مجله بلور شناسی و کانی شناسی ایران
سال سی و یکم شماره 3 (پیاپی 93، پاییز 1402)

The Kimia copper area is located in the Eocene volcano-sedimentary complex northwest of Bardskan in Razavi Khorasan Province. The geology of the area includes volcanic rocks with andesite-basalt composition, conglomerate with andesite fragments, nummulitic limestone and tuffaceous sandstone. Mineralization is found in andesite and conglomerate units as well as at the border between these units in the form of vein-veinlets, disseminated, replacement and open space filling. Primary minerals are chalcocite, pyrite, and secondary minerals are malachite, caveolite, and iron oxide. The faults in this region are formed in two directions, northeast-southwest and northwest-southeast, with a slope of 45 degrees. The main veins in this zone are calcite-quartz-pyrite, calcite-chalcocite and calcite-barite-pyrite. Alterations related to veins are siliceous and carbonate and are related to igneous, propylitic, carbonate and chloritic units. The amount of copper element ranges between 6950 and 47935 ppm and other elements have low values. Based on fluid inclusion study, the minimum formation temperature ranges between 228 and 368 °C and the salinity is between 10.4 and 16.9 percent. Based on the evidence of the host rock, structure, textures and existing alterations, copper mineralization in Kimia area is Manto type.

The Late Cretaceous basaltic magmatism in northern part of the Urumieh-Dokhtar Magmatic Arc (UDMA) includes subalkaline (transitional) basalts and basaltic andesites; which are formed in associated with various pyroclastic and sedimentary rocks. These rocks are charactrized by similar geochemical patterns including enrichment in light rare earth elements (LREEs), large ion lithophile elements (LILEs),  and depletion in high field strength elements (HFSEs; e.g., Nb, Ta, Ti). These geochemical evidence indicates magmatism related to volcanic arcs and subduction setting. In addition, the nearly flat heavy rare earth element (HREE) patterns are similar to that of the oceanic island basalt (OIB). These mafic magmatic rocks are characterized by a mantle dominated composition, evidenced by (87Sr/86Sr)i ratios of 0.70404–0.70414, and uniform positiveεNd(t) values of 1.00–4.14. The trace-element and isotopic modelling indicate that the studied basaltic rocks resulted from partial melting of metasomatized lithospheric mantle wedge at the garnet–spinel stability depth in transitional zone. The magmatism in the study area more likely occurred in an incipient volcanic arc setting due to asthenospheric upwelling in response to lithospheric extension during slab retreat 80 million years ago.

The studied mining area is located in the northeast of the Lut block, within the Ahangaran mountain range. The rock units in the region generally include limestone and metamorphosed carbonate rocks that are penetrated by intrusive masses with the composition of diorite, monzodiorite, granodiorite and granite. Based on the structural control of the mineralization zone and the formation of metasomatism succession with the presence of low-temperature hydrous minerals such as chlorite and epidote along with magnetite, the iron mineralization of the area can be considered as a low-temperature skarn type. The mineral chemistry of magnetite and the amounts of Ca, Ti, Al, V, Cr, Ni and Mn are also similar to skarn deposits. Field studies indicate that another younger intrusive mass at depth is the origin of the iron mineralization of the ore zone. Based on analysis of components, calculated on the basis of REE, the ore solution with magmatic origin has moved upward along the faults and after mixing with atmospheric fluids, as a result, it has created a reaction with the carbonate rocks of the iron ore.

The Gol-e- Gohar iron ore mine, in southwest of Sirjan city, is structurally located in the Sanandaj-Sirjan zone and is mostly composed of Paleozoic metamorphic rocks. The highest degree of metamorphism of the rocks of the region is related to the amphibolite facies. The studied of amphibolite indicates that the hornblende and plagioclase are the main and biotite, sphene, quartz, tourmaline and opaque minerals are the accessory minerals. Secondary minerals include chlorite, epidote, calcite, iron oxides, and sericite that have been developed during the alteration phases, as well as chloritization and epidotization of biotites and amphiboles as evidence of retrograde metamorphism. Based on amphibole mineral chemistry studies, amphiboles are formed as a combinations of magnesio hornblende, paragasite and winchite types. According to Geothermobarometry studies, amphiboles are formed under conditions of high oxygen fugacity and at a temperature of 600 to 750° and an approximate pressure of 3 to 7 kbar.

The Garmkhani-Meyham region is located in SE-Qorveh city, in the northwestern part of the Sanandaj-Sirjan zone. This area includes a variety of regional and contact metamorphic rocks. Microprobe data of mineral chemistry show that amphiboles, magnesium-hornblende type; plagioclases, andesine to albite type; biotite crystals, siderophyllite type; white mica, muscovite type and epidotes, clino-zoisite type are in composition.  Based on the mineral chemistry of amphibole, the magmatic series of its constituent magma is the subalkaline and its tectonic environment is supra-subduction. Geothermometric estimates on the amphibole and plagioclase minerals in amphibole- schists, a temperature ranges from 464 to 570 °C and pressure between 3 to 5.6 kbar illustrate passing from greenschist facies to amphibolite facies.

The Kuh-e-Kalut-e-Ghandehari is located about 40 Km northwest of the Anarak (northeast of Isfahan). This area is a part of the Central Iran that is situated in west of the Yazd block; near to the Ashin ophiolite and drastic directional changes of the Great Kavir Fault. In the northwest of Anarak, the Ashin ophiolite is covered by the Cretaceous limestones, and crossed by the Eocene volcanic rocks. The Upper Eocene gabbro-diorite stock cross cuts the Eocene volcanic rocks. Andesites are the predominant unit of the Eocene volcanic rocks. They are grey to dark- grey in colour and have amphibolite xenolith. The main textures of these volcanic rocks are porphyritic, poikilitic, trachytic, sieved texture and glomeroporphyritic. The main phenocrystic minerals of andesites are plagioclase, amphibole and clinopyroxene situated in a matrix of the same minerals and sanidine, magnetite and apatite. Secondary minerals are formed as a result of the hydrothermal alteration and comprise zeolite, chlorite, epidot, sericite, kaolinite and calcite. Mineral chemistry indicates that plagioclases are andesine to labradorite (An= 30-52%), K-feldspars are sanidine (Or= 68-71%), amphiboles are calcic with pargasite composition (Mg#= 0.58-0.71), and clinopyroxenes are diopside (Mg#= 0.91-0.93) in composition. Whole rocks chemical analyses indicate that these andesite and trachy-andesite rocks have calc-alkaline property. The chondrite and primitive mantle-normalized REE and multi-element patterns show LREE and LILE enrichment and HFSE (Ti, Ta, Nb) depletion, which are characteristics of the subduction-related magmas. These data indicate that the primary magmas were genarated by medium degrees of partial melting of the lithospheric mantle spinel lherzolite. Subduction of the Central-East-Iranian Microcontinent (CEIM)-confining oceanic crusts (Naein and Ashin oceanic crusts) are possibly the reason of this volcanism. Geochemistry of these volcanic rocks are similar to the arc-related ones.

The studied area is located in the high Zagros zone and it is considered a part of the Neyriz ophiolite. In this area, the ophiolitic complex is a small coloured melange including radiolarite cherts and serpentinized peridotite rocks. The peridotite rocks are mostly serpentinized harzburgite. The peridotite rocks are mostly serpentinized harzburgite. These rocks composed mainly of olivine, pyroxene, serpentine and spinel, where olivines have been strongly altered to serpentine and pyroxenes to bastite. So, serpentine group minerals are seen in abundance in these rocks. Also, spinel is found in amorphous and amoebic shape in these rocks. Based on mineral chemistry, serpentines are in the range of stability of all three mineral phases, i.e. lizardite, chrysotile and antigorite, and the range of pseudomorphic serpentinites, which shows they are the result of the regressive replacement of olivine and pyroxene with serpentines. Also, these minerals are mostly located in Ol-mesh and Cpx bastite ranges, which shows they are the result of regressive metamorphism of harzburgite and dunite rocks. The spinels are Cr- spinel and pleonaste type. These Cr spinels are ophiolitic type and have residual nature. The low TiO2 and the enrichment of these spinels from Cr is similar to spinel in fore-arc harzburgites. Also, these spinels, in addition to having the characteristics of alpine peridotites, are placed in the overlapping range between suprasubduction (SSZ) and abyssal peridotites. So, the studied serpentinized peridotites are formed from high degrees of partial melting (25-30%) of a depleted mantle in a suprasubduction (SSZ) - fore-arc setting.

The aim of this study was to determine the distribution of palygorskite and associated silicate clays in selected Cenozoic rocks of the Bushehr Province. Thirteen samples of sedimentary rocks were taken and their clay fractions were examined by X-ray diffraction and scanning electron microscopy. Results showed that some sedimentary rocks contain palygorskite but no trace of this clay mineral was found in calcareous shale and calcareous marl units of the Upper Cretaceous to Eocene period. Among sedimentry rocks studied, the Aghajari Formation (Miocene-Pliocene) has the highest quantity of palygorskite. Chlorite, illite, smectite, kaolinite, and quartz were found as other minerals present in sedimentary rocks of the study area. SEM images clearly show the presence pf palygorskite in some sedimentary rocks of the area. It seems that conditions such as shallow intermountain lakes and lagoons were prevailing in the study area during the Cenozoic time.

The Balestan iron deposit is located about 55 km southeast of Urmia city. The main host rock is the quartz sericite schist unit of the Early Precambrian age. Major mineralization occurred along the schistocytes of the host rock. However, open space filling structure is also abundantly observed in the fault zones. Based on field evidence and microscopic studies, the dominant iron mineralization is in the form of magnetite, which is observed along with pyrite and chalcopyrite. Geochemical investigations revealed that the distribution patterns of trace elements and major oxides are very similar to other hydrothermal iron deposits. The microthermometric studies of fluid inclusions shows an average homogenization temperature and salinity of about 276°C and 7.3 wt% NaCl equivalent, respectively.The variation trends in salinity and Th of fluid inclusions can be explained by a cooling and pressurization of ore-bearing fluids. Also, these data show that the Balestan iron ore deposit is located within the field of mesothermal ore deposits.

The Shadan Porphyry copper-gold ore is located in eastern margin of Tertiary volcano-plutonic belt of the Lut block. Hydrothermal Magmatic solutions of granite-granodiorite stock porphyry rocks that are generally intruded  in the Eocene volcanic rocks resulted  in vast potassic, potassic-phyllic, argillic and propylitic alterations in the area. Mineralization in the Shadan ore has been occurred as porphyry, epithermal-vein and hydrothermal breccia. Mineralization is mostly occurred as scattered, stockworks in granodioritic mass and vein type as sulphide, quartz and carbonate veins, trending northwest-southeast. Mineralization are recognized in two types: oxidized (hematite, magnetite, limonite, goethite)  and sulfide (pyrotite, chalcopyrite ,bornite and covelite). According to microscopic and thermometric studies, genesis of the Shadan copper- gold ore is porphyry-epitermal. The results analysis on the primary ore show that the main metallic minerals in the ore are copper and gold. The EDX spectrum of scanning electron microscopy (SEM) on 53 gold particles shows that gold particles are in the form of native gold and electrum is between 1 and 10 microns in size. The occurrence of gold includes mono gold, trapping gold and intergranular gold. Gold grains are within the limonite, and hematite .

The Iranian plateau is located in one of the most complex geodynamic settings within the Alpine-Himalayan belt. The Sangan mining area is the largest Cenozoic skarn iron ore district in the far eastern part of the Alborz magmatic arc in Iran. Granitoid intrusions in the Sangan mining area are subdivided into the fertile Sarnowsar intrusion composed of syenite, syenogranite, and granite; and the barren Sarkhar and Bermani intrusions composed of monzogranite and syenogranite. In this study, we used the zircon geochemical composition from eight samples of Sarnowsar, Sarkhar and Bermani granitoids as an important exploration tool for reconstructing the crustal thickness and its evolution in the Sangan magmatic arc. Zircon Eu/Eu* [chondrite normalized] correlates with whole rock La/Yb, has been used to estimate the crustal thickness. Our results reveal that fertile Sarnowsar granitoids formed in the thicker crust than barren Sarkhar and Bermani granitoids.

In this research, a new compound of tetramethyl-3,3ʹ,3ʺ,3ʺʹ-(propane-1,2-diylbis(azanetriyl))tetrapropionate (TPAT) was prepared from the reaction of propane-1,2-diamine and methyl acrylate in methanol solvent. The composition of TPAT in the base environment, simultaneously with the formation of the complex, was reaction to the ligand 3,3ʹ,3ʺ,3ʺʹ-(propane-1,2-diylbis(azanetriyl))tetrapropanoic acid (H4PAT). 3,3ʹ,3ʺ,3ʺʹ-(propane-1,2-diylbis(azanetriyl))tetrapropionate copper(II) complex [Cu(H2PAT)] was identified by FT-IR, 1H NMR spectroscopy, elemental analysis (CHN) and its structure was determined by X-ray single crystal. H4PAT ligand is coordinated to copper atom through two nitrogen atoms, two oxygen atoms from propionate ion and one carbonyl group from propanoic acid and has a distorted square pyramidal geometry. This complex is crystallized in orthorhombic crystal system with space group Pna21 and Z=4 with a=14.1429(8) Å, b=14.1429(8) Å and c=9.9781(3) Å. The catalytic application of this complex was investigated. 2 mmol of [Cu(H2PAT)] complex was used for the coupling of phenyl bromide, under reflux conditions, without solvent in 120 minutes, and the biphenyl product was formed with 80% efficiency.

In this study, MNPs-Fe3O4 were synthesized, and the properties of these nanoparticles were investigated by FESEM, XRD, FT-IR and VSM. In addition, the performance of MNPs-Fe3O4 along with ethoxylated tallow amine (TAE) surfactant in crude oil demulsification was evaluated by bottle test. The combination of MNPs-Fe3O4 and TAE improves the efficiency of water separation from oil by 94% and reduces the consumption of commercial demulsifier.

In this study, ZnO, α-Fe2O3 and ZnO/Fe2O3 nanocomposites powders with weight ratios of (1:0/.5), (1: 1) and (1: 2) were prepared using hydrothermal method and their structural, optical and magnetic properties were investigated. The results obtained from analysis of the XRD patterns confirmed formation of the hexagonal structures for ZnO and Fe2O3. The absorption spectra of the synthesized samples showed that the absorption in the visible region increases for ZnO/Fe2O3 nanocomposite and its band gap value reduces (increases) in comparison to the zinc oxide (iron oxide). FESEM images showed that Fe2O3 spherical nanoparticles are located on the surface of the ZnO nano-sheets .The results obtained from magnetic studies by VSM revealed that ZnO has a diamagnetic property and α-Fe2O3 shows soft ferromagnetic behavior and for the nanocomposites, the magnetization values increase with increasing the Fe2O3 concentration. In general, the results show that the particle size, optical property and magnetic property of the ZnO/Fe2O3 nanocomposites strongly depends on the concentration of Fe2O3.