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$Fayek & Kyser 2000 uraninite fractionations.pdf - Queen's University$

tensional mode I vein of Qtz 3 and Cal 3 . D: Reflected light photomicrograph of U 2 replacing Py 3 in vein. E: Transmitted light photomicrograph of mineralized albite-metasomatized granite showing U 3 associated with Hem 5 and Ttn 2 in void left after Cal 5 and Qtz 1 dissolution. F: Reflected light photomicrograph of mineralized albite-metasomatized granite. G: Transmitted light photomicrograph of mineralized breccia with albitized fragments of cataclasite rock in Cal 8 matrix. U 4 rims breccia fragments and disseminated in Cal 8 matrix associated with Chl 7 , and Hem 6 . H: Reflected light photomicrograph of a highly U- mineralized breccia. U 4 with Cal 8 and Chl 7 forming the matrix. I: Transmitted light photomicrograph of breccia vein composed of crushed Qtz 1 , Kfs 1 and Cal 1 embedded in a chlorite-rich matrix. U 5 is disseminated in the matrix associated with Hem 7 , Chl 8 and Ap 1 . J: Reflected light photomicrograph of breccia vein. K: Transmitted light photomicrograph of late mineralized veins containing U 6 , Chl 9 and Hem 8 . L: Reflected light photomicrograph of the late mineralized veins. Locally, U 4 uraninite displays a colloform texture with concentric banding indicating effects of late fluid alteration events. Chl 7 chlorite generally forms radiating aggregates enveloping U 4 uraninite. The size and texture of Chl 7 chlorite indicate growth into open pore spaces that were possibly created by brittle deformation. U 4 is associated with Src 3 sericite, Hem 6 hematite, Py 5 pyrite, and Cpy 4 chalcopyrite. In places, U 4 replaces Py 4 pyrite. U 5 uranium mineralization associated with mafic dikes occurs as veinlets or millimetric to metric breccia-dikes crosscutting the shear zone at Cinch Lake (Dieng et al., 2011). Field observations indicate a spatial relationship between breccia-dikes and mafic dikes. Breccia-dikes are composed of angular country rock fragments, Qtz 1 quartz, Kfs 1 feldspar and Cal 1 calcite grains embedded in a chlorite matrix (Fig. 3.4I). U 5 occurs as disseminated grains cementing altered fragments (Fig. 3.4J) and is intergrown with Chl 8 chlorite, Cal 9 calcite, Src 4 sericite, Hem 7 hematite, Mzn 2 monazite, and Ttn 3 titanite (Fig. 95
3.4J). Py 6 Pyrite and Cpy 5 chalcopyrite are disseminated in the matrix. Ap 1 apatite as tabular crystals is intergrown with U 5 (Fig. 3.4J). Athabasca-type U mineralization fills late fractures and consists of U 6 uraninite associated with Cal 10 calcite, Chl 9 chlorite, Hem 8 hematite, and minor Py 7 pyrite (Fig. 3.4L). These late veins (Fig. 3.4K) crosscut the Murmac Bay Group, the basal conglomerates of the Martin Lake Group and the mafic dikes and are the youngest mineralized phase. U 6 uraninite is typically massive and generally rims Cal 10 calcite veins. Late veins of Cal 11 calcite, Chl 10 chlorite, Qtz 5 quartz and sulfide occur as fracture-filling minerals cutting primary ore assemblages. The sulfides are Gn 1 galena, Cpy 6 chalcopyrite, Py 8 pyrite, Sph 1 sphalerite, and copper minerals. Gn 1 galena forms inclusions or fracturefilling in uraninite and Py 8 pyrite or thin films along Cal 8 calcite cleavage in the breccia rock. Sph 1 sphalerite occurs as irregular masses or fine blebs in Py 8 pyrite. Copper mineralization is present as disseminated aggregates of Bn 1 bornite, Dg 1 digenite, and Cv 1 covellite at the Ace-Fay and Gunnar deposits and appears to postdate the main event of U mineralization. 3.4.2. Crystal Chemistry 3.4.2.1. Mineral chemistry of uraninite and brannerite Electron microprobe and backscattered images reveal that uraninite from all stages of mineralization has been variably altered to different forms of uranyl-silicates (Table 3.1, Fig. 3.5). These uraninites demonstrate evidence of considerable variation in reflectance, suggesting significant heterogeneity in their chemical composition as a result of variable alteration by later fluids (Kotzer and Kyser, 1993; Alexandre et al., 2005). 96
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FLUID EVOLUTION AND STRUCTURAL CONT
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Abstract Uranium deposits associate
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Co-Authorship This thesis and the m
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Sarah Rice and Jonathan Cloutier, a
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TABLE OF CONTENTS Abstract………
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2.5.2. Temporal relationships of fa
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4.5.3. Isotopic compositions of min
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List of Figures Figure 1.1. General
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Figure 4.16. Distribution of 207 Pb
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Table 4.4. Isotopic data of the U-P
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processes by which these deposits f
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Figure 1.1. Generalized geological
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which is the equivalent of the Mill
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dolostone and carbonaceous shale (L
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Mineral Field (Figure 1.2). Many de
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2005). U mineralization is controll
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Figure 1.4. Schematic representatio
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In particular, the key issues to be
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genetic model for the U mineralizat
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fourth and most significant uranium
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The Beaverlodge area is part of the
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1998; Hartlaub and Ashton, 1998). R
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(D 1 ) produced a regional migmatit
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These previous age models do not ta
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the age when the concentrations of
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Figure 2.3. A: Detailed geologic ma
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hornblende-feldspar gneiss showing
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east-west striking en-échelon quar
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and broken Kfs 1 and Qtz 1 embedded
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A Meters LEGEND B Figure 2.6. A: De
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Figure 2.7. Microphotograph of vari
Page 64: eplaces Kfs 1 feldspars (Fig. 2.7A)
Page 67 and 68: the Qtz 1 quartz dissolution result
Page 69 and 70: Figure 2.9. Microphotograph of typi
Page 71 and 72: uraninite (Fig. 2.10). The errors o
Page 73 and 74: Figure 2.10. Backscattered Electron
Page 75 and 76: post-mineralization alteration duri
Page 77 and 78: Post-mineralization alteration even
Page 79 and 80: Volcanic-type ±U 5 (Sample 6139, G
Page 81 and 82: 6134 pt8a 2 Gunnar 82.92 2.92 5.30
Page 83 and 84: Regression to zero content of the s
Page 85 and 86: faults (Fig. 2.13C). The breccias w
Page 87 and 88: Figure 2.13. Schematic cross-sectio
Page 89 and 90: Mylonites were then reactivated at
Page 91 and 92: and thrusting during the 1.94-1.92
Page 93 and 94: Beaverlodge area (Morelli et al., 2
Page 95 and 96: dikes (Ernst and Buchan, 2001b) and
Page 97 and 98: Figure 2.15: Distribution of 207 Pb
Page 99 and 100: CHAPTER 3 GENESIS OF MULTIFARIOUS U
Page 101 and 102: eccia-type. The other styles of min
Page 103 and 104: The basement consist of Neoarchean
Page 105 and 106: of essentially unmetamorphosed arko
Page 107 and 108: WDX X-ray spectrometers at Carleton
Page 109 and 110: 3.4. Results 3.4.1. Paragenesis of
Page 111 and 112: are derived from their chlorite cry
Page 113: Figure 3.4. Photomicrographs of typ
Page 117 and 118: mineralization varies from 25.70 to
Page 119 and 120: 6137APt71 60.67 13.73 4.59 6.48 0.0
Page 121 and 122: Fig. 3.6A). The Ca may result from
Page 123 and 124: Sample ID 1 ± 2 ± 3.a ± 4 ± 5.a
Page 125 and 126: Stable isotopic O and C composition
Page 127 and 128: Sample ID Deposit Mineral Mineral v
Page 129 and 130: equilibrium with a fluid having δ
Page 131 and 132: Syn-ore Chl 8 chlorite sampled from
Page 133 and 134: Figure 3.9. Binary diagrams showing
Page 135 and 136: Figure 3.10. Chondrite-normalized R
Page 137 and 138: Retrograde metamorphism Early vein
Page 139 and 140: contents in syn-ore Chl 4 chlorite
Page 141 and 142: decompression and hydration reactio
Page 143 and 144: mineralizations, which upgraded the
Page 145 and 146: metamorphic origin of the main U 4
Page 147 and 148: y the abundance of Ap 1 apatite and
Page 149 and 150: of late fluid events that have affe
Page 151 and 152: CHAPTER 4 FLUID EVOLUTION AND GENES
Page 153 and 154: 1990, 1991; Wyborn et al., 1990). H
Page 155 and 156: stable isotope geochemistry, U-Pb g
Page 157 and 158: coincident with the initiation of s
Page 159 and 160: plasma mass spectrometry (LA-HR-ICP
Page 161 and 162: The Coronation Hill deposit occupie
Page 163 and 164: arsenides, nickel selenide and copp
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No corrections were made to the 238
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which was interpreted as being asso
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porphyry and coated by Chl 1 formin
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Mineralized breccias showing quartz
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SOUTH ALLIGATOR RIVER GROUP EL SHER
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A Carbonaceous Shale B Src 1 Qtz 1
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A Granite Qtz 0 fragments Qtz 0 B M
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chemical composition as a result of
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Sample I.D SiO 2 CaO FeO ThO 2 MnO
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site occupancy (Cathelineau, 1988).
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Mineral values Temperature Fluid va
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Corrected ratios Apparent ages ( ±
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G H Figure 4.12. U-Pb concordia dia
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Figure 4.13. Pb-Pb isochron diagram
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and 4.12B), and to 207 Pb/ 206 Pb a
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160 o C at Coronation Hill. The tem
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Figure 4.15. Conceptual genetic mod
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of the Koolpin Formation, while dep
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at ca. 1820 Ma, approximately 40 My
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culminating with the formation of R
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deposits is related to fluids deriv
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CHAPTER 5 GENERAL DISCUSSION 5.1. I
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ed-bed strata and associated volcan
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character of the fluid that formed
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5.2.1.2. Metamorphic-related uraniu
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during brecciation or reduction as
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ca. 1820 Ma that triggered reactiva
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Plutons Event at 1.4 Ga (Barinek et
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Kolari-Kittila Province Kuusamo Pro
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The uranium deposits in various pro
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Fig. 5.6. Distribution of the Rorai
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Roraima Basin, similar to what is o
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etween ca. 2.3 Ga and 1.9 Ga. Later
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REFERENCES Adams, J., 1989. Postgla
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Ashton, K.E., 2010. The Gunnar Mine
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Bowles, J.F.W., 1990. Age dating of
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Cuney, M.L., 2005. World-class unco
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deposits in the Athabasca Basin, Sa
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Hartlaub, R.P., Heaman, L.M., Chack
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Saskatchewan Geological Survey, Sas
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Kyser, K., and Cuney, M., 2008. Geo
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two-sided oblique-slip collisional
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Creek Geosyncline: in ‘The minera
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Piper, J.D.A., 2004. Discussion on
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99.Sheppard SMF and Gilg HA 1996. S
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Proceedings Darwin Conference 1984
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Wingate, M.T.D, Pisarevsky SA, Evan
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Sample Deposit 207 Pb/ 206 Pb ±2σ
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APPENDIX B REE contents of various
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Sample Y Zr Cs Ba Th La Ce Pr Nd Sm
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Sample ΣREE TLREE THREE LREE/HREE
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SAMPLE ID. SiO 2 TiO 2 AL 2O 3 CR 2
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SAMPLE ID. SiO 2 TiO 2 AL 2O 3 CR 2
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APPENDIX E Electron microprobe data
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SAMPLE Si 4+ AL 4+ Total AL 6+ Ti 4
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SAMPLE Si 4+ AL 4+ Total AL 6+ Ti 4
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Sample ID. Deposit UO 2 SiO 2 CaO F
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Sample ID. Deposit UO 2 SiO 2 CaO F
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Sample ID. Al 2O 3 CaO FeO K2O MgO
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Sample ID. Al 2O 3 CaO FeO K2O MgO
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250 85 330 40 145 70 25 65 30 30 27
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Mineralized veins Quartz veins 276
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