Karst Processes and Landforms on San Salvador Island, Bahamas

R Laurence Davis
University of New Haven, Biology and Environmental Sciences
Author Profile

Shortcut URL: https://serc.carleton.edu/75531


Continent: North America
Country: Commonwealth of the Bahamas
State/Province:San Salvador Island
UTM coordinates and datum: none


Climate Setting: Humid
Tectonic setting: Passive Margin
Type: Process


San Salvador Island is located in the Central Bahamas, about 225 km ESE of Miami and is about 12 km north to south and about 5 km east to west (Figure 1). It is notable for being Columbus' first landing site in the "new" world and there are five monuments to that event. Like all of the Bahamas, it probably sits on an isolated fragment of continental crust formed during the opening of the Atlantic Ocean. Slow subsidence coupled with the deposition of carbonates resulted in a stack of sediments that is probably more than 8000 m thick (Dietz et al.,1977). While most of the Bahamian Islands are part of large platforms (Figure 1), San Salvador sits on its own isolated platform whose boundaries plunge to depths of over 4000 m at angles up to 85°.

During the Pleistocene glaciations, sea levels changed considerably. They have been as much as 6 m above present (about 125,000 years ago) to about 125 m below (about 70,000 years ago). These fluctuations had a considerable impact on the size of many Bahamian islands. However, because of its steep-walled, isolated platform, the size of San Salvador changed little.

Over most of the past 2 million years, sea levels have been lower. During these times, dust, mostly from the Sahara Desert, accumulated on the islands. It hardened into a red soil (Paleosol) that may be impermeable (Figure 2).

"Karst" is the general term used for cavernous areas. Most karst regions are found on carbonate rocks. The basic geomorphic process is solution. The chemistry is shown in Figure 3. The acids produced by these processes are responsible for much of the dissolution in karst regions. Note, however, that temperature and the concentration of carbon dioxide in the atmosphere (including cave and soil atmospheres) control these reactions. This means that it is possible to produce saturated solutions with many different calcium and carbon dioxide concentrations. When two of these solutions mix, they produce an unsaturated solution which results in more rock dissolution in the zone of mixing (Palmer, 1991). Recently it has been hypothesized that bacteria may play an even more important role in solution than this mixing phenomena (Schwabe, et al., 2008).

Figure 4 shows the ground water hydrology on a typical island. There are two distinct zones where waters with differing chemistry are mixing. The first of these is at the water table and the second is at the halocline (the fresh-salt water boundary). Bacteria may also be active in these places. Because of this, dissolution tends to be concentrated here, resulting in cave formation (Figure 5a). Changing sea level changes the dissolution loci resulting in caves at many different levels (Figure 5b). In addition to the mixing zones, dissolution also takes place at the surface ("Epikarst"). This produces pits large (up to 30 m deep) and small (mm scale).

The processes discussed in the previous paragraphs have all been active on San Salvador resulting in a wide range of features (Figures 6 and 7). Epikarst features include highly pitted surfaces (known as "moon rock" on San Salvador) (Figure 8) and deep shafts (Figure 7a). The pitted surfaces cover large areas of the island's interior (Figure 9). Rainwater charged with carbon dioxide lands on the bare rock and collects in small depressions. Dissolution enlarges these. Because the rock surface is impermeable, water does not infiltrate. Eventually the water begins to flow downhill until it reaches a spot where is can move down into the rock (Figure 10). Additional solution here may produce a deep pit.

Water table caves (Figure 7c and d) are usually shallow. Initially they form with no surface opening. However, dissolution of the rock both at the surface above the cave and within the cave itself eventually causes collapse. The resulting depression is locally called a "banana hole" (Figure 11) because the soils at the bottom are frequently fertile and good for growing bananas. These caves and holes can be quite numerous. On one part of the island, densities reach 2000 per square kilometer (Harris, 1997). Sometimes the banana holes are quite large and, surprisingly, drain poorly, perhaps because the bottoms are covered by paleosols (Gentry, 2005). During the rainy season, these can become deep pools (Figure 12).

Flank margin caves form along the margin of the island under the flank of a ridge where the halocline and the water table merge (Mylroie and Carew, 1990) (Figure 4). The most intense mixing takes place here and the proximity to the surface means that bacteria may also be abundant (Schwabe, personal communication). The result is aggressive dissolution. The caves form with no opening to the surface. Subsequent cliff retreat may expose them as may collapse of the roof. Because of high modern sea levels, most caves of this type are now well underwater and inaccessible. However we can explore those formed at the highest sea level stand (+6 m, 125,000 years ago) (Figure 7b). There are over 50 of these known and more are being found each year.

Associated References

  • Dietz, R.S.; Holden, J.C.; and Sproull, W. P. 1970. "Geotectonic Evolution and Subsidence of the Bahama Platform." Geological Society of America Bulletin (81:1915-1928).
  • Gentry, Cara L. and Davis, R. Laurence. 2006. Geomorphological and Hydrological Controls of Fresh Water Wetlands on San Salvador Island, Bahamas. in Davis, R. Laurence and Gamble, Douglas W., eds. Proceedings of the 12th Symposium on the Geology of the Bahamas and Other Carbonate Regions. San Salvador, Bahamas: Gerace Research Centre.
  • Godfrey, P.J.; Edwards, D.C.; Davis, R.L.; and Smith, R.R. 1994. Natural History of Northeastern San Salvador Island: A "New World" Where the New World Began. San Salvador, Bahamas: Bahamian Field Station. www.geraceresearchcentre.com
  • Harris, Jonathan G. An Analysis of Banana Hole Development on San Salvador Island, Bahamas. Unpublished Masters Thesis. Mississippi State University.Mylroie, J.E. and Carew, J.L. 1990. "The Flank Margin Model for Dissolution Cave Development in Carbonate Platforms." Earth Surface Processes and Landforms (15: 413-424).
  • Mylroie, J.E.; Carew, J.L.; and Vacher, H.L. 1995. "Karst Development in the Bahamas and Bermuda." in Curran, H. Allen and White, Brian, eds. Terrestrial and Shallow Marine Geology of the Bahamas and Bermuda. Geological Society of America Special Paper 300. Boulder, CO.: Geological Society of America. pp 251-268.
  • Palmer, A.N. 1991. "Origin and Morphology of Limestone Caves." Geological Society of America Bulletin (103: 1-21).
  • Schwabe, Stephanie J.; Carew, James L.; and Herbert, Rodney A. 2008. "Making Caves in the Bahamas: Different Recipes, Same Ingredients." in Park, Lisa and Freile, Deborah, eds. Proceedings of the 13th Symposium on the Geology of the Bahamas and Other Carbonate Regions. San Salvador, Bahamas: Gerace Research Centre.
  • Mylroie, John E. and Carew, James, L. 2008. Field Guide to the Geology and Karst Geomorphology of San Salvador Island. an Salvador, Bahamas: Gerace Research Centre.
  • Davis, R. Laurence and Johnson, Calvin R., Jr. 1989 "Karst Hydrology of San Salvador." in Mylroie, John E., ed. Proceedings of the 4th Symposium on the Geology of the Bahamas. Port Charlotte, FL: Bahamian Field Station.