An orogenic vien-type gold mineralization confined to the Precambrian basement complex of the Eastern Desert is recorded at Wadi Allaqi district. The mineralization is reflected in a series of gold-bearing quartz veins spreading over 20 gold occurrences. Regionally, the gold mineralization displays close spatial association with island arc domains and occasionally with ophiolitic mélange ones. Temporally and spatially, the mineralization does not show any association with any phase of magmatic activities, since it was developed prior to the emplacement of late-tectonic intrusions and subsequent to the syn-tectonic intrusions. Within island arc domains, the gold mineralization shows no affinity for any particular lithology. Within ophiolitic mélange domain, the volcano-sedimentary matrix of ophiolitic rocks hosts significant vein-type mineralization while ophiolitic rock silvers, especially the talc-carbonated serpentinites, are usually associated with small-scale less significant stockwork gold mineralization. Structurally, Wadi Allaqi district displays deformation history of two major tectonic episodes; the early one is of transpressional accretionary tectonics induced by SW-directed compressional stress during the Pan-African orogeny. The transpressional accretionary tectonics comprise three deformation events (D1, D2 and D3) that were characterized by the formation of the first generation folding (F1), accretion-related thrusts and the regional sinstral strike-slip faults system, respectively. The later deformation episode is related to continental collision and an E-W compressional stress which induced the second generation folding (F2) supplemented with regional dextral strike-slip faults system at the fourth deformation event (D4). The gold mineralization is commonly recorded in subsidiary steeply planner brittle-ductile shear zones extending mostly in the NW–SE direction and steeply dipping to the NE direction and occasionally in the N-S and NE-SW directions. These shear zones are generally concordant with their enclosing country rock foliation (S1 cleavages). Auriferous extensional shear fracturs were developed at the peak of the transpressional accretionary tectonics in association with the regional sinistral strike-slip system of (D3) with preferential formation in the hinge zones of the first-generation anticlinal folds. The gold-bearing quartz veins show complex laminated texture reflecting intermittently stages of mineralization processes that occurred by the crack and seal mechanism. Mineralogically, the auriferous quartz veins are composed mainly of smoky to milky quartz, calcite, sericite, graphite, pyrite, arsenopyrite, minor chalcopyrite and native gold, but the veins lack Cu-Pb–Zn association. The gold mineralization is restricted to greenschist facies domains and less frequent to the lower amphibolite facies grade ones. Examination of wall rocks alteration zones associated with gold mineralization indicates that the gold-bearing fluids were composed essentially of SiO2-H2O-K-CO2, S, As, Au, Cu and sometimes Cr-Ni. The absence of an association between gold mineralization and any magmatic activity and its strong association with the transpression accretionary tectonics suggest a syn-tectonic metamorphic fluids origin for such mineralization. Metamorphic fluids have been created by dehydration and decarbonation of ophiolitic mélange rocks assemblages located between the two accreted island arc belts in the district during the arc accretion and amphibolite facies regional metamorphism. The created metamorphic fluids had the ability to release and complexing the accessible gold from its original sources which are considered here to be the Cu-Ni sulphide mineralization, magmatic sulphides, arsenides, chromite-platinoids and magnetite enclosed in the mafic–ultramafic ophiolitic slices of the ophiolitic mélange assemblage. Resulting auriferous metamorphic fluids tend to migrate from their high-pressure source zone (closure zone) to low pressure host zones (island arc domains). The migrated auriferous fluids tend to deposit in structural traps of dilation sites along subsidiary brittle-ductile shear zones.