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

ferruginous siltstone of the Koolpin Formation (Ayres et al., 1975). The U mineralization is accompanied by minor amount of galena, chalcopyrite, pyrite, native gold, and clausthatite (Ayres et al., 1975). The syn-ore alteration is characterized by muscovite-chlorite ±hematite±kaolinite±biotite (Wyborn, 1992; Mernagh and Wyborn, 1994). 1.3. Uranium mineralized systems in the Athabasca and Kombolgie basins Uranium deposits in the Athabasca and Kombolgie basins are major sources of high grade U ore (McGill et al., 1993; Bruneton, 1987). These deposits consist of massive pods, veins and disseminations of uraninite spatially associated with unconformities between basement Paleoproterozoic metasedimentary and Archean to Paleoproterozoic granitoid rocks and overlying relatively flat-lying, late Paleoproterozoic siliciclastic fluvial red-bed strata (Hoeve and Sibbald, 1978; Hoeve and Quirt, 1984; Wallis et al., 1986; Sibbald and Quirt, 1987). The uranium deposits can be hosted in structures in the basement (ingress type, Fig. 1.3) or in the overlying siliciclastic strata and paleo-weathered basement rocks (egress type, Fig. 1.3) at the unconformity (Hoeve et al., 1984; Sibbald, 1985; Fayek and Kyser, 1997). The ore-forming fluids originate either from the overlying sandstone (e.g. Kotzer et al., 1995; Polito et al., 2005; Cuney and Kyser, 2008) or the underlying basement (e.g. Cuney et al., 2005). These deposits are associated with alteration zones around the mineralization (Hoeve et al., 1984; Quirt, 2003). In basement-hosted deposits, illitization is predominant in the distal alteration zone from the U mineralization, and chloritization is the typical alteration in the proximal zone (e.g. Wilde, 1989; 1992; Kotzer et al., 1995; Polito et al., 11
2005). U mineralization is controlled by structures that have been reactivated, which are favorable sites for fluid circulation (Schultz, 1991; Tourigny, 2002). Fracture-Controlled Mobilized U Mineralization (Perched) Lake U Mineralization at unconformity (Basin-hosted) Unconformity Pelitic Gneiss Vein & Breccia U mineralization basement-hosted Pelitic Gneiss Granitic Gneiss Graphitic Pelitic Gneiss Arkosic Gneiss Quartzite Figure 1.3. Genetic model for unconformity-type U deposit (modified from Cuney and Kyser, 2008). Unconformity-type U deposits in the Athabasca and Kombolgie basins formed at ca. 1600 Ma and 1675 Ma, respectively, (Alexandre et al., 2006; Polito et al., 2012). Temperatures were 200 o C and involved the interaction of oxidizing, saline basinal fluids carrying U 6+ with either reducing basement rock types (basement-hosted, Fig. 1.3) or reducing fluids from the basement (sediment-hosted, Fig. 1.3), thereby precipitating U 4+ at the unconformity (e.g. Hoeve and Quirt, 1984; Kotzer and Kyser, 1995; Cuney et al., 2005). Unconformity-type U deposits in the Athabasca and Kombolgie basins have produced up to 35% of the world U production (e.g. Ruzicka, 1996; Ghandi, 2007), 12
Page 1 and 2: FLUID EVOLUTION AND STRUCTURAL CONT
Page 3 and 4: Abstract Uranium deposits associate
Page 5 and 6: Co-Authorship This thesis and the m
Page 7 and 8: Sarah Rice and Jonathan Cloutier, a
Page 9 and 10: TABLE OF CONTENTS Abstract………
Page 11 and 12: 2.5.2. Temporal relationships of fa
Page 13 and 14: 4.5.3. Isotopic compositions of min
Page 15 and 16: List of Figures Figure 1.1. General
Page 17 and 18: Figure 4.16. Distribution of 207 Pb
Page 19 and 20: Table 4.4. Isotopic data of the U-P
Page 21 and 22: processes by which these deposits f
Page 23 and 24: Figure 1.1. Generalized geological
Page 25 and 26: which is the equivalent of the Mill
Page 27 and 28: dolostone and carbonaceous shale (L
Page 29: Mineral Field (Figure 1.2). Many de
Page 33 and 34: Figure 1.4. Schematic representatio
Page 35 and 36: In particular, the key issues to be
Page 37 and 38: genetic model for the U mineralizat
Page 39 and 40: fourth and most significant uranium
Page 41 and 42: The Beaverlodge area is part of the
Page 43 and 44: 1998; Hartlaub and Ashton, 1998). R
Page 45 and 46: (D 1 ) produced a regional migmatit
Page 47 and 48: These previous age models do not ta
Page 49 and 50: the age when the concentrations of
Page 51 and 52: Figure 2.3. A: Detailed geologic ma
Page 53 and 54: hornblende-feldspar gneiss showing
Page 55 and 56: east-west striking en-échelon quar
Page 57 and 58: and broken Kfs 1 and Qtz 1 embedded
Page 59 and 60: A Meters LEGEND B Figure 2.6. A: De
Page 62 and 63: 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
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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
Page 111 and 112:
are derived from their chlorite cry
Page 113 and 114:
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
Page 131 and 132:
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
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decompression and hydration reactio
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mineralizations, which upgraded the
Page 145 and 146:
metamorphic origin of the main U 4
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y the abundance of Ap 1 apatite and
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of late fluid events that have affe
Page 151 and 152:
CHAPTER 4 FLUID EVOLUTION AND GENES
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1990, 1991; Wyborn et al., 1990). H
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stable isotope geochemistry, U-Pb g
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coincident with the initiation of s
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plasma mass spectrometry (LA-HR-ICP
Page 161 and 162:
The Coronation Hill deposit occupie
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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 ( ±
Page 189 and 190:
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
Page 207 and 208:
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
Page 219 and 220:
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
Page 225 and 226:
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
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
Page 245 and 246:
Kyser, K., and Cuney, M., 2008. Geo
Page 247 and 248:
two-sided oblique-slip collisional
Page 249 and 250:
Creek Geosyncline: in ‘The minera
Page 251 and 252:
Piper, J.D.A., 2004. Discussion on
Page 253 and 254:
99.Sheppard SMF and Gilg HA 1996. S
Page 255 and 256:
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
Page 261 and 262:
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
Page 271 and 272:
SAMPLE ID. SiO 2 TiO 2 AL 2O 3 CR 2
Page 273 and 274:
SAMPLE ID. SiO 2 TiO 2 AL 2O 3 CR 2
Page 275 and 276:
APPENDIX E Electron microprobe data
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SAMPLE Si 4+ AL 4+ Total AL 6+ Ti 4
Page 279 and 280:
SAMPLE Si 4+ AL 4+ Total AL 6+ Ti 4
Page 281 and 282:
Sample ID. Deposit UO 2 SiO 2 CaO F
Page 283 and 284:
Sample ID. Deposit UO 2 SiO 2 CaO F
Page 285 and 286:
Page 287 and 288:
Page 289 and 290:
Sample ID. Al 2O 3 CaO FeO K2O MgO
Page 291 and 292:
Sample ID. Al 2O 3 CaO FeO K2O MgO
Page 293 and 294:
250 85 330 40 145 70 25 65 30 30 27
Page 295 and 296:
Mineralized veins Quartz veins 276
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