Erdkunde Band XVIII 116_

2: and of ? Fig. Dry deep canyon Bregava River (Hercegovina) Contour intervall 100 m. Although this is an old about 1000 its sides are in canyon (relative depth m) very steep spite of younger evolution of the slope. In the a when the river flowed at means higher parts, during period surface, by of differential erosion in the impermeable rocks Bregava River formed Dabarsko polje.

The eroded detritus must, therefore, have been To conclude: Allogen rivers have only cut ca evacuated It a underground. is, consequently, fea nyons in pure limestone, and this kind of valley ture in in a created karst, i.e., region where during is typical for them. More regular features of river its water creation, deeper fissure-circulation of erosion and slope washing appear in regions of took Its flat limestone bottom place. ideally and mixed lithological composition and do not belong are the sudden transition into steep sides further into typical karst scenery. Unusual features of elements that specific disagree with the laws of surface levelling and differently moulded lime river erosion. stone slopes are remnants of a period when the as well as level Valley-like depressions ground climat favoured plane corrosion (Flachenkorro in pure limestone cannot be explained with river sion).We suggest to discontinue the use of the term which can cut into rock. erosion, only canyons this "karst valley" because it was adopted at a time The other must valley-like features be accounted of insufficient knowledge and of a mistaken con for in the corrosion by changes process in different ception of land form development in limestone. climats and under corresponding ecologic condi Moreover, the term is also illogical. tions.

DRY VALLEYS OF THE SOUTHERN PENNINES, With 2 figures Gordon T. Warwick

Introduction similar features are to be found on many porous sandstones and as In the British Isles most attention has been paid conglomerates such Cannock even on to the dry valleys of the chalk of S.E.England, but Chase, Staffordshire and quartzites they are equally important in areas underlain by (Lickey Hills, Worcestershire) and Keuper Marl, limestones of Cambrian, Silurian, Devonian, Car though the latter are usually confined to valley boniferous, Permian and Jurassic age. In addition heads and minor gulleys. In this paper the author Gordon X. Warwick: Dry valleys of the Southern Pennines, England 117

wishes to discuss the nature of the dry valleys cut ing stages in their progressive incision. These into the Carboniferous Limestone of the Southern valleys are flanked by a series of dry tributary Pennines, an area usually referred to as the Peak valleys. Flanking all but the southern side is an District, mainly inDerbyshire but partly in Staf almost continuous rim of escarpments, interupted fordshire. The general account is illustrated by partially on the eastern side by the Derwent examples chosen mainly from the Dove-Mainfold valley. and Lathkill systems. The central plateau is composed of Carbonife Various have been forward to hypotheses put rous limestones of Visean age, for the most part the of One of explain dry valleys S.E.England. well-bedded, pure limestones interbedded locally themost has been that of Reid and popular (1887) with contemporaneous lavas and tuffs and inparts Bull that were (1936, 1940), considering they of the south-east converted in places to dolomite. the colder of the Pleisto produced during periods Nowhere is the base exposed and the limestones cene when this area was to con subject periglacial rest upon an old basement, presumed to consist of of the and the ditions, involving freezing ground Pre-Cambrian rocks, which has been proved to lie of considerable amounts of snow. Chand melting 270 m below the middle of theWye valley floor ler and Fagg stressed the (1909) (1923, 1954) (Cope, 1949). A further 450 m. of limestone lie of retreat in the water importance scarp lowering above the stratigraphic level of the bore-hole table of whilst Sparks and dip-slope valleys, (Wray, 1954). On the western edge of the block Lewis (1957) advocated spring-head sapping as discrete masses of reef limestone are found which the formative for the which bite agent dry valleys have weathered out into upstanding hills and into the chalk of the Chilterns near escarpment westwards the limestones change to a basin facies Hertfordshire. of Pegsdon, Subsequent lowering with thinner limestones and a greater water proportion the table having lowered the outlet of the of shale. Similar reef limestones flank the northern new saps are now into the spring, proceeding dry edge but basin facies are not exposed there. The floors. A similar has been valley origin suggested old bioherms are traversed by major joints which for Rake Bottom on the Hants-Sussex border by are roughly parallel to the surface of themass, and R. J. Small, (1958). Other writers suggest that the these are the commonest locations for caves. The dry systems an valley originated upon imperme limestones are overlain by Namurian shales and able cover which has now been eroded away and sandstones in an unconformable relationship, in the down of the streams lowered cutting major the south-west they can be seen to be banked up the water table in the chalk and led to the regional against old features with at least 150 m. a landscape progressive dessication of the valleys, view sup of relief. Indications that the limestone surface ported Pinchemel Linton over by (1954). (1956) the plateau area was also irregular are given adopted a similar idea to the explain dry valleys by the two outliers of shale shown on figure 1 of the Southern Pennines, and thismode of origin which lie at the bottom of topographic depressions, is favoured the writer. For certain by dry gorges surrounded by higher limestone hills. The cuestas such as the Cheddar Somerset, Gorge, hypotheses surrounding the plateau are formed of coarse sand of cavern collapse have often been put forward, but stones or grits, but in the south only shales seal with little detailed examination of the and ground off the limestone, succeeded in turn by Triassic of typical cave Trueman marshalled plans. (1938) deposits which only make direct contact with the some of the counter an arguments for entirely sub limestone in the south-west. aerial origin for Cheddar F. Bennet Gorge. J. The dominant structure of the limestone is a (1908) put forward the notion that some of the broad dome with an axis running NW-SE, but this dry valleys in the calcareous sandstones of the is complicated on the east a series of anticlines Hythe Beds of Kent were due to solution and sub by and which eastwards and sidence. synclines pitch produce the sinuous eastern outcrop of the limestone. In The the south-west the structure istmore complicated The heart of the area a a is limestone plateau and series of folds and parallel faults swing from which rises abruptly in the south to a general a NW-SE direction to the east of Dovedale into a of 280?340 metres A a height above sea-level. long N-S direction long the Manifold Valley (Par low rises to m. swelling ridge up 50 above the gene kinson, 1950, Prentice, 1951). Some of these ral level forming the divide between theWye and folds were initiated in Lower Carboniferous times Dove drainage systems. The northern part has but the major earth movements occured in the rather relief and a greater somewhat greater alti main Variscan folding in Permo-Carboniferous tude. The shown on 1 have no major rivers, figure times. There has been further folding though cut into the deep valleys plateau surface, though some upwarping is presumed in connexion with traces are of wider valley floors to be found mark the Alpine disturbances. 118 Erdkunde Band XVIII

LEGEND v?^ limestoneboundary ) s^^^^^^^^^il { T" ) LsC" ~^-A l ^ permanentstreams "^^^^1^^^ '"'''^^^/^^-^Tx r~~^ r" temporarystreams ') j^V^I ^ X

' active effluent \ ....}y" '^<- ^n^.... ^AT^^ ^^aT^C . /^ :\ .^?3 active influent iv-J/ <^^,.

? 1. ? ? 1 ? miles C/^^^^, /C^r^^ 01 234 5678km j ^ I ^'^T^'^CVji l) ^\\^^_x /

Fig. 1: Drainage system and dry valley network of the Peak District Gordon T. Warwick: Dry valleys of the Southern Pennines, England 119

The Dry Valley Systems ses through a flooded section to come into day below the main cave mouth. Here some roof The relationship between the dry valleys and light fall may have assisted the formation of Cave the limestone is clearly shown on figure 1, though Dale, but the action of the outflow must a few small dry valleys do occur on the shales. sapping present two con have been as The stream They fall into main categories, the first ? just important. rising here Peakshole Water, flows in a wide sisting of larger tributary valleys, usually on NW valley cut in the shales but bordered on the southern side SE lines which usually grade into the major val a side of limestone seamed with short leys with little altitudenal discordance. The other by valley dales. group is formed of smaller tributaries with few dry branches which often above themain streams. hang The The upper parts of both types of valleys are usual System ly gently graded and in the case of the first group Only half of the main valley is ever occupied often consist of a wide "bowle", oval or circular by a flowing stream and the upper dry part con a or in shape leading to dry valley gorge with sists of an elongated bowl centred upon the village steep, rocky walls and steeper gradient which may of and leading into a dry gorge with or more exhibit one dry knickpoints of varying steep rocky sides. Near the end of this gorge is a cases ? grades of steepness. In a few water may still large cave Lathkill Head Cave, where the river be flowing in the lower part of the valley, fed commences, but this stream gradually loses its a from spring. Except for the northern flank of water supply underground. This may be due in most areas theWye valley, of the catchment of the part to the driving of drainage levels known as are nar major rivers and dry valley systems very soughs (pronounced "suffs") which have per row and the tributary patterns simple. Many of manently lowered the local water table to assist in streams the discordant junctions with the major mining operations. The last quarter of the valley some show valley development below the "hang", is permanently occupied by water from a large are but they very steep. In the tributary dry val rising in its bed and the nearby discharge from a occur leys bare rock walls sometimes below the sough. Although this stream is subject to consi lips of hanging tributaries suggesting spring head derable interference by weirs, it is possible to see or even sapping waterfall scour in some cases. In a fairly extensive low cliff of bare limestone ris are general the valley sides and floors covered by ing above the river on its right bank. Much higher or grass occasional ash woodlands, but in the stee cliffs are to be seen in parts of the nearby Wye per-sided gorges free faces of bare rock occur dale. scree footed by slopes in varying stages of being Although many of the tributary valleys leading colonised by vegetation. Such bare cliffs, locally into the Monyash Bowl are steep, none of them as are most areas known tors, frequent in the of hang above the main valley floor. This feature reef limestone. begins in the gorge section, e.g. Ricklow Dale and On the northern edge of the limestone small the un-named valley immediately south of Lath streams run off the impervious Namurian rocks kill Head Cave on the left bank. This last has a cave some into systems, of which, like the Mani bare wall below the lip of the valley. Barke and Sink at at fold Perryfoot, lie the head of small Scott (1921) described a similar hanging valley blind cut into floor valleys the of dry valley leading into Cales Dale, the next rightbank tribu cuts systems. This off allogenic supplies of water tary valley below Lathkill Head Cave. In the to area water the dry valleys, though in this the lower half of the valley most of the tributary val moves to drain into Noe to laterally the system leys reach the main valley floor or only hang a the east. None of a cave the dry valleys heads into few metres and thismay be due to valley floor in so cave system, that the collapse hypothesis is in filling which has been swept out of the Lathkill a applicable here, though few old spring heads valley. occur a e.g. Churn Hole off Deepdale, right-bank The gradient of the gorge above the cave steep tributary of the middle Wye. A few of the dry ens considerably up to the level of the floor of contain effluent but are valleys dry caves, these the Monyash Bowl. It is cluttered up by large uncommon, Hob Hirst House in Deepdale is one blocks of limestone, whilst the steep sides are The Lathkill commen coarse scree to example. (described below) footed by up 10?20 cm. in length ces at the flow from an cave now active in the side of which is becoming grassed over. Further its above this the valley, point system is dry. At down the valley where the slopes are less steep, a Castleton dry valley hangs above the short gorge patches of scree may be seen and where the grass of at Cavedale the head of which lies the large has been disturbed much finer frost breccia, of mouth of Peak once a resur cm Cavern, powerful 2?3 length is being distributed in stripes down gence but now dry. The present cave stream pas the coarser material. 120 Erdkunde Band XVIII

Immediately upstream from themain rising are is very marked. Many of them such as Redhurst small rimstone pools or gours of tufa, some of Gorge hang precipitously above the valley side up which are becoming grassed over. Further up the to heights of 150 m. or more. In contrast the Black valley there is a much larger tufa dam nearly 2 m. Meadow's Brook a little way upstream comes high backed by silt through which the stream now down to the general level of theManifold Valley flows, choked by vegetation. This again appears as it is fed from shale lands, but its stream normally to be inactive. These forms appear to be connected disappears in its bed between 50?300 m. from the with past discharges of nearby groundwater re junction. Other valleys show progressive adapta leasing carbon dioxide from solution and precipi tion to the lower levels but all are now dry. Only tating calcium carbonate. the lowest of all has a large spring near the river backed by a low bluff above which the valley TheManifold System gradually slopes up to a steep valley head, prob a former head sap. Some six stages in the rejuvenation of this river ably marking spring have been noted, though there are only four in the On the right bank the upper tributaries are all upper part of the valley due to complications in permanent, though the second one after theMain troduced by an influent cave system which still fold crosses into the limestone has a very steep fall takes all the river's flow in dry weather and whose down the valley side from an intermediate level. dismembered remnants cut through at least two of The reason why this does not sink is probably the higher benches near Wetton Mill (Warwick, beacuse the limestone here is very shaley. Below even are 1955). Dry valleys are found on either side of the Wetton Mill the right bank tributaries or main valley with level stretches backed by dry dry intermittent. The former again show very An knickpoints corresponding to the various past lev ing degrees of hang above the main valley. els of theManifold. exceptional dry valley is a feature more like an Unlike theLathkill the headwaters of theMani abandonned channel, which cuts into the erosion to fold drain land underlain by impervious strata flat, c. 20 m. above river level, sub-parallel the been which provide permanent streams which exhibit general valley direction and whose head has considerable variations in their flow. At low cut off by undercutting of the river in relatively water stage the river sinks at Wetton Mill in its recent times. This is the only dry valley which does bed soon after it encounters the firstmass of reef not have a counterpart at a higher level and which a limestone and the bed is dry from there unto the seems to have been initiated at late stage. main resurgence at Ham, a distance of c. 9 km. The un-named valley above the Castern Valley 2 at its a fan along the stream line. The profiles of the left bank of figure has base small, steep-sided coarse tributaries have been drawn on figure 2, in which composed of earthy material and limestone theMani the vertical scale has been exaggerated five times. blocks which is being actively eroded by next The contrast between the last tributary entirely on fold when it has water in its channel. The also has a fan shales (Ecton Brook) and those cut into limestone right bank tributary downstream

500- S/ia/,^^^^ iWl^C, A25"^+^^ 750/M7y^/pf 50^^_ ^>^yi;800l%c^ V*N/ X ^^Y-wi^"^ //75(T / /900 ^^-^l^^z^^ 7oo//i

30 600/ 950^ ?"S ^-^>--^ / S 5 25^^\^ ^ / /MO'J ? /

horizontal distances 0 in thousands of feet

and its left bank tributaries. Fig. 2: Longitudinal profiles of the Lower Manifold (The vertical scale is exaggerated five times that of the horizontal). Gordon T. Vfarwick: Dry valleys of the Southern Pennines, England 121

but that is much lower and flatter since the dry till lies on the shales, and this forms the edge of a valley into which it heads grades more nearly to sheet V2?1 m. thick on the land to the north, but theManifold. Such fans however are not common little till is to be found resting directly upon the features. limestone though occasional erratics have been In general the sides of both themain valley and found over the Hopedale Bowl and in lower the dry valleys are smooth and covered by vegeta Dovedale. tion, but tors are common in the reef limestones. In the upper Manifold valley just below where it Discussion enters the has a limestone, quarrying exposed large A between the on the of fine scree cemented comparison dry valleys deposit angular loosely limestone and the permanent streams on the together on the undercut slope of a great incised Namurian, especially to the west and north of the meander. It has been suggested by Prentice and limestone, reveals a great similarity in the pattern Morris (1959) that this deposit once filled the and texture of the drainage lines. Both show domi whole valley floor, inferring a drying up of the nant NW-SE trends, though this has been dismem river at that The writer does not agree period. bered to some extent amongst the due with this view of but some reduction in dry valleys infilling, to capture. In both cases there are many head the floor space must be Similar valley accepted. water tributaries, downstream, material has been recovered from the simplifying though nearby there are more first order tributaries on the Elderbush Cave, associated with a cold fauna Namurian rocks. This similarity lends support to indicating that it is a frost breccia which is no the view that the drainage was inherited from an longer being formed. impervious cover. The relationship between the hanging valleys The Dove Valley System and the successive stages of downcutting is a fur course across The Dove maintains its the lime ther indication of a progressive lowering of the stone without disappearing underground but all water table. It is possible that variations in the are of its former tributaries from the limestone height at which the "hang" occurs maybe related streamless. Not only has this valley been subject to former variations in the remaining shale cover to the usual multiple rejuvenation but it and its of the headwaters of the tributaries, such as hap tributary valleys have been considerably modified pens to-day in the case of theManifold. When the by river capture (Warwick, 1953). Capture is highest incisions occurred there would be rela presumed to have been caused by spring-head tively little thickness of limestone exposed above recession from a tributary of theManifold (which the shale seal to the south of themass which would had achieved a lower level than the former tribu maintain high water tables. As the major rivers now tary of the Dove, which has been reversed). cut down and the development of solutionally This capture apparently led to several high level enlarged joints and bedding planes speeded water valleys becoming dry. Small straightenings of movements with consequent lowering of the meanders have also produced high level dry water table gradients, more and more streams one near a valleys, farm called Dunge Bottom and would find themselves above the ground water the second occurring below Milldale (situated at level. As the shale cover was removed this would course the double kink in the limestone of the mean that most of the precipitation would be a in no Dove), but only forming semi-circular alcove absorbed directly with run-off and so the valleys the right hand side of the valley. At Milldale would become dry. The prime cause of this was comes another steep-sided dry valley in from the the lowering of the level of the Dove and Mani west a which leads up into large bowl whose lowest fold in the south-west and of theWye and Noe in at is This point Hopedale still floored with shales. the north, these last two rivers being dependent to leads the conclusion that this feature is in large upon the down-cutting of the Derwent. However measure resuscitated from the old limestone shale this last valley is almost entirely cut into Namu unconformity. The higher parts of this bowl on rian strata, except at Matlock in the south-east are a the northside also covered by thin cover of leaving intact the eastern seal of the limestone shale, above which rise higher reef limestone hills. dome except where theWye and Noe have bre A small temporay stream off these shales sinks in a ached it. combined collapse doline and blind headed valley The dating of the various still-stands recorded known as A locally the Dumble Hole. little fur in the Peak District landscape is very difficult, ther the the is a along edge of shale similar dry but most authorities agree that the higher levels are feature and another occurs near to Alstonfield. pre-Pleistocene but most probably post-date the These minor valleys probably carried meltwater disturbances following the Alpine earthmove the Last Glaciation. A thin ments during covering of inOligo-Miocene times. Linton (1956) has 122 Erdkunde Band XVIII

summarized the available evidence to that date, by solifluction action. The fine scree bears witness a or suggesting late-Cretaceous Eocene date for the to these events both in the river and the dry val drainage pattern to be limned out on a Cretaceous leys, and can be correlated with similar deposits in cover. More recently pollen of Pliocene age have cave mouths. It is likely that as condition began to been reported from the fill of a large doline, cut in ameliorate that there would be increased snow-fall the plateau surface. This all supports the view that and higher spring temperatures producing more the earlier rejuvenations and accompanying valley meltwater than previously and that scouring of desication occurred before the Pleistocene with its the valley floors might take place in some of the cold periods. lower valleys. However Pigott has found his undisturbed in some of the The lack of extensive cavern collapse rules that deposits high-level dry floors. abandoned blind such out as a possible source of dry valleys. Some evi valley Small, valleys as those near Gateham and Alstonfield also dence of spring head recession has been found and may date from a snowier this caused the development of certain valleys period. such as the one below Ham and there is some evi The general effect of post-Mindel periglacial on the to have been dence of this occurring to-day at a lower level periods dry valleys appears one of minor modification of fea leaving the old valleys dry above the spring heads. already existing tures. Some of the steep rocky faces below hanging valleys may also have developed in thismanner. Conclusion The greatest difficulty in assessing the part played by Pleistocene climatic changes is the In view of the evidence cited above the author nature scattered of the evidence regarding former is convinced that the majority of the dry valleys glaciations. There is fairly widespread agreement in the Peak District were evolved from a complex was that the region heavily glacierized during pattern initiated on overlying impervious rocks theAntepenultimate (Mindel) Glacial and erratics and that intermittent rejuvenation of the main are over from this district found widely scattered valleys has led to the progressive elimination of a theTrend valley and East Midlands, but growing the tributary valleys. This was due to rapid adjust suspicion that much of the area was free from ice ment of the water table to the level of the Dove, during the Penultimate and Last Glacials apart Lathkill, Manifold, Noe and Wye rivers, below a stream from of ice passing up the Goyt valley the level of the floors of the tributary valleys. This and thence down theWye. Support for this view was probably helped by the short and therefore is lent by the general absence of bare limestone steep gradients of the side valleys, many of which cover stone solutional forms (karren) and the of were left hanging.lt is thought that much of this cm. on less silt-loam 100?150 thick the gentler adjustment occurred before the Pleistocene Period sloping ground discovered by Pigott (1962) which and that periglacial conditions of the later Plei contains wind-borne material derived from the stocene glacial phases only caused minor modifi a Namurian rocks and only thin basal layer of cations to these valleys. It is difficult to assess the matter mineral from the solution of the limestone effect of glaciation by an ice-sheet, though again (c. 1 cm. thick) Pigott has also found evidence itwould appear to have been slight. cover. for festooning in the lower parts of this Linton on (1949) argued morphological grounds Acknowledgements that the area was an enclave unglaeiated during The author wishes to thank Mr. D. W. Oliver a least the Last Glaciation. For these reasons one for the fair of 1 and 2 must look for evidence of modification of the making drawings figures dry and for them and also the Uni these In 1947 photographing valleys during periglacial periods. of for financial assistance after 2 months of hard frost and thick snow cover versity Birmingham towards the cost of fieldwork. (1?2 metres), meltwater flowed on the surface of many of the dry valleys but quickly died away. Birmingham, 17. Dec. 1963 more Presumably such condition would be of fre occurrence the colder Pleistocene quent during References However the limited amount of material phases. F. and A. Scott. 1921. An Unusual Case of associated with such events indicates that it was Barke, Hang ing Valley. Trans. N. Staffs. Field Club, 55, 51?53. not The of the Manifold important. fans Valley Bennet, F. J., 1908. Solution-Subsidence Valleys and - even Beds Area of West have already been cited. It is possible that the Swallow Holes within the Hythe main rivers would cease to flow in winter and Mailing and Maidstone. Geographical Journal, 32, 277? 288. that frost action was strong upon any faces of Bull, A. J., 1936. Studies in the Geomorphology of the the off of the limestone exposed by killing vege South Downs (Eastbourne to the Arun Gap). Proc. Geo tation and the stripping of much of the regolith logists' Assocn., 47, 99?129. N. A. Gwozdeckij: Bedeckter Karst in der UdSSR 123

?, 1940. Cold Conditions and Land Forms in the South Prentice, J. E., 1951. The Carboniferous Limestone of the Downs. Proc. Assocn., 51. 63?71. Manifold Valley Region, North Staffordshire. Quarterly Geologists' ? Chandler, R. H., 1909. Some Dry Chalk Valley Features. J. Geological Society of London, 106 (for 1950), 171 Geol. Mag., Decade V, 6, 538?539. 209. Cope, F. W., 1949. Report of Boring inWood Dale. Abstract Prentice, J. E. and P. G. Morris, 1959. Cemented Screes of Proc. Geological Society of London, 1446, 24. in the Manifold Valley, North Staffordshire. East Mid Fagg, C. C, 1923. The Recession of the Chalk Escarpment. land Geographer, 11, 16?19. Proc. Croydon Natural History & Scientific Soc, 9, 93? Reid, C, 1887. On the Origin of Dry Chalk Valleys. Quar 112. terly J. Geological Society of London, 43, 364?373. ?, 1954. The Coombes and Embayments of the Chalk Small, R. J., 1958. The Origin of Rake Bottom, Butser Escarpment. Ibid. 12. 117?131. Hill. Proc. Hampshire Field Club, 21, 22?30. Linton, D. L., 1949. Unglaciated Areas in Scandinavia Sparks, B. W. and W. V. Lewis, 1957. Escarpment Dry and Great Britain. Irish Geography, 2, 25?33. Valleys near Pegsdon, Hertfordshire. Proc. Geologists' ?, 1956. Geomorphology, Chapter 2 of Sheffield and Its Assocn., 68, 16?38. Region (Editor, D. L. Linton). British Association Hand Trueman, A. E., 1938. Erosion Levels in the Bristol Dis book. trict and their relation to the Development of the Scene Parkinson, D. L., 1950. The Stratigraphy of the Dovedale ry. Proc. Bristol Naturalists3 Soc. 4th series, 8, 402?428. Area, and Staffordshire, Quarterly J. Geolo Warwick, G. T., 1953. The Geomorphology of the Dove gical Society of London, 105 (for 1949), 265?294. Manifold Region. Unpublished Ph. D. Thesis, University Pigott, C. D., 1962. Soil formation and development on of Birmingham. the Carboniferous Limestone of Derbyshire, I. Parent ?, 1955. Polycyclic Swallow Holes in the Manifold Val Materials. /. of Ecology, 50, 145?156. ley, Staffordshire. Actes du ler Congres Internat. de Spe Pinchemel, Ph., 1954. Les Plaines de Craie. Paris. leologie. 2, 59?68.

BEDECKTER KARST IN DER UdSSR

N. A. Gwozdeckij

Weit verbreitet ist die Auffassung L. Sawitzkls lichen Deekschichten von Meeresablagerungen. (1909), der den Karst in zwei Typen einteilt: den Ausgedehnte Gebiete liegen im Siiden und Siid ?Mittelmeerkarst" und den ?Mitteleuropaischen westen von Kislowodsk imNordkaukasus, wo auf Karst" oder den ?nackten" und ?bedeckten" Karst. Strukturterrassen und flachen Talboden Hohlfor Die Begriindung dafiir wurde im Einflufi des men des bedeckten Karst mit lockeremMaterial er Mittelmeer- und Mitteleuropaischen Klimas ge fiillt iiber Kreidekalken entstehen, (Gwozdeckij, sehen. In der russischen Literatur fand diese Ein 1962, S. 143, 1958, S. 133 und 141). Gipskarst mit teilung eine sehr grofie Verbreitung, (Kruber, ihn bedeckenden Meeresablagerungen beobachtet 1915, S. 278; Schukin, 1933, S. 341?342). Der man in der Umgebung des Baskuntschaker Sees in bedeckte Karst jedoch ist eine Folge der Besonder der Kaspischen Niederung, (Gwozdeckij, 1953, heiten nicht nur des Klimas, sondern auch der geo 1954, S. 245?246). Auch in der Russischen Ebene logischen Struktur. ist der bedeckte Karst sehr weit verbreitet, wo die Unter dem bedeckten Karst soil imwesentlichen Kalke, Dolomiten und Gipse oft von Moranen, ein solcherKarst verstanden werden, bei dem was fluvioglazialen und alluvialen Ablagerungen iiber serlosliches Karstgestein von unloslichen geologi deckt sind (Gwozdeckij, 1954, S. 234?235; schen Formationen geschiitzt wird, die genetisch Jakuschowa, (1949). Im ostlichen Sibirien, in an nicht die Karstdecke gebunden sind, also sandig Priangarie, kommt typisch ausgepragter bedeckter tonige Meeresablagerungen, Moranen, fluviogla Karst auf den alluvialen Angaro-Terrassen, iiber ziale Ablagerungen, alluviale Terrassen und ande kambrischen Dolomitensockeln vor, (Gwozdeckij, res mehr. Im Gebiet des bedeckten Karstes fehlen 1952, 1954). Gipskarst mit Moranenbedeckung oberflachliche Auslaugungsformen, jedoch spielt die finden wir auch im gebirgigen Teil Mittelasiens, so von Bildung Trichtern und Wannen eine grofie im Gebirge ?Peter I." und am Fufie des ?Saalais Rolle. Die Hohlformen im Untergrund wurden kij-Gebirges" in seinem 6stlichenTeil'(GwoZDECKij, auf mechanischem Wege mit dem lehmig-sandigen 1957, 1960; Tesauik, 1958, S. 216). Im Gebirge Material der Deckschicht aufgefullt, (Gwozdeckij, ?Peter I." gibt es typisch ausgepragte Vorkommen 1954, Kap. IV, Sokolow, 1962, Kap. III). Wo sich des bedeckten Kalkkarstes mit durchlassigen Trich unter unloslichen Schichten Gips befindet, ent tern, auf alluvialen Terrassen und Schwemmland stehen gleichfalls recht haufig Einsturzformen, die sowie ausgebildete Talboden. sehr typisch fiir den bedeckten Gipskarst sind. Vom bedeckten Karst sind die Falle zu unter Die Verbreitung des bedeckten Karstes ist in der scheiden, in denen das losliche Gestein nicht von UdSSR sehr u. a. grofi. Beispiele dafiir ergeben sich einer nichtloslichen, geologischen Formation be in Verbindung verkarsteter Schichten mit unlos deckt ist, sondern von einer autochthonen Boden