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Drilling in Nevada
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Pyrite-rich breccia with sedimentary and rhyolite fragments.
Pyrite-rich breccia with sedimentary and rhyolite fragments affect lake sediments and adjacent rhyolite in a breccia zone in the Bell Springs pit. These and other textures suggest a small lake was present at Bell Springs which was affected by periodic hydrothermal eruptions in a high level epithermal setting.
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Silicified, spherulitic flow foliated rhyolite in Bell Springs pit.
Silicified, spherulitic flow foliated rhyolite in Bell Springs pit
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Clay alteration in Cottonwood Basin sediments below the Bell Springs pit.
Clay alteration in Cottonwood Basin sediments below the Bell Springs pit forms a rusty colour anomaly, potentially after pyrite.
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Partially reclaimed Bell Springs pit, looking southeast.
Partially reclaimed Bell Springs pit, looking southeast. Note intense white clay alteration of hosting rhyolite flow dome complex.
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Thinly bedded diatomaceous sediments in the Cottonwood Basin.
Thinly bedded diatomaceous sediments in the Cottonwood Basin. These become highly opal altered in areas of hydrothermal alteration.
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Opaline silica in altered Cottonwood Basin sediments at the Airport zone.
Opaline silica in altered Cottonwood Basin sediments at the Airport zone.
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Looking east from the Cottonwood Lake Basin.
Looking east from the Cottonwood Lake Basin. White lake sediments form the white ridge. The ridge may also be intruded by north-northwest trending rhyolite dykes which occur as float along the ridge tops. Margins of such dykes may potentially host gold mineralization. Hills in the background contain the historically mined pits.
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Flat topography in the Cottonwood Basin Lake sediments at the Airport zone.
Flat topography in the Cottonwood Basin Lake sediments at the Airport zone. The Airport deposit lies beneath this area in strongly opaline silica altered lake sediments associated with pyrite mineralization.
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View northwest into Cottonwood basin from the slopes adjacent to the previously mined pits.
View northwest into Cottonwood basin from the slopes adjacent to the previously mined pits. The white areas in the basin are exposures of lake sediments from a 14 to 16 million year old lake which filled the basin, and which occurred beside the rhyolite volcanic center that is associated with the previously mined mineralization at Hog Ranch. The Hog Ranch property extends into this area and encompasses prospects which occur in the lake sediments such as the Cameco and Airport zones, which may be associated with rhyolite dykes that intrude the lake sediments.
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Fault exploration target northwest of the Geib pit
Fault exploration target approximately 1.5 km northwest of the Geib pit, looking southeast. A northwest trending fault zone passes through the right of the photo, marked by a series of lineaments and disappearance of the resistant rhyolite to the right. The rhyolite here is intensely silicified in the outcrops above, and in the canyon below is affected by intense opaline silica, forming a large silicified zone that may lie above an upflow zone along the fault.
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Silicified tuff breccia unit.
Silicified tuff breccia unit forms a permeable flow unit between rhyolite flows which was locally preferentially silicified.
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Petrified wood fragments adjacent to one of the *craters*.
Petrified wood fragments occur in an Fe-oxide matrix adjacent to one of the "craters". These fragments, along with overall textures and opaline quartz suggest potential formation in a near surface hotspring environment high in the hydrothermal system.
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Sample of intensely opaline altered breccia.
Intensely opaline altered breccia from adjacent to one of the *craters*, as is seen in the previous photo.
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*Crater* feature southeast of the Geib pit.
"Crater" feature southeast of the Geib pit. Chains of such depressions seen at Hog Ranch, which are surrounded by Fe-oxide stained opaline quartz altered wallrock and local breccia, may represent relicts of hydrothermal explosion craters that are seen in recent hot springs environments. While the system here is too old to preserve such features in their original form, their altered cores may subside and create topographic lows. Chains of these features form discrete linear trends at Hog Ranch near the previously mined pits, and may lie above faults that controlled hydrothermal fluid flow and potential veining.
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Contorted flow foliated rhyolite in the Geib pit.
Contorted flow foliated rhyolite in the Geib pit. Such folded rhyolite units are typical of proximity to volcanic vents, and occur in flow dome complexes, which form common heat and potential fluid sources of epithermal systems.
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Fault in the Geib pit offsets clay altered flow banded rhyolite.
Fault in the Geib pit offsets clay altered flow banded rhyolite. Such structures have the potential to host vein gold mineralization where they project into deeper levels of the hydrothermal system.
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Bedded tuffaceous sediments in the Geib pit.
Bedded tuffaceous sediments in the Geib pit. Small lake basins were present and associated with mineralized zones in the Hog Ranch deposits suggesting the presence of fault-controlled minor basins in the rhyolite sequence, as is common in many epithermal systems. The controlling faults could host veins at depth. The sediments here are pyrite-rich and mineralized.
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Detail of silicified water table in the Geib pit.
Further detail of silicified water table in the Geib pit. Bright red mineral is likely cinnabar, a mercury sulphide that typically occurs at high levels in epithermal systems. Note steep flow foliation in clay altered rhyolite below extending into the overlying silicified (brown) zone above.
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Detail of silicified paleowater table which overlies clay altered flow foliated rhyolite in the western Geib pit.
Detail of silicified paleowater table (resistant brown unit above) which overlies cream/pale colored clay altered flow foliated rhyolite in the western Geib pit.
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View eastward into the Geib pit depicting part of a silicified paleowater table in flow banded rhyolite.
View eastward into the Geib pit. Note the resistant rocks in the upper left part of the photo which form part of a silicified paleowater table in flow banded rhyolite which extends into the upper right side of the photo, southeast of the pit. This shallow northwest dipping paleowater table marks the top of the hydrothermal system. Mineralization which was historically mined in this and the other pits lie just below the paleowater table, which is very shallow in the system. Normally vein mineralization is developed at depths commencing between 100 and 250 m below such levels in a hydrothermal system, implying significant depth potential at Hog Ranch.
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View west into the Geib pit, showing strong clay alteration and rusty iron staining after pyrite.
View west into the Geib pit, showing strong clay alteration and rusty iron staining after pyrite.
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View northeast into the now reclaimed historically mined Krista pit, which produced 150,000 ounces of gold.
View northeast into the now reclaimed historically mined Krista pit, which produced 150,000 ounces of gold.
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Sample of crustiform and colloform banded chalcedonic quartz vein material from the Geib pit
Sample of crustiform and colloform banded chalcedonic quartz vein material from the Geib pit. Veining of this style is the target for hosting higher grade mineralization at depth, and is typical of the host to vein systems at other epithermal deposits in northern Nevada, such as Sleeper, Midas and Hollister.
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Sample of very high grade mineralization from the bottom of the 139 pit
Sample of very high grade mineralization which was extracted historically from the bottom of the 139 deposit pit at Hog Ranch. Fine-grained electrum (gold-silver alloy) is present rimming some of the fragments at right. Note the banded colloform nature of much of the quartz. Some of this material may still be in place at the bottom of the 139 pit. This style of mineralization shows both the right texture, and very high grades that are permissive for potential high grade veining at depth.
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