The Project lies within the western Basin and Range structural province in the northern portion of the Walker Lane structural trend which follows the California-Nevada border.  The project sits on the eastern flank of the Virginia Range approximately 20 miles northeast of the historic Comstock Lode Ag-Au District.

At Talapoosa, Tertiary rhyolitic tuffs with interbedded rhyolitic lava and vesicular basalt form the base of the volcanic sequence and are overlain by predominantly dacitic and andesitic volcanic and related intrusive rocks with interbedded sedimentary rocks.  Late Pliocene to Pleistocene basaltic rocks, are widespread throughout the region and represent the youngest episode of volcanism and are post-mineralization (Figure 4).

Cenozoic faulting, tilting and warping is associated with regional extension and oblique and strike‑slip faulting and mineralization.

At Talapoosa, the mineralized area as defined by drilling to-date, is approximately 2,200 ft long, up to 1,000 ft wide, and up to 500 ft thick/down-dip and centered around the northwest trending Talapoosa and associated faults (Figure 5).  Gold and silver mineralization occurs as quartz-chalcedony vein, hydrothermal breccias surrounded by margins of stockwork veining.   Gold primarily occurs as native gold and in electrum.  The upper 70 meters is predominantly oxidized, with the bulk of the oxide mineralization being contained within the Main, Dyke Adit, and East Vein Zones.

Approximately 80% of the resource occurs within the Bear Creek Footwall and Hangingwall Zones (Figure 6).  Mineralization trends northwesterly with a steep dip and occurs within a central core of massive chalcedony veins and hydrothermal breccia up to 50 m wide, surrounded by a halo of stockwork veins up to 150m thick.  Alteration of the rocks hosting Bear Creek Zones mineralization includes propylitic propylitic, phyllic, silicic, argillic, and opaline types, all of which are present at the Project.

The precious metal-bearing quartz veins, stockworks, and breccias at Talapoosa are of the low-sulphidation epithermal type mineralization which formed from boiling of volcanic-related hydrothermal systems (Figure 7).

Emplacement of mineralization is generally restricted to within 1 km of the paleosurface (Panteleyev 1996).  Veins typically have strike lengths in the range of hundreds to thousands of metres; productive vertical extent is seldom more than a few hundred metres.  Vein widths vary from a few centimetres to metres or tens of metres.  Gangue mineralogy is dominated by quartz and/or chalcedony, accompanied by lesser and variable amounts of adularia, calcite, pyrite, illite, chlorite, and rhodochrosite.

Vein mineralogy is characterized by gold, silver, electrum and argentite with variable amounts of pyrite, sphalerite, chalcopyrite, galena, tellurides, rare tetrahedrite and sulphosalt minerals.  Crustiform banded quartz veining is common, typically with interbanded layers of sulphide minerals, adularia and/or illite.  Regional structural control is important in localization of low sulphidation epithermal deposits.  Higher grades are commonly found in dilational zones, in faults, at flexures and splays.