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1.
流体包裹体盐度低温拉曼光谱测定方法研究 总被引：3，自引：3，他引：0
氯盐溶液作为流体包裹体中最普遍和最重要的盐水化合物,是测定包裹体盐水溶液含盐度的主要溶质,但由于其强离子键化合物的分子特性在常温、常压下没有拉曼效应,拉曼光谱测试无法获取氯盐的有效特征信息,使得利用拉曼光谱研究流体包裹体分子组分及含盐度的方法存在严重缺陷。本文联合利用激光拉曼光谱探针和冷热台,原位采集了不同盐度的NaCl-H2O和CaCl2-H2O标准盐水溶液在低温下(-185℃)形成的冰、NaCl水合物和CaCl2水合物的拉曼光谱,分析了不同盐度标准盐水溶液形成的水合物拉曼特征峰的变化规律,尝试建立流体包裹体盐度低温拉曼光谱测定方法。分析表明,NaCl水合物约3425 cm-1拉曼特征峰与冰约3120 cm-1拉曼特征峰峰面积比值和配制的NaCl-H2O标准溶液盐度呈良好的正相关(r2=0.9995),CaCl2水合物约3431 cm-1拉曼特征峰与冰约3120 cm-1拉曼特征峰峰面积比值也和配制的CaCl2-H2O标准溶液盐度呈较好的正相关(r2=0.9458)。利用愈合人工水晶法合成的NaCl-H2O和CaCl2-H2O包裹体标样检验了用上述方法低温测定流体包裹体盐度的可靠性,结果表明该技术用于盐度大于0.5 mol/L的NaCl-H2O体系流体包裹体时,数据精度好于20%;用于盐度大于0.5 mol/L的CaCl2-H2O体系流体包裹体时,数据精度最高可达5%,完全可达到半定量-定量测定的要求。研究还发现,包裹体内压可能对低温拉曼光谱测定流体包裹体盐度影响不大,分析中获得的冰拉曼特征峰的拉曼位移(约3120 cm-1)与前人略有差异,可能与实验条件下获得的冰的多型不同有关。与国内外同行的研究结果比较,本研究更加注重该项实验技术的实际应用,通过对不同体系盐水溶液系列进行拉曼光谱实验分析,对实验条件和方法进行不断优化,在确定流体体系的同时实现了包裹体盐水溶液盐度半定量-定量测定,准确度优于传统方法,并且该方法具有很强的实用性。 相似文献
2.
新疆望峰金矿床流体包裹体地球化学及矿床成因类型 总被引：6，自引：2，他引：4
西天山东缘的望峰金矿床受胜利达坂韧性剪切带的控制,成矿过程包括早、中、晚3个阶段,自然金和矿石矿物主要形成于中阶段。岩相学、显微测温及单个包裹体成分激光拉曼光谱研究表明,望峰金矿床石英中的流体包裹体有CO2-H2O型、纯CO2型、NaCl-H2O溶液型和含子晶多相等4种类型。早阶段石英中原生包裹体主要是CO2-H2O型,其盐度1.62%~8.03% NaCl eqv.,流体密度0.73~0.89g/cm3,均一温度为250~390℃,气相成分为CO2。中阶段石英中的原生包裹体包括了所有4种类型,其CO2-H2O型和NaCl-H2O溶液型包裹体的均一温度分别为210~340℃和230~300℃,显示了流体沸腾现象的存在。CO2-H2O型包裹体的盐度0.83%~9.59% NaCl eqv.,密度0.77~0.95g/cm3,气相成分为CO2±CH4±N2。晚阶段石英只发育水溶液包裹体,具有较低的盐度（0.35%~3.87% NaCl eqv.）和均一温度（120~214℃）。根据CO2-H2O型包裹体估算早、中阶段流体包裹体捕获压力分别为110~300PMa和90~250MPa,成矿深度为9~11km。总体而言,望峰金矿床由低盐度、低密度、富CO2的变质流体系统形成,流体减压沸腾导致矿质沉淀,属于中深带的造山型金矿系统。 相似文献
3.
云南哀牢山老王寨大型造山型金矿成矿流体地球化学 总被引：12，自引：4，他引：8
云南哀牢山金矿带是我国最重要的喜马拉雅期金矿带,而老王寨是其中最大的金矿。流体包裹体研究显示:老王寨金矿含金石英脉中流体包裹体类型主要为NaCl-H2O型和CO2-H2O型,其均一温度为102~302℃, 峰值为160~180℃;流体盐度范围变化较大,介于2.5%~12.9% NaCleqv之间,峰值为6.0%~7.5% NaCleqv,显示老王寨成矿流体具有中低盐度和中低温度的特征。 氢氧同位素测定显示成矿流体δDH2O=-115‰~-90‰,δ18OH2O=5.2‰~6.8‰,显示其组成主要为岩浆水,可能与有机沉积物发生过同位素交换。流体包裹体碳同位素组成(δ13C为-6.5‰~-3.9‰)基本落在幔源碳变化范围之内,说明其中CO2可能来自地壳深部,甚至上地幔。综合成矿地质特征和成矿流体的证据,提出老王寨金矿为喜马拉雅期造山型金矿。 相似文献
4.
小秦岭东桐峪金矿床的流体包裹体研究 总被引：4，自引：2，他引：2
东桐峪金矿床位于小秦岭金矿田的中西部,其含金石英脉受韧性剪切构造带的控制。该矿床的构造-成矿过程可划分为4个阶段:Ⅰ黄铁矿-乳白色石英脉阶段;Ⅱ灰白色石英-黄铁矿阶段;Ⅲ石英-多金属硫化物阶段;Ⅳ石英-碳酸盐阶段。相对于小秦岭地区的其他金矿床,东桐峪金矿床的流体包裹体研究资料相对缺乏。文章表明,该矿床内的流体包裹体类型主要为CO2-H2O包裹体和水溶液包裹体,见少量纯液相CO2包裹体。显微测温表明,Ⅰ阶段的构造-成矿流体以中温、富CO2等挥发分为特征,包裹体均一温度为221~392℃,盐度w(NaCleq)为5.5%~7.9%,密度为0.84~0.93 g/cm3;Ⅱ阶段和Ⅲ阶段以CO2-H2O±CH4流体为主,包裹体均一温度为205~350℃(Ⅱ阶段)和224~271℃(Ⅲ阶段),盐度w(NaCleq)集中于5.1%~7.1%,密度为0.83~0.96 g/cm3;Ⅳ阶段的流体演化为中-低温、低盐度的盐水溶液体系,包裹体均一温度为175~185℃。文章对该矿床各成矿阶段的压力进行了估算,Ⅰ、Ⅱ、Ⅲ阶段的流体最小捕获压力分别为123~160 MPa、160~170 MPa、170 MPa左右。 相似文献
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6.
西秦岭铧厂沟金矿床流体包裹体特征研究及矿床成因 总被引：3，自引：0，他引：3
铧厂沟金矿位于西秦岭勉略缝合带南侧,其产出受韧脆性剪切带控制,赋矿围岩为泥盆系细碧岩、凝灰质绢云千枚岩和灰岩。根据脉体穿切关系和矿物交代关系,可以将铧厂沟金矿分为早、中、晚3个成矿阶段。在铧厂沟金矿的石英中发育了CO2-H2O型、纯CO2型、H2O溶液型和含子矿物型四种类型流体包裹体。早期石英中原生包裹体主要是CO2-H2O型和纯CO2型,其成分为CO2+H2O±N2±CH4±H2S,均一温度集中在320~360℃,盐度为0.43%~5.14% NaCleqv;中阶段为主成矿阶段,该阶段石英中包含了所有四种类型的包裹体,其中H2O溶液型包裹体占了大多数,CO2-H2O和水溶液包裹体均一温度集中在240~320℃,盐度为0.43%~11.19% NaCleqv;晚阶段石英仅发育水溶液型包裹体,具有较低的均一温度(118~228℃)和盐度(0.18%~6.59% NaCleqv)。根据CO2-H2O型包裹体计算主成矿阶段压力为70~195MPa,成矿深度为5~7km。总体而言,铧厂沟金矿的初始流体具有中高温、富CO2、低盐度的变质流体特征,晚成矿阶段流体演化为低温、低盐度水溶液流体,流体的不混溶导致了主成矿期的矿质的大量沉淀,铧厂金矿为中浅成的造山型矿床。 相似文献
7.
藏南折木朗造山型金矿成矿流体地球化学和成矿机制 总被引：5，自引：4，他引：1
折木朗金矿位于青藏高原雅鲁藏布江缝合带东段的南侧,矿体受大型脆-韧性剪切带的次级断裂控制。系统的显微测温和激光拉曼测定显示折木朗金矿矿石中存在3类流体包裹体: NaCl-H2O溶液包裹体(类型Ⅰ);含CO2盐水溶液包裹体(类型Ⅱ),此类包裹体又分为两相(Ⅱa)和三相(Ⅱb)2个小类;Ⅲ纯气相包裹体。折木朗金矿床中流体包裹体显微测温显示该矿成矿流体的盐度范围为2.31%~7.39% NaCleqv,平均值为5.33%% NaCleqv,峰值为4.0%~7.0% NaCleqv;均一温度的范围为164.5~273.1℃,峰值为220~240℃,平均值为221.0℃。相对应的密度范围为0.82~0.93g·cm-3,峰值为0.84~0.90g·cm-3,平均值为0.88g·cm-3。折木朗金矿床成矿流体具有富含CO2、低盐度、低密度、中低温度的特征,与造山型金矿成矿流体相似。此外,同位素测定显示成矿流体的氢氧碳同位素组成分别为δDH2O=-36.7‰~-107.5‰,δ18OH2O=4.1‰~5.5‰,δ13C=-9.6‰~-11.5‰,说明成矿流体主要为变质水,但有地幔流体的加入。综合成矿地质特征和成矿流体的证据,提出折木朗金矿为陆陆碰撞造山型金矿。 相似文献
8.
阿尔泰南缘克兰盆地的脉状金-铜矿化及其流体演化 总被引：3，自引：1，他引：2
阿尔泰山南缘泥盆纪克兰火山-沉积盆地蕴藏有丰富的VMS锌铅铜多金属矿床。自晚泥盆世至早二叠世末, 阿尔泰山南缘为NE-SW向强烈挤压的构造环境, VMS矿石受到变形变质改造,脉状金铜矿化发育。金(铜)石英脉主要有2种产状:(1)白色-灰白色(硫化物)顺层石英脉(QI), 产于韧脆性剪切带发育地段,呈细脉状或透镜状产于绿泥片岩、黑云片岩中;(2)斜切黄铁矿化蚀变岩、层状铅锌矿和变质岩产状的黄铜矿-黄铁矿石英脉(QII),与晚期的脆性构造有关。金(铜)石英脉的流体包裹体发育,按室温下相态特征有3类。第I类为含子矿物的高盐度包裹体(L-V-S型),子晶为NaCl, 有时为KCl,包裹体呈孤立或无序分布,代表变质早期流体特征。一般NaCl子晶先消失(210~357℃),包裹体的最终均一温度369~512℃,其捕获温度与变质相的相平衡计算温度相当,反映了变质早期中高温热液活动的特征。第II类是富CO2 包裹体,包括单相的碳质流体包裹体(L CO2、L CO2-CH4或L CO2-N2)和两相富CO2包裹体(L CO2-L H2O)2个亚类。碳质流体包裹体是常见类型,有时与L CO2-LH2O型伴生,在较晚期的黄铜矿-黄铁矿石英脉中表现为原生特征,而在较早的石英脉中常表现为次生特征。萨热阔布的碳质流体可分为纯CO2包裹体和CO2-CH4体系包裹体,纯CO2包裹体的固体CO2熔化温度(Tm,CO2)为 -60~-56.5℃,CO2部分均一温度(Th,CO2) 变化于-23~+31℃;密度一般为0.85~0.89g·m-3。CO2-CH4包裹体的Tm,CO2＜-57℃,可低达-78.1℃,Th,CO2低达-33.7~-17.7℃, 其密度高达1.01~1.07g·m-3。VMS矿床中晚期叠加的黄铜矿石英脉中碳质流体包裹体可分为贫CH4-N2和富CH4-N2的CO2-CH4-N2包裹体,贫CH4-N2的碳质包裹体Tm,CO2=-63.3~-57℃,Th,CO2=-27.5~+29.7℃;富CH4-N2的CO2-CH4-N2包裹体Tm,CO2=-83.4~-65.5℃,Th,CO2=-56.0~+16.9℃。铜金石英脉中与碳质流体共生的LCO2-LH2O型包裹体均一温度Th,total=205~370℃,略低于第I类高盐度包裹体的Th,total=369~512℃。据CO2流体高温高压相图估算包裹体的捕获压力至少为110~300MPa。金(铜)石英脉的主体在相当于445~566℃的高温条件下形成的,而金铜矿化则是在高于205~370℃、110~330MPa的中高温中深条件下发生的。流体包裹体的δ18O为7.54‰~11.84‰ (QI)和3.82‰~7.82‰ (QII), δD为-84.7‰~-98.2‰(QI)和-75.8‰~-108.8‰ (QII)。结合地质特征和流体研究,说明成矿热液来源与区域变质及相关的岩浆活动有关。 相似文献
9.
贵州太平洞金矿床流体包裹体特征及流体不混溶机制 总被引：7，自引：2，他引：5
太平洞金矿床是兴仁-安龙金矿带灰家堡金矿区的重要卡林型金矿之一。流体包裹体研究证明,石英-黄铁矿阶段(Ⅰ)、石英-黄铁矿-毒砂阶段(Ⅱ)、石英-方解石-雄黄阶段(Ⅲ)的包裹体类型丰富,以气液水两相包裹体、CO2-H2O包裹体和纯液相水包裹体为主,CO2两相包裹体、纯气相有机质包裹体和有机质-H2O包裹体次之,偶见气液有机质包裹体。由Ⅰ→Ⅱ→Ⅲ阶段,气液水包裹体均一温度(200～260℃→180～240℃→100～160℃)呈现逐渐降低的趋势。在Ⅰ阶段的石英中,只在局部偶见到CO2-H2O包裹体和气液两相水包裹体共生;在Ⅱ阶段的石英中,纯液相水包裹体、气液两相盐水包裹体、CO2-H2O包裹体、CO2包裹体及纯气相有机质包裹体共存,它们共生在同一平面中且气液两相盐水包裹体和CO2-H2O包裹体测温数据相差不大,说明当时捕获的是不均匀成矿流体,它是由含有机质的成矿流体经历了CO2-低盐度水的不混溶作用形成的。因而认为,太平洞金矿床中成矿早期流体不混溶作用不明显,主成矿阶段流体的不混溶作用是导致金矿质沉淀的重要原因。 相似文献
10.
根据X射线衍射(XRD)分析发现: A Fe3(SO4)2(OH)6(A=K+、H3O+)系列铁钒的XRD数据十分相近,难以用XRD区别,需通过能谱(EDS)辅助分析,才能区分此类铁矾。另外,此类铁矾的003和107面网间距d随K+含量增大而增大,且呈一元三次方程的关系;而033和220面网间距d随K+含量增大而减小,呈一元二次方程的关系。对该现象从铁矾晶体结构方面进行解释:K+、H3O+离子位于较大空隙中,且沿着Z轴方向排列,当K+、H3O+离子之间相互替换时,会导致该铁矾晶体结构在Z轴方向有较明显的变化。 相似文献
11.
在自然界广泛分布着烃-烃不混溶体系中捕获的流体包裹体,由于这些包裹体具有复杂的组成和相态,因此不混溶包裹体组合的判别和热力学参数的计算常常难以进行。根据烃-烃不混溶体系中两个端员组分流体包裹体室温下的相态特征和在温度-压力平面图上等容线交点显示的位置,划分成三种类型流体包裹体组合,本介绍了三种类型流体包裹体组合特征,叙述了不混溶烃-烃包裹体组合的测定和判别方法,并且阐述均一化包裹体相态方程和气-液平衡常数原理和方法与此同时列举了自然界简单的三种类型不混溶烃-烃包裹体组合的测定、判别和计算的几个实例,利用相态方程和气-液平衡常数,不但精确地计算出包裹体均一压力,并且精确地计算出流体密度和体积等热力学参数。最后,利用均一成气相和液相的两种包裹体在 p-T 平面图上等容线交点同样计算出流体包裹体组合的捕获温度和压力。 相似文献
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赤普铅锌矿床成矿物理化学条件研究 总被引：3，自引：0，他引：3
在对矿物共生组合特征讨论的基础上，利用包裹体测温和成分，以及矿物共生相平衡分析，通过物理化学计算方法，获得了赤普铅锌矿床中各主要成矿阶段的物理化学参数及其变化。并利用气液平衡原理─—亨利定律来探讨成矿流体中气体成分的物理化学行为。 相似文献
13.
流体包裹体在喀斯特溶洞化学沉积物中广泛分布,这些在化学沉积过程中所形成的流体包裹体蕴藏着大量的古环境演化和气候变迁的重要信息。通过采集杭州灵山洞中更新世形成的钟乳石样品,对不同纹圈中流体包裹体进行测定,研究流体包裹体的特征,利用不混溶气-水包裹体中最大密度判别和计算方法确定六个纹圈中精确的形成温度和压力;根据气-水-岩化学反应平衡热力学方法,计算出 CO_2成分浓度和古地下水中 pH 值及钟乳石样品形成过程中的 CaCO_3饱和度等。揭示了杭州地区更新纪古环境演化规律。 相似文献
14.
Michael Zilberbrand 《Aquatic Geochemistry》1999,5(2):195-206
Usually, equilibrium constants for aqueous geochemical reactions in the unsaturated zone are assumed to be equal to those
for free water solutions (at atmospheric pressure) considered in classical water chemistry. This paper shows that high negative
pressures in pore water may essentially change these constants in dry soils and sediments.
The influence of negative capillary pressures on equilibrium constants for some important reactions occurring in the upper
part of the unsaturated zone is analyzed. It is shown that values of these constants at low water contents may differ from
those normally used by orders of magnitude. Sediment drying usually decreases the equilibrium constant for salt dissolution-precipitation
reactions (makes precipitation easier) and for silicate weathering (delays it), whilst in the case of dedolomitization, orthoclase-albite
transition and some types of cation exchange the equilibrium constant grows and these processes in dry soils and sediments
have to be enhanced.
This revised version was published online in July 2006 with corrections to the Cover Date. 相似文献
15.
文中报道在实际储层温压条件下(150℃,40MPa,大约4km深度)成功合成了碳酸盐岩烃类包裹体。通过对合成烃类包裹体的显微观察、荧光分析和傅里叶变换红外光谱分析,证实合成了烃类包裹体,且与真实储层中的包裹体具有相似特征,探讨了油水不混溶条件下的流体包裹体捕获机制。实验研究给出4点重要启示:(1)油水不混溶是造成烃类包裹体和水溶液包裹体分带的主要原因;(2)油气快速成藏过程可以被流体包裹体记录;(3)实际储层温压条件下,合成烃类包裹体实验研究有望为储层包裹体分析提供依据和标准;(4)人工合成烃类包裹体为研究含油气条件下储层水-岩作用机理提供了一种有效手段。 相似文献
16.
Calculation of pH and mineral equilibria in hydrothermal waters with application to geothermometry and studies of boiling and dilution 总被引：1，自引：0，他引：1
Using chemical analyses and 25° pH measurements of quenched high-temperature waters, we calculate in situ pH and distribution of aqueous species at high temperature. This is accomplished by solving simultaneous mass action equations for complexes and redox equilibria and mass balance equations, on all components, including a H+ equation with as many as 60 terms (depending on water composition). This calculation provides accurate values for the activities of aqueous ions in a given water at high temperature, which are used to calculate an ion activity product (Q) for each of more than 100 minerals. The value of log(Q/K) for each mineral, where K is the equilibrium constant, provides a measure of proximity of the aqueous solution to equilibrium with the mineral. By plotting log Q/Kvs. T for natural waters, it is possible to determine: a) whether the water was in equilibrium with a host rock mineral assemblage, b) probable minerals in the equilibrium assemblage and c) the temperature of equilibrium. In cases where the fluid departs from equilibrium with a host rock assemblage, it is possible to determine whether this may result from boiling or dilution, and an estimate of amount of lost gas or diluting water can be determined.The calculation is illustrated by application to geothermal waters from Iceland, Broadlands, and Sulphur Bank, hot spring waters from Jemez, Yellowstone and Blackfoot Reservoir (Idaho) and fluid inclusions from the Sunnyside Mine, Colorado. It is shown that most geothermal waters approach equilibrium with a subsurface mineral assemblage at a temperature close to measured temperatures and that some hot springs also approach equilibrium with the host rock at temperatures above outlet temperatures but commonly below the Na-K-Ca temperatures. The log Q/K plots show that some discrepancies between Na-K-Ca temperatures on spring waters and actual temperatures result from a failure of alkali feldspars to equilibrate with the fluid and with each other.Calculations on Sulphur Bank fluids show that boiling probably caused cinnabar precipitation near 150°C and that the boiled fluids equilibrated with secondary minerals near 150° even though temperatures up to 185° have been measured at depth. For the fluid inclusions, the measured bubble temperatures are close to those calculated for equilibration of the fluid with the observed sulfide mineral assemblage.New estimates of stability constants for aluminum hydroxide complexes are included at the end of the paper. 相似文献
17.
常见成矿流体可以近似为CO2-H2O-NaCl体系及其子体系,在成矿过程中一旦被矿物捕获和封存,就会形成流体包裹
体。基于对流体包裹体的热力学研究,可以获得成矿流体的温度、压力和组成等物理化学参数。虽然pH值是一个重要的物
理化学参数,但是对于含水流体包裹体pH值的研究,一直处于探索阶段。目前只有少数研究者实验测定了CO2-H2O-NaCl体
系的pH值,部分研究者建立了热力学模型来计算该体系的pH值。本文结合前人工作,对重要的流体包裹体系（H2O、
NaCl-H2O和CO2-H2O-NaCl） 的pH值计算模型进行了系统归纳,并给出相关体系精确的计算程序。这些体系的执行程序代码
可以从论文出单位或通讯作者获得。 相似文献
18.
The effect of fluids on recrystallization behaviour is well known; however, the detailed microscale distribution of fluid in grain boundaries and the influence of fluid on grain boundary migration are still unresolved. In this study, in‐situ deformation experiments in transmitted light microscopy were undertaken, as this allows continuous and direct observation of the whole range of processes involved in fluid‐assisted grain boundary migration. A new see‐through deformation apparatus was developed to enable the control of fluid pressure. Bischofite containing small amounts of aqueous fluid was deformed at temperatures between 50 and 90 °C, over a range of fluid pressure from 0.5 to 1 MPa, and strain rates of 5 × 10?6 to 1 × 10?4 s?1. The rates of grain boundary migration were measured at different temperatures and strain rates. Detailed observations during and after the deformation illustrate the evolution of migrating fluid‐filled grain boundaries and show that the incorporation of fluids from inclusions as well as their pinch‐off is dependent on the grain boundary velocity, the thickness of the grain boundary and the size and shape of the inclusions. Direct evidence is presented for the contraction of the grain boundary fluids into isolated inclusions after equilibrium conditions are attained. 相似文献
19.
The phase state of the fluid in the H2O–KF ± KCl ± NaF system is studied in the presence of quartz for an experimental assay of the mutual influence of various salts of the fluid-forming mixture on heterogeneous fluid equilibria. The fluid inclusions were synthesized in quartz by the fracture healing method from solutions with KF + KCl and KF + NaF mixtures at 1 or 2 kbar and 700, 750, or 800°C. The results of the fluid inclusion study indicate a heterogeneous state of the fluid and variation in the fluid composition during experiments as a result of its interaction with quartz. The increase in temperature and pressure, as well as variation in the proportions of the salt contents in the fluid-forming mixture, changed the course of chemical reactions. After all the experiments, a glassy phase was observed in some types of inclusions. It is known that aqueous KF or KCl solutions, the solubility of which increases during heating, are characterized by phase equilibria of systems of the first type (Valyashko, 1990), when liquid and vapor are equilibrated for a heterogeneous state of the fluid. In this case, some inclusions should homogenize to vapor. However, no similar inclusions were observed in contrast to denser fluid phases (liquids), which are typical of the upper heterogeneous area of systems of the second (P–Q) type. Some inclusions host solid phases, the solubility of which decreases as the temperature increases. The results of experiments in the presence of KF + NaF solutions showed that the amount of inclusions of heterogeneous entrapment increases at higher temperatures simultaneously with a decrease in the H2O content of the glassy phase. 相似文献
20.
The SW96 formulation explicit in Helmholtz free energy proposed by Span and Wagner (1996) is the most accurate multifunction equation of state of CO2 fluid, from which all thermodynamic properties can be obtained over a wide temperature-pressure range from 216.592 to 1100 K and from 0 to 8000 bar with or close to experimental accuracy. This paper reports the applications of the SW96 formulation in fluid inclusions and mineral-fluid equilibria. A reliable and highly efficient algorithm is presented for the saturated properties of CO2 so that the formulation can be conveniently applied in the study of fluid inclusions, such as calculation of homogenization pressures, homogenization densities (or molar volumes), volume fractions of vapor phase and isochores. Meanwhile, the univariant curves of some typical decarbonation reactions of minerals are calculated with the SW96 formulation and relevant thermodynamic models of minerals. The computer code of the SW96 formulation can be obtained from the corresponding author. 相似文献