层状地基参数的频域识别

在分析水平层状地基运动特征的基础上, 通过研究地层系统的特征值和特征向量与地层参数之间的关系, 修正测量得到的数据与理论计算结果之间的偏差, 建立了层状地基参数的频域识别方法。并利用大型振动台上的地基模型试验数据, 实施了层状地基的参数识别过程。结果表明, 该方法产生良好的地基参数估计。     

Hamilton体系及弹性波在层状介质中的传播问题

利用结构力学与最优控制的模拟理论,研究弹性波在层状介质中传播的数值计算方法. 将弹性波传播问题导向哈密顿(Hamilton)体系,在哈密顿体系中,推导出一种新的半解析单元,称之为动力-部分杂交元,由此导出一套哈密顿体系下的半解析数值计算方法. 本文给出了该方法在层状正交各向异性材料介质的弹性波传播问题的数值算例,分析了一定频率的弹性波在层状介质中传播时的位移、应力的模式. 计算结果展现了Hamilton体系和辛几何在弹性波传播问题研究的应用前景.     

Fundamental period and mode shape of layered soil profiles

The estimation of the fundamental period of soil profiles has been the subject of numerous studies. An extensive evaluation of several procedures by Dobry et al. [1] concluded that both the Simplified Version of the Rayleigh Procedure [1] and the Successive Use of Two-Layer Solution by Madera [2] give errors of less than 10% for all of the 76 representative soil profiles considered in the evaluation. The simplified Rayleigh procedure is iterative and requires an initial estimate of the mode shape. The Madera procedure is based on the solution of a two-layer system, usually obtained from charts. In this paper the solution charts are replaced by approximate relations for implementation on a spreadsheet. Since the Madera procedure calculates only the fundamental period, mode shapes need to be calculated by other means. The Madera procedure is extended to calculate mode shapes and modal participation factors of layered soil profiles. Unlike the simplified Rayleigh procedure [1], the proposed solution incorporates the different densities of the layers and gives direct results without iterations. The proposed solution can be considered a simpler alternative to the Rayleigh method for shear beams or soil columns.     

柱坐标系下任意埋藏源层状弹性半空间问题的奇异解

通过方位角的Fourier变换及关于径向的Hankel变换，将柱坐标系下一般形式的弹性力学基本方程和本构方程转化为波数域内非齐次的二阶常微分方程组，利用初参数法，建立了介质层传递矩阵．利用层间完全接触条件，给出了任意埋藏源层状弹性半空间频域奇异解，时域奇异解可通过关于频率的Fourier积分得到，该方法可应用到固体、流体层的情况.     

铂族元素地球化学示踪研究──四川新街层状侵入岩体铂族元素地球化学特征

以开展铂族元素地球化学示踪研究为目的,采用高灵敏度、高准确度的中子活化分析和扫描核探针方法,系统测定了四川新街层状侵人岩体的铂族元素分布结果表明,在岩浆演化过程中,硫化物的分凝作用（segregation）是铂族元素富集的主要因素之一、Pt元素主要以砷化物形式独立存在在岩浆分离结晶作用下,铂族元素Os,Ru,Ir和Pt,Pd间出现分组现象,这很可能与他们在岩浆中的难熔程度有关用铂族元素C1球粒陨石标准化图解,对新街岩体的物质来源和岩浆演化过程作了讨论．发现在硫化物析出阶段,随着Pt的富集,出现Ir的正异常,而在岩浆晚期出现Ir的负异常．研究表明,铂族元素可作为岩体物质来源、岩浆演化、硫化物馆和程度的地球化学指示剂．     

Experimental effects of pressure and fluorine on apatite saturation in mafic magmas, with reference to layered intrusions and massif anorthosites

Apatite is a cumulate phase in the upper parts of some mafic layered intrusions and anorthositic complexes. We investigated the effect of pressure and fluorine on apatite saturation in mafic magmas to better understand under which conditions this mineral crystallizes. Apatite saturation gives information about the formation of silicate rocks, and is of interest in explaining the formation of apatite–oxide-rich rocks (e.g. nelsonites comprising approximately, one-third apatite and two-third Fe–Ti oxide). Two models of formation are proposed for this rock type: crystal fractionation followed by accumulation of apatite and Fe–Ti oxides and liquid immiscibility. New experiments carried out with mafic compositions at 500 MPa confirm that the most important variables on phosphate saturation are SiO₂ and CaO. Fluorine addition leads to apatite saturation at lower SiO₂ and higher CaO concentrations. Comparison of our results with those of previous experimental studies on liquid–liquid immiscibility at upper-to-mid-crustal conditions allows us to investigate the relative importance of apatite saturation versus liquid–liquid immiscibility in the petrogenesis of nelsonites and similar rocks. The liquid line of descent of three natural examples studied (the Sept-Îles intrusive suite, the anorthositic Complex of the Lac-St-Jean and the Skaergaard layered intrusion) do not cross the liquid–liquid immiscibility field before they reach apatite saturation. Thus, the apatite–oxide-rich rock associated with these three intrusive suites are best explained by crystal fractionation followed by accumulation of apatite and Fe–Ti oxides.     

Comparison between moving and stationary transmitter systems in induction logging

In a general treatment of the theory of induction logging, an exact integral representation has been obtained for the mutual impedance between a vertical dipole transmitter and a coaxial dipole receiver in a three layered earth. Based on this representation, a computer model has been devised using the traditional Slingram system of induction logging and the comparatively new Turam system, ignoring borehole effects. The model results indicate that due to its much larger response, the Turam system is in general preferable to the Slingram in mineral and groundwater investigations where formation conductivity much less than 1 S/m is generally encountered. However, if the surrounding media are conductive (more than 0.1 S/m), the Turam system suffers from large amplitude attenuation and phase rotation of the primary field caused by the conductive surrounding, and is less useful than the Slingram system which does not so suffer, unless the target bed is shallow. Because it is a more complex function of system parameters than the corresponding Slingram log, a Turam log can be conveniently interpreted only by the modern inverse method using a fast algorithm for the forward solution and a high speed digital computer.     

Thermobarometry and granite genesis: the Hercynian low-P, high-T Velay anatectic dome (French Massif Central)

The Velay dome (French Massif Central) offers a quasi-continuous section across an anatectic domain comprising low- to high-grade schists, gneisses and granites. Two main tectonometamorphic events, and their related generation of granitic material, were recognized in addition to a major Barrrovian tangential event (D2) attributed to intracontinental collision tectonics: (i) a medium- to low- P , high- T event (D3) which gave rise to migmatites and syntectonic monzonitic granites and granodiorites, and (ii) a widespread melting event (D4) which led to the generation of migmatities, the Velay granite and post-anatectic granites.
Thermobarometry on samples collected from both the metamorphic envelope and the granitic core distinguishes two distinct geotherms: (i) a first, associated with the D3 event, characterized by P > 5 kbar, T ≤ 750° C and water-present melting (biotite remains stable) which led to large-scale migmatization but minor amount of granites; (ii) a second, associated with the D4 event and characterized by vapour-absent melting ( P = 4–5 kbar, T = 760–850° C) which gave rise to the Velay granites and late-migmatitic granites. The temperature increase during the D4 event is attributed to the intrusion of hot mafic magmas within the crust.
The time-integrated features of the different granitic rocks in the Velay dome can be directly related to a _H2O in the source region and illustrate the progressive dehydration of a middle to lower crustal segment over 60 Ma.     

What controls partial melting in migmatites?

Abstract The layers of six stromatic migmatites from Northern, Western, and Central Europe display small but systematic chemical and mineralogical differences. At least five of these migmatites do not show any signs of largescale metamorphic differentiation, metasomatism, or segregation of melts. It is concluded, therefore, that the compositional layering observed in most of the investigated migmatites is due to compositional differences inherited from the parent rocks. Almost isochemical partial melting seems to be the most probable process transforming layered paragneisses, metavolcanics, or schists into migmatites.
The formation of neosomes is believed to be caused by higher amounts of partial melts formed due to higher amounts of water moving into these layers. The neosomes have less biotite and more K-feldspar, if K-feldspar is present at all, than the adjacent mesosomes. These differences are small but systematic and seem to control the access of different amounts of water to the various rock portions. Petrographical observations, chemical data, and theoretical considerations indicate a close relationship between rock composition, rock deformation, transport of water, partial melting, and formation of layered migmatites.     

Petrogenesis of ultramafic and mafic xenoliths from Mesozoic basanites in southern Sweden: constraints from mineral chemistry

Jurassic basanite necks occurring at the junction of two major fault zones in Scania contain ultramafic (peridotites, pyroxenites) and mafic xenoliths, which together indicate a diversity of upper mantle and lower crustal assemblages beneath this region. The peridotites can be subdivided into lherzolites, dunites and harzburgites. Most lherzolites are porphyroclastic, containing orthopyroxene and olivine porphyroclasts. They consist of Mg-rich silicates (Mg# = Mg/(Mg + Fe_tot) × 100; 88–94) and vermicular spinel. Calculated equilibration temperatures are lower in porphyroclastic lherzolites (975–1,007°C) than in equigranular lherzolite (1,079°C), indicating an origin from different parts of the upper mantle. According to the spinel composition the lherzolites represent residues of 8–13% fractional melting. They are similar in texture, mineralogy and major element composition to mantle xenoliths from Cenozoic Central European volcanic fields. Dunitic and harzburgitic peridotites are equigranular and only slightly deformed. Silicate minerals have lower to similar Mg# (83–92) as lherzolites and lack primary spinel. Resorbed patches in dunite and harzburgite xenoliths might be the remnants of metasomatic processes that changed the upper mantle composition. Pyroxenites are coarse, undeformed and have silicate minerals with partly lower Mg# than peridotites (70–91). Pyroxenitic oxides are pleonaste spinels. According to two-pyroxene thermometry pyroxenites show a large range of equilibration temperatures (919–1,280°C). In contrast, mafic xenoliths, which are mostly layered gabbronorites with pyroxene- and plagioclase-rich layers, have a narrow range of equilibration temperatures (828–890°C). These temperature ranges, together with geochemical evidence, indicate that pyroxenites and gabbroic xenoliths represent mafic intrusions within the Fennoscandian crust.