0.0879 0.0010 543 6 69.1 545 8 11.321 0.176 0.0596 0.0015 0.0882 0.0014 30.1 271 102 0.38 20.0 - 0.28 11.674 0.137 0.0602 0.0008 0.0854 0.0010 528 6 54.1 546 6 11.293 0.121 0.0598 0.0005 0.0884 0.0010 31.1 55 74 1.35 4.1 0.000418 0.19 11.547 0.195 0.0597 0.0017 0.0864 0.0015 534 9 13.1 549 6 11.238 0.125 0.0586 0.0006 0.0890 0.0010 32.1 29 23 0.80 2.3 - 0.22 10.799 0.223 0.0609 0.0022 0.0924 0.0020 570 12 66.1 550 6 11.223 0.123 0.0592 0.0005 0.0890 0.0010 33.1 67 51 0.77 5.5 0.000254 0.26 10.349 0.160 0.0618 0.0014 0.0964 0.0015 593 9 12.1 556 10 11.085 0.200 0.0599 0.0018 0.0901 0.0017 34.1 74 84 1.14 5.8 0.000354 0.05 10.987 0.173 0.0593 0.0014 0.0910 0.0015 561 9 37.1 558 9 11.059 0.176 0.0593 0.0015 0.0904 0.0015 35.1 92 37 0.40 9.4 - 0.14 8.445 0.120 0.0645 0.0012 0.1182 0.0017 720 10 34.1 561 9 10.987 0.173 0.0593 0.0014 0.0910 0.0015 36.1 630 244 0.39 51.0 0.000023 <0.01 10.625 0.114 0.0593 0.0005 0.0941 0.0010 580 6 38.1 564 6 10.881 0.117 0.0629 0.0005 0.0915 0.0010 37.1 66 48 0.72 5.2 - 0.07 11.059 0.176 0.0593 0.0015 0.0904 0.0015 558 9 32.1 570 12 10.799 0.223 0.0609 0.0022 0.0924 0.0020 38.1 640 198 0.31 50.6 0.000182 0.48 10.881 0.117 0.0629 0.0005 0.0915 0.0010 564 6 7.1 571 6 10.796 0.121 0.0595 0.0006 0.0926 0.0011 39.1 513 113 0.22 34.5 0.000020 0.28 12.781 0.143 0.0591 0.0006 0.0780 0.0009 484 5 3.1 571 7 10.767 0.132 0.0615 0.0009 0.0926 0.0012 40.1 637 151 0.24 36.6 - 0.30 14.959 0.165 0.0575 0.0006 0.0666 0.0007 416 5 17.1 573 6 10.755 0.111 0.0600 0.0003 0.0929 0.0010 41.1 202 87 0.43 69.0 0.000010 0.01 2.514 0.029 0.1914 0.0008 0.3977 0.0046 10.490 0.129 0.1913 0.0008 0.936 2159 21 2753 7 22 62.1 573 15 10.699 0.284 0.0634 0.0031 0.0930 0.0025 42.1 62 13 0.21 8.5 0.000040 0.07 6.266 0.096 0.0726 0.0014 0.1595 0.0024 1.584 0.041 0.0721 0.0015 0.596 954 14 988 42 3 4.1 575 6 10.706 0.114 0.0601 0.0004 0.0933 0.0010 43.1 385 175 0.45 28.1 0.000058 0.24 11.777 0.133 0.0598 0.0007 0.0847 0.0010 524 6 16.1 576 7 10.684 0.127 0.0607 0.0015 0.0934 0.0011 44.1 318 230 0.72 20.5 0.000058 0.45 13.300 0.162 0.0600 0.0009 0.0748 0.0009 465 6 14.1 579 6 10.634 0.114 0.0601 0.0005 0.0939 0.0010 45.1 343 221 0.64 25.1 0.000023 0.21 11.737 0.134 0.0596 0.0007 0.0850 0.0010 526 6 36.1 580 6 10.625 0.114 0.0593 0.0005 0.0941 0.0010 46.1 116 111 0.96 8.7 - <0.01 11.554 0.158 0.0576 0.0016 0.0866 0.0012 535 7 6.1 584 6 10.519 0.117 0.0610 0.0008 0.0949 0.0011 47.1 130 131 1.01 15.0 0.000098 0.17 7.423 0.096 0.0719 0.0010 0.1345 0.0017 1.306 0.028 0.0705 0.0012 0.609 813 10 942 34 14 33.1 593 9 10.349 0.160 0.0618 0.0014 0.0964 0.0015 48.1 318 35 0.11 27.1 0.000034 0.04 10.075 0.115 0.0605 0.0006 0.0992 0.0012 610 7 18.1 593 7 10.356 0.120 0.0610 0.0007 0.0964 0.0011 49.1 2038 100 0.05 103.1 0.023750 45.42 16.976 0.177 0.4137 0.0024 0.0321 0.0006 204 4 48.1 610 7 10.075 0.115 0.0605 0.0006 0.0992 0.0012 50.1 412 323 0.78 165.3 0.000007 0.01 2.140 0.023 0.1912 0.0010 0.4672 0.0050 12.308 0.148 0.1911 0.0010 0.897 2471 22 2751 9 10 60.1 616 10 9.951 0.162 0.0617 0.0019 0.1003 0.0017 51.1 117 67 0.57 11.5 0.000115 0.77 8.766 0.118 0.0688 0.0011 0.1132 0.0016 691 9 61.1 618 10 9.917 0.165 0.0625 0.0016 0.1006 0.0017 52.1 397 280 0.71 29.1 0.000050 0.09 11.732 0.131 0.0587 0.0006 0.0852 0.0010 527 6 67.1 629 11 9.697 0.177 0.0659 0.0018 0.1025 0.0019 53.1 42 49 1.18 2.6 - 0.33 13.530 0.282 0.0588 0.0037 0.0737 0.0016 458 10 51.1 691 9 8.766 0.118 0.0688 0.0011 0.1132 0.0016 54.1 685 126 0.18 52.1 0.000030 0.17 11.293 0.121 0.0598 0.0005 0.0884 0.0010 546 6 35.1 720 10 8.445 0.120 0.0645 0.0012 0.1182 0.0017 55.1 139 92 0.67 10.5 0.000098 0.15 11.378 0.151 0.0595 0.0010 0.0878 0.0012 542 7 65.1 728 8 8.315 0.098 0.0680 0.0013 0.1196 0.0015 56.1 254 255 1.00 18.5 0.000123 0.25 11.787 0.140 0.0599 0.0009 0.0846 0.0010 524 6 47.1 813 10 14 7.423 0.096 0.0719 0.0010 1.306 0.028 0.1345 0.0017 0.609 0.0705 0.0012 57.1 602 9 0.02 193.8 0.000009 0.01 2.670 0.028 0.1348 0.0095 0.3745 0.0039 6.954 0.498 0.1347 0.0095 0.147 2051 18 2160 124 5 23.1 863 9 12 6.978 0.077 0.0716 0.0015 1.418 0.033 0.1433 0.0016 0.470 0.0718 0.0015 58.1 197 86 0.44 30.4 0.000099 0.17 5.575 0.066 0.0814 0.0007 0.1791 0.0021 1.976 0.034 0.0800 0.0010 0.684 1062 12 1197 25 11 22.1 870 9 23 6.522 0.069 0.1250 0.0016 1.546 0.055 0.1445 0.0016 0.304 0.0776 0.0026 59.1 36 46 1.26 2.3 0.000552 0.42 13.556 0.286 0.0596 0.0024 0.0735 0.0016 457 10 42.1 954 14 3 6.266 0.096 0.0726 0.0014 1.584 0.041 0.1595 0.0024 0.596 0.0721 0.0015 60.1 60 62 1.04 5.2 0.000155 0.17 9.951 0.162 0.0617 0.0019 0.1003 0.0017 616 10 58.1 1197 25 11 5.575 0.066 0.0814 0.0007 1.976 0.034 0.1791 0.0021 0.684 0.0800 0.0010 61.1 59 31 0.52 5.1 0.000139 0.26 9.917 0.165 0.0625 0.0016 0.1006 0.0017 618 10 19.1 1583 15 16 4.336 0.050 0.0989 0.0007 3.107 0.043 0.2304 0.0026 0.822 0.0978 0.0008 62.1 16 19 1.14 1.3 0.000993 0.52 10.699 0.284 0.0634 0.0031 0.0930 0.0025 573 15 25.1 1955 9 20 3.620 0.039 0.1200 0.0006 4.567 0.054 0.2762 0.0030 0.915 0.1199 0.0006 63.1 237 24 0.10 17.6 - <0.01 11.546 0.140 0.0580 0.0010 0.0866 0.0011 536 6 57.1 2160 124 5 2.670 0.028 0.1348 0.0095 6.954 0.498 0.3745 0.0039 0.147 0.1347 0.0095 64.1 305 129 0.42 20.8 - 0.17 12.589 0.150 0.0584 0.0008 0.0793 0.0010 492 6 5.1 2357 24 1 2.265 0.027 0.1522 0.0044 9.264 0.290 0.4415 0.0053 0.384 0.1522 0.0044 65.1 211 76 0.36 21.8 0.000065 0.54 8.315 0.098 0.0680 0.0013 0.1196 0.0015 728 8 15.1 2670 14 15 2.355 0.028 0.1821 0.0015 10.644 0.154 0.4245 0.0050 0.810 0.1818 0.0015 66.1 500 246 0.49 38.3 0.000029 0.08 11.223 0.123 0.0592 0.0005 0.0890 0.0010 550 6 10.1 2681 10 13 2.301 0.027 0.1832 0.0011 10.968 0.145 0.4345 0.0050 0.880 0.1831 0.0011 67.1 39 44 1.13 3.4 - 0.63 9.697 0.177 0.0659 0.0018 0.1025 0.0019 629 11 50.1 2751 9 10 2.140 0.023 0.1912 0.0010 12.308 0.148 0.4672 0.0050 0.897 0.1911 0.0010 68.1 246 104 0.42 110.7 0.000010 0.01 1.912 0.021 0.1927 0.0006 0.5231 0.0058 13.887 0.161 0.1925 0.0006 0.962 2712 25 2764 5 2 41.1 2753 7 22 2.514 0.029 0.1914 0.0008 10.490 0.129 0.3977 0.0046 0.936 0.1913 0.0008 69.1 71 39 5.4 - 0.15 11.321 0.176 0.0596 0.0015 0.0882 0.0014 545 8 68.1 2764 5 2 1.912 0.021 0.1927 0.0006 13.887 0.161 0.5231 0.0058 0.962 0.1925 0.0006 70.1 74 28 0.38 112.4 0.002657 0.50 11.463 0.177 0.0622 0.0015 0.0868 0.0014 537 8 27.1 2805 9 17 2.309 0.029 0.1974 0.0011 11.789 0.159 0.4330 0.0053 0.917 0.1974 0.0011

Notes : 1. Uncertainties given at the one s level. Notes : 2. Error in Temora reference zircon calibration w as 0.77% for the analytical session. ( not included in above errors but required w hen comparing 206Pb/238U data from different mounts).

Figure 38. Tera-Wasserburg plot for sample 11-5-15, lower Buckley Formation, Mt Bowers.

Table 7: 11-5-22 (upper Buckley Formation)

Table xyz. Summary of SHRIMP U-Pb zircon results for sample 11-5-22, Upper Buckley, Mt. Bowers.

1.1 285 71 0.25 10.1 0.000193 0.23 24.308 0.301 0.0532 0.0010 0.0410 0.0005 259 3 8.1 231 3 27.039 0.402 0.0620 0.0020 0.0365 0.0006 2.1 235 53 0.22 33.7 0.000204 0.35 5.985 0.073 0.0754 0.0023 0.1665 0.0020 1.664 0.059 0.0725 0.0024 0.346 993 11 1000 67 1 6.1 236 3 26.416 0.378 0.0622 0.0016 0.0373 0.0005 3.1 831 163 0.20 58.4 0.002120 3.80 12.220 0.132 0.0920 0.0008 0.0783 0.0009 486 5 4.1 242 4 25.305 0.306 0.0761 0.0077 0.0383 0.0006 4.1 452 359 0.79 15.3 0.000882 3.13 25.305 0.306 0.0761 0.0077 0.0383 0.0006 242 4 30.1 250 3 25.229 0.317 0.0541 0.0010 0.0395 0.0005 5.1 20 25 1.23 0.8 0.004124 4.06 23.096 0.723 0.0840 0.0084 0.0415 0.0014 262 9 43.1 251 3 24.346 0.282 0.0794 0.0036 0.0396 0.0005 6.1 200 110 0.55 6.5 0.000701 1.41 26.416 0.378 0.0622 0.0016 0.0373 0.0005 236 3 44.1 251 9 24.429 0.892 0.0739 0.0057 0.0398 0.0015 7.1 162 62 0.39 6.5 0.003988 7.86 21.464 0.303 0.1147 0.0237 0.0429 0.0015 271 9 51.1 252 3 24.897 0.304 0.0567 0.0010 0.0399 0.0005 8.1 176 115 0.66 5.6 0.001107 1.40 27.039 0.402 0.0620 0.0020 0.0365 0.0006 231 3 32.1 253 3 24.860 0.342 0.0563 0.0013 0.0400 0.0006 9.1 168 44 0.26 12.7 0.001299 1.98 11.328 0.149 0.0742 0.0012 0.0865 0.0012 535 7 46.1 255 3 24.758 0.319 0.0531 0.0011 0.0403 0.0005 10.1 188 67 0.36 6.8 0.000803 0.96 23.888 0.341 0.0591 0.0014 0.0415 0.0006 262 4 47.1 255 6 24.582 0.555 0.0568 0.0028 0.0404 0.0009 11.1 495 213 0.43 18.2 0.000051 0.04 23.369 0.277 0.0519 0.0008 0.0428 0.0005 270 3 25.1 255 3 24.669 0.302 0.0535 0.0009 0.0404 0.0005 12.1 60 62 1.04 2.2 0.001177 0.37 23.165 0.481 0.0546 0.0024 0.0430 0.0009 271 6 18.1 256 3 24.654 0.274 0.0538 0.0006 0.0404 0.0005 13.1 116 49 0.42 31.6 0.000005 0.01 3.142 0.042 0.1103 0.0009 0.3182 0.0043 4.836 0.077 0.1102 0.0009 0.847 1781 21 1803 15 1 36.1 256 3 24.594 0.293 0.0535 0.0014 0.0406 0.0005 14.1 387 197 0.51 14.0 0.000775 1.83 23.695 0.292 0.0661 0.0011 0.0414 0.0005 262 3 49.1 258 23 18.219 0.499 0.2573 0.0513 0.0408 0.0037 15.1 101 69 0.69 3.6 0.000690 0.65 23.830 0.399 0.0567 0.0019 0.0417 0.0007 263 4 57.1 258 3 24.240 0.328 0.0586 0.0013 0.0409 0.0006 16.1 40 31 0.76 1.4 0.001320 0.89 24.035 0.543 0.0586 0.0029 0.0412 0.0010 260 6 19.1 259 4 24.369 0.332 0.0532 0.0012 0.0409 0.0006 17.1 214 121 0.57 7.8 0.000240 <0.01 23.603 0.314 0.0502 0.0011 0.0424 0.0006 268 4 26.1 259 3 24.374 0.261 0.0530 0.0005 0.0409 0.0004 18.1 781 280 0.36 27.2 0.000226 0.31 24.654 0.274 0.0538 0.0006 0.0404 0.0005 256 3 33.1 259 4 24.378 0.410 0.0522 0.0018 0.0410 0.0007 19.1 191 79 0.41 6.7 0.000291 0.22 24.369 0.332 0.0532 0.0012 0.0409 0.0006 259 4 56.1 259 3 24.359 0.318 0.0517 0.0011 0.0410 0.0005 20.1 124 48 0.39 6.2 0.000175 <0.01 17.190 0.251 0.0523 0.0013 0.0583 0.0009 365 5 1.1 259 3 24.308 0.301 0.0532 0.0010 0.0410 0.0005 21.1 97 85 0.87 34.4 0.000071 0.10 2.427 0.033 0.1461 0.0011 0.4116 0.0057 8.241 0.132 0.1452 0.0012 0.861 2222 26 2290 14 3 58.1 259 4 24.127 0.354 0.0591 0.0015 0.0411 0.0006 22.1 78 69 0.89 5.7 0.000624 1.72 11.768 0.198 0.0716 0.0017 0.0835 0.0014 517 9 50.1 259 3 24.345 0.310 0.0517 0.0010 0.0411 0.0005 23.1 78 69 0.88 2.9 0.000301 0.37 22.872 0.429 0.0547 0.0021 0.0436 0.0008 275 5 65.1 259 3 24.295 0.324 0.0532 0.0012 0.0411 0.0006 24.1 152 8 0.06 12.8 0.000142 0.49 10.191 0.135 0.0640 0.0010 0.0976 0.0013 601 8 52.1 260 3 24.387 0.295 0.0495 0.0019 0.0411 0.0005 25.1 360 268 0.74 12.5 0.000038 0.27 24.669 0.302 0.0535 0.0009 0.0404 0.0005 255 3 39.1 260 4 24.106 0.407 0.0586 0.0019 0.0411 0.0007 26.1 1220 425 0.35 43.0 0.000118 0.20 24.374 0.261 0.0530 0.0005 0.0409 0.0004 259 3 16.1 260 6 24.035 0.543 0.0586 0.0029 0.0412 0.0010 27.1 105 62 0.59 5.3 0.000168 <0.01 16.987 0.256 0.0539 0.0014 0.0589 0.0009 369 5 54.1 261 3 24.189 0.319 0.0528 0.0012 0.0413 0.0006 28.1 366 35 0.09 36.3 0.000027 0.05 8.647 0.097 0.0641 0.0020 0.1156 0.0013 705 8 68.1 261 3 24.216 0.317 0.0512 0.0011 0.0413 0.0005 29.1 340 176 0.52 12.2 0.000011 0.20 23.870 0.290 0.0531 0.0009 0.0418 0.0005 264 3 38.1 261 3 24.084 0.291 0.0540 0.0009 0.0414 0.0005 30.1 356 146 0.41 12.1 - 0.37 25.229 0.317 0.0541 0.0010 0.0395 0.0005 250 3 14.1 262 3 23.695 0.292 0.0661 0.0011 0.0414 0.0005 31.1 240 114 0.48 8.5 0.000228 0.07 24.099 0.323 0.0520 0.0012 0.0415 0.0006 262 3 10.1 262 4 23.888 0.341 0.0591 0.0014 0.0415 0.0006 32.1 215 145 0.67 7.4 0.000669 0.63 24.860 0.342 0.0563 0.0013 0.0400 0.0006 253 3 31.1 262 3 24.099 0.323 0.0520 0.0012 0.0415 0.0006 33.1 113 87 0.77 4.0 0.000108 0.09 24.378 0.410 0.0522 0.0018 0.0410 0.0007 259 4 5.1 262 9 23.096 0.723 0.0840 0.0084 0.0415 0.0014 34.1 194 145 0.75 49.7 0.000038 0.06 3.347 0.040 0.1023 0.0007 0.2986 0.0036 4.192 0.060 0.1018 0.0008 0.839 1684 18 1657 15 -2 71.1 263 4 23.838 0.348 0.0576 0.0015 0.0416 0.0006 35.1 278 131 0.47 20.8 0.000517 1.08 11.486 0.138 0.0669 0.0009 0.0861 0.0011 533 6 15.1 263 4 23.830 0.399 0.0567 0.0019 0.0417 0.0007 36.1 478 257 0.54 16.7 0.000210 0.27 24.594 0.293 0.0535 0.0014 0.0406 0.0005 256 3 29.1 264 3 23.870 0.290 0.0531 0.0009 0.0418 0.0005 37.1 188 42 0.22 59.2 0.000042 0.06 2.721 0.033 0.1804 0.0009 0.3673 0.0045 9.107 0.122 0.1799 0.0010 0.913 2016 21 2652 9 24 61.1 266 4 23.713 0.329 0.0531 0.0013 0.0421 0.0006 38.1 455 242 0.53 16.2 0.000216 0.32 24.084 0.291 0.0540 0.0009 0.0414 0.0005 261 3 45.1 267 4 23.579 0.366 0.0553 0.0016 0.0422 0.0007 39.1 113 73 0.65 4.0 0.000128 0.89 24.106 0.407 0.0586 0.0019 0.0411 0.0007 260 4 40.1 267 4 23.615 0.354 0.0524 0.0015 0.0423 0.0006 40.1 151 122 0.81 5.5 - 0.10 23.615 0.354 0.0524 0.0015 0.0423 0.0006 267 4 17.1 268 4 23.603 0.314 0.0502 0.0011 0.0424 0.0006 41.1 276 94 0.34 20.3 0.000034 0.04 11.698 0.142 0.0583 0.0008 0.0854 0.0011 529 6 69.1 269 4 23.479 0.310 0.0523 0.0011 0.0426 0.0006 42.1 434 66 0.15 34.7 0.000016 0.03 10.728 0.121 0.0594 0.0006 0.0932 0.0011 574 6 11.1 270 3 23.369 0.277 0.0519 0.0008 0.0428 0.0005 43.1 495 323 0.65 17.5 0.001914 3.51 24.346 0.282 0.0794 0.0036 0.0396 0.0005 251 3 7.1 271 9 21.464 0.303 0.1147 0.0237 0.0429 0.0015 44.1 14 12 0.86 0.5 0.003511 2.83 24.429 0.892 0.0739 0.0057 0.0398 0.0015 251 9 12.1 271 6 23.165 0.481 0.0546 0.0024 0.0430 0.0009 45.1 132 89 0.67 4.8 0.000333 0.47 23.579 0.366 0.0553 0.0016 0.0422 0.0007 267 4 23.1 275 5 22.872 0.429 0.0547 0.0021 0.0436 0.0008 46.1 324 136 0.42 11.2 0.000357 0.22 24.758 0.319 0.0531 0.0011 0.0403 0.0005 255 3 64.1 278 4 22.671 0.347 0.0516 0.0015 0.0441 0.0007 47.1 55 55 1.00 1.9 0.000376 0.68 24.582 0.555 0.0568 0.0028 0.0404 0.0009 255 6 67.1 291 8 20.397 0.543 0.1000 0.0052 0.0461 0.0013 48.1 46 25 0.54 2.0 - 6.26 20.031 1.937 0.1025 0.0069 0.0468 0.0046 295 28 48.1 295 28 20.031 1.937 0.1025 0.0069 0.0468 0.0046 49.1 24 17 0.72 1.1 0.019798 25.68 18.219 0.499 0.2573 0.0513 0.0408 0.0037 258 23 20.1 365 5 17.190 0.251 0.0523 0.0013 0.0583 0.0009 50.1 349 277 0.80 12.3 0.000206 0.03 24.345 0.310 0.0517 0.0010 0.0411 0.0005 259 3 27.1 369 5 16.987 0.256 0.0539 0.0014 0.0589 0.0009 51.1 434 242 0.56 15.0 0.000283 0.68 24.897 0.304 0.0567 0.0010 0.0399 0.0005 252 3 55.1 384 8 16.218 0.345 0.0576 0.0024 0.0614 0.0013 52.1 494 235 0.47 17.4 0.000042 <0.01 24.387 0.295 0.0495 0.0019 0.0411 0.0005 260 3 70.1 483 6 12.867 0.153 0.0557 0.0007 0.0778 0.0009 53.1 631 133 0.21 109.5 0.000019 0.03 4.950 0.053 0.0790 0.0007 0.2020 0.0022 2.193 0.031 0.0788 0.0007 0.766 1186 12 1166 18 -2 3.1 486 5 12.220 0.132 0.0920 0.0008 0.0783 0.0009 54.1 246 118 0.48 8.8 0.000281 0.17 24.189 0.319 0.0528 0.0012 0.0413 0.0006 261 3 22.1 517 9 11.768 0.198 0.0716 0.0017 0.0835 0.0014 55.1 44 31 0.71 2.3 0.001161 0.40 16.218 0.345 0.0576 0.0024 0.0614 0.0013 384 8 41.1 529 6 11.698 0.142 0.0583 0.0008 0.0854 0.0011 56.1 279 172 0.62 9.9 0.000464 0.03 24.359 0.318 0.0517 0.0011 0.0410 0.0005 259 3 35.1 533 6 11.486 0.138 0.0669 0.0009 0.0861 0.0011 57.1 237 150 0.63 8.4 0.000203 0.91 24.240 0.328 0.0586 0.0013 0.0409 0.0006 258 3 9.1 535 7 11.328 0.149 0.0742 0.0012 0.0865 0.0012 58.1 164 97 0.59 5.8 0.000505 0.95 24.127 0.354 0.0591 0.0015 0.0411 0.0006 259 4 62.1 568 8 10.814 0.155 0.0617 0.0012 0.0922 0.0014 59.1 102 19 0.19 14.2 0.000086 0.15 6.161 0.087 0.0743 0.0011 0.1621 0.0023 1.633 0.037 0.0731 0.0013 0.625 968 13 1017 36 5 66.1 570 6 10.759 0.123 0.0631 0.0007 0.0925 0.0011 60.1 100 129 1.30 15.5 0.000053 0.09 5.532 0.076 0.0762 0.0011 0.1806 0.0025 1.878 0.039 0.0754 0.0012 0.663 1070 14 1080 31 1 42.1 574 6 10.728 0.121 0.0594 0.0006 0.0932 0.0011 61.1 208 281 1.36 7.5 0.000481 0.19 23.713 0.329 0.0531 0.0013 0.0421 0.0006 266 4 72.1 582 16 10.494 0.290 0.0668 0.0033 0.0944 0.0027 62.1 124 83 0.67 9.8 0.000065 0.33 10.814 0.155 0.0617 0.0012 0.0922 0.0014 568 8 63.1 597 11 10.247 0.191 0.0639 0.0019 0.0971 0.0019 63.1 49 5 0.10 4.1 0.000143 0.50 10.247 0.191 0.0639 0.0019 0.0971 0.0019 597 11 24.1 601 8 10.191 0.135 0.0640 0.0010 0.0976 0.0013 64.1 132 53 0.40 5.0 0.000253 <0.01 22.671 0.347 0.0516 0.0015 0.0441 0.0007 278 4 28.1 705 8 8.647 0.097 0.0641 0.0020 0.1156 0.0013 65.1 231 120 0.52 8.2 - 0.23 24.295 0.324 0.0532 0.0012 0.0411 0.0006 259 3 2.1 993 11 1 5.985 0.073 0.0754 0.0023 1.664 0.059 0.1665 0.0020 0.346 0.0725 0.0024 66.1 401 15 0.04 32.1 0.000338 0.50 10.759 0.123 0.0631 0.0007 0.0925 0.0011 570 6 59.1 1017 36 5 6.161 0.087 0.0743 0.0011 1.633 0.037 0.1621 0.0023 0.625 0.0731 0.0013 67.1 35 28 0.79 1.5 0.002493 5.96 20.397 0.543 0.1000 0.0052 0.0461 0.0013 291 8 60.1 1070 14 1 5.532 0.076 0.0762 0.0011 1.878 0.039 0.1806 0.0025 0.663 0.0754 0.0012 68.1 259 120 0.46 9.2 - <0.01 24.216 0.317 0.0512 0.0011 0.0413 0.0005 261 3 53.1 1186 12 -2 4.950 0.053 0.0790 0.0007 2.193 0.031 0.2020 0.0022 0.766 0.0788 0.0007 69.1 244 69 0.28 8.9 0.000098 0.08 23.479 0.310 0.0523 0.0011 0.0426 0.0006 269 4 34.1 1657 15 -2 3.347 0.040 0.1023 0.0007 4.192 0.060 0.2986 0.0036 0.839 0.1018 0.0008 70.1 297 176 0.59 19.8 - <0.01 12.867 0.153 0.0557 0.0007 0.0778 0.0009 483 6 13.1 1803 15 1 3.142 0.042 0.1103 0.0009 4.836 0.077 0.3182 0.0043 0.847 0.1102 0.0009 71.1 152 61 0.40 5.5 - 0.76 23.838 0.348 0.0576 0.0015 0.0416 0.0006 263 4 21.1 2290 14 3 2.427 0.033 0.1461 0.0011 8.241 0.132 0.4116 0.0057 0.861 0.1452 0.0012 72.1 17 5 0.30 1.4 - 0.91 10.494 0.290 0.0668 0.0033 0.0944 0.0027 582 16 37.1 2652 9 24 2.721 0.033 0.1804 0.0009 9.107 0.122 0.3673 0.0045 0.913 0.1799 0.0010

Figure 39. Tera-Wasserburg plot for sample 11-5-22, upper Buckley Formation, Mt Bowers.

Appendix B: Thin Section Descriptions

11-1-1, Mt Achernar Sandstone, fine grained, well sorted. Quartz grains subangular to angular with primarily straight extinction. Polycrystalline quartz rare. Plagioclase (An 30), highly altered. K-feldspar includes microcline with cross-hatch twinning, other compositions minor, highly altered. Accessory minerals include: Highly weathered biotite showing light pleochroism; trace colorless garnet; trace zircon; trace sphene; opaques with red rims; an unknown mineral with high refractive index, second-order birefringence consisting of radiating prismatic crystals in irregular aggregates, possibly an epidote group mineral. Phyllosilicate cement. Secondary brown phyllosilicate forms aggregates and shreds; common zeolite replacement of feldspar grains showing first- order yellow interference and two cleavages at 90 degrees.

11-1-2, Mt Achernar Sandstone, medium to coarse grained, moderately poorly sorted.

Monocrystalline quartz rounded with predominantly undulose extinction and some overgrowth rims. Polycrystalline quartz uncommon. Plagioclase (composition unknown), highly altered. K-feldspar includes microcline with cross-hatch twinning and some grains with perthitic exsolution, other compositions minor, highly altered. Accessory minerals include: Highly weathered biotite showing light pleochroism; trace colorless garnet; trace zircon. Lithic fragments include: porphyritic volcanic fragments with pilotaxitic texture arising from alignment of feldspar laths; tuffaceous fragments showing wavy foliations;

porphyritic volcanic fragments with microphenocrysts of feldspar in a fine groundmass of quartz and feldspar; aphanitic volcanic fragments, consisting of very fine grained crystalline matrix. Phyllosilicate cement. Secondary brown phyllosilicate forms aggregates and shreds; common zeolite replacement of feldspar grains showing first- order yellow interference and two cleavages at 90 degrees.

11-2-1, Tillite Glacier Sandstone, coarse grained, moderately well sorted.

Monocrystalline quartz rounded with predominantly undulose extinction and some overgrowth rims. Polycrystalline quartz common, with shred-like texture. Trace plagioclase, composition unknown. Accessory minerals include: Highly weathered biotite showing light pleochroism; trace pink garnet; trace zircon; opaques with red rims.

Phyllosilicate cement. Secondary brown phyllosilicate forms aggregates and shreds; uncommon carbonate replacement of grains, common zeolite replacement of feldspar grains showing first-order yellow interference.

11-3-2, Tillite Glacier Sandstone, medium grained, moderately well sorted.

Monocrystalline quartz subrounded to subangular with overgrowth rims and both undulose and straight extinction. Polycrystalline quartz rare. Plagioclase (composition unknown), rare. K-feldspar includes microcline with cross-hatch twinning and some grains with perthitic exsolution, other compositions minor, highly altered. Accessory minerals include: Highly weathered biotite showing light pleochroism; trace pink garnet; trace zircon; opaques with red rims. Lithic fragments include: porphyritic volcanic fragments with microphenocrysts of quartz and feldspar in a fine groundmass of quartz

and feldspar; aphanitic volcanic fragments, consisting of very fine grained crystalline matrix. Phyllosilicate cement. Secondary brown phyllosilicate forms aggregates and shreds; common zeolite replacement of feldspar grains showing first-order yellow interference and two cleavages at 90 degrees.

11-3-3, Bunker Cwm Sandstone, medium grained, moderately well sorted.

Monocrystalline quartz subrounded to subangular with both undulose and straight extinction. Polycrystalline quartz rare. Plagioclase (composition unknown), highly altered. K-feldspar includes microcline with cross-hatch twinning and some grains with perthitic exsolution, other compositions minor, highly altered. Accessory minerals include: Highly weathered biotite showing light pleochroism; trace colorless garnet; trace zircon; opaques with red rims. Lithic fragments include: porphyritic volcanic fragments with microphenocrysts of feldspar in a fine groundmass of quartz and feldspar; aphanitic volcanic fragments, consisting of very fine grained crystalline matrix. Matrix is fine- grained quartz and feldspar. Phyllosilicate cement. Secondary brown phyllosilicate forms aggregates and shreds; common zeolite replacement of feldspar grains showing first- order yellow interference and two cleavages at 90 degrees.

11-3-4, Bunker Cwm Sandstone, fine-grained, well sorted. Quartz grains subangular to angular with primarily undulose extinction. Polycrystalline quartz rare. Accessory minerals include: Highly weathered biotite showing light pleochroism; muscovite showing high interference and one good cleavage; garnet with light pink color; trace zircon; trace tourmaline; opaques with red rims. Phyllosilicate cement. Secondary brown

phyllosilicate forms laths and shreds, with stratification shown by alignment of phyllosilicate shreds; secondary white phyllosilicate forms shreds between grains; common carbonate grain replacement; common zeolite replacement of grains showing first-order yellow interference and two cleavages.

11-4-3, Clarkson Peak Sandstone, medium grained, moderately well sorted.

Monocrystalline quartz subrounded to subangular with both undulose and straight extinction. Polycrystalline quartz rare. Plagioclase (composition unknown), highly altered. K-feldspar includes microcline with cross-hatch twinning, other compositions minor, highly altered. Accessory minerals include: Highly weathered biotite showing light pleochroism; trace colorless garnet; trace zircon; trace sphene; opaques with red rims; unknown mineral with low refractive index and first-order interference that forms radiating aggregates. Lithic fragments include: porphyritic volcanic fragments with microphenocrysts of feldspar in a fine groundmass of quartz and feldspar; aphanitic volcanic fragments, consisting of very fine grained crystalline matrix. Matrix is fine- grained quartz and feldspar. Phyllosilicate cement. Secondary brown phyllosilicate forms aggregates and shreds; common carbonate replacement of grains; common zeolite replacement of feldspar grains showing first-order yellow interference and two cleavages at 90 degrees.

11-4-5, Clarkson Peak Sandstone, medium grained, moderately well sorted.

Monocrystalline quartz subrounded to subangular with both undulose and straight extinction and common overgrowth rims. Polycrystalline quartz rare. Plagioclase

100

(composition unkonwn), highly altered. K-feldspar includes microcline with cross-hatch twinning, other compositions minor, highly altered. Accessory minerals include: Highly weathered biotite showing light pleochroism; trace colorless garnet; trace zircon; opaques with red rims; an unknown mineral with high refractive index, second-order birefringence consisting of radiating prismatic crystals in irregular aggregates, possibly an epidote group mineral. Phyllosilicate cement. Secondary brown phyllosilicate forms aggregates and shreds; common zeolite replacement of feldspar grains showing first-order yellow interference and two cleavages at 90 degrees.

11-4-10, Clarkson Peak Sandstone, medium grained, moderately well sorted.

Monocrystalline quartz subrounded to subangular with both undulose and straight extinction. Polycrystalline quartz rare. Plagioclase (composition unknown), highly altered. K-feldspar includes microcline with cross-hatch twinning, other compositions minor, highly altered. Accessory minerals include: Highly weathered biotite showing light pleochroism; trace colorless garnet; trace zircon; trace sphene; opaques with red rims; an unknown mineral with high refractive index, second-order birefringence consisting of radiating prismatic crystals in irregular aggregates, possibly an epidote group mineral. Lithic fragments include: porphyritic volcanic fragments with pilotaxitic texture arising from alignment of feldspar laths; tuffaceous fragments showing wavy foliations; porphyritic volcanic fragments with microphenocrysts of feldspar in a fine groundmass of quartz and feldspar; aphanitic volcanic fragments, consisting of very fine grained crystalline matrix. Phyllosilicate cement. Secondary brown phyllosilicate forms

101

aggregates and shreds; common zeolite replacement of feldspar grains showing first- order yellow interference and two cleavages at 90 degrees.

11-5-2, Mt Bowers Sandstone, medium to coarse grained, moderately poorly sorted.

Monocrystalline quartz subrounded to subangular with both undulose and straight extinction. Polycrystalline quartz rare. Plagioclase (An 32), highly altered. K-feldspar includes microcline with cross-hatch twinning, other compositions minor, highly altered.

Lithic fragments include: porphyritic volcanic fragments with pilotaxitic texture arising from alignment of feldspar laths; porphyritic volcanic fragments with microphenocrysts of feldspar in a fine groundmass of quartz and feldspar; aphanitic volcanic fragments, consisting of very fine grained crystalline matrix. Accessory minerals include: Highly weathered biotite showing light pleochroism; muscovite showing high interference and one good cleavage; garnet with light pink color; trace zircon; opaques with red rims.

Phyllosilicate cement. Secondary brown phyllosilicate forms aggregates and shreds; common zeolite replacement of grains showing first-order yellow interference and two cleavages.

11-5-3, Mt Bowers Sandstone, fine grained, well sorted. Quartz grains subangular to angular with primarily undulose extinction. Plagioclase (An 38), altered. K-feldspar includes microcline with cross-hatch twinning, other compositions minor, altered. Some rare quartz-feldspar intergrowths showing myrmekitic texture. Accessory minerals include: Highly weathered biotite showing light pleochroism; muscovite showing high interference and one good cleavage; common garnet with light pink color; trace zircon;

102

hornblende(?) showing brown pleochroism and first-order red interference; sphene, showing high-order white interference and relief; opaques with dark red rims.

Phyllosilicate cement. Secondary brown phyllosilicate forms shreds and aggregates; common zeolite replacement of grains showing first-order interference and two cleavages.

11-5-4, Mt Bowers Sandstone, fine grained, well sorted. Quartz grains subangular to angular with both undulose and straight extinction. Plagioclase (An 47). K-feldspar includes microcline with cross-hatch twinning, other compositions minor, altered.

Accessory minerals include: Biotite showing brown pleochroism; muscovite showing high interference and one good cleavage; garnet with gray color; trace zircon; trace tourmaline; opaques. Secondary brown phyllosilicate forms shreds and laths; rare zeolite replacement of grains showing first-order interference and two cleavages.

11-5-5, Mt Bowers Sandstone, very fine grained, well sorted. Quartz grains subangular to angular with straight extinction. Plagioclase (composition unknown, grains too small to get reliable estimate). K-feldspar includes microcline with cross-hatch twinning, other compositions minor, highly altered. Accessory minerals include: Highly weathered biotite showing light pleochroism; muscovite showing high interference and one good cleavage; garnet with light pink color; trace zircon; opaques with red rims. Carbonate cement. Secondary alteration gives common carbonate replacement of grains and infilling of veins; secondary brown phyllosilicate in shreds and aggregates.

103

11-5-6, Mt Bowers Sandstone, fine grained, well sorted. Quartz grains subrounded to subangular with straight and undulose extinction. Plagioclase (An 32). K-feldspar includes microcline with cross-hatch twinning, other compositions minor, highly altered.

Accessory minerals include: Altered biotite showing light pleochroism; White mica showing no pleochroism and higher interference; colorless garnet; trace zircon; opaques with dark red rims. Carbonate cement. Secondary alteration gives common carbonate replacement of grains; Secondary brown phyllosilicate in shreds and aggregates; zeolite showing first-order yellow interference colors, possibly laumontite.

11-5-7, Mt Bowers Sandstone, medium grained, well sorted. Quartz grains subangular to angular with straight extinction. Plagioclase (An 35). K-feldspar includes microcline with cross-hatch twinning, other compositions minor, highly altered. Rare quartz-feldspar intergrowths showing myrmekitic texture. Accessory minerals include: Altered biotite showing light pleochroism; White mica showing no pleochroism and higher interference; colorless garnet commonly found in distinct bands; trace zircon commonly found in bands with garnet; opaques with dark red rims. Brown phyllosilicate cement. Secondary carbonate replacement of grains; brown phyllosilicate shreds and laths; zeolite, showing first-order yellow birefringence and two distinct cleavages, possibly laumontite.

11-5-8, Mt Bowers Sandstone, medium grained, well sorted. Monocrystalline quartz grains subrounded to subangular, some nearly euhedral, showing undulose extinction.

Polycrystalline quartz; rare. Plagioclase (An 43); altered. K-feldspar includes microcline with cross-hatch twinning, orthoclase minor; highly altered. Lithic fragments include

104

aphanititc volcanic quartz aggregates with some white phyllosilicate alteration in aligned shreds and porphyritic volcanic fragments with microphenocrysts of quartz in a fine quartzose groundmass. Accessory minerals include: weathered biotite showing light pleochroism; common garnet light gray in color; trace zircon; opaques with red rims.

Carbonate cement. Secondary alteration gives common carbonate replacement of grains;

Secondary brown phyllosilicate in shreds and aggregates; zeolite showing first-order yellow interference colors, possibly laumontite.

11-5-9, Mt Bowers Sandstone, medium grained, moderately well sorted. Monocrystalline quartz subrounded to subangular with both undulose and straight extinction.

Polycrystalline quartz rare. Plagioclase (An 38); altered. K-feldspar including microcline showing cross-hatch twinning, other compositions minor; altered. Accessory minerals include: Highly weathered biotite showing light pleochroism; muscovite showing high interference and one good cleavage; garnet with light pink color; trace zircon; opaques with red rims. White phyllosilicate cement. Secondary alteration leads to common brown phyllosilicate laths and shreds as well as secondary chlorite showing green pleochroism and anomalous blue-gray interference.

11-5-13, Mt Bowers Sandstone, medium grained, well sorted. Monocrystalline quartz subrounded to subangular with both undulose and straight extinction. Polycrystalline quartz common, probably recrystallized. Plagioclase (composition unknown); altered. K- feldspar including microcline showing cross-hatch twinning, other compositions minor; altered. Lithic fragments include aphanititc volcanic quartz aggregates with some white

105

phyllosilicate alteration in aligned shreds and porphyritic volcanic fragments with microphenocrysts of quartz in a fine quartzose groundmass. Accessory minerals include:

Highly weathered biotite showing light pleochroism; muscovite showing high interference and one good cleavage; garnet with light pink color; trace zircon; opaques with red rims. White phyllosilicate cement. Secondary brown phyllosilicate in shreds and aggregates; secondary carbonate replacement of grains; zeolite showing first-order yellow interference colors and 2 distinct cleavages, possibly laumontite.

11-5-14, Mt Bowers Sandstone, medium grained, moderately well sorted.

Monocrystalline quartz subangular to angular with both undulose and straight extinction.

Polycrystalline quartz common, probably recrystallized. Plagioclase (An 32); altered. K- feldspar including microcline showing cross-hatch twinning, other compositions minor; altered. Lithic fragments include aphanititc volcanic quartz aggregates and porphyritic volcanic fragments with microphenocrysts of quartz and feldspar in a fine quartzose groundmass. Accessory minerals include: Highly weathered biotite showing light pleochroism; muscovite showing high interference and one good cleavage; garnet with light pink color; trace zircon; opaques with red rims. White phyllosilicate cement.

Secondary brown phyllosilicate in shreds and aggregates; secondary carbonate replacement of grains; zeolite showing first-order yellow interference colors and 2 distinct cleavages, possibly laumontite.

11-5-15, Mt Bowers Sandstone, medium grained, moderately well sorted.

Monocrystalline quartz rounded to subrounded with both undulose and straight

106

extinction. Polycrystalline quartz rare. Plagioclase (An 28); altered. K-feldspar including microcline showing cross-hatch twinning, other compositions minor; altered. Lithic fragments include aphanititc volcanic quartz aggregates and porphyritic volcanic fragments with microphenocrysts of quartz and feldspar in a fine quartzose groundmass.

Accessory minerals include: biotite in various stages of weathering, showing both dark and light pleochroism; abundant garnet light pink to gray in color; opaques with brown rims, appearing as crystalline aggregates. Carbonate cement. Secondary carbonate replacement of grains very common; secondary brown phyllosilicate alteration; zeolite showing first-order yellow interference colors and 2 distinct cleavages, possibly laumontite.

11-5-16, Mt Bowers Sandstone, medium to coarse grained, moderately poorly sorted.

Monocrystalline quartz rounded to subrounded with both undulose and straight extinction. Plagioclase (An 33); highly altered. K-feldspar including microcline showing cross-hatch twinning, other compositions minor; highly altered. Lithic fragments include aphanititc volcanic quartz aggregates and porphyritic volcanic fragments with microphenocrysts of quartz and feldspar in a fine quartzose groundmass. Accessory minerals include: Highly weathered biotite showing light pleochroism; abundant garnet, some nearly euhedral with light pink color; trace zircon; opaques with red rims.

Phyllosilicate cement. Secondary brown phyllosilicate in shreds and laths; extensive zeolite replacement of grains showing first-order yellow interference colors and 2 distinct cleavages, possibly laumontite.

107

11-5-17, Mt Bowers Sandstone, medium to coarse grained, moderately poorly sorted.

Monocrystalline quartz rounded to subrounded with both undulose and straight extinction. Polycrystalline quartz common. Plagioclase (An 34); altered. K-feldspar including microcline showing cross-hatch twinning, other compositions minor; altered.

Lithic fragments include aphanititc volcanic quartz aggregates and porphyritic volcanic fragments with microphenocrysts of quartz and feldspar in a fine quartzose groundmass.

Some fragments show pilotaxic texture in aligned feldspar laths. Accessory minerals include: Abundant garnet; trace zircon; trace tourmaline(?) showing blue-green pleochroism and high interference colors. Phyllosilicate cement. Secondary brown phyllosilicate in shreds and laths; rare secondary carbonate replacement of grains; extensive zeolite replacement of grains showing first-order yellow interference colors and

2 distinct cleavages, possibly laumontite.

11-5-18, Mt Bowers Sandstone, medium grained, well sorted. Monocrystalline quartz rounded to subangular with both undulose and straight extinction. Polycrystalline quartz common. Plagioclase (An 38); altered. K-feldspar including microcline showing cross- hatch twinning, other compositions minor; altered. Common quartz-feldspar intergrowths showing myrmekitic texture. Lithic fragments include aphanititc volcanic quartz aggregates and porphyritic volcanic fragments with microphenocrysts of quartz and feldspar in a fine quartzose groundmass. Some fragments show pilotaxitic texture in aligned feldspar laths. Accessory minerals include: Highly weathered biotite showing light pleochroism, concentrated in bands with opaques; muscovite showing high interference and one good cleavage; garnet with light pink color; trace zircon; opaques

108

with red rims, concentrated in micaceous bands. Phyllosilicate cement. Secondary brown phyllosilicate in shreds and laths; rare secondary carbonate replacement of grains; extensive zeolite replacement of grains showing first-order yellow interference colors and

2 distinct cleavages, possibly laumontite.

11-5-19, Mt Bowers Sandstone, medium grained, well sorted. Monocrystalline quartz angular with predominantly straight extinction. Plagioclase (An 36); altered. K-feldspar including microcline showing cross-hatch twinning, other compositions minor; altered.

Accessory minerals include: Highly weathered biotite showing light pleochroism; garnet; trace zircon; opaques with red rims. Carbonate cement. Secondary carbonate replacement of grains common; secondary brown phyllosilicate forming shreds; some zeolite grain replacement showing first-order interference.

11-5-21, Mt Bowers Sandstone, medium to coarse grained, moderately poorly sorted.

Monocrystalline quartz rounded with predominantly straight extinction. Polycrystalline quartz common. Plagioclase (An 28); altered. Accessory minerals include: Apatite, showing first-order gray interference and a uniaxial negative figure; weathered biotite showing light pleochroism. Lithic fragments include: porphyritic volcanic fragments with pilotaxitic texture arising from alignment of feldspar laths; pumice fragments with microphenocrysts of feldspar in a very fine grained groundmass; tuffaceous fragments showing wavy foliations; porphyritic volcanic fragments with microphenocrysts of feldspar in a fine groundmass of quartz and feldspar, distinguished from pumice by higher proportion of microphenocrysts to groundmass; aphanitic volcanic fragments,

109

consisting of very fine grained crystalline matrix. Carbonate cement. Secondary carbonate replacement of grains very common; secondary phyllosilicate forms shreds, laths and aggregates, common zeolite grain replacement, showing first-order interference and two cleavages.

11-5-22, Mt Bowers Sandstone, medium to coarse grained, moderately poorly sorted.

Monocrystalline quartz rounded with predominantly straight extinction. Polycrystalline quartz rare. Plagioclase (composition unknown); altered. Accessory minerals include:

Highly weathered biotite showing light pleochroism; muscovite, showing high interference, trace zircon; opaques. Lithic fragments include: porphyritic volcanic fragments with pilotaxitic texture arising from alignment of feldspar laths; tuffaceous fragments showing wavy foliations; porphyritic volcanic fragments with microphenocrysts of feldspar in a fine groundmass of quartz and feldspar; aphanitic volcanic fragments, consisting of very fine grained crystalline matrix; glass shards with trilobal shape and internal structure with aligned grains on outer margins and coarser unaligned grains in inner space. Carbonate cement. Secondary carbonate replacement of grains very common; secondary phyllosilicate forms shreds and aggregates, common zeolite grain replacement, showing first-order interference and two cleavages.

11-5-23, Mt Bowers Sandstone, medium grained, well sorted. Monocrystalline quartz rounded with predominantly straight extinction. Polycrystalline quartz rare. Plagioclase

(composition unknown); altered. Accessory minerals include: Highly weathered biotite showing light pleochroism; muscovite, showing high interference; trace zircon; opaques.

110

Lithic fragments include: porphyritic volcanic fragments with pilotaxitic texture arising from alignment of feldspar laths; porphyritic volcanic fragments with microphenocrysts of feldspar in a fine groundmass of quartz and feldspar; aphanitic volcanic fragments, consisting of very fine grained crystalline matrix. Carbonate cement. Secondary carbonate replacement of grains very common; secondary phyllosilicate forms shreds and aggregates, very common zeolite grain replacement, showing first-order interference and two cleavages.

11-6-1, Lewis Cliffs Sandstone, medium grained, well sorted. Monocrystalline quartz rounded with predominantly straight extinction. Polycrystalline quartz rare. Plagioclase

(An 40) K-feldspar including microcline showing cross-hatch twinning, other compositions minor; altered. Lithic fragments include: porphyritic volcanic fragments with microphenocrysts of feldspar in a fine groundmass of quartz and feldspar, highly altered, an unknown mineral with high refractive index, second-order birefringence consisting of radiating prismatic crystals in irregular aggregates, possibly an epidote group mineral. Accessory minerals include: Highly weathered biotite showing light pleochroism; garnet; trace zircon; opaques with red rims. Secondary carbonate replacement of grains common; secondary phyllosilicate forms shreds, some zeolite grain replacement, showing first-order interference and two cleavages.

11-7-1, Tillite Glacier Sandstone, medium grained, moderately poorly sorted.

Monocrystalline quartz subangular to angular with predominantly straight extinction.

Polycrystalline quartz rare. Brown cement with second-order blue interference and no discernible crystal structure. Secondary brown phyllosilicate in shreds and laths; some

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zeolite replacement of grains showing first-order interference and two cleavages at 90 degrees

11-7-2, Tillite Glacier Sandstone, medium grained, well sorted. Monocrystalline quartz rounded with predominantly straight extinction. Polycrystalline quartz rare. Plagioclase

(Composition unknown) K-feldspar including microcline showing cross-hatch twinning, other compositions minor; altered. Accessory minerals include: Highly weathered biotite showing light pleochroism; trace garnet; trace zircon; opaques with red rims.

Phyllosilicate cement. Secondary brown phyllosilicate in shreds and laths; zeolite replacement of grains showing first-order yellow interference colors and 2 distinct cleavages, possibly laumontite.

11-7-3, Tillite Glacier Sandstone, medium to coarse grained, moderately poorly sorted.

Monocrystalline quartz rounded with predominantly straight extinction. Polycrystalline quartz common, some large grains showing alternation in crystal sizes. Plagioclase

Secondary brown phyllosilicate in shreds and laths; some secondary white mica; extensive zeolite replacement of grains showing first-order yellow interference colors and

2 distinct cleavages, possibly laumontite.

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11-7-4, Tillite Glacier Sandstone, coarse grained, moderately well sorted.

Monocrystalline quartz angular with both straight and undulose extinction, some showing overgrowth rims. Polycrystalline quartz rare. Plagioclase (Composition unknown) K- feldspar including microcline showing cross-hatch twinning, other compositions minor; altered. Accessory minerals include: Highly weathered biotite showing light pleochroism; abundant garnet, some nearly euhedral with light pink color; trace hornblende; trace zircon; trace white mica; opaques with red rims. Lithic fragments include aphanitic volcanic quartz aggregates and porphyritic volcanic fragments with microphenocrysts of quartz and feldspar in a fine quartzose groundmass. Some fragments show pilotaxitic texture in aligned feldspar laths. Phyllosilicate cement. Secondary brown phyllosilicate forms fine aggregates; common zeolite replacement, showing first-order yellow interference and two cleavages.

11-7-5, Tillite Glacier Sandstone, medium grained, well sorted. Monocrystalline quartz angular with both straight and undulose extinction. Polycrystalline quartz common.

Plagioclase (An 34), altered. K-feldspar including microcline showing cross-hatch twinning, other compositions minor; altered. Common quartz-feldspar intergrowths with myrmekitic texture. Accessory minerals include: Muscovite showing high order interference and one good cleavage; common garnet with light pink color; trace zircon; trace sphene. Phyllosilicate cement. Secondary white mica forms radiating laths; brown phyllosilicate forms fine aggregates; common zeolite replacement, showing first-order yellow interference and two cleavages.

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11-7-6, Tillite Glacier Sandstone, medium to coarse grained, well sorted. Monocrystalline quartz rounded with predominantly undulose extinction, showing very common overgrowth rims. Polycrystalline quartz rare. Plagioclase (An 32). Common quartz- feldspar intergrowths with myrmekitic texture. Accessory minerals include: Muscovite showing high order interference and one good cleavage; Minor garnet with light pink color; trace zircon; trace sphene. Phyllosilicate cement. Brown phyllosilicate forms aggregates, some after andalusite retaining euhedral form. Common zeolite replacement, showing first-order yellow interference and two cleavages.

11-8-1, Moore Mountains Sandstone, medium to coarse grained, well sorted.

Monocrystalline quartz rounded with predominantly undulose extinction, showing very common overgrowth rims. Polycrystalline quartz rare. Plagioclase (An 32). K-feldspar including microcline showing cross-hatch twinning, other compositions minor; altered.

Accessory minerals include: Muscovite showing high order interference and one good cleavage; common garnet with light pink color; trace zircon; trace sphene; trace epidote- group mineral, showing green-yellow pleochroism and high interference. Carbonate cement. Secondary white mica forms radiating laths; brown phyllosilicate forms fine aggregates; secondary grain replacement by carbonate rare; common zeolite replacement, showing first-order yellow interference and two cleavages.

11-8-2, Moore Mountains Sandstone, coarse grained, moderately well sorted.

Monocrystalline quartz rounded with predominantly straight extinction, showing common overgrowth rims. Polycrystalline quartz common. Plagioclase (An 34), altered.

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K-feldspar including microcline showing cross-hatch twinning, other compositions minor; altered. Common quartz-feldspar intergrowths with myrmekitic texture. Lithic fragments include: sandstone, fine grained, well sorted with well-rounded quartz, plagioclase and some white mica sorted into layers; sandstone, fine grained, moderately well sorted with quartz and plagioclase in random arrangement. Accessory minerals include: muscovite, showing high interference colors and one good cleavage; garnet with light pink color; trace zircon. Phyllosilicate cement. Secondary white mica forms radiating laths; brown phyllosilicate forms fine aggregates, especially on unsorted sedimentary lithic fragments; common zeolite replacement, showing first-order yellow interference and two cleavages.

11-8-3, Moore Mountains Sandstone, medium grained, well sorted. Monocrystalline quartz angular with both straight and undulose extinction, showing common overgrowth rims. Polycrystalline quartz common. Plagioclase (composition unknown), altered. K- feldspar including microcline showing cross-hatch twinning, other compositions minor; altered. Lithic fragments include: porphyritic volcanic fragments consisting of microphenocrysts of feldspar in a fine grained quartzofeldspathic matrix. Accessory minerals include: muscovite, showing high interference colors and one good cleavage; garnet with light pink color; trace zircon. Phyllosilicate cement. Secondary white mica forms radiating laths; brown phyllosilicate forms fine aggregates; common zeolite replacement, showing first-order yellow interference and two cleavages.

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11-9-1, Mt Weeks Sandstone, coarse grained, very poorly sorted. Monocrystalline quartz angular with both straight and undulose extinction, some showing overgrowth rims.

Polycrystalline quartz common. Plagioclase (composition unknown), altered. Some quartz-feldspar intergrowths showing myrmekitic texture. Lithic fragments include: sandstone, fine grained, well sorted with well-rounded quartz, plagioclase and some white mica. Matrix is fine grained quartz and feldspar. Accessory minerals include: garnet with light pink color; trace zircon. Phyllosilicate cement. Secondary white mica forms radiating laths; brown phyllosilicate forms fine aggregates; common zeolite replacement, showing first-order yellow interference and two cleavages.

11-9-2, Mt Weeks Sandstone, coarse grained, very poorly sorted. Monocrystalline quartz angular with both straight and undulose extinction, some showing overgrowth rims.

Polycrystalline quartz common, some showing stratified texture alternating between coarse and fine grains. Plagioclase (composition unknown), altered. Some quartz-feldspar intergrowths showing myrmekitic texture. Lithic fragments include: sandstone, fine grained, well sorted with well-rounded quartz and plagioclase; sandstone, fine grained, well sorted, with well-rounded quartz, plagioclase and brown phyllosilicate, showing stratification between grain sizes. Matrix is fine grained quartz and feldspar. Accessory minerals include: garnet with light pink color; trace zircon. Phyllosilicate cement.

Secondary brown phyllosilicate forms fine aggregates; common zeolite replacement, showing first-order yellow interference and two cleavages.

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11-9-4, Mt Weeks Sandstone, fine grained, well sorted. Quartz grains subrounded to subangular with straight and undulose extinction. Plagioclase (An 32). Some quartz- feldspar intergrowths showing myrmekitic texture. K-feldspar includes microcline with cross-hatch twinning, other compositions minor, highly altered. Accessory minerals include: Highly weathered biotite showing light pleochroism; white mica; trace colorless garnet; trace zircon; trace sphene; opaques with red rims. Secondary brown phyllosilicate in shreds and laths; rare secondary carbonate replacement of grains; extensive zeolite replacement of grains showing first-order yellow interference colors and 2 distinct cleavages, possibly laumontite.

11-9-5, Mt Weeks Sandstone, medium grained, well sorted. Monocrystalline quartz angular with both straight and undulose extinction. Polycrystalline quartz rare.

Plagioclase (composition unknown), altered. K-feldspar including microcline showing cross-hatch twinning, other compositions minor; altered. Lithic fragments include: porphyritic volcanic fragments consisting of microphenocrysts of feldspar in a fine grained quartzofeldspathic matrix. Accessory minerals include: muscovite, showing high interference colors and one good cleavage; garnet with light pink color; trace zircon.

Phyllosilicate cement. Secondary brown phyllosilicate forms fine aggregates and shreds; common zeolite replacement, showing first-order yellow interference and two cleavages at 90 degrees.

11-11-1, Mt Kirkpatrick Sandstone, fine grained, well sorted. Quartz grains subangular with straight and undulose extinction. Plagioclase (composition unknown). Some quartz-

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feldspar intergrowths showing myrmekitic texture. K-feldspar includes microcline with cross-hatch twinning, other compositions minor, highly altered. Accessory minerals include: Highly weathered biotite showing light pleochroism; trace zircon; trace tourmaline with light green pleochroism; opaques with red rims. Lithic fragments include: porphyritic volcanic fragments with pilotaxitic texture arising from alignment of feldspar laths; porphyritic volcanic fragments with microphenocrysts of feldspar in a fine groundmass of quartz and feldspar; aphanitic volcanic fragments, consisting of very fine grained crystalline matrix. Phyllosilicate cement. Secondary brown phyllosilicate forms fine aggregates and shreds; common zeolite replacement, showing first-order yellow interference and two cleavages at 90 degrees.

11-11-2, Mt Kirkpatrick Sandstone, medium to fine grained, well sorted. Quartz grains subangular with straight and undulose extinction. Polycrystalline quartz common.

Plagioclase (composition unknown). Some quartz-feldspar intergrowths showing myrmekitic texture. K-feldspar includes microcline with cross-hatch twinning, other compositions minor, highly altered. Accessory minerals include: Highly weathered biotite showing light pleochroism; trace zircon; trace sphene; opaques with red rims.

Lithic fragments include: porphyritic volcanic fragments with pilotaxitic texture arising from alignment of feldspar laths; porphyritic volcanic fragments with microphenocrysts of feldspar in a fine groundmass of quartz and feldspar; aphanitic volcanic fragments, consisting of very fine grained crystalline matrix. Phyllosilicate cement. Secondary brown phyllosilicate forms fine aggregates and shreds; secondary chlorite with blue

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pleochroism and anomalous grey interference; common zeolite replacement, showing first-order yellow interference and two cleavages at 90 degrees.

11-11-3, Mt Kirkpatrick Sandstone, medium to fine grained, moderately poorly sorted.

Quartz grains subangular with predominantly straight extinction and common overgrowth rims. Plagioclase (composition unknown). Some quartz-feldspar intergrowths showing myrmekitic texture. K-feldspar includes microcline with cross-hatch twinning, other compositions minor, highly altered. Accessory minerals include: Highly weathered biotite showing light pleochroism; trace zircon; trace sphene; opaques with red rims.

Lithic fragments include: porphyritic volcanic fragments with microphenocrysts of feldspar in a fine groundmass of quartz and feldspar; aphanitic volcanic fragments, consisting of very fine grained crystalline matrix. Phyllosilicate cement. Secondary brown phyllosilicate forms fine aggregates and shreds; common zeolite replacement, showing first-order yellow interference and two cleavages at 90 degrees.

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