Deltaic environments

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Sandstone Depositional Environments
Series Memoir
Chapter Deltaic environments of deposition
Author J. M. Coleman and D. B. Prior
Link Web page
PDF PDF file (requires access)
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The contrast between the lush vegetation of the Nile delta and river course and the dry sand of the Sahara can be seen spectacularly in this enhanced true colour Medium Resolution Imaging Spectrometer (MERIS) image. The grey area to the bottom of the "triangle" of the delta is Egypt's Capitol, Cairo. On the border between Israel and Jordan is the Dead Sea, at 412m below the level of the Mediterranean, the lowest point on earth. The Dead Sea also has salinity 10 times that of the Mediterranean, and due to the high evaporation rate in the area, salt accumulates, and can be extracted, as can be seen in the southern part of this large inland lake. The lighter blue/green areas are increased evaporite deposits, in this case salt. We can also see the structure of the saltpans crossed vertically by a canal. ESA, 2003 http://bit.ly/1l8WdhM

Deltaic depositional facies result from interacting dynamics processes (wave energy, tidal regime, currents, climate, etc.), which modify and disperse riverborne (fluvial) clastic deposits. The term delta was first applied by the Greek philosopher Herodotus (490 B.C.) to the triangular land surface formed by deposits from Nile River distributaries. In the broadest sense deltas can be defined as those depositional features, both subaerial and subaqueous, formed by fluvial sediments. In many instances the deposition of fluvial sediments is strongly modified by marine forces such as waves, currents and tides, and depositional features found in deltas therefore display a high degree of variability. Depositional features include distributary channels, river-mouth bars, interdistributary bays, tidal flats, tidal ridges, beaches, eolian dunes, swamps, marshes, and evaporite flats.[1]

A significant deltaic accumulation necessarily requires the existence of a river system carrying substantial quantities of clastic sediment from an inland drainage basin to the coast, where the deposits form the delta plain. Modern deltas exist under a wide range of environmental processes; some deltas form along coasts experiencing negligible tides and minimal wave energy, whereas others form in areas where tide ranges are extreme and wave energy is intense. Despite the environmental contrasts, all actively prograding deltas have at least one common feature--a river supplies clastic sediment to the coast and adjacent shelf more rapidly than it can be dispersed by marine processes, and thus a regressive sedimentary deposit forms.

Figure 1 Components of a delta system.[2]

A delta plain generally can be subdivided into physiographic settings. Every delta plain consists of a subaerial and subaqueous component. The subaerial component is often divided into upper and lower delta plains (Figure 1), the upper plain normally being the older part of the subaerial delta and existing above the area of significant tidal or marine influences. Unfortunately, in ancient rock sequences, only faunal evidence can be used to separate these major components. The upper plain is commonly the continuation of an alluvial valley and is dominated by riverine processes. The lower delta plain lies within the realm of river-marine interaction and extends landward from the low-tide mark to the limit of tidal influence; thus a lower delta plain is most extensive in areas where tidal ranges are large and seaward gradients and topographic relief are low. The subaqueous delta plain is that part of the delta lying below the low-tide water level and contains relatively open marine fauna. It is the foundation across which subaerial delta deposits must prograde. The subaqueous delta is most commonly characterized by a seaward fining of sediments, sands and coarser clastics being deposited near the river mouths and finer grained sediment dispersing farther seaward. In most deltas, the coast of the delta plain receives dissimilar rates of sediment introduction, and it is not unusual for one part of the delta shoreline to be rapidly prograding seaward, while other parts are subjected to reworking by marine processes. If wave and current reworking are intense, the delta shoreline undergoes landward transgression, and coastal barriers, beach or dune complexes will often be formed. In other places, particularly when subsidence rates are high, marine waters encroach rapidly across the subsiding delta mass and shallow-water marine deposits will directly overlie the regressive delta deposits with no significant marine reworking taking place.

To systematically describe the sedimentary characteristics of deltaic deposits, it is convenient to subdivide the sedimentary facies into the following categories:

Delta environments have a wide variety of individual depositional facies within the overall delta sequence. This complexity results from the following factors: (a) modern deltas exist in a wide range of geographic settings, ranging in climatic regimes from arctic to temperate to tropical to arid, with basin tectonics ranging from rather stable basins to extremely actively subsiding basins; (b) deltas form primarily in the zone of interaction between freshwater and marine processes, one of the most complex process settings in all coastal environments; (c) deltas carry large volumes of sediment, ranging in grain size from gravel to clay, and deposit these sediments both overbank and into the marine environment through distributary channels; (d) rapid rates of deposition often result in formation of extremely weak foundations, with a wide variety of mass-movement processes resulting in complex redistribution of the deltaic sediment. Thus sand bodies within deltas display a variety of geometries and vertical-sequence characteristics.

The complexity of environmental settings under which deltas exist results in a variety of vertical sequences that can form within the delta facies. Delta types range from river dominated to tide dominated and wave-current dominated.[1] From the standpoint of petroleum accumulation, however, river- and tide-dominated deltas are probably the most important. In these two delta settings, reservoir-quality rocks are often deposited in close proximity to potential source beds, contemporaneous structure which forms major trapping potential is common, and most deltas exist in rapidly subsiding basins, allowing thick deltaic sequences to develop over a rather short time framework. The highly wave-reworked delta sequences are often devoid of major source rock deposits and often do not form in structure settings that result in major trapping characteristics of the deposits.

See also

References

  1. 1.0 1.1 Coleman, J. M., 1976, Deltas: Processes of deposition and models for exploration: Continuing Education Publication Company, Champaign, IL, 102 p.
  2. Coleman, J. M., and D. B. Prior, 1981, Deltaic environments of deposition, in P. A. Scholle and D. Spearing, eds., Sandstone depositional environments: AAPG Memoir 31, p. 139-178.

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