Upper Permian.Trias Sic Facies Zones in the Transdanubian Range

Rivista Italiana di Paleontologia e Stratigra{ia volume I u I numero 3 pagine 249-266 Dicembre 1995

UPPER PERMIAN.TRIAS SIC FACIES ZONES IN THE TRANSDANUBIAN RANGE

JANOS HAAS* & TAMAS BUDAI**

Key-'utords: Upper Permian-Triassic, facies pattern, paleogeo- Alpine relationship of the Mesozoic section of the graphic reconstruction, Transdanubian Range, Hungary. Transdanubian Range was noticed as early as the second Riassunto. Yiene analizzata in quesro anicolo la distribuzione half of the last century (Peters, 1859; Hauer, 1862;Hof- delle facies del Permiano superiore e de1 Triassico nell'ambito della mann, 1871.; Bóckh, 1873). Later on, at rhe beginning of Catena Transdanubiana. Sono state compilate cane di {acies per sei this century others (Taeger, 1912, 1913; Lóczy, 1916) interualli di tempo, sulla base di dati di superficie e sottosuolo, che confirmed these sono state uti\jzzate per le ricostruzioni paleogeografiche. Conside- statements. In accordance with generai rando l'intervallo Permiano superiore-Triassico, le unità della Catena contemponneous concepts, the plausible relationship Transdanubiana mostrano una precisa polarità: la porzione a nordest was explained by assuming narrow seaways between the rappresenta il lato verso il mare aperto, mentre la porzione a sudovest Alpine sedimentary basins and the areas the island costituisce il lato in direzione della terraferma. IJna pane imponante of delle facies può essere correlata con facies coeve del Sudalpino e delle mountains within the Pannonian Basin (I-nczy, 1.91.6; falde dello Austroalpino superiore, fornendo un significativo stru- TelegdiRóth, 1.929 ; Yadlsz, 19 6Q). mento per la ricostruzione della posizione originale delle unità della General acceptance of the mobilistic plate rectonic Catena Transdanubiana. concept established the idea that the Transdanubian Abstract, Facies patterns of the Upper Permian and Triassic Range Unit broke away from its original location and formations within the Transdanubian Range are presented. Based on reached its present-day position as a result of consider- surface and subsurface data, facies maps were compiled for six time able dislocations. slices which served as a basis of the paleogeographic reconstructions. Considering the entire Late Permian - Triassic interval, the Transda- Based on the setting of the Upper Permian facies nubian Range unit shows a definite polarity: its nonheastern pan boundaries, Majoros (1980) suggested a large-scale strike- represents the seaward (internal) side, whereas its southwestern part slip motion of the Transdanubian Range from the South represents the landward (external) side. A remarkable pan of facies units of the Transdanubian Range could be correlated with time equi- Alpine region along the Periadriatic lineament. Later valent facies in the Southern Alps and the Upper Austroàlpine nap- on, a great number of workers (Balla, 1982; Kàzmé4 pes, providing an effective tool for the reconsrrucrion of the original position of the displaced Transdanubian Range Unit.

Introduction.

In the last decades, many studies have proved the heterogeneity of Paleozoic - Mesozoic - Early Tertiary sequences making up the basement of the Pannonian Basin. Based on these studies it has been shown that the present-day setting of the structural units of the basement (Fig. 1) is a result of complicated plate-tectonic rearrangements just prior to the beginning of the evoiu- tion of the Late Tertiary Pannonian Basin. Since the present-day setting does not reflect the original relationships of the structural units, reconstruction of their 0 100 km MT = MID.TRANSDANUBIAN paleo-position became one of the key problems of the structural evolution and paleogeography of the entire Fig. 1 - Megatectonic serting of the Transdanubian Range (Haas et Alpine-Carpathian-Dinarid region. al.,1995).

'r Academic Research Group. Department of Geologn Eòtvós Lorónd University of Sciences. Múzeum karit 4/a. H-1088 BUDAPEST. Hungary. 'r'r F{ungarian Geological Institute. Stefónia út 14, H-i143 BUDAPEST, F{ungary. 250 f. Haas & T. Budai

LITHOSTRATIGRAPHY SI.]BREGIONS

2M 205

DACHSTEIN LMST FM; -J:KOSSEN FM- 2to

(/)F

2r5 F.1 z E MAIN DOLOMITE FM v)F O 220 U

v) 225 V)

BUDAORS DOLOMITE FM. 230 /, t-

235 LMST FM

ITE FM -ISZKAHEGYI LMST FM 240

N-N--N-NPN-N MARL FM- N N - N-N--N---N-N- -CSOPAK - 245

DOL. DINNYÉS 250

r[î\Tîl 2Fì:! 3W 4Ftr; 5l-::l 6[l.l Tfnrl B[y-Tl

F;q ) Stratigraphic chart of the Upper Permian-Triassic formations of the Transdanubian Range (chronostratigraphic scale after Gradstein et a1., 1994). Arrows indìcate the discussed stratigraphic horizons. Abbr.: FÒ - Felsóórs Limestone Fm.; MA - Mótyóshegy Fm.; ED - Ederics Limestone Mb.; SV - Sédvólgy Dolomite Mb.; VA - Vadasken Dolomite Mb.; SH - Sóndorhegy Fm.; FH - Fekerehegy Fm. Legend: 1) shallow-water limestones; 2) dolomites; 3) deep-water limestones; 4) marls; 5) marine sandstones and siltstones; 6) continental sandstones; 7) evaporites; 8) volcanic tuffs. Permian-Triass ic Tran sdanubian Range 251,

1984; Kizmér & Kovócs, 1985; Brezsnyinszky & FIaas, stinction of the Late Permian-Triassic facies zones and 1986; Haas, 1987; Csontos et al., 1992) discussed this to draft facies patterns for several reievant time levels problem, generally accepting the concept that the Tran- within the Transdanubian Range Unit, and b) rc di sdanubian Range Unit was located between the Sout- scuss possibilities and problems of the reconsrruction hern and the Eastern Alps (Upper Austroalpine nappes) of the original position of the Transdanubian Range in in the early period of the Alpine evolutionary phase; the framework of the Alpine system based on correla- however, they differently explained the history and me- tion of the facies zones. In accordance with the main chanism o[ the dislocations. aim of our study, we selected stratigraphic intervals char- The reconstruction of the original setting of the acterized by remarkable facies differences. They are indi- Transdanubian Range (i.e. its setting prior to the major cated in Fíg. 2, where time and space relationships of orogenic movements) is based fundamentally on the fit- the Upper Permian-Triassic iithostratigraphic units o{ ting of the Late Permian-Triassic facies zones of the di- the study a(ea are shown. In Fig. 3 lateral thickness- slocated units (Haas et al., 1995). Flowever, in the paper changes of the lithostratigraphic units are presented by a of Haas et al. (tWS) and also in other previous papers, schematic cross section running along the strike of the the Late Permian and the Norian facies zones were Transdanubian Range. The reference line of the section mainly considered and constrains of facies boundaries is the base of the Main Dolomite Formation. Data to be were generaily missing. This might be the reason, why displayed include results of the latest mapping project in distinction and limitation of the facies zones have been the study area (Fig. 4), studies in the framework of the subject of many debates in the past years. Since outcome national key section project, and other important core of these debates may profoundly influence the recon- data. Fig. 4 also shows localities referred in the text. structions and the interpretation of the structural evolution of the Pannonian Basin and the surrounding re- Facies pattern of the selected stratigraphic intervals. gions, more detailed studies on the facies setting and further evidences for the facies correlation seemed to be Upper Permian (Fig. 5). necessary. Consequently, our paper has two main goals, a) The Upper Permian sequence of the Transdanu- to summarize da-.a which may serve as a basis for di- bian Range can be divided into three, coeval formations

SW BAKONY MTS +BALATON HICHLAND

DACHSTEIN LIMESTONE

base of M.D

.^-J---^ VES ZPRÉM M ARL ---

010

F;- 1 Schematic cross section along the strike of the Transdanubian Range unit fron the Buda Hills to the Zala Basin. Reference line is the base of the Main Dolomite Formation. Abbr.: TA - Tagyon Fm.; MA - MÉtyàshegy Fm.; VE - Veszprém Marl Fm.; SH - S:indorhegy Fm.; VA - Vadasken Dolomite Mb.; FH - Feketehegy Fm. Buchenstein Gr. includes the Felsòórs, Buchenstein and Fiired Formations. For legend see Fig. 2. 252 /. Haas & T. Budai

./---.4 --: Diósjenúrin1_:B:rtt:

Csdvdr block 0 10 20 30km

NORTH A f -

651; Lower Paleozoic metamorphic l-- complex lilîl Pe.mian rìeî --=------Zat 1--Li r flasslc \-_-_-lJ----;=;>--L--- ^lslr-- - - l___] --)_-_-_-_-_- -t-. ! Jurassic pp;1 Lower-Middle Cretacmus of the ll--]'-u Bakony Mts. WZ l-nwer-Middle Cretaceous of the GetecseMls. ^f- f ----l Upper Cretaceous

Fig. 4 - Simplified geological map of the Transdanubian Range (Haas et a1., 1995) showing the referred locations. / // z-\ Upper Permian

\ Budapest \ \

0 20km

h I l) 1V7-V z l--;l 3 Fl..l 1[f-n --

Fig. 5 - Present-day exrension of the Upper Permian lithofacies of the Transdanubian Range. 1) Dinnyés Dolomite; 2) Tabaid Evaporite; 3) Balatonfelvidék Sandstone; 4) Pre-Permian formations; 5) facies boundary; 6) main tectonic line; Z) outcrop; 8) borehole Permian-Triassic Transdanubian Ranpe 253

(Ftilop, 1990) representing characteristic facies zones of in the eastern part of the SE foreiand of the Vértes the continental margin during the Late Permian rrans- Mountains and S of Lake Velence, on the sourhern gression. flank of the Velence anticline. The Balatonfelvidék Sandstone Formation is a flu- Exact drawing of the boundaries of the aforemen- vial facies association made up by cyclic alternation of tioned units is not possible at present. Flowever, lateral conglomerate, sandstone and siltstone layers. Thickness relations of the Upper Permian formations clearly indi- is 400-800 metres, and significantly decreases (to 150 m) cate that transgression reached first the NE part of the northeastward (Fig. 3), where the unit is partially substi- Transdanubian Range (according to the present-day tuted by coastal (Tabajd Fm.) and marine facies (Din- orientation), then it progressed toward S\f, whereas a nyés Fm.). Outcrops of the formation can be followed large part of the Transdanubian Range area was flooded all along the Balaton Highland. It is also exposed by only during the next significant transgression at the be- some drillings in the basement of the Kisalfóld, which ginning of the Triassic (see Fig. 5 and Fig. 6). belongs to the northern limb of the synclinorium of the Transdanubian Range. Lowermost Triassic (Fig. 6). The Tabajd Evaporite Formation consists of red siltstones, with dolomite, anhydrite, and gypsum lenses, no- As a consequence of the above mentioned fast dules and interlayers. It represents the coastal sabkha-salina transgression, an oolite horizon was formed at the base facies belt. Its maximum rhickness is 300 metres. Thick- of the Lowermost Triassic sequences. Based on palynolo- ness decreases northeast'ward, where the unit is partially gical data, oolitic beds are somewhat older in the north- substituted by the Dinnyes Dolomite. This formation is eastern region, where the P/T boundary is within the known exclusively from boreholes in the SE foreiand of oolite horizon, whereas in the Balaton Highland the ba- the Vértes Mountains, NE to the Balaton Highland. sal beds are lowermost Induan (Haas et aI., 1.986; G6czàn The DinnÉs Dolomite Formation is made up by et aI., 1987). After the oolite event, three sedimentary algal dolomite with evaporite interlayers. This cyclic se- environments were established in the area of the Transda- quence represents periodically desiccated lagoon facies. nubian Range. In the southwestern part of the area, in a The thickness of the formation may reach 400 m. The lagoon of periodicaily hypersaline water frequently affec- unit is unknown on the surface but,reached by borehole ted by terrigenous influx, the Kóveskól Formation was

--\ Lowermost Triassic \ \\ [\ )Budapest \ ,)

0 20km \4 1f7V z[=--l 3El 4[--fì 5 _._ 6 ___ 7 Bl -

Fig. 6 - Present-day extension of the Lowermost Triassic lithofacies of the Transdanubian Range. 1) Kóveskól Dolomite; 2) Arícs Marl; 3) Alcsútdoboz Limestone; 4) Pre-Scythian formations; 5) facies boundary; 6) main tectonic line; 7) outcrop; 8) borehole. 1)+ J. Haas & T. Budat

deposited. Northeast'ward, it passes into the predominan- "gastropod oolite" interlayers occur. It is known exclusi- tly shaly Arócs Formation of intertidal- subtidal facies vely from boreholes in the southern {oreland of the which further to NE is partly substituted by shallow ma- Vértes and the Velence Mountains. The thickness of the rine carbonate facies of the Alcsútdoboz Formation. formation is about 150-200 m. The Kòveskól Dolomite Formation consists of The only lateral facies boundary that can be satis- grey, porous, and in the basal layers oolitic dolomites, factorily drawn between the above-mentioned three dolomitic siltstones and sandstones. IJpwards in the se- units is that between the Kòveskól and Arócs Forma- quence, the dolomite content increases whereas the tions. Its direction is roughly N-S in the Balaton amount of siliciclastics decreases. In the southwestern Highland area. The lateral boundary between the Arócs part of the Balaton Highland, this lithofacies represents and Alcsútdoboz Formations might be parallel to this. all of the Lower Scythian. In this region, its thickness is Based on available data, a rightJateral displacement of about 1OO m. Further to N\f, it occurs between the Per- this boundary of 10-15 km amplitude may be assumed mian Balatonfelvidék Sandstone and the Arócs Forma- along the Balaton Line. tion in a significantly reduced thickness. made predomi- The Arócs Marl Formation is up Middle Anisian (Fig. 7). nantly by greenish-grey and brownish-red marls with are faìrly siltstone and "gastropod oolite" intercalations. Bioturba- Olenekian to l-ower Anisian sequences area. In tion is common. In its type locality on the Balaton uniform all over the exposed parts of the study facies pattern Highland, it is not thicker than 1,2Q m. Based on core the Middle Anisian, differentiation of the data, the formation can be followed along the SE limb is visible as a response to initiation of tectonism (B"- of the Bakony. It is also known from boreholes in the dai & Vòrós, 1,992). Platform carbonates (Megyehegy Northern Bakony and in the southern foreland of the Dolomite, Tagyon Limestone) and pelagic limestones Vértes and the Velence Mountains although in the latter were formed (Felsóórs Limestone) coevally. areas the sequences show transitional features towards The Megyehegy Dolomite consists predominantly the Alcsútdoboz Formation. of grey, thick-bedded sparitic, lithologically rather mo- The Alcsútdoboz Formation consists of grey lime- notonous dolomites. Its thickness is markedly variable: stones, caicareous marls and silty marls; in the latter 10-30 m in the S\fl margin of the Balaton Highland and

---\ -/t Nliddle Anisian

\ Budapest \

)

Veszprem y o-----iottt

I NSSI 2: 3[-Tì

5 ó 7 --- -

F;. 7 Present-day exrension of the Middle Anisian lithofacies of the Transdanubian Range. 1) Felsóòrs Limestone; 2) Megyehegy Dolomite + Tagyon Limesrone; 3) Pre-Anisian formations; 4) facies boundary; 5) main tectonic line; 6) outcroP; 7) borehole. Permian-Triasic Transdanubian Ranpe 2s5 in a zone nofth of the Litér Line (Fig. 3), whereas in ced thickness (a few metres) represenr the formation. It the middle part of the Baiaton Highland, at the rim of is also known from cores in the Northern Bakony. the Veszprém plateau and in the eastern Bakony it is The relationships of the basin and platform for- more than 250 m. In the former areas, dolomites are mations are satisfactorily known oniy in the Balaton slightly bituminous and bioclasts are common. In the Highland area. Based on available data, we assume rhe latter ones, the bituminous facies occurs only in the continuation of the basins NSí and Sll of this area, lower part of the formation. In the Northern Bakony whereas shallow platforms might be located north- and in the area south of Lake Velence, the formation is east.ward. known only from boreholes. The Tagyon Limestone Formation occurs only in Upper Ladinian-Lower Carnian (Fig. 8). a small part of the Balaton Highland. The sequence is made up by cyclic alternation of light brown ro yel- Ladinian and lowermost Carnian are represented lowish-white, thick-bedded, subtidal limestones and by thick platform carbonate sequences in the NE part brownish-yellow, thin-bedded, peritidal iimestones and most probably also in the SW part of the Transda- showing fenestral lamination. Its maximum thickness is nubian Range (Budaórs Dolomite). F{owever, in the area about 80 m. of the Balaton Highland and the rim of the Veszprém The Felsóórs Formation locaily overlaps and local- plateau, pelagic basin sedimenrarion was conrinued (Fú- ly replaces the Anisian platform facies. It consists of red Limestone). thick-bedded cherty limestones; brachiopodal-crinoidal Volcanic activity initiated in the Late Anisian and limestones; ammonite-bearing bituminous, laminitic reaching its climax in the Early Ladinian shows a gra- limestones, marls and dolomitic marls. The maximum dual deciine during the Late Ladinian (Budai & Vóròs, thickness of the Felsóórs Limesrone (150 m) occurs in 1993). This trend is reflected by the rransition of the the middle part of the Balaton Highland (in the surroun- tuffaceous Buchenstein Formation into the light-grey, dings of Balatonfùred), from where the unit pinches out well-bedded, slightly cherty Fùred Limestone. In the towards NE. Surface exposures are restricted to the area lower part of the Fùred Formation, limestones are of the Balaton Highland. NE of this area, in a few isola- thick-bedded. Progressing upward, the thickness of beds ted outcrops, brachiopodal limestones of extremely redu- decreases and the limestone succession is punctuated by

Upper Ladinian-Lower Carnian ,/ \ Budapest \

) tre" --_/ 0 20km /

-fl1T1TÉ r FN\ t7=1 r l-l--ll ill t'-L- Ir-.- 5--- 6- 7L

Fig 8 - Present-day extension of the Upper Ladinian-Lower Carnian lithofacies of the Transdanubian Range. 1) Buchenstein + Fùred Lime stone; 2) Budaòrs Dolomite; 3) Pre-Ladinian formations; 4) facies boundary; 5) main tectonic line; 6) outcrop; 7) borehole. 256 t. Haas G T. Budai

marl interlayers. The Fùred Limesrone can be followed westward. The unit pinches out in the NE part of the all along the Triassic zone of. the Balaton Highland Balaton Highland. Apart from its surficial extension south of the Litér Line, whereas to the north only a few area, the Budaòrs Dolomite was also reported from a data are available. The formation attains its maximum borehole, south of the Lake Velence. thickness (60 m) in the middle part of the Balaton Platform dolomites were exposed by drill cores Highland in the vicinity of Balatonfùred and shows gra- below the Carnian shales in the Keszthely Mts., but the- dual thinning both toward SV and NE. In the North- re is no biostratigraphic evidence for their age. ern Bakony, it is exposed only in cores and its thickness is highly reduced (not more than 5 m). Middle-Upper (Fig. Upper Ladinian dark-grey volcanoclastics with Carnian 9). plant remnants showing similarities with the Wengen fa- In the Middle Carnian (|ulian), the significantly cies, are known only from a few cores in a small area in increased terrigenous influx resulted in the infilling of the eastern part of the Bakony Mts. the intraplatform basin of the Balaton Highland-Bakony At the southern rim of the Veszprém plateau and area, whiie new basins came into being in the NE part in the northern range of the Balaton Highland, the Bu- of the Transdanubian Range (in the area between the daórs Formation of carbonate platform facies appears Vértes and the Buda Mountains) above the previous car- above the gradually outpinching Fiired Limestone or, bonate platforms. By the Late Carnian, gradual infilling where it is totally missing, directiy above the Buchen- of the basins attained an advanced stage and the Balaton stein Formation. Highland - Bakony area became a restricted basin The Budaòrs Dolomite is made up by thin- to showing further shallowing-upward trend (Sóndorhegy thick-bedded dolomites. Cyclic alternation of dasyclada- Formation). Flowever, in some places evolution of car- cean dolomites of subtidal logoon facies and peritidal bonate platforms continued or they were affected only beds of algal mat facies is generally characteristic. The by incipient drowning. Consequently, isolated platforms thickness of the formation is about 1000 m in the emerged in the area of the Keszthely Mountains (Ede- northeastern part of. the Transdanubian Range (in the rics Limestone), in the eastern parr of the Bakony (Séd- vicinity of Budapest) and gradually decreases south- vólgy Dolomite) in the Buda Mountains (Vadaskefi Do-

--\ I Middle-Upper Carnian _E -\- \ -/\

Budapest \

A ) //

./ Veszprem K"". r 0 20kn /-_ t,

1-l zB 3-l r[T--fl 5_._ 6___ 7- 8^

Fig. 9 - Present-day extension of the Middle-Upper Carnian lithofacies of the Transdanubian Range. 1) Ederics Limestone, Sédvólgy Dolomr te, Vadasken Dolomite, Nézsa Limestone (Dachstein-riff linestone); 2) Veszprém-Sóndorhegy Formation; 3) Mótyíshegy-Csòvór For- mation; 4) Pre-Middle Carnian formations; 5) facies boundary; 6) main tectonic line; 7) outcrop; 8) borehole. Permian-Triass ic Tran sdanubian R anpe

lomite), and even in the Csóvàr block ("Carnian reef mite only by thin marly intervals; consequently, distinc- limestone'). tion of the three platform dolomite units is not easy. The Sóndorhegy Formation is made up by three In the central part of the Buda Mountains, massi- members. The lower member consists of light-grey, thin- ve platform dolomites of Upper Carnian age occur (Va- bedded, laminitic, bituminous limestones with slump daskert Dolomite), showing features similar to the Séd- folds. its thickness is 30-70 m. The middle member con- vólgy Dolomite. In the noftheasrern and southerfl parf sists of iight-grey, commonly intraclastic dolomites. Its of the Buda Mountains, cherty limestones and dolomi- thickness is variable, increasing towards the coeval car- tes of basin facies are exposed in outcrops and cores. bonate platforms. The 30-50 m thick upper member is Based on conodonts and radiolarians, Middie Carnian, made up by well-stratified, nodular, localiy cherty lime- Lower and Upper Norian, and Rhaetian ages have been stones, mariy limestones with large oncolites, megaio- reported from the pelagic succession (Kozur Ee Mock, dontids and brachiopods. Extension of the Sàndorhegy 1991; Dosztàly pers. com.). According to these data, ac- Formation is restricted to the Balaton Highland. cumulation of basin sediments may have been conti- Platform carbonates may be either practically undo- nuous from the Carnian to the Norian in the intra- Iomitized or pervasively dolomitized. The only locally and platform basins, while on the surrounding piatforms the slightly dolomitized Ederics Limestone is known from the Vadaskert Dolomite was formed. Keszthely Mountains and the surrounding area and from a A similar relationship can be assumed in the Cso- few boreholes also in the southern and northern parts of vír block (NE of Budapest), where the "Upper Carnian the Northern Zala Basin. It is made of massive biogenic reef limestone" deposited coevally with the lower part and ooidic-oncoidal limestones. Its thickness is 2OO-300 m. of the Csovàr Formation of basin and slope facies, is The Sédvólgy Dolomite consists of thick-bedded exposed in core (Detre, 1.970;Kozur & Mostler, 1973). dolomitized biogenic carbonates. Microbial encrusta- tions are common and characteristic. This unit is Upper Norian-Rhaetian (Fig. know"n in the eastern part of the Bakony and in the 10). Vértes Mountains. It is separated from the underlying In the latest Carnian, huge carbonate platforms Budaórs Dolomite and from the overlying Main Dolo- came into being on the Tethyan shelf of levelled topo-

-\ 1 Upper Norian-Rhaetian Danube \

-t\

Budapest \ \

il|l H"*n"

20km 0|-'""g I

I _ t.-_ r Fl -rrurt l----1 e lî,-jJF,l qr: 5ll ll

I 6 1 I r 9A -.- ---

Fio lO Present-day extension of the Upper Norian-Rhaetian lithofacies of the Transdanubian Range. 1) Dachstein Limestone; 2) Kòssen Formation (restricted basin facies); 3) Kóssen Formation (basin-pÌatform cyclic transitional development); 4) Mótyóshegy + Csóvàr Formation; 5) Pre-Upper Norian formations; 6) facies boundary; 7) main tectonic line; 8) outcrop; 9) borehole. 258 J. Haas G T. Budai

graphy, extending over most of the Transdanubian Ran- genetic relation of the two areas. They present-day set- ge. Pervasively dolomitized cyclic shallow subtidal-peri- ting is probably a result of significant right-lateral di- tidal carbonate succession of about 1,000 m was formed splacements (Fig. 10). till the Middle Norian (Main Dolomite Formation). In In the Upper Norian-Rhaetian, a fairly definite the Late Norian-Rhaetian, the Dachstein Limestone was paleogeographic boundary can be drawn between the deposited on the platform, while the shaly Kóssen For- shaly inner basin facies of the Kóssen Formation and mation was accumulated in a newly formed back- the transition zone of the Kóssen and Dachstein Forma- platform basin in the N\l part of the Transdanubian tions. Non-cyciic, oncoidal facies of the Dachstein Range. Limestone probably indicates the offshore marginal The Kóssen Formation consists of dark grey, black zone of the platform. marls and shales with limestone interlayers - a restricted basin facies. Its thickness is 300-500 m Fig. 3). The thi- Discussion. ckness of the formation significantly decreases northeastward, where it interfingers with the Dachstein Lime- Based on the presented data and the outlined fa- stone and finally it pinches out. Three subunits can be cies trends, we have attempted to sketch the paleogeo- differentiated. In the SW part of the Transdanubian Ran- graphy of the area of the Transdanubian Range unit for ge, the formation is thick and predominantly shaly. Pre- the selected time slices. Palaeogeographic sketch maps sent-day extension of the formation was controlled by are shown in Fig. 11 a-f. They also demonstrate the changes the facies patterns Possibility Middle Cretaceous tectonism and subsequent denuda- of through time. of fitting the Transdanubian facies trends a wider pa- tion. In the western part of the Southern Bakony, sequen- in laeogeographic frame, that is in the Alpine domain, is ces are cyclic; they actually represent a wide interfingering also discussed below. zone between the Kóssen and Dachstein Formations. In the middle part of the Southern Bakony and in the North- Late Permian (Fig. 11a). ern Bakony, the Upper Norian-Rhaetian is represented by the Dachstein Limestone, stiil with a few meters thick grey Facies pattern came into being as a consequence pelitic interlayers of the Kóssen Formation. of the Late Permian transgression represenrs a complete The Dachstein Limestone is a carbonate platform series of facies from shallow subtidal lagoon through ti- sequence made up predominantly by cyclic alternation dal flat to alluvial paleoenvironments (Majoros, 1980; of peritidal and lagoonal facies. F{owever, non-cyclic pre- FIaas et al., 1988). Within the unit, facies boundaries are dominantly subtidal oncoidal development of the Dach- fairly well defined and oriented in a NV- SE direction. stein Limestone occurs in the NE part of the Transdanu- Upper Permian facies and their relations in the bian Range (Buda Mountains, blocks E of the Danube) Transdanubian Range show conspicuous similarities which began to accumulate probably in the Early No- with facies pattern in the Southern Alps (Majoros, rian (Balogh, 1981; Végh-Neubrandt, 1982). In the largest 1980). Close genetic relationships of the continental red- part of the Transdanubian Range, the Dachstein Limestone bed facies (Balatonfelvidék Sandstone and Val Gardena began to deposit somewhat later, in the Middle Norian; Formation resp.) are very likely. The Dinnls Doiomite more exactly, this was the time when pervasive dolomi- may correspond to the Fiamazza facies of the Bellero- tization of the platform carbonates (i.e. formation of the phon Formation (based on observed facies trends, corre- Main Dolomite) came to an end. In the S\X/ part of the sponding facies of the calcareous Badiota facies of the Transdanubian Range, in the area of the Kòssen Basin, Southern Alps might be located in the vicinity of Buda- the piatform prograded only after the infilling of the ba- pest, but they has not yet been encountered). The orien- sin in the latest Rhaetian. In the NE part of the Tran- tation of facies boundaries, taking also into considera- sdanubian Range, in the Buda Mountains and in the tion post-Triassic rotations, is N-S roughly coinciding blocks east of the Danube (in the Csóvór block), cherty with South Alpine directions. The boundary between limestone and dolomite sequences occur from the Car- marine and continental facies can be drawn between the nian to the top of the Triassic and even in the Lower Balaton Highland and the southern foreland of the Vértes Mountains in the Transdanubian Range; it is re- Jurassic (Kozur & Mock, 1991,;Kozur & Mostler, 1973). cognizable approximately valley the These sequences (Mótyàshegy Formation, Csóvàr For- at the Adige in Southern Alps (Assereto et al., 1973;Vopfner, 1.984). mation) may have accumulated in restricted intra- piatform basins, as well as on the slopes between the Early Triassic (Fig. 11b). platforms and the basins. Similarities in development of the oncoidal Dach- Akin to the Late Permian, three coeval facies zones stein Limestone, the coeval basin facies (Mótyóshegy and characferrze the Induan in the Transdanubian Range unit Csóvír Formations) in the Buda Mountains, and in the and the orientation of their boundaries are similar to the blocks east of the Danube, respectively suggest intimate Permian directions. The facies pattern is shown in Fig 12. P ermian-Trias s ic Transdanubian Ranse 259

a./ Late Permian b./ Earty Scythian

issl shslf +-

0 20kh

-t//À.t++-ffitv/lt.t+tJ|.ru c./ ùIiddle Anisian d.t

0 20kn

'Nl

-\ î.1 e.l Middle-Late Carnian - -..1 a t--:;-::;:_-fF,/*>:-_-H"\A \ ,/ _-^ \ ./ - -,{f**..}--'-,}*z l ./a:-;é"t:kif-- _- --- X-:-:-J--r,*-z^:- 0 mkn ,/ -./ o 2oh -4:--;,--.v- -r_-2fr>7{-_/7i*;o{/ -J--.-/ j/S;===--z;-- ,: zt*r .Et 2lrrlilill 3l I al-l

Fig.11 - Paleogeographic sketch ofthe relevant time slices: tTaLate Permian: 1) Balatonfelvidék Sandstone; z) Taba;d Evaporite; 3) Dinnyés Dolomite. 11b Early Triassic: 1) Kóveskll Dolomite; 2) Arócs Marl;3) Alcsútdoboz Limestone. 11c Middle Anisian:1) Felsòórs Limestone; 2) Megyehegy Dolomite + Tagyon Limestone. 11d Late Ladinian - Early Carnian: 1) Budaórs Dolomite; 2) Buchenstern + Fùred Limestone. 11e Middle-Late Carnian:1) Ederics Limestone, Sédvólgy Dolonite, Vadasken Dolomite, Nézsa Limestone;2) Veszprém-Sóndorhegy Formation; 3) Mityíshegy-Csòvir Formation. 11f Late Norian - Rhaetian: 1) Kòssen Formation (restricted basin facies); 2) Kóssen Formation (basin-platform cyclic transitional development); 3) Dachstein Limestone; 4) Mótylshegy + Cs6vír Formation.

The Arócs Formation was deposited in a very surface both in the Transdanubian Range and the South- shallow mud-shoal area, where a major part of the terri- ern Alps (Haas et al., 1988; Broglio l-origa et al., t990; genous material was trapped. Southwestward, behind the De Zanche et al., 1993). shoals, in a restricted lagoon dolomites were formed Facies pattern of the Transdanubian Range shows (Kóveskàl Dolomite), however input of fine siliciclastics definite similarities to that of the Southern Alps, where was remarkable during the early phase of accumulation a western and an eastern facies area can be distinguis- of the formation. Northeastward from the mud-shoal hed. Pasini et al. (1986, p. 8 and Fig. 3) assumed a paleo- zone, inner ramp environment with ooidic shoals high iocated in the vicinity of the Brenta Dolomites to ^rr can be assumed. Existence of ooidic shoals is proved by expiain this facies setting. The dolomitic and sandy the frequent oolirc interlayers in the shallow subtidal Lombardian-type Induan sequence (Servino Formation) carbonate sequences (Alcsútdoboz Formation). can be correlated with the Kóveskól Dolomite, whereas A thin oolite horizon is recognizable at the base the Mazztn Member in the Dolomites may correspond of every Induan formation, onlapping the transgression to the Aràcs Marl and the Alcsútdoboz Limestone, re- 260 /. Haas & T. Budai

Early Triassic

General facies model for the Early Triassic. spectively, or more precisely, it represents the rransition - a formation akin to the Lower Anisian Isz- zone between them. The oolitic basal member of the kahegy Limestone is known only from I-ombardy KÒveskól Formation and the Praso Horizon (Neri in Pa- (I-ower Angolo Limestone). sini et al., 1986, p. 163), as well as rhe lowermost oolitic Middle Anisian platform carbonate equivalents of beds of the Alcsútdoboz Formation and the Tesero Ho- the Megyehegy Dolomite (e.g. Dosso dei Morti Lime- rrzon are comparable with each other (Broglio loriga et stone, IJpper Serla Formation) can be found in many al.,1990). parts of the Southern Alps (Gaetani, 1.969; Gaetani et al., 1970; Pisa, 1974; Gaetani &. Gorza, 1989; Jadoul et (Fig. al., 1992b; Senowbary-D et al., 1993) but the intra- Middle Anisian 11c). ^ryaî platform basin facies of the Felsóórs Limestone shows In the Early Anisian, before the Pelsonian tectonic closer affinity with the Lombardian basin facies only activity, a shallow carbonate ramp came into being in (Upper Angolo ?, Prezzo Limestone). the area of the Transdanubian Range (Budai et al., 1993). Tn the Pelsonian, the ramp evolved to platform. Late Ladinian-Early Carnian (Fig. 11d). Later on this platform became dissected by normal faults (Budai & Vóròs, 1992). On the Balaton Highland After the Middle Anisian tectonic activity, and the paleofaults show a NV-SE orientation, as a rule. As most probably in relation with this, acidic volcanism a consequence of tilting of some blocks, narrow resrric- began at the end of the Illyrian. Subsequently, dissected ted basins were formed (Felsòórs Formation). Coevally, topography controlled the sedimentation for a short pe-

Middle Anisian

_..'-////^\ r.-.-^'=È_ :r,;;,!^!J,, _Fetsíórsis.,h

Fio lì General facies model for the Middle Anisian. in the areas remaining in uplifted position, shallow-ma- riod until a large pelagic basin ("Buchenstein Basin') rine carbonate accumulation was continued (Fig. 13). was formed in the area of the southwestern and central A similar tectonically-controlled facies pattern parts of the Bakony Mts. at the beginning of the Ladi- characterizes the Drau Range and the Southern Alps nian. Basin sequences are characrerizedby nodular, cher- (Bechstàdt, 1978; Bechstadt et al., 1978; Farabegoli & ty limestones and radiolarites with tuff interbeds, Guasti, 1980; Blendinger, 1983 etc.). Correlation of showing close relationships and indicating paleogeo- Middle Anisian facies zones, however, is difficult and graphic connections with time-equivalent formations in ambiguous. As compared with the Southern Alps, the the Southern Alps. In rhe area of the Eastern Bakony, following statements can be made (Budai, 1992): Vértes, and Buda Mts., a platform was formed at the - equivalent facies of the I-owermost Anisian same time ("Budaòrs platform') and carbonate accumu- Aszófò Dolomite are known both in l-ombardy (Car- Iation was interrupted by events of volcanic ash falls niola di Bovegno) and the Dolomites (Lower Serla For- only. Another platform can be assumed in the area of mation); the Keszthely Mts., but its extension is unknown. P ermian-Triass ic Transdanubian Range 261,

In contrast with the Southern Alps, the facies par- nous sedimentation became prevaient again (Haas, tern of the Transdanubian Range described above did not 1,ee4). change considerably during the Ladinian. Other differen- By the beginning of the Late Carnian (Fig. 1a) ces between the two domains are summarized belowt the basin in the area of the Balaton Highland filled up - In the Transdanubian Range, the "Buchenstein- to a large extent. In the shallow basin, carbonate accu- type" pelagic sedimentation lasted until the end of the mulation became prevalent and the upward shallowing Ladinian in starved basins, producing a condensed se- trend continued (Sóndorhegy Formation). At the same quence of very reduced thickness during this period. time, platforms began to prograde (Ederics Limestone, tùTengen - The volcanoclastic facies, characteristic Sédvólgy Dolomite, Vadaskert Dolomite). Joint effect of in the Upper Ladinian of the Southern Alps is missing upfilling of the basins and progradation of the platforms in the Transdanubian Range, except for a small areà led to the elimination of the topographic differences by ^t the northeastern end of the Bakony (Budai, 1992). This the end of the Late Carnian. This was the fundamental can be explained by the different paleogeographic set- prerequisite of the initiation of the evolution of the tings of the two areas. Volcanoclastics trapped in "\Wen- huge Dachstein Platform. gen-type" basins of the Southern Alps were transporred Upfiliing of the basins did not rake place in the from the south (Cros Ec Szabó, 1984; Pisa et al., 1980 intraplatform basins of the Buda Mountains and the etc.), consequently influx of volcanoclastic material Csóvàr block, where the terrigenous input was very re- could not reach the basins of the Transdanubian Range stricted and marginal slopes of the basins were probably located further to the north. too steep for significant platform progradation. - Pelagic carbonate sedimentation was continued The system of the Carnian basins and isolated even after the end of the volcanic activity during the platforms fits well into the paleogeographic picture of Cordevoiian. In contrast with the volcanoclastic Wen- the Southern Alps, the Drauzug, and the Northern Cal- gen-St. Cassian sequence of the Southern Alps, pelagic careous Alps, as was discussed in detail by Haas (1994). carbonates (Fùred Limestone) represent the lowermost The essence of this reconstruction is as follows. The Carnian in the Transdanubian Range. deep basin of the Northern Bakony was probably con- The platform progradation in the Early Carnian is nected with the basin assumed to be located offshore a common feature both in the Dolomites and the Bako- the shallow shelf of the Drauzug and the Northern Cal- ny - Balaton Highland area, resulted in step-by-step re- careous Alps (Hagemeister, 1988). The basin of rhe Bala- duction of the extension of the intraplatform basins (Bu- ton Highland, which was separated from the Northern dai & Vórós, 1,993). Bakony basin by a range of isolated platforms, may have

Middle-Late Carnian

/\tr\--s -- >- :,--- - .-rr""*fiffi- \À-= #4 t sídvótst ";;;íù"ì =--==-=-S'm r.n. Fig. 14 - General facies model for the ---' Middle-Late Carnian.

Middle-Late Carnian (Fig. 11e)- been in direct communication with the South Alpine Raibl Basin. At the end of the Early Carnian, as a consequence Essential elements of paleogeographic setting di- of increased terrigenous influx and a penecontempora- scussed above came into being already Middle neous sea level rise, carbonates were replaced by argilla- in the Triassic, as a consequence of tectonic segmentation of ceous sediments (Veszprém Marl Formation - Julian-Ear- ly Tuvalian, Oravecz-Scheffer, 1,987; Góczà.n et al., 1991) the Anisian platforms. Total upfilling of the basins led both in the basins and on the platforms. Extension of to the re-establishment of a levelled topography by the the platforms became markedly reduced, small isolated Late Carnian and to establishment of the large Late Tri- platforms (or ramps) came into being. In the middle assic Dachstein Platform, showing definite zonal facies part of the Carnian, a sea level drop may have resulted pattern. This setting is particularly favourable for deter- in an expansion of the incipientiy drowned platforms, minating the paleoposition of the displaced domains of and even in the basins carbonate sedimentation prevai- the Alpine-Carpathian-Dinarid system, as it was discus- led. Later on, due to a new sea level rise, fine terrige- sed by Kàzmér & Kovócs (1985), and FIaas et aI. (1995). LOZ /. Haas & T. Buclai

Late Norian-Rhaetian

.14--;Y;; t/---=' --.--...-: --

Rezi Dolomite General facies model for the Late Norian-Rhaetian.

Late Norian-Rhaetian (Fig. 11f). basinal formations suggest coeval existence of platforms in the vicinity. At the end of the Middle Norian, most probably The discussed facies setting confirmed our pre- due to joint effect of extensional tectonic motions and a vious conclusion on the general paleogeographic posi- eustatic sea level rise, basins were formed, which resul- tion of the Transdanubian Range unit. Its northeastern ted in the segmentation of the previously uniform car- part represents the offshore shelf margin, whereas its bonate platform (Fig. 1S). In the background of the southwestern part should be located the external remnant Dachstein platform, the large Kóssen Basin be- in (landward) zone of the shelf. This relationship of the gan to evolve, whereas a small intraplatform basin came facies fits well into the Late Norian-Rhaetian paleogeo- into existance in the inner zone of the previous graphic scheme of the Alpine domain. platform (Fekerchegy Basin), in addition to the survi- In the Southern Alps, a dolomitized platform car- ving intraplatform basins near to the offshore platform bonate series, the Dolomia Principale was formed from margin (Csóvír Basin). the latest Carnian onward. l-ombardy, intra- In the Late Norian, basically due to a climatically- In small platform basins began to form the Middle controlled increase in the terrigenous input (Kóssen in Norian, event), pattern of sedimentation significantly changed in the sites of accumulation of carbonates of the Aralalta the back-platform basin; carbonate sedimentation was Group (Jadoul et al., 1.992a), while on rhe platform de- substituted by argillaceous deposits and anoxic condi- position of the Dolomia Principale continued coevally. tions became prevalent. In the Late Norian, shales rich in organic matter began A low-angle slope was formed between the Dach- to be deposited in large areas of Lombardy, the Riva di stein platform and the Kóssen Basin where, controlled Solto Shale (Masetti et al., 1989; Jadoul et al., 1992a) by changes of the sea level, progradations and retrogra- showing great similarity to the Kòssen Formation. The dations of the platform resulted in an aiternation of the Riva di Solto Shale grades upward and eastward into the shaly basinal and calcareous platform facies (4th order Zu Limestone made up by cyclic alternation of the dee- Kòssen cycies - Haas, 1993). The location of this wide per-water shales and limestones of shallower facies. The transitional zone and its boundary towards the inner ba- zone of laterai transition between the restricted basin sin facies are fatly easily recognizable. The inner part and the platform can be drawn between the Adige val- of the Kóssen Basin was located in the area between the ley and Lake Idro (Masetti et a1., t989). East of this ZaIa Basin and the Keszthely Mountains, whereas rhe zone, plafform carbonates accumulated coevally and are transitional zone may be recognized in the western parr pervasively dolomitized, as a rule (Dolomia Principale). of the Southern Bakony. In the Northern Bakony area, In the Late Rhaetian. the shailow-water carbonares ex- platform accretion was interrupted for short episodes tended over the area of the former basins in l-ombardy only during intervals of maximal flooding (intercala- (Conchodon Dolomite). tions of the Kóssen Formation), whereas in the area of In the Northern Calcareous Alps, due to the Gerecse and Pilis Mountains the evolution of the downfaulting of the piatform margin the pelagic facies platforms was continuous during the Late Norian - zone (Hallstafr zone) significantly expanded during the Rhaetian interval. Norian (Lein, 1987). In the Late Norian, an increase of In the Buda Mountains and in the blocks on the the terrigenous influx resulted in change in the sedimen- east side of the Danube, the topmost part of the tary pattern (Zlambach Marl). platform carbonate sequence is missing due to sub- In the Dachstein facies zone of the platform (in sequent erosion. In the same region, the predominantly the sense of Prey, 1928) located in the southern part of carbonate sedimentation continued in the intraplatform the Northern Calcareous Alps, as far as near Salzburg, basins (Mótyóshegy and Csóvór Formation). Resedimen- deposition of the Dachstein Limestone was continued ted bioclasts and lithoclasts of platform origin in these until the end of the Triassic, except for sequences in the Permian-Triassic Transdanubian Ranpe 263

Tirolikum unit, paleogeographicaily representing the metry and small size of the basins and platforms do nor most external parts of the Dachstein facies zone (Gole- allow exact reconstructions. biowsky, 1990). in this unit, the Kóssen Formation ap- 6. In the Ladinian, the facies patrern is simpler. A pears as a thin intercalation within the Dachstein Lime- large platform ("Budaòrs Platform') and a large basin stone. ("Buchenstein Basin") came into existence in the Tran- In the Hauptdolomit facies zone (some parrs of sdanubian Range area. The latter can be correlated with the Tirolikum and the Bajuvarikum), bituminous dolo- the iargest intraplatform basin in the central sector of mites are overlain by the Upper Norian Plattenkalk, the Southern Alps, although numerous smaller plat- which can be considered as a transirional formation be- forms make the picture more complicated. t'ween the platform facies and the Kóssen basin facies 7. In the Transdanubian Range only local and sub- (Fruth & Scherreiks, 1975). The lower part of the Kòs- ordinate occurrence of Vengen-type volcanoclastics is sen Formation is made up by cyclic alternation of shales consistent with the assumed paleogeographic position of with bivalve coquina interlayers and shallow-water car- this unit north to the Southern Alps. bonates. The upper part of the formation consists of 8. In the Carnian, the extension and position of bioclastic limestones and shales (Golebiowsky, 1990). By platforms and basins significantly changed. The forma- the Late Rhaetian large parts of the basin were filled up, tion of a northern and a southern subbasin, separated and carbonate platforms were re-established ("Oberrhdt" by a belt of carbonate platforms, can be assumed. This Limestone). picture easily fits into the formerly published paleogeo- The outpinching zone of the Kóssen Formation ro- graphic reconstructions for the Drauzug - Northern wards the Dachstein platform carbonates, located in the Calcareous Alps and the Southern Alps, respectively. middie part of the Southern Bakony in the Transdanu- 9. The Early - Middle Norian was rhe era of the bian Range, can be fitted to nappes of the Tirolikum in Iargest extension of the "Dachstein platform". Facies zo- the Northern Calcareous Alps and to the zone between nation described in the Northern Calcareous Alps could the Adige valley and Lake Idro in the Southern Alps. also be recognized in the Transdanubian Range. Oncoi- dal outer platform, Lofer-cyclic, partly dolomitized inner platform and organic rich, dolomiric back-platform Conclusions. facies zones were recognizable in both areas (Haas et al., 1. Facies patterns of the Upper Permian and Trias- \995) and a similar trend was also detected in the South- sic formations within the Transdanubian Range Unit ern Alps, although dolomitization was much more ex- may provide a base for the reconstruction of the original tensive in the latter area. structural and paleogeographical setting of this unit. An 10. In the Late Norian - Rhaetian, the "Kóssen improved, more precise reconstruction can be attained by Basin", the "Dachstein Platform" and the transitional paleogeographic analysis of a series of time slices. zone between them can be followed both in the North- 2. In the Late Permian, a complete tracf of facies ern Calcareous Alps and the Southern Alps, offering is known from a continental alluvial ro a coasral sabkha another opportunity for fitting the facies zones. - shallow lagoon environment, and the fitting with rhe 11. Considering the entire 40 Ma Late Permian - South Alpine facies zones (Val Gardena - Bellerophon Triassic interval, the Transdanubian Range unit shows a Formation) is good. definite paleogeographic polarity: its northeasrern parr 3. The lcwermost Triassic is also characterízedby represents the seaward (internal) side, whereas its definite facies zonation: a restricted ramp (lagoon), a southwestern part represents the landward (external) mud-shoal zone and an ooidic outer ramp environment side. can be distinguished. These zones are also correlatable 12. The Transdanubian Range seems to be the with the South Alpine zones - the mud-shoai zone may "missing link" between the Southern Alps and the Up- correspond with the "threshold" facies of the Brenta per Austroalpine nappes. Based on the correlation of Dolomites. the facies zones, the fitting of the Transdanubian Range 4. In the Induan to the Early Anisian, the facies to the Southern Alps may be accomplished x'ith a fairl,r' differentiation .was the least definite. On the uniformly good approximation (with an error of 10-20 km). As to and moderately subsiding shelf, open ramp then restric- the Northern Calcareous Aips, due to its complicated ted ramp environments came into being, followed by nappe structure, less favourable orientation of the facies establishment of the first carbonate platforms in the zones, and more limited data, the uncertainty is greater Middle Anisian. t)u-r)u/F^ , F^ Kmt.I \ 5. In the Middle Anisian, intraplatform basins 13. The essence of the reconstruction for the stu- were formed by normal faulting in the Transdanubian died interval is as follows: Range. They were probably related to basins of similar - the Zala basin and the western part of the South- origin in the Southern Alps. However, complicated geo- ern Bakony may have been located between the North- 264 J. Haas & T. Budai

ern Karawanken Range, as well as the Bajuvarikum, and part of the Tirolikum and the Carnic Alps, Southern the Bergamo Alps (I-ombardy), respectively; Karawanken Range, and the Juiian Alps. - the eastern part of the Southern Bakony, the Northern Bakony, and the Vértes Mts. may have been situated between the western part of the Tirolikum and Acknouledgements, This work was funded Research Fund the Dolomites; by the National (OTKA) grant No 2671. Authors wish to thank prof. Maurizio Gae- - the Buda Mts. and the blocks on the east side of tani, dr. Eduardo Garzanti and an anonymous reviewer for reviewing the Danube may have been located between the eastern the paper and valuable suggestions.

REFERENCES

Assereto R., Bosellini A., Fantini Sestini N. & Sweet 'W. C. Budai T. & Vórós A. (1993) - The Middie Triassic events of (1,973) - The Permian-Triassic boundary in the Southern the Transdanubian Central Range in the frame of the Alps (Italy). In Logan A. & Hills L. V. (Eds.) - The Alpine evolution. Acta Geol. Hung., v. 36, n. i, pp. 3- Permian and Triassic systems and their mutual bounda- 13, Budapest. ry. Alberta Soc. Petrol. GeoL. Mem., v. 2, pp. 176-199, Budai T., Lelkes Gy. & Piros O. (1993) - Evolution of Middle Calgary. Triassic shallow marine carbonates in the Baiaton Balla Z. (1982) - Development of the Pannonian basin base- Highland (Hungary). Acta Geol. Hung., v.36, n. 1, pp. ment through the Cretaceous-Cenozoic collision: A 1,45-165, Budapest. new synthesis. Tèctonopbysics, v. 88, pp. 61,-102, Amster- Cros P. Ec Szabó I. (1984) - Comparison of the Triassic volca- dam. nogenic formations in Hungary and in the Alps. Paleo- Balogh K. (1981) - Correlation of the Hungarian Triassic. geographic criteria. Acta GeoL. Hung., v. 27, n. 3-4, pp. Acta Geol. Hung., v. 24, n. L, pp. 3-48, Budapest. 16J-l/ 6. tlu(laDest. Bechstàdt Th. (1978) - Faziesanalyse permischer und triadi Csontos L., Nagy-a.osy A., Horvàth F. Er Kovíc M. (1992) - scher sedimente des Drauzuges als Hinweis auf eine Tert:nry evolution of the Intra-Carpathian area: a mo- grossraumige Lateralverschiebung innerhalb des Ostal- del. 7èctonoplryslcs, v. 208, pp. 221,-241,, Amsterdam. ptns. Jb. Geol. B.-A.,v. 721, n. 1, pp. 1-121, \lien. De Zanche V., Gianolla P., Mietto P. & Siorpaes Ch. (1993) - Bechstàdt Th., Brandner R., Mostler H. & Schmidt K. (1978) Triassic sequence stratigraphy in the Dolomites (Italy). - Aborted rifting in the Triassic of the Eastern and Mem. Sc. Geol., v. 45, pp. 1-27, Padova. Southern Alps. N. lb. Geol. Palàont. Abh., v. 156, n. 2, Detre Cs. (1,970) - Palàontologische und sedimentologische Yr'nn '"'| ì/- ^'| /X \lrrltoall, IJntersuchungen úber die Triasschollen in der Umge- Blendinger \f. (1983) - Anisian sedimentation and tectonics bung von Csòvír, Nézsa und Keszeg. BuLl. Hung. Geol. on the M. Pore-M. Cernera area (Doiomites). Rio. It. .loc., v. 100, pp. 173-184, Budapest. Paleont. Strat., v. 89, n. 2, pp. 175-208, Milano. Farabegoli E. & Guasti M. (1980) - Anisian lithostratigraphy Bóckh J. (873) - Die geologischen Verhdltnisse des súdlichen and paleogeography oÍ M. Rite (Cadore, Southeastern Theiles des Bakony (I. Theil). Mitt. labrb. Kón. Ung. Dolomites). Ria. It. PaLeont. Strat., v. 85 (1979), n. 3-4, Geol. Anstalt, v. 2, pp. 27-1,82, Budapest. pp. 909-930, Milano. Brezsnyànszky K. t{ Haas J. (1986) - Main features of the Fùlóp J. (i990) - Magyarorszàg geológiíja. Paleozoikum L V. Pre-tertiary basement of Hungary. Geol. Zbornih - GeoL. of 325 pp, Flungarian Geol. Inst., Budapest. Carpatbica, v. 37 , n. 3, pp. 2973A3, Bratislava. Fruth J. & Scherreiks R. (1975) - Facies and geochemical cor- Brogiio Loriga C., G\czin F., Haas J., Lenner K., Neri C., relation in the Upper Hauptdolomit (Norian) of the Oravecz - Scheffer A., Posenato R., Szabó I. & Tóth eastern Lechtaler LIps. Sediment. Geol., v. 13, pp. 27-45, Makk A. (1990) - The Lower Triassic of the Dolomites Amsterdam. (Italy) and Transdanubian Mid Mountains (Hungary) Gaetani M. (1969) - Osservazioni paleontologiche e stratigrafi- and their correlation. Mem. Sc. Geol., v. 42, pp. 6l-113, che sull'Anisico delle Giudicarie (Trento). Rit. It. Pa- Padova. leont. Strat, v.75, n. 3, pp. 469-546, Milano. Budai T. (1992) - Middle Triassic formations of the Balaton Gaetani M. & Gorza M. (1989) - The Anisian (Middle Trias Highland and of the Southern Alps. Stratigraphic corre- . sic) carbonate bank of Camorelli (Lombardy, Southern Iation. Acta Geol. Hung., v. 35, n. 3, pp. 2L7-23a, Buda- Alps). Fzcies, v. 21, pp. 4l-56, Erlangen. pest. Gaetani M., Premoli Silva I. k Zanín Buri C. (1970) - Calca- Budai T. & Vòròs L. (1992) - Middle Triassic history of the re di Dosso dei Morti. In Formazioni geologiche, fasc. Balaton Highland: extensional tectonics and basin evolu- IY. Studi illustr Carta GeoL. Italia, pp. 21-32, Roma. IlOn. AC|A '\/-lJV, lJtJoa- Góczàn F., Oravecz-Schef{er A. & Csillag G. (1991) - The Dest. stratigraphic characterizatron of the Cordevolian and Ju- P ermian- Triassic Transdanubian Range 265

lian Formations of the Csukrét Ravine, Balatoncsicsó. tic lineament system: Evidence for conrinental escape Ann. Rep. Hung. Geol. Inst. 1989, pp.241-325, Budapest. of the Bakony-Drauzug l-lnit. Acta Geol. Hung., v. 28, G6czó,n F., Oravecz-Scheffer A. & Haas I. (1987) - Permian- n. 7-2, pp.71- 84, Budapest. Triassic boundary in the Transdanubian Central Range. Kozur FI. & Mock R. (1991) - New Middle Carnian and Acta Geol. Hung., v. 30, n. 7-2, pp. 35-58, Budapest. Rhaetian Conodonts from Flungary and the Alps. Stra- Golebiowsky R. (1990) - The Alpine Kòssen Formation, a tigraphic Importance and Tectonic Implications {or the key European for topmosr Triassic correlatíons. Alber- Buda Mountains and Adjacent Areas. Jb. Geol. B.-A., v. tiana, v. 8, pp. 25-35, Utrecht. 134, pp.27l-297,Vren. Gradstein F.M., Agterberg F.P., Ogg J.G., Hardenboi J., van Kozur H. Ec Mostler H. (L973) - Mikrofaunistische lJntersu- Veen P., Thierry J. & Huang Z. (1994) - A Mesozoic chungen der Triasschollen im Raume Csovir, IJngarn. time scale. lourn. Geopb. Àes., v. 99 (812), pp. 24,Af- Wrb. Geol. B.-A., v.973, n.2, pp.297-325,.Vfien. 24,A7 4, Y/ashington. Lein R. (1987) - Evolution of the Northern Calcareous Alps Haas J. $987) - Position of the Transdanubian Central Range during Triassic times. In Flùgel H.\L E{ Faupl P. (Eds.) structural unit in the Alpine evolution phase. Acta - Geodynamics of the Eastern Alps, pp. 85-102, Franz Geol. Hung., v. 30, n. 3-4, pp. 243-256, Budapest. Deuticke,'Wien. Haas J. Q,993) - Formation and evolution of the Kóssen Basin I-nczy L. sen. (1916) - Die geologischen Formationen der Ba- in the Transdanubian Kange. Bull. Hung. Geol..Soc., v. latongegend und ihre regionale Tektonik. Result. uissen- 1,23, n. I, pp. 9-54, Budapest. scbaft. Erforscbung Balatonsees, v. 1., n. 1,716 pp., Vien. Haas J. $994) - Carnian basin evolution in the Transdaau- Majoros Gy. (1980) - Problems of Permian sedimentation in bian Central Range, Hungary. Zbl. Geol. Palàont., Tetl the Transdanubian Central Mountains: a paleogeo- 1.. 1,992H. 11/12, pp. 1233-1252, Stuttgan. graphic model and some conclusions. Bull. Hung. Geol. Haas J., G6czàn F., Oravecz-Scheffer A., Barabàs-Stuhl A., Soc., v. 110, n. 3-4, pp. 323-341., Budapest. Majoros Gy. 8< Bérczi-Makk A. (1936) - Permian-Trias- Masetti D., Stefani M. & Burchell M. (1989) - Asymmetric sic boundary in Hungary. Mem. Soc. Geol. It., v. 34, pp. cycles in the Rhaetic facies of the Southern Alps: zztz+1, lJ.ofna. plat{orm-basin interactions governed by eustatic and cli- Haas Kovics S., Krystyn L. & Lein R. (1995) - Significance J., matic oscillations. Rlz. It. Paleont. Strat., v.94, n. 3, pp. Late of Permian-Triassic facies zones in terrane recon- 401-424, Milano. structions in the Alpine-North Pannonian domain. Tec- Oravecz-Scheffer A. (1987) - Triassic Foraminifers of the tonoplrysics, v. 242, pp. 19-40, Amsterdam. Transdanubian Central F.ange. Geol. Hung. ser. Paleont., Haas Tóthné Makk 4., Oravecz-Scheffer F., J., A., Gíczin v. 50,331 pp., Budapest. Oravecz & Szabó I. (1988) - Alsó-triisz alapszelvé- J. Pasini M., Conti M. A., Mariotti N., Nicosia U., Cassinis G., nyek a Dunàntúli- Kózéphegységben (Lower Triassic Oddone M., Vannucci R., Massari F., Fontana D., key sections in the Transdanubian Mid-Mountains). Giobbi E., Ramovs A., Broglio l-origa C., Neri C., Po- Ann. Inst. Geol. Publ. Hung., v. 65, n. 2,356 pp., Buda- senato R., Flúgel E., Noe S., Demelia Pittau P., Amico Pest. C. D., Farabegoli E., Gabriele Ori G., Perri C. & Ven- llagemeister A. (1988) - Cyclic Sedimentation on a Stable turini C. (1986) - Permian and Permian-Triassic bound- Carbonate Platform: The Raibl Beds (Carnian) of the ary in the South-Alpine segment of the Western Tethys. Drau Range,/Carinthia (Austria). Facies, v. 18, pp. 83- Excursion Guidebook, pp. 1-158, 122, Erlangen. Brescia. Peters K.F. (1859) - Geologische Studien Flauer F. (1862) - Úber die Petrefacten der Kreideformarion aus lJngarn II. Die 'Waldes. Umgebung von Visegríd, Gran. Totis u,nd Zsàmbék. des Bakonyer Wrhandl. k.k. Geol. Reicbsanst. Jb. Geol. R.-A., v. 10, pp. 485-521, Sitzb., v. 44, pp. 631-659, \lien. \7ien. Pisa G. (1974) - Tentativo ricostruzione llofmann K. (1871) - Die geologischen Verhàltnisse des Ofen- di paleoambienrale e paleostrutturale dei depositi di piattaforma carbonatica Kovócsier Gebirges. Mitt. /abrb. Kón. ung. Geol. Anstalt, v. 1, pp. 149-235, Budapest. medio-triassica delle Alpi Carniche sud-occidentali. Mem. Sc. Geol. Ital., v. 13, 1, Jadonl F., Berra F. Ec Frisia S. (1992a) - Stratigraphic and pa- n. pp. 35-83, Padova. Pisa G., Castellarin leogeographic evolution of a carbonate platform in an A., Lucchini F., Rossi P.L., Simboli G., extensional tectonic regimer the example of the Dolo- Bosellini A. & Sommavilla E. (1930) - Middle Triassic mia Principale in Lombardy (Italy). Rio. It. Paleont. magmatism in the Southern Alps. L: A review of gene- Strat., v.98, n. 1, pp.29-44, Milano. ral data in the Dolomítes. Rit. It. Paleont. Strat., v. 85 Jadoul F., Gervasutti M" & Fantini Sestini N. (1992b) - The (1979), n. 3-4, pp. 1093-1 1 10, Milano. Middle Triassic of the Brembana Valley: preliminary Prey S. (1978) - Rekonstruktionversuch der alpidischen study of the Esino Platform (Bergamasc Alps). Rlz. 1r. Entwicklung der Ostalpen. Mitt. Òsterr. Geol. Ges., v. Paleont. Strat., v. 98, n. 3, pp. 299-324, Milano. 69, pp. 1-25, \W'ien. Kàzrr'ér M. (1984) - Lateral displacement of the Bakony in Senowbary-Daryan B., Zùhlke R., Bechstàdt Th. & Flùgel E. the Paleocene. General Geol. Rea., v. 20, pp.53-101, Bu- (1,993) - Anisian (Middle Triassic) Buildups of the dapest. Nonhern Dolomites (Italy): The Recovery of Reef Kàzrr'ér M. & Kovícs S. (1985) - Permian-Paleogene paleogeo- Communities after the Permian/Triassic Crisis. Facies. graphy along the easrern part of the Insubric-Periadria- v.28, pp. 181-256, Erlangen. 266 J. Haas tn T. Budai

Taeger H. (1912) - Tovóbbi adatok a Bakony fóldtani viszo- Végh-Neubrandt E. (1982) - Triassische Megalodontaceae. nyalhoz. Ann. Rep. Hung. Geol. Inst. 1911, pp. 61-66, Entwicklung, Stratigraphie und Palaontologie. V. of 526 Budapest. pp., Budapest. Taeger H. (1913) - A tulajdonképpeni Bakony délkeleti részé- Wopfner H. (19s4) - Permian deposits of the Southern Alps nek szerkezeti alapvonósai. Ann. Rep. Hung. Geol. Inst. as product of initial aipidic taphrogenesis. GeoL. Rund., 1912, pp. 756-170, Budapest. v.73, n. 1, pp. 259-277, Stuttgart. Telegdi-Róth L. (1929) - Magyarorszàg geologiója I. rész (Geo- logy of Hungary), Pécs. Yadisz E. (1960) -Magyarorszàg fóldtana (Geology of Hunga- ry), Budapest. Received February 21, 1995; accepted September 11, 1995