Proposed Title 1: - Queen's University
Proposed Title 1: - Queen's University Proposed Title 1: - Queen's University
calculated δ 18 O fluid and δ 13 C fluid values of the fluid from which Cal 9 formed range from 4.7 per mil to 15.7 per mil and -4.9 per mil to -3.1 per mil, respectively (Fig. 3.7; Table 3.5), with most of the δ 18 O fluid values between 5 per mil and 10 per mil. Syn-ore Cal 10 calcite from the Athabasca-type U 6 mineralization yields δ 18 O values of 11.2 per mil and δ 13 C values ranging from -1 per mil to -0.9 per mil (Table 3.5). Using a formation temperature of ca. 235°C (Table 3.3), the calculated δ 18 O fluid and δ 13 C fluid values of the fluid are 3.3 per mil and -1.9 per mil, respectively (Fig. 3.7; Table 3.5). Late Cal 11 calcite veins crosscutting all rocks within the Beaverlodge area have δ 18 O values that range from 12.8 per mil to 14.7 per mil and δ 13 C values between -6.4 per mil and -2.5 per mil (Fig. 3.7; Table 3.5). Using a formation temperature of 140°C, the calculated δ 18 O fluid and δ 13 C fluid values are the lowest and give two components (Fig. 3.7). One has δ 18 O fluid and δ 13 C fluid values ranging from -0.6 per mil to 1.2 per mil and -0.9 per mil to -0.5 per mil, respectively, similar to isotopic compositions of seawater (Fig. 3.7). The second component has much lower δ 13 C fluid and slightly higher δ 18 O fluid values, near -4.5 per mil and 0 per mil, respectively. 3.4.3.2. Oxygen and hydrogen isotopic compositions of chlorite Stable isotopic O and H compositions were determined for chlorite in textural equilibrium with U for the granite-metasomatic, breccia, volcanic, and Athabasca-type U mineralizations (Fig. 3.8; Table 3.6). Syn-ore Chl 5 chlorite in the Gunnar deposit has δ 18 O values that range from 5.8 per mil to 11.1 per mil and δ 2 H values between -75 per mil and -71 per mil (Fig. 3.8; Table 3.6). Assuming a formation temperature of 315°C (Table 3.3), Chl 5 chlorite formed in 109
equilibrium with a fluid having δ 18 O fluid values ranging from 6.1 per mil to 11.4 per mil and δ 2 H fluid values from -48 per mil to -44 per mil (Fig. 3.8; Table 3.6). Figure 3.8. Calculated δ 18 O and δ 2 H values of mineralizing fluids in equilibrium with chlorite minerals. Samples of breccia and Gunnar-type have preferentially exchanged H-isotopes with 2 H-depleted, relatively modern meteoric water; their high δ 18 O values indicate alteration at low fluid/rock ratios. The fields of various fluid reservoirs participating in hydrothermal ore formation are also shown (e.g. Taylor, 1974; Faure, 1989; Cuney and Kyser, 2008). Syn-ore Chl 7 chlorite in the breccia-type U 4 uraninite has a wide range of δ 18 O values varying between 8.6 per mil and 17.1 per mil and δ 2 H values from -86 per mil to - 131 per mil (Table 3.6). The δ 18 O values are the highest compared to other types of mineralization. Using a formation temperature of 330°C (Table 3.3), the calculated δ 18 O fluid and δ 2 H fluid values for the fluid that formed Chl 7 chlorite range from 8.2 per mil to 110
- 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 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: Sample ID Deposit Mineral Mineral v
- 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
- 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
equilibrium with a fluid having δ 18 O fluid values ranging from 6.1 per mil to 11.4 per mil<br />
and δ 2 H fluid values from -48 per mil to -44 per mil (Fig. 3.8; Table 3.6).<br />
Figure 3.8. Calculated δ 18 O and δ 2 H values of mineralizing fluids in equilibrium with chlorite<br />
minerals. Samples of breccia and Gunnar-type have preferentially exchanged H-isotopes with<br />
2 H-depleted, relatively modern meteoric water; their high δ 18 O values indicate alteration at<br />
low fluid/rock ratios. The fields of various fluid reservoirs participating in hydrothermal ore<br />
formation are also shown (e.g. Taylor, 1974; Faure, 1989; Cuney and Kyser, 2008).<br />
Syn-ore Chl 7 chlorite in the breccia-type U 4 uraninite has a wide range of δ 18 O<br />
values varying between 8.6 per mil and 17.1 per mil and δ 2 H values from -86 per mil to -<br />
131 per mil (Table 3.6). The δ 18 O values are the highest compared to other types of<br />
mineralization. Using a formation temperature of 330°C (Table 3.3), the calculated<br />
δ 18 O fluid and δ 2 H fluid values for the fluid that formed Chl 7 chlorite range from 8.2 per mil to<br />
110
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