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The Camsell River area comprises a roof pendant of volcanic rocks within an Aphebian (~1800 m.y.) orogenic belt. Magnetite–apatite intrusions and related bodies are common and are closely associated with plutons of intermediate composition. The magnetitic intrusions are interpreted as immiscible liquids that separated from a magma of intermediate composition. The immiscible fractions were predominantly crystalline when they reached their present higher levels, and final emplacement was facilitated by volatile-streaming and fluidization. Their presence in the orogenic belt is taken as further support for the hypothesis that the orogen was of Andean type.

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A paragenetic sequence of the common mineral constituents of the uraniferous vein deposits of the Fay Mine and Bolger open pit of Eldorado Nuclear Ltd., in northwestern Saskatchewan, is presented.Pitchblende associated with hematite, pyrite, chalcopyrite, bornite, galena, and clausthalite in quartz ± calcite ± dolomite gangues is found in veins cutting folded Tazin metamorphics, adjacent to the St. Louis Fault. Fluid inclusion studies reveal a cooling sequence from the initial phase of mineralization at 440 ± 30 °C down to the final stages at around 80 ± 10 °C. Stable isotope studies, augmented by petrographic data, serve to distinguish at least five generations of carbonate in the ore veins. Early generations of dolomite have apparently not undergone any significant recrystallization or isotopic readjustment and exhibit original restricted δ18O (SMOW) values of 9.5 to 11.0‰ and δ13C (PDB) values of −0.60 to 0.55‰. Isotopic evolution via equilibration with wall rocks has resulted in the deposition of late-stage calcites characterized by δ18O (SMOW) values of + 13.2 to + 14.5% and δ13C (PDB) values of −15.9 to −16.8‰. The strong decrease in δ13C may possibly be explained by a decrease in the amount of CH4 present in the system. It is felt that the deposits were generated by metamorphic hydrothermal fluids with initial δ18O (SMOW) values of + 6 to + 8‰, which during cooling underwent isotopic exchange with the host metamorphic rocks and became depleted in 18O. The final stages of mineralization were possibly effected by some influx of isotopically lighter surface waters into an otherwise essentially 'closed' system. Present day waters from the Fay Mine have δ18O (SMOW) values of −16.0 to −16.2‰ and could represent products of a continuing evolution of the hydrothermal fluids.