在首届成因矿物学会议上

建国以来,我国矿床矿物学、成因矿物学的研究有了很大发展.现代科技理论:量子物理学、固体物理学、量子化学、同位素地质学等的发展,现代实验技术方法:激光光谱、红外光谱、穆斯鲍尔光谱、核磁共振、顺磁共振、扫描电镜、电子探针、气液包裹体测定、同位素分析以及高温高压成矿成岩实验技术等的发展,为成因矿物研究提供了有利的条件.第一届全国矿床矿物成因矿物学术会议表明,我国成因矿物学的研究领域不断扩大.从地壳到地幔,从陆地到海洋,从单矿物到矿物系列,从     

X射线荧光光谱-X射线粉晶衍射-偏光显微镜分析12种产地铜精矿矿物学特征

我国是世界上最大的铜精矿进口国,研究不同产地铜精矿的矿物学特征,能支撑铜精矿原产地分析及相关固体废物属性鉴定.本文研究对象为来自8个国家12个矿区的进口铜精矿样品,采用X射线荧光光谱(XRF)、X射线粉晶衍射(XRD)以及偏光显微镜进行综合分析,探寻这些矿区铜精矿的元素组成、矿物组合特征,探讨不同成因类型铜精矿的矿物学...     

成因矿物学研究在宝石学中的应用

成因矿物学的许多理论,如矿物的物理性质标型、矿物化学成分标型、矿物包裹体成分标型等都已经渗透到了宝石学研究的各项工作中,这些理论为鉴定天然宝石与人工宝石、鉴定宝石是否经过处理以及进一步鉴定天然宝石的成因和产地提供了重要的思路和依据,并且对宝石的优化与合成有着重要的指导作用.本文在总结与分析前人研究成果的基础上,根据某些常见宝石的鉴定特征(如钻石、红宝石、蓝宝石、祖母绿以及其他一些常见宝玉石等),归纳和阐述成因矿物学研究在宝石学中的实际应用.     

坦桑尼亚绿碧玺的矿物学特征及颜色成因

不同产地绿碧玺的产出特征、化学成分、致色机理和形成条件都存在差异.目前关于坦桑尼亚绿碧玺的矿物种属及颜色成因等问题还未得到解决,对其科学鉴定和品质评级造成了一定影响.本文采用红外光谱、拉曼光谱、电子探针、紫外可见光谱等测试技术,对坦桑尼亚绿碧玺宝石矿物学特征及颜色成因进行探究.结果表明:坦桑尼亚绿碧玺呈单晶体产出,无解...     

黄绿色明矾石玉的矿物学特征及颜色成因研究

黄绿色明矾石玉作为近年来市场上新出现的玉石品种,目前有关其宝石矿物学特征的研究相对不足,为其科学鉴定和质量评价造成一定困难。为此,本文采用红外光谱、X射线粉晶衍射、拉曼光谱、扫描电镜、激光剥蚀电感耦合等离子体质谱及紫外可见光谱等测试技术,从矿物组成、显微结构、化学成分等方面对黄绿色明矾石玉进行系统研究,并分析其颜色成因。结果表明:黄绿色明矾石玉的主要矿物组成为明矾石,未见其他矿物成分;玉石整体呈隐晶质结构,粒尺寸小于5μm,这是样品呈现细腻玉石质感的主要原因,但由于缺少如纤维状或鳞片状交织结构,韧性相对较差;黄绿色明矾石玉主要化学成分为O、Al、S、K,此外过渡金属元素V、Fe、Cr含量较高,平均含量分别为23591.52μg/g、4717.99μg/g、2077.67μg/g,结合紫外可见光谱测试存在的500nm以下和以826nm为中心的吸收,认为其黄绿色形成与V~(3+)、Cr~(3+)和Fe~(3+)进入明矾石晶格中类质同相替代Al~(3+)有关;明矾石玉黄褐色风化皮结构相对较粗,主要组成矿物为明矾石和石英,含少量针铁矿和极少量锐钛矿,其黄褐色主要受以针铁矿为主的表生褐铁矿浸染所致。本研究基本明确了黄绿色明矾石玉的宝石矿物学特征及其致色机理,可为今后该玉石的科学鉴定和质量评价提供数据支持。     

《中国金矿床成因矿物学和找矿矿物学论文选集》

最近,武警部队黄金地质研究所将我会成因矿物找矿矿物委员会1986年在成都召开的全国成因矿物找矿矿物学术会议上的有关论文,专辑编篡出版了《中国金矿床成因矿物学和找矿矿物学论文选集》,共计36篇论文,约25万字。该集内容包括:(1)成因矿物学和找矿矿物学的基础理论和研究方法;(2)某些矿物的标型特征,成因和找矿意义;(3)中国金     

第一届全国黄金矿床矿物学与成因矿物学学术会议简况

经中国科协及中国矿物岩石地球化学学会理事会批准,全国黄金矿床矿物学与成因矿物学学术会议于1983年10月5日至10日在山东省掖县、由矿床矿物成因矿物学专业委员会与山东省地质学会联合召开。会议由矿床矿物成因矿物学委员会主任陈光     

成因矿物学在中国的传播与发展

成因矿物学是现代矿物学的重要组成部分。它研究矿物与矿物组合的时空分布、矿物各内外属性间的关联、矿物形成与变化的条件和过程、矿物与其介质间的相互作用及相应的宏微观标志、和矿物成因分类及矿物成因信息的应用等方面的内容。矿物发生史、矿物标型学、矿物温压计、矿物共生分析和矿物成因分类共同构成本学科的理论体系。其中,矿物标型学是该体系的核心。以陈光远先生为代表的中国矿物学家,在20世纪下半叶,创新性地开展了成因矿物族的研究,建立了完善的成因矿物学理论体系,提出矿物标型六性和矿物学填图的四化法则,提出变质岩、花岗岩、铅锌铁金辰砂萤石等矿床的矿物成因标型和找矿标志,有力地指导了中国的地质研究和找矿实践。进入21世纪以来,矿物学填图参数和方法被进一步发掘和完善,矿物磁学和近红外谱学等便捷填图手段得到广泛应用;大纵深蚀变矿化和矿物标型分带规律得以揭示;矿物标型的地球动力学、构造动力学和矿物系统的演化意义得到深度阐释;成因矿物学作为环境与生命过程研究的指导思想,逐步形成了环境与生命矿物学新分支,将矿物个体发生及矿物标型的思想用于对鱼耳石和有孔虫等生物矿物环境响应的研究,将矿物生物交互作用思想用于土壤能量系统修复研究,将矿物环境耦合思想用于生物有机质对矿物自组装结构和过程的调控研究以及海洋矿物对海洋及大气环境的指示研究等,极大地丰富了矿物发生学和矿物标型学的理论。今后应注意有关成果的系统整合,加强矿物个体发生史的实验研究,保障原创性成果的产出;要注重国际交流,使我国成因矿物学的成果真正成为人类的共同精神财富。     

新书《成因矿物学与找矿矿物学》评介

矿物学发展至今,已经出现了不少的分支学科。总起来说,矿物学有三个主要的方向,即矿物晶体化学方向、矿物物理学方向和成因矿物学的方向。其中晶体化学和矿物物理学越向纵深发展,似乎离它的母学科——地质学越来越远,相反,越来越向化学、物理学和材料科学靠近。成因矿物学则不然,越是发展,就越深深地扎根在地质学的土壤中。成因矿物学把矿物学和生产实际密切联系起来。     

《成因矿物学概论》(上册)问世

靳是琴、李鸿超编著的《成因矿物学概论》(上册)已由吉林大学出版社出版。该书全面系统地阐述了成因矿物学的基本问题及其意义。由浅入深、简明扼要地介绍了热力学基本知识,为学习成因矿物学提供了基础。全书共分七章。第三章着重论证了矿物发育史及其研究方向,第四章介绍了典型组合中标型矿物的研究意义,矿物标型     

峨眉山高钛玄武岩中主要的赋钛矿物——榍石的产状、特征及成因

峨眉山玄武岩中钛以什么矿物形式存在一直以来很少有学者提及。本文通过镜下观察、全岩化学分析、X-衍射、能谱、扫描电镜、电子探针、阴极发光对川西南部周公山-汉王场地区钻井岩心中峨眉山玄武岩进行了详细的分析,讨论了其主要赋钛矿物及成因。(1)SiO₂含量46.4%~48.3%和TiO₂>3%显示区内峨眉山玄武岩属于高钛峨眉山玄武岩系列。但多个层段榍石含量>5%,而极少见磁铁矿、钛铁矿;(2)榍石主要以隐晶质的云雾状、雪花状、芝麻点状、枝状等形态分布于微晶长石之间和溶孔、溶洞边缘及裂缝中,少量呈显晶质粒状分布于微晶长石、绿泥石之间。(3)电子探针分析显示:所有含钛矿物中,钛铁矿中TiO₂含量最高,为39.069%,榍石中TiO₂次之,TiO₂含量为17.143%~38.648%,磁铁矿中TiO₂含量最高为12.293%,平均在5%~10%左右,其他矿物基本上都少于1%。(4)扫描电镜及其能谱分析显示:榍石中的Ti含量(2.49%~24.97%)明显高于含钛磁铁矿(2.68%~9.21%)、含钛赤铁矿(3.64%)中Ti含量,与钛铁矿(19.51%)含量相当。分析结果认为:峨眉山玄武岩中大量出现的隐晶榍石可能是岩浆后期产物或期后蚀变的产物。在峨眉山玄武岩中首次鉴别出的大量隐晶质榍石是高钛峨眉山玄武岩中最主要的赋钛矿物。隐晶榍石在玄武岩中的含量是区分"高钛"和"低钛"玄武岩的主要标志之一。     

湖北大冶铁山铁矿床葡萄石和硅硼钙石矿物学特征及形成条件

大冶铁山铁矿床的葡萄石与硅硼钙石均产于夕卡岩的晶洞或裂隙中,与片沸石、菱沸石、辉沸石、方解石等密切共生。本文运用化学分析、X射线粉末衍射、红外吸收光谱和差热分析等现代测试方法,对葡萄石与硅硼钙石矿物学特征及形成条件进行了全面研究。     

矿物学岩石学地球化学研究进展综述

近年来，矿物学除矿物标型特征、成因矿物学、找矿矿物学、矿物物理学等基础研究外，矿物材料及应用研究是其一大特色；岩石研究则更多地与构造演化、地幔作用相联系；研究领域的不断扩大、不同学科相互渗透交叉、新生长点的涌现是当前地球一个发展趋势。     

Observations on the boundary between zeolite facies and prehnite-pumpellyite facies

Using graphical analysis of the system CaO-Al₂O₃-SiO₂-H₂O-CO₂, this paper derives a topology relating the minerals calcite, laumontite, wairakite, prehnite, quartz, and zoisite. Simple thermodynamic reasoning allows this system to be applied to natural rocks and indicates that the first appearance of the assemblage epidote-chlorite-quartz (±albite) should mark the upper boundary of zeolite facies. This assemblage forms at the expense of laumontite+prehnite, laumontite+calcite, or laumontite+pumpellyite, with wairakite likely to replace laumontite as the stable zeolite at low pressures. In natural systems this proposed facies boundary is multivariant and, hence, it is likely to be strongly sensitive to compositional variables. For example, Na-bearing wairakite will be more stable than pure Ca-wairakite and increasing abundance of Fe³⁺ will tend to stabilize epidote+quartz at the expense of the zeolites. Because of this, monitoring the composition of minerals such as epidote, prehnite, or wairakite from lowvariance assemblages may provide a more-sensitive indicator of metamorphic grade than the presence or absence of any particular mineral assemblage.     

Prehnite--Epidote Phase Relations in the Nordre Aputit?q and Kruuse Fjord Layered Gabbros, East Greenland

Layered gabbros at Nordre Aputit?q and Kruuse Fjord were emplacedduring extensional tectonism that led to the formation of theNorth Atlantic basin in the Early Tertiary. Sub-solidus reactionsbetween the gabbros and hydrothermal fluids formed superimposedalteration assemblages in fractures, cavities, and the adjacentgabbros. The earliest secondary minerals are Ca-Al amphibole+ clinopyroxene + biotite ? plagioclase that form thin veinsor porous pegmatitic masses. These minerals are crosscut, overgrownor partially replaced by one or more generations of prehniteand epidote bearing assemblages associated with filling of thefractures and cavities, and with extensive wall rock albitization. Wide variations in the partitioning of Fe³⁺ and Al between coexistingprehnite and epidote solid solutions occur in these alteredgabbros. The partitioning data define distinct clusters in termsof associated mineralogy and paragenetic relations. This, togetherwith prehnite and epidote compositions from active geothermalsystems, are used to evaluate the thermodynamic properties ofthe intercrystalline exchange reaction:When compared to thecompositions of prehnite and epidote in the Nordre Aputit?qand Kruuse Fjord intrusions, it is concluded that the latestand lowest temperature generations of prehnite and epidote displaydisequilibrium partitioning of Fe³⁺ and Al, manifested by theoccurrence of prehnite that is relatively enriched in Fe³⁺ Thermodynamic analysis of phase relations in the system Na₂O-CaO-Al₂O₃-Fe₂O₃-FeO-SiO₂-H₂O-HClis used to determine local equilibrium constraints on Fe³⁺-Alsubstitution in prehnite and epidote. It appears that parageneticand compositional relations of prehnite and epidote are sensitiveindicators of local fluctuations in fluid composition and temperature.The complex magmatic and structural history of the gabbros atNordre Aputit?q relative to Kruuse Fjord is considered to beresponsible for the differences in mineral paragenesis and compositionsof prehnite and epidote within these intrusions.     

Magmatism and Stages of the Tectonic Evolution in the Donets Folded Structure,Eastern Donets Basin

The structure of the Donets Folded Structure underwent a complicated evolution, which included stages of extension, the origin of rift troughs, compression, collision, inversion uplifts, orogenesis, and stages of stabilization and neotectonic reactivation. The paper presents data on the regional tectono-stratigraphic Late Proterozoic–Cenozoic complexes of the Donets Folded Structure, its magmatic complexes, and their setting in this structure, which is identified using geodynamic and paleotectonic analysis. The paper also reports data on the minerageny of the magmatic complexes, which are indicators of tectonic processes and provide guidelines in exploring for and assessing mineral deposits.     

基于FastICA算法的高光谱矿物丰度反演

高光谱分离是定性与定量岩矿分析的核心基础。仿真数据和测量数据可通过FastICA算法处理,计算混合像元中端元数量及端元光谱,并根据计算结果进行丰度反演。实验结果表明：FastICA算法即使在端元光谱、混合矩阵未知且没有任何先验知识的情况下,也能有效分离岩矿高光谱混合像元并得到端元的估计光谱,从而实现矿物识别和矿物丰度反演;但当混合像元中参与混合的端元光谱相似度较高或端元光谱的非高斯性较低时,混合像元的分离精度将降低,混合像元的分离精度越高,端元丰度反演结果越准确。     

会聚束电子衍射对葡萄石空间群的辅助测定

利用透射电子显微技术测定了湖北大冶铁山矿床中的微米级葡萄石空间群。选区电子衍射几何构图法分析表明,该矿物系斜方晶系,衍射消光符号为Ｐｎ－－晶胞参数为α＝０．４５８,ｂ＝０．５５５和ｃ＝１．８５３ｎｍ。（１００）和（３０１）方向的会聚束电子衍射花样研究表明,其空间群为Ｐｎｃｍ。     

Mineral assemblages and phase equilibria of metabasites from the prehnite–pumpellyite to amphibolite facies,with the Flin Flon Greenstone Belt (Manitoba) as a type example

An exceptionally well-exposed part of the Flin Flon Greenstone Belt (Manitoba/Saskatchewan) is used to characterize the mineral assemblage evolution associated with prehnite–pumpellyite through amphibolite facies metamorphism of basalts. Data from these rocks are combined with a large literature data set to assess the ability of current thermodynamic models to reproduce natural patterns, evaluate the use of metabasic rocks at these grades to estimate pressure–temperature (P–T) conditions of metamorphism, and to comment on the metamorphic devolatilization that occurs. At Flin Flon, five major isograds (actinolite-in, prehnite- and pumpellyite-out, hornblende-in, oligoclase-in, and actinolite-out) collectively represent passage from prehnite–pumpellyite to lower amphibolite facies conditions. The evolution in mineral assemblages occurs in two narrow (~1,000 m) zones: the prehnite–pumpellyite to greenschist facies (PP-GS) transition and greenschist to amphibolite facies (GS-AM) transition. Across the GS-AM transition, significant increases in the hornblende and oligoclase proportions occur at the expense of actinolite, albite, chlorite, and titanite, whereas there is little change in the proportions of epidote. The majority of this mineral transformation occurs above the oligoclase-in isograd within the hornblende–actinolite–oligoclase zone. Comparison with thermodynamic modelling results suggests data set 5 (DS5) of Holland and Powell (1998, Journal of Metamorphic Geology, 16 (3):309–343) and associated activity–composition (a–x) models is generally successful in reproducing natural observations, whereas data set 6 (DS6) (Holland & Powell, 2011, Journal of Metamorphic Geology, 29 (3):333–383) and associated a–x models fail to reproduce the observed mineral isograds and compositions. When the data from Flin Flon are combined with data from the literature, two main pressure-sensitive facies series for metabasites are revealed, based on prograde passage below or above a hornblende–albite bathograd at ~3.3 kbar: a low-pressure ‘actinolite–oligoclase type’ facies series, characterized by the appearance of oligoclase before hornblende, and a moderate- to high-pressure ‘hornblende–albite type’ facies series, characterized by the appearance of hornblende before oligoclase. Concerning the PP-GS transition, the mineral assemblage evolution in Flin Flon suggests it occurs over a small zone (<1,000 m), in which assemblages containing true transitional assemblages (prehnite and/or pumpellyite coexisting with actinolite) are rare. This contrasts with thermodynamic modelling, using either DS5 or DS6, which predicts a wide PP-GS transition involving the progressive appearance of epidote and actinolite and disappearance of pumpellyite and prehnite. Patterns of mineral assemblages and thermodynamic modelling suggest a useful bathograd (‘CHEPPAQ bathograd’), separating prehnite–pumpellyite-bearing assemblages at low pressures and pumpellyite–actinolite-bearing assemblages at higher pressures, occurs at ~2.3 to 2.6 kbar. Observations from the Flin Flon sequence suggests devolatilization across the GS-AM transition (average: ~1.8 wt% H₂O) occurs over a very narrow interval within the actinolite–hornblende–oligoclase zone, associated with the loss of >75% of the total chlorite. By contrast, modelling of the GS-AM transition zone predicts more progressive dehydration of ~2 wt% H₂O over a >50°C interval. Observations from the field suggest devolatilization across the PP-GS transition occurs over a very narrow interval given the rarity of transitional assemblages. Modelling suggests fluid release of 1.0–1.4 wt% resulting from prehnite breakdown over a ~10°C interval. This fluid may not be entirely lost from the rock package due to involvement in the hydration of igneous mineralogy across the PP-GS transition as observed in the Flin Flon sequence.