And Outer Carpathian Basins

Rivista Italiana di Paleontologia e Strirtigrafia volutì]1' I I u no. I 'r'rYt'" 5- 1'' I April 2004

JURASSIC PALEOGEOGRAPHY OF THE PIENINY AND OUTER CARPATHIAN BASINS

TAN GOLONKA' E MICHAI- KROBICKIT

Receiu-ecl September 19,2002; accepted Ju$ 26, 2003

Key 'iuortls: Jurrssic, Carpathians, Tethvs, plate tectonics, plle- Masun costituisce la parte più nreridionale dei Flysch Carpatici Ester- or:eography. ni). Il rilt di Pieniny si è aperto durante il Pliensbachiano - Aaleniano. UAtlantico centrale e la Tetide alpin:r subirono uno stadio di drifting Abstr,tct. The Jurassic hisrory of the Pieniny/Outer Carpathian durente il Giurassico nredio. basins reflects the evolution of the Cìrcum-Tethyan area, especillly its I-a storir tardo-giurassic;r (Oxfordiano-Kimnierideiano) del Ba- Alpine Tethys pirrt. The Alpine Tethvs that is Ligurian, Penninic Ocerns cino di Pieniny/Magura rifletre una più nrrrcata differenziaz-ione di fa- and Pieniny/Magur;r Brsin constitute the extcnsion of the Centrll At- cies ;rll'interno dei bacini sedimentari in cui aveva luoso una deposizio- lantic systenr. Thc synrift sr,rge lastecl in the Pieninl'/Mrgur;r Basin ne nrist,r siliceo-carbonatica. Un effetto di malgior approfondimento è from late Eerlv Jurassic to Tithonian (the Magura Unir constitutes the indicato dalle diffuse radiolariti oxfordiane, che si ritrovano in turte le southernnrost pirrt of the Outer Flysch C:rrpathìans). The Pieniny rift successioni bacinali, mentre la zona nreno prolonda è, ìn quel periodo, opened durinu Pliensbachian - Aalenian. Thc central Atlantic and Alpine cor.npletlnrente priva di intercalazioni silicee (sedinrentaz-ione dalla facies Anrnronitico Rosso Tethvs went into a drifting strrfle durinfl the Middle Jurassic. di fino al calcare di scogliera corallina). parte The I-;rte Jurassic (Oxfordian-Kirnnreridqian) history of the Lir nreridionale della Pilttaforma Europea Settentrionale, Pieniny/Magura Basin reflects stronsest facial differentiarion with- a Nord del re;rrne di Pieniny/Magura, ha cominciato a essere rnteressa- in sedinrent,rry basin where nrixed siliceous-cf,rbonrte sedinrentltion t;r da rifting dur;rntc il Giurassico superiore, e sono stari creati il Baci- took place. Grerrtest deepenins elfect is indic:rted by widespread Ox- no della Slesia nei Carpazi Esterni occidentali ed il Bacino di Sinaia nei fordian radiolerites. which occur in the all basinll successions, rvhere;rs Carpazi Orientali, con marne nere, principalmente ridepositate. I bacini esterni the shallowest z-one is completely devoid of siliceous intercirlrrtions at satellite si sono differenziati durante l'ultima fase di sviluppo bacinalc (Hauterìviano-Barremiano). l-a connessione del bacino della thrt time (sedinrentation from Amnronitico Rosso facies up to c<;rtrl reef limestone). Slesia con Sinaia e con le aree sud-carpatiche di Severin suggerisce la di- rezione NV-SE dell'asse del bacino, mentre The southern part of the North European Platforn.r, norrh fronl I'orientazione della Catena di Klippen di Picniny/Bacino di Masura era SV-NE. nei bacini the Pieniny/Maeurl re:rlm, started to be rifred durins Late Jurrrssic time Quindi sono possibili due direzioni Carpatichc Esterne perpendicolari. and Silesian B,rsin in the Outer Western Carplthians and Sinaia Basin Duronte il Titoniano-Berriasiano è avvenuta una nraggior rior- in the E;rstern Ciìrpirthiiìns, s,ith black, nrainlv redeposited m;rrls have ltnizzttzione, rispecchiata sia dir cxmbianlenti pxleoceanografici che pa- been created. The outer sub-basins rvere differentiated durins the l;rtest leoclinratici. GIi eventi tettonici Neocimmerici, così conre la fase prin- (Hauterivìan-Barremìan) phase of basinll developn.rent. The conncction cipale dell'apertura dei bacini dei Carpazi Esterni è connessa a quesra of Silesi;rn Basin rvith Sinaia and Southern Carplthian Sevcrin .rrerrs sus- riorsan izzazion e. gests the NV-SE direction of the basinal ,rxis u,hile the oricntation of the Pieninv Klippen Belt/Magura Basin u,;rs S\W-NE; so, tn'o Ourer C.rr- pathian perpendicul;rr directions are possible rvithin the b.rsins. M;rior reorslnizrtion happened during the Tithonian-Berria- Introduction sian time. It rvas reflected by both plleoceanographic;rl ancl pllcocli- matical ch;rnges. The Neo-Cimr.neriln tcctonic evenrs irs rvell .rs nrlin phase of the Outer Carpathi;.rn b;rsins opening is connected with this The Outer Carpathian and Pieniny Klippen Belt reorgan iz-ation. realm (Fig. l) are the northernmost part of the Polish Carpathians. Their palinspastic reconstructions attempt Riassunto. La storia giurassica dci bacini di Pieninv/C.rrp:rtici to restore the age and past location of basins, their age, Esterni riflette I'evoluzione dell'erea circurl-tetidea, speci;rlnrente del- their floor or basement, relations to the surrounding crus- h sua p,rrtc di Tetide alpina. La Tetide :rlpin;r, ossia gli Oceani I-igure e tal elements as well as character of the paleostructural el- Pennidico ed il tsrcino di Pieniny/Magurr costituisce I'estensione clel sistenrr rthntico centriÌle. Lo stadio di sin-rift è durato nel B:rcino di ements separating them. All this goals are still not easy Pieniny/Magur;r drl tardo Giurrssico infc'riore al Titoniano (l'Uniti di to achieve, many problems have to be solved and many

I Jaeiellonian Universitv, Oleandry 2a, 30-063 Krakórv, Poland. E-nrail: golonk;ì(rr gcos.ing.u j.edu.pl 2 University ol Mininq;rnd MetallurrÌr,, Mickiewicza 30, 30-059 Krak

l:ig. I - Tectonic sketch map of the A lpi n e-C arpat h ian-P:rn n on - i.rrr-DinariJr b,rsin systcnr (after Kor'íò et al. 1998, simplified).

Tertiary Molasse Zone Flysch Belt Pre - Neogene of inner orogenrc zones Neovolcanic areas

pitfalls have to be avoided. This paper discusses sorne Outline of geology problems related mainly to the Jurassic stage of the Car- pathian realm developmenr. This was the age of basins The Northern Carpathians are subdivided into opening (Fig. 2). The basin closure is another issue with an older ranse known as rhe Inner Carpathians and the an additional set of problems. younger ones, known as rhe Ourer or Flysch Carpathians Four time interval nlaps were constructed which (Fig. 1 ). Ar the boundary of these rwo ranges the Pieniny depict the Jurassic-earliest Cretaceous plate tectonic Klippen Belt (PKB) is situated. The Outer Carpathians conficuration, paleogeography and lithofacies of' the cir- are built up of a stack of nappes and thrust-sheets chang- cur.n-Carpathian realnr (Figs. 3-6). The aim of this paper ing along the Carpathians built mainly of flysch. All the is to provide an ourline of the plate tectonic evolution Outer Carparhians nappes are overthrusting onto the paleogeography and position of the major crustal ele- European platform covered by Miocene deposits of the ments of rhe area within the global fran.rework. Therefore, Carpathian Foredeep. These nappes have allochthonous the authors restricted the number of plates and terr,rnes character, and orisinated in basins situated outside their modeled, trying to utilize the existin-g information and present location. The Magura Unit form the innernrost degree of certainty. The authors has tried to apply geo- part of Outcr Flysch Carpirthian Belt. The Macura sub- n.retric rnd kinematic principles, using conlputer technol- basin deposirs were incorporated into the Outer Flysch ogy, to model interrelations between tectonic componenrs Carpathian Belt as rvell irs into the Pieniny Klippen Belt along the Eurasian n.rarsin and in the surroundins areas. during the Cenozoic orosenic process (Birkenmajer 1986; The maps were consrructed using a plate tectonic nrod- Golonka er al. 2000). el, which was consrructed usins PLATES and pALEO- The Outer (Flysch) Carpathians are con.rposed of MAP software (see Golonka 2O0O; Golonka et al. 2OOO; flysch sequences raneing in ase from Jurassic to Early Golonka tr Krobicki 2OO1), which integrare compurer Miocene (Sl4czka 1996). These deposits were folded and uraphics and data manasenlenr technolosv with a highlv overthrust during the Miocene time (Alpine orogeny), structured and quantitative description of tectonic rela- forminq north-versins nappes detached from their origi- tionships. The heart of this prosranl is the rotation file, nalbasenrent (Sl4czka 1996). The Pieniny Klippen Belt is which is consranrly upd:rted, as new paleom,.rrnetic dirta composed of several successions of mainly deep and shal- become available. Hor-spot volcanics serve as referencc low-walter linrestones, covering a rime span fron.r rhe Ear- points for the calculation of paleolongirudes (Golonka ly Jurassic to Late Cretaceous. This strongly tectonized & Bocharova 2000). structure is a terrain of about 600 km long and 1-20 km Pa I eogcogra pb1' of tbc Pi cn i n 1, 7

Fig. 2 - Highly schematic (not to scale) NW SE profiles shoiving the evolution of the Pieniny Klippen Belt/ Magura Basin during theJuras- + + + +L------:-- + + + + sic-elrliest Cret:rceous tinre.

EARTY JUNASSIC

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cffiatqutr IJJJJ;I II atata f++++.1 ll -l !a3 tt f^^.l f---v " vl .. lpmcquqoua DFot lv 1.., ^ | --]l t"l t tIatoE t'-- -l otoaf,ctgtHAu I---t l-l

wide, which stretches fron.r Vienna to the \ùlest, to Ro- lv Cretaceous pelagic cherty limestones (Maiolica type maniil to the East (Fig. t). The PKB is separated from facies) and radiolarites were also deposited in northwest- the present-day Outer Carpathirrns by the Miocene sub- ern (Magura) subbasin. This extremely deep-water basinal vertic:rl strike-slip fault (Birkenmajer 1986). zone of the southern Magura Subbasin is known as Magu- During the Jurassic and Early Cretaceous within ra Succession (equivalent of tectonic Grajcarek lJnit, sen- the Pieniny Klippen Belt/Magura Basin the submarine su Birkenmajer 1970,1986) or Hulina Unit (Golonka tr Czorsztyn Ridge and sourrounding zones ("pelagic Sikora 1981; Golonka et al.2000,2003; Golonka & Kro- swell" - Misík 1994) were an elongated structure with bicki 2002). The paleogeographic extent of the Magura don-rin;rtion of pelagic type of sedimentation. The ori- Subbasin remains somewhat enigmatic and speculative. entation of the Pieniny Klippen Belt/Magura Basin was Also speculative is existence of oceanic crust below the S\í-NE (see discussion in Golonka & Krobicki 2001). whole Masura basin. The presumable transitional slope This basin was divided into the northwestern and south- sequence is known from some outcrops located north of eastern subbasins by the Czorszryn Ridge (Fig. 2). The the Czorsztyn Ridge (such as Zasviasy and Stare Bystre deepest part of the southeastern (Pieniny Klippen Belt) in Poland) (Golonka & Krobicki 2002). fudge sequences subbesin is docurnented by extremely deep waterJurassic- as rvell as transitional slope sequences are also called Ora- Early Cretaceous deposits (pelagic limestones and radi- vicur-r-r (e.g. PlaSienka 1999). Generaly, the Pieniny Klip- olarites) of Zlrna Unit (Golonka 8r Sikora 1981; Golon- pen Belt/Magura Basin history is tripartite (i-iii) - from ka & Krobicki 2002) lirter described also as Ultra-Pieniny the (i) oxysen-reduced dark/black terrigenous depos- Succession (Birkenrnajer 1988; Birkenmajer et al. 1990) its of the Early-early Middle Jurassic age (Fleckenkalk/ or Vahicum (e.g. PlaSienka 1999). The transitional slope Fleckenmergel facies) trough (ii) Middle Jurassic-earli- sequences between deepest basinal units and ridge units est Cretaceous crionoidal, nodular (of the Ammoniti- are known as Pieniny, Branisko (Kysuca), and Niedzica co Rosso type) or cherty (of the Maiolicar : Biancone successions (Fig. 2) . The strongly condensed Jurassic-Ear- type) limestones and radiolarites up to the (iii) Late I. Golonka &. M. Krobichi

Fig. 3 - Paleogeography of the cir- EURASIA cum-Carpathian area during Early J urassic; plates position at 195 Ma (after Golonka et al. 2003, modified). Abbre- viations of oceans and plates names: Ad - Adria (Apulia), Do - Dobrogea, EA - Eastern Alps, IC - Inner Carpathians, Li - Ligurian rift (site of future Ligurian Ocean), Me - Meliata/Halstatt Ocean, Mo - Moesia plate, PB - Pieniny Klippen Belt rift (site of future Pieniny Klippen Belt /Magura Basin), Pn - Penninic rift (site of future Penninic Ocean), Rh - Rhodopes, Sr - Sardinia, Ti - Tisa plate, Tr - Transilvanian Ocean, Va - Vardar Ocean.

LEGEND

tl LAND OR I)NEP OCDAN BASIN ACTIW SUBDUCTION ZONE LITTLE OR NO SEDIMENTS :JJ_L] NORMAL FAULT tì SANDSÎONE, STLTSTONE /\ THRUST FAULT t t------! ,--t SHALE, CLAY, MUDSTONE - PRESENT DAY COASTLINE f^^=" AND SUTURE BIOGENIC SII,ICEOUS DEPOSIT LA'M,ONG TICS ffi LIMESTONE Fffi * VOLCANOES OCEANIC SPREADING CENîER tl AND TRANSFORM I.'AULTS REEF

Cretaceous pelagic marls (i.a. Scaglia Rossa : Couches Map discussion Rouge : Capas Rojas; Bak 2000) facies andlor flysch/ flyschoidal series (i.a. Birkenmajer 1986; Mi5ík 1994; Early Jurassic Aubrecht et al. t9921. The synrift stage lasted in the Pieniny/MaguraBa- On the other hand within Northern Outer Car- sin from late Early Jurassic to îrhonian (Aubrecht et al. pathians, traditionally (e.g. Sl4czka Ec Kaminski 1998) 1997).The earliest stage of the basin history is enigma- the following sedimentary basins have been distinguished tic and documented only by pebbles in the Cretaceous- from south to north: the Magura Subbasin, the Dukla and Tertiary flysch. These pebbles indicate the possibility of Fore-Magura set of basins, the Silesian Basin, the Sub-Si- an existence of an enigmatic embayment of the Vardar- lesian Ridge and the Skole Basin. The main part of Magu- Transilvanian Ocean (see Fig. 3 - Va-Tr) which separated ra flysch sequences is of Late Cretaceous-Paleogene age. the Tisa (Bihor-Apuseni) (Ti) block from the Moesian However, there is also widely accepted possibility of the (Mo)-Eastern European Platform (Sàndulescu 1988). The much earlier, Early-Middle Jurassic origin of the Magu- pelagic Triassic limestones in the exotic pebbles in the ra Subbasin (see e.g. Birkenmajer 1986; Dercourt er al. Pieniny Klippen Belt (Birkenmaier et al. 1990) and the 1993, Golonka et al. 2000). It appears that Magura Sub- Outer Carpathian Flysch (Magura lJnit, see Sotík 1986) basin shared its history with the Pieniny Klippen Basin could have originated in this embayment. The embay- during the Jurassic time. ment position and its relation to the other parts of Te- Fig. 4 - Paleogeography of the cir- curr-Carpathian area during Middle Jurassic; plates position at 166 Ma (after Golonka ct .rl. 1003, nrodified). Abbre- viations of oceans and plates nrmes: Ad - Adria (Apulia), CR - Cz.orsztvn Ridge, Do - Dobrogee, EA - Eastern Alps, IC - Inner Carpathi- rns, Li - Ligurian Ocean, Me - Meliata/Helstatt Ocean, Mg - Magura Subbasin, Mo - Moesia plate, PB - Pien- iny Klippen Belt Subbasin, Pn - Penninic Ocean, Rh - Rhodopes, Sr - Sardinia, Ti - Tisr plate, Tr - Transilvani- an Ocean, Va - Vardar Ocean. For explanation of lithological syrnbols - see Fig. 3.

thys, Vardar Ocean (Va), Meliata-Halstatt Ocean (Me), Middle Jurasssic Dobrogea (Do) rift remain quite speculative. The Pien- The centralAtlantic (Withjack et al. 1998) and Al- iny rift (PB) opened during Pliensbachian - Aalenian pine Tethys went into a drifting stage during the Mid- time (Fig. 3) forming a part of the global system related dle Jurassic. The oldest oceanic crust in the Ligurian- to the opening of the Alpine Tethys. The Alpine Tethys, Piemont Ocean was dated as late as the Middle Jurassic that is Ligurian (Figs 3, 4 - Li), Penninic Oceans (Pn) in the southern Apennines and in the \ùlestern Alps (see and Pieniny/Magura Basin (Figs 3, 4 - PB, Mg) constitute Ricou 1996 and literature cited therein). Billet al. (2001) the extension of the Central Atlantic system (Golonka date the onset of oceanic spreading of the Alpine Teth- 2000). Stampfli (2001) recently postulated single Penninic ys by isotopic methods as Bajocian. According to \Win- Ocean (Pn) separating Apulia (Adria) (Ad) and Eastern kler tc Sl4czka (1994) the Pieniny data fit well with the Alps blocks (EA) from Eurasia. \le proposed similar model supposed openine of the Ligurian-Penninic Ocean (Li- for the Pieniny/Magura Basin (PB/Mg) in the Carpathians. Pn). One of the most rapidly change of sedimentation/ The basins' opening is related to the closure of the Meliata paleoenvironments within this basin took place between Ocean (Me). The restricted environment prevailed in this Early and Late Bajocian when well-oxygenated multicol- newly formed basin. oured crinoidal limestones replaced dark and black sedi- The oldest Jurassic rocks (Hettangian/Sinemurian mentation of Early-early Middle Jurassic period. Howev- in age) of the Pieniny Klippen Belt are more or less com- er, sedimentation of still younger (since latest Bajocian) pletely preserved (mainly due to tectonic movement and red nodular Amn.ronitico Rosso-type limestones was ef- reduction) only in the Slovakian and Ukrainian part of fect of Meso-Cimmerian vertical movements which sub- the region. They consist of different type of Gresten-like sided Czorsztyn Ridge (Figs a-6 - CR) and produced tec- dark/black facies both clastic and limestone sediments. tonically differentiated blocks as well as accompanied by Still younger Toarcian-Lower Bajocian Bositra (" Posido- the formation of neptunian dykes and scarp-breccias (e.g. nia") black shales with spherosiderites (Skrzypny Shale Birkenmajer 1986; Aubrecht et al. 1997;'Wierzbowski et Fm.), as well as dark marls and spotty limestones of wide- a|. tllg; Aubrecht 2001; Aubrecht & Túnyi 2001). The spread Tethyan Fleckenkalk/Fleckenmergel facies (of the Bajocian emergence of the Czorsztyn Ridge (CR) within Krempachy Marl Fm., Harcygrund Shale Fm. and Pod- the Pieniny/Magura Basin (PB/Mg) was connected with z^mcze Limestone Fm. - see Birkenmajer 1977) indi- the postrift ph:rse of the basin evolution (Golonka et cate the oxygen-depleted conditions (Birkenmajer 1986; al. 2003). In the same time in rhe axial, basinal sequenc- Tyszka 1994,2001). es first episode of radiolarite sedimentation took place 10 J. Golonka t< M. Krobicki

Fig.5 - Paleogeography of the cir- cunr-Crrplthiln ercl durinq Lrrrc Jurrssic; pl.rtes position at 152 Ma (after Golonka et al. 2003, modified). Ab- brevi;rtions of oceans and plates names: CR - Czorsz- tyn Ridge, Do - Dobrogea, EA - Eastern Alps, IC - In- ner Carpathians, Li - Ligu- rian Ocean, Me - Melaiata/ Halstart Ocean, Mg - Magu- ra Subbasin, Mo - Moesia plate, PB - Pieniny Klippen Belt Subbesin, Pn - Pennin- ic Ocean, Rh - Rhodopes, Si - Silesirn Basin, Sn - Si- naia Basin, Sr - Sardinia, Ti - Tisa plate, Tr - Transilvani- ln Ocean, Va - Verdar Ocean. For explanirtion of lithological synrbols - see Fig. 3.

(Birkenmajer 1977, 1986; MiSík 1999), which marked ing neptunian dykes of enismatic age (presumable Late great facial differentation between deepest successions Jurassic - Oxfordian?) (Aubrecht et al. 1998). and shallow (ridge) ones (Fig.4). The southern part of the North European Plat- form, north from the Pieniny/Magura realm (PB/Mg) Late Jurassic started to be rifted and Silesian Basin (Figs. 5, 6 - Si) in The Late Jurassic (Oxfordian-Kimmeridgian) his- the Western Carpathians (W-E direction) and Sinaia Ba- tory of the PKB reflects strongest facial differentiation sin (Sn) in the eastern Carpathians, with black, mainly within sedimentary basin (Fig. 4) where mixed siliceous- redeposited marls (?Kimmeridgian-Tithonian) have been carbonate sedimentation took place. Greatest deepening created (Pescatore tr Sl4czka 1984). The other Sub-Ba- effect is indicated by widespread Oxfordian radiolarites sins were differentiated during the latest (Hauterivian- which occur in the all basinal successions, whereas the Barremian) phase of basinal development. The connec- shallowest zone (Czorsztyn Succession) is completely tion of Silesian Basin (Si) with Sinaia (Sn) and Southern devoid of siiiceous intercalations at that time (sedimen- Carpathian Severin areas (Fig. 6 - Sv) (Sàndulescu 1988) tation from Ammonitico Rosso facies up to coral reef susgests the NW-SE direction of the basinal axis; so, two limestones). The change of oceanic circulation in north- Outer Carpathian perpendicular directions are possible ernmost Tethyan Realm during Oxfordian is probably re- within the basins. sponsible for such distribution of facies. It very well cor- responds with microfacial sequence within Ammonitico Latest Jurasssic - Early Cretaceous Rosso-type limestones as well, with domination of: fila- Major plate reorganization happened during the menr (Bositra filaments) (Middle Jurassic) - Globuligerina Tithonian time (Fig. 6). The Central Atlantic began to ex- (" Protoglobigerina") (Oxf ordian) - Sacco coma (Kimmerid- pand into the area between Iberia and the New Foundland gian) microfacies, where boom of planktic Globuligerìna shelf (Ziegler 1988). The Ligurian-Penninic Ocean (Li- forams was simultaneously with maximun.r development Pn) reached its maximum width and the oceanic spreading of radiolarites (Wierzbowski et al. 1999). Similar sequence stopped. The subduction of the Meliata/Halstatt Ocean is known in several European Alpine regions (e.g. Betic (Fig. 5 - Me) and the collision of the Tisa-Pelsonian block Cordillera, Southern Alps, Karavanke, Ionian Zone). On (Ti) with the Inner Carpathian terranes (IC) was conclud- the other hand, extremally shallow water coral reef facies ed at the end of Jurassic (Golonka et al. 2000). The Teth- occur locally in the Slovakian part of the PKB (Mi5ík 1929; yan plate reorsanization resulted in extensive gravitational Aubrecht et a|. 1992) or even oolitic limestones as infill- fault movement. Several tectonic horsts and grabens were PaLeogeography of the Pien iny 11

Fìg.6 - Paleogeography of the cir- cun.r-Carpathian area during latest Late Jurassic - earliest Early Cretaceous; plates position at 140 Ma (after Golonka et :rl. 1003, nrodified;. Abbre- viations of oceans and plates names: Ad - Adria (Apulia), Bk - Balkan rift, Bu - Bu- couini.rn-Getic termne, CR - Czorsz,ryn Ridge, Do - Do- brogea, EA - Eastern Alps, IC - Inner Carpathians, Lì - Ligu- rian Ocean, Mg - Magura Sub- basin, Mo - Moesia plate, PB - Pieniny Klippen Belt Subba- sin, Pn Penninic Ocean, Rh - Rhodopes, SC - Silesian Ridge (Cordillera), Si - Silesian Ba- sin, Sn - Sinaia Basin, Sr - Sar- dinia, Sv - Severin Basin, Ti - Tisa plate, Tr - Transilvanian Ocean, Va - Vardar Ocean. For explanation of lithological synrbols - see Fig. 3.

formed, rejuvenatine some older, Eo- and Meso-Cimme- bian. The rapid supply of shaliow water clastic material to rian faults (Birkenmajer 1986; Krobicki 1996). Such fea- the basin could be an effect of the strong tectonoeustatic tures resulted from the intensive Neo-Cimmerian tecton- sea-level fluctuations known from that time. The marls ic movements which affected the intrabasi nal Czorsztyn pass gradually upwards into calcareous turbidites (Cieszyn pelagic swell and are documented by facies diversification, limestones, see Slomka 1986) which created several sub- hardgrounds and condensed beds with ferromanganese- marine fans. The remnants of carbonate platforms with rich crusts and/ or nodules, sedimentary-stratigraphic hia- coral reefs (Stramberk-type limestones) along the margin tuses, sedimentary breccias, neptunian dykes and/or fau- of Silesian Basin and around intraoceanic cordillera (Sile- na redeposition (for example famous ammonite coquinas sian) (Fig. 6 - SC) and now known only from exotic ma- of the so-called "Rogolnik beds" - sensu Arkell 1956, see terial occurring within Upper Cretaceous/Paleogene fiy- also Kutek & Wierzbowski 1986). These processes were sch deposits of the Outer Carpathians, were results of the caused by formation and destruction of submarine tecton- fragmentation of the European platform in this area. The ic horsts attributed mainly to the Neo-Cimmerian period Silesian Ridge (cordillera) (SC) separated the Silesian Ba- of tectonic activity in the Carpathians (Birkenmajer 1958, sin (on the north) (Si) and Pieniny/Magura Basin (on the 1986; Michalík & Rehíkovi 1,995; Krobicki 1996; Kro- south) (PB-Mg) (l{si42kiervicz 1960; Golonka et al.2000). bickitr Slomka 1999; Golonka et al. 2003). Additionally, The eastward-northeastv/ard subduction along the Silesian these movements €iave rise to the appearance of a shallow Ridge (SC) and Bucovinian-Getic Terrane (Bu) was per- submarine swell which separated the basin into different pendicular or oblique to the general trend of the Czorsz- zones with their own water circulation patterns, probably tyn Ridge (CR) and the margin of the Inner Carpathian upwelling type (Golonka & Krobicki2001). (IC)-Eastern Alps (EA) terrane. TheJurassic blueschists The more northern Outer Carpathian rift had devel- metamorphic rocks found as pebbles (exotics) in the Al- oped in Late Jurassic with the sedimentation of pre-flysch bian flysch in the Pieniny-Magura Basin (PB-Mg) (e.g. black, mainly redeposited marls (?Kimmeridgian-Titho- Faryad 1997) indrcate exisrence of such a subduction. nian). This 'Western Carpathian, so-called Silesian Basin The Outer Carpathian rift had deveioped with the (Si), probably extended in the Eastern Carpathian (Sinaia beginning of calcareous flysch sedimentation. The rem- (Sn) or ,,black flysch") as well as to the Southern Car- nants of carbonate platforms (Olszewska & lWieczorek pathian Severin zone (Sv) (Sendulescu & Visarion 2000). 2OO1) with reefs (Stramberk) along the margin of Silesian The black sediments mark the beginning of an euxinic Basin (Si) were results of the fragmentation of the Euro- cycle of the Outer Carpathian basin that lasted until Al- pean platforn-r in this area. The subsidence in the Silesian t2 J. Golonka t< M. Krobicki

Basin (Si) was accompanied by the extrusion of basic la- by uplifted areas, e.g. Andrychów zone (Olszewska & va (teschenites) in the Western Carpathian and diabase- lWieczorek 2a01). The general downwarping of the Sile- melaphyre within the ,,black flysch" of the Eastern Car- sian Basin was probably due to the cooling effect of the pathians (Golonka et ai. 2000; I-ucióska-Anczkiewicz et al. underlying lithosphere. The sedimentation of calcareous 2002). The spreading stage in the Silesian Basin (Si) was sediments pass upwards gradually into black shales with accompanied by the main phase of intrusion of teschen- turbiditic sequences. ites, which occurred in the Western Carpathians during Hauterivian-Barremian time (Lucióska-Anczkiewi cz et al. 2002). The extension of the Silesian-Sinaia Basin (Si-Sn) Conclusions is marked by the beginning of the sedimentation in the The history of the Pienin y Outer Carpathi- Skole-Tarcàu area. Jurassic / an basins reflects the evoiution of the Circo-Terhyan area, The Jurassic separation of Bucovinian-Getic micro- especially its Alpine Tethys part. The major differentia- plate (Bu) from European plate is perhaps related to the tion of lithofacies took place during synrift phase of the origin of the Silesian Ridge (Fig. 6 - SC). The direct con- basins opening of the Pieniny/Magura Basin. Major reor- nection is obscured however by the remnants of the Tran- ganization happend during the Tithonian-Berriasian time. silvanian Ocean (Tr) in the area of the eastern end of the It was reflected by both paleoceanographical and paleocli- Pieniny Kìippen Basin (PB). These remnants are known matical char-rges (Golonka & Krobicki 2001). The Neo- from the lòaòovce-Krichevo unit in Eastern Slovakia and Cimmerian tectonic events as well as main phase of the Ukraine (Sotík et al. 2000, 2002).In this area existed a junc- Outer Carpathian basins opening is connected with this tion of the different basinal units: Pieniny/Magura Ocean reorp;anization. (PB/Mg), Transilvanian Ocean (Tr) and Outer Carpathian Basin. The eastward subduction of Bucovinian-Getic terranes is connected with the northward subduction under Rhodopes-Moesia plate mentioned above. The displace- Achno'oledgemenrs. This research has been partially supported ment within Transilvanian Ocean (Tr) which is began in financially by the Polish Comnrittee for Scientific Research (KBN) - Barremian is perhaps also related to this subduction. qrants 3 P04D 020 22 and 6 P04D 032 21. It is also a contribution to The Outer Carpathian basin reached its greatest IGCP 453. \We are grateful to Rom:rn Aubrecht, Stanislaw Kruglow, width during the post-Jurassic time. Vith the widening Marek Lewandorvski, Andrz-ej Matyja, Jozef Michalík, Nestor Oszc- zypko, Tadeusz Slon.rka, Andrzej Vierzbowski, for the fruitful discus- of the basin, several subbasins (troughs) began show to sion. \We would like to express our gratitude to the reviewers Andrzej their distinctive features. These subbasins, like Silesian, Wierzborvski and Serge Elrni for their helpful renrarks, which greatly Sub-Silesian, Skole, Dukla, Tarcàu, were locally separated improved the paper. Paleogeograpl4t of the Pieniny 13

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