Stable isotope record of hydrothermal sulfate, sulfide and silicate minerals in the Darreh-Zar porphyry copper deposit in Kerman, southeastern Iran: Implications for petrogenesis and exploration

• The calculated δD values of the aqueous fluids range from − 66 to − 78‰.
• The calculated δ18O of aqueous fluids ranges from 7.8 ± 0.4 to 2.6 ± 0.5‰.
• Magmatic aqueous source suggested for the studied area
• The calculated temperature of 520 ± 50 °C is assumed for sulfate–sulfide minerals.
• High sulfur isotopic composition of gypsum is as an indicator for large porphyry Cu deposits.

The Darreh-Zar porphyry copper deposit is found together with other porphyries such as Sar-Cheshmeh and Sungun in the Cenozoic age Urumieh–Dokhtar magmatic belt that is related to the subduction of the Arabian plate beneath Central Iranian microcontinent. The deposit is associated with Miocene granodiorite porphyry intrusions into Eocene basaltic volcanic rocks. The principal hydrothermal facies of the area are a core zone of potassic alteration enclosed by a peripheral zone of propylitic alteration. Chlorite-sericite, sericitic, advanced argillic and intermediate argillic alteration zones cut the upper part of the potassic zone and are developed near the interface between the potassic and propylitic zones. Chalcopyrite, pyrite or local bornite, and associated anhydrite are the chief hypogene sulfide minerals, and constitute < 0.1 to 0.8 wt.% Cu ores. A ~ 50-m-thick supergene zone containing 0.8 to 1.5 wt.% Cu, characterized by covellite and chalcocite, underlies an oxidized and partially leached ~ 20-m-thick zone containing chrysocolla, malachite and azurite.The hydrogen isotopic composition of biotite from Darreh-Zar ranges from δD of − 89 to − 101‰, and the calculated aqueous fluids (δD of − 66 to − 78‰) in equilibrium with biotite are consistent with a large component of magmatic fluid. Epidote varies from δD of − 56 to − 53‰, and yields calculated fluids responsible for the propylitic alteration that range from − 22 to − 19‰. Oxygen isotopic data for the studied quartz, biotite, anhydrite and epidote vary between δ18O of 0.8 to 9.0‰. The calculated δ18O values for aqueous fluids in equilibrium with the biotite, quartz (from barren type and A veins), anhydrite (from B veins) and epidote are 7.8 ± 0.4, 5.1 ± 0.6, 2.6 ± 0.5 and − 1.1 ± 0.1‰, respectively. This marked decrease likely reflects a change from magmatic-derived fluids in central potassic zone to meteoric or sedimentary-derived fluids in the outer propylitic zone. Sulfur isotope compositions are 11.8 to 14.0‰, for anhydrite (n = 3), 2.4‰ for molybdenite (n = 1), 1.7 to 3.9‰ for pyrite (n = 17), and 1.6 to 2.9‰ for chalcopyrite (n = 2). The sulfide data, alone, suggest a conventionally ‘magmatic’ value of about 1.6 to 2.9‰ for Darreh-Zar sulfur. However, the fairly oxidized granitic parental magma shows relatively heavy bulk sulfur (δ34SΣS ≈ + 5‰) and sulfate–sulfide sulfur isotopic fractionation is consistent with an approach to isotopic equilibrium at calculated temperatures of 520 ± 50 °C for most of the coexisting anhydrite–pyrite pairs (n = 4). An exploration implication is that the identification of isotopically high sulfur isotopic compositions of gypsum from near-surface samples determines a hydrothermal system that contains deeper hypogene anhydrite, a common indicator of large porphyry Cu-Mo deposits. In contrast, isotopically low sulfur isotopic values similar to and derived from weathering of pyrite and other sulfides are common in many hydrothermal environments.