中国南方典型宁乡式铁矿沉积特征与成矿机制分析

宁乡式铁矿是我国南方最具代表性的沉积型铁矿,为了探讨其沉积特征与成矿机制,本文借助偏光显微镜、扫描电子显微镜和TESCAN综合矿物分析仪,选取采自桂东北、鄂西成矿区的若干矿石样品进行岩石学和沉积学研究,深入剖析铁质鲕粒的显微组构和地球化学特征。结果显示宁乡式铁矿为混积岩,具有典型的鲕状结构,可划分为砂岩型、灰岩型和混合型等三种类型,赋存于中泥盆统信都组、上泥盆统黄家磴组和写经寺组地层中,含矿岩系总体为一套砂岩、泥页岩和泥灰岩组合,形成于区域海侵背景下的滨海、滨–浅海转换带;矿石中铁质鲕粒形态多样,粒径多集中于0.2~0.5 mm,少数铁质鲕粒的矿物相和主量元素呈圈层状分布,核心可为石英或生物碎屑充填,外部为赤铁矿、鲕绿泥石及胶磷矿环带互层。研究表明矿石的形成可划分为成矿物质准备期、铁质鲕粒形成期和铁矿沉积期三个阶段,强烈的古陆风化作用提供了成矿物质来源,成矿物质在机械沉积作用、胶体化学沉积作用和生物沉积作用下富集并沉淀,期间经历了复杂的氧化还原过程,最终压实固结为宁乡式铁矿。

     

Aggregation of colloidal iron during estuarine mixing: Kinetics,mechanism, and seasonality

The colloid chemistry of iron and humic aggregation was studied in a series of laboratory experiments, which were related to seasonal aggregation extent data collected in a temperate estuary. Kinetically, the aggregation of iron occurs with a rapid initial reaction, finished within a few minutes, followed by an extensive, slow second reaction, which lasts for several hours. Organic carbon aggregation, however, occurs primarily in the first reaction. The first reaction is perikinetic while the second reaction is observed to be either perikinetic or orthokinetic, depending on the pore size of the filter used to clarify the suspension. The second reaction involves aggregation of small filtrable colloids (<0.5 μm) with larger aggregates formed in the first reaction, and follows pseudo-second order kinetics with respect to the filtrable iron concentration when finer filters (<0.5 μm) are used for clarification. Little or no temperature dependence is evident for the first reaction extent, while increasing temperature strongly enhances the second reaction. An activation energy of 9–11 kcal·mole^?1 for the second reaction is due to a combination of transport and charge repulsion terms. Field data show a correspondingly greater aggregation extent of iron with salinity in warmer months relative to colder months.     

Geochemical mechanism of alkali metasomatism and formation of iron deposits

Discussed in this paper are the processes of albitization and iron activation during the formation of iron deposits, the transport and hydrolysis of iron, chemical reaction characteristic of wall-rock alteration responsible for the localization of iron deposits, the dynamic factors affecting these reactions and systematic variations in pH of ore-forming solutions. A metasomatic series of Na→ Ca→ Fe is noticed when diorite and dark minerals + anorthite + quartz react with 1–3m NaCl solutions at 400°–500°C. Hydrolysis of FeCl₂ has been experimentally studied as a function of temperature and pressure. It is suggested that the pH of ore-forming solutions varies in the direction of alkalic→intermediate→acid→intermediate←kalic from early to late stages.     

Sedimentary pyrite formation: An update

Sedimentary pyrite formation during early diagenesis is a major process for controlling the oxygen level of the atmosphere and the sulfate concentration in seawater over geologic time. The amount of pyrite that may form in a sediment is limited by the rates of supply of decomposable organic matter, dissolved sulfate, and reactive detrital iron minerals. Organic matter appears to be the major control on pyrite formation in normal (non-euxinic) terrigenous marine sediments where dissolved sulfate and iron minerals are abundant. By contrast, pyrite formation in non-marine, freshwater sediments is severely limited by low concentrations of sulfate and this characteristic can be used to distinguish ancient organic-rich fresh water shales from marine shales. Under marine euxinic conditions sufficient H₂S is produced that the dominant control on pyrite formation is the availability of reactive iron minerals.Calculations, based on a sulfur isotope model, indicate that over Phanerozoic time the worldwide average organic carbon-to-pyrite sulfur ratio of sedimentary rocks has varied considerably. High $\text{C}\text{S}$ ratios during Permo-Carboniferous time can be explained by a shift of major organic deposition from the oceans to the land which resulted in the formation of vast coal swamps at that time. Low $\text{C}\text{S}$ ratios, compared to today, during the early Paleozoic can be explained in terms of a greater abundance of euxinic basins combined with deposition of a more reactive type of organic matter in the remaining oxygenated portions of the ocean. The latter could have been due to lower oceanic oxygen levels and/or a lack of transportation of refractory terrestrial organic matter to the marine environment due to the absence of vascular land plants at that time.     

鞍山-本溪地区条带状铁矿的Fe同位素特征及其对成矿机理和地球早期海洋环境的制约

本文报道了鞍山-本溪地区晚太古代条带状铁建造的主量元素、微量元素、稀土元素和Fe同位素的分析结果.结果显示:铁矿主要由Fe2O3T和SiO2组成,具有较低的Al2O3和TiO2含量;微量元素含量和稀土总量均较低;经页岩标准化的稀土元素配分模式呈现轻稀土亏损、重稀土富集;具有明显的La、Eu、Y的正异常;较高的Y/Ho比值.这些特征均表明鞍山-本溪地区条带状铁矿是由极少碎屑物质加入的化学沉积岩,成矿物质主要来源于海底热液的贡献.相对于标准物质IRMM-014,条带状铁矿石的Fe同位素组成最突出的特征是均为正值,这是由于二价铁溶液经部分氧化和沉淀形成富集重铁同位素的三价铁氧化物或氢氧化物的结果,且沉淀程度的不同是控制Fe同位素组成变化的重要因素.条带状铁矿无明显的Ce负异常和Fe同位素组成为正值的特征暗示了铁矿沉淀时的海水为低氧逸度环境.     

中新生代盆地蒸发岩沉积旋回对比及库车盆地成钾探讨

新疆库车盆地古近纪—新近纪发育巨厚的蒸发岩沉积,古近纪蒸发岩沉积主要发生在盆地西部的拜城凹陷,新近纪吉迪克时期,蒸发岩沉积迁移至盆地东部的康村凹陷。根据剖面及钻井资料,利用蒸发岩沉积旋回,对欧洲莱茵地堑盆地、库车盆地、云南兰坪_思茅盆地、江汉盆地、大汶口等盆地蒸发岩沉积特征进行分析和对比。结合蒸发岩沉积背景及库车盆地钻井资料,对库车盆地成钾影响因素、成钾可能性、成钾层位进行了探讨。研究认为,库车盆地的次级构造单元拜城凹陷、康村凹陷具有成钾的能力,钾盐层应位于Ⅰ₂、Ⅰ₄蒸发岩沉积旋回的上部。对比研究显示,库车盆地具有成钾的远景和潜力。     

Sedimentary basins: Regularities in their formation and classification principles. Communication 2. Sedimentary rock basins

The article is dedicated to sedimentary rock basins. It is postulated that sedimentary rock basins represent an element of the Earth’s sedimentary shell characterized by the general thermobaric regime, type of fluidodynamics, and combination of epigenetic mineral resources. Fluidodynamic regimes of three types are recognized in the upper part of the crust: infiltration, elision, and exfiltration. The dominant type of fluidodynamics is reflected in the most widespread mineralogical-geochemical zonality and association of epigenetic mineral deposits. These properties allow us to define the infiltration and elision types of rock basin in the sedimentary shell. The structural features of different-type rock basins are characterized with the emphasis on their relations with geotectonics.     

A preliminary study on the mechanism and physico-chemical conditions of formation of Gongchangling rich iron deposit

Field observations and results of experimental studies show that the Gongchangling rich iron deposit is characterized by multigenesis as a result of repeatition of different geological processes. It probably resulted from the infiltration of silica under the influence of aqueous solutions derived from migmatite-granite. Because the formation of rich iron deposit was accompanied by the formation of skarn minerals and the transformation of sedimentary-metamorphic poor iron deposits, characteristics of both skarn deposits and stratabound ore deposits can therefore be recognized. Experimental data indicate that physico-chemical parameters of formation of the rich iron deposit areP=2kbar,T=500–600°C, pH=8–10, and \(f_{O_2 } = 10^{ - 25} \) bar.     

鲕状铁建造的特征与形成机制——以鄂西泥盆系火烧坪铁矿床为例

鲕状铁建造(Ooidal Ironstones,OIS)是一种独特的含砂质、泥质、硅质或硅质碳酸盐,且铁质鲕粒含量超过50％,铁含量超过15％的沉积铁矿床.上扬子地区中—上泥盆统OIS广泛发育,被称之为"宁乡式铁矿",是我国南方重要的铁矿资源.本文选取鄂西地区的火烧坪铁矿床作为研究对象,通过对沉积相的识别与划分、矿石组...     

沉积型锰矿床的形成及其与古海洋环境的协同演化

海相沉积型锰矿的成矿过程受古海洋沉积环境影响，而古海洋环境又与超大陆聚合与裂解、极端地质事件、生命演化等密切相关，因此，海相富锰地层是岩石圈、水圈、大气圈和生物圈等多圈层耦合关系与物质循环相关信息的重要载体。深层海水缺氧模型、最小氧化带模型和幕式充氧模型都显示海水中氧化还原梯度的变化是导致锰矿形成的最主要原因。全球范围内海相沉积型锰矿主要形成于古元古代、新元古代和显生宙3个地质历史时期。其中，元古宙时期，地球上发育了完善的氧化还原分层的古海洋结构；古元古代早期和新元古代，超大陆裂解引起的海平面升降变化导致古海洋氧化还原结构产生动荡，并促使大规模沉积型锰成矿作用发生；地球沉寂期（1800~800 Ma）涵盖了整个中元古代，这一时期仅在华北地台发育了少量沉积型锰矿床，反映该时期古海洋中锰的迁移受到了抑制；显生宙地球再次进入活跃期，经历了数次海洋缺氧事件，冰室-温室气候交替促使海水的化学性质剧烈变化，并在局部氧化还原分层的沉积盆地中富集形成沉积型锰矿床。总之，古海洋氧化还原环境的变化是沉积型锰矿形成的必要条件，同时，区域性沉积盆地的结构、海平面的升降、火山作用导致的物缘供给等多种因素都会影响沉积型锰矿的形成。与沉积型铁矿相比，沉积型锰矿对局部海水化学性质的变化更加敏感，综合研究铁锰矿床的共生与分异过程，将有助于更加有效的识别不同尺度的沉积过程与古海洋环境变化。     

四川盆地灯影组沉积相及演化规律

通过钻井资料、野外露头、录井、测井等资料的综合应用,系统识别出陆源碎屑滨岸、混积台地、碳酸盐岩台地、斜坡-盆地是四川盆地灯影组主要的沉积相类型.盆地内灯影组二段及四段主要以碳酸盐台地沉积为特征,可细分为碳酸盐潮坪、颗粒滩、灰泥丘、局限泻湖亚相.通过建立沉积模式表明,灯影组大致经历海侵-海退-海侵的沉积旋回,一段至二段为海侵阶段,三段为海退阶段,四段为海侵阶段.     

江汉盆地潜江凹陷上始新统含盐岩系准原生白云岩的沉积学特征与形成机理

江汉盆地是我国东部独具特色的古近纪盐湖盆地，其潜江凹陷上始新统含盐岩系中的泥晶白云岩由泥晶白云石组成。泥晶白云石在阴极发光下呈红色、橙红色，与其伴生的矿物除原生钙芒硝、石盐、陆源泥质外，方解石没有或极少； X衍射分析结果表明，泥晶白云石的CaCO3摩尔含量平均为57.30％，有序度平均为0.40，具高富钙、低有序的特征；与钙芒硝岩的紧密共生，说明泥晶白云岩沉积环境的水介质为高盐度的咸水或淡卤水；根据氧同位素数据计算的沉积环境的水体温度平均为30.5℃，与泥晶白云石伴生的原生钙芒硝晶体中的包裹体均一温度最低值为44℃，这2组温度数据基本接近，表明泥晶白云石沉淀时环境水体的温度大致在30.5～44℃之间。由此推断，潜江凹陷上始新统含盐岩系产出的泥晶白云岩是在具较高温度和盐度、高Mg/Ca比值、常年性分层古盐湖水体中，由化学沉淀作用直接形成的准原生白云岩。     

Kinetics of removal of iron colloids from estuaries

Laboratory experiments indicate that colloidal Fe is aggregated in estuarine waters by a second-order kinetic mechanism. The corresponding rate coefficient is proportional to the square of the salinity. A simple theoretical formulation is presented to describe the distribution of Fe in an estuary, based on observed second-order kinetics. The distribution depends on a single parameter whose value may be determined from measurements of the physical characteristics of the estuary. The theoretical expression accurately predicts observed distributions of Fe in a variety of estuaries, suggesting general applicability.     

Decompression mechanism of ferric iron reduction in tektite melts during their formation in the impact process

The analysis of available data on the Fe³⁺/Fe²⁺ ratio of impact-produced glasses showed that tektites and some other types of impact glasses are reduced compared with the precursor target material. Possible reasons for the change in the degree of iron oxidation in the impact process are still debatable. Based on the analysis of redox reactions in relatively simple systems with iron in different oxidation states (Fe-O and SiO₂-FeO-Fe₂O₃) and the available data on the influence of temperature, oxygen partial pressure (pO₂), and total pressure (P _tot) on the Fe³⁺/Fe²⁺ ratio of silicate melts, a model was proposed suggesting that the lower Fe³⁺/Fe²⁺ values of tektites formed in the impact process compared with the initial target material could be related to the characteristics of oxygen regime during the decompression stage following shock compression. One of the main prerequisites for the occurrence of reduction reactions involving iron and other elements is the attainment of high temperatures (>1800–2000°C) at a certain stage of decompression, providing the complete melting and partial evaporation of the material. When the vapor pressure in the system becomes equal to the total pressure during adiabatic decompression, a further decrease in P _tot will be inevitably accompanied by a decrease in pO₂ and, correspondingly, partial reduction of Fe³⁺ to Fe²⁺ in the melt. The reactions of decompression reduction occur under closed-system conditions and do not require oxygen removal from the system. The higher the temperature and Fe³⁺/Fe²⁺ ratio of the melt, the more extensive iron reduction can be observed during the final stages of decompression. If the temperatures attained during decompression after an impact event are sufficient (>2500–3000°C) for the complete evaporation of the material, the melt produced during subsequent condensation must be significantly more reduced than the initial material. The final stage of the impact process is characterized by a catastrophic expansion of the explosion cloud, condensation, and rapid cooling. During this stage, the system is already not closed. The quenched glasses of this stage record the redox state of earlier melts. In addition, they can contain microinclusions of the products of nonequilibrium vapor condensation with iron compounds of different oxidation states, including metallic iron and iron oxides (wüstite, magnetite, and hematite).     

Banded iron formation to high-grade iron ore: a critical review of supergene enrichment models

All the major worldwide direct-shipping iron ore deposits associated with banded iron formations (BIF) are characteristically deeply weathered. They extend to considerable depths below the water table and show well-preserved primary structures and textures, but characteristically most deposits contain no evidence of chert bands being present prior to weathering. Recent studies have found evidence of hydrothermal and/ or metamorphic influences in the development of certain ore deposits and new genesis models such as the supergene-modified hypogene model have been postulated for major high-grade iron ore deposits. Nevertheless, there are many high-grade deposits that show no evidence of hypogene alteration and for which a hypogene or metamorphic genesis is unreasonable that are automatically ascribed to supergene enrichment, commonly erroneously attributed to lateritic weathering in tropical environments. Laterite (sensu lato) is a soil formation in which primary textures are destroyed and is underlain by a pallid zone showing the preservation of chert and the depletion, not enrichment, of iron oxides and thus is totally incompatible with the formation of the high-grade ore deposits. Various theories and models that purported to explain the conditions under which such a uniquely BIF-related dissolution of quartz and residual accumulation of hematite could occur by supergene processes typically conflict with current understanding of groundwater hydrology, chemistry, weathering processes and soil formation.Supergene enrichment of ore is universal in the leaching of gangue minerals such as iron silicates, carbonates and apatite and supergene enrichment of BIF to low-grade ore is common in near surface environments above the water table such as ferrugenised BIF outcrops, detrital ore deposits, and some shallow ore deposits that have been subjected to prolonged exposure to fresh meteoric water. In all cases of supergene enrichment traces of the chert bands are visible and the dissolution or replacement processes for the removal of quartz are clear, in direct contrast to the most important deep saprolite ore deposits that show no trace of chert bands.The widespread acceptance of an inappropriate and untenable supergene enrichment model inhibits search for the true origin of the ore and our ability to predict and find concealed high-grade ore deposits.     

Lithofacies features and mechanism of formation of “Zihe-type” time- and strata-bound iron ore deposits in central Shandong province

The Lower Palaeozoic system is a series of iron-bearing rocks consisting mainly of shallow sea-fades carbonates. On the basis of microfacies analysis of the carbonate rocks, the Lower Palaeozoic sedimentary sea basin is divided into two broad sedimentary-tectonic regions of four sedimentary facies and eight subfacies. The original iron-rich carbonates were deposited in saltlakes, lagoons, etc. of the restricted basins. Over the long geological history, the original iron formations were reconstructed to various extents by late tectonic processes. Geological observations and studies on the equilibrium mechanism of oxygen/sulfur isotopic fractionation and the composition and temperature of fluid inclusions in the minerals indicate that thermal brines played an important role in reworking of the original iron-rich carbonate rocks, which led to the formation of sedimentary-reworked strata-bound ore deposit.     

湍流混合动力学机理研究

在分析传统混合动力学机理基础上,通过宏观混合与微观混合时间量级的对比,提出了湍流条件下,涡流扩散主导宏观混合,分子扩散主导微观混合,而混合过程由宏观混合主导,欧拉数Eu可作为混合效果的控制指标,并通过3种不同容积反应器的混合搅拌试验,进一步证实了该指标的实用性。     

黄陇煤田侏罗系延安组沉积特征

介绍了煤田各矿区延安组含煤地层的岩性、相序、砂体形态、成煤环境与赋煤规律,还探讨了各矿区沉积环境的演化。

     

Sedimentary basins,regularities of their formation and classification principles: Communication 1. Sedimentation basins

Two types of sedimentary basins are proposed: sedimentation basins and rock formation basins (rock basins). Such an approach reflects a complete cycle of the sedimentary process ranging from the stage of material mobilization and transport to the stage of accumulation of sediments, their transformation into sedimentary rocks, and formation of associated mineral deposits. Sedimentation basins are divided into lakes, intracontinental and marginal seas, and oceans, where phase differentiation of matter proceeds in different manners. It is shown that eupelagic and miopelagic clays, analogues of which are missing from Paleozoic sequences, represent the main indicator of recent sedimentation in the Word Ocean. It is stated that each sedimentation basin is characterized by a specific association of sedimentary mineral deposits.