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

Syn-ore Chl 7 chlorite in breccia-type U 4 mineralization yields the relatively highest Fe contents of 25.78 weight percent (Table 3.3; Fig. 3.6C) and high Fe/(Fe+Mg) ratios of 0.53, indicating that the U-bearing fluid was Fe-rich. The average Fe/(Mg+Fe) ratio is similar to values reported by Tortosa (1983) for Fe-chlorite associated with the mineralized zone at the Cenex mine. Chl 7 chlorite has a composition typical for chamosite corresponding to formation temperatures near 330°C (Table 3.3). Cal 8 calcite and U 4 uraninite intergrowths with Chl 7 chlorite in conjunction with high F contents in Chl 7 chlorite, suggest that the U-bearing fluid contained Ca and F (Table 3.3; Figs..3.6A and 3.6B). Electron microprobe and backscattered images show that Chl 7 chlorite was subsequently altered by fluids that were Mg-rich. These altered chlorites have average formation temperatures near 195 o C (Table 3.4). Syn-ore Chl 8 chlorite in volcanic-type U 5 mineralization is an Mg-Fe-chlorite with a formation temperature of ca. 320°C (Table 3.3). Chl 8 chlorite has the highest Mn and Ti contents (Table 3.3; Figs. 3.6A and 3.6B), although the presence of Ti and Ca reflects Ttn 3 titanite and Ap 1 apatite grains respectively, intergrown with Chl 8 chlorite and U 5 uraninite (Fig. 3.4I). Chl 8 chlorites were subsequently altered by later Mg-rich fluids, resulting in altered chlorites with formation temperatures near 210 o C (Table 3.4). Chl 9 chlorite associated with the Athabasca-type U 6 mineralization has high Mg and Fe contents (15.43 wt.% and 26.01 wt.%, respectively) and is typically F-Cl-rich (Table 3.3; Figs. 3.6A and 3.6B), with formation temperatures of ca. 235°C (Table 3.3). The Fe/(Fe+Mg) ratio of Chl 9 chlorite ranges from 0.56 to 0.67 and indicates that the U-mineralizing fluid was likely Mg-rich. 103
Sample ID 1 ± 2 ± 3.a ± 4 ± 5.a ± 5.a ± 5.a ± 6 ± n= 5 5 5 15 8 9 8 10 Oxides (Wt %) SiO2 30.25 0.66 27.56 2.23 26.84 0.31 25.34 1.21 26.07 0.46 26.66 0.39 26.10 0.48 28.38 0.92 TiO2 0.00 - 0.00 - 0.06 0.02 0.02 - 0.02 - 0.01 - 0.09 0.03 0.02 - AL2O3 14.85 0.94 21.94 3.15 19.41 0.29 19.88 1.44 18.41 0.48 19.12 0.81 18.79 0.47 15.40 0.47 CR2O3 0.02 - 0.05 - 0.00 - 0.10 - 0.02 - 0.03 - 0.01 - 0.17 0.07 FeO 19.45 0.49 14.17 1.94 20.58 0.34 25.78 4.82 28.50 0.95 23.05 2.90 25.65 0.68 26.01 3.08 MnO 0.11 0.03 0.15 0.07 0.38 0.06 0.08 0.07 0.22 0.17 0.51 0.14 0.24 0.05 0.01 - MgO 19.74 0.85 17.03 2.56 18.17 0.38 12.60 2.26 13.18 0.63 16.60 1.39 15.13 0.30 15.43 2.05 CaO 0.15 0.09 3.47 5.00 0.01 - 0.85 1.12 0.01 - 0.02 - 0.02 - 0.08 - NA2O 0.01 - 0.28 0.17 0.02 - 0.04 - 0.01 - 0.02 - 0.03 - 0.05 - K2O 0.01 - 0.31 0.35 0.01 - 0.01 - 0.03 - 0.01 - 0.03 - 0.01 - F 0.45 0.11 0.40 0.36 0.26 0.06 0.17 0.10 0.08 0.05 0.10 0.08 0.18 0.06 0.38 0.20 CL 0.00 - 0.13 0.05 0.00 - 0.01 - 0.00 - 0.00 - 0.01 - 0.04 - H2O 11.16 0.18 11.39 11.25 0.12 10.89 0.44 10.97 0.14 11.23 0.14 11.03 0.03 10.87 0.27 O=F -0.19 - -0.17 - -0.11 - -0.02 - -0.03 - -0.04 - -0.07 - -0.16 - O=CL 0.00 - -0.03 - 0.00 - -0.01 - 0.00 - 0.00 - 0.00 - -0.01 - Total 96.01 1.35 97.08 3.21 96.88 0.91 95.66 5.07 97.48 0.95 97.31 0.64 97.22 0.51 96.94 1.95 Atomic proportion Number of O 28 28 28 28 28 28 28 28 Tetrahedral sites Si 4+ 3.19 0.04 2.85 0.06 2.83 0.02 2.79 0.05 2.84 0.03 2.83 0.02 2.81 0.05 3.08 0.08 AL 4+ 0.81 0.04 1.16 0.06 1.17 0.02 1.21 0.05 1.16 0.03 1.17 0.02 1.19 0.05 0.92 0.08 Total 4.00 4.00 4.00 4.00 4.00 4.00 4.00 4.00 Octahedral sites AL 6+ 1.85 0.11 2.66 0.24 2.41 0.04 2.57 0.08 2.36 0.05 2.40 0.09 2.39 0.06 1.97 0.06 Ti 4+ 0.00 - 0.00 - 0.01 - 0.00 - 0.00 - 0.00 - 0.01 - 0.00 - Cr 3+ 0.00 - 0.00 - 0.00 - 0.01 - 0.00 - 0.00 - 0.00 - 0.01 - Fe 2+ 1.72 0.06 1.22 0.21 1.82 0.03 2.37 0.42 2.60 0.11 2.05 0.29 2.31 0.06 2.36 0.31 Mn 2+ 0.01 - 0.01 - 0.03 0.00 0.01 - 0.02 - 0.05 - 0.02 - 0.00 - Mg 2+ 3.10 0.10 2.62 0.29 2.86 0.05 2.06 0.35 2.14 0.08 2.63 0.01 2.43 0.05 2.49 0.30 Total 6.68 0.04 6.52 0.57 7.12 0.03 7.03 0.16 7.13 0.05 7.13 0.04 7.16 0.07 6.84 0.15 Interlayers sites Ca 2+ 0.02 - 0.40 0.59 0.00 - 0.10 0.13 0.00 - 0.00 - 0.00 - 0.01 - Na + 0.00 - 0.06 0.04 0.00 - 0.02 - 0.00 - 0.00 - 0.01 - 0.01 - K + 0.00 - 0.04 0.04 0.00 - 0.00 - 0.00 - 0.00 - 0.00 - 0.00 - Total 0.02 - 0.50 0.66 0.01 - 0.12 0.07 0.01 - 0.01 - 0.01 - 0.02 Anions F - 0.15 0.04 0.14 0.12 0.09 0.02 0.06 0.03 0.03 0.02 0.03 0.03 0.06 0.02 0.13 0.07 CL - 0.00 - 0.02 - 0.00 - 0.00 - 0.00 - 0.00 - 0.00 - 0.01 - H + 7.85 0.04 7.84 0.12 7.91 0.02 7.94 0.05 7.97 0.02 7.97 0.03 7.94 0.02 7.86 0.07 Total 8.00 0.00 8.00 0.00 8.00 0.00 8.00 0.00 8.00 0.00 8.00 0.00 8.00 0.00 8.00 0.00 O 2- 17.85 0.04 17.84 0.12 17.92 0.02 17.98 0.05 17.97 0.02 17.97 0.03 17.94 0.02 17.86 0.07 ∑Cat 9.89 0.02 9.87 0.19 9.96 0.02 9.93 0.05 9.98 0.02 9.97 0.04 9.99 0.02 9.94 0.07 ∑ions 18.00 0.00 18.00 0.00 18.00 0.02 18.00 0.00 18.00 0.00 18.00 0.00 18.00 0.00 18.00 0.00 Temperatures ( o C) 200 14 310 20 315 6 330 16 311 9 313 7 338 16 235 24 Table 3.3. Representative electron microprobe analysis of different generations of syn-ore chlorite phases from U deposits in the Beaverlodge area, including formation temperatures calculated using the method of Cathelineau (1988). 1=Retrograde metamorphic Chl 1 ; 2=Chl 4 in early tensional vein type U 2 mineralization; 3a=Chl 5 in metasomatic-type U 3 mineralization at Gunnar; 4=Chl 7 in breccia-type main U 4 mineralization; 5a=Chl 8 in volcanic-type U 5 mineralization; 6=Chl 9 in Athabasca-type U 5 mineralization. One sigma variations are also shown. Paragenesis of all phases analyzed is shown in Figures 3 and 4 (see the text for more details). n= number of analyses 104
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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
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eplaces Kfs 1 feldspars (Fig. 2.7A)
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the Qtz 1 quartz dissolution result
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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 and 114: Figure 3.4. Photomicrographs of typ
Page 115 and 116: 3.4J). Py 6 Pyrite and Cpy 5 chalco
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: Fig. 3.6A). The Ca may result from
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
Page 165 and 166: No corrections were made to the 238
Page 167 and 168: which was interpreted as being asso
Page 169 and 170: porphyry and coated by Chl 1 formin
Page 171 and 172: 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
Page 241 and 242:
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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Page 263 and 264:
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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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Page 287 and 288:
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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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