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

associated with cataclasite rocks. Hydraulic fracturing in response to fluid generation via decompression and hydration reactions was probably the mechanism of the early tensional ±U2 veins formation. D: 2.0-1.9: 1.94-1.92 Ga peak metamorphism of the Taltson-Thelon Orogen produced a regional migmatitic foliation (S1) and tight to isoclinal folds of early S1 fabric. 1.91-1.90 Ga metamorphic event of the Snowbird Tectonic Zone produced an overprinting northeast-striking regional fabric associated with tight to isoclinal folds. E: 1850 Ma: U4-rich brecciation of pre-existing rocks along reactivated faults during regional metamorphism of the Trans-Hudson Orogen or most likely post-peak compressional uplift during terminal collision of the Taltson-Thelon Orogen. F: 1820 Ma: Formation of the successor Martin Lake Basin, which developed along lines of pre-existing tectonic weakness during late stage of the Trans-Hudson Orogen. The Martin Lake Basin is associated with extrusion of mantle-affinity alkaline to sub-alkaline mafic dikes around 1818±4 Ma. The volcanic-type ±U5 is spatially associated with the mafic dikes. G: 1620 Ma: Deposition of the Athabasca Basin at ca. 1750 Ma and formation of Athabasca-related ±U6 veins coincident with the age of the unconformity-related U-mineralizing event in the Athabasca Basin that records tectonic reactivation during the 1.65-1.60 Ga Mazatzal Orogen. H: Late alteration events: From the Mesoproterozoic to recent time, far field tectonic events of several orogenic episodes during the thermotectonic evolution of the Laurentian plate caused minor brittle fault reactivation in the Beaverlodge area. 2.5.2. Temporal relationships of fault activities and uranium mineralization to regional tectonic events The oldest observed deformation event corresponds to mylonitization with obliquenormal and dextral sense of shearing in the ductile environment at amphibolite facies metamorphism (Fig. 2.13B). Mylonitization along these faults likely occurred during the Arrowsmith Orogen at ca. 2.33 Ga (Berman, 2005; Hartlaub et al., 2007), concomitant with initial deposition of the Murmac Bay Group sediments. Metamorphic retrogression took place during exhumation to shallower crustal depths, resulting in greenschist facies conditions, probably subsequent to a period of tectonic quiescence and regional erosion. 69
Mylonites were then reactivated at shallower structural levels where brittle-ductile fracturing under hydrated conditions associated with cataclasite faulting became the dominant failure process (Fig. 2.13C). The formation age of the cataclasite ±U 1 and early tensional veins-type ±U 2 mineralization, suggests that these two mineralizing events were coeval and their timing is consistent with fault reactivation during late stage Arrowsmith Orogen that affected the Beaverlodge area (Fig. 2.13C). Post-orogenic exhumation and erosion may have led to the development of fluid-related features (Miller et al., 2002) as deformation occurred under hydrated conditions in the ductile-brittle environment. Hydraulic tensile fracturing in response to fluid generation via decompression and hydration reactions (Miller and Cartwright, 2006) was probably the mechanism of the early tensional ±U 2 -veins formation. The vein-forming fluid was likely driven into these fractures by suction pump processes (Sibson, 1987). Interaction between the hydrothermal brine and the metamorphic host rocks likely promoted the deposition of the ±U 2 uranium mineralization and the Cal 2 -Hem 3 -Chl 3 - Src 2 -Cpy 2 -Py 2 mineral assemblage (Fig. 2.8). The 207 Pb/ 206 Pb system of U 1 and U 2 uraninites displays five groups of ages reflecting post-mineralization alteration by later fluid events that are related to fault reactivation (Fig. 2.15). The intervals 2.2-2.1 Ga and 2.1-2.0 Ga correspond to a period of global extension and rifting related to the protracted breakup of the Kenorland supercontinent (Williams et al., 1991; LeCheminant et al., 1997) (Fig. 2.15). For example, the 2.2-2.1 Ga mafic swarms in the Slave, Churchill, Superior and Nain provinces (LeCheminant et al., 1996; Bleeker et al., 2007) and the 2.2-2.0 Ga intrusive complexes in the Slave province (Buchan and Ernst, 70
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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
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
Page 85 and 86: faults (Fig. 2.13C). The breccias w
Page 87: Figure 2.13. Schematic cross-sectio
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 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
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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
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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
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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
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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 ( ±
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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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