催化分光光度法测定痕量钛   总被引：2，自引：0，他引：2  

周之荣  吴伟 《岩矿测试》1996,15(3):235-237

催化分光光度法测定痕量钛周之荣１吴伟华东地质学院应化系江西临川３４４０００催化褪色光度法测定钛的报道较少［１］，本文研究了痕量Ｔｉ（Ⅳ）催化过氧化氢氧化酸性铬蓝Ｋ褪色反应的影响因素，建立了测定痕量Ｔｉ（Ⅳ）的催化光度法，并用于测定植物及人发中钛。方法...  相似文献   

低温条件下有机酸对铁、铜的淋滤实验研究     

张海祥  王玉荣  梅厚钧 《矿床地质》1997,16(1):86-92

水／岩作用实验研究表明，在低温条件下柠檬酸、草酸和酒石酸对岩石中的铁、铜都有很高的淋滤率。这表明，在表生地质作用过程中有机酸对成矿元素有很强的活化能力。实验研究同时发现，有机酸对成矿元素的活化能力受其分解温度的限制，由于大部分有机酸的分解温度都在２５０℃以下，因而有机酸对成矿元素的活化仅限于低温条件。本次研究还显示，判断一种岩石能否成为矿源层，不能简单的以其中成矿元素的含量高低作为标准，其中更关键的因素是元素在岩石中的存在形式，如果成矿元素在岩石中难以活化的形式存在，那么含量再高也无法提供成矿物质  相似文献   

生物兼容水基磁流体的制备和性质     

王小军  刘云志罗新 《华东地质学院学报》2004,27(4):381-385

用天冬氨酸和谷氨酸化学吸附在纳米四氧化三铁粒子表面，制备得到强生物亲合性的水基磁流体。这种磁流体在磁性药物载体、磁共振造影剂和磁高热治疗肿瘤等领域有良好的应用前景。用体系的电导和旋光度参数表征了两种氨基酸化学吸附在磁粒子表面的过程，研究了酸度、氧化钠浓度、天冬氨酸和谷氨酸的吸附等因素对磁流体的磁性和稳定性的影响。磁测量表明，该磁流体对空气较敏感，60天后饱和磁化强度衰减17％；若保存在磨口瓶中，60天后饱和磁化强度基本不变，可应用于生物医药中。  相似文献   

2-[2-(6-氯苯并噻唑)偶氮]-5-二乙氨基苯甲酸与镍的显色反应     

樊学忠  张国防  范红杰 《岩矿测试》2004,23(1):40-43

研究了2-[2-(6-氯苯并噻唑)偶氮]-5-二乙氨基苯甲酸(6-Cl-BTAEB)与Ni2+的显色反应。结果表明:在pH4.5～7.6的HAc-NaAc缓冲溶液中及十二烷基硫酸钠存在下,试剂与Ni2+形成稳定的蓝紫色配合物,组成为n(Ni2+)∶n(6-Cl-BTAEB)=1∶2,最大吸收波长650nm,表观摩尔吸光系数为1.59×105L·mol-1·cm-1,Ni2+浓度在0～400μg/L内符合比尔定律。用铝合金和合金钢中的微量镍验证该分析方法,所得结果与推荐值相符,6次测定的RSD<2%。  相似文献   

内蒙古镁铁质-超镁铁质岩型铜镍矿床成矿条件与找矿远景分析   总被引：5，自引：2，他引：5  

刘国军  王建平 《地质与勘探》2004,40(1):17-20

按构造环境控岩控矿特点,划分区内铜镍型矿成矿(岩)带,分析成矿条件,研究了与该类矿床成矿有关的镁铁质岩、超镁铁质岩分布规律及铜镍硫化物成矿特征,提出了找矿方向和建议.  相似文献   

石岭沟-拐道沟铜-铅-锌多金属成矿带成矿地质条件分析     

常宗东  韦龙明  王设计  高卫宏  张万业 《矿产与地质》2004,18(2):122-127

成矿带位于北秦岭北部晚元古代-早古生代裂谷带南缘的变质火山岩区，受油房-皇台断裂的次级分支断裂及燕山-印支期的侵入岩体及次火山岩脉的联合控制，成矿地质条件与甘肃白银厂铜-铅-锌矿田相类似，成矿带内地表已发现多条铜-铅-锌矿(化蚀变)体，找矿潜力较大，只要进一步深入开展工作，有望找到与白银厂铜-铅-锌矿田相类似的大型一超大型铜-铅-锌多金属矿床。  相似文献   

药用滑石粉酸中可溶物测定方法考察   总被引：1，自引：0，他引：1  

农以宁  刘珊珊 《矿产与地质》2004,18(6):611-614

考察药用滑石粉酸中可溶物测定方法的重复性、耐用性 ,分析主要影响因素。比较酸溶物提取液滤过介质对测定结果差异的影响 ;采用重量法随机测定酸溶物含量和室间差异。两种滤过介质处理对测定结果没有显著差异 ;室间测定结果没有显著差异 ;30批样品平行测定结果的 RSD值范围为 0 %～ 18.2 %。酸中可溶物测定法存在重复性和耐用性不佳的问题 ,应相应调整酸中可溶物含量限度  相似文献   

Improved Platinum-Group Element Extraction by NiS Fire Assay from Chromitite Ore Samples Using a Flux Containing Sodium Metaphosphate   总被引：1，自引：0，他引：1  

L. Paul Bédard  Sarah-Jane Barnes 《Geostandards and Geoanalytical Research》2004,28(2):311-316

Many chromite-rich rocks contain relatively high concentrations of the platinum-group elements (PGE). In many cases, the phases carrying PGE occur as either platinum-group minerals (PGM) or as base metal sulfides in solid solution in sulfides. In some cases, such as the UG-2 unit of the Bushveld Complex, the PGM are occluded inside chromite grains. Chromites are notably difficult to dissolve in most fluxes and if the chromite contains some PGM the possibility exists that not all the PGE will be recovered during fusion. In this work, shortcomings in published methods of analysis based on the nickel sulfide fire assay procedure were investigated and a new procedure developed based on the addition of sodium metaphosphate to the fusion mixture. Optimum composition of the fusion mixture was found to be 10 g sodium metaphosphate and 9 g silica to 10 g sample, 15 g sodium carbonate, 30 g lithium tetraborate, 7.5 g nickel and 4.5 g sulfur to achieve complete dissolution of chromite grains. The new flux mixture was evaluated by the analysis of reference material CHR-Pt+ (which is known to contain PGM inside chromite grains) and no undissolved chromite grains were found in the glassy slag. Analysis of the nickel sulfide beads from this fire assay using neutron activation analysis showed similar results for Rh and Ru when compared with published conventional true (or accepted) values, while Au, Ir, Os, Pd and Pt values determined here were 10 to 30% higher than the corresponding published conventional true values. It was concluded that the addition of sodium metaphosphate improved chromite dissolution in the flux and appears to improve PGE recovery.  相似文献   

Chemical Composition of Ores from the Takara Volcanogenic Massive Sulfide Deposit, Central Japan     

Daigoro Yakushi  Mamoru Enjoji 《Resource Geology》2004,54(4):437-446

Abstract. The Takara volcanogenic massive sulfide (VMS) deposit occurs in Miocene formation of the Misaka Mountain, the South Fossa Magna region, central Japan. The tectonic setting of the Misaka Mountain is reconstructed to be a part of the paleo Izu-Ogasawara arc which collided with the Honshu arc and to form accreted body in the present position. The Takara deposit, therefore, is considered to have formed in the paleo Izu-Ogasawara arc.
The ores from the Takara deposit are classified into pyrite-type ore, chalcopyrite-type ore, and sphalerite-type ore on the basis of chemical composition and their mineral assemblages. Some pyrite-type ores are characterized by their high Au content. The Au content is hardly recognized in the chalcopyrite-type and sphalerite-type ores.
The ores from the Takara deposit have intermediate bulk chemical composition between those from the Besshi-type deposits and the Kuroko-type deposits that are two representative VMS deposits. However, the bulk chemical composition is closer to that from the Kuroko-type deposits. And moreover, chemical composition of tetrahedrite-tennantite series minerals (tetrahedrite) is similar to that from the Kuroko-type deposits. The bulk chemical composition (Cu, Zn, Co, Pb, and As contents) of ores is affected by the chemical composition of volcanic rocks associated with VMS deposits.  相似文献   

Conditions of pocket formation in the Oktyabrskaya tourmaline-rich gem pegmatite (the Malkhan field, Central Transbaikalia, Russia)     

Igor S. Peretyazhko  Victor Ye. Zagorsky  Sergey Z. Smirnov  Mikhail Y. Mikhailov 《Chemical Geology》2004,210(1-4):91-111

Coexisting melt (MI), fluid-melt (FMI) and fluid (FI) inclusions in quartz from the Oktaybrskaya pegmatite, central Transbaikalia, have been studied and the thermodynamic modeling of PVTX-properties of aqueous orthoboric-acid fluids has been carried out to define the conditions of pocket formation. At room temperature, FMI in early pocket quartz and in quartz from the coarse-grained quartz–oligoclase host pegmatite contain crystalline aggregates and an orthoboric-acid fluid. The portion of FMI in inclusion assemblages decreases and the volume of fluid in inclusions increases from the early to the late growth zones in the pocket quartz. No FMI have been found in the late growth zones. Significant variations of solid/fluid ratios in the neighboring FMI result from heterogeneous entrapment of coexisting melts and fluids by a host mineral. Raman spectroscopy, SEM EDS and EMPA indicate that the crystalline aggregates in FMI are dominated by mica minerals of the boron-rich muscovite–nanpingite CsAl₂[AlSi₃O₁₀](OH,F)₂ series as well as lepidolite. Topaz, quartz, potassium feldspar and several unidentified minerals occur in much lower amounts. Fluid isolations in FMI and FI have similar total salinity (4–8 wt.% NaCl eq.) and H₃BO₃ contents (12–16 wt.%). The melt inclusions in host-pegmatite quartz homogenize at 570–600 °C. The silicate crystalline aggregates in large inclusions in pocket quartz completely melt at 615 °C. However, even after those inclusions were significantly overheated at 650±10 °C and 2.5 kbar during 24 h they remained non-homogeneous and displayed two types: (i) glass+unmelted crystals and (ii) fluid+glass. The FMI glasses contain 1.94–2.73 wt.% F, 2.51 wt.% B₂O₃, 3.64–5.20 wt.% Cs₂O, 0.54 wt.% Li₂O, 0.57 wt.% Ta₂O₅, 0.10 wt.% Nb₂O₅, 0.12 wt.% BeO. The H₂O content of the glass could exceed 12 wt.%. Such compositions suggest that the residual melts of the latest magmatic stage were strongly enriched in H₂O, B, F, Cs and contained elevated concentrations of Li, Be, Ta, and Nb. FMI microthermometry showed that those melts could have crystallized at 615–550 °C.

Crystallization of quartz–feldspar pegmatite matrix leads to the formation of H₂O-, B- and F-enriched residual melts and associated fluids (prototypes of pockets). Fluids of different compositions and residual melts of different liquidus–solidus P–T-conditions would form pockets with various internal fluid pressures. During crystallization, those melts release more aqueous fluids resulting in a further increase of the fluid pressure in pockets. A significant overpressure and a possible pressure gradient between the neighboring pockets would induce fracturing of pockets and “fluid explosions”. The fracturing commonly results in the crushing of pocket walls, formation of new fractures connecting adjacent pockets, heterogenization and mixing of pocket fluids. Such newly formed fluids would interact with a primary pegmatite matrix along the fractures and cause autometasomatic alteration, recrystallization, leaching and formation of “primary–secondary” pockets.  相似文献