مجله بلور شناسی و کانی شناسی ایران
سال بیست و چهارم شماره 1 (پیاپی 63، بهار 1395)

Nakhlak lead deposit, one of the oldest and largest Iranian lead mines, is located in 55 Km from the northeast of Anarak town. Nakhlak deposit occurs as stratabound and epigenetic in Upper Cretaceous dolomitic carbonates host rocks. The hypogene ore deposits include galena and barite that are associated in supergene zone with cerussite. Galena occurs as coarse and fine grains with replacement and open space filling texture and Cuboctahedral form. Inclusion of independent minerals such as fahlore (Tennantite-Tetrahedrite Series), sphalerite, pyrite and chalcopyrite are present with wide diversity in size and type for different veins in galena. ICP-MS Analysis of galena indicates presence of valuable trace elements such as silver (932 ppm), antimony (342 ppm), copper (422 ppm), arsenic (91 ppm), among which silver is the most important. Low values of Bi and high values of Sb as well as high ratio of Sb/Bi represent the Nakhlak galena formed in low temperature - pressure conditions. XPMA analysis indicates these trace elements are concentrated as inclusions in galena. According to the characteristics of the galena and other geological features, Mississippi Valley-type model is proposed for Nakhlak lead deposit.

Pegmatite-aplite dykes from north east of Lorestan Province is located about 25 km east of Boroujerd city and consists of three major zones, from outside to inside including graphic, layered and core zone that obviously shows the effect of fractional crystallization in pegmatites. Microprobe analysis performed on minerals (tourmaline, plagioclase and muscovite) from each three zones. Tourmalines from marginal zone have schorlite to foitite composition and tourmalines from layered zone have foitite composition that both of them lie in magmatic tourmalines category. These tourmalines plotted on FeO/FeO+MgO vs. MgO diagram have Fe# between 0.8 to 1 indicate that  they formed in magmatic conditions and external hydrothermal fluids did not effect  in formation of Tourmalins. Compositions of analyzed plagioclases from all three zones are rich in albite and the average compositions are; marginal zone (Ab98.05), layerd zone (Ab98.78) and core zone (Ab98.43), indicating a high degree of fractionation in source magma.

The Maksan granitoid is located in the south margin of Lut block, and southeastern Iran. It composed of granite, granodiorite, monzodiorite, quartz monzodiorite, diorite and gabbro. Compostions of biotite from different rock types of Maksan granitoid, i. e., granite, granodiorite, monzodiorite (Quartz monzodiorite), diorite and gabbro in SE of Iran have been documented by electron microprobe. Biotite chemical composition is Mg-biotite and based on their TiO2, MgO, MnO, FeO and AlIV content, they are primary magmatic biotites. They have formed in relatively high oxygen fugacity environment and show calc-alkaline characteristic (I-type) that correspond with tectono-magmatic characteristics related to subduction environments. Biotite mineral chemistry shows that magma constitution has low to moderate contamination with continental crust.

The chromite deposits in the Neyriz area have lenticular and sometimes vein-like shape which are replaced in serpentinized dunite and harzburgite. Chromite and serpentinized olivines  are major minerals and hematite and magnetite are minor minerals in the chromitic ores. Except chromite, other minerals have secondary origin that  are related to serpentinization procceses. Whereas along with chromite, only a few of minerals such as  pentlandite have primary origin. Native copper and sulfides such as chalcopyrite and bornite have been formed secondarily in microfracturs of chromite grains filled by serpentine. The results of the geochemical data from chromite ores are indicated by the type of chromite in alpine. Despite being the most abundant element in LREE relative to HREE, only six elements Dy, Eu, La, Lu, Nd, and Y are the most common among other elements. Finally, chromite ore in the area is economic but the frequency of trace elements is minimal and non-economic.

Portland cement could be produced by heating the raw materials (clay, limestone) about 1500°C which clinker will be formed. Geochemical and mineralogical studies of clinker, Portland cement, cement kiln dust and cement mill dust have been carried out by optical microscopy, X-ray diffraction and X-ray florescence. In phase system diagram (CaO-Al2O3-SiO2), chemical components of clinker cement occurred in C3S-C2S-C3A triangular. Clays play important in adsorption of trace elements and heavy metals in the raw materials of cement factory of Neka. According to Bogue equation, this clinker and Portland cement coincide with international standard of cement. Cement kiln dust could be reuse as raw material of cement factory. Mineralogical study of clinker indicates the presence of calcium silicates and brown millerit minerals, while calcium silicates (tricalcium silicate and dicalcium silicate), gypsum, larnit, brown millerit and calcite minerals are indentified in Portland cement. Mineralogical study of cement kiln dust indicates the presence of calcite, quartz, muscovite –illite and chlorite minerals, while calcium silicates (tricalcium silicate and dicalcium silicate), gypsum, larnit and brown millerit minerals are indentified in cement mill dust.

Jebale-Barez plutonic complex is composed of granitoid intrusive bodies and is located in the east- northeast Jiroft, southeastern Kerman Province. The plutonic complex is composed of granodiorite, quartzdiorite and granite - alkaligranite. The Plutonic rocks are mainly composed of plagioclase, alkali-feldspar, biotite, amphibole and quartz. Based on microprobe analysis, plagioclase compositions vary from andesine to labradorite and alkali feldspars occur as orthoclase. Biotite is the common ferromagnesian mineral in Jebale-Barez plutonic complex. Compositionally, it is situated between annite and siderophylite. Most of these biotites are primary magmatic, but some are located in reequilibrated area. The study of oxidation and reduction state of their source magma by biotite chemistry indicates the increasing of oxidation conditions and high oxygen fugacity. Therefore, biotite rich granitoids of Jebale-Barez plutonic complex are I-type or related to magnetite series and the estimated oxygen fugacity imply oxidation magma and its formation in convergent plate boundary. Emplacement or crystallization temperature of the Jebale-Barez plutonic complex, based on the two feldspar thermometer, ranges between 550 to 750 ºC and based on Ti-in-Biotite thermometer ranges between 672 to 720 ºC. Al-barometer shows that the pressure of biotites crystallization is 0.43 to 1.61Kbar and the AlT content of biotite is 2.1 to 2.8. Jebale-Barez plutonic complex has a good ability for copper mineralization based on Uchida et al Method.

The Ma’danjoo prospect area is one of the eastern anomalies of Khaf’s Sangan iron mine in southeast of Mashhad. Geological units in the area include Jurassic sedimentary rocks, skarn, and Tertiary subvolcanic intrusion with monzonitic composition. Skarns have been seprated  in to 7 zones on the basis of abundance and type of the calc-silicate including: garnet, pyroxene-garnet, pyroxene, phlogopite, epidote, chlorite-epidote, and epidote-chlorite skarns. Magnetite and sulfide mineralization were occurred in low temperature phlogopite and epidote skarns. According to electron probe micro analysis (EPMA), the compositions of garnets and pyroxenes are andradite-grossular and hedenbergite to hedenbergite-diopside, respectively. Mineralization at the Ma’danjoo prospect area formed as stratiform and massive bodies in the carbonate rocks. The main ore mineral is euhedral magnetite (40%) with minor amounts of pyrite, pyrrhotite, chalcopyrite, melnikovite, specularite, and pyrolusite. Secondary minerals are hematite and psilomelane. The FeO in the magnetite changes from 84% to 91% and the S content is below 2%. The magnetites are high in Mg (over one percent). Contents of Ni, Cr, V, Ti, Ca, Al and Mn in the magnetite indicate that these magnetites are skarn type. The Ma’danjoo magnesian skarn has some similarities with other magnesian skarns in the Sangan mine especially Dardvey area due to the presence of diopside, phlogopite, termolite and high-Mg magnetite.

The crystal size distribution (CSD) of kyanite and staurolite from the Hamza Qassim and Khazai Bala mtapelites has been studied. All samples show linear CSD pattern for kyanite and nonlinear concave down (with two distinct parts) for staurolite. The linear CSD for kyanite defines high growth rate and equal granular crystals. Two segmental patterns for staurolites can show that they have formed as a result of two possibilities, first is differences on reactions which form the mineral and second is differences on responsible regional metamorphic phase. Although the first case has more evidences. The Gt and nucleation rate (J) for kyanites were 0.931 and -1.6 mm-4. For staurolites the fine and coarse grain parts population density was
 5.25 mm-4 and 6.1 mm-4. Average growth rate at time (Gt) calculated values for fine and coarse staurolite crystals were 0.405mm.t and 0.763mm.t. Detail studies show that nucleation rate ratios for staurolite was 5.5 times more than kyanites, but kyanite crystals were about 2 times coarser than staurolites.  

In this research, Y3-xBixFe5O12 x = (0, 0.1, 0.2, 0.3) were synthesized by a sol–gel method. X-ray diffraction (XRD) patterns confirmed the pure spinel structure for all samples. The magnetic properties of the samples were investigated by the vibration sample magnetometer (VSM). The results obtained from VSM showed that saturation magnetization increases up to x = 0.1 and then decreases for x>0.1. These variations were attributed to increase of superexchange interaction and spin canting. Furthermore, a model which is based on random distribution of Bi ions in yttrium iron garnet structure was used to achieve the best fit for the Mössbauer patterns. This model explained the effect of Bi substitution on the variation of magnetic hyperfine parameters and also verified the VSM results.

Roshtkhar Iron deposit is located in southeast of Khorasan Razavi Province about 48 Km east of Roshtkhar. This deposit is geologically located in the northeast of the Lut block in the Khaf-Bardaskan volcanic- plutonic belt. Intermediate igneous rocks such as stock, dyke, lava and pyroclastic deposits are host rock. Igneous rocks are dioritic porphyry, monzosyenitic porphyry, andesite, basalt and lithic tuff that are granular, porphyry, microlitic porphyry and hyalomicrolitic in texture and consist of plagioclase, K-feldspar, amphibole and pyroxene. The sedimentary units are sandstone, shale and conglomerate. The Fe mineralization in this deposit occurs as east-west veins in the intrusive rocks. These veins are varied in thickness (from a few centimeters to two meters) and length (up to 20 meters?) that are mainly layered and brecciated. The main Iron mineralizations are spicularite and magnetite, whereas primary copper mineral is chalcopyrite that was altered to Cu carbonates (malachite and azurite) and iron hydroxide (goethite and limonite) by supergene processes. The main gangue minerals are calcite and quartz. Propylitic, sericitic-propylitic, silicic and argillic are major alterations, due to alteration of some minerals such as plagioclase, K- feldspar and amphibole to sericite, chlorite and clay mineral.

Khanlogh magnetite-apatite deposit is located in northwest of Neyshabour. This area is situated in Binaloud structural zone and east of Tertiary Quchan-Sabzevar magmatic arc. Geology of the area is dacitic volcanic rock intruded by Oligocene subvolcanic rocks with composition of quartz monzodiorite and granodiorite. Miocene sedimentary rocks trusted on them. The magmatism in the area shows characteristics of I-type granitoids and related to subduction zone. Mineralization occurred in the form of vein and veinlet that is hosted by subvolcanic rocks. Veinlet, brecciate, massive, open space filling, and needle-like structures and textures is observed. Magnetite (low Ti, V, and S) and hydroxyl apatite associated with calcite, epidote, quartz, pyroxene, and chlorite are the most important minerals at deposit accompanied by minor pyrite and chalcopyrite. Hematite and malachite are the main secondary minerals. The main alterations of this deposit are propylitic, carbonate, silicification, and argillic where propylitic and carbonate alteration zones are most abundant than other alterations. Tectonic setting, host rock, mineralogy, alteration, and structure and texture studies indicate the Khanlogh deposit has the most similarity with the Kiruna type deposits.

Granitoid rocks of the central segment of Sanandaj-Sirjan zone, occurring in Lorestan Province, are parts of  a continental arc setting intruded during Mid Jurassic time. Ultramafic rocks are adjacent to this felsic rocks with olivine, orthopyroxene, clinopyroxene and amphibole as their major rock forming minerals. Microscopic observations revealed rounded shape and occurrence of embayments in the olivines attesting different degree of olivine assimilation. By applying electron microprobe analyzes, the chemical compositions of the melts in equilibrium with minerals were calculated. It was revealed that Mg# of the melt is linearly increased as the minerals crystallized. In addition to magmatic origin of the olivine, this trend clearly shows an uncommon behavior of Mg# in the magma that increased during fractional crystallization. Two different possibilities are examined to explain the Mg# increasing. 1- high oxygen fugacity of the magma that led to early crystallization of Fe-oxides; 2- olivine assimilation during fractional crystallization. The results obtained by geochemical modeling and the increase of Ni during fractional crystallization revealed that olivine assimilation during fractional crystallization is the factor that increased Mg# and Ni content of the magma.

Geologically, Shahr-e-Babak playa is located in the southeast of Sanandaj-Sirjan Zone. Based on mineralogical and scanning electron microscopy (SEM) studies, in the studied playa major mineralogical phases include hallosit, kaolinite, illite, quartz, calcite and gypsum. Based on geochemical data, the average aluminum oxide values is 13/93% , silicon oxide is 39/53% and the average of volatiles 18/84% . According to the differential thermal analysis, endothermic reactions of samples occur at temperature approximately 770-810 °C and the exothermic reactions occur at temperature approximately 1120-1140 °C. The main origin of clay minerals  in the studied area is sedimentary and they are formed by erosion and  weathering of a granitoid batholith in the south of Shahr-e-Babak city. Numerous applications of clay minerals in various industries are reasons to do this research.

The ultramafic rocks from the Takht-e-Soleyman metamorphic complex, in Precambrian age, are classified as serpentinized metaperidotites and serpentinites, based on degree of serpentinization. Serpentine forms more than 90 volume% of the serpentinites. On the basis of serpentine polymorphs, textural relations and micro-structure features, variety of serpentinites are determined as massive serpentinites, serpentinite schists and chrysotile-bearing serpentinites.  Chrysotile in serpentinites has been formed due to static condition and brittle deformations. During static state chrysotile and lizardite after olivine and pyroxene are formed as pseudomorphic mesh and bastite textures in the massive serpentinites. Then serpentinization processes reactivated by formation and development of joints and fractures related to brittle deformations at the local sheared zones. Chrysotile occur as fine grained crystals in the serpentinite matrix and veinlets with mm thickness filling fractures of the chrysotile-bearing serpentinites. Sligtht thickness of chrysotile veinlet in the investigated serpentinites can be attributed to the olivine rich composition of protolite. Low amounts of Cr2O3 in composition of the analyzed chrysotile supports low clinopyroxene and high olivine in protolite of serpentinites. Serpentinite schists are formed under ductile deformation condition at the regional sheared zones. Amphibole asbestos occur as veins having meter scale thickness filling of joints and fractures at the regional sheared zone. Length of thin and long asbestos amphibole arrives up to cm. On the basis of petrography, raman spectroscopy, XRD and microprope analysis, both chrysotile- and amphibole asbestos have been recognized in the Takht-e-Soleyman serpentintes.

In the nature, sodium sulfate is one of the most common dissolveds minerals in the water. There are a lot of sodium sulfate in the Tutak craters, which locate in the Rayen city, 120 km southeast of Kerman. Since the perfect time to blooming of sodium sulfate occurs at the late summer and early October, so, sampling of sodium sulfate for this study, done in early September. Samples took from the depths of 30 – 50 cm of the ground surface; and then, they sent to the mineral processing company for XRF, XRD and SEM analysing methods. Mineralogical studies indicate that the sodium sulfate in this area is tenardite type. According to the XRF results and camparison with the major oxides of the Erth,s crust, Na2O is the most abundant oxide in the evaporite minerals of the studied area, SO3 abundances show a direct relationship with the amount of sodium. On the basis of Spearman,s correlation coefficient, which has plotted for XRF data, correlation coefficient of Na2O and SO3, is equal to +1, indicafing dominance of tenardite.

Tertiary igneous rocks of Shurab area in eastern part of Lut block include pyroxene andesite, andesite, trachy andesite, quartz andesite, diorite, quartz diorite and porphyric quartz monzodiorite. Plagioclase, hornblende, pyroxene, biotite and quartz are common minerals and alkali feldspar, opaque, sphene, apatite, tourmaline and zircon exists as minor minerals. Propylitization, chloritization, silisification and tourmalinization are common alterations. Based on electron microprob analysis, tourmaline in quartz monzodiorite is characterized by weakly chemical zoning, high Mg/Fe ratio from dravite type with alkaline nature that originated from Ca-poor metapelites and metapsammites. The studied rocks have low to medium-K calk-alkaline nature and their spider diagrams display enrichment in LILE such as Cs, Rb ,K , Sr and LREE and depletion in Nb,Ti and HREE that indicate their relation to subduction zone. Geochemical characteristics such as high Sr/Y and La/Yb ratios, high SiO2 and no Eu anomaly are comparable to high-SiO2 adakites. Shuorab adakitic rocks are likely originated from partial melting of the crust during delamination process.

9-aminoacridinum acridine-9-carboxylate (1) as a proton transfer ion pair was obtained by the reaction of 9-aminoacridine, acridine-9-carboxylic acid and zinc nitrate (1:1:1 molar ratio) in solvents mixture H2O/MeOH under reflux condition. The crystal structure of this compound was determined by elemental analysis, IR spectroscopy and single crystal X-ray diffraction method. Crystallographic data for 1 was collected at 100 K.  The synthesized compound has been crystallized in monoclinic system with C2/c space group and a = 15.336 (9), b = 14.342(8), c = 19.481(1), β= 109.057(1) cell parameters. The final R value is 0.044 for 4425 independent reflections. There are various types of ionic and non-covalent interactions including N–H∙∙∙O hydrogen bonding, π-π stacking, and cationic-anionic interactions in the crystal structure of (1). This interactions play important role in the expansion of 3D network of (1).

A proton transfer compound (2a4mpH)2(btcH2) was obtained by the reaction of benzene-1,2,4,5-tetracarboxylic acid (btcH4) with 2-amino-4-methyl pyridine (2a4mp), 1:1 mole ratio and is characterized by IR spectroscopy and single crystal X-ray diffraction analysis. The ion pair is crystallized in monoclinic system and P21/c space group with following cell parameters: a = 11.321(2) Å, b = 13.553(2) Å, c =7.026(1) Å, β = 102.473(4)° and Z=2. The final R value is 0.0357 for 9407 total reflections. In the crystal structure, strong and weak O–H···O, N–H···O, C–H···O hydrogen bonds as well as C–H∙∙∙π and ionic interactions connect the various components into a self-associated supramolecular structure.