Proposed Title 1: - Queen's University

Mineral values Temperature Fluid values
Sample ID Deposits δ 18 O δ 2 H o C
δ 18 O fluid δ 2 H fluid
V-SMOW ‰ V-SMOW‰ V-SMOW‰ V-SMOW‰
Basement
Synore muscovite
C29-214 Coronation Hill 11.8 -74 250 2.8 -64
C29-195 Coronation Hill 13.8 -85 250 4.8 -75
C29-202 Coronation Hill 12.0 -67 250 3.0 -57
Pre-ore sericite
C29-189 Coronation Hill 12.7 -73 160 7.7 -81
C77-121 Coronation Hill 10.2 -53 160 5.2 -61
C29-209 Coronation Hill 12.7 -76 160 7.7 -84
C7788 Coronation Hill 11.8 -53 160 6.9 -62
C29-80 Coronation Hill 10.1 -44 160 5.1 -52
C29-80 (dup) Coronation Hill 10.1 -49 160 5.1 -57
E30-81 El Sherana 14.2 -44 300 10.7 -60
Table 4.3. Measured δ 18 O and δ 2 H for muscovite and calculated δ 18 O and δ 2 H values for fluids
in equilibrium with minerals from various alteration stages of the basement rocks at the
Coronation Hill and El Sherana deposits. Temperatures used to calculate the fluid values are
derived from the chlorite crystal chemistry (see Table 4.2)
4.5.4. Geochronology of uraninite and isotopic systematics
Paragenetically constrained uraninite from the Coronation Hill and El Sherana
deposits were dated by LA-HR-ICP-MS (Chipley et al., 2007). Uraninite samples analyzed
have a mottled appearance with micron-size areas that are highly reflective surrounded by
dull areas, which is typical of the ore from both deposits (Figs. 4.6E and 4.6F). The
majority of the U–Pb isotope ratios are significantly discordant, as in other deposits (e.g.
Fayek and Kyser, 1997; Polito et al., 2004). The oldest 207 Pb/ 206 Pb ages are likely to be
closer to the initial formation age because Pb-Pb ratios in U are less susceptible to resetting
by younger fluid events than are the U-Pb ratios (Collins et al., 1954). The errors observed
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