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Mantle Xenoliths from the Attawapiskat Kimberlite Field, James Bay Lowlands, Ontario

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Mantle Xenoliths from the Attawapiskat Kimberlite Field, James Bay Lowlands, Ontario MANTLE XENOLITHS FROM THE ATTAWAPISKAT KIMBERLITE FIELD, JAMES BAY LOWLANDS, ONTARIO Kimberley R. Scully A thesis submitted in conformity with the requirements for the degree of Master of Science Graduate Department of Geology University of Toronto 0 Copyright by Kimberley R. ScuiIy, 2000 ubitions and Acquisitions et 38' bgnphio Services sewkes bibliographiques The author has granted a non- L'auteur a accorde une licence non exclusive licence aüowing the exclusive permettant à la National Library of Canada to Bibliothèque nationale du Canada de reproduce, loan, distribute or seil reproduire, prêter, distri'buer ou copies of this thesis in rnicrofonn, vendre des copies de cette thèse sous paper or electronic formats. la forme de microfiche/fih, de reproduction sur papier ou sur format électronique. The author retauis ownership of the L'auteur conserve la propriété du copyright in this thesis. Neither the droit d'auteur qui prottge cette thèse. thesis nor substantial extracts fiom it Ni la thèse ni des extraits substantiels may be printed or otherwise de celle-ci ne doivent être imprim6s reproduced without the author's ou autrement reproduits sans son pamission. autorisation. Mantle XenoUths from the Attawapiskat Kimbcrlite Field, James Bay Lowlands, Ontario Master of Science January 2000 Kimberley R Scully Department of Geology, University of Toronto A chernical investigation of coarse texttued, gamet-bearing peridotite xenoliths and xenocrysts hmthe Attawapiskat kimberlite field was undertaken. The kimberlites occur in the James Bay Lowlands, in the Sachigo subprovince of the Superior Craton. Fragments of coarse textured lhenoiite, harzburgite and eclogite occur as microxenoliths(I 1.5 cmdiameter). Most ofthexenoliths occuras oneortwo phase assemblages (olivine * orthopyroxene, clinopyroxene, gamet, spinel). Gamet-bearing assemblages were investigated for the purposes of geothermobarometry. Calcdated pressures and temperatures of equilibration indicate that gamet hanburgites equilibrated at depths within the diarnond stability field, and gamet lhenolites at depths within the graphite stability field. Al1 the xenoliths equilibrated near a 40rn~rn-~subcratonic steady-state geothermal gradient. Extensive modal metasomatism occurred in the mantle prior to xeno liths being incorporated into the kimberlite magma This rnetasomatism extended to great depths below the Superior Craton in the Attawapiskat region. ACKNOWLEDGEMENTS 1would like to thank Professor Daniel J. Schulze for his guidance and, most importantly, the patience to supervise my studies for two years. Special thanks also to professor's James Brenan and Mike Gorton, rny illustrious cornmittee members; Claudio Cennignani and George Kretschmann for hours of help on the microprobe; George Taylor and Sean McConville for their ultra-quick thin section preparation; Don Boucher, Herman Gruter, and Julie Kong at Monopros Ltd. for discussion; Bruce Jago and Dante Canil for important data; Professon E.T.C. Spooner and Jim Mungall at UofT; The administrative staffat the Department of Geology, University of Toronto and the Earth Sciences Department at Erindale College; and Lon- ann Pizzolato for important (and sometimes even geological!) discussions. Samples of the Attawapiskat kimberlites were provided to Professor Schulze by Monopros Ltd.. Research was performed grants from Lithoprobe and NSERC. Thank you all. Last, but certainly not least, I thank my family and friends - who pmbably didn't understand most of it, but graciously pretended they did. iii TABLE OF CONTENTS Title Page 1 Aclmowledgements iii Table of Contents iv List of Tables vi List of Plates vii .. List of Figures vsll List of Appendices ix CHAPTER 1 - INTRODUCTION 1.1 Introduction 1 1.2 Regional Setting 2 1.2.1 Kimberlite Geology 8 1.2.1.1 Kimberlite 8 1.2.1.2 Xenoliths 11 1.3 Previous Work 12 1.4 Methodology 13 1 .4.1 Sample Preparation 13 1.4.2 Mineral Chernical Analysis 13 CHAPTER 2 - PETROGRAPHY 2.1 Introduction 15 2.2 Attawapiskat Xenoliths 17 2.2.1 Metasomatic Minenls 19 CHAPTER 3 - MINERAL CHEMISTRY 3 .1 Introduction 25 3.2 Detailed Mineral Chemistry 25 3 1.1 Heavy Mineral Separates 25 32.1.1 Gamet 26 3 3.1.2 Clinopyroxene 35 3 21.3 Orthopyroxene 38 3.2.1.4 Chromite 38 3.2.2 Xenoliths: Primary and MetasomatidSecondary Assemblages-43 3 5.2.1 Primary Minerais: Olivine 43 3.2.2.2 Gamet 45 3.2.2.3 Clinopymxeae 48 3.2.2.4 Orthopyroxene 49 3.2.3 Metasomatic Minerais 49 3.2.3.1 Amphibole 51 3.2.3.2 Phiogopite 51 3.2.3.3 Clinopyroxene 53 3.2.3.4 Chromite 53 CHAPTER 4: THERMOBAROMETRY 4.1 Introduction 60 4.1.1 Geothermometers and Barometers 60 4.1.2 Required Conditions for Equilibnum Estimates 61 4.1.3 The Attawapiskat Mantle Xenolith Suite 62 4.2 Olivine-Gamet Thennometry, Enstatite-Gamet Barometry 63 4.3 Pressure - Temperature Results 66 4.4 Thermometry Results 69 4.4.1 Townfor coarse Gamet Peridoti tes 69 4.4.2 Ni-in-gamet Geothemorneter 71 4.4.3 Cornparkon of TOw79 and TNi 73 4.5 Deformed Lherzolites 74 CHAPTER 5: DISCUSSION 5.1 Introduction 78 5.2 Mineral Chemistry 78 5.3 Geothermobammetry 79 5.3.1 Pressure - Temperature Result s 79 5.3.2 Temperature Results 80 5.3.3 The Attawapiskat P - T "Gap" 8 1 5.4 Metasomatism 8 1 5.5 Deformed Peridotites 83 5.6 Diamond Potential 84 CHAPTER 6: CONCLUSIONS 6.1 The Attawapiskat Mantle Xenolith Suite 85 REFERENCES 86 LIST OF TABLES CHAPTER 2: PETROGWHY Table 2- 1 24 CHAPTER 4: GEOTHERMOBAROMETRY Table 4-1 77 LIST OF PLATES Plate 1 18 Plate 2 18 Plate 3 20 Plate 4 20 Plate 5 22 Plate 6 22 vii LIST OF FiGURES CHAPTER 1: Introduction Figure 1-1 3 Figure 1-2 4 Figure 1-3 5 Figure 1-4 9 CHAPTER 2: PETRQGRAPHY Figure 2-1 16 CHAPTER 3: MINERAL CHEMISTRY Figure 3- 1 27 Figure 3-2 28 Figure 3-3 29 Figure 3-4 31 Figure 3-5 32 Figure 3-6 33 Figure 3-7 34 Figure 3-8 36 Figure 3-9 37 Figure 3-10 39 Fi- 3-1 1 40 Figure 3-12 41 Figure 3-13 42 Figure 3-14 44 Figure 3-15 46 Figure 3- 16 47 Figure 3-1 7 50 Figure 3-1 8 52 Figure 3-19 54 Figure 3-20 56 Figure 3-21 57 Figure 3-22 58 CHAPTER 4: GEOTHERMOBAROMETRY Figure 4-1 68 Figure 4-2 70 Figure 4-3 72 Figure 4-4 75 LIST OF APPENDICES Appendix A: Electron Microprobe Standards and Operations Specifications 93 Appendix B: Mineral Analyses 94 Olivine ftom xenoliths 95 Gamet hmxenoliths 98 ûrthopyroxene hmxenoliths 1 03 Clinopyroxene fkom xenoliths 104 Metasomatic Clinopymxene 1 04 Amphiiole fkom xenoliths 105 Phlogopite fiom xenoliths 1 06 Chromite fkom xenoliths 107 Gamets fiom "Al" concenûate IO8 Gamets fiom "G" concentrate 115 Gamets fiom "V" concentrate 119 Clinopyroxenes nom "V" concentrate 122 Orthopyroxenes fiom "V" concentrate 124 Chmites fiom "V" concentrate 125 LA-ICP-MS for 14 gamets from "Cr' concentrate 128 CEAPTER 1: INTRODUCTION 1.1 Introduction The Earth's made constitutes approximately two thirds of the planet, and yet it remaias largely inaccessible to dctailed study. Geophysical investigations reveal cornplex heterogeneities in the mantle. Geophysical data cannot, however, reveal the chernical processes that take place there to create the observed heterogeneities. Direct chemical analysis of the mantle is possible through analysis ofxenoliths of mantle material (spinel and gamet-bearing peridotites, eclogite, and rare dunite), brought to the surface by kimberlite and certain other alkaline volcanic rocks. Kimberlites are ultrapotassic, volatile-rich magmas which originate at depths greater than 200 km below the surface of the Earth, below thick, cool Archean craton roots (Mitchell, 1986). As they rise towards the surface. kimberlites entrain fragments of the mantle through which they pass. These fragments provide petrologists with small pieces of the mantle rocks, and as such act as "windows" to the maritle below. The cool peridotitic roots of Archean cratons have been identified as the source region for diamonds recovered fiom kimberlites and lampmites (Mitchell, 1986). Academic and economic interest in understanding the way diamonds form in their source region bas sthulated studies of mantle xenoliths recovered from kimberlite pipes. Many rnantle xenoliths are recovered hmactive diamond mines. Diamond exploration and mining companies study xenolith chemistry to help design exploration programs specific to the miderock-îypes sampled by kimberlites in an effort to target the most lucrative prospects. Discovcries of kimberlite pipes and diamonds in Canada during the last two decades have provided opportunities to examine several new suites of mantle xenoliths, aüowing research into the mantle below the Canadian Shield, the wotlds largest Archean craton (Card and Ciesielski, 1986). The Attawapiskat kimberlite field, in the Supenor Province of the Canadian Shield, in northem Ontario, was discovered by Monopros Ltd. in 1984. This study is an investigation of the chemistry of minerals fiom xenoliths recovered from exploration drill core nom the Attawapiskat kimberlites. The data have been used to constrain the composition of the mantle below the western Superior craton, determine the subcratonic geothemal gradient at Attawapiskat, and to qualiQ modal metasomatim in the source region. 1.2 Regional Settlng The Attawapiskat kimberlite field is located approximately 120 km west of James Bay on the Attawapiskat River in Northem Ontario (Figures 1- 1 to 1-3). There are 18 kimberlite pipes in the Attawapiskat cluster. Sixteen of the pipes are owned by Monopros Ltd.. The remaining two pipes, MacFadyen 01 and 02, ore owned by KWG- Spider Resowes. The pipes lie within the James Bay Lowlands physiographic region, an area of dense muskeg swamp and stunted spruce forests on the southem limit of pennafhst (Johnson et al., 1991; Figure 1-2).
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