Evolution of Surfaces of Planation: Example of the Transdanubian Mountains, Western Hungary

Geogr. Fis. Dinam. Quat. 21 (1998), 61-69, 5 Itss. 1 tab.

EVOLUTION OF SURFACES OF PLANATION: EXAMPLE OF THE TRANSDANUBIAN MOUNTAINS, WESTERN HUNGARY

ABSTRACT: PECSI M., Evolution of surfaces of planation: example of tut amente interessate da sollevamenti tett onici , subs idenza e stiramenti tbe Transdanubian Mou ntains, W estern Hungary. (IT ISSN 0391-9838, orizzontali. 1998). Secondo questo modello, 10 spianamento di tipo tropicale (etchplana tion) del tardo Mesozoico con la forma zione di paleocarso e di bauxite This model claims that the surfaces of planat ion I once produced by some erosional processes, were reshaped in the later geological period s by non continuo nelle Mont agne Transdanubiane. Com e conseguenza di una repeated , alterna ting erosional and accumulation processes on the rnor complessa subsidenza tett onica differenziata, la maggior parte dei rilievi ph ostructure also repeatedly affected by tectonic uplift , sub sidence and fu ricop erta in vari rnornenti da variamente spesse coltri sedimenrarie. II horizont al displacement. seppellirnento fu perc seguito da una totale 0 parz iale esumazione almeno According to this model , late Mesozoic tropical etchplanation with in tre momenti, nel Paleogene, nel Neoge ne e nel Quatern ario. Durante paleokarst and bauxite form ation did not continue during the Tertiary in questi avvenimenti la superficie di spianamento di tip o tropicale cretacea the Transdanubian Mountains of Hungary. As a consequence of multiple fu interessata da erosione 0 da sedimentazione attraverso processi non ti differenti al tectonic subsidence, most of the range was buried in various picamente tropic ali (quali la perip edim enta zione, la forma zione di terraz thickness and at various intervals. This burial was followed by complete zi marini, la messa in posto di mantelli alluvionali e altri ). Nelle serie degli or partial exhuma tion on at least three occasions (Paleogene, Neogene horst delle Montagne Transdanub iane, sepa rate da bacini tettonici tipo and Quatern ary). During repeated burial and exhum ation the Cretaceous graben, la posizione e l'evoluzione delle superfici consent e ilricon osci tropical etchplain was affected by further erosion or accumulation mento di alcuni morfotipi principali: through non-t ropi cal processes (such as peripedimentation, marine ter 1. supe rfici di spianamento (etchplain ) in posizione sommitale di horst race form ation , alluvial fan building and oth ers). In the horst series of the parzialment e esumati. Transdanubian Mount ains, divided by graben-like basins, the position 2. sup erfici di spianamento ietcbplain) in posizione tett on icamente solle and evolution of the geomor phological surfaces allows the identification vata di horst sepolti. of some main groups: 3. superfici di spianamento ietcbplain) di horst in posizione di soglia tet 1. (semi) exhumed horst of etchplanation in summit position; tonic a, sepolti 0 esum ati, e rimodellati, frequ entemente interessati da pro 2. buri ed horst of etchplanation in uplifted position; cessi di pedim entazione. 3. horst of etchplanation in thr eshold positi on, buried or exhumed and 4. superfici di spianamento ietchplainssepolte in corrispond enza di bacini. reshaped, mostly pedimented; 5. peripediment , pedim ent in roccia , localmente sepolti da copertura 4. buried etchplain in basin position; detritica. 5. perip edim ents , rock pediments, locally buried under detritus. II modello dell'evoluzione delle superfici geomorfiche att raverso pro The model of geomorphic surface evolution through alternating ero cessi alternati di erosione e sedimentazione puo non soltanto essere appli sion/accumulation does not only apply to the Hungarian medium-height cato alle Monta gne di media altezza dell'Ungheria, rna anche a molte altre mountains, but also to num erous oth er geomorphological regions, egothe regioni, quali le catene Alpin e, Carpatiche e Din arich e, a molte vecchie Alpine-Carpathian-Dinaric Mounta ins, several old mountains Jnd massifs mont agne e massicci dell'Europ a e degli altri continent i. of Europe and other continents. . TERMINICHIAVE: Tardo Mesozoico,Superficie di planazione, Seppel KEY W ORDS:Late Mesozoic, Surface of planation , Burial, Exhum a limento, Esumazione , Sup erfici policicliche. tion, Polycyclic surfaces.

RIASSUNTO: PECSI M., Evoluzione delle superfici di spianamento: l'e INTRODUCTION sempio delle Montagne Transdanubiane, Ungheria Occidentale. (IT ISSN 039 1-9838, 1998). The term geomorphological sur/aces denotes plains and II modello ritiene che le superfici di spianamento , gia prodott e da va ri processi erosivi, vengano rimodellate in piu tardi periodi geologici da gently sloping slopes, which are the products of erosion, of ripetuti , altern i processi di erosione ed accumulo su morfostrutture ripe- accumulation or of their combination, under the influence of tectonic processes. Their formation may be dated from their correlative sediments or by other methods. (,0,) Geographical Research Institute, Hungarian Academy ofSciences, For the timing of successive formation of landforms, P.o.B. 64 H-1388 Budapest, Hungary. i.e. for a reconstruction of the denudational chronology, an

61 interpretation of the different geomorphological surfaces is geomorphological surfaces are the oldest, the lower ones needed. Several models were proposed for the develop are ever younger. Such presumptions might only be valid ment of erosional surfaces (landforms) on great continental for a part of the cases and for some geological times. Pre morphostructures. Some of these have become classic (Da sumably the planation surfaces (models 1 to 5), explained vis, 1906, 1922; Penck, 1924; King, 1949, 1962; Biidel, by different processes, might be attributed to effects of as 1957 and his followers , Bulla, 1958; Bremer, 1986). many different geographical environments. If this is true, 1. According to Davis, the peneplain (ultimate peneplain) is the final each of these models and conceptions generally represent product of fluvial erosion on different humid regions. The almost plane genetically and climatologically different morphofacies sur/ace is the penultimate ph ase of the planation at the base level ", rather than one single, global type of surface. It must be 2. Penck's Primarrumpf (primary peneplain) J is a plain surface just emerged above the sea level. Piedmonttreppen (piedmont benchlands) are mentioned that these early models of planation surfaces explained by fluvial erosion and retre at of valley sides. Erosional surfaces were based on fixist tectonism. on slowly but uniformly elevating morphostructures may be explained In this presentation we want to introduce a polygenetic this way. model of geomorphological surface evolution, through 3. According to King, pediplanation also takes place by the retreat of slopes on slowly but continuously elevating terrains, especially under processes acting on different morphostructures affected by semiarid climates, where the rate of the mechanical weathering exceeds plate tectonic events, particularly in orogenic belts. The tha t of the chemical one. Retre at of slopes results in a gradual surface units studied were horizontally displaced over great dis lowering and pediplain form ation. According to King, pediplanation 4 is tances , tectonically dismembered, recurrently uplifted and the most widespread process reducing relief, this way it replaces Davis' pen eplain theory. subsided, thus the planation surface became repeatedly 4. Biidel proposes that the double etchplain s (doppelte Einebnungs buried, elevated and exhumed again (Pecsi, 1970a,b). Pol flache ) is an erosion surface created by intensive lateritic deep weathering ygenetic morphostructures with planation surfaces, which and strong wash down (stripping) of the thick weathered rock under a were shaped under the influence of alternating erosional seasonal dry and wet tropical climate. 5. A pediment is a gentle erosional foothill slope in front of a steep moun and depositional processes of long duration, were removed tain slope, generally formed of hard rock . Pedimentation is admitted to be from their original place and carried over long distances, the most general erosional, planation process. Mcgee, (1897) believes that passing under various climatic belts. This way units of a river, on leaving a mountain, deposits most of its load , while the rest of most different genesis might have come in each other's the sediment transported causes lateral planation (corrasion). The pedi ment is covered by a thin layer of sediment, deposited by sheetwash or by proximity. small rivers under a semiarid climate. The tectonic and geomorphic history of the Transda nubian Mountains (Western Hungary) was used as a mod Several researchers adhere to the above models for the el for the evolution of such polygenetic planation geomor origin of sur/aces 0/ planation, while others criticise or phological surfaces. Geological and geomorphological modify them. In one respect these models are uniform, studies of the last half century served as a basis of a new they suppose that the studied surfaces were formed during geomorphological evolutionary model, differing from the long geological times, when uplift was slow, continuous or previously mentioned ones (Pecsi, 1968, 1975, 1993; periodical. It is generally admitted that the highest situated Szekely, 1972).

~ Hungarian B k Mt Hungarian Gr~at Plain NW .-Little Plain ---f----- a 0 ny s SE Tel·2 Dudar FOle

-1000

·- 2000

-3000 ------" 01 1::::::::::::::(:12 [-:-:]3 EJ4 !~~m5 1illIIIIllI6 1""17 o 5 10km -4000 ~9 ~10t::=::=311QB112D13~14 '~15 .8 .- 5000

FIG. 1 - Profile across the Bakony Mountains (after Wein & Pecsi ). 1) Holocene-Pleistocene fluvial sand and gravel, alluvial plain; 2) Upper Pannonian sand and clay; 3) Lower Pannonian (Miocene) claymaris; 4) Lower Miocene-Upper Oligocene gravel and sand (in the Dudar Basin); 5) Eoc ene coal seams and carbonate rocks; 6) Lowe Cretaceous (Aptian, Albian and Cenomanian) limestones and calcareous maris; 7) bauxite and related formations; 8) Jurassic limestones; 9) Upper Triassic dolomites and limestones; 10) Middle Triassic limestone; 11) Lower Triassic siltsstone, marl and limestone; 12) Permian sand stones and conglomerat es; 13) Upper Carboniferous granite porphyry; 14) Lower Carboniferous conglomerate and shale; 15) Silurian Devonian ph yllite and marble; t) uplifted remnant of tropical etchplain; fr) buried etchplain; e) exhumed etchplain, locally covered with Miocene grav el; pe l mountain margin benchland; h2) Pannonian marine terrace; hi) piedmont surface (pediment); g) Pleistocene piedmont surface formed on moder , , ) ately consolidated sediments (glacis); k) remodelled tropical etchplain in threshold position; Tet-Z) prospect drilling; SoD) Silurian-Devonian ; T I T2 T3 Lower, Middle, Upper Triassic; M) Miocene; PII) Lower Pannonian (Upper Miocene); P12) Upper Pannonian (Upper Miocene).

62 DISCUSSION with karstic planation. Witnesses of this marked tropical karst planation were buried and preserved by Lower Cre The Transdanubian Mountains (TM) is a low range of taceous (Albian), upper Cretaceous, and , locally, Paleo slightly folded structure, built mainly of Mesozoic and Pa gene sediments in the TM. leogene carbonates (limestone and dolomite), affected by Buried surfaces of karstic planation may be found be overthrusts and faults . Horst and graben structures are tween horsts, forelands and on horsts, buried with Creta common, delimited by mainly NE-SW and NW-SE run ceous or Tertiary strata (figs. 2 and 3). ning structural lines. In the southern foreland a thick Pale The tropical karst planation surface of the TM was ozoic sequence of south Alpine affinities underlies the sim slightly remodelled between the Late Cretaceous and Mid ilarly thick Mesozoic strata (fig. 1). Comparative structural dle Eocene (Laramian tectonic phase?). On horsts summits investigations proved that the TM was a part of the carbo it was well preserved, but on the margins pediments were nate platform formed at the northern margin of the Afri formed due to early Eocene sub arid coarse clast produc can plate in the southern Teth ys, during the Triassic . Dur tion. Dolomite karst towers and bauxites , if not buried, ing the rifting and subsequent convergence of the Tethys were eroded or resedimented. this unit was overthrusted on an oceanic crust fragment, During Middle and late Eocene the area of the TM be the Penninic unit. The TM, as a part of a microcontinent, came an archipelago. Most of its territory subsided contin was subsequently carried into the southern Alpine area , uously , but not uniformly. The sea inundated the low wherefrom, in late CretaceouslPaleogene times it was hori horsts and intramontane basins. Bauxite bearing karstic zontally shifted into the Carpathian basin (H orvath, 1974; surfaces of etchplanation were often buried during the Eo Geczy , 1974; Wein, 1977, 1978; Balla, 1988, Hamor, 1989; cene. Bauxite lenses in sinkholes, capped with Eocene FUlop, 1989; Stegena & Horvath , 1978). layers, are often interpreted as a result of a continuation of During the late Triassic and Early Jurassic the low and tower-karst plain formation and bauxite genesis in the first extended carbonate platform of the TM was cut into a part of the Eocene (Bardoss y, 1977; Mindszenty & alii, horst and graben structure. In the grabens the sedimenta 1984). This would mean that such bauxites are not merely tion went on during the Jurassic and early Cretaceous. On products of Eocene redeposition of earlier deposits. We the elevated parts a long lasting continental downwearing think, however, that early Eocene conditions characterised went on du ring the Jurassic and Cretaceous. The upper by dolomite breccia formation were not favourable for Triassic carbonates were affected by tropical karstification, bauxite genesis and tower karst evolution. Under a suba accompanied by bauxite formation. Cockpits and tower ridic climate predominantly coarse clastics were formed karst may have been formed under tropical savanna cli and transported by ephemeral water-courses and pedimen mate with humid and dry seasons, simultaneously with tation prevailed (Pecsi, 1963, 197Gb). bauxite formation. The initial sediments of the bauxite for From the Eocene-Oligocene boundary the TM was up mation were resedimented from siliciclastic areas by sheet lifted and the previously submerged and buried parts were wash and by small rivers. Lateritification was simultaneous eroded. Some segments or entire horsts were exhumed and

WNW ~! m E G °1 SOD bauxit atGanl Velence Hill 400

300

200._100 7Q o

-100

-200

FIG.2 - Geomorphological surfaces in the Vertes Mountains in Hungary. A) exhumed horst in summit position, a remnant of slightly remodelled Creta

ceous etchplain; C) horst in foothill position; C1) totally buried; C3) totally exhumed; D) buried surface of etchplain in intermontane graben position; D 1) intermontane graben, filled with molasse and alluvial fans; E) glacis d'erosion with terraces ; E 1) rock pediment and glacis d'erosion; F) remnants of marin e terrace (Upper Pannonian); G ) subm ontane basin with river and glacis terr aces; t l -t4) fluvial terraces; rnt.) marine terrace; 1) alluvium and mead ow soil; 2) alluvial fan; 3) loess and loess-like sediments; 4) Pannonian sand y and silty formations; 5) Sarmatian formations; 6) Miocene gravel and sand; 7) Oligocene sand and clay form ations; 7a) Oligocene lignite; 8) Eocene limestone; 9) Cretaceous bau xite; 10) Triassic dolomite and limestone; 11) granite; 12) Carboniferous metamorphic rocks.

63 E w o I----_+___ Budakeszi Basin Szabadsaq Hill Martinovics Hill

0 2km I ! I ,

Q2~2 Pl2~3 M:l~4 0:3 5 ~ 6 QD' t -:.--.-] Ozl- 1 30, ffJIJIJI)/ hOI DB EillIIIIIIl9

bE0Kl .C"E [];[]11 2TN~12 4T k~ OTk~14 I Tk~ 15 RTk Wi/ltd 16 411 ~- - 17 2 TI ~• • 18

FIG. 3 - Alternating erosional/accumulational planation surfaces of the Buda H ighland in Hungary (after Pecsi & Wein). B) buried Cretaceous etchplain in uplifted position; C) surfaces of planation in uplifted position: 1) totally buried, 2) partially exhumed, 3) totally exhumed; D ) buried surfaces of pla nation in grabe n position; E) glacis d'erosio n; 1) Pleistocene loess and wind blown sand ; 2) Pleistocene travertine; 3) Pliocene sand, clay, travertine; 4) Sarmatia n conglome rate. and limeston e; 5) Up per Oligocene sandy clay, silt; 6) Middle Oligocene clay; 7) Lower Oligocene marl; 8) Lower Oligocene sandsto ne; 9) Eo cene forma tions; 10) Eocene reworked bauxite and conglomerate; 11) Eocene acid dyke; 12) Upper Triassic Dachstein Limeston e; 13) Upper Triassic H auptdolomite; 14) Upper Triassic coarse dolom ite; 15) Upper Triassic cherty dolomite; 16) Upper Triassic marl, limestone, dolomite; 17) Middie Triass ic pink dolomite; 18) Middie Triassic Diplopora-bearingdolomite.

subsequently pedimented. Th ere are several horsts, where During the late Miocene by the Sarmatian and P anno bauxite and tropical tower-karstic surfaces were preserved nian transgression (ca 13 to 11 Ma BP ) the TM subsided under a thick Eocene limestone cover (fig. 3). again, but adjacent regions to the south and north (Little During th e second part of the Oligocene the horizontal Plain and Transdanubian Hills) were sub sided at higher shift of the TM was going on , its subsidence was highly rate thus the TM remai ned a mainland or an archipelago ( differentiated. This is supporte d by the fact that sediment s Jambor, 1989). Some mountain groups, marginal horsts of differing facies (coars e clasts, gravel, sand and clay) and intramountain grabens were buried , in fact , for the were de posited on th e surface of the TM, which moved third or fourth time during the Terti ary, under P annonian eastward. The sediments originating from some higher, sands and freshwater limestones, at an elevation close to crystalline mountains in the vicinity. th e base level. During the late Miocene th e majority of During th e Miocene (from 24 to 5.5 Ma) the relief of horsts in the TM were at an elevation of 100 to 200 m the TM and its close environs changed repeatedly and fun abo ve the Pannonian lake level. Due to th e uplift and cli dam entally in cons equent tectoge netic phases, horizontal mate turning from subhumid to semia rid, pedimentation and vertical displacem ents, subduction, a powerful volcan processes int ensified along the margins of ho rsts for short ic activity, partial transgressions and regressions. Th ese periods (eg. at the Sarmatian-Pannonian boundary). Mor processes resulted in a geomorphological inversion at the phological evidence of deflation are wind-abrade d and end of the Miocene . Th e Mountains was uplifted to a mod poli shed rocks , sand blankets, iron-varn ished pebbles, erate altitu de, but definitely over its surroundings, for the iron-oxide con cretions, meridional valleys and ridges (yar first tim e during the Terti ary. On its sinking north-eastern dangs), which were formed during the late Miocene. part andesitic volcanoes erupted during the middle Mio H orsts uplifted during such per iods and especially at the end of the cene (15-14 Ma BP ). Deposition of terrestrial gravel and Pannonian were stripped off a cover of Oligocene and Miocene clastic other clastics continued on the margins of planation sur sediments.In some spots marine shelves were formed, preserved by tra vertine deposits (fig. 4). The horizont al displacement of the TM into its faces, with som e interruptions. recent structura l position lasted from the end of the Oligocene (Baldi, On some low-lying Mesozo ic horsts and in intr amountain small ba 1982; Hamor 1989) to the middle Miocene (12-10 Ma BP, Balla, 1988, sins the remn ants of etch plains were newly but incompletely buried dur Kazmer , 1984), when the subsidence of the Pannonian basin started. ing the late Tertiary. On tecton ically uplifting horsts the old tropical From about this time tecto genet ic processes caused repea ted subsidence karsts were exhumed and remodelled. and uplift of the horst groups and grabens of the TM , upward movements

64 dominated . This resulted in form ation of marine terraces, deltaic depo sits elevation of different geomorphological levels are decreas and erosional foothill slopes on marginal parts of the mountains. ing toward the forelands and basins (Pecsi & alii, 1988). In the Danube bend, near Visegrad, the Mesozoic sur At the beginning of the Pliocene (5.4 Ma BP) uplift in face of the TM lies about 1-1.5 km below the sea level, tensified. From the late Miocene on the climate shifted to a covered by thick Oligocene to Middle Miocene epiconti subhumid one. In consequence, a considerable part of the nental molasse-like deposits. Volcanic rocks of the Tertiary siliciclastic, gravel, sand cover of the TM was Viscgrad Mountains and , partly, of the Borzsony Moun eroded and redeposited on the forelands. On the uncon tains , cover thick middle Miocene (Badenian) sandy de solidated molasse like sediments a broad hillfoot surface posits (juhasz & alii, 1995). Along the Danube Bend there took shape, while in the forelands wide alluvial fans were is a Tertiary molasse corridor, where these volcanic moun deposited. The hot subarid climate was interrupted several tains formed during a rather short time, between 15 and 14 times and followed by sub humid warm periods. This in Ma BP. This young volcanism along the molasse trough creasingly favoured the cyclic development of red and var could hinder but not prevent the flow of the Paleo iegated clays. Danube the carrying water and sediment of confluent riv Neither the considerable time span of variegated and red clay forma ers from the foreland of the northern Alps , the eastern tion nor the cause of the subhumid climate has been investigated in de Alps and western Carpathians towards the Great Hungari tails. Th e effect of the se events on the morphological evolution also needs further studies. an Plain. Consequently, the Paleo-Danube most probably acted as a morphological and sedimentation agent in the In the Bakony Mts. (western TM) basaltic tuffs and la molasse trough between the Buda-Pilis Mts. and Naszaly va were deposited over late Miocene and Pliocene foothill of the TM. Thus, the Miocene quartz-pebble containing surfaces. The basalt-capped mesas are witnesses of the re delta remnants, high valley foothill surfaces and half plains moval of about 100 to 200 m thick Pannonian sequence. of planation may be interpreted on the volcanic build-ups Neogene and Quaternary geomorphological surfaces around the Visegnid-Gorge. (Miocene marine terraces, delta gravel deposits, Pliocene foothill surfaces, Quaternary terraces and alluvial fans) were often preserved by hard travertine deposits capping EROSIONAL SURFACES AND DENUDATION them (fig. 4). A part of these geomorphological surfaces CHRONOLOGY are predominantly erosional (foothill surfaces, glacis), oth ers were formed by the joint work of accumulation and In the Transdanubian Mountains the Mesozoic horsts erosion. The most different elevation of Miocene foothill on which bauxite-bearing ancient tropical karst forms are surfaces, marine terraces and Danube delta gravel renders found overlain by thin Upper Cretaceous or Eocene sedi their correlation difficult. In the Visegrad Gorge of the ments are regarded as remains of the Cretaceous tropical Danube valley pediments were formed on andesitic rocks , etchplain from a geomorphological point of view (fig. 3). presumably during the same interval. Depending on their orographic position, these buried During the Quaternary some horst groups of the TM horsts may occur in uplifted position (summit level), as were further uplifted in a different manner (max. 200 to 250 lower-situated steps or also in threshold position. Their m). In this period valley terraces , alluvial fan terraces, surfaces, however, as fundamental morphogenetic surfaces cryoplanation glacis surfaces were shaped which are juve existed already in the Cretaceous and considerable reshap nile erosional and accumulational surfaces. The number and ing did not follow during the subsequent repeated exhu-

Q) c; t Q) Q) c > t etl Q) ~ ~ c Q) ~ ~ t Q) c I- -ro Q) Q) c; t >- -0 a.s.\. c ~ t ~ g> ~ m .~.= ~ ~ -§, .g Gerecse Mts ~ ~ FIG. 4 - Geomorphological surfaces and J > I- Q) « 500 ~ ~ . E I- 2:0 ..o;r;n ~ travertine horizons in the Gerecse fore 400 a; . ~ ~ . ~ ~g~~'. ~,r land (Pecsi , Scheuer & Schweitzer, 340 ~ '~ . § U5 ~ ~ . . TO . 1988). tI-tvn) river terraces usually cov 320 .... o · I mil 300 '~ ~ ~ • a mill ered by travertines (TI,-T7) and loess; PrPn) Pliocene pediment surfaces cov iE ~ ~~..~ PII ml mil · Tlla T12 ered by travertines (Ts-T9) ; mI-mm) 220 .g if, . ······tv·i,··· PI T9 TIO T11 Upper Pannonian (Upper Miocene) 200 Q; ...:d:]~ ~' •• , . tVI T T8 raised beaches covered by travertines 180 ~ ~ tv 7 160 I ;;;;; t\V tIV-V T6 . (Tw-T 12) ; To) Paleogene -Neogene plana 140 ~ T 120 •.. ~ tion surface sculptured by Oligocene- 100 .. ~'. tllb~.:.:.....tllfb' T4-5 5 _ Miocene pedimentation with sporadic tl tlla T2b T3a T3b gravels. Paleomagnetic polarity accord- • • ing to Marton & Pevzner.

65 mation accompanying uplift. It is also common that the In the mountain margins th e Neogene marin e terr aces Oligocene sandstone covers conformably the ancient etch represent usually younger geomorphological surfaces that plain characterised by tropical tower karst, bauxite and red the uplifted and exhumed horst surfaces. Nevertheless, it is clay (fig. 3). In most cases, during exhumation only the common that the Pannonian marine form ations overlie Tertiary sedimenta ry cover was removed from the horst horsts uplifted to 400 to 500 m height which were buried etchplanated in the Cretaceous and buried in th e Tertiary, in the Paleogene (Buda Mountains), elsewhere upper Pan thus th e exhumed ancient etchp lain represents the geo noni an travertine occurs on the Mesozoic geomorphologic morphological surface. surface (Balaton Upl and , ca 300 m above sea level). In There are horses in great number covered by Eoc ene some cases we find foothill surfaces in marginal positions, and Oligocene clastic rocks , whose ancient surfaces were transformed by Paleogene and/or Neogene pedimentation. not merely lowered but also remodelled . In this case the These may be further shaped by Quaternary cryoplanation surface of th e horst is identified as a younger reworked e.g. and accumulative glacis formation. This way generations of Oligocene geomorphological surfa ce. surfaces of different ages may be preserved on horsts or on It is occasionally difficult to determine the age of re their vicinities. modelling of the uncovered exhumed horst. In the se cases On the margins of horsts of th e Transdanubian Moun one may start from th e fact that the surfa ce of horsts of the tains the Late Cainozoic geomorphological surfaces (ma Transdanubian Mountains was planated already in the Cretaceous, the surface of those of low po sition slightly rine terraces, pediments, river terr aces) were preserved by change d during the Tertiary, it is inh erit ed. The uncovered th e hard strata of travertines from th e subse quent erosion. horsts of morphologically higher po sition could be pedi Travertines were form ed by karst springs in th e base level. planated in th e course of the Paleogene and became pedi In the Transdanubian Mountains 12 Neogene and Qua mented at their rnargin during th e Neogene. Each of the tern ary geomorphological surfaces were preserved by tra horsts etchplanated in the Cretaceous then buried , semi vertines. This ph enomenon is characteristic of the moun exhumed and being uncovered may occur at different ele tain margins and of some larger valleys. In th e valley-side vations (fig. 5). Some types can be found ego at the same terraces a lower sequence of tr avertines is deposited (be height besides each oth er within the same mountain unit. tween 120 and 250 m altitudes). The higher situ ated se It is also common th at the planated horsts covered by Oli quence of travertine covers th e pediments and marine ter gocene sandstone overlie stepwise one another. The surfac races. To determin e their age, fauna remnants paleomag es of different heights of these horst types do not represent netic and absolute chronological data were available geomorphological surfa ces of different ages. (Pe csi & alii, 1988).

a.s.\. m 700

600 500 TI J d I O_~El 400 T'dl~ 300

200 P-PlQC n-: ,....- ~~,..", MrMJ 100 Ez- I jI:;:~~;='; Ctb _~"E

TI d

a, b c d e

F IG. 5 - Geomor phological position of the dislocated and remod elled tropic al etchp lain remnants of the Transdanubian Mountains (after Pecsi ). ai' a2) buried surface of erchp lain in a sub - or intramontane graben; b) surface of planation in threshold position , exhumed and reshaped etchp lain; c) buried planated surface in uplifted position; etchplain remnant partly planated in the course of deposition of Oligocene gravel sheet over it; d) exhu med etch plain in summit position, reshaped erchp lain by (peri) pedimentation; e) uplifted, partially exhumed Cretaceous etchplain remodelled by pedimentation during the Tertiary (eg, Oligocene) in the forelands of the crystalline massifs, with conglomerate covers over their subsided part; P-Plgr) Pliocene

Pleistocene gravel; MrM3) Middle Miocene marl, limestone and gravel; E2l) Middle Eocene limestone; Eld) Lower Eoce ne dolomite detritus; Crb ) Upper Cretaceous bauxite; Tr.d ) Triassic dolomite; M-Pgr) Miocene-Pliocene gravel; Mgr) Miocene gravel; MrM3gr) Middle and Upp er Miocene grav el and conglomerate; Tr. , J.d.l) Triassic and Jurassic dolomite and limestone; O. cong.) Oligocene sandstone and conglomerate; 1) remains of tropical weather ing, with kaolinite and red clays; 2) unconformity; 3) tower karst remnant of a tropical peneplain; 4) gravel patches on the surfa ce.

66 CONCLUSIONS TABLE 1 - Geomorphological surfaces in the Hungarian mountains (Pecsi, 1985) Based on comparative geomorphological observations, a model of surface evolution through alternating erosion I. REMNANTS OF OLD EROSION SURFACES and accumulation is proposed, which is here used as a tool for underst anding the evolution of surfaces on horsts and 1. Remnants of Mesozoic etcbplains with tower karst - bur ied under lower Cretaceous clay or limestone in plate au po sition grabens in the Transdanubian Mountains (TM). This mod (in th e E. Bakon y), or in thresho ld pos ition (in the S. Bakony, H a el aims at an improving of accuracy of terminology (Pecsi lirnba) 1970a,b, 1975, 1993). Th e basis of this model for alternat - buried by Eocene limestone in summit position (in the Buda Mts. ) ing erosion and accumulation is that formerly developed - buried und er Eocene limeston e (at Cant, Vertes Mts.; Nyirad, Ba- kony Mts.) (by tropical etchplanation, pedim ent ation , pediplanation ) - buried under Ol igocene sandstone (in the Buda Mts.) on different surfaces of erosion are rep eatedly reshaped by erosion and elevations accumulation during subsequent geological times. The - remn ant s of an exhume d etchp lain in summit pos ition (in the Buda morphostructural element is repeatedly uplifted and sub Mts ., Keszt hely Mts.) sided and horizontally displaced by tectonic processes. 2.Remnants ofPaleocene (and mostly Mesozoic) etcbplains resculptured by Thi s model proposes that in the TM the conditions re Oligocene and Miocene pedimentation - etchplain b uried by Miocene gravel in summit position (at sulting in erosional surfaces, due to tropical tower-karstic Fark asgyepii , Bakony Mrs.) planation and accompanied by bauxite formation , were in - exhumed etchp lain with patches of Miocene gravel in summit posi terrupted by the beginning of the Tertiary. This was main tion (in the Gerecse Mts. ) ly caused by changes in climate and in tectonic activities. During the Terti ary the bulk of the TM was repeatedly II. REM NA NTS OF NEOGENE SURFACES OF PLANATION buried by tectonic subsidence under sedimenta ry sequenc 1. Miocene raised beaches es of different thicknes s. Some regions were partially or en - Surface with Kar patian conglomerate (in the northern foreland of tirely elevated and exhumed twice or three times (during Bako ny Mrs.) - Surface with Badenian litto ral sandy -gravely limeston e (in th e the Paleogene, Neogene and Quaternary). The karstic Visegrad and Borzsony Mts.) etchplain surfa ce of Cretaceous origin was further eroded - Sarmatian raised beach (in the Buda Mts ., Balaton Up land) or buried under sediments during these repeated burial - Sarrnatia n pediment (in the Ma rra and Zemplen Mts.) and exhumation events (e.g, by peripedim entation , form a 2. Pannonian (Upper Miocene) raised beaches and travertine horizons tion of marin e terraces, or alluvial fans). The TM , subdi - Lower P ann onian (Monacian) raised beach (at Sosk ut ., Di6sd, in vided by grabens, contains five different groups of geo the Buda Mt s. and on th e Balaton Up lands) -Delta deposits (Precsakvarian-Csakvririan, the «Billege» and « morphological surfaces: Kalla» gravel on the Balato n Up land ) 1. horsts of etchplanation in summit level, partly exhumed; - Upper Pann onian (Po nti an) raised beach - two surfaces (in the Ba 2. buried horsts of etchplanation in uplifted position ; kony , Vertes and Buda Mts.). - Upper P annoni an (Csakvarian - Siimegian - Baltavarian) trave rtine 3. horsts of etchplanation in threshold po sition , bu ried or occurring on two or th ree surfaces (Nos 10-12, at Na gyvazsony, exhumed and reshaped , mainly by pedimentation ; Veszprern Plateau and Varp alota in the Bakony Mts ., on Szechenyi 4. buried etchplain in basins (cryptoplain); and Szaba dsag -hill in the Buda Mts ., two surfaces in the Gerecse 5. peripediments, rock y pediments, glacis, partly covered Mt s.) - Upper Pann onian deltaic gravel (on Kopite hill in the Gerecse Mts .), by alluvial fans. - Upper Pannonian-Pliocene basalt lava on pediment (subdivided into two levels?) (e.g. on Kabhegy and Soml6 hills in South Bakony Mts.). On th e «G eomorphological Map of Hungary» (Pecsi, 1976) and on the «Geomorphological Map of the Danubi 3. Uppermost Miocene - Pliocene pediments and travertine levels - Mio-Plioce ne pediment (Baltava rian) locally lowers down and an Countries»(Pecsi, 1977, 1980) and regional landscape for ms a double surface of planation (be tween 360 and 220 m above monographs on the TM(Pe csi, 1988, (Pe csi & Juhasz, sea level along the margins of the Transdanubian Mountains). 1990) the term erosional-accumulational surface evolution - Pliocene (Ruscinian -Csar notian) travertine horizons on pediment (No s 8 and 9; in the Buda Mt s., on th e Kopi te-hill at Sutta in the was used for the development of thos e geomorphological Gerecse Mrs) surfaces for which sufficient information was available , ac cording to the principles and criteria of the proposed mod 4. Upper Pliocene (Ruscinian - Csarnotian - Lower Villdnyian) old alluvial fans and travertine horizons el. Th e model explaining and classifying the erosional sur - the Kerneneshat - Eziisthegy - Kandik6 gravel sheet face evolution describes the surfaces of planation, buried - terr ace No VIII and trave rtine No 8 (in th e D anube Bend Mts. ) surfaces, rep eatedly exhumed and eroded planes, illus - terrace No VII and travertin e No 7 (terrace hills of the Kemeneshat) trates the polycyclic process of their superposition and re veals the main phases of the changes. III. QUATERNARY FLUVIAL TERRA CES, ALL UVIAL FA N After three decades of ob servations in this field we TERRACESAND TRAVERTINE H ORIZONS think that the explanation is not just valid for the individu - Te rrace No VI and tr avertin e No 6 (Upper Villanyian) al Intracarp athian Mountains, but may be applied in the - Terrace No V (Kislangian - Biharian ) and travertin e No 5 (Midd le Biharian?, of reversed polarity) cases of the Alpin e-Dinarid mountain system, of some Eu -Terr ace No IV(Middle Biharian, Vert esszolos phase) , > 350 Ka, rop ean ancient mountains, or of mountains and massifs of terra ce and travertine are of nor mal po larity various continents. Th e superposition of geomorphological - Terrace No IlIa and travertine No 3a (270 Ka)(in the Gerecse Mts.) levels of different ages could be demonstrated in the -Terrace No lIb (R3-Wl) with traverti ne cover (120 to 70 Ka old) - Terrace No II a (W3), ca 26 to 12 Ka case of the units of the TM, using the procedures of - flood- plain No I and H olocene travertine No 1, from 11 Ka to denudation- and accumulation chronology (table 1). Th e present

67 particular case of it has been published several times in er intensities under mod eratel y humid conditions. H e considers the dif Hungarian and in other languages, summarised in a mon o ferences between forms developed in arid, semiarid and moderately hu mid climatic zones to control merel y the intensity of development. graph of the Transdanubian Mountains (Pecsi, 1970a,b, Another open question concerns the criteria of identification for the 1993; (Pecsi & Juhasz, 1990;(Pecsi, & alii, 1985; Szekely, pediplain, as a remn ant of some planated surface outside the semiarid zone. 1972). In the Gerecse, Buda, and Pilis Mountains (TM) the 5 Tropical surfaces of plan ation , the con cept of etchplanation, Way presence of almost all young geomorphological levels land (1933) introduced the concept of etchp lain , the etchplanation has could be demonstrated in some sections , in addition to been attributed to tropical deep weath ering followed by removal (strip older ones. In the forelands of these Mountains the higher ping) of the thic k regolith zone. The idea has been elaborated and furth er levels were represented by 3 or 4 Neogene marine terraces developed by Biidel (1957), partl y mo dified by Bulla (1958), Louis (1957) and some others. to to and deltas , by 1 2 foothill surfaces , and by 4 6 Qua The concept, that extensi ve surfaces of erosion are most readily ternary fluvial terraces (fig. 4). Th ese geomorphological formed under humid or alternately humid and arid tropic al climates, has levels were protected against subsequent denudation by become more and more widely accepted. Th e initi ators of the theory ex travertines capping them. Thus a reconstruction of long plained the lowering and smoothing of large surfaces by extensive col term morphological evolution of geomorphological surfac loidal and sub colloidal weathering as well as by large scale slopewashing. es became feasible (Pecs i, 1975, 1993; (Pecsi , & alii, 1985). Budel interpreted the evolution of the tropical surfaces of planation by developing the theor y of «duplicate planation surfaces» (do ppelte The chronological classification of the geomorphologi Ein ebnungsflachen ). cal surfaces gave us a key to outline the geomorphic evolu In the zone of tropi cal slopewash, the surfaces are thickl y covered tion of TM during the Cainozoic era. with products of weathering , underlain by a less thoroughly smoothed but still hummocky relief of unweathered rock (e.g. granite). This deeper interface is the basal front of planation , smoothed by weathering . Double planation takes place, on one hand , by slopewash on the surface cloak of NOTES weathering products (Spiilobe rflache) and, on the oth er hand , by sub sur face weather ing on the deeper inte rface. 1 Th e genetic and topographic int erpretation of the concept of relief 6 Sporadically in the Carpathian Basin red clays occu rrin g in sub aeral planation is rathe r diverse in the literature. Taking into consideration all Neogene deposits, in basin position , are interfin gered by series of varie definiti ons, bo th narrow and broad , it emerges that surfaces of planation gated clays, sandy clays, silts and sand s. Th ese sequences, under op timal are considered (plane) surfaces of considerable extent and low relief ener geological and climatic conditions, could cover most of the Pliocene and gy, over a stable or gently rising base. Th ey are sculptured by processes of the start of their formation can be dated to the late Miocene (ca 2-5.6 Ma, destruction , and by a well-defined equilibrium of uplift and Pecsi 1985; Pecsi & alii, 1988). The red clay together with the intercalat degrad ation . ed sequence are also products of cyclic climatic changes. Th ey represent W hile some autho rs conside r surfa ces of planation to be results of sub tropic al subhumid climate with alterati on of warm-rainy and warm sculpturing by a single erosive agent, oth ers think that they are polygenet dr y seasons, succ eeded by warm semiarid climatic intervals pre venting ic; i.e. th ey result from the interaction of several processes the rates of red clay formation but favouring pedim ent development . which vary in time and space. Some authors believe that surfaces of pla nation are polygenetic also in space. Th eir complex of forms includes not only sur faces of eros ion, but also surfa ces of accumulation.

2 Davis assumed periods of long tectonic rest in the evolution of a mountain; the evolution during such a period produces a peneplain in the penultimate stage of the cycle of erosion, which subsequentl y undergoes REFERENCES repeated uplifting. On the mountain margins, at the base level of erosion, pa rtial peneplains come into existence. Wherever and whenever the peri ods of tect onic stillstand s were not sufficiently long for the process of pe BALLAZ. (1988) - Tertiary paleomagnetic data for the Carpatbo-Pannonian nepl anation to compl etely wear away the relief form ed durin g the pr evious region in the light of the Miocene rotation kinematics. Foldt ani cycle and subsequently uplifted, there, according to Davis, occur remnants Kozlony, 139,67-98. of older peneplains at higher altitudes, in a stepwise arrangement . BALDI T. & K6 KAYJ. (1970) - Die Tuffitfauna von Kismaros und das after des Borzsonyer Andesitvulkanismus. Foldtani Kozlony, 100,274-284. J In the Penckian interpr etation of stepped Rumplflachen (piedmont BALDI T. (1982) - A Karpdt-Pannon rendszer tek tonikai es osfoldrajzifejlo benchlands) the initial surfa ce is the «P rimarrump]», but it may also be dese a kozepso tercierben. (49-19 millio eu kozott) (Tectonic and pale the Davisian pen eplain, the «En dr umpl», «Endpeneplane». As a result of ogeographic evolution of the Carparho-Pannonian system in the mid arching , a process extending in area and accelerating in time , the longitu dle Tertiary, between 49-19 Ma BP.) . Oslenytani Vitak, 28. 79-155. din al profiles of rivers are broken and the valley flanks gradually retreat BARDOSSY Cv. (1973) - Bauxitleepzodes es lemeztektonika (Bauxite form a and broaden at the expense of the higher surface. Th e broadenin g arch tion and the plate tectonics ). Geon6mia es banyaszat. MT A X. embraces an increasingly wide area and thus and increasingly number of osztaly kozlernenyek, 6 (1-4), 227-240. younger step surfaces are connected to the most highly elevated central BARDOSSY Gy. (1977) - Karsztbauxitok (Karstic bauxites). Akademiai arch. It is this system of stepwise rep eated surfaces of planation that was Kiad6 , Budapest, 413 , pp . called «P iedmont treppen» by an ever broadening area, rath er than to a BREMER H. (1986) - Geomorphologie in den Tropen-Beobacbtungen, Pro protracted and constant- rate uplift. zesse, Modelle. Ge ook od ynamik , 7, 89-112. 4 Pediplains have usuall y been deduced from pediments (Maxson & BULLA B. (1958) - Bemerkungen zur Frage der Entstehung von Anderson 1935, H oward 1942, Mackin 1970). It was in conn ection with Rumpffliichen. Foldraj zi Enesiro, 7 (3),266-274. thes e forms that American geologists and geomorphologists first came to BODEL J. (1957) - Die «doppelten Einebnungsfldcben» in [eucbten Tropen. attribute a decisive role to climatic factors. The y interpreted as pediplains Zeit. Geomorph., N .F, 1,201-228. a nu mb er of extensively planated surfaces regarded as peneplains by Da DAVIS W.M. (1906) Geographical Essays. Ginn, Boston, New edition: vis. King (1962) has lately expressed the view that pediplanation is the 1954, Dover , New York, 777 pp. most general form of surface lowering, substituting, as it were, the peri DAVIS W .M. (1922) - Peneplains and the geographical cycle. Bull. Geol. plan ation concept for the Davisian peneplain concept. In this way, how Soc. Amerika, Baltimore, 33, 587-598. ever, King (1949, 1962) gave an unduly broad context to the term pedi FOLOP J. (1989). - Beuezetes, Magyarorszdg geologiajdba (Introduction in plain, under which heading he included all the extensive planated surfac Geology of Hungary). Akaderniai Kiad6 , 246 pp . es of all continents as far back as the Cretace ous. In King's opinion pedi GECZY B. (1974) - Lemeztektonzka es a paleontol6gia (Plate tectonics and plain s are typical of semiarid tropical zones, but may also develop at low- paleontology). Foldtani Kutatas, 17 (3) , 17-20.

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