Triassic (mostly volcanic-carbonate) and Jurassic (mainly shale and sandstone) rocks in west of Malayer were affected by a number of shear zone, folding, deformation and metamorphic events. Regional metamorphism in the area led to the formation of Triassic and Jurassic rocks such as phyllite, slate and crystalline carbonate which folded during deformational events. In the contact metamorphism event, granitoid plutons with predominantly granodiorite to quartz-diorite composition intruded the metamorphic rocks, forming MINERALized skarn zones in Anjireh, Iraneh and SarabSaman areas. The present research shows that plutons producing the MINERALized skarn zones in the area are on average granodioritic in composition.Pyroxene and garnet MINERALs in the skarn zone comprise of diopside, augite and grandite (mainly andradite), respectively. In these skarns, various sub-zones are recognized and defined on the basis of their MINERAL PARAGENESIS. High temperature facies (pyroxene-fels) formed in the temperature range of 650-800 oC and wollastonite up to 800 oC. However, hornblende-fels and albite-epidote-fels facies formed in the temperature ranges 500-650 and 350-500 oC, respectively.

The Vejeh Skarn is located at 70 km Northeast of Isfahan. The Vejeh intrusive body with granodiorite to tonalite composition have been intruded the lower Cretaceous marl carbonate which caused the formation of skarn rocks. On the basis of field and MINERALogical studies skarn type is calcic with low Mg amount. The MINERAL assemblage including wollastonite, pyroxene, garnet, epidote, quartz and calcite, have been taken place at progressive and retrogressive stages. Wollastonite and pyroxene (diopside – hedenbergite) were formed at primary progressive stage whereas garnet (grossular-andradite) was formed at secondary progressive stage through metasomatism of pyroxene and wollastonite. In the retrogressive stage with increasing ¦O2, the garnet was altered and replaced by epidote and secondary calcite and quartz. Regarding MINERAL assemblage it could be deduced the temperature of skarn formation have been reached to 500 -700oC in the progressive stage and then decreased to 470oC in the late stage.

Estimation of temperature-pressure deformation path for metamorphic rocks experiencing a complex deformation history commonly rely on the relationship between successive metamorphic assemblages and different microstructures that remain. However, by changing the temperature-pressure conditions, metamorphic MINERALs with a microstructure, which are specific to those conditions, can be chemically reequilibrate. Mylonitic paragneisses around the lake of Zayandehrood Dam, have range low-grade to medium-grade mylonites. According to petrographic and microstructural studies, we define at least three stages of metamorphism and deformation. The first stage metamorphism (the earliest recognizable metamorphic stage) took place during eclogite facies conditions. At this stage, high pressure MINERALs such as rutile and graphite formed that enclosed in garnet or feldspar. These hosted garnets and feldspars based on the evidence of petrography formed at the amphibolite facies condition. Eventually a retrograde metamorphism took place in the lower greenschist facies condition, That’ s evidence includes the sericitization of some feldspars, the choloritization of some biotite, and the formation of chlorite and quartz in and around some garnets. Contemporaneous whit these retrograde processes, there is evidence of relatively high-temperature to low-temperature deformation microstructure. The combination of evidence of metamorphism and deformation results is that these rocks have risen from relatively high depths, which during the rising stages undergone the various metamorphism condition, and many deformations have affected on this collection.

MINERALogy, gold MINERALization and metal contents of the Gadir deposit have been investigated during current research in order to determine the geological conditions, temporal and spatial relationship with certain MINERAL assemblages and associations. The MINERALogy of orebodies is mainly composed of pyrite, chalcopyrite, sphalerite, galena, petsite, native gold, electrum and subordinate molybdenite. Gold is hosted by pyrite and chalcopyrite MINERALs in fracture-filling textures and forms a thin dispersion condition. The native gold was observed in chalcopyrite, which is probably related to the second stage of ore deposition. The Gadir deposit can be classified to Au-Ag-Cu-Zn± Pb stockwork-type MINERALization which is characteristic of low sulfidation epithermal deposit.

MINERALogical and geochemical investigations indicate two general stages of skarnification i.e, prograde and retrograde stages in the Mohammad-Abad district, south west of Yazd province. Metasomatic skarn (Prograde stage) occurred with precipitation of anhydrous calc-silicate MINERAL assemblages (andradite and diopside-hedenbergite) within the temperature ranges of 470 to 550oC. During the retrograde stage (<470oC) considerable amounts of anhydrous calc-silicates were altered and replaced by a series of hydrous calc-silicates (epidote, tremolite–actinolite). Finally, both anhydrous and hydrous calc-silicates were altered to fine aggregates of chlorite, calcite, quartz and clay MINERALs at temperatures lower than 300 oC. The absence of wollastonite among the calc-silicate assemblages may suggest that andradite and hedenbergite were crystallized from metasomatizing fluids at lower than 550 oC in the Mohammad-Abad skarn. The presence of intergrowth texture and non-replacive crystal boundaries between garnets and pyroxenes suggest that they were formed contemporaneously within the temperature and fO2 ranges of 430–550oC and 10-26–10-23, respectively. Andradite converted to quartz, calcite and magnetite below 470 oC and fO2=10-24–10-21. Since, both magnetite and pyrite along with quartz and calcite are present in MINERAL assemblages of sub-stage III, it can be reasoned that the metasomatizing fluids probably had an approximate fS2 10-6.5 and a temperature of about 430 oC.

The studied diabase rocks of the Hormuz Formation have undergone a variety of secondary processes and greenschist facies to amphibolite facies metamorphism. These rocks are metasomatized due to the effect of infiltrating metasomatism and hydrothermal alteration and are metamorphed due to CO2-rich aqueous fluids and rock-fluid interaction. Feldespat, pyroxene, olivine, apatite, rutile, magnetite and pyrite are the primary magmatic MINERALs present in these rocks and other MINERALs, are products of the transformation of the primary MINERALs due to metasomatism and thermal metamorphism. Feldspars are labrador, albite and orthoclase. Labrador and albite were crystalized at tempretures of <700 and pressures of <6 kbar which is their recrystallization tempreture. Orthoclase was crystalized at tempretures and pressures of 700, 6 kbar and >1000, >7 kbar and is a magmatic MINERAL. Clinopyroxens are augite and diopside and were crystalized at 1100 to 1300 and are magmatic MINERALs. Pyroxenes are subalkaline to alkaline and were formed within plate tholleitic basalt or oceanic floor basalt environment. Plagioclase and pyroxene MINERALs show oxidation conditions. According to the analyzed zircons from Band-e Moullem (539/4 ± 6/4 Ma) and Champeh (543/5 ± 6/1 Ma) salt dome diabase, these rocks have been crystalized and formed during Early Cambrian time. In addition, most of these zircons have a magmatic origin. This estimated age suggests that the intrusion of these diabase, occurred during and/or after the Neoproterozoic to Early Cambrian rifting of the northern part of the Arabian plate and the sedimentation of the Hormuz Formation in the Persian Gulf Basin.

The studied area as a part of Urmiyeh-Dokhtar magmatic arc, situated in NE of 1:100000 geological map of Kahak and about 10 Km south of Fordu village.The genetic type of MINERALization is intrusion related which a dioritic body influenced the country rocks and produced a pyrometasomatic zone of the following MINERALs such as: magnetite- hematite, andalusite-kyanite, hydrogrossular garnet, tremolite- actinolite, epidote, recrystallized carbonate and chloritized biotite. The fluxing agent of this dioritic intrusion varies from its marginal boundary to farther parts. Magnetite and hematite are the initial ore-MINERALs which accompanied by pyrite in places.The metasomatised country rocks are initially Eocene volcanoclastics and associated carbonates. These data have shown that the studied area is a calcic Fe-skarn and also indicates a hornblende hornfels facies of 460 to 12 650o.The skarn production by dioritic body acrossed the Qom formation specially limestones in outer parts of the studied area also occurred, therefore the age of the dioritic intrusion seems to be post Eocene probably middle Miocene.The initial factors controlling the metasomatism mechanism are the dioritic emplacement, its related fluxing agents and the lithology of the country rocks.The tectonomagmatic site of the above dioritic body and associated metasomatism indicate a subduction zone of continental magmatic arc (VAG) based on the related described diagrams.

The Asinawa iron ore is located about 3km to the southeast of Penjween town, Sulaimaniya Governorate, Kurdistan Region, Northeastern Iraq near the Iraq-Iran border. The exposed iron ore deposit is about 60 and 400m wide and long respectively. The present study is the re-study of the geology and geochemistry of the Asnawan Iron ore deposit and concluded that the country rocks are consist of hornfels in which the original lamination or banding of the parent rocks (calc-silicate low grade metamorphic rocks) are preserved and inherited from its laminated sedimentary precursors. Moreover, the facies that is associated with host rocks is hornblende-hornfels facies with temperature range of 550-650 oC. This range is confirmed through thermo barometry. There are evidences of localized pyroxene-hornfels and sanidine hornfels facies too. Additionally, the detail of the different stages of the iron ore PARAGENESIS is shown by discussion with the aid of suitable graphical drawing and geochemical variation diagrams. By these methods, the sedimentary stratigraphic unit of the parent rock (protolith) was found for the first time which consists of Qulqula Radiolarian Formation (Kermanshah Radiolarites in Iran). The bedded chert, limestone and calcareous shale is the main lithology of the latter formation and after burial and deformation, it is regionally metamorphosed to banded and lamiated calc-silicate rocks of green facies rocks. At a later stage, these rocks, remetamorphosed (polymetamorphism pattern) again to hornfels with concurrent changing to iron ore by basic iron rich hydrothermal solutions during Eocene (37-40Ma). This age is calculated using Ar39/Ar40 method of dating.

The study area is located northwest of Gol-e Gohar mine (Bahram Gur Protected Zone) in Sirjan, the Kerman Province, a part of the Sanandaj-Sirjan zone. The area is mainly dominated by metamorphic rocks with their basic igneous origin and sedimentary including slate, phyllite, schist (garnet schist, amphibole schist, mica schist, kyanite schist), epidote amphibolite, amphibolite, gneiss, quartzite and marble. Among the study rocks, amphibolites with different MINERALs PARAGENESIS, have been experienced the highest metamorphic grade to amphibolite facies. The basic igneous rocks ranging in composition from tholeiitic to calc-alkaline are the source rocks of the studied amphibolites and the oceanic crust is their protolith. As the discrimination geochemical diagrams display the amphibolites of the study area probably belong to back arc tectonic environments, which are very similar to mid-ocean ridges (MORB). The primary magma of the igneous rocks and the protolith of amphibolites were derived from spinel-peridotite. Furthermore, on the geochemical diagrams which were used for the purpose of this study, the positive Ba and negative Nb anomalies along with low Nb/U ratio show that the magma of the protolith has been subjected to crustal contamination during rising to the surface. All the geochemical data indicate that the magma has emplaced in a supra-subduction environment related to Neotethys Ocean.

There are metabasite exposures inside ophiolitic belt of northwest Sabzevar that metamorphosed under high pressure granulite facies. On the basis of MINERALogical PARAGENESIS, reactional textures between different MINERALogical assemblages, textural and MINERALogical relations between inclusion and porphyroblast and stability fields of different MINERALogical assemblages, five stages of evolution of metamorphism is distinguished. These stages consist of prograde metamorphic stage (M1), peak metamorphic stage (M2), garnet kelyphitisation as the formation of Pl+Am symplectite and corona (M3), partial or quite replacement of garnet by Am+Chl+Ep assemblage (M4) and the occurrence of Prh-Zl veins. The thermobarometric data of these stages represent a clock-wise P-T path. This path is consistent with the collision of the Iranian micro-continent with the Alborz block and later erosion and uplifting.