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

C29-217APPr 295.26 13.37 43.50 1.34 0.15 0.005 139 2.11 0.36 0.28 C29-217APPr1 246.05 19.17 39.12 1.72 0.16 0.006 140 1.97 0.21 0.09 C29-217APPq 242.05 24.61 38.84 5.90 0.16 0.009 143 18.50 0.02 0.01 C29-217APPp 195.35 1.13 32.74 0.53 0.17 0.000 154 2.72 0.02 0.01 C29-217APPo 224.24 53.26 38.51 12.99 0.17 0.021 157 61.47 0.02 0.02 C29-217APPm 236.15 7.59 38.67 1.01 0.16 0.005 139 2.80 0.19 0.11 C29-217APPk 211.22 9.58 36.70 2.11 0.17 0.003 142 7.34 0.07 0.04 C29-217APPh 644.46 57.38 81.54 10.87 0.13 0.006 116 15.61 0.07 0.00 C29-217APPg 187.96 16.40 34.21 3.95 0.18 0.009 145 22.67 0.02 0.01 C29-217APPf 247.09 18.16 40.02 4.70 0.16 0.007 145 16.59 0.01 0.00 C29-217APPd 233.28 9.80 38.43 2.41 0.16 0.006 139 7.35 0.08 0.05 Table 4.6. Isotopic analyses data of the Pb-Pb LA-HR-ICP-MS analysis of galena from the Coronation Hill deposit. Result of the age model is shown in Figure 4.12A. 4.5.4.3. Chemical Pb age of the uranium mineralization The chemical Pb age is derived from the assumption that the total Pb present in the sample is of radiogenic origin, resulting exclusively from the decay of U and Th and that the mineral has not lost or acquired Pb since it formed (Bowles, 1990). Different Chemical Pb ages in the same grain reflect variable alteration by subsequent fluids during recrystallization of the uraninite to new uranium minerals, resulting in a decrease in the Chemical Pb age and an increase in elements other than uranium. As alteration is expected to result in a decrease in radiogenic Pb contents, the formation age of the uraninite can be estimated by extrapolating the Chemical Pb ages to when the concentrations of the secondary elements (e.g. Ca, Fe and Si) were negligible (e.g. Alexandre and Kyser, 2005). Chemical Pb ages derived from the composition of U 1 uraninite vary from 341 Ma to 1479 Ma (Table 4.1), suggesting variable recrystallization, Pb loss, and gain of elements that make up new uranium alteration phases. Regression of the SiO 2 +Fe 2 O 3 +CaO+MnO contents to zero in U 1 uraninite corresponds to 1822 Ma (Fig. 4.14), which is within error identical to the U-Pb upper intercept dates of 1823±140 Ma and 1819±150 Ma (Figs. 4.12A 173
and 4.12B), and to 207 Pb/ 206 Pb ages of 1810±15 Ma and 1825±90 Ma (Figs. 4.12B and 4.12C). Chemical Pb ages (Ma) Figure 4.14. Plot of element contents in uraninite as a function of chemical Pb ages. 4.6. Discussion Paragenetic minerals and geochronologic data from the Coronation Hill and El Sherana deposits indicate that basement rocks of the Koolpin Formation and the overlying El Sherana Basin sandstones have been affected by multistage deformation and fluid events, including early stages of basement metamorphism and basin diagenesis followed by hydrothermal alteration and U mineralization and post-ore alteration (Fig. 4.15, Table 4.7). Alteration assemblage Pre-ore Stage Diagenesis Ore Stage Post-ore stage Src 1 -Chl 1 -Hem 1 - Qtz 1 Kln1 -Hem 2 -Qtz 2 U 1 -Au 1 -Gn 1 -Chl 4 - Cal 4 -Hem 4 U 2 -Chl 5 -Cal 5 -Hem 5 Age of formation 1860 – 1840 Ma 1830 – 1820 Ma 1820 Ma Post 1820 Ma 174
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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
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Volcanic-type ±U 5 (Sample 6139, G
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6134 pt8a 2 Gunnar 82.92 2.92 5.30
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Regression to zero content of the s
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faults (Fig. 2.13C). The breccias w
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Figure 2.13. Schematic cross-sectio
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Mylonites were then reactivated at
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and thrusting during the 1.94-1.92
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Beaverlodge area (Morelli et al., 2
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dikes (Ernst and Buchan, 2001b) and
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Figure 2.15: Distribution of 207 Pb
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CHAPTER 3 GENESIS OF MULTIFARIOUS U
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eccia-type. The other styles of min
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The basement consist of Neoarchean
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of essentially unmetamorphosed arko
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WDX X-ray spectrometers at Carleton
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3.4. Results 3.4.1. Paragenesis of
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are derived from their chlorite cry
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Figure 3.4. Photomicrographs of typ
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3.4J). Py 6 Pyrite and Cpy 5 chalco
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mineralization varies from 25.70 to
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6137APt71 60.67 13.73 4.59 6.48 0.0
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Fig. 3.6A). The Ca may result from
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Sample ID 1 ± 2 ± 3.a ± 4 ± 5.a
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Stable isotopic O and C composition
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Sample ID Deposit Mineral Mineral v
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equilibrium with a fluid having δ
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Syn-ore Chl 8 chlorite sampled from
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Figure 3.9. Binary diagrams showing
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Figure 3.10. Chondrite-normalized R
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Retrograde metamorphism Early vein
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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
Page 181 and 182: Sample I.D SiO 2 CaO FeO ThO 2 MnO
Page 183 and 184: site occupancy (Cathelineau, 1988).
Page 185 and 186: Mineral values Temperature Fluid va
Page 187 and 188: Corrected ratios Apparent ages ( ±
Page 189 and 190: G H Figure 4.12. U-Pb concordia dia
Page 191: Figure 4.13. Pb-Pb isochron diagram
Page 195 and 196: 160 o C at Coronation Hill. The tem
Page 197 and 198: Figure 4.15. Conceptual genetic mod
Page 199 and 200: of the Koolpin Formation, while dep
Page 201 and 202: at ca. 1820 Ma, approximately 40 My
Page 203 and 204: culminating with the formation of R
Page 205 and 206: deposits is related to fluids deriv
Page 207 and 208: CHAPTER 5 GENERAL DISCUSSION 5.1. I
Page 209 and 210: ed-bed strata and associated volcan
Page 211 and 212: character of the fluid that formed
Page 213 and 214: 5.2.1.2. Metamorphic-related uraniu
Page 215 and 216: during brecciation or reduction as
Page 217 and 218: ca. 1820 Ma that triggered reactiva
Page 219 and 220: Plutons Event at 1.4 Ga (Barinek et
Page 221 and 222: Kolari-Kittila Province Kuusamo Pro
Page 223 and 224: The uranium deposits in various pro
Page 225 and 226: Fig. 5.6. Distribution of the Rorai
Page 227 and 228: Roraima Basin, similar to what is o
Page 229 and 230: etween ca. 2.3 Ga and 1.9 Ga. Later
Page 231 and 232: REFERENCES Adams, J., 1989. Postgla
Page 233 and 234: Ashton, K.E., 2010. The Gunnar Mine
Page 235 and 236: Bowles, J.F.W., 1990. Age dating of
Page 237 and 238: Cuney, M.L., 2005. World-class unco
Page 239 and 240: deposits in the Athabasca Basin, Sa
Page 241 and 242: Hartlaub, R.P., Heaman, L.M., Chack
Page 243 and 244:
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:
Page 265 and 266:
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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Corrected ratios Apparent ages ( ±
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Corrected ratios Apparent ages ( ±
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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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