محمد ره گشای

The Dalampar ophiolite is an unknown part of the Neo-Tethys ophiolite and is located NW of Iran between Piranshahr and Salmas ophiolites within the Sanandaj-Sirjan metamorphic belt. Serpentinized peridotites, pillow basalt, various gabbro, pelagic limestone, and radiolarite along with volcano-sedimentary units are the main rock types in the area. These rocks are mixed together in most places as tectonic and “coloured” mélanges. Peridotite rocks in the complex were replaced by serpentinite completely or partly due to hydrothermal alteration. Dalampar serpentinites exhibit affinity to the typical metamorphic peridotites with Harzburgitic and Dunitic protolith compositions. Petrographically, they are composed essentially of chrysotile and lizardite with subordinate amounts of chrome spinel, magnetite, talc, calcite, tremolite and chlorite. geochemical features marked by LILE-LREE enrichment, HFSE depletion, and U-shaped chondrite-normalized REE pattern with (La/Sm)N > 1 and (Gd/Yb)N < 1, Suggest multistage petrogenetic processes including refertilization of a depleted, refractory mantle wedge by subduction-derived fluids and boninitic mantle melts operative in an intraoceanic fore-arc environment. The calculated phase diagram for the studied samples shows that serpentinites probably formed in two metamorphism events; the first one includes alteration and hydration of harzburgite in T< 200 Co and P < 4 kbar, while the second one occurred due to increasing T and P to more than 400 Co and 4 kbar.

Ophiolites are slices of oceanic lithosphere obducted onto a continental margin and can be classified as mid-oceanic ridge (MOR) or suprasubduction zone (SSZ) types based on the tectonic setting in which they originally formed (Pearce et al., 2000; Shervais, 2001). The Zagros Orogen extends from eastern Turkey through northern Iraq and northwest of Iran to the Hormuz Strait and Oman (Alavi 1994; McQuarrie, 2003; Homke et al., 2004; Agard et al., 2005; Shafaii Moghadam et al., 2018). The geodynamic evolution of the Zagros Belt is mainly related to the opening and closure of the Neo-Tethys oceanic basin. Ophiolites, as Neotethys oceanic lithosphere remnants, are emplaced along the Zagros Orogen. These ophiolites are emplaced along two main belts (Saccani et al., 2013; Shafaii Moghadam et al., 2018). The Neo-Tethys suture zone coincides with the Main Zagros thrust fault (Agard et al., 2005) and ophiolites are exposed scattered along this zone. 

The Dalampar ophiolite, located between the Piranshahr and Salmas ophiolites. The Dalampar ophiolites consist mainly of strongly sheared serpentinized ultramafic rocks including harzburgite, dunite overlaid by gabbro and basalt units. The emplacement mechanism of the Dalampar ophiolite massifs into the Iranian microcontinent and structural evolution is completely unknown. There has been not performed a systematic investigation of these ophiolites and geodynamic and relation with other ophiolites are not well Studied.
Thus, the main purpose of the present paper is to investigate the petrogenetic processes, tectono-magmatic environment, using mineral chemistry and textural evidences of Dalampar ophiolite which are fundamental for understanding the tectonic evolution of the Neo-Tethyan Ocean.

During the fieldwork, a number of suitable peridotites samples with least alteration effects were selected. Folloing the petrographic studies, a thin polished section was prepared from several harzburgites for microprobe analysis using JEOL JXA-8600 M model,15 kv accelerator voltage and 2-ray current 10-8 Amp, placed at the Department of Earth Sciences and Environment of Yamagata University, Japan.

Harzburgites are the most basic and widespread ultramafic units in Dalampar ophiolite complex. They show evidences including the presence of exsolution of clinopyroxene in orthopyroxene, the orientation and elongation of the crystals indicating these rocks were formed in the upper mantle conditions and reached equilibrium in the crustal environment. Exsolutions of clinopyroxene lamellae from orthopyroxene are one of the textures observed in the rocks under study and is widespread in both abyssal and SSZ peridotites (Tamura and Arai, 2006). The Cr# of spinel in abyssal peridotites is a good indicator of the degree of partial melting for the mantle-derived spinel peridotite. Low Cr# spinels represent less depleted peridotites, whereas the high Cr# spinels highlight more depleted peridotites (Dick and Bullen, 1984; Arai, 1994). in the Mid-oceanic ridges, the degrees of partial melting and depletion are generally low. In contrast, the supra-subduction zone peridotites have a high degree of partial melting and depletion (Niu and Hekinian, 1997). The content of Cr# in presented Cr-spinels are high (78-83%), and associated with boninitic melts formed by high degrees of partial melting or much more extensive melt-rock reaction (Arai, 1994). As the the Cr# of spinel versus the Fo content of olivine diagram shows the harzburgites fall in SSZ domain. Furthermore, all rock types fall into olivine-spinel mantle array (OSMA). This is regarded as the evidence for their residual origin, i.e. they form a trend which was likely caused by partial melting. Experimental studies confirm that the Al2O3 and TiO2 contents, as well as FeO/MgO ratios in chromian spinel are directly related to those of the parental melt (Rollinson, 2008). According to Maurel and Maurel (1982), The Al2O3 contents of the parental melt range from 10 to 11 wt. % for the studied Harzburgites. Such values are consistent with boninitic melts, which typically contain 10–14 wt.%, respectively (Dilek and Thy, 2009). In the Cr# versus TiO2 diagram, the Dalampar peridotites classify as depleted peridotites. In consequence, chemistry of the chromian spinels in the Dalampar peridotites are compatible with a genesis in a suprasubduction zone from boninitic or primitive arc magmas. However, forearc regions may contain both SSZ and abyssal peridotites, although the former are typically dominant (Pearce et al., 2000). Olivine-spinel and orthopyroxene-clinopyroxene thermobarometry in the harzburgites shows equilibrium temperatures of 1000-1100 ºC at a pressure of 28 kbar and suggests that they have been equilibrated in spinel peridotite field.

The Dalampar Ophiolitic Complex as a part of the Tethyan ophiolites is exposed in the northwestern part of the Iranian-Azerbaijan province, extending to the Anatolian ophiolites in southeastern Turkey. The petrography, geochemistry and microstructural studies of the residual mantle sequence in Dalampar Ophiolitic Complex provide important information regarding the degree of partial melting and deformation in the oceanic mantle lithosphere. Mineral chemistry clearly indicate that Dalampar ultramafic rocks record an episode of boninitic magmatism occurred within the southern Neo-Tethys Ocean in the Late Cretaceous. Boninitic melts in Dalampar Ophiolites were formed by partial melting of depleted peridotite, a residue after MORB-type melt extraction. Mineral chemical data indicate that SSZ peridotites are the residues from ∼30–40% of mantle melting. Nonetheless, the very low (< 0.25 wt. %) TiO2 calculated for the parental melt in equilibrium with chromian spinel are only consistent with boninitic-type parental melts. Based on geothermobarometry calibration the temperature and pressure of crystallization of harzburgite rocks were 1000 to 1200 ° C and 24 Kbar, corresponding to the SSZ tectonic environment.

The Laleh-Zar granitoid complex is one of the most important magmatic phases of the Urumieh-Dokhtar belt and is located in the southeast of this belt in Kerman Province, which has a combination of granite and gabbrodiorite. Parts of this vast complex is exposed in the southern part of Hararan region. Based on petrographic studies, these igneous rocks are granodiorite, diorite, and dacite with quartz, plagioclase, amphibole, biotite, pyroxene, and opac minerals. The secondary minerals of chlorite, calcite, epidote and sericite are also present in these igneous units. The results of mineral analysis, using microprobe method, showed that amphiboles are calcite and hornblende. these amphiboles are igneous and belong to the calc-alkaline magmatic series and are of S type (subduction Amphiboles), which are formed in the subductions environment. The pressure and temperature during the formation of these amphiboles were calculated by different methods, therefore the temperature was 650 to 798 degrees Celsius and the pressure was 0.9 to 2.3 kbar. In addition, these amphiboles have high oxygen fugacity and were created at the depths of 9 to 14 kilometers of the earth. Based on the relationships between different elements in these amphiboles, the conducted studies showed that tschermakite and adenitic successions occurred in these amphiboles, but glaucophane, riebeckite and richterite successions did not occur in these amphiboles.

The Lalezar igneous complex is located on the border of the Sanandaj-Sirjan zone and the southeastern parts of the Urmia-Dakhtar volcanic arc and in the northeast of Baft city in Kerman Province. In the northwestern and western boundaries of the intrusive body, there are relatively wide contact metamorphic carbonate rocks. In the southern part of Hararan, the Lalezar igneous body with the Oligo-Miocene limestone and marl complex (equivalent to the Qom Formation), as large contact with metamorphism halo (skarn and marble parts), is the most widespread. Based on microscopic studies, garnet, calcite, wollastonite, pyroxene, olivine, idocrase, and epidote minerals are formed in skarns. Different metamorphic zones including garnet-clinopyroxene, olivine-clinopyroxene, wollastonite-garnet, and garnet-epidote have appeared. Based on the geochemical analysis of the minerals (EPMA), the garnets contain more than 70% grossular (calcium-rich garnet) and less than 30% almandine (iron-rich garnet). The composition of clinopyroxenes belongs to the first group (calcium-iron and magnesium) and of the wollastonite-enstatite type, where the amount of wollastonite is more than 50%. Also, there is less than 10% ferrosilite in the composition of these clinopyroxenes. Based on the garnet-clinopyroxene temperature-pressure measurement, the temperature of skarn formation, based on various equations presented, is between 413 and 530 degrees Celsius and the pressure is 1.5 to 2.5 kbar. The existing paragenesis as well as thermodynamic conditions indicate oxygen fugacity greater than 0.2. This phenomenon indicates the activity of fluids rich in silicate-rich solutions in the formation of these skarns.

The Haji-Abad-Esfandagheh-Faryab ophiolitic belt is one of the most famous chromite-bearing occurrences in the south of Iran that has received considerable attention. Golashkard ultramafic unit includes dunite, highly serpentinized harzburgites, chromitite and wehrlite layers in the Faryab ophiolitic complex located in the southeast of Sanandaj-Sirjan as one of the chromite-bearing areas of the Haji-Abad-Esfandagheh-Faryab ophiolitic belt. Ultramafic rocks and chromitites of Golashkard area consist of 20 to more than 50% of chromite. The studied chromites have variable massive, banded and scattered textures. The geochemistry of Golashkard ultramafic rocks shows that the average Cr# enrichment of chromite in serpentinite rocks (probably dunite and harzburgite) and wehrlite is to Cr/ (Cr + Al) ×100= 70-80 and in chromitite is relatively higher (Cr/ (Cr + Al) ×100= 81). Based on the lithological and mineral chemistry characteristics, Golashkard ultramafic rocks are part of mantle related to ophiolite, which was produced by a homogeneous boninitic melt in the suprasubduction zone and formed high chromium chromitites and related peridotites.

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.

Biotite is usually formed as a rock-forming mineral in a wide range of felsic to intermediate intrusive rocks. Due to complex crystal structure of biotite, different elements can substitute in this rock-forming mineral; therefore can record the physicochemical conditions of the source magma. Based on the chemical classification of mica, the biotites of the igneous rocks, investigated in the Hararan area, can be placed between the poles of phlogopite and annite, and are magnesium type, which indicates their formation in high oxygen fugacity, and according to the amounts of Mg, TiO2 and FeO oxides, these biotites are primary type. These biotites belong to the calc-alkaline magmatic series formed in the subduction environment. Based on the chemistry of biotites, oxygen fugacity in the source magma of Hararan granitoid is in the range of iron oxide. Geothermometry of biotites shows that these biotites formed at temperature ranging between 680 to 780 degrees Celsius and pressure of 2 (1-2) Kbars.

Due to the importance of removing strontium ions in nuclear wastes, in the present work, while synthesizing hydroxybenzaldehyde propyltriethoxysilane ((EtO)3Si-HL) and pyridylmethylidene propyltriethoxysilane ((EtO)3Si-L) ligands, we investigated the properties of silica nanoparticles modified with these ligands as solid adsorbents in The removal of strontium ion from the aqueous solution was investigated and parameters such as pH, time, the mass of adsorbent, temperature, and interfering ions were tested. The adsorption behavior of the adsorbents showed that by modifying the surface of the nano adsorbent, the ability of the adsorbents to adsorb strontium ion at pH=6 increased from 6.31% to 86% and 22.11% using the (EtO)3Si-HL and (EtO)3Si-L ligands, respectively. The results of isotherms and adsorption kinetics indicate that the adsorption process follows the Longmuir isotherm and the pseudo-second-order model, respectively. Also, thermodynamic parameters show that strontium removal from the aqueous solution is an endothermic process. The positive entropy values are the driving force behind the adsorption process.

Garnet amphibolite and garnet micaschists of the Faryab complex, located in the southeast of the Sanandaj-Sirjan zone, are exposed immediately under the peridotites and sometimes a few meters away from the peridotites of this region with fault boundaries. Some garnet amphibolites mainly include poikiloblasts of garnet and amphibole, plagioclase, quartz, secondary minerals of epidote, biotite, chlorite, as well as oxide minerals of, magnetite, ilmenite, titanite and apatite mineral. Garnet micaschists include the main minerals garnet, amphibole, muscovite, epidote, plagioclase, quartz, and secondary minerals biotite, chlorite, rutile, apatite, titanite, and ilmenite. Considering the chemistry of garnet poikiloblasts and the chemistry of amphiboles, temperatures of 505 to 708°C and average pressures of 6.7 to 8.6 kbar (upper amphibolite facies) for garnet amphibolites and temperatures 450 to 650°C and average pressures of 6.7 to 7.2 kbar (lower amphibolite facies) have been determined for garnet micaschists. Accordingly, garnet amphibolites show the highest metamorphic degree, while garnet micaschists show a lower metamorphic degree. Such a situation indicates a type of geothermal gradient. Geochemically, garnet amphibolites can be classified in two groups. Group I, which together with garnet micaschists have the geochemical characteristics of sedimentary rocks, while garnet amphibolites of group II show the typical characteristics of basalts. The Faryab metamorphic complex next to the ophiolitic remnants of the region may indicate the evolution of this ophiolitic complex in a Neotethys accretion-subduction position during the Upper Cretaceous.

In the Chesmeh-anjir, Bandan and Zolfaqari of Nehbandan ophiolitic complex areas, host peridotites of chromitites are of harzburgite type. These harzbogites are composed of olivine, orthopyroxene, clinopyroxene, and spinel. The spinel from Chesmeh-anjir and Bandan aera peridotites is chrome-spinel and in Zulfaqari aera of Al-chromite type, nd the spinel found in the chromitites of Chesmeh-anjir, Bandan and Zolfaqari are all of Cr-spinel type. Only a few samples of Bandan are of Al-chromite type. The chromitites of these areas are alpine type. According to the geochemical studies and determining the tectonic setting, the spinels in the harzburgites of the Zolfaqari aera show a high degree of depletion and partial melting and are of the SSZ type. Spinels in harzburgites of Bandan area have a low degree of depletion and partial melting and are N-MORB type. In the peridotites of Chesmeh-anjir aera, they show the transition state between the two. The spinels in the chromitites of Bandan aera are also SSZ type and have higher Cr. The spinels in the chromitites of Chesmeh-anjir and Zulfaqari are of N-MORB type, nevertheless, they are very similar to SSZ type. In the chromitites of Chesmeh-anjir and Zolfaqari aeras, the amount of Al is higher than in those from the chromitites of Bandan aera.

 

The petrographical examination of peridotites of the Nehbandan ophiolitic complex revealed that the peridotites of Kalateh Shahpouri, Qadamgah, Lah-Kouh, Cheshmeh anjir, Bandan, and Zolfaghari were of harzburgite type and Sefid-Kouh and Nasfandeh-Kouh were of lherzolite type. Generally, the types of clinopyroxenes in the peridotites of this complex were diopside. The geochemical investigation of clinopyroxenes in Mg# vs. Al2O3, Cr2O3, and TiO2 graphs and Ti vs. Nd, Zr, and Sr graphs shows that the peridotites of Nasfandeh-Kouh, Bandan, Zolfaghari, and Sefid-Kouh with a low degree of partial melting belong to the Abyssal tectonic setting and back-arc basin.on the other side, the harzburgites of Kalateh Shahpouri and Cheshmeh anjir were formed in the Supra-subduction zone tectonic setting and fore-arc basin and have a high degree of partial melting. The study of incompatible elements, LILE and HFSE in spider diagrams normalized to the primary mantle and as well as the study of REEs in spider diagrams normalized to the chondrite for clinopyroxenes confirm this issue. Therefore, Nasfandeh-Kouh and Sefid-Kouh lherzolites as well as Qadamgah, Lah-Kouh, Bandan, and Zolfaghari harzburgites with a low degree of depletion were more consistent with the Mid-oceanic ridgestectonic setting, and the harzburgites of Kalateh Shahpouri and Cheshmeh anjir were close to the Supra-subduction zone tectonic setting with a high degree of depletion.

The Faryab ophiolitic complex is located in Golashkard region, in the southeastern part of Sanandaj-Sirjan zone. This complex is mainly composed of the ophiolitic mantle part consisting of dunite, wehrlite, and pyroxenite, as well as chromitite and serpentinite, which was thrusted on the metamorphic rocks of the Bajgan complex. Dunites are found in the form of bodies sometimes containing thin layers of chromitite. Wehrlite and pyroxenite are also exposed as minor dykes in different parts of the complex. The main texture in the wehrlite and dunite is granular and cataclastics. The chromitites appear in both stratiform and podiform. Microscopic evidence indicates that the presence of lattice preferred orientation in minerals may be formed during recrystallization at high- temperature mantle. The chemistry of minerals in the peridotites shows that rocks including forsterite with low chromium and high nickel, diopside and magnesium-bearing Cr-spinel with small amounts of orthopyroxene were partially melted in the upper mantle up to 35 to 40%. Using tectonic setting discrimination diagrams led us to conclude that the Faryab complex peridotites are a part of the oceanic lithosphere which have emplaced in the supra-subduction zone, suffered partial melting evolutions and then tectonically emplaced in the crust in the form of ophiolitic remnants.

Mesozoic-Paleogene ophiolitic sequences in Iran are in association with opening and closing of Neo-Tethyan oceanic crust. Temporally and specially, these ophiolitic sequences subdivided into five different groups (or belts) (Shafaii Moghadam and Stern, 2014):Zagros outer belt (late Cretaceous-Paleogene); Zagros inner belt (late Cretaceous); Sabzevar- Torbat e Heydarieh belt (late Cretaceous-early Paleocene); Birjand-Nehbandan belt (early to late Cretaceous);
Makran belt (late Jurassic-Cretaceous). The Zagros outer belt’s ophiolitic sequences cropped out along the NW-SE trending Zagros main thrust and including Maku-Khoy-Salmas, Kermanshah (-Kurdistan), Neyriz and Esfandagheh (or Haji-Abad) ophiolites. The Kermanshah ophiolite (KO) is an ophiolitic tectonic complex, which comprises imbricated dismembered fragments of mantle peridotites, gabbros, sheet dykes and basaltic rocks which generally occur as thrust-bound tectonic slices. The Sahneh-Harsin ophiolitic complex(SHOC) is the southeastern part of KO. Detail petrological study has not been carried out on the basaltic rocks from Ali-Abad Garos area(AGA) as a part of the SHOC. Thus, the present study focuses on the field observations, petrographic study as well as whole-rock geochemical analyses (XRF and ICP-MS) of the basaltic rocks widespread in AGA.

Regional geology:

KO cropped out in the northwest of Zagros main thrust (ZMT) where Zagros sedimentary belt join the Sanandaj-Sirjan magmatic-metamorphic belt. In SHOC as the southeastern part of Kermanshah ophiolites Triassic-Cretaceous limestone and radiolarites as well as Mesozoic metamorphic-sedimentary rocks are the oldest lithological units. In the following, ophiolitic sequence related lithological bodies such as peridotites, meta-peridotites, gabbros, meta-gabbros, diabasic dikes and volcanic rocks including pillow lava-massive basalts cropped out which are in accompanied by Eocene extrusive and intrusive rocks. Pliocene to Quaternary sedimentary rocks are the youngest lithological units in Sahneh-Harsin region. In Sahneh-Harsin region ophiolitic sequence related basaltic rocks cropped out in Ali-Abad Garos, Tamark, Gashor areas.

We collected ~70 samples of both pillow lava and massive basaltic rocks in-AGA. Based on petrographic characteristics 10 of the freshest samples were analyzed for whole-rock major and trace elements by X-ray Fluorescence (XRF) and Inductively Coupled Plasma-Mass Spectrometry (ICP-MS) in ALS Chemex lab.

Field observations:

Ali-Abad Garos ophiolitic sequence related basaltic rocks mostly show pillow lava structure. However, minor massive basaltic rocks are exist. In the northern part of the study area basaltic rocks are set atop of gabbroic units. However, gabbro-basalt boundary covered by Quaternary sediments. In some parts, basaltic bodies are in association with plagiogranites. Via a fault boundary upper Triassic-Cretaceous limestone units (Biston Formation) thrusted over basaltic rocks.

Petrography:

The rocks under study are dominated by plagioclase (up to 20%), clinopyroxene (up to 10%) and opaque minerals (up to 2%) phenocrysts set in a fine-grained to glassy ground mass. Chlorite, calcite, epidote, quartz, zeolite and opaque minerals as secondary minerals formed by altered phenocrysts and groundmass. Massive basaltic rocks mostly show porphyritic texture and to lesser extent glomeroporphyritic, intergranular and amygdaloidal textures are present. The rocks studied are characterized by plagioclase (up to 10%), clinopyroxene (up to 20%) and opaque minerals (up to 5%) phenocrysts set in a fine grain to glassy groundmass. Secondary minerals in massive basaltic rocks are similar to those presented for pillow lava basaltic rocks. Whole-rock geochemistry, tectonic setting and source characteristics The studied basaltic rocks show tholeiitic signature. Major element oxides values against SiO2 values, as fractionation index, indicate fractional crystallization as an effective parameter in generation of these rocks. In chondrite-normalized REEs diagram, the basaltic rocks exhibit slight LREE enrichment relative to HREEs (LaN/YbN values ranging from 2.91 to 3.35 and Eu/Eu* values vary from 0.91 to 1.01). In primitive mantle-normalized multi-elements diagram, the patterns of basaltic rocks are consistent with plume related mid-oceanic ridge basalts (P-MORB), against within plate basalt (WPB or OIB), normal mid-oceanic ridge basalts (N-MORB) and enriched mid-oceanic ridge basalts (E-MORB). This case is in agreement with situation of the study samples in basaltic rocks with different geochemical signatures on discriminative diagrams. Parallel trends of the studying basaltic rocks on spider diagrams indicate that they are co-genetic. Also, different elemental ratios as well as the situation of the rocks under study in different geochemical diagrams reveal that parental magma (or magmas) could be formed by low degree partial melting (<3%) of a spinel peridotite as a source rock. Integration of our new presented geochemical data from the study basaltic rocks with other previously presented geochemical data from other ophiolitic sequence related basaltic outcrops within (SHOC) (Tamark and Gashor basaltic rocks) reveal that in this ophiolitic complex basaltic rocks are heterogeneous. Briefly, three different groups of basaltic rocks with P-MORB, E-MORB and OIB geochemical features exist in (SHOC). Comprehensive understanding of relation of these three different basaltic groups are needed to further elemental-isotopic geochemical data coupled with geochronological data.

The nurse's knowledge and skills in caring for endotracheal tube cuff pressure can lead to complications in the patient. However, few studies are available in this area. Therefore, this study aimed to determine the knowledge and practice of nurses on how to measure and control cuff pressure of patients admitted to intensive care units.

This descriptive study was performed on 151 qualified nurses working in ICU wards of Shiraz teaching hospitals in 2017. Data collection was performed using a researcher-made checklist.

21.5% of the nurses knew the normal tracheal cuff pressure and tracheostomy range. Regarding the different ways of measuring cuff pressure, 5.3% referred to the minimum leakage method, 86.7% to the manual method, 74.7% to the manometer, and no reference was made to the obstruction method. 60.7% used the manual method to measure cuff pressure, and only 39.3% used a manometer. 3.3% did not know the time interval of cuff pressure measurement. 40% in each shift, and 56.7% stated every 24 hours as the appropriate time to control it.

The results of the present study showed that the performance of nurses concerning the ways of measuring cuff pressure is appropriate. However, the nurses' knowledge in this study is limited about the normal range of endotracheal tube cuff pressure and the complications caused by the abnormal low cuff range.

Agates of the Ferdows area (north of Lut Block) occurred in open space and cracks filling form in the Paleogene volcanic rocks. These rocks are found as red, smoky, blue, violet, green, and colorless and as a vein, mosaic, geode, banded, stellar, cauliflower, moss, and circular fabrics. The altered host rocks’ fragments as enclave occurred within agates without reaction rims. Fluid inclusion studies on some of the agates show arrange of homogenization temperature from 102 to 233 ℃ and salinities from 2 to 11 wt% NaCl equiv. The REE contents of these rocks are low, only the vein-type agates were analyzed for all REEs. Most of the studied agates display Eu negative anomaly and positive Yb anomaly in REE normalized pattern along with

The Kamyaran ophiolites, with the age of Late Cretaceous, are a part of the Iranian Mesozoic ophiolites, which are exposed in the SW of Zagros Main Thrust. This massif is bordered at the NE by the Sanandaj-Sirjan metamorphic rocks and at the SW by the Bisotun limestones and Kermanshah radiolarites and then by the Zagros Fold-Thrust Belt. The Kamyaran ophiolite is made of the mantle and crustal sequences. The crustal sequence is distinguished by pillow lavas, sheeted dike complex, and lava flows. The positive LILE anomalies with the HFSE depleted confirm their arc-related affinity. The geochemistry signatures of sheeted dikes show that these rocks have two different patterns. The REE pattern in some of the sheeted dikes samples with the pillow and flow lavas sample is similar to E-MORB; their element ratios support this likeness too. The positive LREE and LILE anomalies with the depletions of the HFSE suggest the calc-alkalic tendency and subduction-related affinity for these rocks; however, dacitic dikes with the flat REE pattern, LILE enrichment, and HFSE depletions have the Island-arc tholeiites affinity. The similarity of element ratios in all the samples may suggest that these rocks have the same magma source, and the tectonic environment of the ophiolitic rocks can be correlated with the oceanic subduction environment.

Ophiolites are a set of oceanic rocks with different appearance and mineralogy in the world's largest orogenic belt, from the Alpine to the Himalayas. The ophiolites of Iran are also located in this belt. Among ophiolites in Iran, the Nehbandan Ophiolitic Complex in the east of the country is of great importance. The complete ophiolitic sequence consists of two sets. The first is the crust sequence, gabbro, diabase and basalt, and the second is a mantle sequence or peridotites, both of which are sequences in the Nehbandan Ophiolitic Complex. The main purpose of this research study is mantle section. There are three study areas, located near the city of Nehbandan: Kalateh-Shahpori, Qadam Gah peridotites that are about 30 km northwest of the city of Nehbandan near the Chahar Farsang village and the third area is located between the Khansharaf village and Nasfandeh Kuh area that is 10 km east of Nehbandan.

In this lithological and mineralogical research study, thin and polished sections were prepared from samples. The thin sections were analyzed by polarizing OLYMPUS microscope BH-2 and the polished sections were analyzed by the OLYMPUS BX-60 reflecting microscope. A CAMECA SX100 electron probe microanalyzer was used to determine the chemical composition of the minerals in samples. The analytical condition include 15 kV and 20 nA rays with periods of 10 to 30 seconds at peaks for different minerals that are analyzed at the electron probe microanalysis center in the University Of Toulouse, France. The stoichiometry of minerals was used to calculate the amount of Fe3+ for access to the structural formula of minerals (Droop, 1987.

In terms of petrography, the Kalateh Shahpori peridotites are of the Harzburgite type and the Nasfandeh Kuh peridotites are of the Lherzolite type. The Qadam Gah peridotites are both geographically and petrographically indicative of the state of transition between the two other regions. The mineralogy of the Kalateh Shahpori peridotites is composed of olivine (Fo91), orthopyroxene (En90 Fs9), and the Cr-spinel is of the high Cr type. The Nasfandeh Kuh peridotites have olivine minerals that are Chrysolite (Fo89), orthopyroxene (En89 Fs9) and (En86 Fs10), clinopyroxene (En46 Fs5 Wo49) and, the Cr-spinel is of the high Al type. The Qadam Gah peridotites are composed of olivine (Fo90), orthopyroxene (En89 Fs9.5), clinopyroxene (En47 Fs3 Wo50) and, the Cr-spinel is of the medium Cr type.According to geochemical data and petrogenesis, the Kalateh Shahpori harzburgites are of the supra-subduction zone type in the forearc basin. The Nasfandeh Kuh Lherzolites are of the middle-oceanic type. The Lherzolites of Qadam Gah have the same characteristics of both regions in terms of the formation environment. However, they are much more similar to the middle-oceanic peridotites. The degree of partial melting of the peridotite has a direct relationship with the Cr content and it has an inverse relationship with the Al2O3 content in the chromium-spinel of the peridotite (Hellebrand et al., 2001). Probably, these lherzolites formed due to the re-fertilization of harzburgites (Monsef et al., 2018). Accordingly, Kalateh-Shahpori harzburgites with 20% partial melting are of high-grade, and the Nasfandeh Kuh Lherzolites with 5% partial melting are of the low grade type. The herzolites of the Qadam Gah are approximately 11% partial melting and are located between the Kalateh Shahpori peridotites and the Nasfandeh Kuh peridotites. The high degree of melting in the Harzburgites may indicate their remelting in the fluid environment because the hydrosis condition increases the degree of partial melting of peridotite (Hirose and Kawamoto, 1995). The Cr# in Cr-spinel, and the Mg# in olivine of the peridotites indicate the presence of at least 3 types of peridotites in the Nehbandan Ophiolitic Complex. According to mineralogy, petrography, geochemistry, and petrogenesis studies of the peridotites in the Nehbandan ophiolitic complex, it is recommended to explore possible chromite deposits, high melting and supra-subduction harzburgite zones such as Kalateh Shahpori harzburgites which should be considered to be the first priority. Then the peridotites of transition regions such as Qadam Gah should be at second priority and finally the low melting middle-oceanic lherzolites such as the Nasfandeh Kuh shuld be considered to be the third priority.

Hanar intrusion located in 155 km South of Birjand in the east of Lut block and compositionally consist of tonalite, granodiorite, quartz-diorite and diorite that intruded as stock and dikes in volcanic sequence (basic to intermediate) outcropped in this area. Hanar granitoid rocks are metaluminous and show I-type granitoids affinity. In addition, they are belong to calk-alkaline series and reveal the active continental margin geochemical evidences. According to relation of studying intrusion to I type granitoids with oxide (magnesian) state, they have no potential to produce Sn and W mineralization. Also, Low Sr/Y and V/Sc ratios as well as the situation of the studying samples in barren domain of the fertile-barren discrimination diagrams show that Hanar granitoids have no potential for Cu porphyry mineralization. In other hand, Low degree of the magmatic evolution as well as location of the studying samples in different Fe-mineralization potential evaluation diagrams indicate that Hanar granitoids (Diorite unit) has high potential for formation of iron deposits that this case is supporting by occurrence of  Fe-mineralization (as vein-Iron deposit) in association with this intrusion.

Narigan area in the southern part of the Bafq-Saghand metallogenic zone in Central Iran is a host of davidite-bearing quartz veins. Davidite is an important key mineral for exploration of not only uranium but also REE's in Central Iran. Narigan granite in the Narigan area is characterized by high-K calc-alkaline nature and its parental magma was partially contaminated by the Precambrian crust. The REE pattern of quartz veins is brought about by REE contents in davidite. The homogenization temperatures of vapor-liquid-solid (V-L-S) fluid inclusions in quartzes are >500˚C in quartz veins. Furthermore, the ∑REE contents (71910 to 90292 ppm) and U/Th ratios (<1000) in the studied davidites indicate upper 450˚C temperature for the generation of them. Based on the similarity of REE pattern of davidite to REE pattern of oxide-uranium minerals in the vein-type ores (characterized by negative Eu anomaly and high LREE/HREE ratio) as well as achievement of the homogenization temperatures for fluid inclusions and davidite formation; mineralization of this mineral can be related to granite related vein-type uranium deposits.

Koudakan Granitoid located in 100 km South of Birjand and 18 km North of Ghaleh-Zari mine in eastern Iran. It belong to the Lut Block volcanic–plutonic belt. These intrusive rocks (Eocene-Oligocene) petrogaphicaly composed of Diorite, Monzodiorite, Quartzmonzodiorite, Tonalite, Porphyritic Tonalite, Granodiorite, Granite and Porphyritic Granite. Plutonic rocks in this area have features typical of high-K calc-alkaline to shoshonite series, metaluminous and belong to I-type Granitoides. Enrichment in LILE rather than HFSE (RbN/YN: 38.12-124.93), negative anomalies of Nb and Ti and enrichment in LREE rather than HREE (LaN/YbN: 6.74-12.03) in all of samples are important evidences for the formation of this rocks in a subduction related magmatic belt. Positive anomalies of Pb and K indicate the involvement of continental crust in evolution of parental magma. Parallel trend of the samples in spider diagrams show that they are co-genetic. Elements ratios and Different discrimination diagrams show the formation of this rocks in an active continental margin with about less than 45 Km crustal thickness in per-collision steps. Parental magma has been generated by low degree partial melting (less than 5%) of an enriched peridotite in mantle wedge (Spinel lherzolite.).

The article aims in the studying of thermal-hydraulic simulation of the VVER-1000 reactor core fuel assemblies’ reaction to the mass flux changes which are caused by the lose of coolant accident and its sudden pressure drop. The analysis of mentioned accident is performed in concise periods (mili second) by the use of the sound effect. Time-related thermal-hydraulic equations were analyzed by the method of a compressible fluid in a single heated channel and were evaluated by the results of the mentioned transient, in a PWR reactor. The mentioned transient was simulated in RELAP5 code and results were compared to the previous ones. Then, 28 reactor fuel assemblies were studied, considering the 1/6 symmetry of VVER-1000 reactor and unique features of every assembly. Mass flux drop was happened the end of the channel, after a few seconds. It was observed that mass flux is at dependent on the role of every assembly in the production of core heat power. The acoustic effect reveals some of the perturbations in mass flux changes, considering every fuel assembly features.

The magmatic activities in north Qazvin, as a part of the Western Alborz zone, contain a sequences of volcanic lavas associated with pyroclastic rocks with Eocene age. According to petrographical investigations, volcanic lavas are basalt, basaltic andesite, pyroxene andesite, trachy-andesite, dacite and rhyolite. The texture of these rocks is more porphyritic with fine-grained groundmass including plagioclase, clinopyroxene, quartz, alkali feldspar, amphibole and biotite minerals. On the basis of geochemical features, all samples show high-K calc-alkaline to shoshonitic affinities. Also, these rocks are enriched in LREE and LILE, and depleted in HFSE characteristic of calc-alkaline series in subduction-related environment. Petrogenesis indicate that the mafic lavas have been derived from 5 to 10 % partial melting of enriched garnet lherzolite mantle source. Qazvin volcanic lavas have moderate Nb/Yb and Ta/Yb ratios indicative of an enriched mantle source compositions (e.g., E-MORB). Furthermore, these lavas have high values of Th, U and Pb consistent with slab-related sediments and/or crustal contamination in their mantle source.

The Hanar granitoids, geographically located 155 km south of Birjand in the east of Iran. Geologically, It belongs to the Lut block volcanic–plutonic belt and occurs near to the Lut block-Sistan suture zone border. The granitoid rocks consist of tonalite, granodiorite, quartz-diorite, diorite and microdiorite. The predominant textures are granular, porphyritic and myrmekitic. Geochemical evidence reveals that they are co-genetic and have features typical of calk-alkaline to high-K calk-alkaline, metaluminous with I-type nature. Enrichment in LILE (i.e. Cs, K, Rb, U and Th) rather than HFSE (eg., Nb, P, Zr and Ti), typical negative anomalies of Nb and Ti and LREE enrichment in comparison to HREE, are important characteristics indicating that these rocks were formed in a magmatic belt in a subduction zone. Positive anomalies of Pb and K demonstrate the involvement of continental crust in evolution of parental magma. Trace element ratios and adakitic discrimination diagrams point to the non adakitic nature of the magma. Tectonic discrimination diagrams show formation of these rocks in an immature continental arc setting with less than 45 Km crustal thickness in pre-plate collision event. Primitive magmas should have formed by low degree melting (less than 8%) of an eneriched mantle wedge peridotite (spinel lherzolite). During magma ascent, fractional crystallization and crustal contamination (AFC) took place simultaneously. Field observation and petrography studies support this hypothesis.

The Paleogene volcanic rocks in southwest of Basiran belong to the Lut Block volcanic–plutonic belt in eastern Iran. The studied rocks range from basaltic to rhyolitic compositions (basalt, andesite, dacite and rhyolite) with a peak in intermediate compositions. These rocks are dominated by porphyritic and glomeroporphyric textures with microlitic groundmass. Geochemical evidence reveals that they have typical features of calc-alkaline, high-K calc-alkaline to shoshonitic rocks. Generally, enrichment in LILEs (like Cs, K, U and Th) rather than HFSEs (like Nb, P, Zr and Ti), negative anomalies of Nb and Ti and high LREEs/HREEs ratio in these rocks are similar to magmatic rocks in subduction zones. Positive anomalies of Pb show involvement of continental crust in evolution of parental magma. However, geochemical difference of acidic and basic-intermediate rocks may be resulted from more evolved nature of acidic magma compared to basic-intermediates or alteration effects. Based on geochemical characteristics and tectonic discrimination diagrams the studied volcanic rocks presumably formed in an immature to normal continental arc setting. Furthermore, primitive magma of basic-intermediate associations could be generated by low degree partial melting (less than 5%) of mantle peridotite (garnet lherzolite) in depth of 90-110 km.