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

16.6 per mil and -103 per mil to-59 per mil, respectively (Fig. 3.8; Table 3.6). The lowest δ 2 H fluid values likely reflect the influence of modern meteoric water with which Chl 7 chlorite has reacted (Wilson and Kyser, 1987; Kyser and Kerrick, 1991). Sample ID Deposits Metasomatic-type U3 mineralization Mineral values Temperature Fluid values δ 18 O V-SMOW per mil δ 2 H V-SMOW per mil o C δ 18 O fluid V-SMOW per mil δ 2 H fluid V-SMOW per mil GN-06 Gunnar 9.2 -75 315 9.4 -48 GN-06B Gunnar 7.9 -71 315 8.1 -44 GN-36 Gunnar 5.8 -75 315 6.1 -48 GN-01 Gunnar 11.1 -71 315 11.4 -44 Breccia-type U4 mineralization 5810 Ace-Fay 8.6 -90 330 8.2 -63 5812 Ace-Fay 17.1 -104 330 16.6 -77 5812-Dup Ace-Fay 17.1 -104 330 16.6 -77 VR Ace-Fay 15 -108 330 14.6 -81 VR-2 Ace-Fay 14.2 -88 330 13.8 -61 CL47 Cinch Lake 15.4 -99 330 14.9 -72 6124 Cinch Lake 13.3 -130 330 12.8 -103 C-09-21 Cinch Lake 12.5 -86 330 12.1 -59 C-09-21S Cinch Lake 12.5 -99 330 12.1 -72 C-37-128 Cinch Lake 9.9 -109 330 9.5 -82 Volcanic-type U5 mineralization CL Cinch Lake 10.4 -126 320 10.2 -99 CL-19 Cinch Lake 9.2 -101 320 9 -74 CL-19S Cinch Lake 9.2 -113 320 9 -86 CL-25 Cinch Lake 6.8 -104 320 6.6 -77 CL-25B Cinch Lake 8.9 -94 320 8.7 -67 CL-48 Cinch Lake 6.4 -71 320 6.2 -44 CL-48b Cinch Lake 7.3 -75 320 7.1 -48 CL-49 Cinch Lake 7.3 -99 320 7.1 -72 CL-55 Cinch Lake 7.3 -79 320 7.1 -52 CL-55S Cinch Lake 7.3 -93 320 7.1 -66 CL-64 Cinch Lake 6 -82 320 5.8 -55 Cl-64B Cinch Lake 10.4 -97 320 10.2 -70 F19-08 Ace-Fay 6.9 -100 320 7.1 -73 F230-30 Ace-Fay 8.3 -72 320 8.5 -45 F230-24 Ace-Fay 9.2 -79 320 9.4 -52 F19-09 Ace-Fay 9.3 -98 320 9.5 -71 Athabasca-type U6 mineralization F230-14a Ace-Fay 3.5 -67 235 2.2 -40 F230-14b Ace-Fay 2.8 -65 235 1.5 -38 F230-14c Ace-Fay 5.2 -71 235 3.8 -44 F230-25 Ace-Fay 3.5 -63 235 2.2 -36 F230-25 Dup Ace-Fay 3.5 -68 235 2.2 -41 F230-46 Ace-Fay 7.7 -87 235 6.3 -60 F230-31 Ace-Fay 4.1 -68 235 2.8 -41 Table 3.6. Measured δ 18 O and δ 2 H for chlorite and calculated δ 18 O and δ 2 H values for fluids in equilibrium with chlorite minerals from different generations of U mineralizing events in the Beaverlodge area. Temperatures used to calculate the fluid values are derived from the chlorite chemistry (see Table 3.3). 111
Syn-ore Chl 8 chlorite sampled from the volcanic-type U 6 mineralization has a narrow range of δ 18 O values between 6 per mil and 10.4 per mil and a wide range of δ 2 H values comprising between -126 per mil and -71 per mil (Table 3.6). Using a formation temperature of 320°C (Table 3.3), δ 18 O fluid and δ 2 H fluid values for the equilibrium fluid range from 5.8 per mil to 10.2 per mil and -99 per mil to -44 per mil, respectively (Fig. 3.8; Table 3.6). Chl 8 chlorite also records late alteration associated with the influence of modern meteoric water (Fig. 3.8). In contrast, Syn-ore Chl 9 chlorite in Athabasca-type U 6 mineralization has the lowest δ 18 O values that range from 2.8 per mil to 7.7 per mil and δ 2 H values comprising between -87 per mil and -63 per mil (Table 3.6). These values indicate formation in equilibrium with brines having δ 18 O fluid values of 1.5 per mil to 6.3 per mil and δ 2 H fluid values of -60 per mil to -38 per mil based on a formation temperature of 235°C (Fig. 3.8; Table 3.6). The calculated values of δ 18 O fluid and δ 2 H fluid are similar to those from unconformity-type U mineralization in the proximal Athabasca Basin (Wilson and Kyser, 1987; Kotzer and Kyser, 1995). 3.4.4. Rare earth elements (REE) geochemical characteristics of the U mineralization REE contents of uraninite can constrain the origin and evolution of mineralizing fluids (Alexander et al., 2010; Mercadier et al., 2011). Based on REE patterns, several distinctions can be made between different types of U-mineralizing events. For example, the REE contents in the granite-related metasomatic-type U 3 uraninite at Gunnar are high (17834 ppm, Tables 3.7 and 3.8; Fig. 3.9B) and chondrite-normalized REE patterns indicate a slight LREE enrichment (La/Yb) N =5.8, Figs. 3.9A and 3.10A) and pronounced negative Eu and Ce anomalies (Eu/Eu*=0.1 and Ce/Ce*=0.1, Fig. 3.10A). In contrast, U 2 112
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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
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uraninite (Fig. 2.10). The errors o
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Figure 2.10. Backscattered Electron
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post-mineralization alteration duri
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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 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: equilibrium with a fluid having δ
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
Page 173 and 174: SOUTH ALLIGATOR RIVER GROUP EL SHER
Page 175 and 176: A Carbonaceous Shale B Src 1 Qtz 1
Page 177 and 178: A Granite Qtz 0 fragments Qtz 0 B M
Page 179 and 180: 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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