مجله بلور شناسی و کانی شناسی ایران
سال هشتم شماره 1 (پیاپی 16، بهار و تابستان 1379)

Qaleh-Zari mine is the largest Cu-Au vein type deposit in Iran and is located about 182 km south of Birjand (Khorasan province). The ore grade ranges from Cu= 0.5-8%, Au= 0.5-15 ppm, and Ag= 20-150 ppm. Mineralization concentrated in three major veins. Host rock. .. are mainly andesite to basaltic andesite (paleocene-Eocene). The main paragenesis is: quartz. hematite (specularite), chlorite, chalcopyrite, ± pyrite, ± Ag-sulfosaJts, and ± gold. Samples were collected from three veins at depth of -70, -100, -135, and -1 70 meters. At each level, sample. .. are taken every 10m. Chlorite. .. arc mainly Fe-rich ripidolite, however a few sam pels are brunsvigite and pycnochlorite. Temperature or chloritcs formation were calculated based on the Cathelineau and Nieva (1985) equation. The chlorites were formed between 260-300"C. The temperature of chlorite fonnation is to-3erC less than temperature measured from fluid inclusion. Using chlorite composition and fluid inclusion data from Qaleh- Zari, new equation ichr('39')l presented for calculation of temperature for chlorite formation . The ore tluid contained log mH,S= -3 to -3.5 , log mH, < -5.5 , log f02= -30 to -29.

in this research, Complex (o.l(phcnh(N03hl was synthesizcd and the structure was determined by single-crystal X-ray diffraction method. This complex was synthesized by using 1, 10 - Phcnanthrolinc and each of complexes ]Cd(Meurea)61(NO,h and [Cd(urea),(NO,hl at 50-600C. This complex crystallizes in triclinic crystal system, space group P( -. )(2) with two molecules in the unit cell. Laaice parameters of this compound are:a= 9.6008(5)A h= 9.6044(3)A c= 13.4376(1I)A a= 99.5624(4)° (J= 99.5564(6)° y= 105.0862(3)" V= 1152.65(13)A D,",,= 1.7221 mglmchr('39') After structural determination, Rand Rw constants decreased to 0.0772 and 0.0935 respectively. The Cd atom in this complex was eight-coordinated. In addition, If and XRD studies also carried out. -

Based on this study, the avcfiige gold and silver graJcs in the SaT Chesbmeh porphyry copper deposil arc 0.06 and 1.22 gil re.chr('39')ipcct ivcly which arc very different from the o nes repon ed previously. In the bioti lic andes ite and a!ICrcd phyllic/potassic samples from the siock, the high positin: correlation between the hypogene copper and gold grades ( r=0.81 ), and gold chr('39')lIld silw.f grades (1"=0.6 1), and gold and si lver with the hypogene copper grade (r;:::U.72), indicatc:( I) the contemporaneous deposition of C(lpper, gold ami silver, <lnd (2) gold is probably prescnt in the form of exsolution, invisihle solid solution and nalive or elect rum within the chalcopyri te gwins. Within the secondary sulfide enrichment zone, the gold grade is two times more than the hypogene grade, Silver also indicates the highest concentration within the lellched/oxidc and secondary sulfide enrichment w nes. This st udy indicm(:s th ~l t the Sar Chcshmeh deposit is a gold and silver poor porphyry COPP!;;I - molybdenum deposit.

Antimony mineralization occured in Hamedan district (Faghireh) which is related to Alvand Granitoids. The mineralization occurcd as a series of veins. Thickness of veins are variable and reach up to 0.7m. The veins are emplaced along high angle faults. These faults acted as a pathway for migration of are nuids. Veins are composed of stibnite, pyrite, realgar and orpiment with quartz as a gangue. The textures of veins are open space filling, however brecciations also occured. Monzogranites, which formed the main part of Alvand pluton, is the host of quartz - stibnite veins. Monwgranites are composed of quartz, sodium plagioclase (oligoclase), orthoclase, biotite and sometimes muscovite. The veins arc composed of 30.5% antimony , 0.83 ppm gold and 498 ppm arsenic. Based on geochemical studies, Sb, Au, AS, Ag, Hg, Sn, Ni, Co and Cr contents of host rocks are much higher than the world chr('39')s average monwgraniets and have probably anomalies. Spiderdiagrams show an identical pattern for host rocks and veins, which strongly suggests that these veins are cogenetic with the intrusive rocks (monzogranite). 1n summary, with all geological evidences In the region, it can be concluded that the mineralization is probably occured in the epithermal type.

EfIloresce means formation or crystals or whitish deposits on the surfaces of objer.:ls. The appeflrance of these crystals are due to the type ot" <lrt works, pigment, binding factor used, conselVation treatments and the environment in which the objects arc kept. In order to study the components of eftlorescence and the reasons for thier formation, samples were collected from the sedimenls present on the surface.chr('39'). of twenty six ceramic objects. 111cse objects were excavated from regions with different dimaticconditiolls, Hnd were all unglazed, and belonged to the first or second millcnium BC. Fourier transform infrared spectroscopy (FT~ JR), X~ray diffntction (XRD) and wet chemical analysis were used for analysing of these minute samples. The results showed thAt the deposits consisted 01" either one or ,1 mixture of hchr('39')Ypsum, r.:alcitc, hydrated ferric chloride, feldspa r, pyroxene, hematite and halite. Also the soil of region was analysed <lnd the effects of the cnvironmental ("actors on components and amount of cfllorcscence w.]s studied.

رOpticully sector· twinned ga rn et was found in a piemontite quartz sch ist in Ihe Asemi.gawa area from the Sanbagnwa metamorphic helt. The Sanbagawa metamorphic hell wa.~ formed during a regional Cretaceous intermediate high pressure type of metamorphism which is present through Southwest Japan. The garnet contains abundant inclusions of piemontite, quartz, hematite, braunite, talc and sodie amphibole. It is almost homogenous spessartine garnet (Xsps = 0.85). Piemontite occurs botb in matrix and as inclusion in garnet and albite and it usually shows distinct zonation in which core of the grain contains lower Fe3+ and higher Mn3+ . and AJ-contents than those of the rim. The garnet is .. nisotropic and composed of several parts or sectors visible in crossed polars. They show ditTerent patterns such as octahedral, hexahedral and tetrahedral in which optical orientation and ext inction position are roughly symmet rica l. A rhombododecahedral model ga rnet was used to interpret the geometry of the optically sector structure and show thitl sectors with symmetrical Millerchr('39')s indices have similar optical properties. Textural relation and sys tematic partitioning of Mn3 + , Fe3+ and Al among garnet, picmontite and bntunite indicate that gal net formalion is due to the picmontitc und braunite reaction