Geology of the Georgia Coast
The geological development of the Georgia coast and shoreline is the result both of ongoing, and geologically long-term, physical processes and of their interaction with a rapidly increasing population intent on settling and developing the most dynamic portion of the coastal zone.
The state is divided into five major physiographic provinces based primarily on geologic age and origin,
The fall line also represents the inland edge of the oldest Coastal Plain sediments that were deposited in the sea of the Cretaceous period more than 100 million years ago. Tens of millions of years of Piedmont surface erosion provided sediment to the Cretaceous shoreline until the Coastal Plain built out and up to its present extent.
Although the Coastal Plain is the youngest province, it occupies more than half of the state's land surface. The Coastal Plain is divided into upper and lower regions, the latter of which is distinguished by the ocean's highest incursion during the geologically recent Pleistocene epoch, which began almost 2 million years ago.
The Lower Coastal Plain extends inland for approximately sixty-five miles between the Savannah and St. Marys rivers, and includes eleven counties. Within this region, the remains of six progressively
The modern (Holocene) Georgia coast is bordered by a series of relatively short, wide barrier islands separated by relatively deep tidal inlets, or sounds. Extensive sand shoal systems are present seaward of the inlets and central portions of the island.
Eight major islands and island groups comprise the 100 miles of coast between the Savannah and St. Marys rivers. These are Cumberland/Little Cumberland, Jekyll, St. Simons/Sea Island/Little St. Simons, Sapelo/Blackbeard, St. Catherines, Ossabaw, Wassaw, and Tybee/Little Tybee. Tybee, St. Simons/Sea Island, and Jekyll are accessible by roadway and are the only developed barrier islands.
Popularly known as the Golden Isles, the barrier islands are composed of dune and beach ridge sands formed by the interaction of wind, waves, currents, sand supply, and a slowly rising or stable sea level. The availability of sand largely determines whether the shoreline will erode or build. In addition to providing natural habitat for numerous plant and animal communities, as well as recreational destinations for nearby human populations, the barrier islands protect the mainland from the brunt of major storms and hurricanes. The developed barrier islands have no such outer defense.
Six of the eight largest islands are composite barriers consisting of a core of beach and dune deposits
About 5,000 years ago, the rate of sea-level rise decreased from three feet per century to a little less than a foot per century. The Holocene barrier islands began to form at, or near, their present locations and, in most cases, welded onto the Pleistocene barriers. Only vestiges of the Holocene barriers remain on Cumberland, Jekyll, and St. Catherines islands, the major portions having been eroded away by the slow but inexorable rise of the sea.
With the exception of wave action associated with seasonal storms (nor'easters) and infrequent hurricanes, the tide's twice-daily ebb and flow is by far the dominant physical process along the Georgia coast. Because of the concave shape of the shoreline and a broad, shallow continental shelf, wave energy is low with wave heights averaging from two to less than four feet at the breaking point.
Prevailing onshore winds are from the northeast and southeast, whereas prevailing offshore winds are from the northwest and southwest. On the eastern coast of the United States, the prevailing alongshore current and sediment transport is from north to south. However, summer wind conditions frequently cause a south to north nearshore sediment transport. (It should be noted that current direction relates to destination, while wind direction relates to origin.)
The average tidal range is just higher than six feet. Seasonal spring (biweekly) tides range up to ten feet and are the highest along the U.S. South Atlantic coast. The geological development of the Georgia coast is profoundly influenced by the large, but cyclic, storage capacity of the tidal marshlands behind the barrier islands. Powered by the six- to ten-foot tides, nearshore waters are forced in and flushed out of the sounds through the constricted inlets between the barrier islands.
Ebb-tide deltas, inlets, and relatively short, wide barrier islands are associated with tide-dominant, low-wave-energy coasts. Flood-tide deltas, which form in the interior of the inlets, together with long, narrow barriers that have few inlets, are associated with wave-dominant, low-tidal-range coasts, such as those along Texas and North Carolina.
The coastal sand-sharing system consists of the ebb-tide delta; the alongshore, downcurrent drift of sediment; and the adjacent dynamic beach and dune system. Under natural conditions, the ebb-tide delta is slowly skewed downcurrent, and its southern component welds onto and nourishes the northern, or upcurrent, portion of the adjacent barrier island. Thus the inlet/alongshore drift system passes, or shares, sand from upcurrent sources to downcurrent recipients. Any interruption of this flow of sand, including inlet dredging, jetties, shoreline armoring, and so on, results in the starvation and erosion of downcurrent shorelines.
Georgia tidal marshlands include the saltwater Spartina sp. wetlands, which are predominant in the two- to five-mile-wide
Salt marsh vegetation consists chiefly of smooth cordgrass (Spartina alterniflora) in the widespread low marsh areas. The lower marshes are fringed by the needlerush (Juncus roemarianus), spike grass or saltgrass (Distichlis spicata), and glasswort (Salicornia spp.) in the higher marshland adjacent to marsh islands (hammocks) and the mainland.
The present marshlands developed over the past several thousand years, as the Holocene sea slowly rose to reoccupy the area behind the existing Pleistocene Silver Bluff barriers
Scattered throughout the tidal marshlands are numerous erosional remnants of Pleistocene and Holocene barrier islands and back barrier deposits. These are the vegetated hammocks, or back barrier islands, that because of increasing development pressure and the desire for overmarsh access have been the subject of recent study by the Georgia Department of Natural Resources Coastal Marsh Hammocks Advisory Council. According to the March 2002 council report, 1,200 hammocks, ranging in size from less than one acre to more than 1,000 acres, are located in the six shoreline counties.
History of Shoreline Change
Studies of the historical changes in the mean high-water shoreline of Georgia indicate that the basic causes of shoreline erosion are:
—The worldwide rise in sea level (an average of one to two feet per century);
—Seasonal storms and hurricanes. The Georgia coast has not had a major hurricane (defined as at least a category 3 hurricane) since the late 1890s;
—Man's activities, including channel dredging with offshore disposal of dredged material, jetty construction, shoreline structures, and damming of rivers.
The long-term trend of worldwide sea level rise dictates that shoreline erosion will increase. Where shorelines of the developed islands have been fixed by the emplacement of man-made structures, beach slopes have been flattened so that the time the beach can be used between high tides is greatly shortened. In order to have and retain a recreational beach, sand must be brought in from a nearby source. Such beach "nourishment" is costly and repetitious and often has negative environmental aspects.
Future Management of Georgia Coast
With the exception of Tybee, St. Simons/Sea Island, and Jekyll, the remaining Georgia barrier islands
A 2003 Pew Oceans Commission Report states that more than half of the U.S. population resides in coastal counties comprising only 17 percent of the nation's land area. This has resulted in a coastal population density almost five times the national average. According to a 2002 Pew Oceans Commission report, the national coastal population will increase 20 percent by 2015, amounting to a daily increase of 3,600 people.
Following the national trend, Georgia's coastal population grew by about 30,000, or about 5.5 percent, between 1998 and 2002. During this same period the state population as a whole increased by an estimated 696,774 people, mostly in the Atlanta region. More specifically, the population growth in the eleven counties of the Georgia coastal zone between 1970 and 2000 was 210,505, an average growth of 16 percent per decade. Thus the coastal marshlands and estuaries are being affected by products and activities of the local population, as well as by those of a much larger portion of the state by way of the five major watersheds that empty into coastal estuaries.
In addition to an expanding resident population, the growing tourism industry creates am impact on coastal ecosystems. The National Oceanic and Atmospheric Administration estimates that coastal tourism and recreation account for 85 percent of all U.S. tourism revenues.
To effectively deal with population impacts as well as those caused by natural processes, decision makers and state management agencies must understand the processes, dynamic nature, and value of the Georgia coast.
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John R. Hails and John H. Hoyt, "The Nature and Occurrence of Heavy Minerals in Pleistocene and Holocene Sediments of the Lower Georgia Coastal Plain," Journal of Sedimentary Petrology 42 (1972): 646-66.
Paul F. Huddlestun, A Revision of the Lithostratigraphic Units of the Coastal Plain of Georgia: The Miocene through Holocene, Bulletin 104 (Atlanta: Georgia Geologic Survey, 1988).
James E. Kundell et al., The Georgia Coastal Management Incentive Grant Program: Review of Performance 1998-2002 (Athens: Carl Vinson Institute of Government, University of Georgia, 2003).
G. F. Oertel, "Ebb Tidal Deltas of Georgia Estuaries," in Estuarine Research, vol. 2, Geology and Engineering, ed. L. Eugene Cronin (New York: Academic Press, 1975).
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Vernon J. Henry, Applied Coastal Research Laboratory, Skidaway Island
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