Direct Measurment of the Rate of Erosion of Cave Passages [Summary Only], 1968, Hanna F. K. , High C.

Biological erosion of limestone coasts, 1968, Neumann A. C.

A Study in Jamaica - Micro Erosion Measurments made in Jamaica in 1967, 1969, High C. , Hanna F. K.

A Study in Jamaica - The Solutional Erosion of Limestone in the Area around Maldon and Maroon Town, St. James, 1969, Smith D. I.

Erosion in the Limestone Stream System - some recent Results and Observations, 1969, Newson M. D.

Cooleman and Right Cooleman Caves, Kosciusko National Park, and the Shift of Risings, 1971, Jennings, J. N.

The Cooleman-Right Cooleman system is an abandoned, nearly horizontal outflow cave of shallow phreatic nature, modified by breakdown. It lies just inside and parallel to a gorge wall of Cave Creek. This relationship, and others like it here, are attributed to a greater water input into the limestone along the lines of dissection of Cooleman Plain rather than to the mechanical effects of slope retreat such as Renault has favoured. This outflow cave has been replaced as the major rising of this karst by the Blue Waterholes a short distance down valley; shallow incision of the valley has accompanied the shift of the rising. This down valley movement does not seem to be explicable by removal of overlying impervious beds in this direction to expose more limestone but by a displacement of the main artery feeding the risings in the course of the deepening of underground karst development as a result of incision. However, this displacement is not more favourable to the emergence of the underground drainage of the Plain as a whole. The downstream shift of the rising therefore remains problematic. Discussion favours interpretation of Cooleman Cave entrance as a secondary breach into the outflow cave previously emerging at Right Cooleman entrance, aided by lateral erosion of the surface stream, but it is recognised that the evidence is far from conclusive.

Seminar on Karst Denudation - Some Notes on Chalk erosion in Denmark, 1972, Aub Conrad

Seminar on Karst Denudation - The Merits of a Hydrological Bias to Karst Erosion Studies, 1972, Newson M. D.

Seminar on Karst Denudation - Opening Address : A Brief analysis of problems in Karst Erosion Studies, 1972, Panos Vladimir

Seminar on Karst Denudation - Quantification of Limestone erosion in Intertidal, Subaerial and Subsoil Environments with special reference to Aldabra Atoll, Indian Ocean, 1972, Trudgill S. T.

Black Phytokarst from Hell, Cayman Islands, British West Indies, 1973, Folk Rl, Roberts Hh, Moore Ch,

Erosion by filamentous algae, comparison with ordinary karst, scanning electron microscopy, Bluff Limestone

Evolution of the Wellington Caves Landscape, 1973, Francis, G.

Wellington Caves, New South Wales (figure 1), have attracted scientific attention for more than a century, largely through discoveries in the cave sediments of bones from extinct animals. These bone discoveries provided impetus for a number of early speculations about the geomorphology of the caves area and its relationship to the caves. Notable among these was the conjecture of Mitchell (1839) that the valley floor sediments of the Bell River and the cave fills had been deposited during a marine transgression about one million years ago. The first systematic geomorphological work was carried out by Colditz (1943), who argued for two distinct relict erosion levels in the Bell Valley; the older level was assigned to the Lower Pliocene and the younger to the Upper Pliocene. Colditz considered that these levels provided evidence for two phases of uplift in late Tertiary times. More recently Frank (1971) made detailed studies of the cave sediments, and devoted some attention to landscape evolution. He believed that the Bell River had been captured by Catombal Creek, during the late Pliocene or early Pleistocene.

Karst processes of the eastern upper Galilee, Northern Israel, 1974, Gerson R,

Karst processes dominate most of the geomorphic activity in the Upper Galilee, consisting mainly of dolomites and limestones. Study of the chemical evolution of water passing through the karst hydrologic cycle clearly shows that the major portion of its carbonate solute is gained subaerially and in the upper part of the vadose zone. Most cave and spring water is already saturated with respect to aragonite and calcite.The karst depressions typical to surface morphology are mostly associated with fault-line traces. Their evolution is possible mainly in areas sloping initially less that 5[deg].The absence of evolved caves, representing well-developed karst of an earlier period, is attributed mainly to the marginal climate throughout the past combined with tectonic, and hence hydrologic, instability of the region.The discharge of the karst prings shows clearly dependence on annual precipitation, with a lag of about 2 years of the response to drought or more humid periods. Long-term fluctuations are larger in the smaller T'eo Spring than in the affluent 'Enan Springs.Most of the denuded material is extracted from the region as dissolved load via underground conduits and only small amounts as clastics. Mean long-term denudation is approximately 20 mm/1000 years, averaged for the surface area contributing to the springs.In spite of the above, most topographic forms are shaped by runoff erosion, active during medium to high intensity rainstorms. Solution processes prevail during low to medium rainfall intensities, while different parts of the region are denuded at similar rates. Even in karst depressions, erosion becomes dominant after their bottoms are covered by almost impervious terra-rossa mantle

The dynamics of solutional and mechanical erosion in limestone catchments on the Mendip Hills, Somerset, 1974, Smith D. I. , Newson M. D.

Sedimentary Development of the Walli Caves, New South Wales, 1974, Frank, R.

The sedimentary history of the Walli Caves began with the deposition of finely laminated clay during the latter part of bedrock development in the phreatic zone. After aeration and entrance development, entrance facies accumulated, and this was followed by the deposition of large amounts of fluvial and lacustrine deposits. Episodic fluvial erosion of these deposits then took place, and flowstone was formed extensively during periods between each active erosion phase to produce a striking sequence of suspended flowstone sheets.