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Geological Structures通用Sedimentary rocks occupy the great part of the earth’s land surface, they occur essentially as layers or strata and are part of the stratigraphical sequence of rocks. A single stratum may be of any thickness from a few millimeters to a meter or more, and the surfaces which separate it from the next stratum above or below are called bedding plans. In this part we are concerned with the arrangements of sedimentary rocks as structural units in the earth’s crust.Dip and strikeConsider a flat uniform stratum which is tilted out of the horizontal. On its sloping surface there is one direction in which a horizontal line can be drawn, called the strike. It is a direction that can be measured on beds that are exposed to view and recorded as a compass bearing. At right angles to the strike is the direction of maximum slope, or dip. The angle of inclination which a line drawn on the stratum in the dip direction makes with the horizontal is the angle of dip (or true dip), and can be measured with a clinometer and recorded to the nearest degree. For example, a dip of 25 in a direction whose bearing is N.140 would be written 25 at 140. The bearing is taken from north (or, in the southern hemisphere, from south). A line on a sloping rock-surface in any other direction than that of the true dip makes a smaller angle with the horizontal, called an apparent dip. Apparent dips are seen in quarry faces where the strike of the face is not parallel to the true dip direction.Strike and dip are two fundamental conceptions in structural geology, and are the geologist’s method of defining the attitude of inclined strata. The information is placed on a map as a short arrow (dip arrow) with its tip at the point of observation, together with a number giving the angle of true dip.UnconformityThere is frequently a discordance in dip between older and younger strata, where older beds have been folded and denuded during a rise of sea floor before the younger series was deposited on them. The unconformity was later tilted to its present position. An unconformity marks both a break in the process of deposition and an interval of time when no sediments were laid down in the area.FoldsIt is frequently seen that strata in many parts of the Earth’s crust have been bent
dipping beds, mentioned above, are often parts of such structure. An arched fold in which the two limbs dip away from one another is called an antiform, or an antcline when the rocks that forms its central part or core are older than the outer strata. A fold in which the limbs dip towards one another is a synform, or a syncline when the strata forming the core of the fold are younger than those below them. It is necessary to make this age distinction before naming a fold (which may be turned on its side, or inverted); if the relative ages of the core and “envelop” rocks around it are not known, the terms antiformand synform are used.In the cross-section of an upright fold the highest point on the anticline is the crest and the lowest point of the sy the length of the fold extends parallel to the strike of the beds. The line along a particular bed where the curvature is greatest is called the hinge or hinge- and the part of a folded surface between one hinge and the next is a fold limb. The surface which bisects the angle between the fold limbs is the axial surface, and is defined as the locus of the hinges of all beds forming the fold (Fig.1). This definition allows for the curvature which is frequently found in an axial surface. The intersection of an axial surface with the surface of the ground can be called the axi in some instances it is marked on a geological map as “axis of folding”.
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FaultsThe state of stress in the outer part of the earth’s crust is complex, and earlier in this part we have seen how some rocks respond to compression by folding and buckling. Commonly also, fractures are formed in relief of stress which has accumulated in rocks, either independently of folds or associated with them. The fractures inclu faults are fractures on which relative displacement of the two sides of the b joints are those where no displacement has occurred. Groups of faults and sets of joints may both form patterns which can be significant in indicating the orientation of the stresses that resulted in the fracturing, though a clear indication of this is not always forthcoming. In this account our discussion is limited to the geometrical description of fractures and some of the structural patterns to which they give rise.A normal fault is an inclined surface along which a rock mass slipped downward. A normal fault is the result of tension in the crust and increases the area covered by the rocks involved. A reverse fault is an inclined surface along which a rock mass has moved upward to override the neighboring mass. If the inclination of the fault surface is less than 45 it is called a thrust fault. A reverse fault is the result of compression in the crust and decreases the area covered by the rocks involved. A strike-slip fault is a surface along which one rock mass has moved horizontally with respect to the other. A strike-slip fault is the result of oppositely-directed forces in the crust that do not act along the same line, so that the result is a distortion of the crust rather than a change in area.JointsParting-plane known as joints are ubiquitous in almost all kinds of rocks. They are the most common structure to affect the behavior of soil and rock in engineering works. The fissures of many overconsolidated sediments are joints. They are fractures on which there has been no movement, or no discernible movement, of one side relative to the other. In this way joints differ from faults. Groups of parallel joints are called joint sets, and for two or more sets which intersect the term joint system is used. Many joints are developed in the relief of tensional or shearing stresses acting on a rock mass. The cause of the stresses has been variously ascribed to shrinkage or contraction, compression, unequal uplift or subsidence, all are a relief of in situ stress. Geological structures and economic depositsGeological structure influences the original location of economic deposits and modifies the shape of previously formed accumulation. The influence geological structure may have upon the location of mineral accumulations is most clearly demonstrated by the geometry of deposits formed from mineralized fluids. Many hydrothermal lode deposits occupy voids created by faults and joints formed when the intruding parent magma deformed surrounding rock. Joint sets and faults existing early in the hydrothermal phase may contain different minerals from those formed later, if there is a change in the character of the hydrothermal fluids. One joint set may be rich in one mineral association whilst a second may be barren. Some faults and joints contain mineral deposits that are zoned, the first formed mineral being in contact with the wall of the fracture, with later deposits sandwiched in between. These fractures may have been used many times to conduct fluids away from magma at depth.
地质结构？好多专业名词啊，发到英语翻译吧吧~
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小CASE， 一千字200元，这样的翻译常做，想的话你可以留下QQ
1楼地质构造通用沉积岩占地球陆地面积的很大一部分，他们
的出现主要是层或地层和岩石的地层序列的一部分。单一阶层可以是任何厚度从1
毫米至1米的几个或更多，而这表面层分开的未来高于或低于它被称为床上用品的计划。在这部分我们对在地球的地壳构造单元沉积岩石的安排。DIP和罢工考虑一个单位统一地层是倾斜出水
平。在它的表面有一个倾斜的方向，一个水平线上，可以得出，所谓的罢工。这是一个可以在暴露在视图和一个指南针轴承测量记录病床方
罢工的直角是最大坡度，或浸方向。在倾斜的一条线就在地层倾斜方向与水平的角度制定出来的将是对倾角（或真倾角），并且可以用测斜仪测量并记录到最近的
程度。例如，倾角25的方向，其轴承是N.140将被写入25在140。轴承是来自北方（或在南半球，由南）。阿坡岩上，在任何比真正的倾角与水平，使被称为一个明显的倾斜角度较小，
其他方向的水面线。显然逢低在采石场看到面临的脸部位置罢工是不平行
的真实倾角方向。罢工和浸两个基本概念在构造地质学，而且是地质学家的界定斜地
层的态度方法。这些信息放置在一个简短的箭头（箭头浸同其在尖端的观测
点），以使真正的倾角地图串在一起。不整合有一个经
常在浸老年人和青年人之间的不协调阶层，其中年龄较大的折叠床，并在之前的海床裸露的年轻系列上升了，在上面沉积。不整合其后
倾斜到现在的位置。一
个不整合标志着双方在沉积过程的时间休息和在没有沉积物在该地区埋下了间隔。褶
皱这是常见的，在地壳岩层许多地方已经弯曲或屈曲成倍;浸渍床，
上面提到的，往往是这种结构件。一个拱形倍，其中两肢浸远离彼此称为背形式，或antcline当岩石形成了中央的部分或核心是早于外阶层。阿倍四肢浸在其中对彼此是synform，或向斜地层时形成的褶皱核心比低于他们的年轻。要
作出一个前命名倍（这可能是其副作用，或倒转身）;如果核心的和相对年龄“信封”不知道它周围的岩石，这些词汇antiformand
synform使用这个年龄段的区别。在跨第一个直立褶皱背斜上的最高点是波峰与向斜最低点是谷底，折叠长度的平行延伸到床的罢工。沿特定的床上曲率最大的是所谓的铰链或铰链的折叠线线，以及一个铰链和1至下
一折叠表面部分是肢体倍。该平分的表面之间的角度是四肢褶皱轴面，并为所有组成倍（图1）病床的铰链的轨迹定义。这一定义允许的曲率是经常在一轴表面发现。一个与地面相交轴表面可称为褶皱轴迹，有些是在为“折叠”邪恶轴心地质地图上标出的实例。2楼故障作者强调在地球的地壳外层部分国家是复杂的，在这方面我们已经看到一些岩石反应，折叠和屈曲，以压缩的部分提前。通常也，骨折形成的岩石中应力的
积累已救济，无论是独立或与他们相关的褶皱。骨
折包括断层和节理，断层裂缝上的破裂，双方已经发生相对位移;接头是那些没有发生位移。断层和节理组组都可能形成的模式，可显着标明的压力，在导致破裂，方向虽然这是一个即将并不总是清楚地表明。在这个帐户我们的讨论
仅限于裂缝几何描述和结构模式的一些它们所引起。阿正断层是倾斜的表面沿一
名岩体向下滑落。一个正常的故障是在地壳紧张的结果，并增加了
有关岩石的覆盖范围。阿逆断层是倾斜的表面沿岩体提出一个向上覆盖邻近的质量。如果断层面倾角小于45就被称为逆冲断层。阿逆断层是地壳中的压缩结果，降低了有关岩石
的覆盖范围。阿
走滑断裂是沿着哪一个岩体已迁往其他方面的水平表面。阿走滑断层是地壳中的行为不沿同一路线相反指导力量的结果，因此，其结果是地壳，而不是土地面积的变化
变形。接头临别平面为关节，几乎所有的岩石类型称为无所不在。他们是最常见的结构，影响土壤和岩石工程的行为。许多固结沉积物中的裂缝是关节。他们是骨折上一直没有动作，或者没有明显的运动一方面，相对于其他。这样关节不同故障。平行关节组被称为联合组，以及
两个或更多集的相交长期的联合系统的使用。许多
关节是发达国家在拉张或剪切应力对岩体救援行动。对事业的压力已不同程度归因
于收缩或收缩，压缩，隆起或沉降不均等现象，全都是在地应力援助。地质结构和经济存款地质结
构影响着经济存款原来的位置，并修改了原来的形状形成的积累。地质构造的影响可能对囤积位置的矿产是最明显的从几何矿化液形成的存款证明。许多热液矿脉存款占受断层和关节造成空洞形成
时的岩浆侵入父围岩变形。联合组和现有的早期阶段的热液故障可能包含来自不同矿物组成后，如果有一个在热液流体性质的变化。一个联合集
可能在一，而丰富的矿产协会第二次可能是不毛之地。一些断层和节理含有矿物质，划
为存款，第一次组成矿物与墙接触的骨折与被夹在中间稍后存款。这些裂缝可能已被多次使用，进行从岩浆流体远
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哈哈 ，典型的翻译软件的作品！DIP是地层倾角，没翻译出来，DIP and Strike是地层倾角及走向； Faults,是断层啊，可不是错误；
真是乐死人！
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