Numerous massive and sheared, milky quartz veins cut a sequence of Neoproterozoic island arc metavolcanic/ volcaniclastic rocks and related banded iron formation (BIF) at the Abu Marawat area, central Eastern Desert of Egypt. Sulphide-bearing quartz veins and related hydrothermal breccia masses display a range of textures including sheared, boudinaged and recrystallised quartz, quartz with open space filling and microbreccia, implying a complex history of crack- seal processes characterising the relationship between mineral deposition and a major N-S-trending shear zone, during a late brittle- ductile deformation event that affected the area at y550 Ma. Gold- base metal mineralisation is associated with brecciation and fracturing of the iron ore bands, close to silicified shears and related quartz veins. The auriferous quartz lodes are characterised by the occurrence of visible pyrite- chalcopyrite pyrrhotite +/- sphalerite +/- galena mineralisation. Gold is refractory in pyrite and chalcopyrite, but rare visible gold/ electrum and telluride specks were observed in a few samples. Hydrothermal alteration includes selectively pervasive silicification, pyritisation, sericitisation, carbonatisation that are confined to a delicate set of veins and altered shears, and a more widespread propylitic alteration assemblage (quartz+vertical bar vertical bar chlorite+pyrite+calcite +/- epidote). The predominance of hydrated silicate phases (i. e. chlorite and sericite) within and adjacent to the shear zones points toward fixation of H2O during the shear zone development, while CO2 was consumed to form carbonate in halos around the chloritedominated zones, leading to variations in the H2O/ CO2 ratio of the ore fluid with progression of the hydrothermal alteration. Ore textures, including hydrothermal quartz intimately associated with replacement of magnetite by pyrite, suggest the introduction of ore fluids via epigenetic conduits into the iron-rich wallrocks. Fluid inclusion textural and microthermometric studies indicate heterogeneous trapping of a low-salinity (1.4-6.7 wt-% eq. NaCl) aqueous solution that coexisted with a carbonic fluid. Evidence for fluid immiscibility during ore formation includes variable liquid/vapour ratios in inclusions along individual trails and bulk inclusion homogenisation into liquid and occasionally to vapour at comparable temperatures. The trapping conditions of intragranular aqueous-carbonic inclusions approximate 264-378 degrees C at 700-1300 bar. Similar temperature estimates have been obtained from Al-in-chlorite geothermometry of chlorite associated with sulphides in the mineralised quartz veins. Fracturing enhanced fluid circulation through the wallrock and related BIF, allowing reaction of the S-bearing ore fluid with iron oxides. This caused formation of pyrite, a rise in Eh and concomitant Au precipitation, which was enhanced by fluid immiscibility as H2S partitioned preferentially into the carbonic phase. The ore fluids have probably originated from felsite intrusions, whereas Abu Marawat gold deposit and the post-Hammamat felsites is assumed in view of their communal relationship with the N-S fault/shear trend and high geothermal gradient calculated from the fluid inclusion data.
