情感与教学

情感是每个人的需求,健康的情感对中学生优秀道德品质的形成起良好的促进作用。语文新课标要求,要加大对学生情感的教育。笔者从亲身的教学实践中谈到语文教学对学生情感教育起到的重要作用和深刻影响。     

在英语课堂教学中应用角色扮演法应注意的若干问题

通过阐述在英语课堂教学中应用角色扮演法在培养学生听说能力和合作精神方面的积极作用说明研究意义；而后分析论证了在其应用过程中存在的若干问题；最后，结合交际教学法的理论和原则，以及中国外语教学的实际情况，从任务的设计、语言的操练、教师的反馈、方法的指导和教师的风格等五个方面，提出了成功运用角色扮演法应注意的问题及其解决办法。     

西藏措勤地区典中组火山岩地球化学特征及构造背景

措勤盆地位于西藏冈底斯构造-岩浆岩带的西段北侧,该区古新世火山活动十分强烈,形成了一套厚度大于1 000 m的中酸性火山岩地层,火山岩K-Ar和Rb-Sr同位素年龄为63.9～61.0 Ma,区域上可与古近纪林子宗群下部层位相对比,归为古新统典中组.火山岩岩石化学、地球化学特征分析表明,该火山岩系属高钾钙碱性-钙碱性系列,轻稀土富集,负Eu异常明显.与原始地幔相比,微量元素Rb,Ba,K,Th,U富集;Ti,P,Sr,Ta(Nb)亏损.锶、氧同位素组成显示岩浆来源与陆壳物质关系密切,推测是来自于俯冲带的幔源基性岩浆与陆壳重熔酸性岩浆以不同比例混合所形成.综合研究认为,这套火山岩形成于陆缘弧构造环境,与喜马拉雅特提斯洋壳向北俯冲消减作用有关.     

产学研一体化与就业导向的职业教育

随着市场经济体制的不断完善，生源和就业源日益成为高职院校生存和发展的核心要素。谁掌握了生源和就业源，谁就掌握了高职院校发展的命脉。本文拟从产学研一体化的视角，探索就业导向的职业教育发展之路。     

矿井井筒提升容器活塞风效应分析及计算

矿井提升容器在井筒中占据了部分井筒空间,升降运动时,产生活塞作用效应,提升容器周围的流场和压力场均发生变化,产生动态局部阻力.根据流体力学理论,分析了罐笼在井筒内升降过程中空气的速度变化情况,采用相对坐标法推导了在井筒风速影响下罐笼顺风、逆风和相会时的活塞风速数学计算模型.研究结果表明,井筒提升容器活塞效应的影响因素主要有提升容器的外形尺寸、井筒内的机械通风风速和阻塞比等.研究结论为研究由于矿井井筒提升容器活塞作用效应产生动态局部阻力提供了理论依据.图2,参11.     

黄河中游风水两相作用对侵蚀产沙地域分布的影响

着眼于风力、水力两相作用，对黄河中游风沙—黄土过渡带高强度侵蚀的形成机理进行了研究,并提出用某一地点年降水量Pm与年均沙尘暴日数Dss之比Pm/Dss来定量表达风力、水力两相作用，称为风水两相作用指标.研究表明，风水两相作用通过对泥沙供应条件的调节，来控制悬移质泥沙的粗细颗粒搭配关系，并进而实现最优组合，从而使水沙两相流的输沙能力得到强化,地表物质抗蚀性和植被对地表物质保护作用的地域分布均与风水两相作用有密切的关系，因而形成了不同的地域类型;进而划分了风力作用主导类型、风水两相作用主导类型和水力作用主导类型等3种类型;认为产沙模数与年降水量、年沙尘暴日数和风水两相作用指标之间存在着非线性关系,在这3个关系中，均表现出一个产沙模数的峰值区，与之相对应的年降水量为350—450mm，年均沙尘暴日数为5—15d，风水两相指标值为30—80mm·d-1.这些成果丰富了著名的Langbein-Schumm关系的内涵，为其形成机理提供了一个新的解释.     

[Zn(PBIMH)2(H2O)]n的合成及晶体结构

水热条件下,合成了配位聚合物[Zn（L）2（H2O）]（nLH=2-吡啶-2-苯并咪唑）.X-射线单晶衍射分析结果表明：配合物属单斜晶系,P2（1）/c空间群,晶胞参数分别为：a=12.5657（2）,b=12.9258（2）,c=13.2403（3）A°,β=102.738（1）A°.锌离子与两个LH的4个氮原子,1个端基水配位形成变形的四角锥,（I）通过O---H---N氢键形成一维超分子结构.     

三丁基锡对水生生物毒理学影响的研究进展

综述了三丁基锡(TBT)对水生生物的毒理学效应,认为主要表现在干扰海产腹足类的内分泌而诱导性畸变现象的产生,抑制微藻的光合作用和呼吸作用,破坏水生动物超氧化物歧化酶、酸性磷酸酶、碱性磷酸酶等蛋白质的活性,对软体动物的DNA造成不同程度的损伤.同时,探讨了TBT的降解、伤害作用机制及研究前景等.     

Biomineralization of phototrophic microbes in silica-enriched hot springs in South China

Microbial mats in two hot springs in South China were sampled for the research of mineralization of microbes and its mechanism by the methods of geology and modern biology. The results show that hot spring microbes have the key capability for enrichment of Si, Al, Fe, Ca and other elements, and the microbes are also crucial for the formation of SiO2, CaCO3, clay and so on. The extracellular polymeric substances (EPS) play important roles in the process of mineralization of hot spring microbes, which mainly takes place in the layer of EPS outside cell wall or sheath of cyanobacteria. The sheath outside cell wall, which keeps the normal metabolism of cyanobacteria during the process of mineralization on its surface, is also considerable for the biomineralization of cyanobacteria. According to structure and mineralization characteristics of two microbial mats, the process of mineralization can be divided into three stages, namely, early surface mineralization, middle degradation mineralization, and late des- quamation of mineral. The above conclusions are significant for comprehension of the process of mineralization, the process of deposition and the preservation of microfossil in modern and ancient extreme environments.     

When and how did plate tectonics begin？ Theoretical and empirical considerations

Plate tectonics is the horizontal motion of Earth’s thermal boundary layer (lithosphere) over the convecting mantle (asthenosphere) and is mostly driven by lithosphere sinking in subduction zones. Plate tectonics is an outstanding example of a self organizing, far from equilibrium complex system (SOFFECS), driven by the negative buoyancy of the thermal boundary layer and controlled by dissipation in the bending lithosphere and viscous mantle. Plate tectonics is an unusual way for a silicate planet to lose heat, as it exists on only one of the large five silicate bodies in the inner solar system. It is not known when this mode of tectonic activity and heat loss began on Earth. All silicate planets probably experienced a short-lived magma ocean stage. After this solidified, stagnant lid behavior is the common mode of planetary heat loss, with interior heat being lost by delamination and “hot spot” volcanism and shallow intrusions. Decompression melting in the hotter early Earth generated a different lithosphere than today, with thicker oceanic crust and thinner mantle lithosphere; such lithosphere would take much longer than at present to become negatively buoyant, suggesting that plate tectonics on the early Earth occurred sporadically if at all. Plate tectonics became sustainable (the modern style) when Earth cooled sufficiently that decompression melting beneath spreading ridges made thin oceanic crust, allowing oceanic lithosphere to become negatively buoyant after a few tens of millions of years. Ultimately the question of when plate tectonics began must be answered by informa- tion retrieved from the geologic record. Criteria for the operation of plate tectonics includes ophiolites, blueschist and ultra-high pressure metamorphic belts, eclogites, passive margins, transform faults, paleomagnetic demonstration of different motions of different cratons, and the presence of diagnostic geochemical and isotopic indicators in igneous rocks. This record must be interpreted individually; I interpret the record to indicate a progression of tectonic styles from active Archean tectonics and magmatism to something similar to plate tectonics at ~1.9 Ga to sustained, modern style plate tectonics with deep subduction——and powerful slab pull——beginning in Neoproterozoic time.