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3.4. Results
3.4.1. Paragenesis of the alteration minerals and types of U mineralization
The paragenetic mineral assemblage is based on detailed petrographic analysis of
550 samples collected from the Ace-Fay, Gunnar and Cinch Lake deposits and on field
relationships. These deposits are the largest in the Beaverlodge area (Fig. 3.2). There are
six mineralogically, temporally, and structurally distinct U ore and related alteration
assemblages within the U deposits in the Beaverlodge area (Figs. 3.3 and 3.4).
Mylonitization is the earliest deformation observed (Dieng et al., 2011). The
hornblende-feldspar gneiss at Cinch Lake and the Foot Bay gneiss at Ace-Fay define an
amphibolite metamorphic assemblage of Kfs 1 +Pl 1 +Hbl 1 . Retrogression to greenschist
metamorphic grade is indicated by the assemblage Bt 1 +Chl 1 +Src 1 +Hem 1 (Fig. 3.3). The
mylonitic foliation is cut by Chl 2 chlorite, Qtz 2 quartz, Ab 1 albite, Cal 1 calcite, and Ep 1
epidote veinlets (Fig. 3.3). The mylonites are further overprinted by a network of ductilebrittle
and brittle features that host the U mineralization (Dieng et al., 2011). The
cataclasite comprises mylonite fragments (Fig. 3.4A), Qtz 1 quartz and Kfs 1 feldspar clasts,
and disrupted Cal 1 calcite and Qtz 2 quartz veinlets embedded in a matrix composed of
recrystallized Qtz 1 quartz, Cal 2 calcite, Hem 3 hematite, Chl 3 chlorite, Src 2 sericite, and
disseminated U 1 uraninite (Fig. 3.4B). Cataclasite rocks are occasionally cut by tensional
Qtz 3 quartz-Cal 3 calcite and U 2 uraninite veins (Fig. 3.4C). Fine-grained Cal 4 calcite, Chl 4
chlorite, Hem 4 hematite, and Py 3 pyrite are intergrown with U 2 uraninite (Fig. 3.4D). Qtz 3
and Cal 3 display evidence of tensional opening (Sibson et al., 1975) and a syntaxial
growth with fibers perpendicular to vein wall (Fig. 3.4C).
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