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ed-bed strata and associated volcanic rocks were deposited in continental environments
along pre-existing faults that were reactivated during the waning stage of a major orogen.
Most of the U deposits in successor basins are structurally controlled and are affected by
repeated deformation events that affected the host rock.
In the Beaverlodge area, the Martin Lake Basin formed at ca. 1820 Ma (Langford,
1981; Morelli et al., 2001) but was immediately deformed, fractured and folded during
tectonism following the peak Trans-Hudson Orogen (Hoffman, 1990; Corrigan, 2009). The
main U mineralization event predated the deposition of the Martin Lake successor basin
and is associated with regional metamorphism and deformation during early stages of the
Trans-Hudson Orogen (Dieng et al., 2011). These deposits are classified as metamorphicrelated
uranium mineralization system (Fig. 5.1) (e.g Cuney and Kyser, 2008).
In the South Alligator River area, the El Sherana Basin formed at ca. 1830 Ma
(Jagodzinski, 1992) during crustal extension following the peak Nimbuwah event that
reactivated previous fault zones (Needham et al., 1988). The main U mineralizing event
that affected both the supracrustal rocks and sediments of the successor basin is associated
with basinal brines generated from the successor basin itself. Deposition of the El Sherana
Basin is followed by a period of relative tectonic quiescence during which time
sedimentary and associated volcanic rocks of the El Sherana group were altered by basinal
brines capable of transporting and depositing the scavenged U at the unconformity between
the basement rock and sediments of the El Sherana Basin. These deposits are variants of
unconformity-related U mineralization system (Fig. 5.1), similar to those in the younger
overlying Kombolgie Basin (e.g. Polito et al., 2004, 2006).
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