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The Bozjani copper deposit is located about 30 km west of Fariman city, Khorasan Razavi Province. Host rocks to mineralization are mostly pridotites and basalts of Fariman ophiolitic sequence. Ore body consists of two parts: lower and upper. Lower part has formed a stringer of primary sulfides as stockwork, veinlets, and disseminated. Uppermost part has lenticular shaped dominated by ribbon-like, fine grain and rounded primary sulfides. Mineralogical investigations show pyrite, marcasite, chalcopyrite, bornite, sphalerite, galena, native copper, and magnetite are primary minerals of ore body associated with secondary minerals as coprite, tenorite, covellite, chalcocite, chrysocolla, malachite, azurite, jarosite, limonite, and hematite. According to geochemistry of immobile elements, the host mafic rocks fall in boninite tectonic setting. Mass balance calculations show enrichments of Cu, Pb, Th, As, Ag, Tl and U during evolution of Bozjani copper deposit. The results of host rock, structure, texture, mineralogy and geochemistry in this research reveal that Bozjani deposit resemble volcanic massive sulfide deposit dominated by mafic rocks. Evolution of this deposit is related to four stages including hydrothermaly alteration, seafloor weathering, regional metamorphic and weathering of terrestrial.

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The Seranjic skarn occurs as invading of Late Jurassic intrusive body with granite composition within impure carbonate rocks. Field observation and mineralogical investigations show the exoskarn is the most widespread skarn in the Seranjic skarn and is mostly calcic skarn together with magnesium skarn as a narrow marginal zone. The mineral assemblages indicate two stages of evolutions: the prograde and the retrograde stages. The prograde stage is characterized by garnet and clinopyroxene. The texture evidences and EPMA chemical analysis of clinopyroxene and garnet show two types of clinopyroxene and three types of garnet in various zones during the prograde skarn. Type 1 clinopyroxene show salitic (Hd_27-40 Di_58-51 Jo_8-14) and ferrosalitic (Hd_58-75 Di_27-16 Jo_8-13) compositions in the forsterite- clinopyroxene and garnet- vesuvianite- clinopyroxene zones respectively. Type 2 clinopyroxene has the intermediate compositions of salitic and ferrosalitic (Hd_36-48 Di_43-51 Jo_7-12) in the garnet- vesuvianite- clinopyroxene zone, which is accompanied by scheelite crystallization. Garnet mostly occurred in the center near the exoskarn zones to the plutonic body. Type 1 garnet is characterized by grossular-rich granditic composition (Grs₆₅ And₂₅ to Grs₄₅ And₄₀) with pyralspite< 10 mol percent, and the textural evidences show coexisting type 1 garnet and type 1 clinopyroxene that is widespread in the garnet- vesuvianite- clinopyroxene zone. Type 2 garnet (Grs₅₀ And₂₅ Pyr₂₅ to Grs₄₅ And₂₀ Pyr₃₅) and type 3 garnet (Grs₇₀ Pyr₃₀ to Grs₆₀ Pyr₄₀) have the highly pyralspite and occurs as proximal zones from the plutonic bodies. Based on mineral assemblages, the formation of type 1 garnet, comparative to type 2 and type 3 garnet, is in more oxidized condition in the distal zones of the skarn. Moreover, garnet/clinopyroxene ratios observed at the skarn is affected by the F high volume of magma-fluid. Also, the abundance of F in the volatile phase is probably largely responsible for the abundance of F-bearing minerals, such as vesuvianite, and the scarcity of pyroxene in the skarn. Composition of the variation types of clinopyroxene and garnet show the prograde skarn can be stable at relatively oxidized to relatively reduced and LogfO₂ = -18 to -30.