The Lead Smelting Mills of Yorkshire - Part I, Airedale, Wharfedale and Nidderdale, 1948, Clough R. T.

The Lead Smelting Mills of Yorkshire - Part II, Wensleydale, 1949, Clough R. T.

The Lead Smelting Mills of Yorkshire - Part III [a], Swaledale and Arkengarthdale, 1949, Clough R. T.

The Lead Smelting Mills of Yorkshire - Part III [b], Swaledale and Arkengarthdale, 1949, Clough R. T.

The Lead Smelting Mills of Yorkshire - Interesting Kettlewell Data [a], 1950, Balderson J.

The Lead Smelting Mills of Yorkshire - Interesting Kettlewell Data [b], 1950, Balderson J.

The Lead Smelting Mills of Yorkshire - Part III [c], Swaledale and Arkengarthdale, 1950, Clough R. T.

The Lead Smelting Mills of Yorkshire - Part III [d], Swaledale and Arkengarthdale, 1950, Clough R. T.

The Lead Smelting Mills of Yorkshire - Comments and Notes [Kettlewell], 1950, Clough R. T.

A possible mechanism for growth of calcite speleothems without participation of biogenic carbon dioxide, 1982, Dreybrodt W,

Using Plummer et al.'s [11] rate equations on the dissolution and deposition of CaCO3 in H2O---CO2 systems, we have calculated deposition rates of CaCO3 to stalagmites in caves which are covered by glaciers or bare karst. In this case no biogenic CO2 from vegetated soil is available and the deposition of CaCO3 involves only atmospheric CO2. The mechanism of deposition proceeds by a temperature effect. Cold melting waters of about 0[deg]C dissolve CaCO3 under open system conditions at the surface of the rock. When this solution saturated with respect to CaCO3, flows through the limestone rock its temperature increases by several degrees. Therefore, it becomes supersaturated, and CaCO3 is deposited under open system conditions in the warmer cave. Maximal growth rates of about 10-3 cm/year are possible. From the kinetics of the deposition of CaCO3 from the thin water films present at the surface of stalagmites we are able to estimate the isotopic composition of carbon in the CaCO3 deposited on the stalagmites to be approximately [delta]13C = %, which is close to some observed values.From our data we conclude that substantial growth of stalagmites is possible during glacial periods as well as in areas of bare karst, a question which was not resolved up to now

Le rôle des héritages quaternaires dans les karsts alpins : le cas des Alpes du Nord, 1984, Chardon, M.

THE PART OF THE QUATERNARY INHERITED FEATURES IN THE ALPINE KARSTS: THE EXAMPLE OF THE NORTHERN ALPS - In the western part of the Alps, limestone mountains have been built mainly during Miocene and Pliocene. The relicts of pre-quaternary alterations or karstifications are scarce and difficult to identify. The most part of the morphological features can be related to the quaternary glacial stages. The main landforms of the high and low alpine mountains are described. The glaciers and their melting waters have excavated deep gorges-valley and caves.

Approche géomorphologique des karsts du gypse de la Vanoise (la zone alpine et glaciaire du vallon du Fruit-Gébroulaz,Alpes), 1991, Chardon, M.

GYPSUM KARSTIC LANDFORMS IN VANOISE: the alpine and glacial valley of Vallon du Fruit-Gébroulaz (Alps, France) - In the inner part of the northern french Alps, the higher regions of the Vanoise offer outcrops of Triassic gypsum of which the surface and thickness vary. In the “vallon du Fruit”, the “Gébroulaz” glacier partially covers a long strip of gypsum, which reaches its highest point at the “Roc de la Soufrière” (2940 m). Rivers and springs in the “vallon du Fruit” are fed both by sub-aerial glacial outflows and by karstic underground flows, which are pro-glacial and sub-glacial. A very low chemical dissolution exists under the glacier and along the fast pro-glacial underground and sub-aerial flows, whereas the rate of karstic denudation is high in the margin of the glacier where it reaches 1500 mm/ky at around 2500m (1 ky = 1000 years). The formation and evolution of the dolines is rapid and occurs through underground sucking and dissolution once the area is deglaciated, thanks to underground active flows fed by the glacier and snow melting. Gypsum domes are uplifted under the effects of neotectonic movements and postglacial decompression brings about considerable superficial fissuring because of the elasticity of the rock. Over 10,000 years, the morphogenesis of these domes in the humid and cold climatic conditions of these high alpine mountains has transformed them into “perforated ladle” and domes. Small outcrops are changed into monoliths or gypsum inselberg. A model of the geomorphologic post-glacial evolution of these domes, over some 20,000 years, is proposed.

Contribution to geomorphological and hydrogeological study of karst in Mediterranean environment: the Aït Abdi plateau (central limestone High Atlas, Maroc),PhD thesis, 1995, Perritaz, L.

The Ait Abdi karstic plateau is located in the heart of the calcareous High Atlas (32°N/6°W). With an area of 160 km2, it is situated between 2,200 and 3,000 meters above sea level, i.e. 800 meters above the nearest valleys and canyons. It consists of a large series of massive Bajocian limestones which form a large brachysyncline, the axial plane of which dips gently to the NE. These limestones overlie a thick series of Toarcian-Aalenian detritic sediments forming the regional aquiclude and the top of the half captive Middle Liasic aquifer. The plateau is limited both in the N and S by strong changes in dip to the vertical of the sedimentary layers (ejective thrusted anticlines), and in the W and E by deep canyons created by major rivers. Therefore the plateau is a totally isolated calcareous compartment, from both a morphologic and a hydrogeologic point of view.
The climate of this region is Mediterranean with an altitude modification: maximum rainfall occurs in winter and in spring, snow cover is not durable but sometimes important, storms are common for dry season in summer. The precipitations comprise only 500 to 700 mm/year (subhumide zone) and the effective evapotranspiration is approximately 400 mm/year, including the losses due to sublimation. The snow coefficient is 60 %. This means that the recharge of the aquifer, occurring almost entirely during snow melting, is limited, but the large bare surfaces of the plateau with typical well developed karst forms (dolines, poljes, dry valleys, holes) improve the infiltration rate (40%). The specific discharge is only 8.1 L/s/km2.
The morphologic peculiarity of this nival karst consist of a succession of small parallel and asymmetric dry valleys forming some "waves". For that reason, the French geomorphologist Couvreur termed these climate controlled features "karst en vagues". The role of wind and snow in the genesis of these forms is predominant. The most of time structure controlled plateau's poljes are quasi inactive today. All kinds of high mountain karren landforms are present on the plateau and prove the great role of snow role in the microforms genesis.
An ancient speleological network with vertical shafts occluded lower down suggest of ancient more humid climatic conditions. U-Th dating indicates ages between 3,200 and 220,000 years, or outside the range of the method (more than 400,000 years). The lateral flow is conducted by an interstrata network, inactive and dry in the upper part, or active and phreatic at the base, near the regional aquiclude, attesting three karstification phases.
The water discharges as typically karstic hillfoot springs, most of the time oversaturated and forming tufas. Large doleritic vertical dykes cut the plateau and form major drainpipes. The physical-chemical and chemical signature of these spring waters is quite different of the signature of other springs of this area, which discharge whether from small local Toarcian-Aalenian aquifers or from the huge semi confined karstic Middle Liasic aquifer. The plateau springs hydrodynamic response is characteristic for an elevated karstic aquifer with rapid flow. The aquifer geometry does not allow important reserves, but the mean discharge from all perennial springs (about 1 m3/s) is a precious resource for the population of this far area of the Atlas Mountains.

Le “karst en vagues” des Aït Abdi (Haut-Atlas central, Maroc), 1996, Perritaz, L.

The Aït Abdi plateau (2200-3000 m, 160 km2) is located in the calcareous High Atlas (32? N). It consists of massive Bajocian limestones, which form a large brachysyncline and overlie the clastic Toarcian-Aalenian forming the regional aquiclude and the top of the half captive Middle Liassic aquifer. The rainfall comprises only 500 to 700 mm/yr and the effective evapotranspiration is about 400 mm/yr with a snow coefficient of 60 % and an infiltration rate of 40 %. This means that the recharge of the aquifer mainly occurs during snow melting. The morphology of this nival karst consists in a succession of little parallel and asymmetric dry valleys forming some "waves" ("karst en vagues"). The role of wind and snow in the genesis of these forms is predominant. An old cave system with vertical shafts occluded lower down is proof of ancient more humid climatic conditions. U-Th dating methods on speleothems indicate ages between 3,200 and 220,000 yrs, or more than 400,000 yrs. The horizontal transfer is made by an interstrata network, ancient and dry in the upper part, or recent and phreatic at the base, near the regional aquiclude, attesting three karstification phases.

Formation des réseaux karstiques et creusement des vallées : l’exemple du Larzac méridional, Hérault, France, 1997, Camus, Hubert

The Causses and mediterranean Garrigues present a long continental evolution from late Cretaceous. The karstic network analysis and the dynamic study give geomorphological indicators to reconstruct the paleogeography of this area when the geological indicators are not present. The paleoclimatic action and the tectonic movements make the actual landscape melting a lot of ages and genesis different elements. The endokarst preserves sedimentological and paleoclimatic witnesses and also hollowing shapes that traduce the successive steps of the paleogeographic evolution. The network's levels of the South Larzac are connected with the landscape karstic forms : poljes, canyons, peripheric valleys. The reef limestone of the Seranne and the dolomite of the Monts de St-Guilhem explain this good conservation of the endokarst and of the landscapes.