《工程地质专业英语》.docx
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1、工程地质专业英语教学大纲课程代码:课程名称:工程地质专业英语学时安排:总学时 36学分: 2适合专业:工程地质先修课程:大学英语 , 工程地质学 ,工程岩土学等教材:工程地质专业英语郑孝玉编,吉林大学校内讲义,2005,7 参考书:编写人:郑孝玉 教学目的和要求工程地质专业英语是工程地质专业 4 年级学生的选修课,是在学生学习和掌握了基础理论课,专业课及大学英语之基础上为培养和提高学生专业英语能力而设置的。通过讲授和与学生交流为他们灌输一些相关专业词汇,表述方式及科学文献的翻译、课程写作技巧和规范等。为将来学习和工作储备一些相关知识。 课程内容概要1. 本课程教学内容l The Enginee
2、ring Properties of Rocks1) rock index propertiesCertain index properties of rocks are of particular importance to the engineering, which are defined below.Specific gravity (Gs and Gb). Gb is the specific gravity of the solid mineral material of the rock by itself. Gb is the specific gravity of the c
3、omplete rock, grain plus voids, with the voids empty except for air. Both are defined as a weight per unit volume.Saturation moisture content (is). This is the total amount of water present in a rock with the voids full.The ratio of weight of water to dry weight of rock sample, expressed as a percen
4、tage, is the saturationmoisture content (is).Moisture content ( W). This is the amount of water normally present in the voids of a rock , again expressed as a percentage (see is) above. Rocks are rarely saturated with water, thus in normalcircumstances w is less than is.Porosity (n). This is the rat
5、io of volume of voids in a rock total volume of the sample. It is expressedas a percentage; 10% average, 5% is low and more than 15% is high.The factors that control the porosity of terrigenous sedimentary rocks and soils are as follows:(a) The degree of cementation(b) The sorting of the sediment(c)
6、 The packing of the grains(d) The shape of the grainsWater-yielding capacity. Not all of the water in a rock can be removed from it by flow under the force of gravity. Some is held as a film on the surface of the grains by capillary forces.Permeability (k). This is a measure of the fluid conductivit
7、y of the rock for a given hydraulic gradient.2) basic characteristics of soils2.1 the nature of soilsThe destructive process in the formation of soil from rock may be either physical or chemical. The physical process may be erosion by the action of wind, water or glaciers, or disintegration caused b
8、y alternate freezing and thawing m in cracks in the rock.The chemical process results in changes in the mineral form of the parent rock due to the action of water (especially if it contains traces of acid or alkali), oxygen and carbon dioxide. Chemical weathering results in the formation of groups o
9、f crystalline particles of colloidal size (0.002 mm) known as the clay minerals.Particle sizes in soils can vary from over 100 mm to less than 0.001 mm. Most types of soil consist of a graded mixture of particles from two or more size ranges. All clay size particles are not necessarily clay mineral
10、particles: the finest rock flour particles may be of clay size. If clay mineral particles are present they usually exert a considerable influence on the properties of a soil, an influence out of all proportion to their percentage by weight in the soil.2.2 particle size analysisThe particle size anal
11、ysis of a soil sample involves determining the percentage by weight of particles within the different size ranges. The particle size distribution of a coarse-grained soil can be determined by the method of sieving. The soil sample is passed through a series of standard test sieves having successivel
12、y smaller mesh sizes. The weight of soil retained in each sieve is determined and the cumulative percentage by weight passing each sieve is calculated. If fine-grained particles are present in the soil, the sample should be treated with a flocculating agent and washed through the sieves.The particle
13、 size distribution of a soil is presented as a curve on a semi-logarithmic plot, the ordinates being the percentage by weight of particles smaller than the size given by the abscissa. The flatter the distribution curve thelarger the range of particle sizes in the soil; the steeper the curve the smal
14、ler the size range. A coarse-grained soil is described as well graded if there is no excess of particles in any size range and if no intermediate sizes are lacking. In general a well graded soil is represented by a smooth, concave distribution curve. A coarse-grained soil is described as poorly grad
15、ed (a)if particles of both large and small sizes are present but with a relatively low proportion of particles of intermediate size (a gap-graded soil). Particle size is represented on a logarithmic scale so that two soils having the same degree of uniformity are represented by curves of the same sh
16、ape regardless of their positions on the particle size distribution plot. The particle size corresponding to any specified value on the percentagesmaller scale can be read from the particle size distribution plot.2.3 plasticity of fine-grained soilsPlasticity is an important characteristic in the ca
17、se of fine-grained soils, the term plasticity describing the ability of a soil to undergo unrecoverable deformation at constant volume without cracking or crumbling. Plasticity is due to the presence of clay minerals or organic material.Most fine-grained soils exist naturally in the plastic state. T
18、he upper and lower limits of therange of water content over which a soil exhibits plastic behaviour are defined as theliquid limit (LL or wL) and the plastic limit (PL or wP) respectively.2.4 soil compactionCompaction is the process of increasing the density of a soil by packing the particles closer
19、 together with a reduction in the volume of air: there is no significant change in the volume of water in the soil. In the construction of fills and embankments, loose soil is placed layers ranging between 75 mm and 450 mm in thickness, each layer being compacted to a specified standard by means of
20、rollers, vibrators or rammers. In general the higher the degree of compaction the higher will be the shear strength and the lower will be the compressibility of the soil.The degree of compaction of a soil is measured in terms of dry density, i.e. the mass of solids only per unit volume of soil.The d
21、ry density of a given soil after compaction depends on the water content and the energy supplied by the compaction equipment (referred to as the compactive effort).The compaction characteristics of a soil can be assessed by means of standard laboratory tests. After compaction using one of the three
22、standard methods, the bulk density and water content of the soil are determined and the dry density calculated. For a given soil the process is repeated at least five times, the water content of the sample being increased each time. At low values of water content most soils tend to be stiff and are
23、difficult to compact. As the water content is increased the soil becomes more workable, facilitating compaction and resulting in higher dry densities. At high water contents, however, the dry density decreases with increasing water content, an increasing proportion of the soil volume being occupied
24、by water.In SituTesting1. penetrometersPenetrometer test evolved from the need to acquire data on subsurface soils which could not be obtained by other means. Basically a penetrometer consists of a conical point attached to a drive rod which is forced into the ground either by hammer blows or by jac
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