Proposed Title 1: - Queen's University
Proposed Title 1: - Queen's University Proposed Title 1: - Queen's University
Deformation-Metamorphism: 1860-1840 Ma (Nimbawah Event) Deposition of El Sherana Group (ca. 1830 Ma) Deposition of Kombolgie Group (ca. 1750 Ma) feldspar xenoliths in the matrix (Fig. 4.5A). In places, Kfs 0 feldspar xenoliths are completely replaced by Src 1 . Minerals Deposition of Koolpin Formation and associated volcanic rocks (1900-1870 Ma) Quartz Qtz 0 Feldspar KFs 0 Biotite* Bt 0 Muscovite Ms 0 Pre-Ore alteration Quartz overgrowth Qtz 1 Sericite Src 1 Monazite Mzn 1 Titanite Tt 1 Chalcopyrite Cpy 1 Pyrite Py 1 Apatite* Ap 1 Early quartz vein Qtz 2 140 o C Hematite Hem 1 Chlorite Chl 1 160 o C Calcite Cal 1 Main U mineralization Event 250 o C Chlorite Chl 2 Calcite Cal 2 Muscovite Ms 2 Uraninite U 1 1820Ma Hematite Hem 2 Galena Pb 1 Gold Au 1 Chalcopyrite Cpy 2 Late alteration Event Chlorite Chl 3 100 o C Secondary uraninites U 2 Calcite Cal 3 Quartz Qtz 3 Hematite Hem 3 Azurite Az 1 Kaolinite Kln 1 Relative timing Host rock Pre-ore Syn-ore Post-ore Figure 4.4. General mineral paragenesis of the Coronation Hill deposit. The three main alteration stages include a pre-, syn-, and post-ore alteration of the basement rocks. The thickness of the lines indicates the relative mineral abundance. An asterisk (*) marks the primary minerals present in quartz feldspar porphyry and granophyre rocks. Temperatures associated with the different alteration minerals are derived from their chlorite crystal chemistry. The temperature of 140 o C for the pre-ore Qtz 2 is from Mernagh et al. (1994), 147
which was interpreted as being associated with the U mineralization. The age of 1820 Ma is interpreted from U-Pb geochronology of paragenetically constrained U 1 . (See text for details). Disseminated Cpy 1 chalcopyrite and Py 1 pyrite are present in the most altered samples. Mzn 1 monazite associated with Ttn 1 titanite occurs as disseminated aggregates of grains (Fig. 4.5B) and Ap 1 apatite occurs as elongated euhedral and transparent tabular crystals (Fig. 4.5C). Early Qtz 2 quartz veins crosscut the quartz-feldspar porphyry (Fig. 4.5D) and occur locally as stockworks. Chl 1 chlorite is present as replacement of Src 1 sericite in the matrix (Fig. 4.5E) or frequently as coarse, felty-textured, radiating aggregates coating Qtz 2 veins (Fig. 4.5D) where it forms thin needles crosscutting Qtz 2 veins (Fig. 4.5D). Hem 1 hematite forms primary inclusions in Qtz 2 veins where it replaces Chl 1 chlorite needles (Fig. 4.5D) and Src 1 sericite (Fig. 4.5E) in the matrix. Cal 1 calcite also replaces Src 1 sericite and Chl 1 chlorite in the matrix (Fig. 4.5F). The granophyre rock displays a similar pre-ore alteration pattern. Src 1 sericite replaces Kfs 0 alkali feldspar in quartz-alkali feldspar intergrowths. Src 1 sericite is later replaced by Cal 1 calcite. Bt 0 biotite and Ms 0 muscovite laths are typically pseudomorphous after Chl 1 Chlorite. Ap 1 apatite, Hem 1 hematite and Ttn 1 titanite are part of the pre-ore assemblage. 148
- 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
- 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
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- 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 and 192: Figure 4.13. Pb-Pb isochron diagram
- Page 193 and 194: and 4.12B), and to 207 Pb/ 206 Pb a
- 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
Deformation-Metamorphism:<br />
1860-1840 Ma (Nimbawah Event)<br />
Deposition of El Sherana Group (ca. 1830 Ma)<br />
Deposition of Kombolgie Group (ca. 1750 Ma)<br />
feldspar xenoliths in the matrix (Fig. 4.5A). In places, Kfs 0<br />
feldspar xenoliths are<br />
completely replaced by Src 1 .<br />
Minerals<br />
Deposition of Koolpin Formation and associated volcanic rocks (1900-1870 Ma)<br />
Quartz Qtz 0<br />
Feldspar KFs 0<br />
Biotite* Bt 0<br />
Muscovite Ms 0<br />
Pre-Ore alteration<br />
Quartz overgrowth Qtz 1<br />
Sericite Src 1<br />
Monazite Mzn 1<br />
Titanite Tt 1<br />
Chalcopyrite Cpy 1<br />
Pyrite Py 1<br />
Apatite* Ap 1<br />
Early quartz vein Qtz 2 140 o C<br />
Hematite Hem 1<br />
Chlorite Chl 1 160 o C<br />
Calcite Cal 1<br />
Main U mineralization Event<br />
250 o C<br />
Chlorite Chl 2<br />
Calcite Cal 2<br />
Muscovite Ms 2<br />
Uraninite U 1 1820Ma<br />
Hematite Hem 2<br />
Galena Pb 1<br />
Gold Au 1<br />
Chalcopyrite Cpy 2<br />
Late alteration Event<br />
Chlorite Chl 3 100 o C<br />
Secondary uraninites U 2<br />
Calcite Cal 3<br />
Quartz Qtz 3<br />
Hematite Hem 3<br />
Azurite Az 1<br />
Kaolinite Kln 1<br />
Relative timing<br />
Host rock<br />
Pre-ore Syn-ore Post-ore<br />
Figure 4.4. General mineral paragenesis of the Coronation Hill deposit. The three main<br />
alteration stages include a pre-, syn-, and post-ore alteration of the basement rocks. The<br />
thickness of the lines indicates the relative mineral abundance. An asterisk (*) marks the<br />
primary minerals present in quartz feldspar porphyry and granophyre rocks. Temperatures<br />
associated with the different alteration minerals are derived from their chlorite crystal<br />
chemistry. The temperature of 140 o C for the pre-ore Qtz 2 is from Mernagh et al. (1994),<br />
147
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