https://nova.newcastle.edu.au/vital/access/ /manager/Index ${session.getAttribute("locale")} 5 https://nova.newcastle.edu.au/vital/access/ /manager/Repository/uon:3415 chlorite-quartz-calcite and in the interstices of bladed hematite and magnetite aggregates. The age of the Au-Cu mineralizing event at Cadia is constrained by 40Ar/39Ar dating of accompanying muscovite at 438.2 ± 4.2 Ma (1σ). Gold to copper ratios within the skarns are generally lower than for porphyry Au-Cu deposits at Cadia, particularly the high tonnage, low-grade Cadia Hill deposit. Ore and calc-silicate gangue mineralogy are similar to other oxidized Fe-Cu-Au skarns associated with porphyry deposits. Iron skarn at Big Cadia occurs several hundred meters distant from the margin of a mineralized intrusion of quartz monzonite porphyry. Magmatic-dominated fluids reacted with carbonate in the wall rocks and produced classic skarn zonation over an 800-m interval from the intrusive contact, located at Cadia Quarry, toward more distal environments at Big Cadia. Skarn zonation comprises (1) proximal garnet >> pyroxene, (2) intermediate garnet > pyroxene + scapolite, and (3) distal Fe-Au-Cu skarn. Alteration of noncalcareous metavolcanic rock units (fine-grained pyroxene-phyric volcanic rocks and volcaniclastic rocks) adjacent to the mineralizing quartz monzonite porphyry includes hydrothermal biotite-K-feldspar-quartz hornfels and magnetite-quartz-biotite hornfels. Gold-copper mineralization formed adjacent to garnet-bearing veins peripheral to the main garnet-rich zone, indicating that garnet-forming fluids carried the ore metals. At Little Cadia and Cadia East, mineralization and skarn zonation similar to Big Cadia developed above additional intrusions of quartz monzonite porphyry. Retrograde hydrous alteration replaced much of the prograde garnet-dominant mineralogy at Cadia, with the strongest overprint at Little Cadia. The styles and distribution of alteration and mineralization suggest that the Big Cadia skarn formed from fluids that migrated laterally within calcareous units from strongly altered quartz monzonite phases of the Cadia Intrusive Complex at Cadia Quarry. At Little Cadia, skarn formation was probably related to fluids derived from the Cadia Intrusive Complex that migrated vertically and laterally within permeable calcareous units. Structural controls were important in focusing fluids and localizing the emplacement of late mineralizing phases of the Cadia Intrusive Complex.]]> Sat 24 Mar 2018 07:21:39 AEDT ]]> https://nova.newcastle.edu.au/vital/access/ /manager/Repository/uon:3421 21.0 eq. wt.%, respectively). Heating experiments indicate minimum temperatures of trapping of 350 641°C for Type-I inclusions, 207 660°C for Type-II inclusions, and 143 <637°C for Type-III inclusions. Oxygen isotope compositions of quartz–actinolite and albite–actinolite pairs indicate a temperature of gold-associated alteration of ~350°C, consistent with arsenopyrite thermometry, which indicates gold mineralization at <480°C. The early CO₂-rich fluid inclusions have densities that range from 0.6 to 1.05 g/cm3 which, at 350°C, correspond to 1–2 kbar pressure, consistent with geological relations indicating that the McPhees deposit formed at <7 km. Type-I inclusions are interpreted to contain early vein-related fluids that carried gold, but this assemblage (nearly pure CO₂ and subordinate, coexisting H₂O-rich fluid inclusions) is unusual for orogenic gold deposits. It is most likely a result of fluid mixing that may have played a role in gold deposition in veins; however, host-rock lithology seems to have been a first-order control in localizing the gold.]]> Sat 24 Mar 2018 07:21:37 AEDT ]]>