The LOGHAR OPHIOLITE is located in ophiolitic belt of Kabul block (southeast of Afghanistan) and it is a part of Neotethyan OPHIOLITEs in Alpine - Himalayan orogenic system with Eocene age. Olivine, orthopyroxene, clinopyroxene and spinel are rock forming minerals of LOGHAR OPHIOLITE mantle peridotite. Most of the olivines from different rock types are serpentinized but some fresh are present with forsterite composition. Orthopyroxene and clinopyroxene are enstatite (Mg# 0.961-0.972) and diopside (Mg# 0.976-0.999) in composition. The Cr# of vermicular and unhedral spinels of lherzolite and subhedral reddish brown spinels of harzburgite are 0.547 and 0.625 respectively. The Cr# of subhedral to euhedral spinels of dunite is 0.477, induced by high content of Al2O3 and low level of Cr2O3. The Cr# of dark red and euhedral spinel of chromitite is 0.633. The peridotites of the studied area belong to sub-oceanic crust mantle. The low content of Al2O3 in pyroxenes (opx and cpx) and the low amount of Na2O in clinopyroxene indicate high degree of partial melting of mantle peridotites. The chemical compositions of minerals in dunites are different from that of lherzolite and harzburgite but present considerable similarity with that of the pillow lavas. The dunites of LOGHAR mantle peridotite (LMP) do not share features with those derived by partial meltiny, but represent sub lithospheric melt channels.

The Siah-Cheshmeh OPHIOLITEs at the north-northwest part of the Khoy OPHIOLITEs show a dismembered pile of metamorphic units, mantle sequence, and basaltic-andesitic lavas associated with Late Cretaceous pelagic limestones and cherts. The basaltic-andesitic lavas can be divided into alkaline and calc-alkaline varieties. The presence of Ti-rich amphibole prisms and Ti-bearing clinopyroxenes is characteristic of these lavas. The calc-alkaline lavas are characterized by enrichment in LREE and depletion in HFSE while the alkaline lavas display positive LREE and HFSE anomalies. The interaction between mantle plumes with a spreading center can be considered for generation of alkaline basalts while a subduction zone is responsible for the genesis of calc-alkaline basalts.

The Khoy OPHIOLITE with Precambrian basement rock is located in north western of Iran.The tectonite peridotites are most formed by clinopyroxene harzburgites. These harzburgites characterized by protogranular, porphyroclastic and transformation textures, and composed of olivine (with kink band), orthopyroxene (with wavy extinction and exsolution clinopyroxene), spinel (like Holly – Leaf and shaped) and less than 10% of clinopyroxene. Two stages of alteration occur in these rocks, including static and dynamic. These peridotites are partial melting residual of spinel lherzolites.The Khoy taconite periodontitis show the U-form pattern in the REEs. These patterns are probably related to the partial melting procedures and the process following the partial melting such as influence of felsic magmas after emplacement of OPHIOLITEs.

Sabzevar OPHIOLITE Zone (SOZ) is located in northern Central Iran (north of Great Kavir fault and south of Miamey fault) and separates Kopp e Dagh sedimentary basin (in the north) from the Central Iran plateau (in the South). The evolution and replacement time of this OPHIOLITE complex has been in the Upper Cretaceous) Santonian – Campanian) and the Middle Campanian to Upper Maastrichtian respectively. This OPHIOLITE belt contains a high amount of ultramafic rocks, small masses of gabbros and a thick sequence of submarine basaltic lavas with Upper Cretaceous pelagic limestone and radiolarite, which are angular unconformable and have a base of conglomerates of volcanic and sedimentary rocks. This study examines the brittle structures of SOZ and carries out a geometrical analysis. The purpose of this study is to obtain a suitable structural model consistent with the area structures. In this paper, the geometrical condition is compared with all the area structures and a logical relationship between fractures has been identified. Also the relationship between the regional macro-structures and area fractures has been identified. For this purpose during the field visits and study of the satellite imagery, structures and exposure which make the base of a structural map of the area have been provided.. Then with the surveyed data and provided rose and contour diagrams the main direction of fractures and the pattern of orientation were obtained. This direction is N59W, the same trend as the Miamey fault. The structures in the region are affected by this fault. If this direction is considered the main right-lateral shear trend, other trends are consistent with pattern of fractures orientations Related to fault cutting. Generally the fractures with N14E, N68E, N86E, N77W, N59W and N41W trend, respectively are consistent with type X, R', T, R, D and P fractures.

The Kahduiyeh tectonized OPHIOLITE exposed at the extreme northern part of Dehshir-Baft OPHIOLITE belt in the southern margin of centeral Iran microcontinent, comprise of mantle peridotites and crustal sequence. The serpentinized peridotites have cpx- bearing harzhburgite and lherzholite compositions which cross cut by diabase isolated dikes. The plutonic part of crustal sequence consist isotropic gabbro, diabase sheeted dike complex, intruded by wherlitic intrusion, quartz diorite, pegmatite gabbro and plagiogranite-tronjemite. The volcanic sequence consist of the intercalation of the chert and radiolarite, pelagic limestone have the Upper Cretaceous micro faunas at base of sequence and hyaloclasic braccia, hyaloclastite, sheet flow, tuff and pillow lave on top of the sequence. Study of chemical analysis indicating a suprasubduction origin and enrichments for REE, Rb, Ba and Th might be affecting of slab-derived fluids. It seem that Kahduiyeh tectonized OPHIOLITE display a consistent sequence of events during their formation and evolution, includes birth, youth and maturity stages which is a natural consequence of OPHIOLITE formation in the Supra-subduction zones.

The principal rock units are a gabbro sequence, late intrusive rocks that consist largely of the plagiogranite and volcanic rocks, which are largely pillow basalts interbedded with pelagic sedimentary rocks, including radiolarian cherts. Chondrite-and primitive mantle-normalized incompatible trace element data indicate that the Lahroud OPHIOLITE was derived from a within plate basalt-like mantle source. All rocks are cogenetic geochemically and were derived by fractionation from melts with a composition similar to average E-MORB with calc-alkaline signatures. Plate reconstructions suggest that the rocks appear to be approximately contemporaneous with the Mashhad OPHIOLITEs and Rasht OPHIOLITE, which has a crystallization age of ~380 Ma. Rocks from the Lahroud OPHIOLITE complex represent northern Paleo-Tethyan ocean crust that was formed distinctly earlier than crust preserved in the Ma Paleo-Tethys suture zone OPHIOLITE from upper Paleozoic to Later Teriassic. The results from microfossil studies show the presence of Paleozoic biostratigraphy (e. g., Paleotextularia, Nodosinella cf. concinna, Pseudokahlerina, Cylindrica, Earlandia, Endothyra baileyi, pachyphloia, Fusulinella Stafella and Bivalve, Paratikhine). The data suggest that although the initial rifting and crystallization of the oceanic crust of the Lahroud OPHIOLITE began in the Carboniferous, with volcanic activities continuing through to the late Triassic.

Siahjangal OPHIOLITE is located in the North and Northeastern part of Taftan volcano in the Sistan Suture Zone (SSZ). This OPHIOLITE (Upper Cretaceous) is exposed in the Flysch rocks (Eocene). Harzburgite, lherzolite, serpentine, spilite and gabbro are major rocks in this OPHIOLITE. Ultramafic units have olivine, orthopyroxene and clinopyroxene minerals. Mafic units have clinopyroxene and plagioclase. Ultramafic rocks have mainly granular and gabbro rocks have ophitic, sub-ophitic and granular textures. Geochemical verities of major, minor and rare earth elements in the Siahjangal OPHIOLITE revealed that the ultrabasic and basic rocks were formed due to partial melting than crystal differentiation. REE elements diagrams normalized to the Chondrite and MORB and their comparison with the normal and enriched MORBs, chemical differentiation diagrams, the ratios of accessory elements and changes of Zr, Nb, Y, U, Ti elements against Zr / Nb ratio all indicates the similarity to N-MORB. Transition elements diagrams (V, Co, Cr, Ni) against La / Ce ratio and the ratio of (La / Yb) N, La / Yb, La / Ce versus (La / Sm) N, show that these ratios compared with N-MORB and E-MORB represent enrichment and geochemical similarities to N-MORB. Tectonomagmatic diagrams show Siahjangal OPHIOLITE belongs to supra-subduction zone.

Two types of rodingitization (static and dynamic) are observed in the rodingites of the OPHIOLITE in the North Of Nain. Two stages have occurred in the formation of static rodingites. In the initial stage, epidote, prehnite and hydrogrossular have crystallized respectively, at the expense of plagioclase, with the increase of calcium content rodingite forming fluid. In the advanced stage, xonotlite in the expense of plagioclase, and Mg chlorite, tremolite and secondary diopside, at the expense of pyroxene, have been formed simultaneously with an increase of Si content of rodingite forming fluid. During rodingitization, the Ca and OR content, have increased, whereas the amounts of K, Al and Na are reduced. Mn, Fe and Mg values are slightly reduced but Si remains constant.

In this study, some mantle lherzolites of Ashin OPHIOLITE are investigated which contain evidence of a geotectonic/metamorphism during exhumation and obduction of oceanic lithosphere on the continental crust, after closure of Neo-Tethys Ocean. Based on petrography, their primary rock-forming minerals are orthopyroxene, clinopyroxene, olivine, and chromian spinel. Mineralogy and geothermobarometry indicate that these 4-phase lherzolites were formed in the lithospheric mantle (at pressures ~ 21. 6 to 8. 6 kbar) by melt/wall rock reactions (at temperatures ~ 1012-1183 ° C). Then, they were emplaced and obducted on the continental crust along the fault zone of this region, and consequently deformed. The first ductile deformation event occurred in the depth of lithosphere and resulted in high-temperature mylonitization at temperatures higher than 600 to 800 ° C. Mineralogical features confirm pressure decreasing of this stage by subsolidus reaction of pyroxene and spinel and substitution of plagioclase and olivine. Therefore, petrography and thermobarometry data are indicative of the spinel to plagioclase lherzolite facies for these rocks. Finally, they partially underwent brittle and cataclastic deformation at temperatures below 600° C and lower pressures and depth during exhumation. However, most of plagioclases were replaced by with prehnite, pumpellyite, chlorite, hydrogrossular and xonotlite minerals by further alterations.

The Nehbandan OPHIOLITE complex (NOC) crops out in the Sistan suture zone, which marks the boundary between the Lut and Afghan continental blocks in the east Iran. After field studies in this area, 21 thin sections plus 32 polished sections were prepared for petrological and mineralogical studies, respectively. Furthermore, 6 least-altered and fractured samples were selected for geochemical studies. Major oxides were determined using XRF analyses.9 samples were selected for ICP-OES and Fire Assay analysis.Three different sequences of ophiolitic rocks can be recognized in the NOC: 1) mantle derived peridotites consisting of clinopyroxene- (Cpx-) rich harzburgites and depleted harzburgites; 2) olivine websterite-pyroxenite-gabbronorite sequence; 3) wehrlite-troctolite-cumulate gabbro-basalt sequence. Clinopyroxene bearing harzburgite and harzburgite are common rock types in the area. These rocks underwent strong serpentinization, during sea floor hydrothermal alteration. Listvenite occurs as dykes or pods in the peridotites. In the study area, more sulfide mineralization (chalcopyrite, chalcocite, covellite, digenite and bornite) occurred in the Cpx-rich harzburgite rocks. In addition of sulfide minerals, native copper, oxides minerals such as cuprite-tenorite and carbonate of copper was observed. Petrographic investigation of sulfides in host ultramafics indicated two sulfide generations. In the first generation, primary magmatic sulfide minerals occurred as interstitial disseminations, generally as anhedral grains. In the second generation, sulfide minerals formed as veinlets along host rock fractures. Grade of gold in mineralized samples is high and shows good correlation with copper and iron elements, whereas free mineral of Au wasn't recognized. Considering the extensive outcrops of serpentinized ultramafic rocks and listvenite in the region can be considered the source of Cu, Au and Fe in related to serpentinized ultramafic rocks.