Karst and Glades
Text by EF (Pat) Hollyday, USGS (ret.)
Karst is an area of land that is underlain by rock that dissolves slowly with slightly acid rainwater. There are many types and degrees of development of karst (Brahana and others, 1988, table 4; Herak and Stringfield, 1972); cedar glades, however, occur on pavement karst with thin (less than a few inches thick), or no, soil covering limestone rock in a moderate temperature climate.
Karst may be recognized by the presence of several, or all, of the following features:
sinkholes (natural, closed topographic depressions); sinking streams
photo by US Army Corps of Engineers
of sinkhole at 3 Hickories Trail.
seasonally dry or wet streams, ponds, or lakes; caves; and large springs
Photo by Pat Hollyday
Cedar (or limestone) glades are natural openings in a (typically red cedar) forest with rock pavement grading to shallow soil and with plant communities dominated by grasses and herbaceous flowering plants or by forbs, mosses, and lichens (Baskin and Baskin, 1999, p. 206 and 216).
Photo by Jeff Walck
When pointed out, the pock marked landscape of karst is perhaps the easiest feature to recognize; however, the less obvious hydrologic and biologic features integrate one part of the karst with another and are particularly sensitive to changes resulting from human activities. Sinkholes commonly connect vertically, through natural pipes in the soil, with narrow dissolution openings, larger caves, or even huge caverns in the bedrock below. The caves and caverns commonly have streams that collect water from the sinkholes and transmit the water long distances underground to large springs under, or in the banks of, nearby rivers. Thus, mature karst is drained by an underground plumbing system.
Within the twilight to total darkness of the caves and caverns, a specialized flora and fauna have evolved in response to the absence of light and to a severely diminished food supply. Some species are restricted to a single cave (Mohr and Poulson, 1966, p. 175).
The Mammoth Cave system and adjacent Pennyroyal Plain in central Kentucky comprise an extensive karst near middle Tennessee that is formed on thick, soluble limestone (Quinlan and others, 1983). Sinkholes are so numerous in the plain that they might appear to result from aerial bombing. Streams flow north into rock bluffs, follow deep caves, flow under caves of the national park, and discharge into the Green River. On a smaller scale, the Snail Shell Cave system just west of Murfreesboro, Tennessee, exhibits similar topographic and drainage features (Thompson and others, 1989).
Karst forms primarily on and in limestone when rainwater picks up acids in the soil zone, and the acid attacks the calcium carbonate fragments of seashells that make-up the rock, releasing carbon dioxide, water, and calcium and bicarbonate ions. The ions are swept away by subsurface water leaving an opening in the rock. These openings form most readily along bedding planes, joints, and fractures in the rock. With time (thousands to millions of years), the openings widen to caves. When surface streams get into the caves, sand and gravel carried by the water abrades the walls of the cave and any collapsed rock on the cave floor to eventually form caverns. This process of cavern formation is sometimes reversed as streams and surface openings allow sediment to enter the cave and partly backfill the openings, resulting in a complex geometry of openings.
Problems of sinkhole flooding, sinkhole collapse, water pollution, and species extinction often follow human development in karst
areas (Dilamarter and Csallany, 1977). Construction of roads and structures in sinkholes
may plug the underground outlet from the sinkhole resulting in increased flood heights
and flooding of upstream properties (fig. 3). Conversely, cleaning and widening of
the outlet may allow large slugs of storm water to rapidly enter the underlying cave
system, exceeding its water carrying capacity and resulting in collapse of the soil
above the cave (fig. 4). Increased flooding also occurs down the cavern system where
this extra water reverses the normal downward flow of water from sinkholes that are
at a lower land-surface elevation than the sinkhole whose outlet was widened.
Parking lots and large paved areas collect abnormally large volumes of water during an intense storm. If this water is discharged to a single point at the edge of the pavement, the water may erode new vertical channels through the saturated soil. Water passing vertically through these pipes may overload the natural, underground drainage system and result in the collapse of the land surface. Collapse may occur not only at the point of discharge but also along the length of the receiving cave at points least expected such as under roads and valuable buildings.
Water draining from lawns, gardens, and parking areas often contains fertilizer, animal waste, and pesticides that are delivered untreated to a nearby river by the receiving cave. These pollutants add to the cost of water treatment by downstream water users. Fertilizer also stimulates the growth of unsightly algae that robs the stream water of oxygen possibly resulting in fish kills. Pollutants and sediment resulting from human activity upset the aquatic ecology of the cave-dwelling plants and animals, leading in some cases to their extinction.
The karst (limestone or carbonate) aquifers found in the Central Basin are only one of several kinds of aquifers found in Tennessee
An aquifer is a rock unit that will yield usable quantities of water to a well or spring. Below the land surface, ground water is in openings in the rock. These openings may take several forms, depending upon the rock type. Particularly in West Tennessee, water is stored in and slowly moves through the natural, irregular pore spaces between grains of sand that make-up sand aquifers like the Memphis aquifer (hyperlink to TDEC/DWS site). In much of Middle and East Tennessee, water is stored in and rapidly moves through openings that result from the dissolution of carbonate rock (limestone or dolomite) like the Knox aquifer. These openings may be small and narrow (typically along cutters, joints, and bedding planes), or enlarged to caves that a diver could stand-up in, or even huge caverns. Under the Cumberland Plateau and the Unaka Mountains of East Tennessee, water is stored in and slowly moves through fractures and faults along which little if any dissolution has taken place. Above the bedrock, a considerable amount of water can be stored temporarily in soils and weathered rock that is thicker than several tens of feet. Depending upon the size, interconnectedness, and extent of openings in any type of rock, the rock may yield only a few gallons per minute to as much as several thousand gallons per minute. Depending upon the presence and thickness of clay-rich material above the rock, the water in the openings in rock may, or may not, be exposed to contamination from chlorinated solvents or petroleum products (typically) placed on the land surface. The outcrop area of sand aquifers and areas of thinly mantled karst aquifers are considered by the State of Tennessee as the most vulnerable areas for ground-water contamination.
Map from Tennessee Ground Water 305b Water Quality Report. November, 2002
Baskin, J. M., and Baskin, C. C., 1999, Cedar Glades of the Southeastern United States
in Anderson, R. C., Fralish, J. S., and Baskin, J. M., eds., Savannas, barrens, and
rock outcrop plant communities of North America: Cambridge University Press, p. 206-219.
Brahana, J. V., Thrailkill, J., Freeman, T., and Ward, C. C., 1988, Carbonate rocks, in Back, W., Rosenshein, J. S., and Seaber, P. R., eds., Hydrogeology: Boulder, Colorado, Geological Society of America, The geology of North America, v. O-2, p. 333-352.
Dilamarter, R. R., and Csallany, S. C., eds., 1977, Hydrologic problems in karst terrains, Symposium, Western Kentucky University, Boling Green, Kentucky, Proceedings: Dublin, Ohio, National Water Well Association, p…..
Herak, M., and Stringfield, V. T., 1972, Karst—Important karst regions of the Northern Hemisphere: Amsterdam, Holland, Elsevier, 551 p.
Mohr, C. E., and Poulson, T. L., 1966, The life of the cave: New York, N.Y., McGraw-Hill, Our Living World of Nature, 232 p.
Quinlan, J. F., Ewers, R. O., Ray, J. A., Powell, R. L., and Krothe, N. C., 1983, Ground-water hydrology and geomorphology of the Mammoth Cave region, in Shaver, R. H., and Sunderman, J. A., eds., Midwestern geology: Boulder, Colorado, Geological Society of America and Indiana Geological Survey, v. 2, p. 1-85.