The Mamzar granitoid pluton is located in the Kerman Province and structurally in southeast of Urumieh-Dokhtar magmatic zone. Based on petrographic studies, the granitoid consist of four rock type of diorite, tonalite, granodiorite and monzogranite. They are mainly composed of plagioclase (andesine), alkali-feldspar (orthoclase), quartz, amphibole (magnesiohornblende), biotite and clinopyroxene. Mineral chemistry of plagioclase indicate that their composition are andesine with An33-47 and the amphibole (calcic) have magnesiohornblende compositions that is feature of I-type granite. The biotites with Fe/ (Fe+Mg)>0. 33 are magnesio-biotites. Based on TiO2 versus Al2O3 diagram, composition of amphiboles indicate crust and mantle mixing in the formation of the Mamzar granitoid magma. Application of different barometers and thermometers such as Al-in-hornblende, plagioclase-amphibole pair exhibit an average pressure of 1. 14 kbar and temperatures of 660-730 ° C for the intrusion. The mineral chemistry of the biotites and amphiboles indicate that this granitoid pluton is calc-alkaline and formed at the depth of less than 8 km.

Metamorphic rocks in the Faryab complex are part of the Bajgan metamorphic complex with Upper Cretaceous age that crops out in the southeast of Sanandaj-Sirjan zone, south Iran. The metamorphic rocks of Faryab Complex have been metamorphosed in greenschist and amphibolite facies include garnet mica schist, epidote schist, epidote amphibole schist, amphibole schist, epidote amphibolite, amphibolite and garnet amphibolite. Minerals composing amphibolites are garnet, amphibole, epidote, plagioclase, quartz, chlorite and sphene as well as titanite and magnetite as secondary minerals. The composition of amphiboles in amphibolite and epidote amphibolite are made of calcic types and their chemistry varies from magnesio-hornblende through ferro-tschermakite-hornblende, ferro paragasite-hornblende, ferro edenite-hornblende to ferroedenite. The composition of plagioclas ranges from albite to oligoclase. The protolith of most amphibolites and epidote amphibolites in the Faryab complex are defined by the occurrence of key minerals in metabasites and are considered as basalt and gabbro. Several thermobarometeric calculation methods indicate that the highest temperature and pressure for the amphibolites, which were appeared adjacent to peridotites and located in the northern part of the complex, are about 700 °C and 9. 7 kbar. By moving away from the peridotites into the lower structural units in the southern part of the Faryab complex, the temperature and pressure range in the amphibolite and epidote amphibolite and decrease to 510°C and 4. 34 kbar on average, which is beginning of amphibolite and middle amphibolite facies. Investigation of the P-T pathes in conjunction with close associations of isograde lines show that geothermal gradients were high even at the beginning of metamorphism. Mineral chemistry and thermobarometric calculations along with consideration of the structural position of the Faryab complex indicate that the tectonic position of the Faryab complex in the Sanandaj-Sirjan zone may remined us an accretion-subduction complex. This complex was constructed in the north-dipping Neo-Tethyan subduction zone during the Late Cretaceous time, which caused the higher degree metamorphic rocks were thrusted onto the shallower ones.

Introduction The Sabalan is one of the Pliocene-Quaternary volcanoes in northwestern Iran. Based on the activity history, the Sabalan volcanic rocks can be classified into two rock groups: Paleo-and Neo-Sabalan volcanic rocks. Paleo-Sabalan was constructed during the Pliocene-Pleistocene inmultiple eruptions between 4. 5 and 1. 3Ma, whereas Neo-Sabalan activity initiated after a series of violent explosive eruptions during the middle to late Pleistocene (545 to 149 ka,Ghalamghash et al, 2016). The Paleo-Sabalan volcanic rocks are trachy-andesitic to andesitic and rarely trachy-dacitic and Neo-Sabalan volcanic rocks are generally dacitic to andesitic. Materials and methods Field investigation and sampling, petrography and mineral geochemistry are different part of our studies during this project. Mineral chemistry have been performed on two thin-polished sections of Paleo-Sabalan olivine basalt and Neo-Sabalan trachyandesite in Iran Mineral Processing Research Center. In this center, a Micro-probe model EPMA Sx100 model made by Cameca company with a voltage of 15 kV (Kv: 15 Kev), current intensity of 20 nm (nA), a diameter of 5 um and a detection limit of 500 ppm for microscopy and point chemical analysis Used. Sample preparation for microprobe studies has also been done in Iran Mineral Processing Research Center using carbon coating device. Results and discussion Plagioclase composition in the Paleo-Sabalan volcanic rocks in the oligoclase to andesine range, and in the Neo-Sabalan volcanic rocks in the range of oligoclase, to andesine. K-feldspars are sanidine and orthoclase. The Olivine and pyroxenes of the Paleo-Sabalan volcanic rocks have chrysotile and diopside-augite compositions, respectively. The most of the mica in Neo-Sabalan lava are Biotite. The most amphibole of Neo-Sabalan lavas are Magnesiohornblende, and rarely are edenite. Based on the mineral chemistry diagrams of Sabalan volacic rocks have a sub-alkaline and calc-alkaline nature that have formed in the orogenic environment. Paleo-Sabalan clinopyroxenes have crystallized at 5 to 10 kbar pressure (equal 17. 5 to 35 Km depth). The amphibole phenocrysts have crystallized at a pressure of 1 to 3 kbar (equal 3. 5 to 10. 5 Km depth) and a temperature of about 725 to 750 °C. Conclusion Considering the crystallization temperature of amphibole (725 to 750° C) and biotite modeling with FMQ buffer oxygen fugacity at the time of biotite crystallization was estimated to be-16 to-16. 50. Probably, high oxygen fugacity and the presence of aqueous minerals indicate the effect of water-rich old subduction environment on the source of primary magma of Sabalan volcano.

The kalasur_Kharil granitoid complex with Oligocene age, is located in SW Kaleybar of NW Iran, Alborz-Azarbaijan zone. The rocks  are  intruded into the Cretaceous  volcanic and sedimentary rocks. The composition of plutonic rocks are consist of  gabbro-diorite, diorite, quartz monzodiorite and granite. The major minerals in gabbro-dioritic and dioritic rocks are plagioclase, clinopyroxene, amphibole, biotite and major minerals in quartz monzodioritic and granitic rocks are potassium feldspar, plagioclase, quartz, amphibole and biotite. On the basis of mineral chemistry, the composition of clinopyroxenes is in diopside range. Amphibole minerals are calcic in study area. The calcic amphiboles indicates that the rocks of the studied area belong to type I granitoids. The Khari- Kalasour amphiboles are magnesio hornblende. The biotite in Kharil- Kalasur granite with Fe/(Fe+Mg)>3 is magnesio-biotite. The feldspar composition is albite-andesine in granite, labradorite, andsine and orthoclase in dioritic and quartz monzodioritic rocks. Mineral chemistry of the biotite, amphiboles and pyroxenes indicate that this rocks are calc-alkaline and have been crystallized in a subduction zone setting.

Kuh e-Dom intrusion, located at the northeast of Ardestan, consists of granodiorite and diorite. The granodiorites have been intruded by various basic dikes. Plutonic rocks are mainly composed of plagioclase, biotite, amphibole, pyroxene, alkali-feldspar and quartz. Based on microprobe analysis, the biotite is classified as magnesiobiotites which typically occur at calc-alkaline orogenic igneous rocks. The amphibole belongs to calcic-amphibole group but its composition varies from magnesiohornblende to actinolite in granodiorite and from hornblende-actinolite to actinolite both in diorite and basic dikes. The plagioclase also shows variable composition from oligoclase to andesine in the granodiorite and from andesine to labradorite both in diorite and basic dikes. Based on the mineral chemistry data, the equilibrium temperature of the mineral crystallization is estimated at about 700°C, the pressure equilibrium occurred at ~1.5 Kb, which is consistent with a depth of 5.5 Km.

1-Introduction: Bazman volcano is located on Chgay-Makran magmatic arc. This magmatic arc with east-west trend is 500 km long and 150 km wide and extends from southeastern Iran to southwestern Pakistan. Early evolution of the Makran zone from the upper Oligocene to the upper Miocene is characterized by turbidite sediments deposited on the oceanic crust. There are several quaternary volcanoes such as Bazman, Taftan, Shahsavaran and Soltan (southern Pakistan) which situated along northward of Makran subduction zone as continental arc magmatism. Bazman volcano as an astratovolcano have been explosive and non-explosive eruptions in Quaternary. The purpose of this paper is to investigation of mafic minerals chemistry and thermobarometry of Bazman Quaternary volcanic rocks. 2-Materials and Methods: Based on field studies, its volcanic rocks are classified into two groups Quaternary and Neogene volcanic rocks. Petrographic studies were conducted with the preparation of thin sections of rock and were named rocks. Three samples Quaternary units (Qa1, Qa2, Qa3) were selected for microprobe analysis. Mineral analyses were conducted at Iran Minerals Processing Research Center Electron Microprobe Laboratory using a Cameca SX100 electron probe microanalyzer outfitted with combined WDS and EDS systems. The analyses were conducted at an accelerating voltage of 15 kV and a beam current of 10 nA. 3-Results and discussion: According to Petrographic studies, unit Qa1 was formed of andesite, andesitic basalt, basaltic andesite and andesite lithic crystal tuff, unit Qa2, andesite to trachyte andesite and basaltic andesite, unit Qa3, andesitic basalt, olivine basalt and basaltic andesite. 3 sample basaltic andesite and olivine basalt Quaternary units were selected for mafic mineral microprobe analysis. Olivine phenocrysts of olivine basalt are chrysolite mineral. Clinopyroxenes are augite and orthopryoxene are clinoenstatite. Amphibole minerals are hornblende, magnesio-hornblende, hastingsite hornblende, tschermakite hornblende and tschermakite. Pyroxene composition in igneous rock depends on the chemical composition and tectonic setting of the host lava which can be used widely to determine the series of magmatic and physicochemical conditions such as pressure, temperature, oxygen fugacity. Ca+Na vs Ti diagram define that the pyroxenes occur in the range of tholeiitic calc-alkaline. Al2O3 vs TiO2 diagram was drawn to identify the nature of magma. This diagram shows orthopyroxene of both the Quaternary units and clinopyroxene unit Qa1 calc-alkaline ranges and clinopyroxene unit Qa2 tholeiitic tendency. The chemical composition of the samples pyroxenes evaluates the physicochemical conditions of magma such as pressure, temperature, oxygen fugacity. Using Al IV + Na vs Al IV + 2Ti + Cr diagram which depend on the amount of 3-valent iron in pyroxenes, we can get oxygen fugacity. The diagram is set based on the aluminum balance in the tetrahedral position and Cr3+in the octahedral position. The Fe3+ in pyroxenes can be displaced 3-valence elements such as AlVI, Ti and Cr in the octahedral position. In the other hand, Fe3+in pyroxenes depends on the amount of AlVI which means that it depends on the aluminum balance in tetrahedral and octahedral position. The pyroxenes which crystallized at high oxygen fugacity, has been situated above the line of Fe3+. Furthermore, Papike and Cameron (1976) have mentioned the distances of the samples from the Fe3+ line and noted that further distances of the samples from this line were indicating more oxygen frugalities in their geological setting. In this diagram samples are located above the line of Fe3+. In order to study thermodynamic conditions pyroxene crystallization is used methods Soesoo (1997) and Patrikia (2008). By Soesoo (1997) clinopyroxene samples operating temperature range 1200c°-1300c° and comprised approximately at 1250 c° . Orthopyroxene samples are composed at temperatures from 1150c°-1200 c° . Accordingly, the pressure range of clinopyroxenes is 6-10 kbar and Orthopyroxenes 2-5 kbar. By Patrkia (2008) orthopyroxenes crystallization temperature Qa1 unit is 1124c° and clinopyroxene and 1145c° and the setting pressure at the orthopyroxene is 5 Kbar and clinopyroxene 8 Kbar. Orthopyroxenes crystallization temperature Qa2 unit is 1068 c° and clinopyroxene and 1100 c° and the setting pressure at the orthopyroxene is 2. 2 Kbar and clinopyroxene 4. 3 Kbar. According to both methods clinopyroxene crystallization, temperature is higher than orthopyroxene in Quaternary units. Temperature and pressure of the magmatic Qa1 little more than Qa2. Reduce pressure and temperature conditions of crystallization orthopyroxene can be attributed to an increase in the amount of iron in the crystal lattice orthopyroxene. The temperature and pressure determined on the basis of the mineral olivine in olivine basalt rock (Qa3 unit) are about 1100 ° C and 5. 5 Kbar. 4-Conclusion: 3 sample Quaternary units were selected for microprobe analysis. According to the pyroxenes chemical composition in basaltic andesite rock, orthopyroxene of both the Quaternary units and clinopyroxene unit Qa1 are calc-alkaline ranges and clinopyroxene unit Qa2 is tholeiitic tendency. The pyroxenes which crystallized at high oxygen fugacity. Clinopyroxene crystallization temperature is higher than orthopyroxene in Quaternary units. Temperature and pressure of the magmatic Qa1 little more than Qa2. Reduce pressure and temperature conditions of crystallization orthopyroxene can be attributed to an increase in the amount of iron in the crystal lattice orthopyroxene. It could be related to tholeiite conditions magma before crustal contamination. The average pressure and temperature of the Quaternary magma chamber based on mafic minerals can be estimated at 1141 ° C and 5. 5 Kbar.

Hercynite-rich spinel is a typical mineral of both quartz-bearing and quartz-free metapelitic rocks that form under low-pressure high-temperature conditions in the granulite facies (Sengupta et al., 1991) or upper-amphibolite facies of regional and contact metamorphism (Pattison and Tracy, 1991). Temperature-pressure estimation of metamorphic terrains is necessary to understand how large-scale crust evolution has occurred. High-temperature phase equilibrium cannot be properly evaluated solely based on normal cationic couple geothermobarometers, as ferromagnesian cationic exchange undergoes processes related to retrogression during cooling after peak metamorphism. Instead, key mineral parageneses are preserved and standard petrogenetic grids study based on reaction textures and mineral chemistry can be very helpful in better estimating temperature pressure. Regional Geology Dorbeh's contact aureole is formed in West Azerbaijan province, south of Urmia, north of Oshnavieh, and the Sanandaj-Sirjan zone around Dorbeh diorite. The intrusion is one of the components of the Urmia Plutonic Complex (UPC) which is spread along with granites and alkali syenites/granites at the northwest end of the Sanandaj-Sirjan zone in the south of Urmia. This diorite intruded sedimentary units of shale and carbonate belonging to Permian to Triassic-Jurassic including the Doroud and Ruteh Formations and have metamorphosed them in contact aureole, causing hornfels and calc-silicate to sometimes scarn deposits in the area (Modjarrad and Mohamed, 2015). This intrusion is covered by Miocene units (Ghalamghash, 2009). The observed parageneses in Dorbeh aureole including Cld + Chl, Ctd + And, Alm + Cld, And+Alm, Hc+Alm, Chl + Hc + And + Sil, Alm + And + Sil, Alm + And + Sil + Hc. The peak metamorphism assemblage is Alm + And + Sil + Hc. The reactions responsible for the parageneses productions were introduced in the previous studies (Modjarrad and Mohamed, 2015). Materials and Methods 50 microscopic thin sections were prepared and petrographically examined. A reagent sample with the highest number of parageneses and experienced peak metamorphism was analyzed by JEOL JXA-8200 microprobes electron device for garnet, chlorite, chloritoid, spinel, iron oxide, aluminosilicate, and apatite at the University of Potsdam, Germany. For whole rock chemistry, several metapelite samples were analyzed by XRF at the ALS-Chemex Laboratory of Canada. Discussion and Conclusions The main purpose of the present paper is to investigate the parageneses, the mineral chemistry, and the temperature-pressure estimation in the metamorphic contact aureole around Dorbeh intrusive. This intrusion consists of amphibole, plagioclase, and clinopyroxene, is a part of the Urmia Intrusive Complex (UPC), and with dioritic composition was intruded the Upper Cretaceous into the Paleozoic pelitic and limestone sedimentary rocks and metamorphosed them. The metapelite section of the aureole has exhibited interesting parageneses due to the exceptional iron-rich composition of the protolith. The hornfels part of the Dorbeh aureole is dominated by chlorite + chloritoid + garnet + aluminosilicates + spinel + opaque minerals and less quartz in the matrix. Mineral chemistry studies showed that Fe-chlorite between Repidolite to Bronswigite, Fe-chloritoid, Almandine garnet, Hercynitic spinel, and ilmenite are the minerals composition which is in agreement with the Fe-rich content of the parent rock. There was no specific zoning pattern in the metapelites garnet grains. It was also found that there is a reverse relationship between Si content and iron, magnesium, titanium, and chromium in chlorite and aluminosilicate structures. The metamorphic conditions for Dorbeh aureole by the multi-equilibria method by THERMOCALC software have been estimated at 570±7°C, at a pressure of 2. 8±0. 2 kbar. Detailed investigation of phase relationships of metamorphic rocks can be considered a desirable method along with quantitative data-based methods to evaluate the occurrence of progressive metamorphism. This method is based on direct observation of reaction textures and is more objective in estimating metamorphic conditions by the method of the intersection of equilibrium reactions. Most of the time, secondary cationic exchanges penetrate from the mineral boundary to a considerable stratum and question the accuracy of the temperature and pressure calculated on the cationic couple's geothermometers to a large extent. The contact aureole with higher than normal temperatures specific to the margins of dry mafic intrusives is sometimes associated with the formation of special parageneses such as Grt+Sil+And+Hc. This paragenesis has also been reported from high-temperature (granolithic) regional metamorphic terrains, but its production conditions are more limited in contact aureoles and require a high molar fraction of iron/aluminum or mass dryness and/or aureole. Therefore, the composition of all ferromagnesian minerals is very close to the final iron end member and no specific temperature fluctuation in the aureole is understood from the garnet zoning pattern. Although staurolite has not been seen in the studied sections, the evidence suggests that hercynite in the area was caused by staurolite breakdown. With precision in the composition of analyzed chlorites, it was found that there is a direct relationship between Si and alkaline content in chlorite structure, but titano-ferromagnesian content is in contrast with Si content. An almost similar relationship was observed in the aluminosilicate crystals. The inverse relationship between silica and Fe, Ti, and Cr oxides prevails.

2The study of granitoides bodeis in the west of Taft, is located in the middle part of the central Iran, indicates the presence of quartz, orthoclase, plagioclase minerals as main minerals and amphibole, biotite, sphene, zircon and apatite as secondary minerals. In these rocks, medium-grained to fine-grained, granophyric and myrmikite textures are observed. The data of mineral chemistry analysis show that calcic type amphiboles of magnesiohornblende to actinolite nature belonging to temperature 659-891 C, pressure 2.1- 4.9, and depth 4.4- 6 have been crystallized. However, feldspars are oligoclase to andesine type that belonging to 700-800 C, and biotites have been crystallized 700-750 C. The minerals chemistry of biotite was indicated to the mantle nature of the magma, which has suffered from moderate to severe crustal contamination during ascent. The mineral chemistry of chlorite refers to the involvement of alteration processes and the formation of this mineral at the temperature of 330 to 360 C. All of the data indicates to the calc-alkaline granitoides I type, which were formed in the structural zone of subduction and in connection with the active continental margin

The cratonic basement in the Kabul district is dominated by gneiss, migmatite, schist, and amphibolite and is characterized by extensive outcrops. Orthopyroxene and garnet are the index minerals of some of the gneisse, hence, they are considered as charnockite. Biotite, quartz and feldspar are the rock-forming minerals of the migmatites and their modal abundances vary between melanosome and leucosome. The predominant minerals of the schistic samples are garnet, kyanite, quartz, feldspar, muscovite and biotite. Amphibole (pargasite), garnet and plagioclase are the essential minerals of amphibolitic samples. Based on thermocalc software, petrogenetic grade and conventional thermobarometers the calculated average pressure and temperature for charnockitic, schistic and garnet-amphibolitic samples are 7. 03 kbar and 590 ℃ , 9. 94 kbar and 518 ℃ and 9. 24 kbar, 664 ℃ respectively. The mineralogical paragenesis and the geothermal gradient resulted from thermobarometry calculations of metamorphic basement of the Kabul block is in accordance with metamorphic gradient of collisional orogenic belts. The cratonic basement of the Kabul block is possibly representing metamorphic rocks of the deep level of Proterozoic collisional orogenic belts during the formation of Columbia and Rodinia supercontinents.

Soltanabad metamorphic complex cropped out in the ophiolitic range of NE Sabzevar. There is a distinct gneissic body exposed in this complex which is associated with metabasite, serpentinite and adakitic intrusions. Quartz, albite, epidote, amphibole, garnet and chlorite are the rock forming minerals of gneissic samples. Based on abundances of light and dark minerals, different types of felsic, intermediate and mafic gneisses are distinguishable. Metamorphic conditions of the Soltanabad complex gneisses is estimated as 462 (± 39)° C at pressure of 12. 4 (± 2. 15) kb indicating a hot thermal regime of a subduction setting. Based on the whole rock geochemistry gneisses have plagiogranitic composition and formed by partial melting of mafic sequence in oceanic crust. Isotopic ratio of zircon’ s Hf and REE pattern confirm a MORB affinity of these gneisses. The Soltanabad metamorphic complex gneissesdisplay considerable compositional similarity with plagiogranite of Iran and Cyprus ophiolitic zones and thier geochemical characteristics are comparable with plagiogranites of supra-subduction zone setting. Probably gneisses and blueschists of the Soltanabad metamorphic complex are plagiogranites and mafic rocks of the Sabzevar oceanic lithosphere that experienced subduction zone metamorphism.