the czertezik suc ces sion in the pi en iny na tional park...

S T U D I A G E O L O G I C A P O L O N I C AVol. 127, Kraków 2007, pp. 7–50.

Geology of the Pieniny Klippen Belt and the Tatra Mts, CarpathiansEd ited by K. Birkenmajer

Part XVIII

Krzysz tof BIRK EN MA JER1

The Czertezik Suc ces sion in the Pi en iny Na tional Park(Pi en iny Klip pen Belt, West Car pa thi ans):stra tigra phy, tec ton ics, palaeo geog ra phy2

(Figs 1–20)

Ab stract. The stra tigraphic col umn of the Czertezik Suc ces sion (Pi en iny Klip pen Belt, WestCar pa thi ans) in cludes Up per Li as sic through Up per Cre ta ceous rock units. The suc ces sion crops outin sev eral tec tonic win dows from be low the Pi en iny Nappe and/or the Brani sko Nappe which werethrust over the Czertezik Unit dur ing La ramian fold ing of the Klip pen Belt. Litho logi cal de vel op mentand suc ces sion of strata of the Czertezik Unit in these win dows prove that its origi nal sedi men taryzone was a di rect south ern con tinua tion of the Czorsz tyn one.

In the pres ent author’s opin ion, con trary to Wierzbowski et al. (2004), the Czertezik Suc ces sion in the ter ri tory of Po land lacks the Ba jo cian–Cal lovian am monitico rosso unit = the Niedzica Lime stoneFor ma tion. The Czorsz tyn Lime stone For ma tion (Kim me ridgian, also am monitico rosso fa cies)dis tin guished by the pres ent author in the Czertezik Suc ces sion at Czertezik and Pi eni ñski Stream(Pi en iny Range), and at Wy soka Mt (Lit tle Pi en iny Range), at trib uted by Wierzbowski et al. (2004) to the “Niedzica Lime stone For ma tion”, did not yield any age- diagnostic fos sils to sup port their changeof its Kim me ridgian (resp. Ox for dian–Kim me ridgian) age to an Up per Ba jo cian–Cal lovian one. Thislime stone oc curs al ways above, and not be low the ra dio larite ho ri zon (Cza jakowa Ra dio larite Fm.).

In the pres ent author’s opin ion, two klippes with fos si lif er ous Niedzica Lime stone For ma tionde scribed by Wierzbowski et al. (2004) from Lit ma nová and Mil poš, East Slo va kia, do not rep re sentthe Czertezik Suc ces sion but are typi cal ex am ples of the Niedzica Suc ces sion.

A palinspastic- sedimentological model pro posed in this pa per shows prob able Mid dle Ju ras sicpalaeo geo graphic po si tion of the very dis con tinu ous sedi men tary area of the Niedzica Suc ces sion,be tween larger sub ma rine cri noid lime stone fans de vel oped in the Czorsz tyn and Czertezik sedi men -tary zones.

Key words. Ju ras sic, Cre ta ceous, Czertezik Suc ces sion, Pieniny Klip pen Belt, Car pa thi ans, stra ti-gra phy, tec ton ics, palaeo geog ra phy

1 Mail ing ad dress: In sti tute of Geo logi cal Sci ences, Cra cow Re search Cen tre, Pol ish Acad emy ofSci ences, ul. Senacka 1, 31- 002 Kraków, Po land. E- mail: ndbirken@cyf- kr.edu.pl.

2 Ma nu script ac cepted for pub li ca tion De cem ber 30, 2006.

IN TRO DUC TION AND TEC TONIC SET TING

The Czertezik Suc ces sion con sists of ma rine de pos its of Early Ju ras sic throughLate Cre ta ceous age. It is a part of the Pi en iny Klip pen Belt, an im por tant tec tonicstruc ture of the West Car pa thi ans, some 600 km long (Fig. 1).

Though dis tin guished nearly a half cen tury ago in the Pi en iny Na tional Park ofPo land (Birk en ma jer, 1959b), the Czertezik Suc ces sion (“Se ries”, op. cit.) has only in com pletely been de scribed in later pa pers: (1) from the Czertezik and WielkaPus tel nica mounts, in the Pi en iny Range (Birk en ma jer, 1977, 1979); (2) from iso -lated tec tonic blocks in the Czorsz tyn Range (Birk en ma jer, 1960a, 1977); (3) andfrom the Ma³e Pi en iny (Lit tle Pi en iny) Range south of Ja worki (Birk en ma jer,1970).

The Czertezik Suc ces sion crops out mainly in tec tonic win dows ex posed byero sion from be low the La ramian thrust- sheets: the Pi en iny Nappe, and/or theBrani sko Nappe.

8 K. BIRKENMAJER

Fig. 1. Lo ca tion of the Pieniny Klippen Belt in the Carpathians. 1 – Autochthonous Neo genemolasse (Foredeep, outer zone); 2 – Allochthonous Neo gene molasse (Foredeep, in ner zone); 3 –Ter tiary flysch nappes; 4 – Mid-Cre ta ceous nappes in the East and South Carpathians, and com pa -ra ble folded/thrust outer zones else where; 5 – Pieniny Klippen Belt; 6 – East ern and South ern Alps,Cen tral Carpathians, and com pa ra ble folded/thrust and un folded in ner zones else where; 7 – Inter-arcpost-nappe cover in the Carpathians and the Apuseni Mts (Palaeogene, partly Late Cre ta ceous); blank– Fore land, intramontane molasse and Tertiary volcanics

Con trary to the Brani sko and Pi en iny Nap pes, which are in tri cately folded, theJu ras sic rocks of the Czertezik Suc ces sion form rigid slabs and plates usu ally de -void of in ter nal fold ing. They are ar ranged as ver ti cal to steeply dip ping bod ies ofcom pe tent lime stones pierc ing soft marls, marly shales and flysch rocks of Up perCre ta ceous age. In its tec tonic fea tures and field ap pear ance, the Czertezik Unit isvery simi lar to the Czorsz tyn Unit which, like wise, be haved as an “auto chthone”with re spect to the over thust La ramian nap pes (e.g., Birk en ma jer, 1965, 1970,1979). The sub stra tum of the Czertezik Unit is not ex posed at the sur face, ei ther inthe Pi en iny Range (type area – 1) or in the Lit tle Pi en iny range (area 3).

The Pieniny Range, be tween Czorsztyn-Niedzica in the west, and Szczawnica-Kroœcienko in the east, has from 2001 to 2005 been re mapped by the pres ent au thorto a very de tailed scale 1:5,000. This has al lowed him, i.a., to elu ci date geo met ri calre la tions be tween the tec tonic units, such as: the Czertezik Unit/Czorsztyn Unit; the Niedzica Nappe/Czorsztyn Unit; the Branisko Nappe/Czertezik Unit; the BraniskoNappe/Niedzica Nappe; and the Branisko-Pieniny Nappe/Czertezik Unit. Thesetec tonic stud ies have ob vi ous im pli ca tions on palaeogeographic re con struc tions ofsed i men tary zones and fa cies dis tri bu tion in the Ju ras sic–Cretaceous KlippenBasin.

CZORSZTYN RIDGE AND SLOPE VER SUS BASINAL FUR ROWS

Dur ing the Me so zoic, the Klippen Ba sin be longed in a north ern part of theTethys. This was a ma rine ba sin of oce anic char ac ter is tics, sit u ated be tween the In -ner Carpathian Subtatric-Tatric ma rine bas ins (Tri as sic to mid-Cre ta ceous) lo catedin the south, and the Outer Carpathian, pre dom i nantly flysch bas ins (Early Ju ras sicthrough Oligocene/Early Mio cene) lo cated in the north (Fig. 2). The Klippen Ba sinwas opened by the pro cess of oce anic-type rift ing most prob a bly al ready dur ingEarly Tri as sic (see Birkenmajer, 1985, 1986a, b; Birkenmajer et al., 1990), and anoce anic crust had prob a bly been formed. The Tri as sic rift of the Klippen Ba sin,which was 500–600 km long but rather nar row (Fig. 2), most prob a bly con tin uedeast ward at Transylvania (Ro ma nia), then curved out west ward and south ward toreach the Vardar Zone of the Dinarides. Its spread ing prob a bly died out dur ing LateTri as sic.

Dur ing Early Ju ras sic, the rift was re lo cated north ward and an oce anic MaguraBa sin had thus opened. This ba sin was most prob a bly di rectly linked with the Ju ras -sic Penninic oce anic realm of the pres ent day East ern Alps. It be came sep a ratedfrom the Klippen Ba sin by the Czorsztyn Ridge – a splin ter of the North Eu ro peancon ti nen tal crust left be hind dur ing rift re lo ca tion (op. cit.) – see Fig. 2.

Dur ing its Early Ju ras sic through Late Cre ta ceous his tory, the Czorsztyn Ridgebe haved mostly as an aseismic ridge. Only oc ca sion ally it was dis turbed by fault -ing, no ta bly at the Mid dle/Late Ju ras sic, and the Ju ras sic/Cre ta ceous tran si tions, by Mesocimmerian and Neocimmerian synorogenic dis tur bances, re spec tively (seeBirkenmajer, 1958b, 1963a, 1975, 1987; Birkenmajer & G¹siorowski, 1963).

THE CZERTEZIK SUC CES SION, PIENINY KLIPPEN BELT 9

10 K. BIRKENMAJER

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For most of its his tory the Czorsztyn Ridge was sub merged, but dur ing Late Li -assic–Mid dle Ju ras sic times it was mod er ately up-warped above sea level and sup -plied a re stricted amount of clastics to the Klippen Ba sin in the south, and theMagura Grajcarek Ba sin in the north.

The no tions: north, south, west and east, re fer to the pres ent geo graphic ori en ta tion of the PieninyKlippen Belt and its neigh bour ing tec tonic units. Palinspastic re con struc tions pro vided by var i ousau thors sug gest that ori en ta tion (geo graph ical co or di nates) of the Klippen Ba sin dur ing Ju ras sic andCre ta ceous times might have been dif fer ent from the pres ent one.

The Czorsztyn Ridge most prob a bly had an asym met ric struc ture. Its north ernslope abruptly deep ened and reached abys sal depths, some 3000 m or more, al ready at the Mid dle/Up per Ju ras sic tran si tion when radiolarites were formed (see Bir-kenmajer, 1998b). Fine clastic ma te rial was sup plied from north ern coast of theRidge to the ad join ing Magura (Grajcarek) Ba sin dur ing the Toarcian–Aalenian, inform of turbidites and sub ma rine slumps (Szlachtowa For ma tion). Some coarsergrades of the lat ter, al low to re con struct the Ridge’s struc ture and com po si tion, asfol lows (data from: Birkenmajer, 1958a, 1963a; Birkenmajer & Turnau, 1962;Krawczyk & S³omka, 1986, 1987, Krawczyk et al., 1987; see Birkenmajer et al.,1960, 2006):

(1) From the pre-Up per Car bon if er ous base ment might de rive quartz-feld -spar-mica-schists, gneiss, meta-mudstone and quartz ite clasts found by Krawczyk& S³omka (1987) and Krawczyk et al. (1987);

(2) The Up per Car bon if er ous coal-mea sures were the source for allochthonouscoal intercalations up to 8 cm thick (known al ready to Horwitz & Doktorowicz-Hrebnicki, 1932) which oc cur at top of some sand stone turbidite lay ers (Birken-majer, 1977, figs 10, 12B). They yielded re cy cled micro spores (Birkenmajer &Turnau, 1962): Sporonites unionus (Horst) Dybova et Jachowicz, Punctatisporitessp., Calamospora sp., Granulatisporites sp., Tuberculatisporites permagnus Dy-bova et Jachowicz, Lycospora granulata Kosanke, Annulatisporites baccatusDybova et Jachowicz, Densosporites spinosus Dybova et Jachowicz, D. granula-tus Dybova et Jachowicz, D. sp., and Cirratriradites saturni (Ibrahim) Schopf,Wil son et Bentall. This microspore asemblage is youn ger than the Namurian A (oc -cur rence of C. saturni), and older than the Westphalian C (oc cur rence of D.spinosus);

(3) To the Perm ian volcanics can be at trib uted dacite and rhy o lite lavas, tuffs,and lam pro phyre (Birkenmajer et al., 1960; Krawczyk & S³omka, 1987; Krawczyket al., 1987);

(4) The Tri as sic cover de pos its was rep re sented by: quartz and quartz ite(Werfenian); dolostone and lime stone (Mid dle Tri as sic); red, blue and var ie gatedshales (Carpathian Keuper) – see Birkenmajer (1958a, 1963a, 1979); Krawczyk &S³omka, 1987; Krawczyk et al., 1987);

(5) From the ?Lower Ju ras sic ma rine de pos its might de rive clasts of marls,sparitic-oolitic-, sparitic-pel let-, and micritic-organodetrital lime stones, arena-ceous claystone and si li ceous rocks (Krawczyk & S³omka, 1987; Krawczyk et al.,1987).


The south ern, prob a bly rather gen tle slope of the Czorsztyn Ridge was drowneddur ing the Li assic. Fossiliferous dysoxic to anoxic dark marls, marly shales andlime stones (Fleckenkalk and Fleckenmergel fa cies) spread out in the ba sin sincePliensbachian (or even ear lier) through Aalenian, both over the sub merged south -ern slope of the Czorsztyn Ridge (Czorsztyn, Czertezik and Niedzica suc ces sions)and in the basinal fur row (Branisko and Pieniny suc ces sions) – see Birkenmajer(1977); Birkenmajer & Myczyñski (1994); Tyszka (1994a, b, 1999, 2001); Tyszka& Kaminski (1995); Myczyñski (2004).

An abrupt change in sed i men tary con di tions – re place ment of dysoxic-anoxiccon di tions by open-sea well-ox y gen ated ones – hap pened in Mid dle Ju ras sic. Withonly one ex cep tion (at Dursztyn – see Birkenmajer, 1963a, G³uchowski et al.,1986), there is a non-tran si tion re la tion ship be tween black spherosiderite clays/shales (Skrzypne Shale Fm.: Aalenian–low est Bajocian) and the suc ceed ing whitecri noid lime stone (Smolegowa Lime stone Fm.: Bajocian) – see Birkenmajer(1963a). Krobicki and Wierzbowski (2004) ac cept a sed i men tary hi a tus be tweenthese for ma tions em brac ing at least two ammonite zones of Early Bajocian age, theLaeviuscula Zone, and the Propinquans Zone (the Pa tella Subzone and part of theHebridica Subzone).

Ap pear ance of phosphorite con cre tions at base of the white crinoidal lime stone(Krobicki, 2002, 2003) sug gests shallowing and ac tion of sub ma rine cur rents. Oc -cur rence of clasts of green micritic lime stone in the basal part of the SmolegowaLime stone For ma tion, was sug ges tive to Krobicki and Wierzbowski (2004) thatsuch rock might have formed in the Klippen Ba sin prior to the crinoidal lime stone

12 K. BIRKENMAJER

Fig. 3. Basinward thick ness re duc tion from north to south of the white crinoidal lime stonesub ma rine fan (Smolegowa Lime stone Fm.). Czorsztyn Suc ces sion at Bia³a Woda and Homole nearJaworki, Lit tle Pieniny Range, Po land (af ter Birkenmajer, 1977). JF – Jaworki Fm.; PF – PomiedznikFm.; h – hiatus

de po si tion. In fact, such lime stones have al ready been de scribed by G³uchowski etal. (1986) from pas sage beds be tween the Skrzypny Shale and the SmolegowaLimestone for ma tions at Dursztyn. It is an open ques tion, how ever, whether thephosphorite con cre tions have grown si mul ta neously with white cri noid lime stonede po si tion or were they re cy cled from some ear lier formed phosphorite-rich bed(s)unknown at present?

Dur ing the Bajocian, the Czorsztyn Ridge was mod er ately upwarped above sealevel, and sup plied a re stricted amount of clastics to the Klippen Ba sin, such as:quartz and quartz ite (Lower Tri as sic, Werfenian), lime stone and dolostone (Mid dle Tri as sic), red, blue and var ie gated shale (Carpathian Keuper = Up per Tri as sic). It iswell known (Birkenmajer, 1958a, 1963a) that the larg est frag ments of these Tri as -sic rocks oc cur in white crinoidal lime stones of the Czorsztyn Suc ces sion de pos ited clos est to the then emer gent Ridge, while the small est ones – in the Niedzica Suc -ces sion most distant from it.

The white and red cri noid lime stones (the Smolegowa Lime stone, and theKrupianka Lime stone, re spec tively) had orig i nated un der oce anic shelf con di tionsas over lap ping sub ma rine fans of cri noid de tri tus swept downslope by sub ma rinecur rents from shal low-wa ter hab i tats (see G³uchowski, 1986, 1987). Shal low-ma -rine con di tions are con firmed by oc cur rence of Curvolithes trace fos sils (Krobicki& Uchman, 2003). Lens-shaped cri noid-de tri tus bod ies were thick est in the Czor-sztyn Suc ces sion, 150–100 m, drop ping to 60–50 m in the Czertezik Suc ces sion, fi -nally to 10–5 m in the Niedzica Succession (Figs 3–5).

Synsedimentary tec ton ics could, lo cally, mod ify such thick nesses, as there areev i dences for Mid-Cim mer ian fault ing and brecciation both from the Pol ish(Wapiennik Brec cia Mbr – see Birkenmajer, 1952; 1958a; 1963a, pp. 231, 338;1977, pp. 71–72) and the West Slo vak parts of the Klippen Belt (Krasin Brec cias –Mišík et al., 1994; Aubrecht, 1997). Krobicki and Wierzbowski (2004, p. 78) be -lieved that “strong and rapid tec tonic move ments” and the re sul tant horst struc turesin the ba sin bot tom were re spon si ble for thick ness changes in the white crinoidallime stone. How ever, the scale, ex tent and pat tern of such changes are still highlyhy po thet i cal, and care ful field stud ies would be needed to dis crim i nate be tweensed i men tary con den sa tion ver sus tec tonic re duc tions of the cri noid lime stonethick nesses.

Sed i men tary hi a tuses, deep-wa ter hardgrounds, and con den sa tion of deep-wa -ter sed i ment are fre quent fea tures within the ammonitico rosso fa cies (= red nod u lar lime stones), par tic u larly in the Czorsztyn Lime stone For ma tion of the CzorsztynSuc ces sion (see Birkenmajer, 1963a, 1977; Myczyñski & Wierzbowski, 1994).

It seems that the ammonitico-rosso fa cies had ap peared in the Niedzica Suc ces -sion (as the Niedzica Lime stone For ma tion), and in the Czorsztyn Suc ces sion (asthe Czorsztyn Lime stone For ma tion) roughly si mul ta neously, dur ing the LateBajocian Parkinsoni Zone (see Birkenmajer & Znosko, 1955; Birkenmajer &Myczyñski, 1984; Krobicki & Wierzbowski, 2004). Krobicki and Wierzbowski(op. cit., fig. 2) sup pose that a sed i men tary hi a tus which cov ers most of theGarantiana Zone and a half of the Parkinsoni Zone sep a rates these nod u lar


(ammonitico rosso-type) lime stones from the un der ly ing crinoidal lime stones(white and red) ar bi trarily at trib uted by them to the Mid dle Bajocian. How ever,Bathonian ammonites, e.g. ‘Oppelia fusca‘ (Oppel), Bullatimorphites ymir (Oppel) and Lissoceras psilodiscus (Schloenbach), have been de ter mined from the redcrinoidal lime stone (= Krupianka Lime stone Fm. – Birkenmajer, 1977) al readydur ing the 19th cen tury (see Birkenmajer, 1963a, pp. 40–41, 265–266).

Since the ap pear ance of nod u lar lime stones (Niedzica and Czorsztyn for ma -tions), the Czorsztyn Ridge prac ti cally ceased to sup ply clastics to ei ther theMagura (Grajcarek) or the Klippen bas ins, and open-sea con di tions were es tab -lished. Dur ing the Callovian through Maastrichtian, the Ridge played the role of ador mant sub ma rine swell, but it was ac ti vated by fault ing at the Ju ras sic/Cre ta ceous

14 K. BIRKENMAJER

Fig. 4. Basinward thick ness re duc tion of the white crinoidal lime stone sub ma rine fan (Smolegowa Lime stone Fm.). Czorsztyn Suc ces sion (in the north) through the Czertezik Suc ces sion (moresouth ward) to the Niedzica suc ces sion (in the south). Area of Jaworki and Bia³a Woda, Lit tle PieninyRange, Po land (af ter Birkenmajer, 1970, ex pla na tions mod i fied af ter Birkenmajer, 1977). 1 –Krempachy Marl Fm.; 2 – Skrzypny Shale Fm.; 3 – Smolegowa Lime stone Fm.; 4 – KrupiankaLime stone Fm.; 5 – Flaki Lime stone Fm.; 6 – Niedzica Lime stone Fm.; 7 – Czajakowa RadiolariteFm; 8 – Czorsztyn Lime stone Fm.; 9 – Dursztyn Lime stone Fm.; 10 – Spisz Lime stone Fm.; 11 –Chmielowa Fm.; 12 – Pomiedznik Fm.; 13 – Pieniny Lime stone Fm.; 14 – Kapuœnica Fm.; 15 –Jaworki Fm.; 16 – Sromowce Fm. (16a – Bukowiny Gravelstone Mbr)

tran si tion (Neocimmerian move ments – see Birkenmajer, 1958b, 1963a). Lo calemersions may have taken place, as sug gested, e.g., by the ap pear ance of re de pos -ited Lower Cre ta ceous non-ma rine al gae in re sid ual man ga nese-rich hardground-type crusts and fills of cracks, pock ets etc., some times as so ci ated with bi valve bor -ings, in var i ous lime stones of the Czorsztyn Suc ces sion in West Slovakia (Draga-stan & Mišík, 2001).


Fig. 5. Cor re la tion of the Ju ras sic radiolarite ho ri zon in the Pieniny Klippen Belt Ba sin and theMagura Ba sin (Grajcarek Unit), af ter Birkenmajer & Widz (1995). Radiolarite com plex (1–3): 1, 2 –Czajakowa Radiolarite Fm. (1 – red radiolarites: Kamionka Radiolarite Mbr, KRM, and Buwa³dRadiolarite Mbr., BRM; 2 – Podmajerz Radiolarite Mbr, PRM); 3 – Sokolica Radiolarite Fm. (spottyman ga nese radiolarites, SF). Other ma rine de pos its: 4 – red nod u lar lime stone (ammonitico rossofa cies) = Niedzica Lime stone Fm. and Czorsztyn Lime stone Fm.; 5 – cherty lime stone (biancone/maiolica fa cies) = Pieniny Lime stone Fm.; 6 – grey crinoidal lime stone (Flaki Fm.); 7 – white and redcrinoidal lime stones (Smolegowa and Krupianka lime stone fms); 8 – dark-grey lime stones and marls(Fleckenkalk-Fleckenmergel fa cies) = Podzamcze Lime stone Fm.; 9 – dark-grey shales (Dogger).Suc ces sions: G – Grajcarek; C – Czorsztyn; Ct – Czertezik; N – Niedzica; B – Branisko; P – Pieniny;H – Haligovce

STAN DARD STRA TIG RA PHY OF THE CZERTEZIK SUC CES SION

The stan dard strati graphic col umn of the Czertezik Suc ces sion in cludes LateLiassic through Late Cre ta ceous ma rine strata. It is based mainly on type ex po suresin the Pieniny Moun tains, in two most im por tant tec tonic win dows: the Czertezik-Zamkowa Góra Tec tonic Win dow (Birkenmajer, 1959b, 1973a, 1976a, 1977,1979), and the Ociemne-Sutrówka-Bojków Groñ Tec tonic Win dow (new ob ser va -tions, 2001–2005).

Prior to de tailed geo log i cal map ping, 1:5000 scale, of the area north of the Sokola Peræ tour istpath, the pres ent au thor at trib uted rocks of the Ociemny Wierch-Bojków (Bajków) Groñ ridge to theBranisko Nappe (see Birkenmajer, 1959a: map). How ever, dis cov ery of thick crinoidal lime stones(the Smolegowa and the Krupianka lime stone for ma tions) there (see be low), con vinced him that wedeal here with the Czertezik Suc ces sion and not the Branisko Suc ces sion.

The ma jor ity of lithostratigraphic units of the Czertezik Suc ces sion are the same as those ones in the Czorsztyn Suc ces sion, how ever, two of them – the CzajakowaRadiolarite Fm. and the Pieniny Lime stone Fm., which oc cur in the Czertezik Suc -ces sion (and in the re main ing Klippen suc ces sions), are ab sent from the CzorsztynSuc ces sion (Figs 5–7).

Palaeontological age de ter mi na tion of lithostratigraphic units is usu ally in ad e -quate in the Czertezik Suc ces sion. There fore, their age ranges are mainly based oncom par i son with well-dated units of the Czorsztyn-, Niedzica- and the Braniskosuccessions.

Szlachtowa For ma tion (Birkenmajer, 1977). The Wspólna Ska³a klippe, ex -posed in the Niedzica Cas tle-Czubata Ska³a Tec tonic Win dow, has long been at -trib uted to the Czertezik Suc ces sion (Birkenmajer, 1960).

Its old est unit, the Szlachtowa For ma tion, con sists of grey to black fri a ble sand -stones and shales (flysch fa cies) about 5 m thick (see Birkenmajer, 1977, p. 30 andfig. 19A). By com par i son with well dated Szlachtowa For ma tion in the GrajcarekUnit (see Birkenmajer, 1977, pp. 25–31; Birkenmajer & Tyszka, 1996; Birken-majer & Gedl, 2004; Birkenmajer et al., 2006 – in press), the age of the unit mostprob a bly cor re sponds to Toarcian.

New in ves ti ga tions sug gest, how ever, that the whole sec tion of the WspólnaSka³a klippe might rep re sent a va ri ety of the Branisko Suc ces sion and not theCzertezik Suc ces sion (a de tailed de scrip tion of the sec tion will be pre sented in asep a rate pa per).

Krempachy Marl For ma tion (Birkenmajer, 1977). The best site of this for ma -tion at trib uted to the Czertezik Unit is that at Szczawnica Ni¿na. This is a sec tionabove the road Szczawnica-Kroœcienko (see Myczyñski, 2004, fig. 3), known al -ready to Horwitz (1922: “Dumortieria beds”). Grey, spotty marly shales and marls,some 5 m thick, yielded there a con sid er ably rich ammonite fauna de ter mined byMyczyñski (2004). It con sists of: Calliphylloceras connectens (Zittel), C. nilssoni(Hébert), Holcophylloceras ultramontanum (Zittel), Ptychophylloceras tatricum(Pusch), P. chonomphalum (Vacek), Dumortieria cf. levesquei (d’Orbigny), D. cf.flexicosta Ernst, D. cf. radiosa (Seebach), Pleydellia aalensis (Zieten), P. (Walke-

16 K. BIRKENMAJER

riceras) lugdunensis Elmi et Rulleau, P. cf. fluensBuckman, Tmetoceras scissum (Benecke), Leiocerasopalinum (Reinecke), L. comptum (Reinecke), Costi-leioceras costatum (Quenstedt), Pseudaptetoceras cf.klimakomphalum (Vacek) and Osperlioceras alternans(Monestier). This fauna in di cates the pres ence of thefol low ing ammonite zones: the Dumortieria pseudora-diosa Zone and the Pleydellia aalensis Zone (LateToarcian); the Leioceras opalinum Zone (Early Aale-nian); and the Ludwigia murchisonae Zone, lower part(Mid dle Aalenian, pre vi ously at trib uted to the Tmeto-ceras scissum Zone) – see Myczyñski (2004, pp.14–15).

Poorly ex posed grey marls, prob a bly up to 10 mthick, at trib ut able to the Krempachy Marl For ma tion ofthe Czertezik Suc ces sion, have also been found at NEslope of the Stachurówka Mount, south of Jaworki, Lit -tle Pieniny Range (Birkenmajer, 1970).

Skrzypny Shale For ma tion (Birkenmajer, 1977).Black spherosiderite-bear ing shales (10–5 m thick) arepoorly ex posed at sev eral lo cal i ties, e.g. at a pass east of Wysoka (Wysokie Ska³ki) Mt, Lit tle Pieniny Range(see Wierzbowski et al., 2004, figs 2C, 4C), and atSzczawnica Ni¿na (Myczyñski, 2004, fig. 3).

Black shales with spherosiderites (pelosiderites),some 5 m thick, were ex posed at the Wspólna Ska³aklippe in the Niedzica Cas tle-Czubata Ska³a Tec tonicWin dow (see Birkenmajer, 1963b, 1977, fig. 19A),orig i nally at trib uted to the Czertezik Suc ces sion. Newin ves ti ga tions sug gest, how ever, that this klippe mightbe long to a va ri ety of the Branisko Suc ces sion (seeabove: the Szlachtowa Formation).

By com par i son with well dated Skrzypny ShaleFor ma tion of the Czorsztyn Suc ces sion (see Birken-majer, 1963a, 1977, p. 41; Myczyñski, 1973, 2004), the age of this for ma tion in the Czertezik Suc ces sion could cor re spond to Mid dleAalenian (Ludwigia murchisonae Zone) through lower Mid dle Bajocian(Hyperlioceras discites Zone).

Scheibner (1964a, b) at trib uted to the Czertezik Suc ces sion spherosideriteshales (= the Skrzypny Shale For ma tion) ex posed in a stream bed at Litmanová(above the vil lage), East ern Slovakia, which yielded ammonites of Aalenian toEarly Bajocian ages: the Murchisonae, the Bradfordensis, the Concavum and theDiscites zones. Scheibner (1964a, p. 642) also stressed that “at the end of theDiscites Subzone there was a great break in sed i men ta tion... Lo cally there was a


Fig. 6. Lithostratigraphic col umn of the Czertezik Su-c ces sion at Czertezik Mt,type sec tion (af ter Birken-majer, 1977, 1979, sup ple -mented). 1 – SmolegowaLime stone Fm.; 2 – Kru-pianka Lime stone Fm.; 3, 4 – Czajakowa Radiolarite Fm.(3 – Podmajerz RadiolariteMbr; 4 – Buwa³d RadiolariteMbr); 5 – Czorsztyn Lime -stone Fm.; 6 – DursztynLime stone Fm.; 7 – PieninyLime stone Fm.; 8 – Kapuœ-nica Fm.; 9 – Jaworki Fm.

sed i men tary gap (Litmanová un con form able con tact of crinoidal lime stone on theMurchisonae Beds and the lack of the Sonninia sowerbyi and Otoites sauzeiZones)”.

Smolegowa Lime stone For ma tion (Birkenmajer, 1977). This is a very char ac -ter is tic mas sive, light-col oured cri noid lime stone. Its colours vary be tween whiteand light-grey in the type area (Pieniñski Potok stream) through grey to dark-grey(in the Jaworki area, Lit tle Pieniny Range). The cri noids (G³uchowski, 1987, fig. 5)are rep re sented, i.a., by: Isocrinus nicoleti (Desor), Chariocrinus bathonicus (deLoriol), Balanocrinus subteres (Münster in Goldfuss), Pentacrinus dargniesiTerquem et Jourdy, Cyclocrinus rugosus (d’Orbigny) and Saccocoma sp. Otherfos sils in clude in fre quent brachi o pods de ter mined by Uhlig (1890, p. 748) as:“Terebratula ventricosa Hartm., Rhynchonella cf. subtetraedra Dav., R. cf. plica-tella d’Orb., R. cf. ferryi Desl., R. sp. ind., R. spinosa (Schloth.)”, more over bi -valves Bositra buchi (Roemer) [pre vi ously Posidonia alpina (Gras)] – see Birken-majer (1970, p. 20).

Krobicki and Wierzbowski (2004) re strict the age of the Smolegowa Lime stoneFor ma tion in the Pieniny Klippen Belt to the Bajocian only: from an up per part ofthe Propinquans Zone (Early Bajocian) through a lower/mid dle part of the Garan-tiana Zone (Late Bajocian). This age is ten ta tively ap plied here to the SmolegowaLime stone For ma tion of the Czertezik Suc ces sion. Thick ness of the SmolegowaLime stone For ma tion at tains 50 to over 70 m in the Pieniñski Potok stream area(Figs 6, 7; see also Birkenmajer, 1977, fig. 21A), and 50–70 m in the Jaworki area(Lit tle Pieniny Range – see Birkenmajer, 1970).

18 K. BIRKENMAJER

Fig. 7. Geo log i cal cross-sec tion be tween Sokolica Mt and Czertezik Mt (af ter Birkenmajer, 1979,fig. 84). Pieniny Nappe: 1 – Kapuœnica Fm.; 2 – Pieniny Lime stone Fm.; 3 – Czajakowa RadiolariteFm. (Podmajerz Radiolarite Mbr); 4 – Sokolica Radiolarite Fm.; 5 – Podzamcze Lime stone Fm.Czertezik Unit (type sec tion): 6 – Jaworki Fm.; 7 – Kapuœnica Fm.; 8 – Pieniny Lime stone Fm.; 9 –Czorsztyn Lime stone Fm.; 10, 11 – Czajakowa Radiolarite Fm. (10 – Buwa³d Radiolarite Mbr; 11 –Podmajerz Radiolarite Mbr); 12 – Krupianka Lime stone Fm.; 13 – Smolegowa Lime stone Fm.

The Smolegowa Lime stone For ma tion of the Wielka Pustelnica klippe has re -cently been in ves ti gated in de tail by Wierzbowski et al. (2004, sec tion “A”, pp.239–240; units 1–5 = Smolegowa Lime stone Fm.; unit 6 = Flaki Lime stone Fm.):

Smolegowa Lime stone Fm.:Unit 1 (10.2 m thick): poorly bed ded grey crinoidal grainstone, with bi valve and brachi o pod

de tri tus. Quartz grains are pres ent. There oc curs a red-col oured crinoidal lime stone bed (No 5b). Inthe pres ent au thor’s opin ion, it could rep re sent a nep tu nian dyke;

Unit 2 (9.1 m thick): very thick-bed ded grey crinoidal-spiculite grainstone, with in fre quentforaminifer and bi valve shell de tri tus;

Unit 3 (1.1 m thick): me dium-bed ded red dish crinoidal grainstone stained by Fe-Mn ox ides.Bryo zoan frag ments and foraminifers (Textularia sp.) oc cur. Quartz grains, dolostone clastad mix ture, and sin gle chlorite grains have been rec og nized. In the pres ent au thor’s opin ion, this unitcould also rep re sent a nep tu nian dyke con nected with a Mid-Cim mer ian disturbance;

Unit 4 (7.7 m thick): very thick-bed ded, grey crinoidal grainstone to packstone with fre quent greychert in ter ca la tions. Con sid er able quartz-grain ad mix ture (lo cally, even a sand stone bed) has beenob served. Sponge spicules, foraminifer tests (Lenticulina sp., nodosarids and nubecularids), ostracodand bi valve shell de tri tus have been recognized;

Unit 5 (10.75 m thick): thick- to very thick-bed ded grey, coarse-crinoidal grainstone, weath er ingto thin plates. Bi valve and brachi o pod shell de bris is pres ent.

Flaki Lime stone Fm.Unit 6 (5.05 m thick): thick to very thick-bed ded grey crinoidal lime stones with fre quent green ish

(lower) and red dish (higher) chert in ter ca la tions. Bi valve shell frag ments, a brachi o pod Septocrurellacf. defluxa (Oppel) shell, bryo zoan de tri tus and sin gle foraminifer tests (Lenticulina sp., Tetrataxissp.) have been found. Quartz sand ad mix ture is pres ent, lo cally in creas ing to form fine-grainedsand stone to siltstone.

This unit be longs to the Flaki Lime stone For ma tion (see Birkenmajer, 1977, fig. 21B).

From the Flaki Lime stone For ma tion of the Czertezik Suc ces sion, G³uchowski(1987, fig. 5) has de ter mined, i.a.: Isocrinus nicoleti (Desor), Balanocrinus sub-teres (Münster in Goldfuss), Cyclocrinus rugosus (d’Orbigny) and Saccocoma sp.

Krupianka Lime stone For ma tion (Birkenmajer, 1977). Red crinoidal lime -stone which di rectly over lies the Smolegowa Lime stone For ma tion has not beenrec og nized in the Wielka Pustelnica klippe (Birkenmajer, 1977, fig. 21B). How -ever, it is known from the Czertezik mount sec tion (Birkenmajer, 1977, fig. 21A;1979, fig. 84).

At the Sokola Peræ ridge (blue tour ist path be tween Czertezik mount and PolanaBurzana alp), the Krupianka Lime stone Fm. poorly crops out at only one site (seeFig. 16): this was prob a bly the rea son that Wierzbowski et al. (2004, fig.3:Czertezik), ques tioned its oc cur rence there. How ever, this unit, 2–5 m thick, con -tin ues at steep north ern slope of the mount for about 150 m down from the tour istpath, at the base of the Czajakowa Radiolarite For ma tion. Still fur ther north east, ina mor pho log i cal de pres sion be tween Czertezik and Kurnikówka mounts, there is alarge rockslip (from the Czertezik mount) in which rocks be long ing to the Czor-sztyn Lime stone Fm., the Krupianka Lime stone Fm., and the Smolegowa Lime -stone Fm., have been recognized.

Be tween the Polana Burzana alp and the Wielka Pustelnica klippe, the Kru-pianka Lime stone For ma tion is miss ing due to tec tonic causes, and the SmolegowaLime stone For ma tion co mes into di rect con tact with strongly tec toni cally re duced


radiolarites (Czajakowa Radiolarite Fm.) and red nod u lar lime stone (CzorsztynLimestone Fm.).

Two ex po sures of the Krupianka Lime stone For ma tion are vis i ble on left slopeof the val ley, just above the Potok Pieniñski stream bed: (1) west of the WielkaPustelnica klippe, and (2) east of it (see Fig. 10C, 16). None of these sites wereknown to Wierzbowski et al. (2004):

(1) At the west ern site, we see the Krupianka Lime stone Fm. steeply dip ping SEto gether with the un der ly ing Smolegowa Lime stone Fm., and the over ly ingradiolarites of the Czajakowa Radiolarite Fm. and red nod u lar lime stone of theCzorsztyn Lime stone Fm. The Krupianka Lime stone Fm. con sists there of red,fine-grained crinoidal lime stone and red to pur ple shaly crinoidal lime stone rich inFe-Mn ox ides, al to gether 2–3 m thick.

(2) At the east ern site, which be longs to an other klippe, the Krupianka Lime -stone Fm., to gether with the un der ly ing Smolegowa Lime stone Fm., dips 45–60°NW un der radiolarites (Czajakowa Radiolarite Fm.); then co mes strongly tec toni -cally re duced red nod u lar lime stone (Czorsztyn Lime stone Fm.) and a klippe ofwhite cherty lime stone (Pieniny Lime stone Fm.). The lat ter lime stone forms asyncline, the NW limb of which re peats the se quence: the Czorsztyn Lime stoneFm. and the Czajakowa Radiolarite Fm. dip ping SE at 80°.

At foot of the Wielka Pustelnica klippe, the Pieniñski Potok gorge fol lows afault di rected NW–SE. This fault di vides the Czertezik Suc ces sion into two parts:(i) with the Krupianka Lime stone Fm. (in the NE: Czertezik-Potok Pieniñski zone);(ii) with out the Krupianka Lime stone Fm., but with its strati graphic equiv a lent de -vel oped as the Flaki Lime stone Fm. (in the S and SW: Wielka Pustelnica-Zamkowa Góra mount zone).

On north ern slope of the Wielka Pustelnica klippe which is densely crossed byMio cene faults (NNE–SSW – see Fig. 16) we see small ex po sures of dark-greyspotty Li assic lime stones be long ing to the Pieniny Nappe, and of red Up per Cre ta -ceous marls (Jaworki For ma tion of the Czertezik Unit) wedged inbetween twoklippes of white/grey crinoidal lime stone (Smolegowa Lime stone Fm., CzertezikUnit). At the north ern fault con tact, the Li assic lime stone wedge is sep a rated fromthe crinoidal lime stone klippe (Smolegowa Limestome Fm., Czertezik Unit) by ared brec cia band con sist ing of an gu lar clasts of white crinoidal lime stone in redhaematitic ma trix. This rock looks very much like a nep tu nian dyke, pos si blylinked with Meso-Cim mer ian fault ing at the time of de po si tion of the KrupiankaLimestone Fm. (see Fig. 10B).

The age of the Krupianka Lime stone For ma tion, by com par i son with this unit inthe Czorsztyn Suc ces sion, may cor re spond to mid dle Up per Bajocian (GarantianaZone af ter Krobicki & Wierzbowski, 200, fig. 2) through a part of the Bathonian(cf. Birkenmajer, 1963a, pp. 40–44, 265–266; 1977).

Czajakowa Radiolarite For ma tion (Birkenmajer, 1977). This unit is ratherpoorly de vel oped in the Wielka Pustelnica klippe (“A” klippe in Wierzbowski etal., 2004). It be gins at about 20 m above the Pieniñski Potok stream bed, and con tin -ues up ward the klippe to about 70 m above the stream bed.

20 K. BIRKENMAJER

Wierzbowski et al. (2004, fig. 2A–C) have in ves ti gated only the low est part of the sec tion, up to c.10 m above stream. Ap par ently, they did not climb up to higher parts of the ex po sure. This is therea son that their con clu sions as to strati graphic po si tion and age of the nod u lar lime stone in thissec tion are in cor rect.

In the up per part of the ex po sure, we see the fol low ing suc ces sion of rocks of theCzertezik Suc ces sion (see Birkenmajer, 1977, fig. 21B) – Figs 8, 9:

Pieniny Lime stone For ma tion (> 30 m):4f. Lime stone, bed ded, grey-blu ish, with black chert in ter ca la tions;4d–e. Lime stone, bed ded, light-grey, slightly spotty, rich in sty lo lites, with black chert in ter -

ca la tions;4c. Lime stone, grey-green ish, poorly bed ded, lo cally strongly brecciated and calcitized;4b. Lime stone, bed ded, light-grey, with brown ish chert in ter ca la tions;

Dursztyn Lime stone For ma tion (3–4 m):4a. Lime stone, grey-green ish, poorly bed ded, strongly brecciated and calcitized;

Czorsztyn Lime stone For ma tion (1 m):3c. Slightly nod u lar lime stone, light-pink to green ish;3b. Typ i cal nod u lar lime stone, red, strongly tectonized;3a. Lime stone, fine-crys tal line, trochitic, green ish-pink;

Czajakowa Radiolarite For ma tion (1–2 m):2b. Radiolarite beds, red, choc o late-brown, brown ish- green, yel low ish (Buwa³d Radiolarite

Mem ber);2a. Radiolarite beds, green, blu ish, very strongly brecciated, al ter nat ing with whit ish crinoidal

lime stone (Podmajerz Radiolarite Mem ber);Flaki Lime stone For ma tion (5 m):

Grey crinoidal lime stone with chert in ter ca la tions (pas sage to the Czajakowa Radiolarite For ma -tion, Podmajerz Radiolarite Mbr);Smolegowa Lime stone For ma tion (> 50 m):

White to light grey, mainly mas sive crinoidal lime stone.

The Czajakowa Radiolarite For ma tion thick ens up to 5–10 m eastwards fromthe Wielka Pustelnica klippe. It is well trace able along left slope of the PotokPieniñski val ley as far as the Polana Burzana alp, then on south ern and south east ernslopes of the Czertezik Mt (see Fig. 16A). A still better de vel op ment of the for ma -tion (mainly red radiolarites = Buwa³d Radiolarite Mbr, but also green radiolarites= Podmajerz Radiolarite Mbr) oc curs in the Ociemne-Sutrówka-Bojków GroñTec tonic Win dow (see Fig. 16B).

The age of the Czajakowa Radiolarite For ma tion, as based on Aptychi fau nas(Birkenmajer & G¹siorowski, 1960, 1961; G¹siorowski 1962) cor re sponds in theCzertezik Suc ces sion to the ?Lower and Up per Oxfordian (Birkenmajer, 1977, p.62). The Oxfordian age of the radiolarites is also con firmed by de tailed stud ies ofthe radio lar ians (Widz, 1991; Widz & De Wever, 1993; Birkenmajer & Widz,1995).

The fol low ing stan dard Late Ju ras sic Uni tary As so ci a tions have been dis tin -guished in the Czajakowa Radiolarite For ma tion in the basinal Klippen suc ces sions and in the Grajcarek Unit in Po land (op. cit.): U.A.7-8 (Oxfordian), U.A.8 (LateOxfordian), U.A.8-9 (Late Oxfordian–Kimmeridgian), and U.A.9 (Kimmerid-gian). No radiolarian as so ci a tions older than Oxfordian have been found in thisfor ma tion. Thus, it is un clear why Wierzbowski et al. (2004, fig. 9) and Krobicki


22 K. BIRKENMAJER

Fig. 8. Pieniñski Potok stream val ley. Geo log i cal pan orama of right slope of the val ley be tweenWielka Pustelnica and Ostry Wierch (del. K. Birkenmajer, 24 Aug. 1952). Czertezik Unit: 1 –Smolegowa Lime stone Fm. and Flaki Lime stone Fm. (F); 2a, b – Czajakowa Radiolarite Fm. (2a –Podmajerz Radiolarite Mbr; 2b – Buwa³d Radiolarite Mbr); 3a–c – Czorsztyn Lime stone Fm.; 4a –Dursztyn Lime stone Fm.; 4b–e – Pieniny Lime stone Fm.; 5 – Jaworki Fm. Pieniny Nappe: 6 –Podzamcze Lime stone-, Sokolica Radiolarite-, and Czajakowa Radiolarite for ma tions; 7 – PieninyLime stone Fm. Other sig na tures: f – fault; ta lus – stippled

and Wierzbowski (2004, fig. 2) be gin the Czajakowa Radiolarite For ma tion in theCzertezik Suc ces sion al ready in the Up per Bajocian Parkinsoni Zone (sic!), andcon tinue it through Bathonian and Callovian up to the Oxfordian, to which it in factbe longs.


Fig. 9. Geo log i cal struc ture of a klippe im me di ately south of Wielka Pustelnica (= “klippe A” ofWierzbowski et al., 2004). Pieniñski Potok stream val ley, Czertezik Suc ces sion (del. K. Birkenmajer,24 Aug. 1952). For lo ca tion and ex pla na tions see Fig. 8

Czorsztyn Lime stone For ma tion (Birkenmajer, 1977). Strati graphic su per po -si tion of the Czorsztyn Lime stone For ma tion above the Czajakowa Radiolarite For -ma tion is well doc u mented in the area of the Czertezik-Zamkowa Góra Tec tonicWin dow (see Figs 6–9, 11, 16A) and the Ociemne-Sutrówka-Bojków Groñ Tec -tonic Win dow – see Fig. 16B). This red nod u lar lime stone is usu ally more mas sive(less nod u lar) than that in the Czorsztyn Suc ces sion. Its strati graphic con tacts withthe un der ly ing red radiolarites (Czajakowa Radiolarite Fm.: Buwa³d RadiolarieMbr.) and the over ly ing Dursztyn Lime stone For ma tion/Pieniny Lime stone For -ma tion, leave no doubt that we deal here with the Czorsztyn Lime stone For ma tion(Kimmeridgian, resp. Oxfordian?–Kimmeridgian) and not the Niedzica Lime stone For ma tion (Up per Bajocian–Up per Callovian).

How ever, Wierzbowski et al. (2004; see also Krobicki & Wierzbowski, 2004)at trib uted red nod u lar lime stones at the Wielka Pustelnica klippe and in its vi cin itynot to the Czorsztyn Lime stone For ma tion but to the Niedzica Lime stone Forma-tion.

(1) In their “Klippe A” (op. cit., fig. 2C: Wielka Pustelnica klippe) they in cluded to the ‘NiedzicaLime stone For ma tion’ a thin ver ti cal band of red lime stone, sandwitched be tween the SmolegowaLime stone Fm. and the Pieniny Lime stone Fm., just above the Pieniñski Stream bed. In thin sec tionsfrom this lime stone, they rec og nized a “fil a ment and fil a ment-ju ve nile gas tro pod microfacies”,more over plank tonic foraminifers Globuligerina sp.

These au thors (op. cit.) did not il lus trate the “fil a ments” (ap par ently cross-sec -tions of thin shells of pe lagic bi valve Bositra buchi ?) which they con sider proof ofa Mid dle Ju ras sic age of the lime stone. How ever, the age range of this bi valve isknown to be Toarcian–Oxfordian (see Jefferies & Minton, 1965; Birkenmajer &Tyszka, 1996). More over, Hud son et al. (2004, p. 5, Pl. 1B) re port the oc cur rence of the foraminifer ‘Globuligerina with rare sec tions through “fil a ments” of Bositra‘ in the Oxfordian of the Czorsztyn Lime stone For ma tion at Stankowa Klippe (see alsoSidorczuk, 2005: Oxfordian of the Stankowa and Wapiennik klippes).

Pe lagic globigerinids have long been known from the Czorsztyn Lime stoneFor ma tion (e.g., Birkenmajer, 1963a, pp. 42, 267). Ac cord ing to Wierzbowski etal. (1999, fig. 14), the ge nus Globuligerina first ap pears in Oxfordian, and ac cord -ing to Hud son et al., (2004), it even ranges from Bathonian through Kimmeridgian.Thus, nei ther Bositra fil a ments (Toarcian–Oxfordian), ei ther sin gle, or in as so ci a -tion with Globuligerina, nor the sole oc cur rence of the ge nus Globuligerina(Bathonian–Kimmeridgian) could be a proof for a Mid dle Ju ras sic age of thediscussed limestone.

(2) In their “Klippe B”, Wierzbowski et al. (2004, fig. 2E), at trib uted to the ‘Niedzica Lime stoneFor ma tion’ a bed (1 m thick) of red nod u lar lime stone which oc curs be tween the radiolarites(Czajakowa Radiolarite Fm.) in the east, and a klippe of the Smolegowa Lime stone Fm./FlakiLime stone Fm. in the west. They be lieved that the sec tion is continuous.

How ever, they are cer tainly wrong, be cause all these con tacts are tec tonic, caused byNNE–SSW-trending Mio cene faults which densely cut the area (see Figs 10A, 16A).

The Globochaete zoospores rec og nized by Wierzbowski et al. (2004) in rednod u lar lime stone at trib uted by them to the ‘Niedzica Lime stone For ma tion’ can -

24 K. BIRKENMAJER

not be con sid ered as a Mid dle Ju ras sic age-in di ca tor. The zoospores Globochaetealpina Lombard have a very long strati graphic range (?Tri as sic–Ju ras sic–EarlyCre ta ceous). In the Pieniny Klippen Belt they range from Bajocian/Bathonian(Krupianka Lime stone Fm. – G³uchowski, 1987, fig. 4) up to Tithonian–Berriasian, where they are most fre quent (Birkenmajer, 1954: Globochaete lime stones =Dursztyn Lime stone For ma tion – see Birkenmajer, 1963a; 1977, pp. 75, 78, 80; seealso Rehákova & Wierzbowski, 2004).

The above crit i cism as to the oc cur rence of the sup posed ‘Niedzica Lime stoneFor ma tion’ (Wierzbowski et al., 2004) in the Czertezik Suc ces sion, ex tends mu ta -tis mu tan dis, to the Wysokie Ska³ki (Wysoka Mt) sites in the Lit tle Pieniny Range.Again, the pres ence of Globuligerina in not a proof for a Mid dle Ju ras sic age of thenod u lar lime stone at trib uted by them to the “Niedzica Lime stone For ma tion” in -stead of the Czorsztyn Lime stone Fm. (Kimmeridgian or Oxfordian– Kimmerid-gian), as es tab lished earlier (Birkenmajer, 1970).

Wierzbowski et al. (op. cit.) have pre sented some very sche matic, poorly tec -toni cally in ter preted, field sec tions of the Czertezik Suc ces sion at Wysokie Ska³ki.Ac cord ing to my ob ser va tions, the Czajakowa Radiolarite For ma tion is much morestrongly folded than it was shown in their fig. 4A: at least two folds with cores (re -


Fig. 10. A. Pieniñski Potok stream val ley, right slope. Re in ter pre ta tion of geo log i cal struc ture of“klippe B” (Wierzbowski et al., 2004, fig. 2E). Czertezik Unit: 1 – Smolegowa Lime stone Fm.; 2 –Czajakowa Radiolarite Fm.; 3 – Czorsztyn Lime stone Fm.; f – Mio cene transversal fault (see Fig. 15).B. Pieniñski Potok stream val ley, right slope, slightly up stream from the Wielka Pustelnica klippe(see Fig. 15). Czertezik Unit: 1 – Smolegowa Lime stone Fm.; 2 – crinoidal lime stone brec cia(nep tu nian dyke); 3 – Jaworki For ma tion (red marls). Pieniny Nappe: 4 – Up per Li assic spottylime stones; f – Miocene faults

cum bent anticlines) built of green radiolarites (Podmajerz Radiolarite Mbr) andlimbs (re cum bent syn clines) – of red radiolarites (Buwa³d Radiolarite Mbr), oc curthere, in stead of ap par ently ‘strati graphic’ al ter na tion of the green and red radiola-rites. Their “ammonitico rosso-type red nod u lar lime stone of the Niedzica Lime -stone For ma tion” (fig. 4: 2), at trib uted by me to the Czorsztyn Lime stone Fm. (seeBirkenmajer, 1970), forms a thin tec tonic slab inbetween the red crinoidal lime -stone (Krupianka Lime stone Fm.) and the folded radiolarites (Czajakowa Radiola-rite Fm.), both con tacts be ing tec tonic (overthrusts).

Wierzbowski’s et al. field in ves ti ga tions at Wysokie Ska³ki were very in com -plete, in deed. How ever, if care fully mapped, the au thors would find that, in manyparts of this moun tain group, there are well ex posed strati graphic sec tions show ingnor mal suc ces sion of strata: from the Smolegowa Lime stone Fm. (at the bot tom);through the Krupianka Lime stone Fm. or the Flaki Lime stone Fm.; then theCzajakowa Radiolarite Fm. (with the Podmajerz Radiolarite Mb. at the base, andthe Buwa³d Radiolarite Mbr higher up); the Czorsztyn Lime stone Fm.; the Dur-sztyn Lime stone Fm.; and, fi nally, the Pieniny Lime stone Fm. (see Birkenmajer,1970, Pls I, V). And not a trace of the ‘Niedzica Lime stone For ma tion’ in strati -graphic po si tion be tween the Krupianka Lime stone Fm., resp. the Flaki Lime stoneFm., and the Czajakowa Radiolarite Fm. (!)

Dursztyn Lime stone For ma tion (Birkenmajer, 1977). This unit is dis tin guish -able at the base of the Pieniny Lime stone For ma tion in case of not too-strong tec -tonic de for ma tion. This is a mas sive, un bed ded, pink ish (in lower part) to cream-white (in higher part) lime stone, 2–4 m thick, pre vi ously de scribed as the Calpio-nella lime stone. It cor re sponds to the Korowa Lime stone Mem ber (lower unit) andthe Sobótka Lime stone Mem ber (up per unit) in typ i cal de vel op ment of the for ma -tion (see Birkenmajer, 1977, p. 75).

The lime stone is best vis i ble at Sutrówka (748 m), in the Ociemne-Sutrówka-Bojków Groñ Tec tonic Win dow, and in a small klippe at east ern most tip of theCzertezik klippe (Fig. 16A). In the Wielka Pustelnica klippe, this lime stone is rec -og niz able in mid dle part of the sec tion (Fig. 8, 9: 4a; see also Birkenmajer, 1977,fig. 21B). It is also vis i ble in a ra vine at left slope of the Huliñski Potok val ley, northof blue tour ist path (see Fig. 16A).

The Dursztyn Lime stone For ma tion (red and white Calpionella lime stone), 6–8m thick, is well de vel oped in the Jaworki area: at Wysoka Mt (Wysokie Ska³ki Mt,1051,8 m), and at sev eral smaller klippes be tween Wysoka and Stachurówka(Birkenmajer, 1970).

Pieniny Lime stone For ma tion (Birkenmajer, 1977). This lithostratigraphicunit, con sist ing of bed ded white to grey, slightly spotty lime stones with con cre tions and bands of brown ish to black cherts (Hornsteinkalk fa cies of Uhlig, 1890; chertylime stone vel Biancone fa cies of Birkenmajer, 1977) is well de vel oped in theCzertezik Suc ces sion where it is 40–60 m thick. Its age cor re sponds to Berriasianthrough Hauterivian, pos si bly to Barremian–Aptian (cf. Birkenmajer, 1977, p. 98).

Kapuœnica For ma tion (Birkenmajer, 1977). There is a grad ual pas sage fromthe Pieniny Lime stone For ma tion to the Kapuœnica For ma tion ob serv able at

26 K. BIRKENMAJER

Czertezik Mt. (Birkenmajer, 1979, p. 180): black shale in ter ca la tions ap pear be -tween white-grey spotty lime stone lay ers (which rep re sent an up per part of thePieniny Lime stone Fm.). They are soon re placed by black shaly lime stone anddark-green spotty marls (Brodno Mbr), fi nally by light-green and blackish spottylime stone lay ers with green and brown chert bands, al ter nat ing with green shale and marl (Rudina Mbr). The age of the for ma tion cor re sponds to Aptian–Albian(Birkenmajer, 1977, p. 102). Thick ness of the for ma tion var ies be tween 15 and30 m.

In the area of the Pieniny Na tional Park, the for ma tion is ex posed at only foursites:

(i) At blue tour ist path, south ern ap proaches to Czertezik Mount, at 600 m a.s.l.(Birkenmajer, 1977, fig. 21A; 1979, figs 84, 86; see Figs 7, 16A);

(ii) At SE slope of Czertezik Mt (blue tour ist path), at 630 m a.s.l. (Fig. 16A);(iii) At blue tour ist path south of the Burzana Polana alp (Fig. 16A);(iv) At left slope of the Pieniñski Potok stream val ley op po site the Wielka

Pustelnica klippe (Fig. 16A).Jaworki For ma tion (Birkenmajer, 1977: Jaworki Marl For ma tion; Birken-

majer & Jednorowska, 1987: Jaworki For ma tion). Green marls (Brynczkowa MarlMbr) and red marls (Macelowa Marl Mbr) have been rec og nized in the JaworkiFor ma tion of the Czertezik Suc ces sion. The for ma tion poorly crops out at nu mer -ous sites, coat ing the Ju ras sic–Lower Cre ta ceous klippes ex posed in all tec tonicwin dows of the Czertezik Suc ces sion in the Pieniny Mts (Figs 16A, B, 19). The ageof the for ma tion cor re sponds to Up per Albian–Coniacian (cf. Alexandrowicz,1966; Birkenmajer, 1977; B¹k, 1998). The for ma tion seems to be de void offlysch-sand stone in ter ca la tions (mem bers). Its thick ness is dif fi cult to es tab lish due to strong tec tonic dis tur bances: it prob a bly does not ex ceed 50–60 m.

Sromowce For ma tion (Birkenmajer, 1977). A very poor ex po sure of cal car e -ous sand stones and shales south west of Stachurówka (val ley slope south of bluetour ist path) rep re sents the Sromowce For ma tion (Santonian–Campanian – op.cit.). Its thick ness prob a bly ex ceeds 30–50 m (Fig. 11).

DIS TRI BU TION OF THE CZERTEZIK SUC CES SIONIN THE PIENINY NA TIONAL PARK (Figs 12–19)

In the Pieniny Na tional Park and its near est vi cin ity, the Czertezik Suc ces sionoc curs in the fol low ing ar eas:

I. Kotuñka klippe and vi cin ity, Szczawnica Ni¿na. It is di vided from the east bythe Orlica Dis lo ca tion Zone; and from the west by the Zawiesy-Kras Dis lo ca tionZone (Fig. 15);

II. The area be tween the Zawiesy-Kras Dis lo ca tion Zone in the east and theSzopczañski (Sobczañski) W¹wóz (gorge) Dis lo ca tion Zone in the west. There arethree tec tonic win dows: IIA. the Czertezik-Zamkowa Góra Tec tonic Win dow (Fig.16A); IIB. the Kurnikówka Tec tonic Win dow (Fig. 16A); IIC. the Ociemne-Sutrówka-Bajków Groñ Tec tonic Win dow (Fig. 16B);


III. The area be tween the Szopczañski (Sobczañski) W¹wóz (gorge) Dis lo ca -tion Zone in the east, and the Straszny Potok stream Dis lo ca tion Zone in the west.Three sep a rate ar eas: III.A. Pod Zagroñ Potok (stream); III.B. Polana Pod Macela-kiem alp; and III.C. Koœció³ek-Gumionek-Kirowa Ska³ka klippes, will be de -scribed (Fig. 16B).

Note: In the area be tween the G³êboki Potok stream near Sromowce Wy¿ne and the CzubataSka³a klippe (IVa. Piekie³ko-G³êboki Potok stream Tec tonic Win dow; IVb. Niedzica Cas tle-CzubataSka³a klippe Tec tonic Win dow), sev eral small klippes have been mapped, orig i nally at trib uted to theCzertezik Suc ces sion (see Birkenmajer, 1960a, 1963b; 1977). Dur ing the pres ent re vi sion of thegeo log i cal map, to 1:5,000 scale, it was found that, most prob a bly, we deal here with a va ri ety of theBranisko Suc ces sion and not the Czertezik Suc ces sion. A closer de scrip tion of geo log i cal re la tionswill be presented in another paper.

28 K. BIRKENMAJER

Fig. 11. Lithostratigraphic logs of the Czertezik Suc ces sion at the Pieniñski Potok stream (A – rightslope; B – left slope). Black – con densed zone of haematite-man ga nese lime stone/marl; h – hi a tus;hatched – brec cia of the nep tu nian dyke

I. Kotuñka klippe and vi cin ity (Fig. 15)

A small iso lated klippe called Kotuñka, con sist ing of the Czorsztyn Lime stoneFm. and the Dursztyn Lime stone Fm., which sticks out of the Dunajec River bed,to gether with a nearby ex po sure of the fossiliferous Krempachy Marl For ma tion,and the Skrzypny Shale For ma tion (re cently de scribed by Myczyñski, 2004, fig. 3), above the road from Szczawnica to Kroœcienko, pre vi ously dis tin guished byHorwitz (1922) as the “Dumortieria beds”, have been at trib uted to the CzertezikSuc ces sion. The sec tion of the lat ter is tec toni cally re versed: the fossiliferous bedsdip north un der black flysch strata of the Szlachtowa For ma tion, and sand stonesand con glom er ates of the Jarmuta For ma tion, both rep re sent ing the Grajcarek Unit.

In the area be tween Szczawnica and Toporzyska (above Kroœcienko, yel lowtour ist path), the Czorsztyn Unit is miss ing at tec tonic con tact of the PieninyKlippen Belt with the Magura Nappe. Be tween Toporzyska and Zawiesy (Kroœ-cienko), the Czertezik Unit co mes to this tec tonic con tact. This was the rea son thatboth the Kotuñka klippe and the fossiliferous strata (Krempachy Marl andSkrzypne Shale for ma tions) were in cluded by the pres ent au thor to the CzertezikSuc ces sion and not to the Czorsztyn Suc ces sion where they could al ter na tively be -


Fig. 12. Dis tri bu tion of the Czorsztyn and Czertezik units in the Pieniny Na tional Park of Po land(af ter Birkenmajer, 1973a, 1976a, slightly mod i fied and sup ple mented). 1 – Czorsztyn Unit; 2 –Czertezik Unit; 3 – Niedzica-, Branisko-, Pieniny- and Haligovce nappes; 4 – Ju ras sic and Cre ta ceousof the Grajcarek Unit, and transgressive Jarmuta Fm. (Maastrichtian) in the Pieniny Klippen Belt; 5 –Palaeogene of the Magura Nappe and transgressive Palaeogene in the Pieniny Klippen Belt; 6 –Podhale Palaeogene (Podhale De pres sion and transgressive Podhale Palaeogene in the PieninyKlippen Belt); 7 – se lected transversal faults (Mio cene). Tec tonic Win dows: C – Czertezik-Zamkowa Góra; M – Polana pod Macelakiem; O – Ociemne-Sutrówka-Bojków Groñ. Note:Fresh-wa ter Neo gene de pos its and Mio cene an de site intrusions omitted

long. How ever, in the lack of ex po sures of in ter me di ate strata, the pres ent at tri bu -tion cannot be regarded definite.

II. Area be tween the Zawiesy-Kras Dis lo ca tion Zone and the W¹wózSzopczañski Dis lo ca tion Zone (Figs 16A, 17)

II.A. The Czertezik-Zamkowa Góra Tec tonic Win dow is the area of type oc -cur rence of the Czertezik Suc ces sion (Birkenmajer, 1959b, 1977, 1979). Ex po -sures of this suc ces sion oc cur at blue tour ist path of the Sokola Peræ ridge from thePolana Sosnów alp, through Czertezik mount (772–774 m) to the Prze³êcz CzerteŸpass. Then, be fore the Polana Walusiówka alp, they turn south-west wards down the Pieniñski Potok stream val ley, through Czerwone Ska³ki klippes to the WielkaPustelnica klippe (684 m) and the Zamkowa Góra mount (799 m), fi nally to klippesex posed in a deep ra vine, left trib u tary to the Potok Huliñski creek.

This tec tonic win dow, its axis strik ing ENE–WSW, is 2 km long and 200–250 m wide. From the west (Polana Wyrobek alp), and from the east (west ern area ofKras), the win dow ter mi nates at submeridional (NNE–SSW) faults, partly rec og -

30 K. BIRKENMAJER

Fig. 13. Dis tri bu tion of the Niedzica-, Branisko-, Pieniny-. Haligovce- and Magura suc ces sions inthe Pieniny Klippen Belt (af ter Birkenmajer, 1973a, 1976a, slightly mod i fied and sup ple mented). 1 –Niedzica Suc ces sion/Nappe; 2 – Branisko Suc ces sion/Nappe; 3 – Pieniny Suc ces sion/Nappe; 4, 5 –Haligovce Suc ces sion/Nappe (4 – Ju ras sic and Cre ta ceous de pos its; 5 – Tri as sic de pos its); 6 –Czorsztyn and Czertezik units); 7 – Ju ras sic and Cre ta ceous of the Magura Suc ces sion (GrajcarekUnit) and transgressive Jarmuta Fm. (Maastrichtian) in the Pieniny Klippen Belt; 8 – Palaeogene ofthe Magura Nappe and transgressive Palaeogene in the Pieniny Klippen Belt; 9 – Podhale Palaeogene(Podhale de pres sion and transgressive Palaeogene in the Pieniny Klippen Belt); 10 – se lectedtransversal faults (Mio cene). Note: Fresh-wa ter Neo gene de pos its and Miocene andesite intrusionsomitted

nized al ready by Horwitz (1963, east ern map sheet). Along its whole length, thetec tonic win dow is densely cut by such faults, ev ery ten to sev eral tens of metres.

The Pieniny Nappe bor ders the tec tonic win dow from the south, while theBranisko Nappe – from the north. Palaeogene rocks of the klippen man tle (Szcza-wnica For ma tion: Paleocene–Lower Eocene, cf. Birkenmajer & Dudziak, 1988;Birkenmajer & Oszczypko, 1989) un con form ably cover var i ous lithostratigraphicunits of these two nappes and of the Czertezik Unit ex posed in the tec tonic win dow.This sug gests that the tec tonic win dow was al ready ex posed to the sur face, itsnappe cover eroded, prior to the Paleocene trans gres sion. All pre-Palaeogene tec -tonic units (the Czertezik Unit, the Branisko and the Pieniny nappes), and theirPalaeogene cover are tra versed by the same me rid i o nal fault sys tem (NNE–SSW)at trib uted to Mid dle Mio cene (cf. Birkenmajer & Pécskay, 1999, 2000).


Fig. 14. Geo log i cal map of an area at Szczawnica Ni¿na: be tween the Orlica Dis lo ca tion Zone(east) and the Zawiesy-Kras Dis lo ca tion Zone (west). Magura Nappe: 1 – Szczawnica Fm. (Up perPaleocene–Lower Eocene); 2 – in ter ca la tions of “Magura”-type sand stone in the Szczawnica Fm.Grajcarek Unit: 3 – Jarmuta Fm. (Maastrichtian–Lower Paleocene); 4 – Malinowa Shale Fm.(Cenomanian–Campanian); 5 – Szlachtowa Fm. (Toarcian–Aalenian). Czertezik Unit: 6 – DursztynLime stone Fm. (Tithonian–Berriasian); 7 – Czorsztyn Lime stone Fm. (Kimmeridgian); 8 – SkrzypneShale Fm. (Aalenian–Lower Bajocian) and Krempachy Marl Fm. (Toarcian–Aalenian). PieninyNappe: 9 – Jaworki Fm., green marls (Albian–Cenomanian) and Kapuœnica Fm. (Aptian–Albian);10 – Pieniny Lime stone Fm. (Berriasian–Barremian). Blank – cov ered; 11 – con glom er ate in ter ca la -tions; 12 – faults; 13 – north ern bound ary fault zone of the Pieniny Klippen Belt; 14 – es carp ments;15 – strike and dip; 16 – strike and dip with nor mal po si tion of sole mark ings; 17 – strike and dip withtec toni cally over turned po si tion of sole markings; 18 – vertical dip

Lithostratigraphic suc ces sion of the Czertezik Unit in this tec tonic win dow isnearly com plete (Bajocian–Santonian): the Smolegowa Lime stone Fm. (white andgrey crinoidal lime stone); the Krupianka Lime stone Fm. re placed to wards SW bythe Flaki Lime stone Fm; the Czajakowa Radiolarite Fm.; the Czorsztyn Lime stoneFm.; the Dursztyn Lime stone Fm.; the Pieniny Lime stone Fm.; the Kapuœnica Fm.;the Jaworki Fm.; and the Sromowce Fm. (Birkenmajer, 1959b, 1977, 1979). Com -pe tent lime stones (Bajocian, and Berriasian–Barremian) are rep re sented best,while poorly ex posed, in com pe tent Cre ta ceous shales and marls (Kapuœnica andJaworki for ma tions) are of ten very strongly tec toni cally de formed, their thick nessbe ing tec toni cally re duced un der the overthrust Pieniny and Branisko nappes.

II.B. Kurnikówka Tec tonic Win dow. In this tec tonic win dow (Figs 16, 17),we find grey crinoidal lime stone (Smolegowa Lime stone Fn.) stick ing out of redand green marls of the Jaworki For ma tion. The win dow is 50–100 m wide, itslength amounts to about 500 m. The Branisko Nappe bor ders the tec tonic win dowfrom the south and the north. Patches of the Klippen Palaeogene (the SzczawnicaFm., and the Piwniczna Sand stone Mbr of the Magura Fm.) are scat tered over theBranisko Nappe.

II.C. Ociemne-Sutrówka-Bojków Groñ Tec tonic Win dow.This tec tonicwindow (Figs 16, 17, 18) is well ex posed along left slope of the Ociemne val ley,along a moun tain ridge which runs from the Ociemny Wierch hill (615 m) to theSutrówka hill (748 m) and, fur ther west, to the Bojków Groñ hill (cross ing of tour ist paths: yel low, to Kroœcienko-Trzy Korony/blue, to Sokolica). Ju ras sic–Lower Cre -ta ceous rocks of the Czertezik Suc ces sion are mostly ex posed here: the Smolegowa Lime stone Fm. (> 50 m thick, vis i ble north of the Ociemny Wierch peak, 615 m,and on north ern slope of Sutrówka, 748 m); red crinoidal lime stone of theKrupianka Lime stone Fm. (poorly ex posed near Ociemny Wierch); radiolarites ofthe Czajakowa Radiolarite Fm. (green radiolarites = Podmajerz Radiolarite Mbr,> 2 m thick, and red radiolarites = Buwa³d Radiolarite Mbr, 2–3 m thick), are wellde vel oped, ex posed over a large area, from the Ociemny Wierch hill in the east,along the Ociemne val ley and ridge, and at Sutrówka-Bojków Groñ; the redradiolarites are fol lowed by well de vel oped red nod u lar lime stone (CzorsztynLime stone Fm., 1–4 m thick); mas sive pink ish and white Calpionella lime stone(Dursztyn Lime stone Fm., 2–4 m thick) may lo cally be found; the Pieniny Lime -stone Fm. (> 50 m thick) is best ex posed along moun tain ridge from OciemnyWierch to Sutrówka.

The Ju ras sic–Lower Cre ta ceous rocks of the Czertezik Unit con tact at both sides of the tec tonic win dow with in com pe tent marls of the Jaworki For ma tion, lo callyalso with flysch rocks of the Sromowce Formation.

The Branisko Nappe forms south ern frame of the tec tonic win dow, as is wellseen on right slope of the Ociemne val ley. The north ern frame of the win dow,formed by this nappe, is much re duced at Toporzyska and eastwards, where Cre ta -ceous marls of the win dow come into di rect tec tonic con tact with the MaguraNappe Palaeogene flysch (Fig. 16).

32 K. BIRKENMAJER

aj c

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Miocene faults

Laramianoverthrusts

Escarpments

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Smolegowa Limestone Formation

Krupianka Limestone Formation

Czajakowa Radiolarite Formation

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Kapuœnica Formation

Jaworki Formation

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Fig. 15. Geological structure of the Czertezik-Zamkowa Góra Tectonic Window, and the Polana Kurnikówka Tectonic Window

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Szczawnica Formation and PiwnicznaSandstone Member (Magura Fm.)

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Branisko and Pieniny nappes

Magura Nappe: Szczawnica Formation andPiwniczna Sandstone Member (Magura Fm.)


Covered

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Fig. 16. Geological structure of the Ociemne-Sutrówka-Bojków Groñ Tectonic Window and the Polana Kurnikówka Tectonic Window

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Palaeogene mantle: Szczawnica and Magura formations

Magura Nappe: Szczawnica Formation

Skrzypny Shale Formation




Cze

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Kapuœnica Formation and Jaworki Formation

Miocene faults

Laramianoverthrusts

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Czertezik – Zamkowa GóraTECTONIC WINDOW

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Zamkowa Góra

Ostry Wierch854

Po lana Kosa rzyska

Trzy Korony(923)

(?)Czorsztyn Unit: 1 – Smolegowa Limestone Fm.; 2 – Krupianka Limestone Fm.; 3 – Czorsztyn Limestone Fm., 4 – Dursztyn Limestone Fm.; 5 – Cretaceous limestones and marls (mainly Jaworki Fm.).Branisko Nappe: 6 – Harcygrund Shale Fm.; 7 – Podzamcze Limestone Fm.; 8 – Sokolica Radiolarite Fm.; 9 – Czajakowa Radiolarite Fm.; 10 – Czorsztyn Limestone Fm. (Upszar Limestone Mbr); 11 – Pieniny Limestone Fm.Pieniny Nappe: 12 – Liassic spotty limestones and Skrzypny Shale Mbr; 13 – Podzamcze Limestone Fm.; 14 – Sokolica Radiolarite Fm.; 15 – Czajakowa Radiolarite Fm.; 16 – Czorsztyn Limestone Fm. (Upszar Limestone Mbr); 17 – Pieniny Limestone Fm.

m a.s.l.m a.s.l.

CZE

RE

ZI

UN

IT

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NP

IEI

NY

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A

Fig. 17. Geological cross-section between Trzy Korony and Ociemny Wierch, across three tectonic windows: the Czertezik-Zamkowa Góra Tectonic Window, the Polana Kurnikówka Tectonic Window, and the Ociemne-Sutrówka-Bojków Groñ Tectonic Window

A small klippe con sist ing of green and red radiolarites (Czajakowa Radiolarite Fm), red nod u larlime stone (Czorsztyn Lime stone Fm.) and pink mas sive lime stone (Dursztyn Lime stone Fm.), isex posed at Toporzyska at green tour ist path lead ing from Toporzyska to Sokolica. It oc curs at faultcon tact of the Pieniny Klippen Belt with the Magura Nappe rep re sented here by the SzczawnicaFor ma tion. This klippe, at trib uted now to the Czertezik Unit, has pre vi ously been marked on maps asthe Niedzica Suc ces sion (e.g., Birkenmajer, 1959a).

The dis cussed tec tonic win dow is about 1700 m long and 200–400 m wide. Itsaxis, ENE–WSW, is ro tated coun ter clock wise by about 30° with re spect to axis ofthe Czertezik-Zamkowa Góra Tec tonic Win dow, and to strikes of the overthrustBranisko Nappe, both be ing nearly lat i tu di nal (E–W). The tec tonic win dow and itslimbs are tra versed by submeridional to me rid i o nal faults, NNE–SSW to N–S,dated at Mid dle Mio cene (Birkenmajer & Pécskay, 1999, 2000).

III. The area be tween the Szopczañski W¹wóz Dis lo ca tion Zoneand the Straszny Potok Dis lo ca tion Zone (Fig. 19)

Three small ar eas of Ju ras sic–Lower Cre ta ceous klippes are ex posed here. Thefirst two, III.A and III.B, rep re sented by the Czertezik Suc ces sion, are within alarge field of the Klippen Palaeogene; the third one, III.C – is rep re sented by theCzorsztyn Suc ces sion at its con tact with the Pieniny Nappe.

III.A. Potok Pod Zagroñ creek. In the up per most part of right trib u tary to theBia³y Potok stream (south of Tylka vil lage), called here the Potok Pod Zagroñcreek, a row of 6 klippes crops out. They are sur rounded by the autochthonousPalaeogene flysch: the Szczawnica For ma tion very rich in con glom er ates and sed i -men tary brec cias con tain ing lo cal Klippen ma te rial (mainly clasts from the PieninyLime stone Fm.). As a whole, the klippes and the Palaeogene form an an ti cli nal


Fig. 18. Geo log i cal cross-sec tion of the Czertezik Unit at Sutrówka. 1 – Smolegowa Lime stoneFm.; 2, 3 – Czajakowa Radiolarite Fm. (2 – green radiolarites = Podmajerz Radiolarite Mbr; 3 – redradiolarites = Buwa³d Radiolarite Mbr); 4 – Czorsztyn Lime stone Fm.; 5 – Dursztyn Lime stone Fm.; 6 – Jaworki Fm. (marls); f – gap ing fault

struc ture strik ing ESE–WNW, its north ern and south ern limbs rimmed by thePiwniczna Sand stone Mem ber of the Magura For ma tion (Lower Eocene). Theanticline is cut by submeridional (NNE–SSW) faults which dis place both theklippes and their Palaeogene cover.

The klippes dip 80° NW or SE, ei ther in nor mal po si tion (east ern klippes) or inover turned po si tion (west ern klippes). The fol low ing for ma tions have been rec og -nized: white to grey, of ten shaly crinoidal lime stone (Smolegowa Lime stone Fm.,40–50 m thick), red crinoidal lime stone (Krupianka Lime stone Fm., 3 m); red nod -u lar lime stone (Czorsztyn Lime stone Fm. 1–3 m thick); and white cherty lime stone(Pieniny Lime stone Fm., c. 10 m).

No radiolarites (Czajakowa Radiolarite Fm.) have been found in the klippes,how ever the pres ence of the Pieniny Lime stone Fm. in the wes tern most klippe(small wa ter fall) sup ports at tri bu tion of these klippes to the Czertezik Suc ces sion.

III.B. Polana Pod Macelakiem alp. West from the III.A. site, there is an otherrow of 5 klippes, sur rounded by the same Palaeogene cover as at the pre vi ous site.The klippes run nearly SW–NE, and are tra versed by submeridional faults(NNE–SSW).

(1) Start ing from the east, the first klippe is rep re sented by grey crinoidal lime -stone (Smolegowa Lime stone Fm.); east from it, at for est mar gin, we see weath er -ing cover of red marls (Jaworki Fm., Macelowa Marl Mbr).

(2) The sec ond klippe (at about 800 m a.s.l., in mid dle part of the alp) con sists of grey, shaly crinoidal lime stone (Smolegowa Lime stone Fm.) some 20 m thick, dip -ping south un der poorly ex posed red fine-crystalline lime stone (Czorsztyn Lime -stone Fm., c. 5 m thick).

(3) The third klippe (at a large land slide mar gin) con sists of the same fine-crys -tal line red lime stone (Czorsztyn Lime stone Fm.), c. 5 m thick.

(4) The fourth klippe (in NW part of the alp) shows an ti cli nal struc ture withgrey or slightly pink, shaly crinoidal lime stone (Smolegowa Lime stone Fm.), >15m thick, in the core, lo cally pass ing into dark-red shaly lime stone (KrupiankaLime stone Fm.), 1–2 m thick. Both limbs of the anticline con sist of red nod u larlime stone (Czorsztyn Lime stone Fm.), c. 5 m thick, pass ing up wards into mas sivepink ish to white lime stone (Dursztyn Lime stone Fm.), 2 m thick, fi nally into white,banded lime stone (Pieniny Lime stone Fm.), 3–5 m thick. The beds dip 45° NW ineast ern part of the klippe, and 75–80° NE in its west ern part (the beds are here tec -toni cally over turned to SSW).

(5) The fifth klippe, at NW mar gin of the alp, is sep a rated from the fourth one by a well vis i ble fault trending NNE–SSW. The klippe con sists of the CzorsztynLime stone, the Dursztyn Lime stone, and the Pieniny Lime stone for ma tions dip -ping nor mally at 60°NE.

West from this klippe, poor ex po sures of green marls (Jaworki Fm.: Bryncz-kowa Mbr) are vis i ble in for est road-cut tings.

Sim i larly, as in the III.A. row of klippes, we deal here with a va ri ety of theCzertezik Suc ces sion which is de void of radiolarites (= the Czajakowa RadiolariteFm.) but shows the pres ence of the Pieniny Lime stone Fm.

34 K. BIRKENMAJER

II

II

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yP

ook

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t

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od Z

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3

(Sromowce Ni¿ne)

(Tylka)

(Prz

e³ê

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ka)

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Bia³aSka³a

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P o l a n a p o d M a c e l a k i e m

(Nowa Góra)

Branisko and Pieniny nappes

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Covered

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80

Miocene faults

Laramian overthrusts

Escarpments

Tourist paths

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Jaworki Formation

Sromowce Formation

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00 100100 200 m200 m

Fig. 19 Geological structure of the Polana Pod Macelakiem Tectonic Window

III.C. Koœció³ek-Gumionek-Kirowa Ska³ka klippes. A belt of 7 klippes runsW–E at south ern mar gin of the Polana Pod Macelakiem alp and its Palaeogenecover, to the south of the III.B. klippes. The III.C. klippes are sep a rated from thePieniny Nappe, well ex posed fur ther south, by a zone of Up per Cre ta ceous marls(Jaworki Marl Fm.) and flysch rocks (Sromowce Fm.) be long ing to the same suc -ces sion as the klippes. The beds in most klippes are ver ti cal, the older ones be ingex posed in north ern part of the klippes.

(1) The first klippe (wes tern most), its beds ver ti cal and strik ing W–E, con sistsof mas sive white and pink lime stone (Dursztyn Lime stone Fm.) from the south, and of red nod u lar lime stone (Czorsztyn Lime stone Fm.) from the north.

(2) The sec ond klippe – named Koœció³ek (lo cated near for est road lead ingfrom Sromowce Ni¿ne and the Cyrlowa Ska³ka klippe to blue tour ist path atMacelak), is built by anal o gous rocks as the first one. Well dis tin guish ablesubmeridional faults (NNE–SSW) sep a rate the first from the sec ond, and the sec -ond from the third klippes.

(3) The third klippe (the larg est one) – called Gumionek (vel Gumionko),shows a good strati graphic sec tion, from north to south: mas sive white and greyshaly crinoidal lime stone (Smolegowa Lime stone Fm.), about 10 m thick; redbanded or shaly crinoidal lime stone (Krupianka Lime stone Fm.), 6 m thick; rednod u lar lime stone (Czorsztyn Lime stone Fm.), 3–4 m thick; mas sive pink lime -stone, pass ing stratigraphically up wards into mas sive white Calpionella lime stone(Dursztyn Lime stone Fm.), 2 m thick. The lat ter lime stone was in cluded byHorwitz (1963, east ern map sheet) to the “Tithonian–Neocomian”; the lat ter unitusu ally cor re sponds to the Pieniny Lime stone For ma tion of the stan dard col umn(see Birkenmajer, 1977), how ever we deal here with the Dursztyn Lime stone Fm.,and not with the Pieniny Lime stone Fm.

(4, 5) Two klippes, Nos 4 and 5, di vided from the Gumionek klippe, and fromone an other, by faults (NNE–SSW), ap pear fur ther east. In the fourth klippe, theCzorsztyn Lime stone Fm. passes stratigraphically up wards (to the south) into theDursztyn Lime stone Fm. In the fifth klippe, red crinoidal lime stone (KrupiankaLime stone Fm.) oc curs in its north ern part, and red nod u lar lime stone (CzorsztynLime stone Fm.) in its south ern part; in this klippe, the beds are tec toni cally over -turned to SSE (they dip 70–30° NNW).

(6) A small sixth klippe, con sist ing of pink ish mas sive lime stone (DursztynLime stone Fm.) is vis i ble in a for est road. It con tacts in the north with thePalaeogene Szczawnica For ma tion flysch, and in the south – with red marls of theJaworki For ma tion (Macelowa Marl Mbr), at trib uted to the Czorsztyn Suc ces sion.

(7) Fi nally, the sev enth klippe – called Kirowa Ska³ka, shows the same strati -graphic se quence of rocks as in the Gumionek klippe: ver ti cal Smolegowa-,Krupianka-, Czorsztyn-, and Dursztyn lime stone for ma tions.

Green (Brynczkowa Marl Mbr) and red (Macelowa Marl Mbr) marl and marlyshales of the Jaworki For ma tion, and flysch rocks of the Sromowce For ma tion, at -trib uted to the Czorsztyn Suc ces sion, are ex posed in road-cut tings south of theklippe, at their con tact with Dogger rocks of the Pieniny Nappe.


The whole suc ces sion of rocks in the klippes Nos 1–7 is de void of radiolarites(i.e. the Czajakowa Radiolarite Fm.) and cherty lime stones (i.e. the Pieniny Lime -stone Fm.). This in di cates that we deal here with the Czorsztyn Suc ces sion and notthe Czertezik Suc ces sion. Ap pear ance of grey crinoidal lime stone in the Smole-gowa Lime stone For ma tion, may be an in di ca tion of prox im ity of this va ri ety of theCzorsztyn Suc ces sion to the Czertezik Suc ces sion. A sim i lar de vel op ment of theCzorsztyn Suc ces sion has been rec og nized in the south ern most tec tonic win dow inthe Czorsztyn-Niedzica area (see Birkenmajer, 1963a, tab. 4; pl. XXII, fig. 4:Niedzica Cas tle type, Miêdzyhombark va ri ety).

Lo ca tion of the Koœció³ek-Gumionek-Kirowa Ska³a klippes (III.C) to the southof the Polana Pod Macelakiem alp klippes (III.B), poses some tec tonic prob lemswhich are im pos si ble to be solved cor rectly, tak ing into ac count the fact that theseklippes are to a great ex tent cov ered by Palaeogene de pos its, while dis sec tion of thearea by river ero sion does not reach deep enough to show its subsurface struc ture.We may con sider two options:

(1) That con tact of the Czorsztyn Suc ces sion sed i men tary zone with theCzertezik Suc ces sion sed i men tary zone orig i nally did not run par al lel to theCzorsztyn Ridge, but had some bays and cur va tures (maybe struc tur ally-con -trolled) where the radiolarite fa cies (Czajakowa Radiolarite Fm.) and/or the chertylime stone fa cies (Pieniny Lime stone Fm.) reached far ther north and north-westthan usual;

(2) That we deal here with a tec tonic win dow com pa ra ble in its struc ture with the Niedzica Cas tle-Czubata Ska³a one (cf. Birkenmajer, 1998b, 1999). The klippes ofthe Koœció³ek-Gumionek-Kirowa Ska³ka belt (III.C) would thus rep re sent the win -dow’s core built of the Czorsztyn Unit, while the klippes of the Czertezik Suc ces -sion (III.A and III.B) would be long to a Czertezik “Nappe” thrust over theCzorsztyn Unit from the south.

This op tion may find sup port from geo log i cal in ter pre ta tion of tec tonic struc -ture of the Jaworki area, fur ther east, where the Czertezik Unit of the Wysoka(Wysokie Ska³ki) mount ap par ently floats over the Czorsztyn Unit (see Birken-majer, 1970, Pl. V: cross-sec tions I and II.).

IV. The area be tween Czubata Ska³a and Piekie³ko near Czorsztyn

On left slope of the Dunajec River val ley, near Sromowce Wy¿ne, there are twotec tonic win dows of the Czorsztyn Unit flanked by the overthrust Branisko Nappe(IV.A. and IV.B.), with small klippes built of the Niedzica and the ?Czerteziksuc ces sions.

IV.A. Piekie³ko-G³êboki Potok Tec tonic Win dow. This is a nar row, ver ti caltec tonic win dow ex pos ing Cre ta ceous flysch rocks (Sromowce Fm.) and marls(Jaworki Fm.) of the Czorsztyn Unit from be low the Dogger rocks of the overthrustBranisko Nappe. To the Czertezik Unit have been in cluded six small klippes form -ing sep a rate tec tonic blocks squeezed at the con tact of the Dogger strata of theBranisko Nappe with the Cre ta ceous strata of the Czorsztyn Unit (see Birkenmajer,

36 K. BIRKENMAJER

1960: Piekie³ko hill above Kapuœnica ham let – pres ently above the Czorsztyn wa ter dam).

The klippes in ques tion in clude: grey crinoidal lime stone with chert in ter ca la -tions (= Flaki Lime stone Fm.) up to 10 m thick; green and red radiolarites(Czajakowa Radiolarite Fm.: Podmajerz Radiolarite Mbr and Buwa³d RadiolariteMbr.), al to gether 5–7 m thick; red nod u lar lime stone (Czorsztyn Lime stone Fm.),4–5 m thick; and Calpionella lime stones (Dursztyn Lime stone Fm.), 2–3 m thick.The Pieniny Lime stone For ma tion and the suc ceed ing Cre ta ceous strata have notbeen recognized.

This suc ces sion of strata is close to that of the Czertezik-Zamkowa Góra se -quence. How ever, lack of the Smolegowa Lime stone For ma tion at its bot tom, andof the Pieniny Lime stone For ma tion, cast doubts whether they re ally be long to theCzertezik Suc ces sion or are an in com plete suc ces sion be long ing to a north ern va ri -ety of the Branisko Suc ces sion. The lat ter one is well de vel oped nearby, atPiekie³ko (Birkenmajer, 1977, fig. 19C), at G³êboki Potok Stream, and at the FlakiRidge.

IV.B. The Niedzica Cas tle-Czubata Ska³a Tec tonic Win dow. This ver ti caltec tonic win dow is known by its well ex posed klippes of the Czorsztyn Unit whichforms the core of the win dow. It is di rectly over lain by the Maastrichtian JarmutaFor ma tion, and by sev eral overthrust tec tonic blocks and scales of the NiedzicaSuc ces sion/Nappe. The Branisko Nappe forms both flanks of the win dow (see de -tailed de scrip tion, and fig ures in Birkenmajer, 1998a, 1999).

In east ern part of the win dow, eastwards from the Czubata Ska³a klippe, there isa klippe called Wspólna Ska³a (pres ently: Zbójnicka Ska³a), known al ready toUhlig (1890, fig. 20), and at trib uted to the Czertezik Suc ces sion by Birkenmajer(1963b, 1977, fig. 19A).

The sec tion of the klippe ex posed the fol low ing for ma tions: the Szlachtowa Fm. (>3 m); the Skrzypny Shale Fm. (2–2.5 m); the Smolegowa Lime stone Fm. (1.5–3m); the Flaki Lime stone Fm. (2.5–3 m); the Czajakowa Radiolarite Fm. (Podmajerz Radiolarite Mbr: 1–1.5 m; Buwa³d Radiolarite Mbr: 5–6 m); and the CzorsztynLime stone Fm. (4 m).

The Dursztyn Lime stone For ma tion, the Pieniny Lime stone For ma tion, and thesuc ceed ing Cre ta ceous lithostratigraphic units have not been rec og nized in theklippe.

Small thick ness of the Smolegowa Lime stone For ma tion is at vari ance with typ -i cal sec tions of the Czertezik Suc ces sion as known from its type area (Czertezik-Zamkowa Góra – vide), and from the area south of Jaworki, Lit tle Pieniny Range(cf. Birkenmajer, 1970) in which thick ness of the Smolegowa Lime stone For ma -tion does not drop be low 50–70 m.

This klippe re sem bles those ones of the Piekie³ko Tec tonic Win dow (IV.A.).Sim i larly, it could be long to the Branisko Suc ces sion in stead of the CzertezikSuc ces sion.


DIS TRI BU TION OF THE CZERTEZIK SUC CES SION ELSE WHEREIN PO LAND AND EAST ERN SLOVAKIA

Pol ish/Slo vak fron tier

The Czertezik Suc ces sion of the Lit tle Pieniny Range con tin ues east ward fromthe Durbaszka mount (942 m) along the Pol ish-Slo vak fron tier: at Stachurówka (velBorsuczyny, 887 m) in the west, at Wysoka (Wysokie Ska³ki, 1052 m), Jaworzyna(1001 m), Smerekowa (1014 m), and fur ther east at Wstysie Ska³ki (vel Watrisko,960 m). South of Jaworki, its stra tig ra phy (see Birkenmajer, 1970) re sem bles verymuch that one of the Czertezik-Zamkowa Góra Tec tonic Win dow. Anal y sis of thede tailed geo log i cal map, 1:10,000 scale, in di cates that the Czertezik Unit prob a blyforms a nappe-like slab there thrust over the Czorsztyn Unit (see Birkenmajer,1970, Pl. V: cross-sec tions I, II).

At Homole Gorge and in its vi cin ity, there are many ex cel lent rock ex po sureswhich pro vide ev i dence that the Niedzica Nappe (lower) and the Branisko Nappe(up per) rest upon al most hor i zon tal slab of the Czorsztyn Unit – a cu ri os ity in thePieniny Klippen Belt as a whole (see Birkenmajer, 1970). How ever, there are nocon tacts of the Czertezik Unit and the Niedzica Nappe ex posed in the Homole area.

East ern Slovakia

(1) At Litmanová, East ern Slovakia, a site of the Czertezik Suc ces sion was vis -ited by the au thor in 1967, in the com pany of Drs Stefan W. Alexandrowicz, VieraScheibnerová and Ervín Scheibner. In the Velky Lipník stream (Litmanová, northof the church), the fol low ing strati graphic suc ces sion has been in ves ti gated.

Fossiliferous black shales with fos sil-bear ing (mainly ammonites) sid er ite con -cre tions at trib uted by Scheibner (1964a, b) to the “Murchisonae beds” (= SkrzypnyShale Fm.); grey crinoidal lime stone (= Smolegowa Lime stone Fm.), about 2 mthick, which, ac cord ing to Scheibner, yielded Stephanoceras humphriesianum.Strati graphic bot tom (ver ti cal lime stone wall in the ex po sure) of the lime stone wasstrongly pyritized, hardground-type. There was a sed i men tary break be tween theshales and the lime stone, cor re spond ing – ac cord ing to Scheibner – to amonitezones which are miss ing be tween the Hyperlioceras discites Zone (in thespherosiderite-bear ing shales) and the Stephanoceras humphriesianum Zone (inthe crinoidal lime stone). Higher upslope have been found, in the suc ces sion: greenradiolarites (= Podmajerz Radiolarite Mbr, Czajakowa Radiolarite Fm.); redradiolarites (= Buwa³d Radiolarite Mbr, Czajakowa Radiolarite Fm.); red nod u larlime stone (= Czorsztyn Lime stone Fm.); and pink ish to white Calpionellalimestone (= Dursztyn Limestone Fm.).

Small thick ness of the Smolegowa Lime stone Fm. in this sec tion may sug gestthat we deal here with the Niedzica Suc ces sion. How ever, when go ing up stream asmall west ern trib u tary (Rozdziel stream) to the Velky Lipník stream, we have ob -served that the white crinoidal lime stone (= Smolegowa Lime stone For ma tion)quickly thick ened to sev eral tens of metres, as is the case with the Czertezik Suc ces -

38 K. BIRKENMAJER

sion, and not the Niedzica Suc ces sion. This was the rea son that Scheibner (1964a,p. 642) at trib uted the dis cussed se quence to the Czertezik Suc ces sion.

North wards from this ex po sure, in an other tec tonic scale of the spherosideriteshales (= Skrzypny Shale Fm.), Scheibner found Graphoceras v-scriptum. Theshales were folded to gether with red Globotruncana marls (= Jaworki Fm.:Macelowa Marl Mbr) and green lime stones of the Pomiedznik Fm. – both rocksrep re sent ing the Czorsztyn Unit. Still fur ther north, there were con glom er ates andsed i men tary brec cias of the Jarmuta For ma tion, some 20–30 m thick, con sist ingmainly of rock frag ments de rived ei ther from the Czertezik- or the Czorsztyn Suc -ces sions, or from both. They could rep re sent the Grajcarek Unit.

(2) An other klippe in north ern part of the Litmanová vil lage, de scribed and il -lus trated as the Czertezik Suc ces sion by Wierzbowski et al. (2004, fig. 3: 3; fig. 6,beds 1–6; but not bed 7?) be longs, in my opin ion, to the Niedzica Suc ces sion. Thesec tion shows (from top down wards):

The Dursztyn Lime stone Fm. (> 1 m); the Czorsztyn Lime stone Fm. (c. 1 m); the Czajakowa Radiolarite Fm. (3.4 m); very thin Niedzica Lime stone Fm. (0.75 m); fi -nally very thin (2.4 m) crinoidal lime stones: Krupianka Lime stone Fm.(?) and theSmolegowa Lime stone Fm. (2.4 m); they are un der lain by the Skrzypny Shale Fm.

By its field ap pear ance, lithological char ac ter and small thick nesses of the par -tic u lar lithostratigraphic units, this sec tion re sem bles very much a sec tion of theNiedzica Suc ces sion which is ex posed at en trance to the Skalski Potok Na ture Pre -serve (“Bodnarówka”), at Jaworki, Po land.

(3) In the pres ent au thor’s opin ion, also the sec tion at Milpoš quarry (TorysaRiver val ley), still fur ther east, is a typ i cal rep re sen ta tive of the Niedzica Suc ces -sion, and not the Czertezik Suc ces sion. In this sec tion (Wierzbowski et al., 2004,figs 3, 7), the fol low ing lithostratigraphic units oc cur:

The Smolegowa Lime stone Fm., 3 m thick; the Krupianka Lime stone Fm., 0.8m thick; the Niedzica Lime stone, 1.5 m thick; the Czajakowa Radiolarite For ma -tion, c. 5 m thick; the Czorsztyn Lime stone (1 m thick). Then, sep a rated by a fault,co mes the “Horná Lysa Lime stone Fm.” (equiv a lent to the Dursztyn Lime stoneFm.), c. 7 m. thick.

The char ac ter, mode of ap pear ance and age of the ammonite fauna de scribedfrom the Niedzica Lime stone For ma tion in Milpoš quarry by Wierzbowski et al.(2004, fig. 8) are the same as those ones in the Niedzica Lime stone For ma tion (Up -per Bajocian–Lower Callovian) of the Niedzica Suc ces sion at its type lo cal ityNiedzica vil lage (Birkenmajer & Znosko, 1955; Birkenmajer & Myczyñski, 1984), and at Czajakowa Ska³a klippe (Birkenmajer et al., 1960; Birkenmajer & My-czyñski, 1984).


TEC TONIC AND PALAEOGEOGRAPHIC PO SI TION OF THECZERTEZIK SUC CES SION, DIS CUS SION AND CON CLU SIONS

Car to graphic and tec tonic data

Try ing to re con struct palaeogeographic po si tion of a tec tonic or sed i men taryunit in pri mary sed i men tary ba sin in so tec toni cally com pli cated zone as thePieniny Klippen Belt, we need – first of all – a de tailed geo log i cal map, no less that1:10,000 scale, sup ported by nu mer ous care fully elab o rated field sec tions. A re -view given be low re fers to the three north ern units of the Pieniny Klippen Belt inPo land: the Czorsztyn-, the Czertezik-, and the Niedzica suc ces sions/tec tonic units.

Type area of the Czertezik Suc ces sion. When the Czertezik Suc ces sion wasdis tin guished by the pres ent au thor (Birkenmajer, 1959b) in the Pieniny Na tionalPark, a re vi sion of the geo log i cal map of this area, 1:10,000 scale, pre pared ear lierby Horwitz (1963), was in prog ress, in or der to solve palaeogeographic po si tion ofthis new suc ces sion with re spect to the Niedzica- and Branisko ones, the lat ter al -ready dis tin guished and mapped to 1:10,000 scale (Birkenmajer, 1953, 1958a,1960a, b, 1963b). Un for tu nately, in the area around the Czertezik mount and thePieniñski Potok stream – the type area of the Czertezik Suc ces sion, be sides theCzertezik Unit, there oc cur only the Branisko and Pieniny nappes thrust over it,while both the Niedzica and the Czorsztyn suc ces sions are miss ing.

Area be tween the Szopczañski W¹wóz and the Straszny Potok dis lo ca tionzones. Be tween the Szopczañski (Sobczañski) W¹wóz Dis lo ca tion Zone and theStraszny Potok Dis lo ca tion Zone (area III), the Czertezik Unit oc curs as smallklippes within an ex ten sive field of the transgressive Palaeogene strata (III.A. andIII.B.). In the south ern part only, they are tec toni cally as so ci ated with the Czorsztyn Unit klippes (III.C.). Un for tu nately, no di rect con tacts be tween these two dif fer enttec tonic units are avail able for study.

Area of tec tonic win dows near Niedzica Cas tle and Sromowce Wy¿ne.West wards from the Straszny Potok Dis lo ca tion Zone, south of Ha³uszowa, thereoc cur three tec tonic scales of the Niedzica Nappe (the Ha³uszowskie Ska³ki; theHa³uszowska Sajba – the larg est one; and the Sromowska Sajba), thrust over Cre ta -ceous rocks of the Czorsztyn Unit, ex posed in a large tec tonic win dow from be lowthe Branisko Nappe. No Czertezik Suc ces sion rocks oc cur there.

Still fur ther west, in the Niedzica Cas tle-Czubata Ska³a Tec tonic Win dow(IV.B.), there oc cur small klippes of the Niedzica Suc ces sion, rest ing di rectly uponUp per Cre ta ceous rocks of the Czorsztyn Unit. The lat ter forms the win dow’s an ti -cli nal core, and is capped by the overthrust Branisko Nappe (Birkenmajer, 1960a,1963b, 1998a, 1999). Tec tonic scales of the Niedzica Unit are, more over, thrustover the Maastrichtian Jarmuta For ma tion (Birkenmajer, 1998a, 1999). The spa tialre la tion ships in di cate that the Niedzica Suc ces sion was orig i nally lo cated be tweenthe Czorsztyn and the Branisko depositional zones, but again give no clues as tomu tual re la tion ships of the Czertezik and the Niedzica ones.

Pol ish Spisz. The Niedzica Suc ces sion con tin ues in the Pol ish Spisz area. Itswell known klippes oc cur at the Niedzica vil lage, in the Falsztyñski Stream val ley,

40 K. BIRKENMAJER

and even near Dursztyn (see Birkenmajer, 1953, 1954, 1958a, 1959a, 1960a, b,1963b, 1979). There are no traces of the Czertezik Suc ces sion in this area.

Lit tle Pieniny Range (Jaworki area). Strati graphic and tec tonic stud ies, alongwith de tailed geo log i cal map ping to 1:10,000 scale, per formed in the area ofJaworki be tween Homole Gorge in the north, and the Pol ish/Slo vak fron tier in thesouth (Birkenmajer, 1970), did also fail to solve pre vi ous palaeogeographic re la -tion ship be tween the Czorsztyn, the Czertezik and the Niedzica suc ces sions. Thesethree units are well ex posed there (Birkenmajer, 1970, pls I, III–VI):

(i) The Czorsztyn Unit is overthrust by sev eral north-vergent folds and tec tonicscales of the Niedzica Nappe and by the Branisko Nappe;

(ii) The Niedzica Nappe is overthrust di rectly by the Branisko Nappe;(iii) The Czertezik Unit is prob a bly “float ing” upon the Czorsztyn Unit (un for -

tu nately, the lat ter is not ex posed there be low the Czertezik Unit), and is overthrustby the Branisko Nappe.

Sedimentological data

In or der to solve mu tual palaeogeographic po si tions of the Czorsztyn-, Czer-tezik- and the Niedzica suc ces sions, the de vel op ment and thick nesses of their Mid -dle Ju ras sic crinoidal lime stones, the Smolegowa and the Krupianka lime stone for -ma tions (see Birkenmajer, 1977), were taken into con sid er ation. The crinoidallime stones in the Homole Gorge area (Birkenmajer (1970, Pl. II) are thick est in theCzorsztyn Suc ces sion (> 114 m). They thin out in the more south ern Czertezik Suc -ces sion (down to 60–80 m), and be come thin nest in the south ern most Niedzica Suc -ces sion (7 m). The thick ness de crease of the crinoidal lime stones in a south ern di -rec tion, i.e. off shore from the Czorsztyn Ridge, cor re lates with de crease in size ofre cy cled Tri as sic car bon ate and si li ceous clasts in these lime stones, the coars estones known from the Czorsztyn Suc ces sion, and the fin est ones – from the Niedzica Suc ces sion (cf. Birkenmajer, 1958a, 1963a).

These crinoidal lime stones rep re sent sub ma rine fans (sed i ment wedges) whichcon sist of crinoidal os si cles, re de pos ited post mor tem from a pri mary hab i tat off -shore Czorsztyn Ridge by bot tom cur rents and grav ity sed i ment creep (Birken-majer, 1963a; G³uchowski, 1986, 1987). Ra dii of these crinoidal sub ma rine fanswere prob a bly in ex cess of 45 km. This as sump tion is based on the following data:

(1) A min i mum dis tance of 30 km has been cal cu lated for the Czorsztyn Suc ces -sion width on un fold ing tec tonic struc tures in the area of Czorsztyn (see Birken-majer, 1963a, pp. 229–230, 337);

(2) No less than 5 km should be added for a pri mary width of the Czertezik Suc -ces sion on un fold ing the area be tween the Czertezik-Zamkowa Góra (in the south)and the Ociemne-Sutrówka-Bojków Groñ (in the north) tec tonic win dows (see Fig.17).

Dis cus sion

Ksi¹¿kiewicz (1972, pp. 90–92; but not Ksi¹¿kiewicz, 1977), fol lowed byGolonka and R¹czkowski (1984, p. 50), by Kulka et al. (1991, p. 59) and, re cently,


by Wierzbowski et al. (2004) and Krobicki and Wierzbowski (2004), tried to re -verse the or der of palaeogeographic zones in the north ern part of the PieninyKlippen ba sin, as fol lows (north to south): (i) the Czorsztyn Suc ces sion; (ii) theNiedzica Suc ces sion, and (iii) the Czertezik Suc ces sion. None of the above au thorsper formed, how ever, any de tailed geo log i cal map ping in the Pieniny Klippen Beltto sup port their views.

Wierzbowski et al. (2004) fragmentarily de scribed some field ex po sures at thebot tom of the Potok Pieniñski stream. How ever, they did not rec og nize transversalfaults which densely cut the Czertezik Suc ces sion, and of ten tec toni cally di videpar tic u lar lithostratigraphic units there (e.g., in their “Klippe B” – see Fig. 10A).Also, they did not even try to climb up the Wielka Pustelnica klippe: thus, they were un able to find the Czorsztyn Lime stone For ma tion which oc curs in its proper strati -graphic po si tion be tween the radiolarites (= the Czajakowa Radiolarite Fm.) andthe cherty lime stone (= the Pieniny Lime stone Fm.), and is known there since 1959(see Birkenmajer, 1959b, 1977).

As al ready proven (see pre vi ous chap ters), their sup po si tion about the oc cur -rence of the ‘Niedzica Lime stone For ma tion’ (Up per Bajocian–Callovian) in theCzertezik Suc ces sion both in the Pieniny Na tional Park, and in the Lit tle PieninyRange, has not been sup ported by age-di ag nos tic fos sils, and by a de tailed field sur -vey, geo log i cal mapping inclusively.

More over, at tri bu tion by Wierzbowski et al. (op. cit.) of some klippes in East ern Slovakia (Litmanová and Milpoš quar ries) to the Czertezik Suc ces sion was cer -tainly in cor rect: these klippes ev i dently be long to the Niedzica Suc ces sion in stead,show ing, i.a., a very small thick ness of the crinoidal lime stones (the Smolegowaand the Krupianka lime stone for ma tions) and the pres ence of typ i cally de vel oped,very thin, fossiliferous ammonitico rosso Niedzica Lime stone For ma tion (seeprevious chapters).

Mod i fied palaeogeographic model

Dur ing Mid dle Ju ras sic through Lower Cre ta ceous time span, three palaeogeo-graphic zones were dis tin guish able in the Czorsztyn Suc ces sion:

(i) A south ern zone, ex posed in suc ces sive tec tonic win dows be tween Niedzicain the south, and Czorsztyn in the north;

(ii) A more north ern zone ex posed in the area of Krempachy and Nowa Bia³a,and

(iii) A north ern most zone, in the area be tween Nowy Targ and RogoŸnik(Birkenmajer, 1963a, pl. I. fig. 2; tab. 4).

It has been found that fa cies di ver si fi ca tion, fre quency of sed i men tary breaks,and ev i dences of syn-sed i men tary tec ton ics, all be came better and better ex pressedin a north ward di rec tion, ob vi ously on ap proach ing the Czorsztyn Ridge (op. cit.) .

Still more north ern de vel op ments of the Czorsztyn suc ces sion might be thosere cently de scribed from the Pieniny Klippen Belt of West Slovakia and Transcarpa- thian Ukraine, which show the pres ence of stromatactis mud-mounds, and large-

42 K. BIRKENMAJER

scale cross-bed ding in some Ju ras sic lime stones (Mišík et al., 1994; Aubrecht et al., 2000a). In the Pol ish sec tor of the Klippen Belt, large-scale cross-bed ding is sel -dom rec og niz able in the white crinoidal lime stone (the Smolegowa Lime stone For -ma tion), e.g., in the Czorsztyn Cas tle klippes (see Krobicki & Golonka, 2006, fig.A16).

The pres ent mod i fi ca tion of palaeogeographic model of the Bajocian stage inthe Klippen Ba sin (Fig. 20), takes into ac count the fol low ing data:

(1) The Czorsztyn Suc ces sion/Unit is the most sta ble, north ern most struc turalel e ment of the Pieniny Klippen Belt Ju ras sic–Cre ta ceous ba sin, trace able prac ti -cally along its whole length;

(2) The Czertezik Suc ces sion oc curs dis con tin u ously along the Pieniny Klippen Belt. It is best de vel oped in cen tral part of the Belt, in the Na tional Park of thePieniny Mts, and along the Pol ish-Slo vak fron tier in the Lit tle Pieniny Range. Itsoc cur rence in East ern Slovakia (with the ex cep tion of some klippes at Litmanová)is still ques tion able. In West Slovakia (Krivanská Mala Fatra), its oc cur rence hasbeen re ported by Haško and Polák (1978). In Transcarpathian Ukraine, someklippes re cently at trib uted to the Czorsztyn Suc ces sion (see Krobicki et al., 2003;Lewandowski et al., 2002, 2003a, b, 2005), but show ing the pres ence of apoorly-de vel oped Up per Ju ras sic radiolaria-bear ing ho ri zon, might be long to a va -ri ety of the Czertezik Suc ces sion closest to the Czorsztyn Succession;


Fig. 20. A model of sedimentary zones in the Klippen Basin, Middle Bajocian–Early Bathonianstage. CR – emergent Czorsztyn Ridge. Submarine crinoid limestone fans (dotted), areas ofdeposition of the Smolegowa Limestone Fm. (white crinoid limestone), the Krupianka LimestoneFm. (red crinoid limestone), and the Flaki Limestone Fm. (f – crinoid-cherty limestone).Sedimentary/stratigraphic successions: C – Czorsztyn (continental platform, inner part); Ct –Czertezik (continental platform, outer part); N – Niedzica (platform, outer part and slope: ammonitico rosso facies); B – Branisko (basinal trough: Fleckenkalk facies). Other signatures: cm – crinoid“meadows”; cp – coastal plain; sl – sea level

(3) In a va ri ety of the Czertezik Suc ces sion in Po land (Pieniny Range, ar easIII.A. & III.B. – see above), the Up per Ju ras sic (Oxfordian) radiolarite ho ri zon(Czajakowa Radiolarite Fm.) wedges out, and the Tithonian–Neocomian chertylime stone (Pieniny Lime stone Fm.) is much re duced in thick ness, whilst the Mid dle Ju ras sic crinoidal lime stones (Smolegowa and Krupianka lime stone fms) re maincon sid er ably thick. Thus, this va ri ety be comes closer in its de vel op ment to theCzorsztyn Suc ces sion. It is pos si bly tec toni cally as so ci ated with the CzorsztynSuc ces sion klippes, and might rep re sent tec tonic slabs (“nappe”) thrust directlyover the latter;

(4) In a south ern va ri ety of the Czorsztyn Suc ces sion (Miêdzyhombark –Birkenmajer, 1963a), white crinoidal lime stone of the Smolegowa Lime stone For -ma tion is re placed by grey crinoidal lime stone – a de vel op ment typ i cal of theCzertezik Suc ces sion and of a va ri ety of the Branisko Suc ces sion, but un knownfrom the Niedzica Succession;

(5) Ap pear ance of Mid dle Ju ras sic crinoidal-cherty lime stone (= Flaki Lime -stone Fm.) in the south ern most de vel op ment of the Czertezik Suc ces sion in the type area (Pieniñski Potok stream), makes it close to a north ern type of the Branisko Suc -ces sion, as known from the Flaki Range. This sug gests a pri mary lack of theNiedzica Suc ces sion in be tween these two successions;

(6) Ar eal dis tri bu tion of the Niedzica Suc ces sion is even more dis con tin u ousthan that of the Czertezik Suc ces sion. The Niedzica Suc ces sion oc curs mainly incen tral sec tor of the Pieniny Klippen Belt (the Spisz Range, the Czorsztyn Range,Jaworki in the Lit tle Pieniny Range), but cer tainly con tin ues in East Slovakia(Litmanová, Milpoš), mainly in as so ci a tion with the Czorsztyn and Czertezik suc -ces sions. Its char ac ter is tic fea tures are: very thin Mid dle Ju ras sic crinoidal lime -stones (Smolegowa and Krupianka limestone fms); well de vel oped, but thin, redMid dle Ju ras sic fossiliferous nod u lar lime stone (Niedzica Lime stone Fm.); wellde vel oped Oxfordian radiolarite zone (Czajakowa Radiolarite Fm.); and well de -vel oped Kimmeridgian (resp. Oxfordian– Kimmeridgian) red nod u lar lime stone(Czorsztyn Lime stone Fm.); poorly de vel oped cherty/pseudo-cherty Neocomianlime stone (Pieniny Lime stone Fm.). White Calpionella lime stone (Dursztyn Fm.)lo cally ap pears at the base of the latter;

(7) In West Slovakia, no ex act equiv a lents of the Niedzica Suc ces sion have been found so-far, how ever some de vel op ments (e.g., the Podbiel Suc ces sion) re sem blethe Niedzica one.

Con clu sions

(1) Dur ing the Bajocian, the Czertezik Suc ces sion oc cu pied outer/mar ginal,deeper parts of crinoidal sub ma rine fans. The ma jor depocentres of these sub ma rine fans were lo cated fur ther north within the Czorsztyn Suc ces sion sed i men taryrealm;

(2) The Niedzica Suc ces sion oc cu pied rather deep, nar row troughs lo catedalong outer mar gins of the Bajocian crinoidal fans, par al lel to the ba sin axis, andtransversal to it – be tween the fans, far thest from the clastic source. This was the

44 K. BIRKENMAJER

rea son that its Mid dle Ju ras sic crinoidal lime stones are very thin, and their land-de -rived clastic ad mix ture very fine.

(3) Along the Klippen Ba sin, the Niedzica Suc ces sion might thus con tact di -rectly the ar eas of de po si tion of the Branisko-, the Czertezik- or even the Czorsztynsuc ces sions.

Ac knowl edge ments

I thank my wife, Doc. Dr Franciszka Szymakowska-Birkenmajer who helped me with prep a ra tion of fig ures. Prof. Jerzy Lefeld most kindly re viewed this pa per.

REF ER ENCES

Alexandrowicz, S. W., 1966. Stratygrafia œrodkowej i górnej kredy w polskiej czêœci pieniñskiegopasa ska³kowego (Stra tig ra phy of the Mid dle and Up per Cre ta ceous in the Pol ish part of thePieniny Klippen Belt). Zeszyty Naukowe Akademii Górniczo-Hutniczej, 157 (Rozprawy), 78: 142pp.

Aubrecht, R., 1997. In di ca tions of the Mid dle Ju ras sic emer gence in the Czorsztyn Unit (PieninyKlippen Belt, West ern Carpathians). Geologica Carpathica, 48 (2): 71–84.

Aubrecht, R., Krobicki, M., Matyja, B. A., Wierzbowski, A. & Schlögl, J., 2002a. Ju ras sic stroma-tactis mud-mounds in the Pieniny Klippen Belt (West ern Carpathians) – pe trog ra phy andstra tig ra phy. In: Bucur, I. I. & Filipescu, S. (eds), Re search ad vances in cal car e ous al gae andmi cro bial car bon ates. Cluj Uni ver sity Press: 1–16.

Aubrecht, R., Krobicki, M., Kruglov, S., Matyja, B. A. & Wierzbowski, A., 2002b. Strati graphic andpalaeogeographic sig nif i cance of pe lagic microfacies in the Mid dle to Up per Ju ras sic of thePieniny Klippen Belt, Carpathians. VI In ter na tional Sym po sium on the Ju ras sic Sys tem (Palermo, 12-13 Sept., 2002): 4–5.

B¹k. K., 1998. Foraminiferal biostratigraphy of the Up per Cre ta ceous red deep wa ter de pos its in thePieniny Klippen Belt, Carpathians, Po land. Studia Geologica Polonica, 111: 7–92.

Birkenmajer, K., 1952. W sprawie morskiego miocenu na Podhalu (La ques tion du MiocÀne marin dePodhale, Karpates Centrales). Rocznik Polskiego Towarzystwa Geologicznego (Annales de laSociété Géologique de Pologne), 21 (2) 235–278.

Birkenmajer, K., 1953. Pre lim i nary re vi sion of the stra tig ra phy of the Pieniny Klippen belt se ries inPo land. Bul le tin de l’Académie Po lo naise des Sci ences, III Cl., 1 (6): 271–274.

Birkenmajer, K., 1954. Sprawozdanie z badañ geologicznych wykonanych w pieniñskim pasieska³kowym w latach 1950–1951 (Geo log i cal re searches in the Pieniny Klippen Belt, Cen tralCarpathians). Instytut Geologiczny, Biuletyn, 86: 81–115.

Birkenmajer, K., 1958a, Przewodnik geologiczny po pieniñskim pasie ska³kowym (Pieniny KlippenBelt, Geo log i cal Guide – in Pol ish). I (135 pp.), II (74 pp.), III (88 pp.), IV (55 pp.). WydawnictwaGeologiczne, Warszawa.

Birkenmajer, K., 1958b. Sub ma rine ero sional breaks and Late Ju ras sic synorogenic move ments in the Pieniny Klippen-Belt geosyncline. Bul le tin de l’Académie Po lo naise des Sci ences, Sér. sci.chim., géol., géogr., 6 (8): 551–558.

Birkenmajer, K., 1959a. Przekroje geologiczne przez Polskê – Pieniny (Geo log i cal cross-sec tions ofPo land: Pieniny Mts – in Pol ish): 20 pp. Wydawnictwa Geologiczne, Warszawa.

Birkenmajer, K., 1959b. Seria czertezicka – nowa seria ska³kowa Pienin (A new Klippen Se ries in thePieniny Mts, Carpathians – the Czertezik Se ries). Acta Geologica Polonica, 9 (4): 499–515.

Birkenmajer, K., 1960a. Mapa geologiczna pieniñskiego pasa ska³kowego, 1:10.000, ark. Niedzica(Geo log i cal map of the Pieniny Klippen Belt, 1:10,000 scale, sheet Niedzica – ex pla na tions inPol ish). Instytut Geologiczny, Warszawa.

Birkenmajer, K., 1960b. Mapa geologiczna pieniñskiego pasa ska³kowego, 1:10.000, ark. Dursztyn


(Geo log i cal map of the Pieniny Klippen Belt, 1:10,000 scale, sheet Dursztyn – ex pla na tions inPol ish). Instytut Geologiczny, Warszawa.

Birkenmajer, K., 1963a. Stratygrafia i paleogeografia serii czorsztyñskiej pieniñskiego pasa ska³ko-wego Polski (Stra tig ra phy and palaeo ge ogra phy of the Czorsztyn Se ries, Pieniny Klippen Belt,Carpathians). Studia Geologica Polonica, 9: 380 pp.

Birkenmajer, K., 1963b. Mapa geologiczna pieniñskiego pasa ska³kowego, 1:10.000, ark. Czorsztyn(Geo log i cal map of the Pieniny Klippen Belt 1:10,000 scale, sheet Czorsztyn – ex pla na tions inPol ish). Instytut Geologiczny, Warszawa.

Birkenmajer, K., 1965. Zarys budowy geologicznej pieniñskiego pasa ska³kowego Polski (Out linesof ge ol ogy of the Pieniny Klippen Belt in Po land). Rocznik Polskiego Towarzystwa Geolo-gicznego (Annales de la Société Géologique de Pologne), 35 (3): 327–356, 401–407.

Birkenmajer, K., 1970. Przedeoceñskie struktury fa³dowe w pieniñskim pasie ska³kowym Polski(Pre-Eocene fold struc tures in the Pieniny Klippen Belt, Carpathians). Studia Geologica Polo-nica, 31: 77 pp.

Birkenmajer, K., 1973a. Jura, obszary wystêpowania i stratygrafia: pieniñski pas ska³kowy. In:Budowa Geologiczna Polski. 1. Stratygrafia, 2. Mezozoik. Wydawnictwa Geologiczne & Instytut Geologiczny, Warszawa: 408–429.

Birkenmajer, K., 1973b. Kreda, obszary wystêpowania i stratygrafia: pieniñski pas ska³kowy. In:Budowa Geologiczna Polski. 1. Stratygrafia, 2. Mezozoik. Wydawnictwa Geologiczne & Instytut Geologiczny, Warszawa: 669–690.

Birkenmajer, K., 1975. Tec tonic con trol of sed i men ta tion at the Ju ras sic–Cre ta ceous bound ary in thePieniny Klippen Belt, Carpathians. Col lo quium sur la limite Jurassique–Crétacé (Lyon-Neu-châtel). Mémoirs du BRGM (Paris): 394–399.

Birkenmajer, K., 1976a. The Ju ras sic. The Carpathian Ju ras sic: the Pieniny Klippen Belt. In: Ge ol ogy of Po land, 1 (2: Me so zoic). Instytut Geologiczny & Wydawnictwa Geologiczne, Warszawa:421–443.

Birkenmajer, K., 1976b. The Cre ta ceous. The Carpathians: the Pieniny Klippen Belt. In: Ge ol ogy ofPo land, 1 (2: Mezozoic). Instytut Geologiczny & Wydawnictwa Geologiczne, Warszawa:680–702.

Birkenmajer, K., 1977. Ju ras sic and Cre ta ceous lithostratigraphic units of the Pieniny Klippen Belt,Carpathians, Po land. Studia Geologica Polonica, 45: 159 pp.

Birkenmajer, K., 1979. Przewodnik geologiczny po pieniñskim pasie ska³kowym (Pieniny KlippenBelt of Po land, Geo log i cal Guide – in Pol ish). Wydawnictwa Geologiczne, Warszawa: 236 pp.

Birkenmajer, K., 1985. Main geotraverse of the Pol ish Carpathians (Cra cow-Zakopane), Gen eralin tro duc tion. Carpatho-Bal kan Geo log i cal As so ci a tion, XIII Con gress (Cra cow, 5-10 IX 1985).Guide to Ex cur sion, 2: 5–13.

Birkenmajer, K., 1986a. Stages of struc tural evo lu tion of the Pieniny Klippen Belt, Carpathians.Studia Geologica Polonica, 88: 7–32.

Birkenmajer, K., 1986b. Zarys ewolucji geologicznej pieniñskiego pasa ska³kowego (Out line ofgeo log i cal evo lu tion of the Pieniny Klippen Belt, Carpathians). Przegl¹d Geologiczny, 34 (2):219–226.

Birkenmajer, K., 1987. Me so zoic and Ce no zoic tec tonic struc tures of the Pieniny Klippen Belt,Carpathians. In: Mahel’, M. (ed.), Strukturny vyvoj karpatsko-balkanského orogenného pásma(Bratislava): 74–75.

Birkenmajer, K., 1998a. Tektonika wzgórza zamkowego w Niedzicy, pieniñski pas ska³owy (Tec -ton ics of the Niedzica Cas tle hill, Pieniny Klippen Belt, Pol ish Carpathians). Studia GeologicaPolonica, 111: 155–179.

Birkenmajer, K., 1998b. Evo lu tion trends in basinal de pos its of Ju ras sic–Early Cre ta ceous age.Ex am ples from the West ern Carpathians and the North ern Cal car e ous Alps. Acta GeologicaHungarica (Bu da pest), 41 (3) 283–311.

Birkenmajer, K., 1999. Stages of struc tural evo lu tion of the Niedzica Cas tle tec tonic win dow, Pieniny Klippen Belt, Carpathians, Po land. Studia Geologica Polonica, 115: 117–130.

Birkenmajer, K. & Dudziak, J., 1988. Age of Palaeogene flysch in the Pieniny Klippen Belt,

46 K. BIRKENMAJER

Carpathians, Po land, based on cal car e ous nannoplankton. Bul le tin of the Pol ish Acad emy ofSci ences: Earth Sci., 34 (1) 15–24.

Birkenmajer, K. & Gedl. P., 2004. Dinocyst ages of some Ju ras sic strata, Grajcarek Unit at SztolniaCreek, Pieniny Klippen Belt (Po land). Studia Geologica Polonica, 123: 245–277.

Birkenmajer, K. & G¹siorowski, S. M., 1960. Stra tig ra phy of the Malm of the Niedzica and BraniskoSe ries (Pieniny Klippen Belt, Carpathians), based on Aptychi. Bul le tin de l’Académie Po lo naisedes Sci ences, Sér. sci. géol., géogr., 8 (2): 137–143.

Birkenmajer, K. & G¹siorowski, S. M., 1961. Sed i men tary char ac ter of radiolarites in the PieninyKlippen Belt, Carpathians. Bul le tin de l’Académie Po lo naise des Sci ences, Sér. sci. géol., géogr.,9 (3); 173–180.

Birkenmajer, K. & G¹siorowski, S. M., 1963. Ruchy neokimeryjskie w polskich Karpatach Zachod-nich (Neo-Cim mer ian move ments in the Pol ish West ern Carpathians). Przegl¹d Geologiczny, 7(124): 314–318.

Birkenmajer, K. & Jednorowska, A., 1987. Late Cre ta ceous foraminiferal biostratigraphy of thePieniny Klippen Belt (Carpathians, Po land). Studia Geologica Polonica, 92: 7–28.

Birkenmajer, K. & Myczyñski, R., 1984. Fauna i wiek jurajskich wapieni bulastych okolic Niedzicy iJaworek, pieniñski pas ska³kowy (Fauna and age of Ju ras sic nod u lar lime stones near Niedzica and Jaworki, Pieniny Klippen Belt, Carpathians, Po land). Studia Geologica Polonica, 83: 7–24.

Birkenmajer, K. & Myczyñski, R., 1994. Pliensbachian (Early Ju ras sic) fauna from the PieninyKlippen Belt, Carpathians (Po land): its strati graphic and palaeogeographic po si tion. Bul le tin ofthe Pol ish Acad emy of Sci ences: Earth Sci., 42 (4): 223–245.

Birkenmajer, K. & Oszczypko, N., 1989. Cre ta ceous and Palaeogene lithostratigraphic units of theMagura Nappe, Krynica Sub unit, Carpathians. Annales Societatis Geologorum Poloniae, 59:117–253.

Birkenmajer, K. & Pécskay, Z., 1999. K-Ar dat ing of the Mio cene an de site in tru sions, Pieniny Mts,West Carpathians. Bul le tin of the Pol ish Acad emy of Sci ences: Earth Sci., 47 (2-3): 155–169.

Birkenmajer, K. & Pécskay, Z., 2000. K-Ar dat ing of the Mio cene an de site in tru sions, Pieniny Mts,West Carpathians, Po land. A sup ple ment. Studia Geologica Polonica, 117: 7–25.

Birkenmajer, K. & Turnau, E., 1962. Car bon if er ous micro spores as sec ond ary de posit in the Aalenian Flysch of the Pieniny Klippen Belt (Carpathians). Bul le tin de l’Académie Po lo naise des Sci ences, Sér. sci. géol., géogr., 10 (2): 99–103.

Birkenmajer, K. & Tyszka, J., 1996. Palaeoenvironment and age of the Krzonowe For ma tion (ma rineToarcian–Aalenian), Pieniny Klippen Belt, Carpathians. Studia Geologica Polonica, 109: 7–42.

Birkenmajer, K. & Widz, D., 1995. Biostratigraphy of Up per Ju ras sic radiolarites in the PieninyKlippen Belt, Carpathians. In: Baumgartner, P. O., et al. (eds), Mid dle Ju ras sic to LowerCre ta ceous radiolaria of Tethys: oc cur rences, sys tem at ics, biochronology. Mémoires de Géo-logie, Lausanne, 23: 889–896.

Birkenmajer, K. & Znosko, J., 1955. Przyczynek do stratygrafii doggeru i malmu pieniñskiego pasaska³kowego (Con tri bu tion to the stra tig ra phy of the Dogger and Malm in the Pieniny Klippen-belt, Cen tral Carpathians). Rocznik Polskiego Towarzystwa Geologicznego (Annales de laSociété Géologique de Pologne), 23: 3–36.

Birkenmajer, K., G¹siorowski, S. M. & Wieser, T., 1960. Frag ments of ex otic rocks in the pe lagicde pos its of the Bathonian of the Niedzica Se ries (Pieniny Klippen Belt, Carpathians). RocznikPolskiego Towarzystwa Geologicznego (Annales de la Société Géologique de Pologne), 30 (1):29–57.

Birkenmajer, K., Gedl, P., Myczyñski, R. & Tyszka, J., 2006. “Cre ta ceous black flysch” in thePieniny Klippen Belt, West Carpathians: a case of geo log i cal mis in ter pre ta tion. Cre ta ceousReseach (in press).

Birkenmajer, K., Kozur, H. & Mock, R., 1990. Ex otic Tri as sic pe lagic lime stones from the PieninyKlippen Belt in Po land: a fur ther ev i dence for Early Me so zoic rift ing in West Carpathians.Annales Societatis Geologorum Poloniae, 60: 3–44.

Dragastan, O. & Mišík, M., 2001. Non-ma rine Lower Cre ta ceous al gae and cyanobacteria from theCzorsztyn Unit, West ern Carpathians. Geologica Carpathica, 42 (4): 229–237.


G¹siorowski, S. M., 1962. Aptychi from the Dogger, Malm and Neocomian in the West ernCarpathians, and their strati graphic value. Studia Geologica Polonica, 10: 151 pp.

G³uchowski, E. A., 1986. Liliowce (Crinoidea, Articulata) jury i dolnej kredy pieniñskiego pasaska³kowego Polski (Ju ras sic and Lower Cre ta ceous ar tic u late cri noids of the Pieniny KlippenBelt, Carpathians, in Po land). Przegl¹d Geologiczny, 6: 304–309.

G³uchowski, E. A., 1987. Ju ras sic and Early Cre ta ceous Ar tic u late Crinoidea from the PieninyKlippen Belt and the Tatra Mts, Po land. Studia Geologica Polonica, 94: 100 pp.

G³uchowski, E., Krawczyk, A., Myszkowska, J. & S³omka, T., 1986. Litofacje i fauna wapieniakrynoidowego bajosu jednostki czorsztyñskiej ko³o Dursztyna, pieniñski pas ska³kowy (Litho-facies and fauna of Bajocian cri noid lime stone near Dursztyn, Czorsztyn Suc ces sion, PieninyKlippen Belt, Carpathians). Studia Geologica Polonica, 88: 143–155.

Golonka, J. & R¹czkowski, 1984. Objaœnienia do Szczegó³owej Mapy Geologicznej Polski, ArkuszPiwniczna, 1:5.000. Wydawnictwa Geologiczne, Warszawa: 85 pp.

Haško, J. & Polák, 1978. Geologická Mapa Kysuckich Vrchov a Krivánskej Malej Fatry (Geo log i calMap of the Kysucké Vrchy and Krivánska Mala Fatra Mts.). Geologicky ¤stav Dionyza Štóra,Bratislava.

Horwitz, L., 1922. Sprawozdanie z badañ geologicznych wykonanych w lecie 1921 r. w pasie Ska³ekPieniñskich (Compte-rendu des ex plo ra tions géologiques éffectuées en 1921 dans les Piénines).Posiedzenia Naukowe Pañstwowego Instututu Geologicznego, 3: 18–21.

Horwitz, L., 1963. Budowa geologiczna Pienin: wydanie poœmiertne – przygotowa³ do druku iopatrzy³ przypisami K. Birkenmajer (Ge ol ogy of the Pieniny Mts – post hu mous pa per. Com -ments by K. Birkenmajer). Prace Instytutu Geologicznego, 38: 152 pp.

Horwitz, L. & Doktorowicz-Hrebnicki, S., 1932. O wêglu w Szczawnicy i okolicach (Sur la houille ́Szczawnica et aux en vi rons). Posiedzenia Naukowe Pañstwowego Instytutu Geologicznego(Warszawa), 33: 65–68.

Hud son, W., Hart, M. B., Sidorczuk, M. & Wierzbowski, A., 2004. Ju ras sic plank tonic foraminiferafrom the Pieniny Klippen Belt and their tax o nomic and phylo gen etic im por tance (Carpathians,south ern Po land). Tomy Jurajskie, 3: 1–10.

Jefferies, R. P. S. & Minton, P., 1965. The mode of life of two Ju ras sic spe cies of Posidonia(Bivalvia). Palae on tol ogy, 8 (1): 156–185.

Krawczyk, A. & S³omka, T., 1986. Wykszta³cenie i sedymentacja formacji szlachtowskiej (jura) nawschód od Szczawnicy, jednostka Grajcarka, pieniñski pas ska³kowy (De vel op ment and sed i -men ta tion of the Szlachtowa For ma tion, Ju ras sic flysch, east of Szczawnica: Grajcarek Unit,Pieniny Klippen Belt, Carpathians). Studia Geologica Polonica, 88: 129–134.

Krawczyk, A. & S³omka, T., 1987. Egzotyki z formacji szlachtowskiej pieniñskiego pasa ska³kowego (Ex otic rocks from the Szlachtowa For ma tion, Ju ras sic flysch) of the Pieniny Klippen Belt,Carpathians). Studia Geologica Polonica, 92: 69–74.

Krawczyk, A., Muszyñski, M. & S³omka, T., 1987. Okruchy ska³ w psamitach formacji szlach-towskiej pieniñskiego pasa ska³kowego (Ex otic rock frag ments from psam mit ic rocks of theSzlachtowa For ma tion, Ju ras sic flysch, of the Pieniny Klippen Belt, Carpathians). StudiaGeologica Polonica, 92: 75–86.

Krobicki, M., 2002. Bajocian phos phatic event in the Pieniny Klippen Belt, Pol ish and SlovakianCarpathians. VI In ter na tional Sym po sium on the Ju ras sic Sys tem (Palermo, 12-22 Sept., 2002):103.

Krobicki, M., 2003. Œrodkowojurajska (bajos) fosfatyzacja w pieniñskim pasie ska³kowym. TomyJurajskie, 1: 116–117.

Krobicki, M. & Golonka, J., 2006. Field trip A – From Tethyan to plat form fa cies. In: Wierzbowski,A., Aubrecht, R., Golonka, J., Gutowski, J., Krobicki, M., Matyja, B. A., Pieñkowski, G. &Uchman, A., Ju ras sic of Po land and ad ja cent Slovakian Carpathians (Field-trip Guide book ofthe 7th In ter na tional Con gress on the Ju ras sic Sys tem, Po land, Kraków, Sept. 6-18, 2006). Pol ishGeo log i cal In sti tute, Warszawa: 11–78.

Krobicki, M. & Uchman, A., 2003. Trace fos sil Curvolithus from the Mid dle Ju ras sic crinoidallime stones of the Pieniny Klippen Belt (Carpathians, Po land). Geologica Carpathica, 54 (3):

48 K. BIRKENMAJER

175–180.Krobicki, M. & Wierzbowski, A., 2004. Pozycja stratygraficzna i paleogeograficzne znaczenie

bajoskich wapieni krynoidowych w ewolucji pieniñskiego pasa ska³kowego (Strati graphicpo si tion of the Bajocian crinoidal lime stones and their sig nif i cance in evo lu tion of the PieninyKlippen Belt). Tomy Jurajskie (Warszawa), 2: 69–82.

Krobicki, M., Kruglov, S. S., Matyja, B. A., Wierzbowski, A., Aubrecht, R., Bubniak, A. & Bubniak,I., 2003. Re la tion be tween Ju ras sic klippen suc ces sions in the Pol ish and Ukrai nian parts of thePieniny Klippen Belt. Mineralia Slovaca, 35: 56–58.

Ksi¹¿kiewicz, M., 1972. Budowa Geologiczna Polski. IV (tektonika), 3 (Karpaty). Instytut Geolo-giczny & Wydawnictwa Geologiczne: 228 pp.

Ksi¹¿kiewicz, M., 1977. The tec ton ics of the Carpathians. In: Ge ol ogy of Po land, IV (PieninyKlippes Belt: pp. 519–552). Geo log i cal In sti tute and Pub lish ing House Wydawnictwa Geolo-giczne: 476–669.

Kulka, A., R¹czkowski, W., ¯ytko, K. & Paul, Z., 1991. Objaœnienia do Szczegó³owej MapyGeologicznej Polski w skali 1:50.000. Arkusz Szczawnica-Kroœcienko (1050). WydawnictwaGeologiczne, Warszawa: 93 pp.

Lewandowski, M., Krobicki, M., Matyja, B. M. & Wierzbowski, A., 2002. Mid-Ju ras sic palaeo ge o-gra phy of the Pieniny Klippen Ba sin – palaeomagnetic ap proach. VI In ter na tional Sym po sium onthe Ju ras sic Sys tem (Palermo, 12-22 Sept. 2002): 106–107.

Lewandowski, M., Krobicki, M., Matyja, B. A. & Wierzbowski, A., 2003. Paleogeografia pie-niñskiego basenu ska³kowego: œrodkowojurajsko-wczesnokredowa ewolucja na podstawie ba-dañ paleomagnetycznych sekwencji Kamenca (Ukraina Zakarpacka). Tomy Jurajskie, 1: 29–33.

Lewandowski, M., Krobicki, M., Matyja, B. A. & Wierzbowski, A., 2005. Palaeogeographicevo lu tion of the Pieniny Klippen Ba sin us ing strati graphic and palaeomagnetic data from theVeliky Kamenets sec tion (Carpathians, Ukraine). Palaeo ge ogra phy, Palaeoclimatology,Palaeo ec ol ogy, 216: 53–72.

Mišík, M., Siblík, M., Sykora, M. & Aubrecht, R., 1994. Ju ras sic brachi o pods and sedimentologicalstudy of the Babiná klippe near Bohunice (Czorsztyn Unit, Pieniny Klippen Belt). MineraliaSlovaca, 26 (4): 255–266.

Myczyñski, R., 1973. Stratygrafia jury œrodkowej serii braniskiej okolic Czorsztyna, pieniñski passka³kowy (Mid dle Ju ras sic stra tig ra phy of the Branisko Suc ces sion in the vi cin ity of Czorsztyn,Pieniny Klippen Belt, Carpathians). Studia Geologica Polonica, 42: 122 pp.

Myczyñski, R., 2004. Toarcian, Aalenian and Early Bajocian (Ju ras sic) ammonite fau nas andstra tig ra phy in the Pieniny Klippen Belt and the Tatra Mts, West Carpathians. Studia GeologicaPolonica, 123: 7–131.

Myczyñski, R. & Wierzbowski, A., 1994. The ammonite suc ces sion in the Callovian, Oxfordian andKimmeridgian of the Czorsztyn Lime stone For ma tion at Halka Klippe, Pieniny Klippen Belt,Carpathians. Bul le tin of the Pol ish Acad emy of Sci ences: Earth Sci., 42: 155–164.

Rehaková, D. & Wierzbowski, A., 2004. Microfacies and strati graphic po si tion of the Up per Ju ras sicRogo¿a Coquinas at RogoŸnik, Pieniny Klippen Belt, Carpathians. Tomy Jurajskie, 3: 15–27.

Scheibner, E., 1964a. The prob lem of Aalenian and stra tig ra phy of Lower Dogger in the WestCarpathians. Col lo quium sur Jurassique (Lux em bourg, 1962): 639–648.

Scheibner, E., 1964b. Con tri bu tion to the knowl edge of Murchisonae beds in the Klippen Belt of West Carpathians in Slovakia. Geologicky Sborník (Bratislava), 15 (1): 27–55.

Sidorczuk, M., 2005. Mid dle Ju ras sic ammonitico rosso de pos its in the north west ern part of thePieniny Klippen Belt in Po land and their palaeogeographic im por tance; a case study fromStankowa Ska³a and “Wapiennik” Quarry in Szaflary. Annales Societatis Geologorum Poloniae,75 (3): 273–285.

Tyszka, J., 1994a. Palaeoenvironment of basinal Mid dle Ju ras sic car bon ates, Pieniny Klippen Belt,Carpathians. Bul le tin of the Pol ish Acad emy of Sci ences: Earth Sci., 39 (3): 231–251.

Tyszka, J., 1994b. Palaeoenvironmental im pli ca tions from ichnological and microfaunal anal y ses ofBajocian spotty car bon ates, Pieniny Klippen Belt, Pol ish Carpathians. Palaios, 9: 175–187.

Tyszka, J., 1999. Foraminiferal biozonation of the Early and Mid dle Ju ras sic in the Pieniny Klippen


Belt (Carpathians). Bul le tin of the Pol ish Acad emy of Sci ences: Earth Sci., 47 (1): 27–46.Tyszka, J., 2001. Microfossil as sem blages as bathymetric in di ca tors in the Toarcian/Aalenian

“Fleckenmergel” fa cies in the Carpathian Pieniny Klippen Belt. Geologica Carpathica, 52 (3):147–158.

Tyszka, J. & Kaminski, M. A., 1995. Fac tors con trol ling dis tri bu tion of ag glu ti nated foraminifera inAalenian–Bajocian dysoxic fa cies (Pieniny Klippen Belt, Po land). In: Kaminski, M. A., Geroch,S., Gasiñski, M. A. (eds). Pro ceed ings, 4th In ter na tional Work shop on Ag glu ti nated Forami-nifera, Kraków (Sept. 12-19, 1995). Grzybowski Foun da tion, Spe cial Pub li ca tion, 3: 271–291.

Uhlig, V., 1890. Ergebnisse geologischer Aufnahmen in den westgalizischen Karpathen. II. Derpieninische Klippenzoug. Jahrbuch der k.k. geologischen Reichsanstalt, Wien, 40 (3-4): 559–824.

Widz, D., 1991. Les radiolaires du Jurassique supérieur des radiolarites de la zone des Klippes dePieniny (Carpathes Occidentales, Pologne). Re vue de Micropaléontologie, Paris, 34 (3): 231–260.

Widz, D. & De Wever, P., 1993. Nou veaux Nassellaires (Radiolaria) des radiolarites jurassiques de lacoupe de Szeligowy Potok (Zone des Klippes de Pieniny, Carpathes occidentales, Pologne).Re vue de Micropaléontologie, 36 (1): 77–90.

Wierzbowski, A., Jaworska, M. & Krobicki, M., 1999. Ju ras sic (Up per Bajocian–low est Oxfordian)ammonitico rosso fa cies in the Pieniny Klippen Belt, Carpathians, Po land: its fauna, age,microfacies and sed i men tary en vi ron ment. Studia Geologica Polonica, 115: 7–74.

Wierzbowski, A., Aubrecht, R., Krobicki, M., Matyja, B. A. & Schlögl, J., 2004. Stra tig ra phy andpalaeogeographic po si tion of the Ju ras sic Czertezik Suc ces sion, Pieniny Klippen Belt (West ernCarpathians) of Po land and East ern Slovakia. Annales Societatis Geologorum Poloniae, 74:237–256.

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