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.     

Study on crustal, lithospheric and asthenospheric thickness beneath the Qinghai-Tibet Plateau and its adjacent areas

Based on the results of pure dispersions of Rayleigh wave tomography in the Qinghai-Tlbet Plateau and its adjacent areas, tsklng S wave velocities from previous linear inversion as the initial model, using the simulated annealing algorithm, a nonlinear simultaneous inversion has been carried out for S wave velocity and thickness of different layers, including the crust, the lithosphere and the asthenosphere. The results indicate： The crustal thickness shows strong correlation with geology structures sketched by the sutures and major faults. The crust is very thick in the Qinghal-Tibet Plateau, varying from 60 km to 80 kin. The Ilthospherlc thickness in the Qinghai-Tibet Plateau Is thinner （130-160 kin） than Its adjacent areas. And two blocks can be recognized, divided by an NNE strike boundary running between 90°E-92°E inside the plateau. Its asthenosphere is relatively thick, varies from 150 km to 230 kin, and the thickest area is located in the western Qiangtsng. India has a thinner crust （32-38 kin）, a thicker lithosphere of 190 km and a rather thin asthenosphere of only 60 kin. Sichuan and Tarlm basins have the crust thickness less than 50 kin. Their Iithospheres are thicker than the Qinghai-Tibet Plateau, and their asthenospheres are thinner. A discussion has been made on the character and formation mechanism of the typical crust-mantle transition zone in the western Qiangtsng block.     

利用接收函数方法研究大盈江断裂两侧S波速度结构

 利用研究区(24.2°~25.2°N,97.5°~98.5°E)内大盈江断裂两侧5个流动数字地震台站记录到的宽频带远震P波波形数据进行接收函数反演,得到台站下方0~100km深度范围内地壳、上地幔S波速度细结构.结果表明:研究区内,以大盈江断裂为界,其西北侧Moho面深度约为38km;东南侧Moho面深度为40~42km.断裂两侧地壳、上地幔S波速度结构存在显著差异,东南侧台站下方地壳和上地幔均存在大范围低速区;西北侧台站下方地壳内存在低速层,而上地幔中无明显低速层.研究区内的S波速度结构存在明显的横向非均匀性.     

深松整地播种机的探究

本文主要探讨深松整地播种机的结构、工作原理及主要的技术参数。深松整地播种机属于多用属复式作业机械,是深松、旋耕、施肥播种机构的共用机件,达到了机具用作各种不同形式作业、安装不同机构的要求,且机具配套动力小,碎土效果好,适应性强,能够彻底打破犁底层,在不翻动土壤的前提下有效改善土壤的透水、透气性,为植物根系发育提供更大的伸展空间,对粮食增产增效有明显效果,是理想的深松整地机具。     

高低组合跳深练习法对中学生跳高、跳远、三级跳远成绩影响的实验研究

本文通过文献资料法，实验法和数理统计的方法对高低组合跳深练习法对中学生运动员的跳高、跳远、三级跳远的成绩影响进行统计学对比分析，以验证高低组合训练法训练效果，并简要分析其优点，以期为广大教练提供才能考。     

浅谈地下原地浸出深孔微差挤压爆破与VCR法相结合技术

我国有部分矿山（如：铀、金等矿山）采用地下原地浸出金属的采矿方法,这种方法即减少了出矿量同时也对采场形成充填作用,使工作人员有安全的工作空间。但是,这种采矿方法采场爆破设计及施工技术对后续生产有直接影响作用,并关系到年生产量任务是否能完成。根据多年来矿山采用地下原地浸出金属的普通深孔爆破技术,大部分矿山爆破效果达不到预计效果。所以,根据国内矿山多年来的总结经验选择地下原地浸出深孔微差挤压爆破与VCR法相结合技术会取得比较好的爆破效果。     

Al_xGa_(1-x)As中3d过渡金属杂质深能级

由于Al_xGa_(1-x)As半导体合金在光电子学中得到重要的应用,故它的各种物理性质引起人们广泛的兴趣,其中包括各种深浅杂质的电子结构。但是,相对而言,人们对Al_xGa_(1-x)As中3d过渡金属杂质电子态了解还很不够,对不少3d杂质实验研究还很缺乏,尤其是由于3d杂质复杂的多电子特性,迄今还没有见到关于Al_xGa_(1-x)As中3d杂质深能级的详细理论研究。另外,了解这样一种典型的阳离子准二元合金中3d过渡金属杂质深能级随合金成份的变化趋     

谈露天深孔爆破技术

随着深孔钻机如全液压钻机、高风压及中风压钻机的出现和不断完善以及装运设备的不断改进,爆破技术的迅猛提高和爆破器材的日益发展,深孔爆破在改善和控制爆破质量、提高大型机械设备装运效率和经济效益方面的优越性已明显地为人们认识与重视。     

台湾地区地壳厚度的研究——三维重力反演的初步结果

布格重力异常可以看成地面观测点以下,不同规模、不同密度和不同深度地质体引力效应的总和。换言之,在布格异常中,混有地壳浅层和深部的信息。台湾既有前第三系变质岩,也有第三、第四系沉积岩。一些地层夹有混杂岩、蛇绿岩和外来岩块.特别是还存在着大量密度倒置的推覆体(毕庆昌,1989)。面对如此复杂的三维图象,怎样从布格异常中提取深部信息呢?     

金雕:不报杀子之仇誓不罢休

金雕的两只大爪子力量很大,可以一下子扭断猎物的脖子,它那展开超过两米的巨大翅膀,也是攻击的有力武器。今年8月的一天清晨,在黑龙江省一个村庄的麦田上空,盘旋着一只金雕,突然,它以迅雷不及掩耳之势向一位正在收割小麦的杨氏农民俯冲而来,未等杨氏做出任何反映,他的头部就已被抓得鲜血直流了……金雕的攻击力为何如此强大?回答这个问题首先要从金雕的爪说起。金雕的爪在鹰