内蒙古多伦县沸石岩特征研究

本文首次报道内蒙古多伦县的白石头沟口和二等泉两个矿区的沸石岩特征。研究区沸石岩的矿物组合为斜发沸石、蒙脱石、长石、鳞石英、石英和少量的丝光沸石。沸石岩化学成分比较稳定,两个矿区沸石岩的ＳｉＯ２／Ａｌ２Ｏ３比值均在５．６左右,属高硅型沸石岩;白石头沟口沸石岩ｗ（Ｋ２Ｏ）＞ｗ（ＣａＯ）＞ｗ（Ｎａ２Ｏ）;二等泉沸石岩ｗ（ＣａＯ）＞ｗ（Ｋ２Ｏ）＞ｗ（Ｎａ２Ｏ）,属钙－钾型或钾－钙型沸石岩。沸石岩平均吸铵量约为９４×１０－２ｍｍｏｌ／ｇ,阳离子选择交换性能表现为Ｋ＋＞Ｎａ＋,Ｃａ２＋＞Ｍｇ２＋。多数沸石岩的热稳定性可稳定至７００℃不破坏结构。酸碱度平均值为７．３４～７．７５。     

江苏镇江沸石矿石特征研究

通过对江苏镇江沸石矿石某钻孔样品和开采露头捡块样进行X衍射分析、化学成分分析、吸铵量分析、吸蓝量分析、阳离子交换容量、酸碱度分析等,与样品的颜色相结合分析沸石特征,该钻孔沸石岩矿石的矿物组成主要为斜发沸石、蒙脱石等。     

黑龙江省穆棱沸石矿田矿石矿物特征及物化性能分析

综合应用显微观测、化学分析和物化检测手段，对黑龙江省穆棱沸石矿床沸石岩进行了系统研究，确定其矿物组成主要为斜发沸石和丝光沸石，二可单独产出，也可形成混合型矿石。该矿石在成分上属高硅型沸石，SiO2／Al2O3比值均大于8，有富元素As、Pb等较低。物化性能测试表明，穆棱沸石矿为高品级沸石矿，矿石平均热失重值达12．8％，NH4^ 交换容量为146．10meq/100g^,K^ 交换容量平均9．58mmol/100g，丝光沸石热稳定性可稳定至800℃-900℃，具有良好的开发应用前景。     

沸石的热分析

沸石类矿物因具有阳离子交换作用、催化作用及分子筛作用.它作为工业原料、农业原料、以及公害处理材料有多方面利用价值,很值得注意,还有这种矿物在比较低温条件下脱水,产生“沸石水”,这种热的特性也使人深感兴趣.本研究是想通过用差热分析,研究日本国内产斜发涕石(Clinop-tilotite)的热特性,作为探索天然沸石生成状态的一个线索.实验方法将日本岛根县产斜发沸石选纯.在IN、KCI、NaCI、CaCI_2水溶液中进行离子交换,作成K型、Na型、Ca型沸石,然后通过加热使结构发生变化,经化学分析确认已成为所要求的沸石.然后使用“岛津制作所的A30型热分析装置”以至少33毫升/分钟的N_2进行热矢量分析、差热分析,从沸石中存在的U~+、Na~+”、Ca~(2+)的离子比率中求出     

关于沸石类矿物命名法的建议(Ⅰ)

本文系对IMA CNMMN批准的沸石命名法的修改建议。其中扩展了沸石类矿物的定义 ,今后凡具有沸石的性质 ,但其结构中含有四面体格架者则可视为沸石 ;亦允许非硅和铝的元素在格架内的完全替换。在具特定结构的组成系列中 ,格架外的不同阳离子中的原子比值最大者可确定为独立的矿物种 ,命名时采用相应的元素符号作为后缀 ,用连字符加在系列名称之后 [钙十字沸石类 (philipsite)和方沸石 (analcime)系列中的交沸石 (harmotome)、铯沸石 (pollucite)和斜钙沸石 (wairakite)除外 ]。具有相同结构格架的沸石中空间群对称和有序—无序关系的差异一般不作为建立独立矿物种的根据。除片沸石 (heulandite) (Si∶Al<4 .0 )和斜发沸石(clinoptilolite) (Si∶Al>4 .0 )外 ,沸石的矿物种不能只靠Si∶Al值来区分。失水、部分水化和过量水化不能作为区别沸石独立矿物种的根据。在涉及到沸石的简化分子式或平均分子式时 ,应当避免使用“理想分子式”这一术语。在不同的组成系列中最近确定的矿物种有 :brewsterite Sr、 Ba(锶沸石 Sr、 Ba)、chabazite Ca、 Na、 K(菱沸石 Ca、 Na、 K)、clinoptilolite K、 Na、 Ca(斜发沸石 K、 Na、 Ca)、dachiardite Ca、 Na(环晶沸石 Ca、 Na)、erionite Na、 K、 Ca(毛沸石 Na、 K     

斜发沸石岩的阳离子交换性能——对钾离子选择吸附的研究

斜发沸石是天然沸石中较常见和具有实际应用价值的一种。其化学分子式为:Ca（Na·K）₄Al₆Si₃₀O₇₂·24H₂O。关于斜发沸石的吸附、阳离子交换等性能,国外已有很多研究,并已将天然的斜发沸石、丝光沸石应用于从空气中富集氧、石油化工、原子能放射性废水和工业污水的处理、干燥剂,土壤改良剂、造纸充填剂等许多方面。     

天然沸石岩对铁的离子交换性能

沸石是一种廉价的、可供实际利用的天然无机离子交换剂。近年来国内已相继开展了天然沸石岩对碱金属、碱土金属、重金属和一些放射性元素的交换性质的研究及在海水提钾、污水处理、硬水软化等方面的应用试验。本文研究的目的是考察我国天然沸石岩对铁的交换能力及除去水中微量铁的可能性。研究结果表明,天然斜发沸石岩经过适当的     

斜发沸石对钾离子的吸附/解吸动力学研究

以KCl为钾源、新疆某地所产斜发沸石为吸附剂,研究斜发沸石对K+的动力吸附与解吸效果,并探讨吸附时间、K+初始浓度与吸附量的关系。用pH=5的HCl溶液和(Ca2++Mg2+)浓度/(mmol.L-1)为1.6,3.2,6.4,12.8,19.2,25.6的混合溶液对饱和吸附了K+的斜发沸石进行解吸,实验结果表明:沸石对K+的吸附在4min能达到最大吸附率的96%,30min内达到平衡。Langmuir吸附等温式能对吸附曲线进行很好的描述。单位质量沸石对K+的最大吸附量为44.53×10-3,以阳离子交换吸附为主。pH=5的HCl溶液对K+的解吸量最小,随解吸溶液中(Ca2++Mg2+)浓度增加,解吸滞后系数减小,解吸速率远小于吸附速率。解吸量的自然对数与解吸时间的自然对数呈现明显的线性关系,用指数方程对(Ca2++Mg2+)浓度为25.6mmol/L的解吸曲线进行拟合,R=0.998,拟合方程为qt=3.890t0.210。理论上将吸附的K+全部解吸出来需要74.4d。     

天然沸石岩对铁的离子交换性能

沸石是一种廉价的、可供实际利用的天然无机离子交换剂。近年来国内已相继开展了天然佛石岩对碱金属、碱土金属、重金属和一些放射性元素的交换性质的研究及在海水提钾、污水处理、硬水软化等方面的应用试验。本文研究的目的是考察我国天然沸石岩对铁的交换能力及除去水中微量铁的可能性。研究结果表明,天然斜发沸石岩经过适当的     

NH_4~+型斜发沸石对Zn~(2+)和Ag~+两种抗菌离子的离子交换热力学研究

通过液相离子交换试验研究了Zn2+和Ag+两种抗菌金属离子与NH4+型斜发沸石离子交换的热力学特征,绘制了Zn2+和Ag+的离子交换等温线,计算了不同条件下达到离子交换平衡时,NH4+型斜发沸石对Zn2+和Ag+的选择性校正系数Kc和交换平衡常数Ka,得出了ln Ka值与1/T之间的线性关系,导出了反应标准摩尔焓变(ΔrHθm)、反应标准摩尔Gibbs自由能变(ΔrGθm)和反应标准摩尔熵变(ΔrSθm)。结果表明:达到离子交换平衡时,NH4+型斜发沸石对Zn2+和Ag+的最大交换度分别为0.668和0.856,ΔrHθm分别为7.165 k J/mol和5.276 k J/mol,ΔrGθm0,ΔrSθm0,即该过程是吸热和熵增加反应,并且该反应在20℃能自动发生,升高温度有利于NH4+型斜发沸石交换Zn2+和Ag+;在相同条件下,NH4+型斜发沸石对Ag+的离子交换能力大于Zn2+。     

含蛭石晶层间层矿物的可交换性阳离子及交换容量研究

对采自新疆尉犁蛭石矿、河南灵宝-陕西潼关蛭石矿的工业蛭石矿物样品进行了可交换性阳离子与交换容量研究，发现新疆尉犁蛭石矿金云母-蛭石中可交换性阳离子主要为Na^ 和Ca^2 ，其次为Mg^2 、K^ 、Ba^2 和Sr^2 ；而河南灵宝-陕西潼关蛭石矿工业蛭石样品的可交换性阳离子主要为Ca^2 和Mg^2 ，其次为Na^ 、K^ 等。金云母-蛭石和绿泥石-蛭石间层矿物的阳离子交换容量随间层结构中蛭石晶层的含量增加而增大，一般在56．92～98．95mmol／100g之间，仅为蛭石最大阳离子交换容量的一半。金云母-蛭石样品阳离子交换容量大小与K2O含量呈负相关关系，与(Na2O CaO)含量呈正相关关系。     

流体—岩石相互作用—流体包裹体及蚀变岩某些成分变异的特征

以五龙金矿为例，在同一剖面上采集了不同成矿阶段的含金石英脉和近矿蚀变岩样品，．根据矿物流体包裹体和蚀变岩成分地的测定结果，系统地讨论了不同成矿阶段流体包裹体成（K^ 、Na^ 、Ca^＋、CO2等）和不同蚀变岩成分（K2O、Na2O、CaO1、MgO、CO2等）的变化规律，结果表明，从第二成矿阶段到第四成矿阶段，流体中的Na^ 、Ca^ 、Mg^ 含量有明显的升高的趋势，K^ 含量降低，蚀变岩中，K2O由远离矿体的原岩到靠近矿体的蚀变岩其含量增加，而Na2O、CaO、MgO逐渐降低，这种流体包裹体和蚀变岩中的某些相应成分的变化特征，应该是流体－岩石相互作用的结果。     

唐古拉山发源的河水主要元素与锶同位素来源及环境意义

发源于唐古拉山山脉的河流在青藏高原地区具有流域面积大、径流距离长以及流量大等特点,与喜马拉雅山地区河流共同组成全球河源区最高的水流系统。它们的物理与化学侵蚀在很大程度上代表了在全球气候变化的条件下,大陆的侵蚀作用所发生的变化,即大陆与海洋的物质运移和平衡。发源于唐古拉山北坡的长江源头主要支流楚玛尔河与沱沱河的物理化学特点是溶解的化学成分含量较高,一般为10.66～410.81mmol/L,主要阳离子为Na+、Ca2+和Mg2+,占阳离子总量的97%以上。Ca2+/Na+、Mg2+/Na+、K+/Na+的比值较低,87Sr/86Sr值为(0.708954±0.000020)～(0.711860±0.000011),表明唐古拉山北坡的河水成分以蒸发岩类溶解为主。发源于唐古拉山南坡的怒江源头以及雅鲁藏布江及其支流等的主要阳离子为Ca2+、Mg2+、Na+,占阳离子总量的97%以上。Ca2+/Na+、Mg2+/Na+、K+/Na+的比值较高,87Sr/86Sr值为(0.705534±0.000016)～(0.722856±0.000014),表现为以碳酸盐岩和硅酸盐岩的溶解为主。长江河源区河水中主要化学成分来自蒸发岩,其中Na+和Cl-在河流水化学成分中占比例最大,经计算,唐古拉山北坡长江源头地区的物理侵蚀率为77kg/(km.2a),蒸发岩的化学侵蚀率为49～72.7t/(km.2a),碳酸盐岩的化学侵蚀率为15～20t/(km.2a),硅酸盐岩的化学侵蚀率为2～5t/(km.2a);南坡物理侵蚀率为34kg/(km.2a),碳酸盐岩的化学侵蚀率为25～30t/(km.2a),硅酸盐岩的化学侵蚀率为7～10t/(km.2a)。这些特征反映出北坡高寒干旱环境下河流蒸发岩的化学侵蚀作用较强,南坡碳酸盐岩和硅酸盐岩的化学侵蚀作用大于北坡。     

Carbonate weathering and connate seawater influencing karst groundwaters in the Gevas–Gurpinar–Güzelsu basins,Turkey

There are 59 springs at the Gevas–Gurp?nar–Güzelsu basins, 38 of these springs emerge from the fractured karst aquifers (recrystallized limestone and travertine) and 21 emerge from the Yuksekova ophiolites, K?rkgeçit formation and alluvium. The groundwater samples collected from 38 out of the total of 59 springs, two streams, one lake and 12 wells were analyzed physico-chemically in the year 2002. EC and TDS values of groundwater increased from the marble (high altitude) to the ophiolites and alluvium (toward Lake Van) as a result of carbonate dissolution and connate seawater. Five chemical types of groundwater are identified: Ca–Mg–HCO₃, Mg–Ca–HCO₃, Mg–Na–HCO₃, Na–Ca–HCO₃ and Mg–Ca–Na–HCO₃. The calculations and hydrochemical interpretations show that the high concentrations of Ca²⁺, Mg²⁺ and HCO₃ ^? as predominant ions in the waters are mainly attributed to carbonate rocks and high pCO₂ in soil. Most of the karst springs are oversaturated in calcite, aragonite and dolomite and undersaturated in gypsum, halite and anhydrite. The water–rock interaction processes that singly or in combination influence the chemical composition of each water type include dissolution of carbonate (calcite and dolomite), calcite precipitation, cation exchange and freshening of connate seawater. These processes contribute considerably to the concentration of major ions in the groundwater. Stable isotope contents of the groundwater suggest mainly direct integrative recharge.     

A Comparative geochemical study of pelitic schists and metamorphosed carbonate rocks from south-central Maine,USA

Whole-rock major element chemical analyses of progressively metamorphosed impure carbonate rocks and pelitic schists, collected from the same metamorphic terrain, reveal similarities and differences in the chemical response of these rock types to the metamorphic event. Relative to a constant aluminum reference frame, both schist and carbonate exhibit no detectable change in their contents of Fe, Mg, Ti, Si, and Ca with change in metamorphic grade. Carbonate rocks become progressively depleted in K and Na with increasing grade of metamorphism, while schists exhibit no statistically significant change in their contents of K and Na. Both rock types become depleted in volatiles (principally CO₂ and H₂O) with increasing grade.Whole-rock chemical data permit two mechanisms for migration of K and Na from the carbonate rocks during metamorphism: (a) diffusion of alkalis from carbonate to adjacent schist; (b) transport of alkalis by through-flowing metamorphic fluid (infiltration). Mineral equilibria in schist and metacarbonate rock from the same outcrops allow calculation of the affinity for cation exchange between the two rock types during metamorphism. Measured affinities indicate that if mass transport of K and Na occurred by diffusion, chemical potential gradients would have driven the alkalis from schist into carbonate rock. Because diffusion cannot produce the observed chemical trends in the metacarbonates, K and Na are believed to have been removed during metamorphism by infiltration.The disparity in chemical behavior between the pelitic schists and metacarbonate rocks may be a result of enhanced fluid flow through the carbonates. The carbonate rocks may have acted as metamorphic aquifers; the greater flow of fluid through them would then have had a correspondingly greater effect on their whole-rock chemistry.     

The mobility of rare-earth and other elements in the process of alteration of rhyolitic rocks to bentonite (Lebombo Volcanic Mountainous Chain, Mozambique)

Ca-type bentonite deposits of economic interest occur associated with rhyolitic rocks in the Lebombo volcanics. From previous geological studies on the deposits, besides the economic aspects, little is known about the main formation mechanism of beds of bentonite that can be more than 15 m thick, in some places. Chemical analyses of bentonite samples indicate that elements such as Ca, Mg, Sr, Zn, Cu and Sc are markedly enriched in bentonite in comparison to the parent rock. Other elements such as K, Na, Rb and Ba are depleted in bentonite. HREE (Yb, Lu) and Y are depleted in the bentonite samples, as well as Cs, Rb, Ta, U, Ba, Co, Cr and Pb. Concentrations of the LREE (La, Ce, Nd, Sm, Eu), Sc and Ga are slightly higher in the bentonites than in the parent rocks. The chondrite-normalized REE patterns show identical trends both in the rhyolites and bentonites samples. Alteration of the parent rocks to bentonite is associated with leaching and subsequent removal of, principally, K and Na in open-system conditions.     

Hydrogeochemical investigations of thermal waters in the northeastern part of Morocco

Northeastern Morocco is characterised by a large number of surface geothermal manifestations. Thermal waters are hosted within sedimentary rocks, and in particular the Liassic dolomitic limestones act as a reservoir. The presence of geothermal waters is closely related to important fault systems. Meteoric water infiltrates along those fractures and faults, gets heated, and then returns to the surface through hydrothermal conduits. Most of the thermal waters are of Na–Cl and Ca–Mg–HCO₃ types. In this paper different geochemical approaches were applied to infer the reservoir temperature. Na–K–Mg^1/2 ternary diagram points to temperatures ranging from 100 to 180 °C. Cation geothermometers suggest an average reservoir temperature of about 100 °C. Mineral solution equilibria analysis yields temperatures ranging from 50 to 185 °C. The silica enthalpy mixture model gives an average value (about 110 °C) higher than that inferred from cation geothermometers.     

Ore-forming solution and genesis of a rock crystal deposit in south Hunan,indicated by fluid inclusion studies

Si, Al, Ca, Mg, Fe, Na, K, CO ₃ ^?2 , F, etc. are detected from the fluid inclusion leachates. Among these constituents, Si, Na, and CO ₃ ^?2 are predominant, amounting to more than 80 percent. This indicates that the ore-forming solution must be alkaline with Si, Na, and CO ₃ ^?2 as its dominant components. Homogenization temperatures for the solution range from 80 to 360°C. Although rock quartz can crystallize at the above temperature interval, perfect crystals of economic importance are largely formed below 260°C. The temperature of formation increases toward the granite intrusives at a rate of about one degree per meter. It is estimated from the lithostatic load that the salinity of rock quartz is 17–23 (NaCl wt%), while that of vein quartz is relatively high as compared with the former. There is a tendency for the salinity of the ore-forming solution to increase with depth.     

Relationship between exchangeable cations and palaeosalinity

In Carboniferous shales a relationship has been found between exchangeable cations and palaeosalinity. In the marine shales the concentration of exchangeable Mg is higher than in shales deposited in fresh and brackish water, and the concentrations of exchangeable Ca, Na and K are lower. The same relationships have been observed in modern sediments. When the cation concentrations in the whole rock are compared with the exchangeable cation concentrations, incorporation into the sediment of K and possibly Mg in the marine environment is indicated. Furthermore, the loss of Ca and Na from the sediment can be accounted for by the loss from exchange sites. Reactions taking place during halmyrolysis would appear to be more important than those taking place during diagenesis.