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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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