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Chah Zard Deposit: Breccia-Hosted Epithermal Ag-Au Mineralization in the Urumieh-Dokhtar Belt

Document Type : Original Research Paper

Authors

1 Associate Professor, Department of Economic Geology, Tarbiat Modares University, Tehran, Iran

2 Ph.D. Student, Department of Economic Geology, Tarbiat Modares University, Tehran, Iran

3 Associate Professor, Islamic Azad University, Islamshahr Branch, Tehran, Iran; Research Institute for Earth Sciences, Geological Survey of Iran, Tehran, Iran

4 Professor, CODES ARC Centre of Excellence in Ore Deposits, University of Tasmania, Hobart, Australia

Abstract

The breccia-hosted epithermal Ag-Au deposit of Chah Zard is located within an andesitic to rhyolitic volcanic complex in the central part of the Urumieh-Dokhtar magmatic belt. At this location, magmatic and hydrothermal activity was associated with local extensional tectonics, formed in the Dehshir-Baft strike-slip fault system. The host rocks of the volcanic complex consist of Eocene sedimentary and volcanic rocks covered by Miocene sedimentary rocks. LA-ICP-MS U–Pb zircon geochronology yields ages between 6.36±0.14 and 6.19±0.24 Ma, and a mean age of 6.23±0.16 Ma for magmatic activity at Chah Zard. Breccias and veins were formed during and after the waning stages of strong explosive eruption of magmatic-hydrothermal and phreatomagmatic brecciation events due to shallow emplacement of the rhyolite porphyry. Detailed systematic mapping leads to the recognition of three distinct breccia bodies: the volcaniclastic breccia with a dominantly clastic matrix, the gray polymict breccia with a greater proportion of hydrothermal cements, and the mono-polymict breccia with argillic groundmass matrix. The polymictic breccias generated bulk-mineable ore, whereas the volcaniclastic breccia is relatively impermeable and largely barren. Variable hydrothermal alteration occurs in outcrops, covering about 9 km2 at Chah Zard. Hydrothermal alteration assemblages are zoned around the breccias and veins, consisting of secondary quartz, illite, pyrite, adularia, chlorite, various carbonate minerals, and minor K-feldspar. Iron oxide-hydroxide, jarosite, gypsum, kaolinite, halloysite and rare alunite are the supergene alteration minerals replacing primary minerals, and filling the fractures and vugs. Precious metals occur with sulfide and sulfosalt minerals as disseminations in the veins and breccia cement. There is a progression from pyrite-dominated (stage 1) to pyrite-base metal sulfide and sulfosalt-dominated (stages 2 and 3) to base metal sulfide-dominated (stage 4) breccias and veins. Deposition of gangue minerals progressed from illite-quartz to quartz-adularia, carbonate and finally gypsum-dominated assemblages. Free gold occurs in stages 2 and 4, principally as intergrown with pyrite, quartz, chalcopyrite, galena, sphalerite, and Ag-rich tennantite-tetrahedrite; and also as inclusions in pyrite. The U-Pb zircon age of 6.19±0.24 Ma for emplacement of the rhyolitic magmas represents the maximum age of mineralization at Chah Zard. It may indicate that there was a previously unrecognized mineralization event in Urumieh-Dokhtar at this time.

Keywords

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Scientific Quarterly Journal of Geosciences
Volume 22, Issue 87
December 2013
Pages 9-24
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