The Browns Creek Au–Cu skarn is restricted to a 50 m-wide fault zone developed in an interbedded sequence of Upper Ordovician mafic Blayney Volcanics and Cowriga Limestone Member adjacent to the mid-Silurian (434–425 Ma) Carcoar Granodiorite. The mineralised skarns are hosted within and controlled by the Mount David/4000E Fault zone, a dextral transtensional strike-slip fault that in cross-section has the form of a negative flower structure. This is consistent with components of dextral strike-slip motion recorded on regional faults likely guiding magma emplacement during the Benambran Orogeny. The skarns comprise a barren Stage 1 prograde pyroxene–garnet–wollastonite–anorthite assemblage followed by Stage 2 hornblende–biotite–epidote–magnetite–Fe–Cu–As sulfide skarn. These are overprinted by the strongly mineralised Stage 3 retrograde epidote–andradite garnet–chlorite Cu–Au skarn containing the bornite–chalcopyrite–chalcocite–gold ore, when probable magmatic-dominated hydrothermal fluids were channelled through the previously skarned strike-slip fault system that had become a permeable fault zone. Stage 4 sheeted vein-hosted prehnite–epidote–chlorite Au–Cu skarn formed when the strike-slip fault subsequently failed in tension to form gold-rich vertical extensional veins. Conditions for extensional fault reactivation and vein formation are discussed in terms of reshear criteria and fluid overpressure. The age of the mineralisation is constrained by late-stage monzonitic dykes that both crosscut and are themselves skarned by stages 3 and 4 assemblages. These co-magmatic dykes were dated at ca 435–425 Ma, which closely corresponds with the age of the Carcoar Granodiorite itself. Stable and radiogenic isotopes indicate that hydrothermal fluids associated with prograde and retrograde skarns are within the range for magmatic fluids with some mixing with fluids of meteoric origin during later stages of mineralisation. The Browns Creek Au–Cu skarn is typical of Au-skarns worldwide and is linked to mid-Silurian magmatism at a late stage in the Benambran Orogeny.
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