Beach processes and sedimentation pdf

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beach processes and sedimentation pdf

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Sediment transport occurs in natural systems where the particles are clastic rocks sand , gravel , boulders , etc. Sediment transport due to fluid motion occurs in rivers , oceans , lakes , seas , and other bodies of water due to currents and tides. Transport is also caused by glaciers as they flow, and on terrestrial surfaces under the influence of wind. Sediment transport due only to gravity can occur on sloping surfaces in general, including hillslopes , scarps , cliffs , and the continental shelf —continental slope boundary. Sediment transport is important in the fields of sedimentary geology , geomorphology , civil engineering , Hydraulic engineering and environmental engineering see applications , below.

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Beach sediments are derived from a wide variety of sources, including cliff erosion, rivers, glaciers, volcanoes, coral reefs, sea shells, the Holocene rise in sea level, and the cannibalization of ancient coastal deposits. The nature of the source and the type and intensity of the erosional, transportational, and depositional processes in a coastal region determine the type of material that makes up a beach. In turn, the characteristics of the sediments strongly influence beach morphology and the processes that operate on it Trenhaile, The weight-percentages of the sediment can be plotted against the diameter in phi units in the form of histograms or frequency curves.

Grain-size distributions are most frequently represented, however, by plotting the grain size data on a probability, cumulative percentage ordinate, and the phi scale on an arithmetic abscissa. The percentiles on the cumulative size distribution can be used to estimate the mean, standard deviation, and other simple descriptive statistical measures, although the calculations can also be made by computer.

For comparative purposes, sediment samples can be represented by the mean or median grain size, or by the size of the grain that is coarser than some percentage of the sample. There have been many attempts to identify the transportational processes and the depositional origin of sediments based on their sediment-size distributions.

The grain-size distributions of beach sediments often consist of three straight-line segments, rather than the single straight line of a normal distribution plotted on a Gaussian probability axis. The three segments have been variously interpreted as representing: coarse bed load, fine suspended load, and intermediate-sized grains that move in intermittent suspension; the effect of packing controls on a grain matrix, the larger grains being a lag deposit, with the finest grains resting in the spaces between grains of median size; and different laminae in the beach, representing several depositional episodes.

A further possible explanation is that the segmentation of grain-size distributions on log-normal cumulative probability paper may reflect the use of an inappropriate probability model. The log-normal model poorly represents the extremes of natural grain-size distributions, which may conform much better to a hyperbolic probability function Trenhaile, Some workers believe that the four parameters of a logarithmic hyperbolic distribution are more sensitive to sedimentary environments and dynamics than the statistical moments of the normal probability function, but others have found that there is little difference Sutherland and Lee, Grain sizes may also be fitted to a skew log-Laplace model, a limiting form of the log-hyperbolic distribution which is essentially described by two straight lines, and is defined by three parameters Fieller et al.

The shape of coarse clasts can be determined fairly easily by direct measurement, but this is usually impossible or too time-consuming for sand and other small grains. Therefore, the roundness and sphericity of sand grains has often been estimated by visual comparison with a set of standard grain images of known roundness, although Fourier analysis is increasingly being used Powers, ; Thomas et al. The density of a grain is determined by its mineralogy Table B5. In temperate regions, most beach sediment originated from the granitic rocks of continents, and they largely consist of quartz and, to a much lesser extent, feldspar grains, but carbonates may dominate in the tropics, especially where there are coral reefs.

The sediments in pocket beaches enclosed between prominent headlands, and in beaches derived from other restricted source areas, however, can be strongly influenced by the mineralogy of the local geological outcrops, or by the accumulation of shelly carbonate material.

Beaches can consist almost entirely of heavy minerals in volcanic areas, and the usually small amounts of heavy minerals in continental beach sediments, such as magnetite, hornblende, and garnet, help to identify the source rocks, their relative importance, and the direction of longshore transport.

Bulk density reflects the way the grains are arranged or packed together. Spherical grains of uniform size can be packed in four ways. The centers of grains in unstable cubic packing describe the corners of a cube, whereas a tetragonal arrangement is formed by moving the upper layer of grains so that they occupy the hollows between the grains below.

With orthorhombic packing, the centers of the lower layer of grains form a diamond pattern, with the centers of the grains in the upper layer directly above. A rhombohedral arrangement is created by moving the upper layer of grains into the hollows created by the lower layer.

Grains are sorted or separated according to their shape, size, and density Table B6. Beach sediments are generally better sorted than river sediments, but less well than dunes. Beach grain-size distributions are occasionally positively skewed, but the skew is generally negative. Although the presence of a tail of coarse grains has been attributed to the removal of fine grains, or the addition of coarse clasts or shells, skewness can also arise from a single sedimentary event, and it is not necessarily symptomatic of the mixing of two or more sediment populations McLaren, Cross-shore and longshore changes in beach sediment characteristics can result from mechanical and chemical breakdown, differential transport of grains according to their size, longshore variations in wave energy, the addition or loss of sediment, or the mixing of two or more distinct sediment populations.

Sorting occurs through selection, breaking, and mixing Carter, Rejection and acceptance phenomena play an important role in the selection process, and in perpetuating sorted grain distributions on beaches.

Rejection accelerates the transport of coarse grains over finer grains, whereas shielding impedes the movement of fine grains over coarser grains.

Grains moving over material of similar size have a high probability of being assimilated or accepted by the underlying material. Erosion of a source material produces a lag deposit that is coarser, better sorted, and more positively skewed than the original sediment.

If all the transported sediment is deposited, the deposit will be finer, better sorted, and more negatively skewed than the source. If the transported sediment is only selectively deposited, the deposit will be better sorted and more positively skewed than the source. The deposit will be finer than the source if only material finer than the mean size of the source is eroded, but it may be coarser if sediment larger than the mean size is removed from the original deposit McLaren, Factors controlling sediment sorting Steidtmann, 1 ; with permission of Blackwell Science.

Beach sediments are also sorted according to grain density, and particularly to the abundance and mineralogy of the heavy mineral component.

Small heavy mineral grains occupy the spaces between the larger and less dense quartz and feldspar grains, shielding them from the flow so that they are less easily entrained. The lighter quartz grains are transported alongshore more rapidly than the heavy minerals, even when both types of grains have the same settling velocity—presumably because the smaller size of the heavy mineral grains inhibits entrainment during each brief suspension episode. Selective longshore transport of quartz grains may therefore result in heavy minerals becoming concentrated in erosive lag deposits.

There are often concentrations of heavy minerals on beaches in the form of bands or streaks near the high tide or upper swash zones, in the troughs of ripples, or where there are shells, coarse clasts, or other flow obstructions. The upper swash zone may consist of dark layers of fine, heavy mineral grains grading upwards into light colored layers of coarser, quartz-feldspar grains. The alternating layers are between about 1 and 25 mm in thickness, and they typically extend along the beach for a few tens of meters Clifton, The formation of swash laminae has been attributed to shear sorting in the downrush, which causes the coarser grains to migrate upwards into the zone of lower shear, while the finer and heavier grains move downwards, into the zone of maximum shear at the bed.

An alternate explanation is that the smaller particles tend to fall into the spaces between the larger grains, thereby displacing coarser grains toward the surface. Heavy mineral concentrations in the cross-shore direction have either been attributed to wave asymmetry, the heavy minerals being carried onshore by high current velocities, but not by the weaker offshore flows, or to beach erosion and offshore transport of the quartz-feldspar grains.

There may be poor separation under vigorous wave conditions, however, and the heavy and light minerals can be entrained and transported together. There has been little research on the effect of sand grain shape on longshore and cross-shore sorting patterns.

The proportion of angular grains increases in the direction of longshore transport between Delaware and Chesapeake Bays, possible because their lower settling velocities allow them to remain in suspension longer, so that they are carried further and at higher rates than more rounded grains. On Long Island, however, grains become rounder with longshore transport.

In a laboratory and field study, grains of similar size and mineralogy quartz were differentially transported and sorted within the swash zone, with the more rounded grains being deposited near the top of the uprush Trenhaile et al. Skip to main content Skip to table of contents. This service is more advanced with JavaScript available. Encyclopedia of Coastal Science Edition.

Editors: Maurice L. Contents Search. Beach Sediment Characteristics. Download entry PDF. How to cite. Grain size The grain size of pebbles and other large clastic material can be measured with callipers, and sieves are used for sand and other coarse beach sediments.

A number of techniques are used to determine the size of finer sediments including Coulter Counters, pipettes, hydrometers, optical settling instruments, and electron microscopes. The grain size can be expressed using the Wentworth scale, which is based on classes that are separated by factors of two, so that each is twice the size of the one below. A log 2 transform can be used to provide integers for each of the Wentworth class limits: Open image in new window.

Table B4 Sediment grain size classification. The shape of beach grains can be expressed in various ways. The roundness of a grain, which refers to the smoothness of its surface, has been defined as the ratio of the radius of curvature at its corners to the radius of curvature of the largest inscribed circle.

Grain sphericity describes the degree to which its shape approaches that of a sphere with three equal orthogonal axes. The shape of a grain can range from spherical, to plate, to rod-like forms, according to the relationship between the three axes, which can be depicted in the form of a ternary diagram.

Grain shape can be measured and defined using a variety of indices. The shape of the grains exerts an important influence on the bulk properties of a sediment, including its packing geometry, stability, porosity, and permeability. Small cavities are created in a deposit by shell fragments and other flat, flaky, or plate-like particles, which greatly increase its porosity.

Differences in the size of the grains also affect packing density and porosity. Smaller grains occupy the spaces between larger grains, increasing the packing density and decreasing the porosity. Table B5 The mean density of some minerals found in beach sands. The mean grain size of beach sediments depends on the characteristics of the source and the nature of the sedimentary processes. Mean grain size varies according to differences in wave energy along beaches and on the exposed and sheltered sides of islands, and it also changes through time as gently sloping, storm-eroded beaches recover to their steeper, fully accreted states.

In the cross-shore direction, the coarsest sediments are generally found on a beach at the plunge point of the breaking waves, and the grains tend to become finer seawards and Table B6 Factors controlling sediment sorting Steidtmann, 1 ; with permission of Blackwell Science. Rate of sediment accumulation Slow—allows reworking of grains Rapid—allows little or no reworking of grains None—scour Nature of the sediment surface Size distribution of grains Packing and arrangement of grains Type of bedforms present Style of grain motion Traction, including sliding and rolling Saltation Suspension Fluid characteristics Velocity or shear velocity Turbulence Depth Grain characteristics Size Shape Density.

Carter, R. Coastal Environments. London: Academic Press. Google Scholar. Clifton, H. Beach lamination: nature and origin. Marine Geology , 7 : — Fieller, N. A new method for environmental analysis of particle size distribution data from shoreline sediments. Nature , : — McLaren, P. An interpretation of trends in grain size measures.

Journal of Sedimentary Petrology , 51 : — Powers, M. A new roundness scale for sedimentary particles. Journal of Sedimentary Petrology , 23 : — Sleath, J. Sea Bed Mechanics.

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Komar, P. Beach processes and sedimentation. Upper Saddle River, N. Komar, Paul D. Beach Processes and Sedimentation.

Beach sediments are derived from a wide variety of sources, including cliff erosion, rivers, glaciers, volcanoes, coral reefs, sea shells, the Holocene rise in sea level, and the cannibalization of ancient coastal deposits. The nature of the source and the type and intensity of the erosional, transportational, and depositional processes in a coastal region determine the type of material that makes up a beach. In turn, the characteristics of the sediments strongly influence beach morphology and the processes that operate on it Trenhaile, Skip to main content Skip to table of contents. This service is more advanced with JavaScript available.


Beach Processes and Sedimentation,. Second Edition. PAGE Paul D. Komar, Prentice-Hall, Upper Saddle. River, N.J., x + pp., ISBN ​5.


Beach Sediment Characteristics

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Beach sediments are derived from a wide variety of sources, including cliff erosion, rivers, glaciers, volcanoes, coral reefs, sea shells, the Holocene rise in sea level, and the cannibalization of ancient coastal deposits. The nature of the source and the type and intensity of the erosional, transportational, and depositional processes in a coastal region determine the type of material that makes up a beach. In turn, the characteristics of the sediments strongly influence beach morphology and the processes that operate on it Trenhaile, The weight-percentages of the sediment can be plotted against the diameter in phi units in the form of histograms or frequency curves. Grain-size distributions are most frequently represented, however, by plotting the grain size data on a probability, cumulative percentage ordinate, and the phi scale on an arithmetic abscissa.

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Sediment transport

Туда и обратно, - повторил он мысленно. ГЛАВА 31 Сьюзан вернулась в Третий узел. После разговора со Стратмором она начала беспокоиться о безопасности Дэвида, а ее воображение рисовало страшные картины.

 Опоздала на самолет. Она кивнула. - Потеряла билет.


The coastal sedimentation model in the Doce River mouth and surroundings extends beyond the hydraulic jetty effect created by its stream-flow.


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