A Review of Magnesium Isotope System in Rivers

In recent years, a series of important progresses have been made in the aspect of magnesium isotopes behavior in weathering processes. These progresses are not only favorable to understand the change of the magnesium isotopic compositions in rivers, but also establish the foundation to further reveal the magnesium isotope geochemical cycle. The magnesium in rivers is both magnesium sink for weathering and magnesium source for the ocean. The Mg isotopic compositions in rivers are dominated by the magnesium sources and Mg isotope fractionations processes. The sources of magnesium in rivers originate mainly from draining rocks, as well as less contribution from the eolian deposition, groundwater, plant debris, and precipitation. The Mg isotope fractionations in rivers are mainly related to precipitation and dissolution of carbonate minerals, silicate mineral hydrolysis, adsorption on mineral or colloidal matter surface, and plant uptake. Generally, the contribution of carbonate minerals dissolution or precipitation is equal to add or reduce magnesium from carbonate endmember, which has a remarkably negative δ²⁶Mg value. Based on the fact that most clay minerals are rich in ²⁶Mg during nature silicate mineral hydrolysis, then it is possible to infer that residual weathering products enrich in ²⁶Mg. However, there is no significant Mg isotope fractionation causing by the adsorption on mineral or colloidal matter surface during river water migration. For the plant uptake, the root prefers to have ²⁶Mg, leading the plant itself rich in heavier Mg isotopic composition. In addition, formation of secondary minerals in rivers could also reflect the changes of chemical parameters in rivers (such as major elements, CO₂ solubility, pH, etc.). Hence, Mg isotopic composition in rivers and associated isotope fractionations are not only the basis for the application of magnesium isotope to trace surface material cycle, but also have important significance for the further understanding the geochemical cycle of magnesium isotopes.     

电阻率法评价膨胀土改良的物化过程

掺石灰、粉煤灰是工程中通常采用的改良膨胀土的方法。土电阻率是土的基本物理指标之一,其变化可反映土的其他物理性质指标的变化。通过掺灰改良膨胀土不同养护龄期下的电阻率测试以及膨胀量、膨胀力及无侧限抗压强度等试验研究,探讨了掺灰改良膨胀土养护过程中的物理化学反应过程。根据养护过程中的电阻率随龄期的变化规律,可将改良膨胀土的物理化学反应过程划分为瞬时反应阶段、主体反应阶段、残余反应阶段和稳定阶段4个不同阶段。针对改良膨胀土质量控制和评价体系中存在的不足,提出了基于电阻率指标的改性膨胀土的质量评价方法,通过试验证实了该方法的有效性和实用性。     

纵横向受荷基桩变形内力的矩阵传递解

针对地基的土体屈服性状,将桩侧土体分为弹性变形区域与塑性变形区域两种情况。假定地基反力系数为3参数的一般形式,同时考虑桩身 效应并计入桩身自重、桩侧摩阻力的影响,根据地基反力法分别建立桩身弹性段和塑性段挠曲线微分方程。在解微分方程的过程中,采用矩阵传递法结合Laplace正逆变换的方法解得桩顶作用轴向力、水平力、弯矩时桩身内力和变形的矩阵传递解,并用Fortran语言编制了相应计算程序。最后将试验数据对上述方法进行验证,结果表明计算值与模型试验的实测值吻合很好,采用文中3参数地基反力法反算所得的地基参数离散性很小,研究结果具有较高的应用价值。     

胶北地区早前寒武纪孔兹岩系的变质演化

在胶北地区出露大面积早前寒武纪孔兹岩,主体岩石为富铝片岩-片麻岩,夹有大理岩等变沉积岩。岩相学、成因矿物学和变质反应性质的研究以及温压条件估算结果表明,研究区孔兹岩系经历了四个阶段的变质演化。早期进变质阶段(M1)的矿物组合为石榴石及其内部的黑云母+斜长石+石英;峰期中-高压麻粒岩相变质阶段(M2)的矿物组合以含蓝晶石的麻粒岩相矿物组合为标志,该阶段最高的温压条件可达760℃、10.0kb;峰后近等温减压麻粒岩相退变质阶段(M3)发生一系列典型减压反应,以新生堇青石的出现为标志,形成了含堇青石的中-低压麻粒岩相矿物组合,稳定的温压条件为750～800℃、4.0～5.4kb;晚期降温退变质阶段(M4)以石榴石转变形成细小黑云母等退变矿物为特征,该阶段的温压条件为550～650℃、4.0kb。孔兹岩系变质演化P-T轨迹具有顺时针型式,先后经历了近等温减压(ITD)和近等压冷却(IBC)的P-T演化,标志着胶北地区早前寒武纪孔兹岩系曾经历了地壳加厚-构造隆升的动力学过程。     

斜方辉石筛状反应边的成因机制及其对岩石圈地幔性质转变的意义

本文利用电子背散射衍射(EBSD)技术对河北张家口大麻坪汉诺坝玄武岩橄榄岩捕虏体中斜方辉石与玄武岩反应结构的显微构造进行了详细研究。研究结果表明: ① 其反应边具有复杂的多层筛状结构特征,包括玄武岩层、富橄榄石层以及橄榄石和单斜辉石交生层;② 由外至内,橄榄石的Mg值逐渐升高,而单斜辉石的Mg值变化不大;③ 反应边结构中的单斜辉石与斜方辉石残斑之间存在很好的结晶学拓扑关系,即(100)_opx//(100)_cpx、(010)_opx//(010)_cpx、(001)_opx//(001)_cpx;④ 橄榄石的结晶学取向无序且与斜方辉石和单斜辉石均无关。这个反应过程可以用贫硅熔体先与斜方辉石反应形成单斜辉石,并导致熔体富硅,从而橄榄石从反应熔体中结晶出来合理地解释。相对富硅熔体与橄榄岩的反应,贫硅熔体与橄榄岩的反应过程由于筛状反应边的存在可能更容易进行,筛状结构反应边可以为熔体在橄榄岩中沿颗粒边界运移提供通道,并使橄榄岩主要组成矿物发生细粒化和岩石结构变得松散,可以有效保证熔体上升过程中对橄榄岩的持续侵蚀和破坏,从而可能导致岩石圈地幔性质的迅速转变。     

川滇西部地区钾质煌斑岩特征及其成因

川滇西部地区钾质煌斑岩带产物扬子板块西缘与三江褶皱带之间的过渡地带，侵位于老第三系地层。岩石化学特点具有中等含量钾、钛和钠、铝弱饱和，属岛弧环境的钙碱性煌斑岩与板内环境的钾镁煌斑岩（超钾）之间的过渡类型。微量元素Sr相对于Rb,Ba,K等元素具有明显的负异常，是地幔交代作用的产物。区域上与其伴生的壳源型花岗岩侵位在前，分布于西侧；碱性岩层中；钾质煌斑岩侵位在后，分布于东侧，属反序侵位序列，为喜山期陆壳碰撞、褶皱造山运动所触发的被动地幔作用产物。     

Formation of low-pressure reaction textures during near-isothermal exhumation of hot orogenic crust (Bohemian Massif,Austria)

Two types of aluminous paragneiss from the Loosdorf complex (Bohemian Massif, NE Austria) contain coarse-grained granulite assemblages and retrograde reaction textures that are investigated to constrain the post-peak history of the Gföhl unit in the southern Bohemian Massif. Both types have a peak assemblage garnet–biotite–sillimanite–plagioclase–K-feldspar–quartz–granitic melt ± kyanite ± ilmenite ± rutile, recording peak metamorphic conditions of $$0.9–1.1 GPa and $$780–820°C estimated by isochemical phase equilibrium modelling. The first sample type (Ysper paragneiss) developed (i) cordierite coronae around garnet and (ii) cordierite–spinel and cordierite–quartz reaction textures at former garnet–sillimanite interfaces. Calculated chemical potential relationships indicate that the textures formed in the course of a post-peak near-isothermal decompression path reaching $$0.4 GPa. Texture formation follows a two-step process. Initially, cordierite coronae grow between garnet and sillimanite. As these coronae thicken, they facilitate the development of local compositional domains, leading to the formation of cordierite–spinel and cordierite–quartz symplectites. The second sample type (Pielach paragneiss) exhibits only discontinuous cordierite coronae around garnet porphyroblasts but lacks symplectites. The formation of cordierite there also indicates near-isothermal decompression to 0.4–0.5 GPa and 750–800°C. This relatively hot decompression path is explained by the contemporaneous exhumation of a large HP–UHT granulite body now underlying the Loosdorf complex. The timing of regional metamorphism in the granulites and the southern Bohemian Massif in general is well constrained and has its peak at $$340 Ma. Monazite from Loosdorf paragneiss samples yield a slightly younger age of $$335 Ma. Although the ages overlap within error, they are interpreted to reflect near-isothermal decompression and exhumation resulting in the formation of the observed reaction textures.     

简单体系水溶液包裹体pH和Eh的计算

流体包裹体pH和Eh参数的计算一直处于探索阶段。已经发表的计算公式,由于缺少高压(＞1bar)环境下化学组分反应平衡常数,常常利用常压(1大气压)下化学组分反应平衡常数代替而推导出的,对于大多数自然界捕获的包裹体,不可避免地产生较大计算误差。根据水溶液包裹体中离子反应热力学特征,结合前人推导的计算公式,我们分别建立简单体系水溶液包裹体pH和Eh计算公式。由于利用较高压(＞1bar)化学反应平衡常数,基本上解决不同条件下、特别在较高温度、压力下捕获的水溶液包裹体pH和Eh的计算难题。4种简单体系水溶液包裹体pH计算公式:① H2O包裹体:pH=pKw② CO2-H2O包裹体: 3－(mCO2Ka,1+KW)· －2mCO2Ka,1Ka,2=0③ NaCl-H2O包裹体: 2= ④ CO2-H2O-NaCl包裹体: 3+ 2－(mCO2·Ka,1+Kw)· －2mCO2·Ka,1·Ka,2－ =0计算数值精度分析表明:CO2-H2O和NaCl-H2O包裹体的pH值按照公式计算,相同或接近于实际测定的天然酸雨、海水pH数值范围。CO2-H2O-NaCl包裹体与Crerar(1978)公式计算误差不超过10%。4种简单体系水溶液包裹体Eh的计算,引用Ryzhenko and Bryzgalin (1984)年推导的Eh公式。文中列举了3个实例,详细叙述不同类型包裹体捕获温度、压力下pH和Eh计算过程。自然界中水溶液包裹体成分十分复杂,本文涉及的只是自然界几种简单体系水溶液包裹体,给出的pH和Eh公式只对特定组分组合反应平衡条件有效,它不适合另外一种组分组合平衡条件下的关系,因此使用时务必注意平衡的组分组合条件。     

地电化学测量法寻找隐伏金矿的机理及其应用效果

地电化学测量法是在前苏联的地电提取技术基础上进一步发展起来的,以电场形式激发、离子形式记录电化学反应结果的轻便、快速的找矿方法,在探测隐伏矿体方面具有明显优势.通过对该方法的机理和应用效果研究,证明了利用地电化学测量法来寻找隐伏金矿的可行性.