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Location: 9 km NE from Baie Verte, Newfoundland and Labrador, Canada
232 Highway 410PO Box 238Baie VerteNewfoundland and Labrador, CanadaA0K 1B0
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Maritime acquired 100% of the common shares of Point Rousse Mining Inc., a wholly owned subsidiary of Signal Gold, which holds all related mineral licenses, fixed assets and equipment, liabilities, rights and obligations related to Point Rousse, including the fully permitted Pine Cove mill and in-pit tailings facility.
The Point Rousse Complex is host to orogenic-style gold mineralization. Mineralization comprises both vein-hosted and altered-wall rock or replacement styles of mineralization and both exhibit features common to orogenic gold deposits. The mineralization is typically structurally controlled and developed within subsidiary deformation zones, such as the Scrape Trust Fault, to major regional structures, like the Baie Verte – Brompton Line fault. gold mineralization is intimately associated with disseminated and massive pyrite within the host rock indicating that iron rich rocks are an important precursor to mineralization. Alteration within mafic volcanic and gabbroic rocks can be is characterized by albitization and carbonitization. Iron and titanium rich lithologies associated with the Scrape Thrust are typical host rocks. The Point Rousse gold mineralization exhibits relatively narrow, but distinctive alteration haloes dominated by Fe-carbonate, albite, sericite, chlorite and leucoxene (Plate 9). The ore mineralogy is relatively simple and is generally comprised of non-refractory gold either as free gold or as coatings on, or along fractures/grain boundariesin pyrite. Silver and base metals can be present in minor amounts and the deposits typically exhibit only trace arsenic. D3 deformation produced F3 mesoscopic northward-verging asymmetric folds that affect all the D1/D2 fabrics, shear zones and related alteration. The F3 folds trend roughly southeast and plunge shallowly to the northwest and southeast. The associated S3 axial planar cleavage dips gently towards the south and cuts the S2 fabric. D4 deformation produced asymmetric to tight, generally north verging folds with subhorizontal to gently south-dipping axial surfaces. The D4 deformation is marked by broad regional northnortheast-trending anticlines and synclines which affect D1 through D3-relatedstructures and impart a doubly geometry to many of the pre-existing folds. S4 is a roughly northeast-trending fracture cleavage. Four alteration zones are recognized (Ramezani, 1992). These include; i) a chlorite-calcite zone, ii) an ankerite-sericite zone, iii) a chlorite-magnetite zone, and IV a red albite-pyrite (+gold) zone. The fourth zone of albitization is readily observed in outcrop even from a distance and results in the rocks having a general pink appearance that is readily mapped. Locally leucoxene is observed as part of the alteration assemblage. Quartz veins occur within the mineralized zones both as barren tension gash veins, which are interpreted to postdate the mineralization, and as shear-parallel, quartz– albite–ankerite veins. The gold within the Stog’er Tight Deposit occurs as fine-grained (<.05 mm) micro veinlets and disseminated blebs within the coarse pyrite aggregates. Visible gold was observed as rare very delicate flakes localized within weathered-out pyrite cubes and in narrow quartz veins. Generally, higher grades are associated with coarse mottled pyrite.
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