مجله بلور شناسی و کانی شناسی ایران
سال بیست و چهارم شماره 3 (پیاپی 65، پاییز 1395)

Cheshmeh Gaz (Nasim) copper deposit is located in northwest of Bardaskan, Khorasan Razavi province. Geology of the area is consist of andesite, basalt, nummulitic limestone, and marl with gypsum intercalations Eocene in age, Pliocene conglomerate, and Quaternary sediments. Mineralization has been formed in andesites and contact between andesitic units and limestone as stratabound with disseminated, veinlets, and open space filling textures. Orebody consist of primary minerals such as chalcocite, native copper, and pyrite and secondary minerals including malachite, covellite, azurite, and goethite. Based on microscopic studies and XRD analysis, mineralogy of alteration zones is chlorite, calcite, zeolite (natrolite, thomsonite, and analcime), quartz, and minor epidote. Considerable anomaly of Cu (up to 3.36%) is present in the area. The hosted volcanic rocks are calc-alkaline type and are formed in subduction zone volcanic arc. Host rock type and geochemical features, alteration, structure and texture of mineralization, and ore types in Cheshmeh Gaz deposit are similar to Manto-type deposits and epigenetic-diagenetic model is suggested for formation of it.

The Sarvian magnetitic skarn deposit has been formed due to the granodiorite injection into the oligomiocene limestones. It is a calcic skarn deposit with dominated exoskarn section. Garnet and pyroxene are two coupled indicator minerals that have been formed by Mg-Si-Fe-bearing fluid remained from magma crystallization. These minerals are observed extensively in the metasomatic haloes in the country rocks and could be used to determine the conditions of temperature and pressure that have been governed on skarnization. It is revealed from microprobe analysis that the garnets in the Sarvian deposit are of the grossular-andradite type that are enriched in Fe & Ca, and depleted in Mg & Mn. These garnets show a sharp zoning structure. The distributions of MnO, CaO, Al2O3 and FeO in the zoned garnets indicate that from the core to rim, their composition changes gradually from grossular to andradite. The composition of the garnets and pyroxenes in the Sarvian ore deposit is compatible with the Fe-skarn deposits. Pyroxenes in the Sarvian ore deposit are of Ca-riched diopsid-hedenbergite type. During the prograde stage in which the anhydrous minerals such as garnets and pyroxenes were formed, the temperatures are comparable with albite-epidote and hornblende-hornfelse facieses. According to the temperatures of the garnet-clinopyroxene minerals formation, the temperatures of prograde stage have been determined between 370-500 °C. On the other hand, the results of fluid inclusion studies on quartz grains obtained from mineralized veins suggest that the temperatures during the iron mineralization in the retrograde stage of skarnization have been 400-380 ° C.

The Chalu Fe skarn developed at the contacts of the part of intrusive body with monzodiorite composition and Cretaceous carbonate rocks. Endoskarn which occurs in a limited area is characterized by andradite rich garnet (Ad90Gr5Sp3) and clinopyroxene. The calcic exoskarn shows a continuous mineralogical evolution and zonation with increasing distant from contact. It is composed mainly of coarse- grained vesuvianite and garnet (Ad53Gr43Py2), in proximal zone to fine grained calcite, garnet (Ad27Gr71Py2) and vesuvianite in distal zone. The chemical compositions of garnet and vesuvianite in different parts of exoskarn indicate an evolutionary trend of increasing CO2 and H2O in the fluid, decreasing fO2, decreasing temperature. Hematite flakes (specularite) and magnetite which contain the main ore mineralization accompanied by Fe sulphides (pyrite and chalcopyrite) and secondary malachite, limonite and goethite.

The study area is located at 220 km southwest of Mashhad and 80 km south of Neyshabur and is situated between 58° 40' 30" to 58° 43' 30" E longitudes and 35° 47' 30" to 35° 52' 00" N latitudes. The study area is part of Sabzevar zone. The lithology of the area consists mainly of volcanic rocks with trachyte, trachy andesite, and basaltic trachy andesite composition and in some parts has been subjected to argillic, carbonate and propylitic alteratins. The dominent phenocrysts in these rocks are plagioclase, alkali feldespar, opacitized hornblende and pyroxene. The main texture in these rocks is porphyritic with fine and medium grain matrix. These rocks have calc-alkaline nature and show enrichment in LILE (except for Ba) and depletion of HFSE. The enrichment of LREEs relative to HREEs indicates that the parental magma formed in a subduction zone, which is well manifested by the volcanic rocks of Golcheshmeh area. Tectonic setting diagrams and geochemical properties of volcanic rocks of the study area suggest an active continental margin setting. The low ratios of (La/Yb)N (5.3 to 9.3) and (Ce/Yb)N (4.2 to 7) point to low degree partial melting at shallow depths and low garnet in the source magma. The source magma formed by 2 to 5% partial melting of a spinel-garnet lherzolite source (low garnet) accompanied by crustal contamination.

N'-(2-hydroxy-3-methoxybenzylidene)-4-methylbenzenesulfonohydrazide (1) was prepared by the reaction of p-Toluenesulfonyl hydrazide and 2-hydroxy-3-methoxy benzaldehyde (1:1 molar ratio) in ethanol under reflux condition. The crystal structure of the compound was determined by X-ray crystallography. Crystal data for 1 at -100 K: space group C/2c with: a = 15.807(1) Å, b = 10.457(1) Å, c = 20.779(1) Å, β = 109.68º (1). The final R value is 0.0574 for 3155 independent reflection. The N -H …O hydrogen bond converts the molecules into an infinite chain along [010].

Hezar complex is a part of Dehaj-Sarduiyeh volcano-plotunic belt in southwest of Rayen (Kerman province). Investigations on lava flows show that they have basalt, basaltic-trachy-andesite, trachy-andesite ,and trachy-basalt composition. On the basis of petrographic studies, the rocks contain plagioclase (Oligoclase - Andesine), pyroxene (Augite - Diopside) and much altered olivine. Plagioclases show disequilibrium textures as a result of magma pressure decreasing. The formation of large plagioclase crystals is due to small amount of nucleation, rapid growth of crystals in the magma, because of magma's composition, and probably crystallization in low pressure. Geochemical investigations display that these lavas belong to calc-alkaline magmatic series and have characteristics of volcanic arc, and probably, the parent magmas were originated from the partial melting of an enriched mantle wedge above the subduction zone in Garnet stability field.

SnO2 nanoparticles have been synthesized via sol-gel method in different annealing temperatures. TEM, FESEM and XRD techniques have been used to investigate the structure and morphology of SnO2 nanoparticles. The XRD pattern analysis shows all samples are single phase. XRD patterns show as the annealing temperature increases, the peaks become sharper which is related to the increase in the crystallite size of nanoparticles and enhancing the crystalline order and reducing lattice strain. The Williamson-Hall analysis and Halder-Wagner method were used to study the individual contributions of crystallite sizes and lattice strain to the peak broadening of nanoparticles. The physical parameters such as strain, stress and energy density values were calculated for three major reflection peaks of XRD patterns. Williamson-Hall analysis of XRD patterns show that increasing the annealing temperature causes the crystallite size to increase and to reduce lattice strain. TEM and FESEM images showed that by increasing temperature, nanoparticle size increases.

A wide range of plutonic rocks, ranging from mafic to felsic compositions, including various gabbros, diorites, tonalites, granodiorites, monzogranites, syenogranites and leucocratic granitoids, occur in the Alvand plutonic complex, Sanandaj-Sirjan zone, Iran. Age of this complex is middle Jurassic. In this complex, granitic and dioritic rocks occur as major constituents. Granites contain plagioclase, K-feldspar, quartz and bitite and diorites comprise plagioclase, hornblende, biotite and minor titanite and apatite. In some outcrops, contaminated granites and diorites occur which contain abundant large undigested xenocrysts of andalusite (partly to wholly converted to sillimanite) with spinel-rich and feldspathic reaction rims around them. These xenocrysts resulted from disintegration of minerals from pelitic rocks and their incorporation into host magmas. The 87Sr/86Sr isotope ratios in the studied granitic rocks vary from 0.7101 to 0.7245 and in the contaminated diorites from 0.7084 to 0.7079 (Sri more than 0.704). The range of 143Nd/144Nd ratios in granitic rocks is from 0.51234 to 0.51240 and for contaminated diorites from 0.51244 to 0.51252.The εNd(t) values for the studied granites vary from -3.2 to -3.98 and for contaminated dioritic rocks from -0.78 to -2.35.  In the 143Nd/144Nd versus 87Sr/86Sr diagram, granites plot in the field of crustal rocks; also diorites with mantle origin, in response to contamination by meta-pelitic rocks, are shifted towards rocks with crustal origin. These results indicate the importance of recognizing contamination of plutonic rocks by upper crustal (meta-pelitic) material when interpreting petrogenesis of such rocks.

Chaharfarsakh intrusive and extrusive rocks are located in 25 Km northwest of Nehbandan and 165 Km south of Birjand and in terms of geology, suituated in the eastern of Lut block. Chaharfaraskh intrusive rocks with Jurassic age were injected into shales and sandastons Shemshak Formation. Intrusive rocks are gabbro, diorite, synogranite, quartz monzonite, hornblend tonalite, granodiorite, granite, pegmatite and aplitic in composition. These rocks are composed of quartz, plagioclase, orthoclase, hornblend and biotite minerals but pyroxine minerals observed in gabbro rocks. They are dominating granular texture. Andesite and dacite are main extrusive rocks in Chaharfarsakh bodies and composed of plagioclase, hornblende, quartz, biotite minerals with porphyritic texture. Chaharfarsakh granitoid have subalkaline, meta to peralominouse nature, I type granitoids and show tendancy to contamination continental crust.Tectonic setting discrimination diagrams show these rocks belonging to volcanic arc granitoids position. It seems Chaharfarsakh extrusive rocks with Eocene age can be related to subduction of Neotethys ocean in the Cretaceous time, while Chaharfarsakh intrusive rocks to Jurassic are not justified with Cretaceous magmatism and probably differentiation formed from extousive rocks. It seems Chaharfarsakh granitoed formed similar to ShahKuh intrusive have been formed by partial melting the base of continental crust that was contamination during replacement with assimillation of metamorphic and sedimentary host rocks the upper crust.

In this study, aluminum ion (Al3+) substituted yttrium iron garnet nanoparticles Y3AlxFe5-xO12 (x = 0.0, 0.2, 0.4) were fabricated by the sol-gel method. X-ray diffraction (XRD) patterns confirmed the pure garnet structure for all samples. The chemical bonds and the garnet phase were studied by using FT-IR, Far-FTIR. The cation distribution and the magnetic hyperfine parameters were obtained by MÖssbauer spectroscopy and confirmed the VSM results. The results of vibrating sample magnetometer (VSM) show that saturation magnetization decrease with increasing aluminum ion concentration. These changes assigned to the Neel theory and the spin canting due to the reduction of superexchange interactions between iron ions in the octahedral and tetrahedral and octahedral sites.

Kashmar subvolcanic and plutonic bodies have compositional ranges from quartz gabbro to alkali granite. With exception of several small stock with alkaline  Tholeiitic basalts characteristic (minimum amounts of SiO2 and CaO; maximum amount of MgO; high amounts of Na2O and K2O and LOI and high meta-luminous to peraluminous (1.33-2.32)), all rocks have high-k calc-alkaline to shoshonitic, meta-luminous to weak peraluminous (mostly ASI<1.1 and maximum to 1.3) characteristic. Normalized REE patterns show enrichment in LILE (such as Ba,Th, Rb, U and K) and LREEs, depletion of Nb-Ta-Ti (arc-like indicators) and flat HREE patterns with negative Eu anomalies. Thus the rocks are essentially co-magmatic and I-type. On the discrimination diagrams, Granitoids plots in the arc-collision continental domain. K, Rb, Ba, Eu and Sr variations for granitoids show role of partial melting and AFC process in formation of Kashmar granitoids. The flat HREE patterns also indicate no residual or fractionating garnet. Base on Sr, Y, Al2O3, La and Yb, the all Kashmar rocks are no adakite-like and forms from about 50% partioal melting of  amphiboliths.

The title compound, [Cu(hpydc)(DMP)].5H2O (2) (where H2hpydc and DMP are 4-hydroxypyridine-2,6-dicarboxylic acid and 2,9-dimethyl-1,10-phenanthroline, respectively), was synthesized via the proton transfer method and its structure was determined by single crystal X-ray diffraction. This compound crystallizes in the monoclinic crystal system with P2/c space group and the unit cell parameters are a = 10.8423(4), b = 13.4457(5), c = 13.6447(4) Å and β = 90.004(2)º. The final R value is 0.046 for 4425 independent reflections. The asymmetry unit of compound 2 contains one molecule of the Cu complex and five molecules of water of hydration. The CuII central atom in compound 2 adopt a distorted square-pyramidal coordination geometry being penta-coordinated by one N and two O atoms of 4-hydroxypyridine-2,6-dicarboxylate and two N atoms of DMP ligands. This compound is a pseudopolymorph of the previously reported compound of [Cu(hpydc)(DMP)].3H2O, (1). Non-covalent interactions and different number of solvent molecules are responsible for the hydrophilic channels in the structure of compound 2 which have been occupied by water molecules.

In this research, nanoparticles Bi1-x-yBayLaxFeO3 (BByLxFO (with values (x = 0.0, 0.05, 0.1) and (y = 0.0, 0.15) synthesized by a sol–gel  method. The structural, microstructural and magnetic properties have been investigated, using X-ray diffraction, Raman scattering, field emission scanning electron microscopy (FE-SEM), FTIR  spectroscopy, and magnetometry measurements at room temperature. The refinement of X-ray diffraction pattern of samples indicates a phase transition from rhombohedral (R3c) to rhombohedral-tetragonal. In addition, The refinement of X-ray Assigned  lattice parameters and unit cell volume.  Analysis of FT-IR confirmed Perovskite structure of samples. The FE-SEM analysis show nanoparticle size it decreases with La  concentration. Finally, the hysteresis loop of nanoparticle BByLyFO shows ferromagnetic behavior, that may be attributed to the collapse of spin structure and modifying exchange interactions because of La+3  and Ba+2 co-doping. The remenant  magnetization of  BB0.15L0.1FO sample (Mr = 1.166 emu/g) is approximately two and half times greater than that of  BB0.15L0FO (Mr = 0.514 emu/g). This enhancement in magnetic properties at room temperature can play an important role for the practical applications.

A new tetraorganotin(IV) complex, {bis(µ3-oxo)-bis(µ-isopropoxo)-dichloro-octakis(4-methyl)-tetra-tin, has been synthesized by dimethyltin dichloride in the presence of potassium iso peroxide. This Complex with a general formula of {(CH3)8Sn4Cl2(C3H7O)2O2} is classified in the category of tetraorganodistannoxanes. Solid state crystal structure of this compound  was determined  by single crystal X-ray diffraction. The titled complex is centerosymmetric and exists as a tetranuclear molecule which involves three staircase rings with a Sn4O4 core. The asymmetric unit of the complex contains two atoms of tin (IV) and an infinite two-dimensional structure is formed by CH...Cl interactions between tetranuclear units. Two types of bridged oxygen are present in this compound. One of them has an alkoxide nature and the other one is a bridge between three tin centers. The results of studies on tin multi-core systems have shown that in addition to the bulk effect, the size and the nature of different attached organic groups, the nature of the participating ligands in coordination environment influence the physical and chemical properties of these compounds.

4-(4H-1,2,4-Triazol-4-yl)phenol (compound I) as a triazol aromatic compound was obtained by the reaction diformylhydrazineand p-aminophenol in dimethylformamide (DMF) under hydrothermal condition. The crystal structure of this compound was determined by FT-IR spectroscopy, NMR, elemental analysis and single crystal X-ray diffraction method. Crystallographic data for I was collected at 298 K. The synthesized compound has been crystallized in orthorhombic system with pbca space group and a = 10.9373(15) Å, b = 7.4539(10) Å, c = 18.530(3) Å, Z = 8. The crystal structure was solved by direct methods and refined by full-matrix least squares to final values of R1 = 0.0682 and wR2 = 0.1361 with 1328 reflections. There are various types of supramolecular interactions including hydrogen bonding and π-π stacking in the crystal structure of I. These interactions play important role in the expansion of 3D network of compound I.

In this research, magnetic anisotropy of Co68.15Fe4.33B12.5Si15 microwires were investigated. For this purpose, VVSM (Vector Vibrating Sample Magnetometer) analysis, which measures the transverse components of the magnetization simultaneously with the longitudinal one, was used. The magnetic field is applied in different directions with respect to cylindrical axis of wire and magnetization were recorded along X and Y direction. The component of magnetization along X direction decreases with increasing angle, while for Y component the magnetization increases with increasing angle of applied field. The results are explained in terms of unusual magnetic domain structure of wires.

Qroqchy area is located northwest of Isfahan, in the central Iranian structural zone. The Nayband black shale is a significant geological unit which is widespread occurrences in the study are. Weathering process lead to black sale alteration and formation of acidic pool. The pool is located on the black shale basement. Around of the pool sulfate minerals occur with various colors. The aim of the research is identify rare sulfate minerals around acidic pool and investigation of formation mechanism of these minerals. On the base of XRD results, the most important minerals are :(ferricopiapite (hydrous iron sulfate,) tamarugite (hydrous sodium sulfate, (kieserite (hydrated magnesium sulfate, ) blodite (sodium, magnesium hydrous sulphate, and gypsum. Weathering process and decomposition of black shale minerals lead to release sulfate mineral components. Presence of pyrite in black shale is an effective factor increasing weathering and resulting acidic conditions. Acid drainage leads to decomposition of black shale and released cations of crystalline framework. Deposition of secondary minerals resulted acidic equilibrium. Geochemically, the Qoroqchi black shale characterized by LREE enrichment
(ΣLREE = 140/463) and HREE depletion (ΣHREE = 5/037ppm), in comparison NASC has similar pattern.

Studying of the ferromagnesian rocks, including metaperidotite and metabasite, as well as the calcium-bearing ones such as calc-silicate in the different parts of the Deh-Salm metamorphic complex (DMC) in the east of the Lut block caused a widespread recognition of various paragenesises of amphiboles. Focused EPMA studies represent amphiboles with the different compositions and PT conditions. The most important amphiboles in the metaperidotite are composed of magnesium type, including anthophyllite, and calcium type, including tremolitic hornblende, magnesium-hornblende, and tremolite.  While in the metabasite mineral assemblage, especially in the amphibolies, pargasite and tschermakite are the main constituents. The clear changes in the amphibole’s compositions can be attributed to the two reasons of the different protoliths and the physical conditions of metamorphism. The thermo-barometry conditions of the metamorphism based on amphibole chemistry document a respectively mean temperature and pressure of 527.8 °C and 6.24 Kbar for the Galugah’s metabasits and the comparable amounts of 707.7°C and 5.86 Kbar for the DMC. The measured P-T conditions may represent that the eastern part of the DMC, which have been in direct contact to the late Jurassic felsic intrusions and the migmatitic zones, exhumed to the higher levels than its colder western part. This uplifting may be occurred due to ascending of the ShahKuh pluton and the activity of the associated NS-trending main faults in the studied area such as the Kahur fault.