![]() 86–89.īull, P.A., 1983, Chemical sedimentation in caves, in Goudie, A.S., and Pye, K., eds., Chemical sediments and geomorphology: precipitates and residua in the near-surface environment: London, Academic Press, p. 31–42.īull, P.A., 1977, Laminations or varves? Processes of fine-grained sediment deposition in caves: Proc. 83–112.īroughton, P.L., 1983, Environmental implications of competitive growth fabrics in stalactitic carbonate: Int. 447–463.īrod, L.G., 1964, Artesian origin of fissure caves in Missouri: Bull., Nat. 675–81.īretz, J.H., 1949, Carlsbad Caverns and other caves of the Guadalupe Block, New Mexico: J. La Baconniere.īogli, A., 1980, Karst hydrology and physical speleology: Berlin, Heidelberg, New York, Springer- Verlag, 284 p.īretz, J.H., 1942, Vadose and phreatic features of limestone caves: J. 83–92.īogli, A., 1970, Le Holloch et son karst: Neuchatel, Ed. 1–21.īogli, A., 1964, Mischungskorrosion, ein Beitrag zum Verkarstungs-problem: Erdkunde, v. 735–751.īocker, T., 1969, Karstic water research in Hungary: Internat. 1235–1252.īlumberg, P.N., and Curl, R.L., 1974, Experimental and theoretical studies of dissolution roughness: J. 22–51.īerner, R.A., 1978, Rate control of mineral dissolution under earth surface conditions: Am. 13–19.īeaupre, M., 1975, Les regions karstiques du Quebec: Speleo-Quebec, v. Soci, in press.īastin, B., 1979, L’analyse pollinique des stalagmites: une nouvelle possibility d’approche des fluctuations climatiques du Quaternaire: Annales de la Societe Geologique de Belgique, t. 280–293.īakalowicz, M., Ford, D.C., Miller, T.E., Palmer, A.N., and Palmer, M.V., Thermal genesis of solution caves in the Black Hills, South Dakota. 523–536.īack, W., Hanshaw, B.B., and Van Driel, J.N., 1984, Role of groundwater in shaping the eastern coastline of the Yucatan Peninsula, Mexico, in LaFleur, R.G., ed., Groundwater as a geomorphic agent: London, Allen and Unwin, Inc., p. 3–19.Ītkinson, T.C., 1983, Growth mechanisms of spe- leothems in Castleguard Cave, Columbia Icefields, Alberta, Canada: Arctic and Alpine Res., v. 123–135.Īllen, J.R.L., 1972, On the origin of cave flutes and scallops by the enlargement of inhomogeneities: Rass. This process is experimental and the keywords may be updated as the learning algorithm improves.Īcaroglu, E.R., and Graf, W.H., 1968, Sediment transport in conveyance systems, 2:the modes of sediment transport and their related bedforms in conveyance systems: Bull., Int. ![]() These keywords were added by machine and not by the authors. Calcitc is predominant and the most significant for paleo- environmental reconstructions. More than 100 secondary minerals are precipitated in caves. Both may display solutional scalloping or a paleoflow indicator, or may be modified or destroyed by breakdown.Ī variety of clastic deposits accumulate in cave interiors. Vadose cross-sections are canyon-like or trapezoid. Phreatic passage cross-sections tend to be elliptical but are complicated by differing solubility or armoring of the floor. Many irregular honeycomb caves develop where salt and fresh water mix in the coastal zone. Some large caverns may develop where H 2S-rich waters are oxidized. ![]() Caves formed by CO 2-rich thermal waters display distributary dendritic or 2-D or 3-D maze forms. Two-dimensional joint-guided mazes of passages develop as anomalous portions of common cave systems or as separate caves, due to artesian confinement or diffuse input or to rapid flooding. Many caves are multi-phase features with sequences of levels. On the long profile, caves may display drawdown or invasion, vadose morphology, and shallow, deep, or mixed phreatic morphology. Thus, patterns are not precisely predictable. Their plan pattern building is governed by hydraulic gradients in penetrable fissures, complicated by reorientation of gradients when initial conduits connect and by microfeatures of the fissures. Thousands that are of explorable dimensions are known the greatest contain more than 100 km of accessible galleries or are more than 1000 m deep.Īpproximately 80% of these caves were created by meteoric water circulating without unusual geologic confinement these are common caves. A dissolutional cave or cave system is defined as a solution conduit of 5 to 15 mm minimum diameter that extends continuously between groundwater input points and output points.
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