生物矿化作用机理

生物矿化作用类型可分为诱导和控制两种。生物从空间、构造和化学二方面进行控制、形成大小均匀、形状一致和排列规则的生物晶体。生物矿化位有胞内外泡囊、合胞体和有机基质、细胞层、生物矿物体后三者两两组合的空间。生物矿化作用经历核化、沉淀或生长和相变三个过程。生物利用有机基质，以结构大分子作为间隔底质，以酸性糖朊作为核化模板，来控制生物晶体的核化和牛长。由于过饱和度大、活化能大和抑制剂存在，生物矿物经常先沉淀含水非晶质相，再相变为含水结晶矿物相，最后相变为不含水的结晶矿物。     

生物矿化及其形成机制

生物矿化及其形成机制唐志华（陕西省汉中师范学院化学系）生物体利用一些无机材料以获得机械强度。譬如骨骼和牙齿,其主要成分是一种磷酸钙矿,且由碳酸钙组成的钙化层。一种被称为硅藻的海生水藻利用硅作为其构架。本文拟探讨钙和硅化合物被生物体作为骨骼等材料的原因...     

贝类生物矿化中的生物大分子与分子识别

综述了贝类生物矿化相关的生物大分子性质及其分子识别过程的最新研究进展.生物矿化原理为仿生材料科学和分子构造学提供了崭新的思路.贝类生物矿化过程是生物大分子指导无机晶体的晶核形成、定向及生长的过程,是有机相-无机相、无机相-无机相界面分子识别的过程.     

纳米细菌与生物矿化关系研究现状

纳米细菌（Nanobacteria NB）是芬兰科学家KAJANDER等在培养哺乳动物细胞时发现在无污染的情况下,仍有部分细胞生长繁殖不佳,发生空泡样变性、溶解或凋亡。针对此种现象他们对已知所有微生物进行了检测,结果都为阴性。于是对这些细胞进行透射电镜观察,结果在细胞内发现了一种很小的原核微生物,在上世纪90年代由KAJANDER命名这种生物为Nanobacteria并申请了专利。     

蜡状芽孢杆菌与金矿化的协同演化作用机制

提出了以蜡状芽孢杆菌与金矿化作用及有机质、流体矿化系统协同演化作用机制,认为生物矿化作用是随着其他地质作用的发展而不断发展和演化的过程.阐述生物-蜡状芽孢杆菌、有机质、流体矿化及生物矿化作用演化机制,从而把构造演化与生物矿化作用结合起来研究.主要介绍有机流体的主要来源,着重探讨生物矿化作用子系统,其中包括活生物体的作用,有机质的作用及有机流体的相互作用机制.     

生物矿化一蜡状芽孢杆菌聚金作用的研究

介绍了生物矿化-蜡状芽孢杆菌聚金作用原理.生物活动对矿石的风化、淋滤和沉积都有很大的影响.蜡状芽孢杆菌聚金作用主要与蜡状芽孢杆菌细胞壁的化学成分和结构功能有关.原因是其细胞壁有一层很厚的网状的肽聚糖、多糖、核酸和蛋白质结构,并且在细胞壁表面存在的磷壁酸质和糖醛酸磷壁酸质连接到网状的肽聚糖上.磷壁酸质的磷酸二脂和糖醛酸磷壁酸质的羧基使细胞壁带负电荷,具有离子交换的性质,能与溶液中带正电荷的金属离子进行交换反应.这些过程是蜡状芽孢杆菌细胞壁聚集金的主要作用机制.     

海洋软体动物组织中的铁生物矿化研究概况

海洋软本动物组织中存在铁的生物矿化,并且部分矿化组织含有生物磁铁矿（Ｆｅ３Ｏ４）就无脊椎动物组织中的铁生物矿化及Ｆｅ３Ｏ４形成机理的研究作一综合介绍。     

贝壳的有机质及生物矿化机制分析

以腹足纲贝壳香螺壳为研究对象,用弱酸去钙法进行蛋白提取,采用280纳米(A280)光吸收法测定蛋白含量,并通过聚丙烯酰胺(SDS-PAGE)凝胶电泳法对蛋白按照分子量大小的区别进行分离.实验结果表明香螺壳中蛋白含量和种类较少,其文石层比方解石层蛋白含量高的多,总量分别为0.89%和0.0533%;文石层分离出五种分子量的可溶性蛋白和四种分子量的不可溶性蛋白;而方解石层中分离出三种分子量的可溶性蛋白和三种分子量的不可溶性蛋白,且分子量不相同.正是这少量的蛋白质对贝壳的生物矿化过程和不同晶型的形成起着决定性作用.     

生物矿化硬体显微构造（生矿体结构）的分类和演化

生物矿化硬体显微构造（生矿体结构）的分类和演化戴永定，沈继英（中国科学院地质研究所北京１０００２９）关键词生矿体结构，类型划分，门类分布，发生顺序，演化关系生物矿化硬体的显微构造亦可称为生物矿物体结构，简称生矿体结构。它指的是组成矿物结晶个体或复体的...     

CRYSTALLOGRAPHY AND DIAGENESIS IN FOSSIL CRANIID BRACHIOPODS

Abstract:  One of the fundamental questions in biomineralization is how organisms control crystallographic orientation during biomineral production. The understanding of how diagenetic changes influence the preservation of original crystallographic patterns in fossilized biomineral structures provides a priori fundamental information for such an assessment. Fossil craniid brachiopods Petrocrania scabiosa (Late Ordovician) and Crania craniolaris (Late Cretaceous) are analysed using electron backscattered diffraction (EBSD) to provide crystallographic data at high spatial resolution in the structural context. EBSD analyses show that P. scabiosa maintains most of the original crystallographic signature, including data from individual calcite tablets and laminae, while C. craniolaris only retains fragmentary crystallographic data reflecting the crystallographic continuity of tablets across laminae. Data show that the preservation of the original crystallographic signature is independent of that of shell ultrastructure and geological time. In addition, results allow us to propose a series of steps in the evolution of 'crystallographic loss' due to diagenesis.     

Geomicrobiology of Cave Ferromanganese Deposits: A Field and Laboratory Investigation

Abstract

Unusual ferromanganese deposits are found in several caves in New Mexico. The deposits are enriched in iron and manganese by as much as three orders of magnitude over the bedrock, differing significantly in mineralogy and chemistry from bedrock-derived insoluble residue. The deposits contain metabolically active microbial communities. Enrichment cultures inoculated from the ferromanganese deposits produced manganese oxides that were initially amorphous but developed into crystalline minerals over an 8-month period and beyond; no such progression occurred in killed controls. Phylogenetic analyses of sequences from clone libraries constructed from culture DNA identified two genera known to oxidize manganese, but most clones represent previously unknown manganese oxidizers. We suggest that this community is breaking down the bedrock and accumulating iron and manganese oxides in an oligotrophic environment.     

The Influence of Carbon Source on the Products of Dissimilatory Iron Reduction

We have examined the influence of carbon source on both the rate of iron reduction and the mineralogy of the reduction products with Shewanella putrefaciens strain W3-18-1. When pyruvate was the carbon source, the secondary products were spherules composed of siderite. When uridine was used as the carbon source, the products were hexagonal plate-like structures identified as iron carbonate hydroxide hydrate, also known as carbonate green rust, a precursor to fougerite. When lactate was used as the carbon source, products were a mixture of iron carbonate hydroxide and magnetite. In terms of reaction stoichiometry, there were differences in the amount of acetate produced depending on the starting organic carbon source. Incubation with pyruvate produced a relatively large amount of acetate compared to incubation with uridine and lactate. There were also differences in the final pH of the cultures. While the pH for incubations with lactate started at 8.6 and ended between 8.0–8.3, the pH of cultures incubated with uridine was found to be almost a full unit lower at the conclusion of the experiment (～7.4). Solubility diagrams based on the chemistry found in our experiments predict that the production of Fe²⁺ _(aq) should always lead to the formation of magnetite. However, strain W3-18-1 produced different minerals depending on the carbon source utilized as the electron acceptor.     

Oxygen isotope analysis of bacterial and fungal manganese oxidation

The ability of micro‐organisms to oxidize manganese (Mn) from Mn(II) to Mn(III/IV) oxides transcends boundaries of biological clade or domain. Many bacteria and fungi oxidize Mn(II) to Mn(III/IV) oxides directly through enzymatic activity or indirectly through the production of reactive oxygen species. Here, we determine the oxygen isotope fractionation factors associated with Mn(II) oxidation via various biotic (bacteria and fungi) and abiotic Mn(II) reaction pathways. As oxygen in Mn(III/IV) oxides may be derived from precursor water and molecular oxygen, we use a twofold approach to determine the isotope fractionation with respect to each oxygen source. Using both ¹⁸O‐labeled water and closed‐system Rayleigh distillation approaches, we constrain the kinetic isotope fractionation factors associated with O atom incorporation during Mn(II) oxidation to ?17.3‰ to ?25.9‰ for O₂ and ?1.9‰ to +1.8‰ for water. Results demonstrate that stable oxygen isotopes of Mn(III/IV) oxides have potential to distinguish between two main classes of biotic Mn(II) oxidation: direct enzymatic oxidation in which O₂ is the oxidant and indirect enzymatic oxidation in which superoxide is the oxidant. The fraction of Mn(III/IV) oxide‐associated oxygen derived from water varies significantly (38%–62%) among these bio‐oxides with only weak relationship to Mn oxidation state, suggesting Mn(III) disproportionation may account for differences in the fraction of mineral‐bound oxygen from water and O₂. Additionally, direct incorporation of molecular O₂ suggests that Mn(III/IV) oxides contain a yet untapped proxy of of environmental O₂, a parameter reflecting the integrated influence of global respiration, photorespiration, and several other biogeochemical reactions of global significance.     

胞间连丝的次生形成和次生变化

本文介绍了胞间连丝次生形成和次生变化的研究进展,用统计特定细胞壁区段上胞间连丝数量与密度的变化,电镜观察嫁接组合中接穗与砧水间细胞壁上胞间连丝的形成等方法,证明了在植物生长发育过程中,存在着胞间连丝的次生形成。在某些特定部位,某一发育阶段,已形成的胞间连丝常会发生可逆的次生变化,这种变化和植物发育过程中的共质体隔离以及物质运输的调节有关。     

石鳖主侧齿齿尖铁矿化途径与铁蛋白定位

生物矿化在自然界广泛存在。矿化过程通过精确控制形成精致、有序的分级结构,如骨骼、牙齿、贝壳、齿舌等,迄今已发现约60多种生物矿化物,其中钙化物的种类最多,铁化物有5—6种1,2。磁铁矿(Fe3O4)在众多的生物体内均有发现3。纳米磁铁矿在生物医学领域有广泛的应用前景,如制备磁性微球、磁性微囊、磁性脂质体、磁性微乳等4,5。生物矿化吸引着众多科学家的关注,人们期望通过矿化结构的研究,了解矿化机理,并利用仿生学原理合成功能性材料。       

Eridites undulatum壳体微细构造

利用偏光显微镜及扫描电子显微镜观察了假直角石类Ｅｒｉｄｉｔｅｓｕｎｄｕｌａｔｕｍ的体管沉积及气室沉积微细构造特征,体管沉积内部有机质层及矿物晶体层形态及厚度较稳定。气室沉积中有机质层及矿物晶体层形态及厚度变化大,晶体层内部具有柱状晶体。基于内部微细构造特征,推测体管沉积由软体上皮细胞直接分泌而成,气室沉积由体液渗透连接环在气室内表面上形成矿化基质后通过有机质层及矿物晶体层不断加积而成。另外,通过与石炭纪其它假直角石类内部沉积微细构造特征的比较,认为假直角石类内部沉积的微细构造特征不具有分类学意义。     

Structure and composition of the boundary zone between aragonitic crossed lamellar and calcitic prism layers in the shell of Concholepas concholepas (Mollusca,Gastropoda)

Mollusc shells are composed of two or three layers. The main layers are well‐studied, but the structural and chemical changes at their boundaries are usually neglected. A microstructural, mineralogical, and biochemical study of the boundary between the inner crossed lamellar and outer prismatic layers of the shell of Concholepas concholepas showed that this boundary is not an abrupt transition. Localized structural and chemical analyses showed that patches of the inner aragonitic crossed lamellar layer persist within the outer calcitic prismatic layer. Moreover, a thin aragonitic layer with a fibrous structure is visible between the two main layers. A three‐step biomineralization process is proposed that involves changes in the chemical and biochemical composition of the last growth increments of the calcite prisms. The changes in the secretory process in the mantle cells responsible for the shell layer succession are irregular and discontinuous.