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S T U D I A G E O L O G I C A P O L O N I C A Vol. 123, Kraków 2004, pp. 133–197. Geology of the Pieniny Klippen Belt and the Tatra Mts, Carpathians Edited by K. Birkenmajer Part XVII

Andrzej PSZCZÓ£KOWSKI & Ryszard MYCZYÑSKI1

Ammonite-supported microfossil and nannoconid stratigraphy of the Tithonian–Hauterivian limestones in selected sections of the Branisko Succession, Pieniny Klippen Belt (Poland)2 (Figs 1–20; Tables 1–5)

Abstract. The studied sections of the Tithonian–Hauterivian deposits of the Branisko Succession in the Polish part of the Pieniny Klippen Belt (Figs 1–7) yielded micro-, nanno- and macrofossils, which allowed to elaborate more detailed stratigraphy of these strata, especially in the lowermost Cretaceous interval of the Pieniny Limestone Formation. The calpionellids, radiolarians and other microfossils (mainly calcareous dinoflagellate cysts) were studied in thin sections, whereas the calcareous nannofossils were analysed under SEM. The Berriasian–Hauterivian ammonites are described and illustrated. In the Kapuœnica I section, the Upszar Limestone Member of the Czorsztyn Limestone Formation seems to be exclusively of Tithonian age. At present, the Upper Tithonian deposits of the Crassi- collaria Standard Zone are missing in the studied section. In the £ysonka Klippe, the Lower Berriasian limestones are subdivided on the basis of the Nannoconus assemblages. The ammonites of the Jacobi Zone occur in the limestones of the N. steinmannii steinmannii Zone. In the Kapuœnica I section, the sedimentation rate of the limestones assigned to the Elliptica Subzone was about 1.3 m/Ma. The Oblonga Subzone (sensu lato) coincides with the marly deposition episode in this section; the £ysonka Marl Bed is assigned to the lower interval of this subzone. However, the overall sedimentation rate during the Late Berriasian Oblonga Subzone was low (about ~1.7 m/Ma). Presence of the ammonite Tirnovella otopeta Zone was documented in the Kapuœnica II and £ysonka sections. In the Kapuœnica II section, the minimum value of sedimentation rate of the radiolarian-calpionellid limestones assigned to the Lower Valanginian Calpionellites Zone is about 4.1 m/Ma. The Tintinno- psella Zone of the uppermost Lower Valanginian–Hauterivian is represented by a limestone succession about 51 m thick. In the £ysonka section, the Upper Valanginian limestones of this zone are probably older than those exposed in the Zaskale section. In the latter section, some ammonites are indicative for the Upper Valanginian Criosarasinella furcillata Zone. In the upper part of the

1 Institute of Geological Sciences, Polish Academy of Sciences, ul. Twarda 51/55, 00-818 Warszawa, Poland. E-mail: [email protected]; [email protected] 2 Manuscript accepted for publication August 24, 2004. 134 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI

Kapuœnica II section, the limestones of the Tintinnopsella Zone yielded Olcostephanus sp. and Neolissoceras desmoceratoides (Wiedmann) found 4.5 m below the top of this section. These ammonites indicate the Early Hauterivian age of the sparsely fossiliferous limestones. The Upper Hauterivian deposits may be represented in the topmost limestones of the Kapuœnica II section.

Key words: Pieniny Klippen Belt, Branisko Succession, Pieniny Limestone Formation, £ysonka Marl Bed, Czorsztyn Limestone Formation, Upszar Limestone Member, Tithonian–Hauterivian, calpionellids, ammonites, radiolarians, nannoconids, biostratigraphy

INTRODUCTION The Tithonian and Lower Cretaceous limestones of the Branisko Succession are represented by the Czorsztyn Limestone Formation and the Pieniny Limestone For- mation (Birkenmajer, 1977). In the Polish part of the Pieniny Klippen Belt (PKB), strictly biostratigraphic studies of these limestones were rather infrequent (Birken- majer & G¹siorowski, 1962; Nowak, 1976; Obermajer, 1987). There are also vari- ous papers dealing with stratigraphy of the Late Jurassic–Early Cretaceous limestones of the Kýsuca Succession in the Slovakian part of the PKB (Borza, 1969; Mi- chalík et al., 1990; Vašíèek et al., 1994; Houša et al., 1996; see also Vašíèek, 1997). Especially, the Brodno and Rochovica sections were studied in detail (Michalík et al., 1990; Vašíèek et al., 1992), also from the point of view of magnetostratigraphy in the Jurassic–Cretaceous boundary interval (Houša et al., 1996, 1999). In the Polish part of the PKB, lack of updated and/or sufficiently detailed biostratigraphic data concerning stratigraphy of the uppermost Jurassic–Lower Creta- ceous deposits in the Branisko Succession was inconvenient not only for stratigraphic reasons but also because it hampered palaeomagnetic and stable isotope studies. To fill this gap, we have elaborated biostratigraphy of the limestones currently exposed in the following sections (Fig. 1): Kapuœnica Klippe (Titho- nian–Hauterivian interval), £ysonka Klippe (Berriasian–Valanginian interval) and Zaskale (Upper Valanginian–lowermost Hauterivian? interval). The microfossil stratigraphy was elaborated by the first author (A. P.), and the macrofauna was studied by the second author (R. M.).

PREVIOUS WORK Neumayr (1868), Zittel (1870) and Uhlig (1890) published the earliest information concerning stratigraphy and age of the Upper Jurassic and Lower Cretaceous deposits in the Pieniny Klippen Belt. In the deposits later assigned to the Branisko Succession, Uhlig (1890) found Crioceratites ex. gr. duvali Léveillé = Criocer- atites (Crioceratites) ex. gr. duvali Léveillé and Lamellaptychus didai (Coquand) (cf. Birkenmajer, 1958, p. 64). In those early papers, fauna collected from the Branisko and Pieniny Successions in the Polish part of the PKB was published together. Birkenmajer (1958) attempted to subdivide the abovementioned faunal lists between the Branisko and Pieniny successions. Nevertheless, according to Birken- majer (1958), macrofauna listed in his paper could have been collected from the de- MICROFOSSIL AND NANNOCONID STRTIGRAPHY 135 A Kraków R CARPA TE TH U IAN O CAR S ER PAT N HI IN AN Bratislava S Budapest 100 km

Du B c n e a j je a c

u D CZORSZTYN

Zas- y C ³ a

kale i

B NIEDZICA I £ysonka SZAFLARY Kapuœnica CASTLE II sections 10 km NIEDZICA

C ZASKALE

Zaskale

c n section

p e j y £ysonka a z

r n

k section u S g r bo D s k any R y o ³ ¯d¿ar t a o i

P B SZAF- 1 km LARY MARUSZYNA

Fig. 1. Location map of the studied sections in the Pieniny Klippen Belt (Poland): A – position of the area shown in B on a generalized tectonic map of the Western Carpathians (partly after Birkenmajer, 1977); B – location of the Kapuœnica I and II, £ysonka and Zaskale sections in the Pieniny Klippen Belt in Poland (after Birkenmajer, 1977); insert shows the position of area enlarged in C; barbed lines denote tectonic boundaries of PKB; C – Zaskale and £ysonka sections situated between Maruszyna, Szaflary and Zaskale (after Birkenmajer, 1977)

posits that belong to both successions: (1) ammonites – Phylloceras sp., Protetra- gonites quadrisulcatus (d’Orbigny), Neolissoceras grasianum (d’Orbigny), Hol- codiscus (Spitidiscus) incertus (d’ Orbigny) and Perisphinctes sp., (2) belemnites – Pseudobelus bipartitus Blainville and Duvalia dilatata (Blainville), (3) aptychi – Lamellaptychus angulocostatus (Peters), Lamellaptychus didayi (Coquand), and (4) brachiopods – Terebratula subtriangulus Gümbel and Pygope janitor (Pictet). This faunal assemblage is of Tithonian–Barremian age. More numerous and better preserved macrofaunal specimens were collected from the Pieniny Limestone For- mation of the Kýsuca Succession in Slovakia (cf. Birkenmajer, 1958). Vašíèek 136 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI

(1997) reported new data concerning ammonite findings in the deposits of this succession. Birkenmajer (1958) published calpionellid assemblages indicating the Titho- nian–Berriasian age of the lower part of the “cherty limestone” (= Pieniny Lime- stone Formation of Birkenmajer, 1977). In the Kapuœnica section (Fig. 1), the Czorsztyn Limestone Formation belongs to the Upszar Limestone Member; its age was defined to be Kimmeridgian or Kimmeridgian to Lower Tithonian (Birkenma- jer, 1977). The Kapuœnica section was designated as the type locality of the Pieniny Limestone Formation (op. cit.). The standard Crassicollaria, Calpionella, Calpi- onellopsis and Calpionellites Zones have been identified in the Pieniny Limestone Formation and compared with the Vocontian zones established by J. Remane (Bir- kenmajer, 1977, tab. 13). In his table (op. cit.), the calpionellid zones are correlated also with the aptychus zones (after Durand-Delga & G¹siorowski, 1970), and the ammonite zones. Proposed correlation of the calpionellid and ammonite zones may, however, need rectification in the light of later publications (for example, Re- mane, 1985; Tavera et al., 1994; Blau & Grün, 1997). G¹siorowski (1962) reported aptychi of Late Kimmeridgian to Early Tithonian age from the “pseudonodular limestone” (= Czorsztyn Limestone Formation – Birkenmajer, 1977) and Berria- sian to Lower Barremian from the “biancone limestone” (= Pieniny Limestone For- mation of Birkenmajer, 1977). Nowak (1976) recognised the Carpistomiosphaera borzai (Nagy) and Parasto- miosphaera malmica (Borza) zones (Late Kimmeridgian–Early Tithonian) in the lower part of the “pseudonodular limestone” (= Czorsztyn Limestone Fm.) exposed in the Kapuœnica section. According to this author (op. cit.), microfossils characteristic for the Chitinoidella Zone were found in the “passage beds”, 0.6 m below the lower boundary of the “cherty limestone” (= Pieniny Limestone Fm.). Nowak (op. cit.) mentioned also a calpionellid assemblage from a sample collected in the basal part of the Pieniny Limestone Fm., composed of Crassicollaria intermedia (Du- rand-Delga), Cr. massutiniana (Colom), Cr. parvula Remane, Cr. sp. (“pathological forms”), Calpionella elliptica Cadisch, C. alpina Lorenz and ?Amphorellina subacuta Colom. The listed calpionellids were correlated with the upper part of the Berriasian Zone B of Remane (Nowak, 1976), but the presence of Cr. intermedia and Cr. massutiniana is not in accordance with this interpretation. Birkenmajer and G¹siorowski (1962) studied the Tithonian–Valanginian deposits of the Branisko Succession exposed in the £ysonka Klippe situated near Ma- ruszyna on the right bank of the Ma³y RogoŸnik (or Skrzypny) stream (Fig.1). They described a marly unit named “variegated nodular marls” and established its Late Berriasian age on the base of calpionellids and aptychi. This marly unit was for- mally named the £ysonka Marl Bed of the Pieniny Limestone Formation, and correlated with the Calpionellopsis Zone (Birkenmajer, 1977). Golonka and Sikora (1981) described microfacies “of the Jurassic and Lower Cretaceous sedimentarily thinned deposits” of the Pieniny Klippen Belt in Poland, attributed mainly to their Hulina and Z³atne successions (not accepted by Birken- majer, 1977, 1979 and later papers). Their “Stare Bystre-school” section, assigned MICROFOSSIL AND NANNOCONID STRTIGRAPHY 137 to tectonically reduced Branisko Succession by Birkenmajer (1958, 1979), includes the “cherty limestone” (= Pieniny Limestone Formation – Birkenmajer, 1977) 7 m thick, only. Obermajer (1987) published results of his preliminary micropaleontological characteristics of the Pieniny Limestone Formation based on a few samples only. This author (op. cit.) studied the Kapuœnica, Zawiasy and the Pasieczny Stream sections of the Branisko Succession, and the Sobczañski Gorge section of the Pieniny Succession. He confirmed an earlier view on the Late Kimmeridgian/Early Titho- nian to Barremian age of the Pieniny Limestone Formation (cf. Birkenmajer, 1977), and correlated the age of the lower boundary of the Pieniny Limestones Fm. (in the Kapuœnica section) with the Crassicollaria Zone (= A Zone of J. Remane).

DESCRIPTION OF THE STUDIED SECTIONS Kapuœnica I and II sections We have studied two sections in the Kapuœnica Klippe: Kapuœnica I and II (Fig. 1B; Fig. 2). These sections are located in the northern part of the klippe (see Birken- majer, 1958, 1965, 1979 for information on its tectonic structure) being separated from one another by a tectonic zone with brecciated and folded limestone. This is the type locality of the Pieniny Limestone Formation (Birkenmajer, 1977). The Ka- puœnica I section, located in the northern part of the klippe, begins with the Czorsz- tyn Limestone Formation overlying the Czajakowa Radiolarite Formation (Fig. 3; cf. Birkenmajer, 1977, fig. 33A). Before the dam construction, the Czorsztyn Lime- stone Fm. (about 4 m thick) was exposed at the level close to the Dunajec River (Birkenmajer, 1958; Nowak, 1976, fig. 10). At present, thin-bedded green and red limestones about 2.5 m thick of the Upszar Limestone Member (Birkenmajer, 1977) crop out at the dam’s level. This is because of a tectonic contact between the Czorsztyn Limestone Fm. and the Pieniny Limestone Fm. (cf. Fig. 4). The limestones of the Upszar Limestone Member, currently preserved in the section, belong to the Lower Tithonian (Fig. 3). The overlying Pieniny Limestone Formation is 5.5 m thick (Fig. 3) between the Czorsztyn Limestone Fm. and a zone of tectonic deformation separating the Kapuœnica I and II sections. Because of their lithological features (but not age), the limestones occurring in this part of the section may correspond to the lower unit of the Pieniny Limestone Fm. (Birkenmajer, 1977). The exposed bedded light-grey micritic limestones are strongly tectonically disturbed; their age is Early to Middle Berriasian (Fig. 3). Therefore, the Upper Tithonian limestones of the basal part of the Pieniny Limestone Fm. (Nowak, 1976) are missing in the Kapuœnica I section. The Kapuœnica II section of the Pieniny Limestone Formation begins with Up- per Berriasian grey and greyish-green spotty limestones, with chert nodules and lenses, about 6 m thick (Fig. 5A). These limestones dip to NE, being in a tectonically reversed position. The limestones still resemble the lower unit of the formation (cf. Birkenmajer, 1977) and are Late Berriasian in age. Brown spotty limestones appear in the section at the Berriasian–Valanginian boundary, whereas black 138 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI

Fig. 2. Pieniny Limestone Formation of the Branisko Succession, Pieniny Klippen Belt (Poland): 1 – Lower Valanginian limestones of the Calpionellites Zone, lower part of the Kapuœnica II section (sampled beds 2K-15 through 17 in Fig. 5A); 2 – a prominent limestone bed with chert lenses and nodules in the middle part of the Kapuœnica II section (Tintinnopsella Zone, Upper Valanginian bed; sample 2K-57 was taken from this bed – cf. Fig. 5A); 3 – Valanginian limestones exposed in the upper part of the £ysonka Klippe section (basal interval of the Tintinnopsella Zone – cf. Fig. 6); 4 – Upper Valanginian limestones with marl interbeds exposed in the lowermost part of the Zaskale section (cf. Fig. 7) MICROFOSSIL AND NANNOCONID STRTIGRAPHY 139 cherts are present in the Lower Valanginian limestones (Fig. 2: 1). Yellowish spotty limestones with nodules and lenses of chert are common in the Upper Valanginian interval of the section (Fig. 2: 2). These limestone types represent the middle unit of the Pieniny Limestone Fm. (Birkenmajer, 1977). Grey-brown and grey micritic limestones with common cherts occur in the upper part of the section. These deposits of Hauterivian age may correspond to the upper unit of the formation (cf. Bir- kenmajer, 1977). A grey radiolarian limestone with nodules and lenses of black chert terminates the Kapuœnica II section (Fig. 5B). The top of the section does not correspond to the upper boundary of the Pieniny Limestone Formation, as younger Early Cretaceous deposits occur in an outcrop situated south of the studied interval (Birkenmajer, 1977). £ysonka section The £ysonka section is located in the £ysonka Klippe near Maruszyna (Fig. 1C; see also Birkenmajer, 1977, fig. 7R); this section, designated one of the reference sections of the Pieniny Limestone Formation (Birkenmajer, 1977), was studied earlier (Birkenmajer & G¹siorowski, 1962). At present, however, the outcrop is not strictly the same as it was 40 years ago. The deposits of the Czorsztyn Limestone Formation are poorly exposed there. The contact of this unit with the Pieniny Lime- stone Formation is covered by alluvial deposits, soil and vegetation. Therefore, only the lower part of the Pieniny Limestone Formation could be studied. Micritic limestones with small chert nodules, marly limestones and marls 21.5 m thick crop out in this section (Fig. 6), which is not fully continuous because of two gaps in the outcrop. Nevertheless, the exposed deposits are better preserved and less deformed in comparison with many other sections of the Pieniny Limestone Formation. The lower part of the section consists of bedded light-green and light-grey micritic limestones about 9 m thick, with occasional chert nodules. Rare ammonites occur in the upper interval of this part of the section that is Early Berriasian in age. The described part of the section corresponds to the “biancone” (informal unit) of Bir- kenmajer and G¹siorowski (1962). Grey marls and marly limestones, sometimes nodular, appear after a gap in the section. These deposits correspond to the “variegated nodular marls” (informal unit) of Birkenmajer and G¹siorowski (1962), later renamed the £ysonka Marl Bed of the Pieniny Limestone Fm., of Late Berriasian to Valanginian age (cf. Birkenmajer, 1977). According to our observations, the deposits of this bed are 1.4 m thick. The upper part of the section (about 9 m), consists of bedded grey-yellow micritic limestones with thin interbeds of marly shales and marls, and occasional chert nodules. Thin-bedded marly limestone 1.3 m thick occurs in the lower part of this interval (Fig. 6). In the uppermost part of the section (Fig. 2: 3), the yellow spotty limestones contain common chert nodules and some limestone beds are strongly bioturbated. Birkenmajer and G¹siorowski (1962) named this part of the section “cherty limestone” (informal unit) of Valanginian (or Valanginian–Lower Hauterivian) age. Our study confirms a Valanginian age of the upper part of the £ysonka section, except its basal interval about 2.7 m thick, which belongs to the Upper Berriasian (Fig. 6). 140 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI MICROFOSSIL AND NANNOCONID STRTIGRAPHY 141 - - s y – i n n e c r e o G e i g d , t p i NE s s a – t i n I s i 0 v I a y I 0 e t c r ; r 1 s b e e > t e c b a n a n l N l ; o u t s e n s – e e g l e ? a h

p K-11 l ; m f i w i m ( o l K-11A m a n s d s i o l n e d – o o d i s c 9 K-10 d t u . 2 e c f o e b h c e

- K-9 s r g a n a l n i u l i c h o l e K-8 h t r i t

a K-6 h h n c t n s a i i – 1 d - m

N K-14 d e D

K K7- s e , R ; r s n ) K-13 K-17 – e d d 7 i f n l 9 m c l

a K-15 i 9 ; e c ) 1 n n e ( e o % p e i u s r 0 K-12 a p l l g 4 e - l a > B h c b ( s d a t i – i n n f y a i a e C t r d n : n g n s ü e t r u – d n i b G I e I a f n d ; o – o n e l t a p 5 i a ) ; t r m ) a 4

o 0 1 m l t o 9 % o c a 9 i 0 s 1 f d 4 e ( a o i – r p c 0 e d o a 2 g f e ( P a r o t , r n 2 3

) 1 n – c o 1 e i I 7 c : m r m s 9 l e f m 1 o p ( o o b .

c Fig. 4. Sketch of the tectonic contact between the Czorsztyn a s l m a n – s t o y a Limestone Formation (Upszar Limestone Member) and the Pieniny 4 i e s t ; d ) c a n

e Limestone Formation in the Kapuœnica I section (for location of the i i n n g % v i a e o 0 f section see Fig. 1B). 1 – greyish-green and reddish limestones of the l r e m 2 o b e d – l

h b Upszar Limestone Member; 2 – grey bedded limestones of the l 5 t a a i ( x A ; t

L Pieniny Limestone Formation (lower part); 3 – location of collected a r a n t . l e ) e l t

d a samples (cf. Fig. 3) u e f i B i l a q m 1 l n e s . o e r a e c g f n i n m o o – F i e o c z 3 c p e R l ; b a e a ) – s u S c . s n % f – R d o 5 o i , n S – t a y a , a 1 l c ( l s c s t e n n e o l e n d a n i i r e u o r o o u q z a Zaskale section f n l e q i ( d r t o e i f i i r n l l f h d o e e i n a v C t i r n i c t o – – This section of the Pieniny Limestone Formation is lo- – e i a . l s 2 p h e l ; I R )

a cated on the right (eastern) bank of the Ma³y RogoŸnik , C R a a : . c C % i s . a n 1 i n

e stream (= Skrzypny stream), south of Zaskale (Fig. 1C). This n x œ < p n a o ( l t u o x a e t l p is a relatively recent outcrop. Its sub-vertical wall is inacces- a i r s a t e s a e t f s r K e o

o sible for sampling in its upper part; only the topmost lime- m – a i f l n h 1 o o r c : d i

. stone bed could be sampled (sample ZK-16 in Fig. 7). The ) c t o e i 3 s a b d . n c m o d g i Zaskale section consists of micritic limestones, marly lime- e l i f e f i F b m t o G stones and soft marly shales (Fig. 2: 4) about 18.5 m thick 142 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI

(Fig. 7). These Upper Valanginian–lowermost Hauterivian? deposits dip gently (about 30°) to the northeast. Yellow and greyish-green limestones are sometimes silicified and contain occasional grey, brown and black chert nodules, lenses and thin layers. These limestones are often bioturbated (“spotty”) and contain scarce macrofauna, namely ammonites, belemnites, aptychi and rare crinoid fragments.

MICROFACIES Microfacies (MF) of the Tithonian–Hauterivian limestones belonging to the Czorsztyn Limestone Formation and Pieniny Limestone Formation were studied in the Kapuœnica I and II sections. The MF types comprise Saccocoma-bearing biomicrites in the Lower Tithonian limestones of the Upszar Limestone Member, with Globochaete alpina Lombard and/or calcareous Dinoflagellata cysts (Fig. 3). Radiolarians begin to appear as an important microfacies component in the upper part of the member. The Upper Tithonian and, probably, the basal Lower Berriasian limestones are missing in this section because of tectonic causes. A lower part of the exposed Lower Berriasian limestones (Pieniny Lst. Fm.) is developed as calpionellid-Globochaete biomicrites; radiolarians soon appear in this interval, about 1 m above the obliquely truncated base of the formation (Fig. 3). The calpionellid-Glo- bochaete and calpionellid-radiolarian microfacies still occur in the Lower and Mid- dle Berriasian limestones between the Radiolaria-rich biomicrites. Radiolarians became a dominant microfacies constituent from the Middle Berriasian upward and, in general, their frequencies show a growing trend in the Late Berriasian–Hau- terivian limestones (Fig. 5A, B). Calpionellids are the second important component in the Upper Berriasian–Lower Valanginian interval (Fig. 5A), and calcareous dinoflagellate cysts play this role during the Late Valanginian–earliest Hauterivian one (Figs 5A, B). The monotonous radiolarian microfacies of the Hauterivian is rarely interrupted by appearance of redeposited calpionellids in sample 2K-81 and common benthonic foraminifers and echinoderm bioclasts in samples 2K-97 and 2K-99, respectively (Fig. 5B). In the £ysonka section, the calpionellids are the main component of the Lower Berriasian microfacies (Fig. 6). Calpionellid-radiolarian-Globochaete MF pre- dominates in biomicrites of this age. The Upper Berriasian microfacies types are also rich in calpionellids, whereas Globochaete alpina Lombard is not an important constituent being partly replaced by calcareous dinoflagellate cysts. Calpionellid- rich microfacies disappears during earliest Valanginian time being substituted by the radiolarian biomicrites (Fig. 6). The radiolarian microfacies is characteristic for the (Upper) Valanginian limestones exposed in the uppermost part of the section. The microfacies types of the limestones exposed in the £ysonka section, although similar to those observed in the Kapuœnica I and II sections, differ in their composition as concerns the uppermost Berriasian–Lower Valanginian interval. The calpionellids are the main microfacies constituent in the £ysonka section, whereas the radiolarians are the principal component in the Kapuœnica II section. E

sp. CALPIO- Ammonites, Lithological MICRO-

sp.

sp. CALPIO-

sp. sp. NELLID belemnites

E sp. B features FACIES NELLID ZONE and aptychi

heliosphaera

Ammonites Lithological MICRO- cf

STAGE STAG ZONES . cf.

DINOCYSTS

cf.

P sigali

Colomisphaera

Schizosph.

St. echinata T. carpathica

Cpst. valangin.

St. wanneri

CALCAREOUS

C. . carpathica A and aptychi features FACIES C. vogleri sp. AND

.gr.

semiradiata

STAGE STAG SUBZONES Calcareous 2K-104 Grey R

C. carpathica

Dinofl. cysts

C. vogleri

P sigali

Stomiosph.

Calpionellites

Lorenziella

C. conferta C. cieszynica Cd. semirad. C. heliospha.

“Cd.” minuta

Praecalp. Cps. simplex Cs. darderi

R. cadischiana L. hungarica Remaniella

Cpst. valangin.

Cs. major Cs. coronatus

St. echinata

Cps. oblonga

C. alpina

T. carpathica

T. longa 2K-64 Cr. ? Lytoceras lepidum R 66 radiolarian ? (scree) 2K-103 limestone 32 2K-62 R 2K-102 ? R 2K-60 R-D Banded chert Neolissoceras sp. 64 Olcostephanus sp. layer 2K-58 R-D 2K-101 30 Teschenites sub- R 2K-56 Echinata (p.p.) flucticulus (scree) P.) R-D Neolissoceras Lamellaptychus sp. 62 2K-100 R Yellowish N desmoceratoides 28 2K-54 cf.L. seranoni s R-D 2K-99 (?) R-E

spotty O 2K-52 ? limestones R 60 2K-98

LLA (P. 2K-97 Grey R-Fb 26 Protetragonites 2K-96 2K-50 E quadrisulcatus R-D 2K-95 limestones R MATI 58 2K-94

IAN

24 2K-48 R-D R

O 2K-93 I ? R

O N Neolissoceras sp. Thin-bedded

2K-46 G R 56 2K-92

22 N spotty

I 2K-91 2K-44 R limestone R

T ATION 54 2K-90

MATI 2K-42 N R N Grey and

20 IAN R ? Laminated 2K-89 R

VALANGINIAN VALAN

LLA TINTINNOPSELLAT (P.P.) grey-brown O R-D 2K-40 limestones V

F 52 I spotty 2K-38 R 2K-88

18 STO

E 2K-87 R limestones PS Lytoceras sp. R

N 2K-36 ? Dark-brown R-C E 2K-86 Lytoceras sp. 50 O 2K-34 R-D 2K-85

M R 16 Neolissoceras cf. cherts N Phylloceras sp. Black cherts ? Valanginiana STO 2K-32 2K-84 grasianum R N

I E 2K-83 Lytoceras sp. R 2K-30 R-C-G 48 Grey-brown

T M 14 ? Protetragonites Black Pseudobelus 2K-28 R-C 2K-82 HAUTERIVIAN HAUTE spotty quadrisulcatus cherts N ex gr. bipartitus 2K-26 ? R-C-D 2K-81 I limestones R NY LI 46 Lamellaptychus sp.

TINTINNOPSELLA T 2K-24 ? R-C I 2K-80 NY LI 12 2K-22 R

I Neolissoceras N 2K-79 R cf major C-R

E 2K-20 grasianum (scree) R-C 44 2K-78 Echinata Brown cherts R-D E 2K-77 10 2K-18 Minuta 2K-76 ? R-D

PIENINYPI LIMESTONE FORM R-C PIENINYPI LIMESTONE FORMATION 42 2K-75 2K-16 Brown, R 2K-74 ?

CALPIONELLITES R 8 2K-14 ? spotty R 2K-73

darderi R-C 2K-12 micritic R-C 40 2K-72 R-D 2K-10 limestones 6 Tirnovella R-C 2K-71 Neolissoceras 2K-8 R Black

IAN cf. otopeta grasianum 2K-6 R-C 38 2K-70 marlstone D-R ? Neolissoceras 2K-69 4 2K-4 grasianum R-C Black

2K-2 ? IAS Elenaella cf. Grey and R-C 2K-68 cherts

R 36 R 2K-1 subcularense greyish-green R-C 2K-67 Lamellaptychus sp.

oblonga 2 R B. cf. callisto 2K-09a spotty R m E Leptoceras ex gr. R 2K-09 jelevi 2K-66 ? BERRIASIAN B limestones R-C 34 0 2K-07 CALPIONELLOPSIS Neolissoceras sp. m 2K-65 I II III 1 2 3 4 5 I II III 1 2 Fig. 5. Kapuœnica II section (for location see Fig. 1B); A. Lower part of the section, B. Upper part of the section. Lithologic symbols: I – grey, greyish-green, brown and yellowish well-bedded limestones (biomicrites, often spotty); II – chert nodules, lenses and interbeds; III – covered intervals (no outcrop); dashed line in B (between samples 2K-93 and 94) – local tectonic contact. Relative frequency of calpionellid taxa: for theCalpionellopsis and CalpionellitesZones as in Fig. 3; for the Tintinnopsella Zone – two categories only (1 – rare, 2 – infrequent), because of scarcity of identifiable specimens (N <100); cf –Colomisphaera cf. heliosphaera; ? – uncertain identification of taxon; abbreviations of calpionellid taxa: Cr. – Crassicollaria ; C. – Calpionella ; Cps. – Calpionellopsis ; Cs. – Calpionellites ; L. – Lorenziella ; Praecalp. – Praecalpionellites; R. – Remaniella; T. – Tintinnopsella ; other microfossil taxa: C. – Colomisphaera ; Cd. – Cadosina ; "Cd" . – "Cadosina" ; Cpst. – Carpistomiosphaera ; Schizosph. – Schizosphaerella ; Stomiosph. or St. – Stomiosphaera ; P. – Praehedbergella ; calpionellid zones and subzones after: Remane et al. (1986) and Grün & Blau (1997); calcareous dinoflagellate cyst zones adapted from: Borza (1980, 1984), Lakovaet al . (1999) and Reháková (2000a); 2K-07 through 2K-104 – samples; abbreviations of microfacies components as in Fig. 3 (except for: E – echinoderm bioclasts and Fb – benthic foraminifers MICROFOSSIL AND NANNOCONID STRTIGRAPHY 143

The limestones exposed in the Zaskale section (Fig. 7) belong to the Upper Valanginian–lowermost Hauterivian (?). Echinoderm debris and common benthonic foraminifers characterize the limestones of the basal part of the section. The remaining limestones of the Zaskale outcrop are radiolarian-rich biomicrites, sometimes with an admixture of frequent echinoderm (crinoid) bioclasts and/or benthonic foraminifers, and also dinoflagellate cysts. In general, microfacies composition of the studied limestones is partly different from that of the coeval deposits exposed in the Kapuœnica II section being richer in the benthonic constituents.

BIOSTRATIGRAPHY Microfossil stratigraphy Saccocoma Zone (Early Tithonian). In the studied sections, the Tithonian deposits are represented in the Kapuœnica I section (Fig. 3) by the Upszar Limestone Member of the Czorsztyn Limestone Formation (cf. Birkenmajer, 1977). The lower part of this member, about 2.5 m thick, is exposed there, whereas the upper one is not preserved because of tectonic causes. Lower boundary of this zone is not recognised, and the upper one is placed at the base of the overlying Chitinoidella Zone (Fig. 3). Malmica Subzone (EarlyTithonian). The Malmica Zone was recognised by Nowak (1968) in the Lower Tithonian, and accepted by Borza (1969, 1984), Lakova et al. (1999) and Reháková (2000a, b). Nowak (1976) has identified this zone in his Kapuœnica profile (op. cit., fig. 10), in the lower part of the “pseudonodular limestone” (= Upszar Lst. Mbr), about 1 m above (not below, as erroneously stated in the cited paper) the top of the red radiolarites (= Czajakowa Radiolarite Formation of Birkenmajer, 1977). However, in our Kapuœnica I section, the taxon Parastomiosphaera malmica (Borza) (Fig. 8: 1) occurs in the lowermost limestone beds of the Upszar Lst. Mbr. and, therefore, these strata belong to the Malmica Sub- zone of the Saccocoma Zone (Fig. 3). As this unit is transitional to the Czajakowa Radiolarite Fm., the whole Upszar Lst. Mbr is Tithonian in age in the studied section (Fig. 3). Chitinoidella Zone (upper Early Tithonian–lowermost Late Tithonian). Presence of Chitinoidella gr. boneti-elongata in sample K-8 (Fig. 3) indicates the Chitinoidella Zone (Kreisel & Furrazola-Bermúdez, 1971; Borza, 1984). Repre- sentatives of Chitinoidellidae were not found in samples K-9 and 10, but thin- section from sample K-11 contained a few poorly preserved specimens. The original thickness of the limestones belonging to the Chitinoidella Zone in the Ka- puœnica section was 1.8 to 2.4 m, because Nowak (1976) reported Chitinoidella sp. from his sample Kap. 5 collected 0.6 m below the lower boundary of the “cherty limestone” (= Pieniny Limestone Formation). Crassicollaria Standard Zone (Late Tithonian). The Crassicollaria Zone of Late Tithonian age (Allemann et al., 1971) was not recognised in our samples. However, the limestones of this zone are probably present in the Kapuœnica section. According to Nowak (1976), his sample Kap. 1 (from the basal layer of the Pieniny 144 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI MICROFOSSIL AND NANNOCONID STRTIGRAPHY 145 . - e – – i p n . I I s m a C Limestone Formation) contained Crassicollaria intermedia ; ; r C m s e a ; e e n h s (Durand-Delga), Cr. massutiniana (Colom), Cr. parvula Re- t i n i R s s o o ; t o p r 1 s mane, Cr. sp. (“pathological forms”), Calpionella alpina Lo- d o o 7 e l f a l 9 m s e C 1 i renz, C. elliptica Cadisch and ?Amphorellina subacuta Colom. e n l , i – . o r l c . i i o a d t Although Nowak (1976) considered this calpionellid assem- p i t g l r C e e a c t ; i

n blage to be of Berriasian age, it could rather be a Late Tithonian a C a n c r m – a e o . d one. According to Obermajer (1987, fig. 2A), the basal beds a s m e w h e p t d l p l d C

s about 4 m thick of the discussed formation in the Kapuœnica y 5 i l e ; A n b a : d m i r o section could be assigned to the Upper Tithonian (Crassicol- o n r e w l ; a t a o o 3 f l l l 3 . a l laria Zone). C o g e s s i – c y e g i . F - i Calpionella alpina Subzone of the Calpionella Standard s n y F s C n o e i : a z r n a r

s Zone (Early Berriasian). This subzone occurs in the lower i b g x a C u s a d s – a t –

n part of the Calpionella Zone (cf. Allemann et al., 1971; Re- l d a s . a i t n r s x y n a s a

C mane et al., 1986; Grün & Blau, 1997). In the Kapuœnica I sec- e t e o s r : f n e d a g i o o n - l

x tion, limestones about 1.7 m thick belong to this subzone; cer- r t p l o a c h e t i z m g n

d tainly, this is not a complete original thickness because of the i d o m o i l i c i l l r , l l p e s n e e l sheared base of the Pieniny Limestone Fm. (Figs 3, 4). In the h e e a n n t i e c o o o c r i i f ; a limestones assigned to this Subzone, the following calpionellid g p p f o a - l l l t o a a l y r h

c taxa occur: C. alpina Lorenz, Crassicollaria parvula Remane, c e c c g s ; i f i n l a p o e l m

o Cr. sp., Lorenziella plicata Remane, Tintinnopsella carpathica l – u s f e n I q n o n g e : o i r

r (Murgeanu et Filipescu), Remaniella cf. catalanoi Pop (Fig. 9: s s i t f l t e n n a o b i e o i i b

d 1) and Remaniella sp. Moreover, Stomiosphaera aff. echinata T v v t i e t e a – m h i r a . y l e Nowak, 1968 (Fig. 8: 2) was found in the middle of the interval v b s T e a e b ; r c r a R i a b assigned to the C. alpina Subzone. This microfossil is similar to P l . ; g l b ) n o – e a p l i o . ;

o St. echinata Nowak, but occurs in much older strata. o n x P r s h a a ; c e t t t l i a

m In the £ysonka section, limestones 9.4 m thick are assigned f u p L n e o i o . m r R ) n o a

e to the Alpina Subzone (Fig. 6); this value, however, is also in- – C s o n a i . ( , t h – R s a

B complete, as bottom and top boundaries of this subzone are not p l ; c 0 s 1 a i s 4 . f o v e - i i t

g exposed. In this section, the following calcareous dinoflagel- r t i i £ e l m n t l F e o h n e t late cysts occur in the Alpina Subzone (Fig. 6): Stomio- e i d g n i S e u d o s – i n e o

i sphaerina proxima Øehánek (Fig. 8: 4), and Colomisphaera cf. . n r r p a l S e o h t i t a ; r v t

c carpathica (Borza). e a o a 1 e r c - c c e a n o £ – r

a Remaniella ferasini Subzone of the Calpionella Standard l u ; h P r ) – V p o I 7 – f s Zone (Early Berriasian). The Ferasini Subzone (Pop, 1994) is ? . ; 9 ( o ; s c 9 i t l n r P 1

n distinguished in the Kapuœnica I section, only (Fig. 3). The first o m ( a ; i e o t a t u u m l c l S a q occurrence (FO) of the index taxon was considered as an im- e l y e e s l – i r B . z a f e t portant phyletic event placed approximately in the middle of n h n p S i s & e p ; r i – – l n a

o the Jacobi-Grandis or Euxinus Zone of the Early Berriasian (cf. r I ü 2 K L I r e , I a a – e G Pop, 1994). However, Grün and Blau (1997) reported FO of R. ; . k r h s a d n L p e r s ; n o

n ferasini as early as in the Crassicollaria Zone. Therefore, the s s a o – o i e t y ) t 1 s i m 6 £ Ferasini Subzone (sensu Pop, 1994) may represent an acme l e : l o 8 s t e l m 9 s i i n i

1 zone. In this case, its lower boundary may not be coeval be- l s . ( o p s i y 6 r . o l l p . a f r

l tween distant sections. In the studied section, the limestones as- a g a o a C i r t

F m c C – e signed to this subzone are about 0.7 m thick (Fig. 3). In fact, the 146 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI a n a i E n i N g n O a S a a Z c l c

i a E i i i t a r I h l h v D a e a t t

a Ammonites, I C . n n d a a a g i i L n p p i p r A c h E s r s r a e

L belemnites Ammonite

c u F a a l a e w a E

c c .

l G h

O l a and aptychi zone p a a a N p a a r e s r r r R l r s A e l g e e e O e o r a C e I i a a a a a e I s h l h h h h P l m b p p p p p p e o L M d s o s s i s s t i i e n z s o A o o i i h i i m n n m i e p C e o o t m m m r l l r a n o o o r a o o o i t t t P L S C S C S T C ZK-16 ? E-R 18 N A I V I R

16 E T N

Protetragonites U O

I ex gr . H

T ? quadrisulcatus T S A 14 (scree) E I L M

R R

12 ZK-15a A R O E

ZK-14a ?Pseudobelus sp. - D-Fb F

N Olcostephanus sp. E A

Lamellaptychus sp. I N N 10 ZK-14 Protetragonites I R-D O quadrisulcatus G T ZK-13 N R Pseudobelus sp. A S

L A ex gr . P. bipartitus E 8 ZK-12 A

L L. cf. bermudezi V M

ZK-11 L R

I O. densicostatus E E T L

ZK-10 ?Karakaschiceras sp. A S

6 P. quadrisulcatus L

Y R ZK-9 N P C. furcillata C. furcillata

A N I

ZK-8 O (lower part)

I R-Fb Criosarasinella

N I ZK-7 N R-Fb

furcillata N

4 G

ZK-6 N E

N I I ZK-5 Phylloceras (H.) R-Fb A T

P thetys L

ZK-4 N

Pseudobelus sp. A I

2 ZK-3 ? V E-Fb

T ex gr . P. bipartitus Neolissoceras sp . E

ZK-2 T m Phylloceras (H.) A 0 ZK-1 thetys L E-Fb I II III IV 1 ? 2

Fig. 7. Zaskale section (for location see Fig. 1B, C). Lithologic symbols: I – yellow and greyish- green micritic limestones; II – chert nodules, lenses and interbeds; III – marly limestones; IV – marls. Occurrence of microfossil taxa: 1 – rare; 2 – uncertain identification of taxon; calpionellid zone after Borza (1984) and Grün & Blau (1997); ammonite zone – after Hoedemaeker et al. (2003); ZK-1 through ZK-16 – samples; abbreviations of microfacies components as in Figs 3 and 5 MICROFOSSIL AND NANNOCONID STRTIGRAPHY 147 index taxon was identified in one sample, only. Specimens of R. duranddelgai Pop (Fig. 9: 2–3) also occur in the interval assigned to the Ferasini Subzone. In the Ra Stua section (Italy), R. duranddelgai was reported to occur also in the Upper Berria- sian limestones (Grün & Blau, 1997; but see Reháková, 1998). Calpionella elliptica Subzone of the Calpionella Standard Zone (Early- Middle Berriasian). The lower boundary of this Subzone is designated by FO of the index taxon, whereas its upper boundary (sensu Grün & Blau, 1997) is indicated by FO of Remaniella cadischiana (Colom). In the Kapuœnica I section, R. cadischiana appears 1.7 m above the base of the Elliptica Subzone. Remaniella duranddelgai Pop and R. cf. colomi Pop (Fig. 9: 5) and R. sp. gr. R. ferasini-colomi (Fig. 9: 6) also occur in this subzone. Calcareous dinoflagellate cysts found in the Elliptica Subzone belong to the following taxa: Cadosina semiradiata fusca (Wanner) (Fig. 8: 3), Colomisphaera carpathica (Borza) and Stomiosphaera wanneri Borza (Fig. 3). Remaniella cadischiana Subzone of the Calpionella Standard Zone (Middle Berriasian). This Subzone was documented with one sample only (K-28 in Fig. 3). The next sample (K-29) contains radiolarians, but not calpionellids. The upper boundary of the Cadischiana Subzone was not identified because of strong tectonic reduction of the Middle to Upper Berriasian limestones in the Kapuœnica sections. Currently, the uppermost Lower Berriasian through lowermost Upper Berriasian deposits are not exposed in the £ysonka section (Fig. 6). According to Birkenmajer and G¹siorowski (1962), a complete transition was exposed between the “variegated nodular marls” (= £ysonka Marl Bed of Birkenmajer, 1977) and the underlying (biancone) limestones of the Pieniny Limestone Formation. Their sample 2c was taken from the uppermost part of these limestones and contained Calpionellop- sis simplex (Colom), Tintinnopsella (= Remaniella) cadischiana (Colom) and other calpionellid taxa (Birkenmajer & G¹siorowski, 1962). This assemblage is early Late Berriasian in age (Simplex Subzone of the Calpionellopsis Standard Zone); evidently, the Cadischiana/Simplex boundary was located still in the biancone limestone underlying the £ysonka Marl Bed (Birkenmajer & G¹siorowski, 1962). Simplex Subzone of the Calpionellopsis Standard Zone (lower part of the Late Berriasian). This subzone was not documented from the Kapuœnica sections; its uppermost part is exposed however in the £ysonka section (Fig. 6). Our sample £-19 was collected from the topmost limestone bed underlying the £ysonka Marl Bed and may correspond to the sample 2c of Birkenmajer and G¹siorowski (1962). Oblonga Subzone of the Calpionellopsis Standard Zone (Late Berriasian). This subzone (sensu lato) is applied herein in accordance with its definition given by Remane et al. (1986). In the Kapuœnica II section (Fig. 5A), bioturbated (“spotty”) limestones assigned to the Oblonga Subzone are about 6.6 m thick, although this value is a minimum one because the lower boundary of this subzone is not seen. In this section, the microfossil “Cadosina” minuta Borza (Fig. 8: 8) was recorded (FO) in the uppermost Berriasian strata (Fig. 5A). In the £ysonka section (Fig. 6), the £ysonka Marl Bed of the Pieniny Lst. Fm. (Birkenmajer, 1977) belongs to this subzone (cf. Birkenmajer & G¹siorowski, 148 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI

1962). Our study reveals that this bed correlates with the lower part of the Oblonga Subzone (Fig. 6). The following calpionellids were found in this subzone: Calpi- onella alpina Lorenz, Calpionellopsis oblonga (Cadisch), Cps. simplex (Colom), Calpionellopsis sp. (Fig. 9: 7), Lorenziella plicata Remane, L. hungarica Knauer et Nagy, Lorenziella sp., Remaniella cadischiana (Colom) (Fig. 9: 4), R. cf. duranddelgai Pop, R. catalanoi Pop, R. colomi Pop, Remaniella sp. and Tintinnopsella carpathica (Murgeanu et Filipescu), The upper boundary of the Oblonga Subzone, MICROFOSSIL AND NANNOCONID STRTIGRAPHY 149 and of the Calpionellopsis Zone as well, is situated 2.7 m above the top of the £ysonka Marl Bed, and directly above the thin-bedded marly limestone 1.3 m thick (Fig. 6). Therefore, in the £ysonka section, the deposits assigned to the Oblonga Subzone are about 4.2 m thick being more marly in comparison with the coeval interval exposed in the Kapuœnica II section. Calpionellites Standard Zone (Early Valanginian). In the Kapuœnica II section, the limestones correlated with the Calpionellites Zone are 8.3 m thick (Fig. 5A). The lower boundary of this zone is concordant with a lithological change in the section: the Berriasian grey and greyish-green spotty limestones are being replaced by brown spotty limestones of the Lower Valanginian. The Darderi Subzone is thin- ner (about 3 m) in comparison with the Major Subzone (5.3 m). The upper boundary of the Calpionellites Zone is delineated by the last occurrence (LO) of the index taxon. Besides Calpionellites spp. (Fig. 9: 9–12), the species Calpionellopsis oblonga (Cadisch) (Fig. 9: 8) still occurs in the lower part of the Major Subzone. Rep- resentatives of Tintinnopsella carpathica (Murgeanu et Filipescu) (Fig. 9: 13–14), relatively common in some samples, became less frequent in the uppermost interval of the Calpionellites Zone (Fig. 5A). Specimens of Calpionella alpina Lorenz and Crassicollaria sp. occur at the top of the zone (sample 2K-29), indicating reworking of older sediments and redeposition of Late Tithonian–Early Berriasian microfossils. Calcareous dinoflagellate cysts also occur in this zone: Colomisphaera cf. heliosphaera Vogler (Fig. 8: 5, 6), C. carpathica (Borza) (Fig. 8: 7), C. conferta Øehánek (Fig. 8: 9) and Stomiosphaera sp. (Fig. 8: 10), although these microfossils are uncommon in the Calpionellites Zone. In contrast, “Cadosina” minuta Borza is relatively frequent in the limestones of this zone (Fig. 5A).

Fig. 8. Calcareous cysts of Dinoflagellata from the Tithonian–Hauterivian limestones of the Branisko Succession, Pieniny Klippen Belt. 1 – Parastomiosphaera malmica (Borza, 1964), Kapuœ- nica I section, sample K-1, Early Tithonian (scale bar = 50 µm); 2 – Stomiosphaera aff. echinata Nowak, 1968, Kapuœnica I section, sample K-17, Early Berriasian (scale bar = 50 µm); 3 – Cadosina semiradiata fusca (Wanner, 1940), Kapuœnica I section, sample K-23, Mid Berriasian (scale bar = 50 µm); 4 – Stomiosphaerina proxima Øehánek, £ysonka Klippe section, sample £-11, Early Berriasian (scale bar = 50 µm); 5 – Colomisphaera cf. heliosphaera Vogler, 1941, Kapuœnica II section, sample 2K-21, Early Valanginian (scale bar = 50 µm); 6 – Enlarged fragment of specimen shown in Fig. 5 (scale bar = 25 µm); 7 – Colomisphaera carpathica (Borza, 1964), Kapuœnica II section, sample 2K-21, Early Valanginian (scale bar = 10 µm); 8 – “Cadosina” minuta Borza, 1980, Kapuœnica II section, sample 2K-11, Late Berriasian (scale bar = 50 µm); 9 – Colomisphaera conferta Øehánek, Kapuœnica II section, sample 2K-15, Early Valanginian, scale bar = 50 µm; 10 – Stomiosphaera sp., Kapuœnica II section, sample 2K-19, Early Valanginian, scale bar = 50 µm; 11, 12 – Colomisphaera vogleri (Borza, 1969), Kapuœnica II section (11 – sample 2K-21, Early Valanginian; 12 – sample 2K-76, Hauterivian), scale bar = 50 µm; 13 – Colomisphaera heliosphaera Vogler, 1941, Kapuœnica II section, sample 2K-36, Valanginian, scale bar = 50 µm; 14 – Carpistomiosphaera valanginiana Borza, Kapuœnica II section, sample 2K-38, Late (?) Valanginian (scale bar = 50 µm); 15 – Stomiosphaera echinata Nowak, 1968, Kapuœnica II section, sample 2K-91, Hauterivian, scale bar = 50 µm 150 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI MICROFOSSIL AND NANNOCONID STRTIGRAPHY 151

In the £ysonka section (Fig. 6), the Calpionellites Zone is 2.3 m thick only, and could not be subdivided into subzones. It was recognised in the middle part of the interval named “cherty limestone” by Birkenmajer and G¹siorowski (1962). Tintinnopsella Zone (uppermost Early Valanginian–Hauterivian). This is the only calpionellid zone documented in all three studied sections. In the Ka- puœnica II section, the limestones assigned to this zone are about 51 m thick (Figs 5A, B). The species Tintinnopsella carpathica (Murgeanu et Filipescu) is the only calpionellid species occurring throughout the whole interval correlated with this zone. The taxa Tintinnopsella longa (Colom) (Fig. 9: 15–16) and Lorenziella hungarica Knauer et Nagy were found in a few samples only. Other calpionellid occurrences (Remaniella ? sp. and Praecalpionellites ? sp.) are doubtful and practically unimportant from a stratigraphic point of view. Therefore, a subdivision of the Tin- tinnopsella Zone into subzones is not possible in this section. Its upper boundary is tentatively placed 2.5 m below the top of the section, above the banded chert layer (Fig. 5B). However, this is a local boundary probably not corresponding to the LO of the representatives of the genus Tintinnopsella Colom, 1948. The lower interval of the Tintinnopsella Zone is reported here from the £ysonka section; the exposed limestones belonging to this zone are about 4 m thick (Fig. 6). According to Birkenmajer and G¹siorowski (1962), the aptychi and a belemnite found in their “cherty limestone” correspond to the Valanginian and Early Hau- terivian. Our data from this section do not allow to extend the stratigraphic range of the limestones assigned to the Tintinnopsella Zone beyond the Valanginian. How- ever, our section may not include the uppermost limestone layers once exposed in the £ysonka klippe (cf. Birkenmajer & G¹siorowski, 1962).

Fig. 9. Calpionellidae from the Berriasian and Valanginian strata of the Pieniny Limestone Formation of the Branisko Succession in the Kapuœnica and £ysonka Klippe sections (scale bar = 50 µm). 1 – Remaniella cf. catalanoi Pop, Kapuœnica I section, sample K-17, Calpionella Standard Zone, Alpina Subzone, Lower Berriasian; 2, 3 – Remaniella duranddelgai Pop, Kapuœnica I section, sample K-21, Calpionella Standard Zone, Ferasini Subzone, Lower Berriasian; 4 – Remaniella cadischiana (Colom), £ysonka klippe section, sample £-26, Oblonga Subzone, Upper Berriasian; 5 – Remaniella cf. colomi Pop, Kapuœnica I section, sample K-23, Elliptica Subzone, Lower-Middle Berriasian; 6 – Remaniella sp. gr. R. ferasini-colomi, Kapuœnica I section, sample K-25, Calpionella Standard Zone, Elliptica Subzone, Lower-Middle Berriasian; 7 – Calpionellopsis sp. (form transitional between Cps. simplex and Cps. oblonga), £ysonka Klippe section, sample £-20, Oblonga Subzone, Upper Berria- sian; 8 – Calpionellopsis oblonga (Cadisch), Kapuœnica II section, sample 2K-19, Calpionellites Standard Zone, Major Subzone, Lower Valanginian; 9 – Calpionellites darderi (Colom), Kapuœnica II section, sample 2K-20, Major Subzone, Lower Valanginian; 10 – Calpionellites major (Colom), Kapuœnica II section, Major Subzone, Lower Valanginian; 11 – Calpionellites cf. major (Colom), Kapuœnica II section, sample 2K-19, Major Subzone, Lower Valanginian; 12 – Calpionellites coronatus Trejo, Kapuœnica II section, sample 2K-22, Major Subzone, Lower Valanginian; 13 – Tintinnopsella carpathica (Murgeanu et Filipescu), Kapuœnica II section, sample 2K-19, Major Subzone, Lower Valanginian; 14 – Tintinnopsella carpathica (Murgeanu et Filipescu), Kapuœnica II section, sample 2K-21, Major Subzone, Lower Valanginian; 15 – Tintinnopsella longa (Colom), Kapuœnica II section, sample 2K-54, Tintinnopsella Zone, Upper Valanginian; 16 – Tintinnopsella longa (Colom), Kapuœnica II section, sample 2K-57, Tintinnopsella Zone, Upper Valanginian 152 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI

The Tintinnopsella Zone is present also in the Zaskale section (Fig. 7), where it includes limestones with marl interbeds 10 m thick of Upper Valanginian age. The boundaries of this zone are situated beyond the range of the section. Calpionellids are rare in all thin sections studied, and they were not observed in a few samples collected in the upper part of the outcrop. In general, the deposits exposed in the Za- skale section are more marly in comparison with the coeval strata in the Kapuœnica II section. Minuta Zone (latest Berriasian–Early Valanginian). Microfossils named Cadosina minuta by Borza (1980) occur in the uppermost Berriasian (Fig. 8: 8) and Lower Valanginian strata of the Pieniny Limestone Formation (Figs 5A, 6). Status of Cadosina minuta Borza is not clear, as these microfossils differ from the typical representatives of the genus Cadosina Wanner, 1940, by their thin and indistinct test wall in many specimens and common occurrence in groups composed of 2–6 specimens (cf. Borza, 1980, figs 5-10; Pszczó³kowski, 2003, fig. 13: 9-10). It is probable that the discussed microfossil should be excluded from the genus Cados- ina Wanner, 1940. To indicate this possibility, we put the generic name in quotation marks (“Cadosina” minuta). According to Borza (1980), “Cd.” minuta forms an important zone in the Upper Berriasian–Lower Valanginian. Øehánek (1992) placed the Minuta Zone in the uppermost Berriasian (upper part of the calpionellid Zone D), whereas Reháková (2000a) proposed the Minuta Acme Zone in the late Early Valanginian. In the latter paper, the total range of the index taxon is correlated with a part of the Early Valang- inian, only. In another paper, Reháková (2000b, fig. 1) correlated the Minuta Acme Zone with the early (but not the basal) part of the Early Valanginian Calpionellites Zone and, simultaneously, mainly with the latest Berriasian Otopeta Zone (?) in the ammonite zonation. However, Michalík et al. (1990, fig. 2) reported occurrence of Cadosina minuta also from the Early Berriasian Calpionella Zone. In the Kapuœnica II section, occurrence of “Cadosina” minuta Borza is indicative for the Minuta (Acme?) Zone of latest Berriasian–Early Valanginian age (Fig. 5A). Its lower boundary is indicated by appearance of the index taxon, whereas the upper one is indicated by FO of Carpistomiosphaera valanginiana Borza. There- fore, the range of the Minuta Zone in this section comprises the topmost part of the Calpionellopsis Zone, the whole Calpionellites one and the basal interval of the Tintinnopsella Zone. In the £ysonka section (Fig. 6), this range is slightly shorter, as “Cd.” minuta Borza was not found there in the Calpionellopsis Zone. Valanginiana Zone (Valanginian). The taxon Carpistomiosphaera valanginiana Borza was identified in samples from the Kapuœnica II, £ysonka and Zaskale sections. In the first section, the Valanginiana Zone is confined to the lowermost, but not the basal, part of the Tintinnopsella Zone (Fig. 5A). The upper boundary of the Valanginiana Zone is uncertain, as there is a broad gap between the “LO” of Cpst. valanginiana Borza and FO of Stomiosphaera echinata Nowak. According to Lakova et al. (1999) and Reháková (2000a), the former taxon occurs up to the Late Hauterivian, whereas the latter one appears in the middle of the Late Valanginian. Reháková (2000b) correlated the Valanginiana Zone with the Valanginian–Hau- MICROFOSSIL AND NANNOCONID STRTIGRAPHY 153 terivian boundary interval. However, in the Kapuœnica II section, this zone is probably of late Early Valanginian age. Therefore, this calcareous dinocyst zone may be narrowed there in comparison with the interval occupied in some other sections. In the £ysonka section, the record of Cpst. valanginiana is discontinuous, but clearly related to the lower part of the Tintinnopsella Zone (Fig. 6). Infrequent occurrences of this taxon in the Zaskale section correspond to the Echinata Zone (Fig. 7). Echinata Zone (Late Valanginian–Hauterivian). In the Kapuœnica II section, the Echinata Zone (as established by Lakova et al., 1999) is identified in the Upper Valanginian and Hauterivian limestones (Figs 5A, B). Its lower boundary is indicated by FO of Stomiosphaera echinata Nowak in the Upper Valanginian strata. In general, however, occurrence of this calcareous dinocyst taxon is discontinuous in the section under study. The upper boundary of the Echinata Zone (cf. Reháková, 2000a) occurs above the top of the studied section. It seems that the radiolarian-rich microfacies of the (Late) Hauterivian in general was not favourable for St. echinata Nowak and other calcareous dinoflagellate cysts. Lack of St. echinata Nowak record in the £ysonka section may be due to the Late Berriasian–early Late Valangin- ian age of the limestones exposed there above the £ysonka Marl Bed (Fig. 6). Occurrence of St. echinata Nowak in the Zaskale section indicates the presence of the Echinata Zone in this outcrop. The ammonites found in the lower part of the section are characteristic for the middle Late Valanginian Trinodosum Zone (Fig. 7). Therefore, the base of the Echinata Zone is located within, or even below, the Trinodosum Zone. Early appearance of St. echinata Nowak in the basal interval of the Tintinnopsella Zone was recorded outside the Pieniny Klippen Belt (in the Tatra Mts – Pszczó³kowski, 2003). This is not in accordance with the previous estimates of the stratigraphic position of the lower boundary of the Echinata Zone (Lakova et al., 1999; Reháková, 2000a, b).

Radiolarian assemblages (studied in thin sections)

Calcitized radiolarians are abundant in the studied sections of the Pieniny Lime- stone Formation. Usually, they are poorly preserved as their tests are completely replaced by calcite or, less frequently, by secondary silica. A few radiolarian tests are, however, better preserved, and structure and/or shape of their tests may be observed in thin sections. Some of these specimens could be identified to a generic level, only; in other cases, it was possible to indicate a species or a group of species. Nu- merous radiolarian taxa have very long ranges; some species, however, are known to occur during shorter intervals (Jud, 1994; Baumgartner et al., 1995a). Identifica- tions made in thin sections (Figs 10–13) do not permit to propose a radiolarian zonation, because of highly selective and incomplete character of the data collected from this type of analysis. According to Jud (1994, p. 50), “the radiolarian zones are not defined only by first and last appearance datum (LAD) of one species but by the co- existence of several species within one zone”. Baumgartner et al. (1995b) presented the Tethyan radiolarian zonation that spans the Aalenian to early Aptian time inter- 154 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI

Fig. 10. Berriasian radiolarians identified in thin sections from the Pieniny Limestone Formation of the Branisko Succession exposed in the £ysonka and Kapuœnica II sections, (scale bar = 100 µm). 1 – Triactoma cf. tithonianum Rüst, sample £-2, Early Berriasian; 2 – Parvicingula gr. boesii (Parona), sample £-4, Early Berriasian; 3 – Canoptum banale Jud, sample £-2, Early Berriasian; 4 – Archaeo- dictyomitra gr. apiarum-excellens, sample £-4, Early Berriasian; 5 – Xitus (?) sp. gr. X. (?) alievi (Foreman), sample 2K-12, latest Berriasian; 6 – Obesacapsula cf. verbana (Parona), sample £-22, Late Berriasian; 7 – Pantanellium sp. aff. P. cantuchapai Pessagno et Mc Leod, sample £-2, Early Berriasian; 8 – Obesacapsula cf. rusconensis umbriensis Jud, sample £-11, Early Berriasian; 9 – Sethocapsa cf. uterculus (Parona) sensu Foreman, sample 2K-16, Early Berriasian; 10 – Sethocapsa cf. dorysphaeroides Neviani sensu Schaaf, sample £-4, Early Berriasian; 11 – Sethocapsa cf. kitoi Jud, sample £-15, Early Berriasian MICROFOSSIL AND NANNOCONID STRTIGRAPHY 155 val and is based on a synthesis including 127 Unitary Associations grouped into 22 Unitary Association Zones (UAZones 95). Ranges for 451 taxa with respect to the UAZones are shown in their Fig. 6a-g (op. cit.); these UAZones 1–22 were cali- brated to the standard stages and correlated to earlier zonations (Baumgartner et al., 1995b). Identifiable radiolarians (from one to 15 taxa in a single sample) have been found in thin sections made from 16 samples collected in the £ysonka section. In general, microfossils are better preserved in the limestones exposed in this section in comparison with other studied sections of the Branisko Succession. In the Ka- puœnica I and II sections, radiolarians were identified in 42 samples: the list of determined microfossils comprise from one to 13 taxa. In the Zaskale section, better- preserved radiolarians have been found in three samples, only. The most important results of these identifications are summarized below.

A. Kapuœnica I and II sections (Figs 5A, B) (1) The radiolarians are poorly preserved in thin sections made from the samples of Czorsztyn Limestones Formation and Pieniny Limestone Formation in the Ka- puœnica I section. In general, one or two taxa were identified in some thin sections, only. Usually, the better-preserved specimens, as for example, Sethocapsa uterculus (Parona) sensu Foreman (Fig. 11: 2) belong to the long-ranging taxa. Obesacap- sula gr. polyedra (Steiger) was identified in the sample K-19 (Alpina Subzone of Lower Berriasian according to calpionellid assemblage – Fig. 3), whereas the species O. polyedra (Steiger) was reported from the UAZones 13–17 (latest Titho- nian–Late Valanginian, Baumgartner et al., 1995a). (2) Samples 2K-07 and 2K-08 were collected from the basal beds of the Ka- puœnica II section (Fig. 5A). The former sample (thin section) yielded Stichomitra sp. aff. asymbatos Foreman (Fig. 11: 11 ), only. The radiolarians found in the latter sample, especially Ristola cf. asparagus Jud (Fig. 11: 3), Pseudoeucyrtis cf. sceptrum Jud (Fig. 11: 5), Obesacapsula sp. gr. O. bullata Steiger (Fig. 11: 8) and Parvicingula usotanensis Tumanda (Tab. 1), are consistent with the Upper Berria- sian age of this limestone as established on calpionellids and ammonites. Other taxa, such as Wrangellium sp. gr. W. depressum-puga (Fig. 13: 3), are of little help in stratigraphic correlation of the studied sample. (3) Samples from the Upper Berriasian limestones contain relatively numerous radiolarians of variable preservation. Sample 2K-5 contains: Hsuum cf. raricosta- tum Jud, Obesacapsula cf. breggiensis Jud, Sethocapsa tricornis Jud (Fig. 13: 2) and Sethocapsa sp. gr. S. uterculus-trachyostraca. Occurrence of these taxa is consistent with the Upper Berriasian age of the sample (Fig. 5A). The age of radiolarians identified from samples 2K-7 and 2K-10 is poorly constrained, as almost all are the long-ranging taxa. Four taxa from a total of twelve are shown in Tab. 1 for sample 2K-7. Presence of Obesacapsula cf. rusconensis umbriensis Jud indicates that sample 2K-7 probably is not younger than Upper Berriasian–lowermost Valangin- ian (see Baumgartner et al., 1995a). Calpionellids determine its age as uppermost 156 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI

Fig. 11. Tithonian–Early Valanginian radiolarians identified in thin sections from the Czorsztyn Limestone Formation and the Pieniny Limestone Formation of the Branisko Succession exposed in the Kapuœnica I and II sections (1–9, 11) and the £ysonka section (10), Pieniny Klippen Belt (scale bar = 100 µm): 1 – Tritrabs sp., sample 2K-10, Late Berriasian, Pieniny Lst. Fm.; 2 –Sethocapsa uterculus (Parona) sensu Foreman, sample K-10, Early Tithonian, Czorsztyn Lst. Fm.; 3 – Ristola sp. cf. R. asparagus Jud, sample 2K-08, Late Berriasian, Pieniny Lst. Fm.; 4 – Ditrabs sansalvadorensis (Pessagno), sample 2K-12, latest Berriasian, Pieniny Lst. Fm.; 5 – Pseudoeucyrtis cf. sceptrum Jud, sample 2K-08, Late Berriasian, Pieniny Lst. Fm.; 6 – Obesacapsula gr. breggiensis-morroensis, sample 2K-16, Early Valanginian, Pieniny Lst. Fm.; 7 – Obesacapsula gr. polyedra (Steiger), sample K-19, Early-Mid Berriasian, Pieniny Lst. Fm.; 8 – Obesacapsula sp. gr. O. bullata Steiger, sample 2K-08, Late Berriasian, Pieniny Lst. Fm.; 9 – Mirifusus cf. apenninicus Jud, sample 2K-15, earliest Valanginian, Pieniny Lst. Fm.; 10 – Syringocapsa cf. limatum Foreman, sample £-22, Late Berria- sian, Pieniny Lst. Fm.; 11 – Stichomitra sp. aff. S. asymbatos Foreman, sample 2K-07, Late Berriasian, Pieniny Lst. Fm. MICROFOSSIL AND NANNOCONID STRTIGRAPHY 157 158 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI MICROFOSSIL AND NANNOCONID STRTIGRAPHY 159

Berriasian. In contrast, only two taxa were identified from sample 2K-10 (uppermost Berriasian); these are Tritrabs sp. (Fig. 11:1) and Eucyrtideillum sp. aff. E. pyramis (Aita) (Fig. 13: 1). The latter taxon is similar to E. pyramis (Aita), but this species was reported from the Tithonian only (Baumgartner et al., 1995a). (4) Twelve radiolarian taxa were identified in thin sections from samples 2K-12, 2K-15 and 2K-16 (Early Valanginian Calpionellites Zone – Fig. 5A). Radiolarians: Xitus (?) sp. gr. X. (?) alievi (Foreman) (Fig. 10: 5), Sethocapsa cf. uterculus (Parona) sensu Foreman (Fig. 10: 9), Ditrabs sansalvadorensis (Pessagno) (Fig. 11: 4), Mirifusus cf. apenninicus Jud (Fig. 11: 9) and Obesacapsula gr. breggiensis-morroensis are compared with the long-ranging taxa and, therefore, are not helpful in stratigraphic interpretation of this assemblage. (5) Seventeen radiolarian taxa are reported herein from samples (thin sections) 2K-44 and 2K-46 from the lower part of the Tintinnopsella Zone (Fig. 5A). The assemblage found in the latter sample ranges from Late Berriasian to Late Valangin- ian, whereas the age of the sample is probably “mid”-Valanginian. A characteristic taxon, Deviatus sp. gr. D. diamphidius s.l. (Foreman) (Fig. 12: 1), is known from Mid-Callovian to Late Berremian/Early Aptian (Baumgartner et al., 1995a). (5) Sample 2K-57 was taken from a prominent limestone bed 0.5 m thick in the middle part of the section (Figs 2: 2 and 5A). The identified radiolarian taxa suggest a Valanginian age of the sample (Tab. 1). Other microfossils and ammonites indicate a Late Valanginian age of the interval comprising the sampled bed. (6) Sample 2K-62: taxa identified in thin section suggest a Late Valangi- nian–Hauterivian age of the whole assemblage composed of 12 taxa identified in thin section. Occurrence of Ristola cf. martae Jud is consistent with this stratigraphic interval. However, Xitus cf. horridus Jud (Fig. 12: 6) suggests a Hau- terivian age of the limestone (Baumgartner et al., 1995a). Other radiolarians, some of them relatively well-preserved, as Syringocapsa sp. gr. S. limatum-longitubus – Fig. 13: 4, are less suitable for detailed stratigraphic interpretation because of their long-ranging occurrence. (7) Thirteen radiolarian taxa have been identified in sample 2K-66; the most important ones are shown in Tab. 1. Presence of Syringocapsa aff. spinosa (Squina- bol) suggests a Hauterivian age of this assemblage (cf. Baumgartner et al., 1995a).

Fig. 12. Valanginian–Hauterivian radiolarians from the Pieniny Limestone Formation, Branisko Succession, exposed in the Kapuœnica II section; scale bar = 100 µm (1–4, 6–11) or 50 µm (5). 1 – Deviatus sp. gr. D. diamphidius s. l. (Foreman), sample 2K-44, Valanginian; 2 – Deviatus diamphidius s. l. (Foreman), sample 2K-104, Hauterivian; 3 – Bistarkum irazuense (Aita), Kapuœnica II section, sample 2K-66, Hauterivian (?); 4 – Wrangellium (?) cf. columnum (Rüst), sample 2K-104, Hauterivian; 5 – Xitus sp. cf. X. channelli Jud, sample 2K-104, Hauterivian; 6 – Xitus cf. horridus Jud, sample 2K-62, Late Valanginian (?); 7 – Dictyomitra cf. pseudoscalaris (Tan) sensu Schaaf, sample 2K-104, Hauterivian; 8 – Pseudodictyomitra cf. carpatica (Lozyniak), sample 2K-104, Hauterivian; 9 – Stichocapsa cf. altiforamina Tumanda, sample 2K-102, Hauterivian; 10 – Ristola cretacea (Baumgartner), sample ZK-16, Late Valanginian–Early Hauterivian (?); 11 – Dibolachras sp. cf. D. tytthopora Foreman, sample ZK-15a, Late Valanginian (?) 160 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI

Fig. 13. Radiolarians identified in thin sections from the Pieniny Limestone Formation, Branisko Succession, exposed in the Kapuœnica II section. 1 – Eucyrtidiellum sp. aff. E. pyramis (Aita), sample 2K-10, latest Berriasian; 2 – Sethocapsa tricornis Jud, sample 2K-5, Late Berriasian; 3 – Wrangellium sp. gr. W. depressum-puga, sample 2K-08, Late Berriasian; 4 – Syringocapsa sp. gr. S. longitubus- limatum, sample 2K-62, Late Valanginian (?); scale bar = 100 µm

Other taxa, such as Bistarkum irazuense (Aita) (Fig. 12: 3), are less useful for stratigraphic dating of the sample under study. (8) Samples 2K-102 and 2K-104 were collected from the uppermost part of the Kapuœnica II section (Fig. 5B). Two taxa were identified from the former sample: Mirifusus cf. apenninicus Jud and Stichocapsa cf. altiforamina Tumanda (Fig. 12: 9). The most significant taxa identified in thin section from sample 2K-104 are shown in Tab. 1. The specimen identified as Dictyomitra cf. pseudoscalaris (Tan) sensu Schaaf (Fig. 12: 7) is close to D. pseudoscalaris known from Late Valangin- ian to Late Barremian/Early Aptian (Baumgartner et al., 1995a). Taxon Xitus cf. horridus Jud indicates a Hauterivian age of this sample, while presence of Pseudo- MICROFOSSIL AND NANNOCONID STRTIGRAPHY 161 dictyomitra cf. lanceloti Schaaf suggests that it may be post-Lower Hauterivian (Tab. 1). Therefore, the age of sample 2K-104 may correspond to the lower interval of Zone F3 proposed by Jud (1994), which was referred to Late Hauterivian–earliest Barremian (op. cit, fig. 25). Other taxa, such as Deviatus diamphidius s.l. (Fig. 12: 2), Wrangellium (?) cf. columnum (Rüst) (Fig. 12: 4), Xitus sp. cf. X. channelli Jud (Fig. 12: 5), and Pseudodictyomitra cf. carpatica (Lozyniak) (Fig. 12: 8), are stratigraphically less diagnostic. (8) A limestone fragment labelled MK-1 (collected from scree as shown in Fig. 5A) contained the ammonite Teschenites subflucticulus Reboulet and rare calpionellids assigned to Tintinnopsella carpathica (Murgeanu et Filipescu). Radiolar- ian assemblage found in that fragment consists of the following taxa: Mirifusus cf. odoghertyi Jud, M. cf. petzholdti (Rüst), Obesacapsula gr. bullata-polyedra, Setho- capsa cf. uterculus (Parona) sensu Foreman and Thanarla (?) sp. This assemblage may be Valanginian in age, because M. petzholdti is known from this stage, only (Baumgartner et al., 1995a, b). A Valanginian age of the sample is consistent with age of the ammonite, as T. subflucticulus is known from the Late Valangin- ian–Early Hauterivian (see below). Another ammonite, identified as Late Valang- inian Lytoceras lepidum (d’Orbigny), was also collected from scree, but above T. subflucticulus (Fig. 5A).

B. £ysonka section (Fig. 6) (1) Radiolarians identified in thin sections from the Lower Berriasian samples contain taxa that only poorly constrain age of limestones in the lower part of the section (Tab. 2): Triactoma cf. tithonianum Rüst (Fig. 10: 1), Parvicingula gr. boesii (Parona) (Fig. 10: 2), Archaeodictyomitra gr. apiarum-excellens (Fig. 10: 4) and Sethocapsa cf. dorysphaeroides Neviani sensu Schaaf (Fig. 10: 10) are given as ex- amples (cf. Baumgartner et al., 1995a). Some other taxa (Canoptum banale Jud – Fig. 10: 3, Cinguloturris gr. cylindra Kemkin et Rudenko, Pantanellium cf. berria- sianum Baumgartner, Obesacapsula sp. cf. O. rusconensis umbriensis Jud – Fig. 10: 8, and Sethocapsa cf. kitoi Jud – Fig. 10: 11 ) belong to a radiolarian assemblage of pre-Hauterivian age (op. cit.). Pantanellium sp. aff. P. cantuchapai Pessagno et Mc Leod (Fig. 10: 7) was reported from the latest Tithonian to Early Barremian (Baumgartner et al., 1995a). (2) Fifteen taxa were identified in sample £-22 from the £ysonka Marl Bed, although only six are listed in Tab. 2. The Late Berriasian–Early Valanginian age of the analysed assemblage is suggested by co-occurrence of the following taxa: Sethocapsa gr. kitoi Jud, Stichomitra aff. asymbatos Foreman and Parvicingula sphaerica Steiger. The radiolarians Obesacapsula cf. verbana (Parona) (Fig. 10: 6) and Syringocapsa cf. limatum Foreman (Fig. 11: 10) belong to long-range taxa (Tab. 2). Presence of Mirifusus sp. gr. M. petzholdti (Rüst) may suggest Valangin- ian age of the identified radiolarian assemblage (cf. Baumgartner et al., 1995a, b). However, the discussed sample contains calpionellids of the Oblonga Subzone; thus its Late Berriasian age is well established (Fig. 6). 162 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI MICROFOSSIL AND NANNOCONID STRTIGRAPHY 163

(3) Valanginian radiolarians occur in samples £-37, £-38 and £-40. Twenty one taxa were identified in these samples, but only 7 taxa are shown for samples £-37 and £-40 in Tab. 2. The sample £-40, which is the highest one collected in the £ysonka section, contains radiolarians consistent with the Late Valanginian age of the uppermost limestones exposed in this outcrop (Fig. 6). Ristola cretacea (Baum- gartner) and Syringocapsa vicetina (Squinabol) occur from the Tithonian to Late Valanginian, but are not reported from the latest Valanginian (Baumgartner et al., 1995a).

C. Zaskale section (Fig. 7) The taxon Dibolachras sp. cf. D. tytthopora Foreman (Fig. 12: 11 ) is the only one identified in thin section from the sample ZK-15a. It was reported from the Late Valanginian to Late Barremian/Early Aptian (UAZones 17–22, Baumgartner et al., 1995a). Radiolarians identified in sample ZK-16 are: Eucyrtis cf. columbaria Renz, Ristola cretacea (Baumgartner) and Xitus sp. aff. X. horridus Jud. The species R. cretacea (Baumgartner) (Fig. 12: 10) was reported from deposits not younger than lower Upper Valanginian, whereas E. columbaria is known from Lower Valangin- ian–Upper Barremian/Lower Aptian (Jud, 1994; Baumgartner et al., 1995a). In this radiolarian faunule, the specimen assigned to Xitus sp. aff. X. horridus Jud is the most “inconvenient” one, because X. horridus was reported from the Hauterivian, only (Jud, 1994; Baumgartner et al., 1995a, b). Perhaps, the specimen from the studied sample belongs to Late Valanginian forms similar to this taxon, or – alterna- tively – R. cretacea reaches the basal Hauterivian (?) in the Zaskale section. The first option seems to be more probable; in this case all the deposits of the Pieniny Limestone Formation exposed in the Zaskale outcrop may, in fact, belong to Upper Valanginian.

Nannofossils and nannoconid stratigraphy Nannoconus assemblages. Systematic position of nannofossils assigned to the genus Nannoconus Kamptner, 1931, is still uncertain, although different interpreta- tions have been proposed (cf. Deres and Achéritéguy, 1980; Busson and Noël, 1991; Kremer & KaŸmierczak, 2001). Some Nannoconus species (N. steinmannii Kamptner and N. colomii Lapparent) formed a rosette-like groups with a central cavity (Trejo, 1960; Deres and Achéritéguy, 1980), whereas N. abundans Stradner et Grün was found to occur as twin specimens (van Niel, 1995). Opinions concerning stratigraphic significance of nannoconids evolved during the past decades, from a very optimistic interpretation (Deres and Achéritéguy, 1980) to more realistic propositions (Bralower et al., 1989; Erba, 1989 etc.). In the Berriasian, one Nanno- conus zone and one subzone were introduced to the nannofossil zonation (Bralower et al., 1989, 1995). There is no zonal subdivision of the Tithonian based on nannoconids; however, some Nannoconus events were reported from this stage (Bra- lower et al., 1989; Erba, 1989; Tavera et al., 1994). 164 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI

Fig. 14. Berriasian nannofacies of the Pieniny Limestone Formation (Branisko Succession) in the £ysonka Klippe section. 1 – Nannomicrite with Ellipsogelosphaera keftalrempti Grün, in Grün and Allemann 1975 – at right, sample £-3, Lower Berriasian; 2 – Marly nannomicrite with Nannoconus kamptneri Brönnimann subsp. kamptneri Bralower, Monechi et Thierstein, 1989, emended (in the centre of the photograph), sample £-18, Lower Berriasian MICROFOSSIL AND NANNOCONID STRTIGRAPHY 165

Table 3 Nannoconids identified in samples of the Tithonian–Lower Valanginian limestones (Kapuœnica I and II sections, Pieniny Klippen Belt)

During the present study, the nannoconids were investigated in the Kapuœnica I and II sections and in the lower part of the £ysonka section. Some samples collected in the Zaskale section were also studied. The £ysonka section was selected to ana- lyse the Nannoconus assemblages because of (1) possibility to subdivide the Lower Berriasian interval and (2) relatively good preservation of nannofossils in limestones exposed in this outcrop (Fig. 14: 1–2). In the Kapuœnica I section, the Upszar Limestone Member (Czorsztyn Lst. Fm.) was studied to detect the early occurrences of Nannoconus in the Tithonian deposits. The first nannoconids (Nannoconus sp.) were found in sample K-1, whereas sample K-3 contained N. compressus Bralower et Thierstein (Fig. 15: 2 and Tab. 3). The latter taxon was reported by Bralower et al. (1989) from the Middle Tithonian, with its base (FO) in Chron CM21. Our sample K-3 is correlated with the Malmica Subzone, and therefore is Early Tithonian in age (Fig. 3). Bralower et al. (1989) and Ogg et al. (1991) placed the base of the Chitinoidella Zone in Chron M21n, thus FO 166 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI of N. compressus should correspond to the lower part of this chron or to Chron M21r. If this correlation is correct, appearance of N. compressus above the Cza- jakowa Radiolarite Formation (Fig. 3) may roughly be coeval with the FO of this taxon as defined by Bralower et al. (1989). Golonka and Sikora (1981) reported Nannoconus div. sp. from the uppermost part of “red and green radiolarites” (informal unit) at Stare Bystre – Potok Szeligowy (”Z³atne succession”). The next nannoconid event is related to the appearance of N. cf. wintereri Bra- lower et Thierstein, in the Chitinoidella Zone (sample K-10 in Tab. 3). The N. steinmannii minor Subzone (NKJ-D) was not documented and only the upper part of the N. steinmannii steinmannii Zone could be recognised in the Kapuœnica I section (Tab. 3). In this interval, N. steinmannii Kamptner subsp. minor Deres et Achérité- guy (Fig. 15: 8) occurs together with N. steinmannii Kamptner subsp. steinmannii Deres et Achéritéguy (Fig. 15: 9). In the Kapuœnica II section, the Late Berria- sian–Early Valanginian Nannoconus assemblage is rather monotonous in its composition, with N. steinmannii steinmannii, N. steinmannii minor and N. kamptneri kamptneri as the principal components (Tab. 3). All samples collected from the lower part of the £ysonka section (Fig. 6) were analysed to define a composition of the Nannoconus assemblage. The N. steinmannii minor Subzone was recognized in the lowermost interval of the section (Tab. 4). Conusphaera mexicana Trejo subsp. mexicana Bralower, Monechi et Thierstein (Fig. 15: 1), and Nannoconus sp. aff. N. infans Bralower (Fig. 15: 4) are also present in this part of the section. The N. steinmannii steinmannii Zone is distinguished from the sample £-15 upward, above an interval with N. steinmannii Kamptner subsp. minor Deres et Achéritéguy (Fig. 15: 5), N. kamptneri Brönnimann subsp. minor Bralower (Fig. 15: 6) and only occasional occurrences of N. sp. gr. N. steinmannii steinmannii. Within this interval, the LO of N. wintereri Bralower et Thier- stein is recorded. This species occurs beginning with the lowermost samples of this section (Fig. 15: 3, 7 and Tab. 4). According to Bralower et al. (1989), LO of N. wintereri was recorded within the N. steinmannii steinmannii Zone and directly below

Fig. 15. Conusphaera and nannoconids from the Tithonian–Berriasian limestones (Pieniny Limestone Formation, Branisko Succession) in the studied sections of the Pieniny Klippen belt. 1 – Conusphaera mexicana Trejo subsp. mexicana Bralower, Monechi et Thierstein, £ysonka Klippe section, sample £-1, Lower Berriasian; 2 – Nannoconus compressus Bralower et Thierstein, Kapuœnica I section, sample K-3, Lower Tithonian; 3 – N. wintereri Bralower et Thierstein, £ysonka Klippe section, sample £-1, Lower Berriasian; 4 – Nannoconus sp. aff. N. infans Bralower, £ysonka Klippe section, sample £-6, Lower Berriasian; 5 – N. steinmannii Kamptner subsp. minor Deres et Achéritéguy, £ysonka Klippe section, sample £-10, Lower Berriasian; 6 – N. kamptneri Brönnimann subsp. minor Bralower, £ysonka Klippe section, sample £-11, Lower Berriasian; 7 – N. wintereri Bralower et Thierstein, £ysonka Klippe section, sample £-10, Lower Berriasian; 8 – N. steinmannii Kamptner subsp. minor Deres et Achéritéguy, Kapuœnica I section, sample K-25, Middle Berriasian; 9 – N. steinmannii Kamptner subsp. steinmannii Deres et Achéritéguy, Kapuœnica I section, sample K-25, Middle Berriasian; 10, 11 – N. kamptneri Brönnimann subsp. kamptneri Bralower, Monechi et Thierstein, emended, £ysonka Klippe section (10 – sample £-17, 11 – sample £-16), Lower Berriasian; 12 – N. broennimanni Trejo, £ysonka Klippe section, sample £-13, Lower Berriasian MICROFOSSIL AND NANNOCONID STRTIGRAPHY 167 168 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI

Table 4 Nannoconids identified in samples of the Lower Berriasian limestones (£ysonka section, Pieniny Klippen Belt)

TAXA i i n n a m s n i u e s t Nannoconus s i s i

e r i r n i o i p

n zonation n r n a i i n m e r i r a o m

n (after Bralower m i e s t

o c n r r m i n i p m n . i o e n i e f a t o

i et al ., 1989 and n t n i f m f l i n e s m n n n a i a

o i i i a m k n s

c i i

Bralower et al .,

i a . i . m n n s s r r N n n N n m N u e u e i . i 1995) a a . f n n n n e n . t t t r o o f m f m n s p p c g c c a n n e .

i i o . o . m . m f o e e f n r p n p a p a t t a s s s n k s b n k s

a . . . a ...... N N N N N N N N N N SAMPLES N £-18 N. steinmannii £-17 steinmannii Zone £-16 (NK1 - lower part) £-15 £-14 £-13 (?) £-12 £-11 £-10 N. wintereri £-9 £-8 £-7 £-6 ? N. steinmannii £-5 minor Subzone (NJKD) £-4 £-3 £-2 £-1 MICROFOSSIL AND NANNOCONID STRTIGRAPHY 169

Fig. 16. Calcareous nannofossils from the Lower Berriasian limestones of the Pieniny Limestone Formation (Branisko Succession) in the £ysonka Klippe section. 1 – Rotelapillus laffittei (Noël), sample £-6; 2 – Diazomatolithus sp., sample £-12; 3 – Watznaueria barnesae (Black) Perch-Nielsen, sample £-10; 4 – Bidiscus ignotus (Górka) Hoffman, sample £-7; 5 – Ellipsagelosphaera britannica (Stradner) Perch-Nielsen, sample £-7; 6 – Ellipsagelosphaera keftalrempti Grün in Grün and Allemann 1975, sample £-7; 7 – Cruciellipsis cuvillieri (Manivit) Thierstein, sample £-5; 8 – Biscutum ellipticum (Górka) Grün and Allemann 1975, sample £-6; 9 – Cyclagelosphaera margereli Noël (coccosphere), sample £-6 170 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI the Elliptica Subzone. Our LO of N. wintereri appears to be placed also below the Elliptica Subzone. Therefore, it is possible that the uncertain interval between the NJKD and NK1 zones (Tab. 4) belongs, in fact, to the latter nannoconid zone. This interpretation may be strengthened with an almost continuous occurrence of N. kamptneri Brönnimann subsp. kamptneri Bralower, Monechi et Thierstein, emended (Fig. 15: 10–11) from sample £-10 upward (Tab. 4). The species N. broennimanni Trejo (Fig. 15: 12) was also recorded in the discussed interval though in one sample, only. In the Zaskale section (Fig. 7), the Nannoconus assemblage is also dominated by the taxa: Nannoconus steinmannii steinmannii, N. steinmannii minor and N. kamptneri kamptneri, sometimes with N. colomii. This assemblage is consistent with the Late Valanginian to earliest Hauterivian ? age of the deposits exposed in the section. Other nannofossil taxa. Other nannofossils were not investigated systemati- cally, as their presence was recorded only occasionally during the SEM study of nannoconids (as Conusphaera mexicana mexicana reported above). The observed nannofossils belong mainly to taxa most resistant to diagenetic transformations. All figured specimens (Fig. 16: 1–9) were recorded in samples collected from the £ysonka Klippe, because of better preservation of calcareous nannoplankton in this section. Rotelapillus laffittei (Noël) (Fig. 16: 1) was recorded in sample £-6 (Fig. 6). This taxon is the index species of the R. laffittei Subzone (NJK-C) established across the J/K boundary (Bralower et al., 1989), but in the £ysonka section it was found in the Early Berriasian N. steinmannii minor Subzone (NJK-D). Diazomato- lithus sp. (Fig. 16: 2) occurs in sample £-12; the figured specimen is similar to D. subbeticus Grün in Grün et Allemann (1975) known from Late Tithonian to Valanginian. Watznaueria barnesae (Black) Perch-Nielsen (Fig. 16: 3), Bidiscus ignotus (Górka) Hoffman (Fig. 16: 4), Ellipsagelosphaera britannica (Stradner) Perch-Nielsen (Fig. 16: 5), E. keftalrempti Grün in Grün and Allemann (1975) (Fig. 16: 6), Biscutum ellipticum (Górka) Grün and Allemann (Fig. 16: 8) and Cyclage- losphaera margereli Noël (Fig. 16: 9) are the long-ranging taxa. The species Cru- ciellipsis cuvillieri (Manivit) Thierstein (Fig. 16: 7) was reported from the latest Ti- thonian–Late Hauterivian (Grün and Allemann, 1975; Bralower et al., 1989). In summary, the recorded nannofossil occurrences are too sparse to form a basis for any improvement of the stratigraphic subdivision of the Pieniny Limestone Forma- tion in the studied sections. Nevertheless, our observations indicate that a separate study of calcareous nannoplankton is possible to carry out, especially in the £ysonka section.

AMMONITE STRATIGRAPHY All collected ammonites are preserved as internal moulds, only. Such a state of ammonites preservation may indicate that the deposits of the Pieniny Limestone Formation accumulated below the aragonite compensation depth (ACD). The specimens of the genera Lytoceras and Phylloceras represent an important part of MICROFOSSIL AND NANNOCONID STRTIGRAPHY 171

Table 5 Selected ammonites found in the studied sections of the Branisko Succession compared with the ammonite and calpionellid zonations and ammonite assemblage from the Pieniny Klippen Belt in Slovakia; CALPION. ZONES = calpionellid zones and subzones after Remane et al. (1986) and Grün & Blau (1997)

STAGES HOEDEMAEKER ET AL. (2003) CAL- AMMONITES FROM AMMONITES FROM AND SUB- Ammonite Ammonite PION. PKB IN POLAND PKB IN SLOVAKIA STAGES zones subzones ZONES (THIS PAPER) (VASICEK, 1997, 2002) P. ohmi R E N P

A B. balearis P I (?) U P. ligatus V I S. sayni

R Subsaynella sayni

E Olcostephanus sp.

T L. nodosoplicatum Neolissoceras R U

E desmoceratoides

A Crioceratites nolani W A

H C. loryi L O Crioceratites loryi L L

A. radiatus E Lytoceras subfimbriatum S O. densicostatus Olcostephanus cf. detonii C. furcillata P C. furcillata C. furcillata O Himantoceras trinodosum N R

N Teschenites

A Neocomites praediscus E I N. peregrinus N subflucticulus P I N

P Protetragonites

T Valanginites nucleus I

U quadrisulcatus N

G Bochianites neocomiensis S. verrucosum I Neolissoceras cf. N T Neocomites teschenensis grasianum A Neolissoceras cf. grasianum R L Bochianites oosteri E B. campylotoxus A CALPIO- W V NELLI- O

L T. pertransiens TES

S Tirnovella cf. otopeta T. otopeta I S P a O

g Neolissoceras R L n E L salinarium o E

P S. boissieri l N

b Berriasella cf. callisto P N O o I U

A Elenaella cf. P I L subcularense A S

C simp. A . E I h c A L s R i L d D R L S. occitanica a D E C E I a N B c i M t O p i I l l R e P E a L Dalmasiceras cf. n

W B. jacobi i A p O l

C djanelidzei L a the collected ammonites. Chert nodules and interbeds common in the discussed formation were interpreted as siliceous horizons that originated as a result of early- diagenetic transformations of pelagic calcareous-siliceous ooze (Kasiñski et al., 1981). Occurrence of silicified moulds of ammonites in the Zaskale section, in the Criosarasinella furcillata Zone, seems to confirm this interpretation. We follow the ammonite zonation recently published by Hoedemaeker et al. (2003), shown in Table 5. Tithonian. A juvenile ammonite identified as ?Protancyloceras sp. was found in thin section from sample K-6. This is the only ammonite found in the Tithonian limestones of the Upszar Limestone Member in the Kapuœnica I section. Berriasian. The oldest Berriasian ammonite – Phylloceras sp. ex. gr. P. serum (Oppel) – was collected from scree in the Kapuœnica I section; it derived from basal 172 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI part of the Pieniny Limestone Formation (Fig. 3). This species is known to occur in the Tithonian and Early Berriasian (Sapunov, 1979). Berriasian ammonites were also found in the uppermost interval of the lower part of the £ysonka section (Fig. 6, samples £-17 and 18). The following taxa have been identified: Dalmasiceras cf. djanelidzei Mazenot (Fig. 17: 7), Berriasella (Berriasella) ex. gr. B. moreti Maze- not (Fig. 18: 2), Neolissoceras grasianum (d’ Orbigny) (Fig. 18: 10, 11 ; 19: 3, 6, 8), Leptoceras ex gr. jelevi Nikolov (Fig. 19: 1), ?Jabronella sp., Berriasella sp., Ele- naella cf. subcularense Nikolov (Fig. 17: 3) and Holcophylloceras cf. calypso (d’Orbigny) (Fig. 20: 2). The aptychi comprise two taxa: Lamellaptychus trauthi Renz & Habicht (Fig. 18: 8) and Lamellaptychus ex. gr. herthae (Winkler) (Fig. 17: 12). This fauna indicates the Berriasella jacobi Zone and correlates with the Alpina Subzone in the calpionellid scheme (Fig. 6). Punctaptychus cinctus Trauth (Fig.19: 7) was collected from a lower part of the Calpionellopsis Zone (Simplex Subzone). Presence of the Tirnovella otopeta Zone was documented in the Kapuœnica II (Fig. 5A) and £ysonka sections (Fig. 6). This zone corresponds to the Calpionellop- sis Standard Zone (Oblonga Subzone). In the first section, the T. otopeta Zone is represented by Tirnovella cf. otopeta Thieuloy (Fig. 19: 4), and in the second one by Phyllopachyceras ex. gr. beneckei Zittel (Fig. 18: 5), Neolissoceras salinarium Uh- lig (Fig. 17: 9) and Protetragonites sp. Valanginian–Early Hauterivian. An ammonite assemblage composed of: Ly- toceras lepidum (d’Orbigny) (Fig. 17: 2; Fig. 18: 4, 7, 9), Lytoceras sp., Protetrago- nites quadrisulcatus (d’Orbigny) (Fig. 17: 4; Fig. 18: 6; Fig. 19: 5), Neolissoceras grasianum (d’Orbigny) (Fig. 17: 11 ), Teschenites cf. subflucticulus Reboulet (Fig. 18: 12), and Pseudobelus ex. gr. bipartitus (Oppel), was identified in the Kapuœnica II section (Fig. 5A), along with Lamellaptychus sp. The ammonites are assigned to the Late Valanginian Criosarasinella furcillata Zone (Hoedemaeker et al., 2003), previously Himantoceras trinodosum Zone (cf. Reboulet, 1995), which is correlated herein with the lower part of the calpionellid Tintinnopsella Zone. The C. furcillata Zone was found also in the lower part of the Zaskale section (Fig. 7). There, this zone is represented by the following ammonites: Phylloceras (Hypophyllo- ceras) thetys (d’ Orbigny), Protetragonites quadrisulcatus (d’ Orbigny) (Fig. 17: 4; Fig. 18: 6), Criosarasinella furcillata Thieuloy (Fig. 17: 1, 5, 6, 8, 13), ?Karaka- schiceras sp. (Fig. 17: 10), Olcostephanus (Olcostephanus) densicostatus (Weg- ner) (Fig. 18: 3) oraz Pseudobelus ex. gr. bipartitus Blainville (Fig. 20: 4). The ammonites and aptychus collected from the higher part of this section, namely Pro- tetragonites ex. gr. quadrisulcatus (d’Orbigny), Olcostephanus sp. and Lamellap- tychus sp., are known from the Late Valanginian and Early Hauterivian. Vašíèek (1997) described ammonites collected from the Pieniny Limestone Formation in the Slovak part of the Pieniny Klippen Belt. His faunal list contains the following taxa of the Late Berriasian–Valanginian age (selected taxa are shown in Tab. 5): Partschiceras winkleri (Uhlig), Phylloceras (Hypophylloceras) ex. gr. thetys (d’ Orbigny), Protetragonites quadrisulcatus (d’Orbigny), Neolissoceras grasianum (d’Orbigny), Neocomites platycostatus (Sayn), Neocomites teschenensis (Uhlig), N. praediscus Reboulet, Jeanthieuloites cf. quinquestriatus (Besaire), MICROFOSSIL AND NANNOCONID STRTIGRAPHY 173

Fig. 17. Ammonites of the Pieniny Limestone Formation in the Branisko Succession (Pieniny Klippen Belt, Poland). 1, 5, 6, 13 – Criosarasinella furcillata Thieuloy [1 – ZK-8/3a, × 0.6; 5 – ZK-8/3, × 0.6; 6 – ZK-8/3b, × 0.9; 13 – ZK-8/3c, × 0.6], Zaskale section; 2 – Lytoceras lepidum (d’Orbigny); [£-38], £ysonka section, × 0.4; 3 – Elenaella cf. subcularense Nikolov [10b/2K-1], Kapuœnica II section, × 0.8; 4 – Protetragonites quadrisulcatus (d’Orbigny) [ZK-(R)], Zaskale section, × 0.6; 7 – Dalmasiceras cf. djanelidzei Mazenot [£-17/5], £ysonka section, × 0.6; 8 – Criosarasinella furcillata Thieuloy [ZK-8/2], Zaskale section, × 0.8; 9 – Neolissoceras salinarium (Uhlig) [£-23-32], £ysonka section, × 1.4; 10 – ?Karakaschiceras sp. [ZK-9], a whorl fragment, C. furcillata Zone (cf. Fig. 7), Zaskale section, × 0.9; 11 – Neolissoceras grasianum (d’Orbigny) [2K-71/72], Kapuœnica II section, × 0.7; 12 – Lamellaptychus ex. gr. herthae (Winkler) [£17-1], £ysonka section, × 1.2 174 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI MICROFOSSIL AND NANNOCONID STRTIGRAPHY 175

Olcostephanus cf. detonii (Rodighiero), Olcostephanus sp., Valanginites nucleus (Roemer), Oostrella ex. gr. gaudryi (Nickles), Himantoceras trinodosum Thie- uloy, Bochianites neocomiensis (d’Orbigny), and B. oosteri Sarasin et Schoendel- mayer. From the Lower Hauterivian strata, this author (op. cit.) has described the taxa: Lytoceras subfimbriatum (d’ Orbigny), Neolissoceras grasianum (d’Or- bigny), Teschenites flucticulus Thieuloy, Spitidiscus cf. rotula (Sowerby), Criocer- atites loryi Sarkar, C. nolani (Kilian), Abrytusites thieuloi Vašíèek et Michalík, Bo- chianites oosteri Sarasin et Schoendelmayer and Olcostephanus (Jeannoticeras) jeannoti (d’Orbigny). The Late Hauterivian ammonites comprise: Subsaynella sayni (Paquier) and Crioceratites ex. gr. duvali Léveillé. The abovementioned faunal lists were completed with the recently published taxa (Vašíèek, 2002): Oostrella ondulata Reboulet (Late Valanginian–basal Hau- terivian), Neolissoceras desmoceratoides (Wiedmann), Jeanthieuloites nodosus (Mandov), ?Eleniceras transsylvanicum (Jekelius), Sarasinella sp., Eleniceras nikolovi Breskovski and Abrytusites julianyi (Honnorat-Bastide) of Early Hau- terivian age, and ?Pseudothurmannia “binelli” Thomel (latest Hauterivian).

Systematic description

Ammonites All specimens of ammonites described here are housed in the Institute of Geo- logical Sciences, Polish Academy of Sciences (00-818 Warsaw, Twarda 51/55, Po- land). In descriptions of the ammonites, classification of the Jurassic Ammonoidea proposed by Arkell (1950) and Arkell et al. (1957) was adopted. Synonymy lists for particular species include reference to the figured type specimens and those of recent papers which present a wider list of references. The collection of Lower Creta- ceous ammonites studied consists of about 25 specimens, of which 15 better preserved ones were determined to specific level.

Ammonite shell measurements (in mm): D – maximum diameter; H – whorl height; E – whorl width; O – umbilical width; H/D – whorl height/shell diameter (in percentages); H/E – whorl height/ whorl width (in percentage); O/D – umbilical diamenter/shell diameter (in percentage); R – primary ribs number on the last whorl; R/2 – primary ribs number on the half last whorl; r – secondary ribs number on the last whorl; r/2 – secondary ribs number on the half last whorl, No – specimen number.

Fig. 18. Ammonites and aptychus from the Pieniny Limestone Formation in the Branisko Succe- ssion (Pieniny Klippen Belt, Poland). 1 – Olcostephanus sp. [MK-8], Kapuœnica II section, × 0.5; 2 – Berriasella (Berriasella) sp. ex. gr. B. moreti Mazenot [£-17], £ysonka section, × 1; 3 – Olcoste- phanus (Olcostephanus) densicostatus (Wegener) [ZK-10-14], Zaskale section, × 0.7; 4, 7, 9 –Lytoceras lepidum (d’ Orbigny) [4, 9 – MK-3, Kapuœnica II section, × 0.7; 7 – £-38, £ysonka section, × 0.9]; 5 – Phyllopachyceras sp. ex gr. P. beneckei (Zittel), £-23-32, £ysonka section, × 0.8; 6 – Protetragonites quadrisulcatus (d’Orbigny) [A-12, Kapuœnica II section, × 0.5]; 8 – Lamellaptychus trauthi Renz et Habicht [£-6], £ysonka section, × 0.9; 10, 11 – Neolissoceras grasianum (d’Orbigny) [10 – MK-9, × 0.9; 11 – 2K-71-72, Kapuœnica II section × 1]; 12 – Teschenites cf. subflucticulus Re- boulet [£-36-1], £ysonka section, × 1.5; 13 – ?Malbosiceras sp. [MK-15], Kapuœnica II section, × 1.5 176 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI MICROFOSSIL AND NANNOCONID STRTIGRAPHY 177

Order Ammonoidea Zittel, 1884 Suborder Phylloceratina Arkell, 1950 Family Phylloceratidae Zittel, 1884 Subfamily Calliphylloceratinae Spath, 1927 Genus Holcophylloceras Spath, 1927 Type species: Phylloceras mediterraneum Neumayr, 1871

Holcophylloceras cf. calypso (d’Orbigny, 1841) (Fig. 20: 2) cf. 1995 Salfeldiella (Gyrophyllites) calypso (d’Orbigny); Reboulet, p. 187, pl. 35, fig. 7 1997 Sowerbyceras (Holcophylloceras) calypso (d’Orbigny); Vašíèek, p. 233 1999 Holcophylloceras calypso (d’ Orbigny); Vašíèek et al., p. 628, pl. 1, fig. 5 Material: One incomplete specimen (£-18-3, H = 25 mm). Description and remarks: Fragment of whorl with convex whorl side and strong, prorsiradiate constrictions. The specimen from the Pieniny Klippen Belt agrees well with description and ammonites listed in the synonymy but incomplete preservation of the specimen precludes its identification with certainty. Occurrence: The specimen was found in the Pieniny Limestone Formation at £ysonka section. The species Holcophylloceras calypso (d’Orbigny), which is similar to our specimen is known from the Late Tithonian ?, Berriasian and Early Valanginian ? (Reboulet, 1995).

Subfamily Phyllopachyceratinae Collignon, 1937 Genus Phyllopachyceras Spath, 1925 Type species: Ammonites infundibulum d’Orbigny, 1840

Phyllopachyceras sp. ex. gr. P. beneckei (Zittel, 1868) (Fig. 18: 5) Material: One small, incomplete specimen (£-23-32/1, H = 12 mm). Description and remarks: Fragment of whorl with flat, weakly convex whorl side, rounded ventral margin and deep constriction. Incomplete preservation of the

Fig. 19. Ammonites and aptychus from the Pieniny Limestone Formation, Branisko Succession (Pieniny Klippen Belt, Poland). 1 – Leptoceras ex. gr. jelevi Nikolov [2K-09], Kapuœnica II section, × 1.8; 2 – Teschenites subflucticulus Reboulet [MK-1], Kapuœnica II section, × 1.2; 3, 6 – Neolisso- ceras grasianum (d’Orbigny) [3 – £-36/3, £ysonka section, × 1; 6 – MK-6, Kapuœnica section, × 0.9]; 4 – Tirnovella cf. otopeta Thieuloy [2K-9], Kapuœnica II section, × 0.9; 5 – Protetragonites quadrisulcatus (d’ Orbigny) [Z 1/15], Zaskale section,× 1; 7 – Punctaptychus cinctus Trauth [£-17], £ysonka section, × 0.8; 8 – Neolissoceras grasianum (d’Orbigny) [8 – MK-7], Kapuœnica II section, × 1.2 178 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI

Fig. 20. Ammonites and belemnite of the Pieniny Limestone Formation in the Branisko Succession (Pieniny Klippen Belt, Poland). 1 – Neolissoceras desmoceratoides (Wiedmann) [2K-100], Kapuœnica II section, × 1.2; 2 – Holcophylloceras cf. calypso (d’ Orbigny) [£-18-3], £ysonka section, × 0.4; 3 – Berriasella (Berriasella) cf. callisto (d’Orbigny) [2K-09c], Kapuœnica II section, × 1.4; 4 – Pseudobelus ex. gr. bipartitus Blainville [ZK-3], Zaskale section, × 1.4 specimen precludes its identification with certainty. Whorl shape and presence of constriction on the ventral side seem similar to those of Phyllopachyceras from Ph. beneckei (Zittel, 1868) group (see Khimshiashvili, 1976, p. 60, pl. 1, fig. 4; Reboulet, 1995; p. 186, pl. 35, figs 1-6). Occurrence: The specimen was found in the Valanginian part of the Pieniny Limestone Formation at £ysonka section. The species Phyllopachyceras beneckei (Zittel, 1868) is known from the Tithonian to Valanginian (Reboulet, 1995).

Suborder Lytoceratina Hyatt, 1889 Superfamily Lytocerataceae Neumayr, 1875 Family Lytoceratidae Neumayr, 1975 Subfamily Lytoceratinae Neumayr, 1875 Genus Lytoceras Suess, 1865 Type-species: Ammonites fimbriatus Sowerby, 1817

Lytoceras lepidum (d’Orbigny, 1841) (Fig. 17: 2; Fig. 18: 4, 7, 9) 1986 Lytoceras subfimbriatum (d’Orbigny); Vašíèek & Michalik, p. 453, pl. 4, fig. 1 1995 Lytoceras lepidum (d’Orbigny); Reboulet, p. 192, pl. 38, figs 1-4 Material: Three specimens: MK-3, £-38, ZK-9/1. MICROFOSSIL AND NANNOCONID STRTIGRAPHY 179

Dimensions:

No D (mm) H (mm) O (mm) H/D (%) O/D (%) MK-3 ? 63 29 34 ? 46 ? 53 £-38 75 25 35 33 46 ZK-9/1 30

Description: Shell evolute with elliptical cross-section, sides convex. Umbilicus wide and shallow, with steep walls. Ornamentation consisting of numerous, simple, thin ribs curved prosiradiately at the umbilicus. In inner whorls, ribs are more loosely spaced. On the last whorl ribs are more closely spaced and situated between collars of lytoceratid type. Suture line not preserved. Remarks: The specimens resembles Lytoceras lepidum (d’Orbigny) as described and illustrated by authors cited in the synonymy. Occurrence: Specimen MK-3 was found in a limestone fragment from the Pieniny Limestone Formation in the middle part of the Kapuœnica II section. Specimen £-38 was collected from the Pieniny Limestone Formation at £ysonka section. Specimen ZK-9/1 was found in the Pieniny Limestone Formation at Zaskale section. The species Lytoceras lepidum (d’Orbigny) is known from the Upper Valanginian strata of south-east France (Reboulet, 1995).

Protetragonites quadrisulcatus (d’Orbigny, 1841) (Fig. 17: 4; Fig. 18: 6; Fig. 19: 5) 1901 Lytoceras quadrisulcatum (d’Orbigny); Sayn, p. 2, pl. 1, fig. 1a-b 1964 Protetragonites quadrisulcatus (d’Orbigny); Fülöp, p. 162, pl. 16, fig. 4; p. 178,pl. 24, fig. 2 1987 Protetragonites quadrisulcatus (d’Orbigny); Immel, p. 62, pl. 2, fig. 3 1995 Lytoceras quadrisulcatum (d’Orbigny); Reboulet, p. 191, pl. 38, figs; 8 2002 Protetragonites quadrisulcatus (d’Orbigny); Vašíèek, p. 195 Material: Six specimens. Dimensions:

No D (mm) H (mm) O (mm) H/D (%) O/D (%) A-12 41 12 18 29 43 Z-1/15 50 15 23 30 46 MK-4 18 6 8 33 44 ZK-(R) 49 17 26 35 46 ZK-14 65 20 39 30 44 £-36-2 19 6 10 31 52

Description: Shell evolute with slightly rounded side and steeply inclined umbilical wall. Umbilicus wide and shallow. Whorls smooth with four constrictions slightly inclined forward, but not pronounced. 180 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI

Remarks: All specimens agree well with description of ammonites listed in the synonymy. Other similar species of this genus have more constrictions on the whorl. Occurrence: Specimens A-12 and MK-4 were found in the Kapuœnica II section of the Pieniny Limestone Formation, four specimens were found in the Zaskale section of the same formation.

Superfamily Haplocerataceae Zittel, 1884 Family Haploceratidae Zittel, 1884 Genus Neolissoceras Spath, 1923 Type species: Ammonites grasianus d’Orbigny, 1841

Neolissoceras grasianum (d’Orbigny, 1841) (Fig. 17: 11 ; Fig. 18: 10, 11; Fig. 19: 3, 6, 8) 1960 Haploceras grasianum (d’Orbigny); Drushchits, p. 268, pl. 13, fig 6 1964 Neolissoceras grasianum (d’Orbigny); Fülöp, pl. 13, fig. 2 1967 Neolissoceras grasianum (d’Orbigny); Dimitrova, p. 85, pl. 42, fig. 2 1987 Haploceras (Neolissoceras) grasianum (d’Orbigny); Immel, p. 67; pl. 3, fig. 1 1992 Neolissoceras grasianum (d’Orbigny); Wierzbowski & Remane, pl. 3, fig. 7 1995 Neolissoceras grasianum (d’Orbigny); Reboulet, p. 164, pl. 34, figs 1-14 Material: Seven specimens and four fragments of shell, MK-10 (H = 15 mm); MK-11 mm (H = 11 mm); ZK-1-2 (H = 15 mm); £-17/3 (H = 15 mm). Dimensions:

No D (mm) H (mm) O (mm) H/D (%) O/D (%) MK-5 26.5 11.5 5 43 19 MK-6 22 9 6.5 41 29 MK-7 29 12 10 41 34 MK-9 28 12 7 42 25 £-36/3 25 12 5 48 20 A-13 32 15 9 46 28 2K-71-72 26 8.5 8 32 30

Description: Shell small-sized, moderately involute, with sub-rectangular whorl section and flat sides slightly inclined towards umbilicus. Ventral side rounded, slightly flattened. Distinct umbilical margin rounded. Umbilical wall inclined. Umbilicus wide and deep. Ornamentation absent. Suture line obscured. Remarks: Our specimens agree well with description of ammonites listed in the synonymy. They differ from the subspecies Haploceras (Neolissoceras) grasianum subgrasianum Drushchits, 1960 (see Drushchits, 1960, p. 268, pl. 13, figs 4-5, text-fig. 74; Cecca et al., 1998, p. 69, pl. 1, fig 19-20, text-fig. 7) by wider umbilicus (19–34%) and slightly lower whorls (41–46%). MICROFOSSIL AND NANNOCONID STRTIGRAPHY 181

Occurrence: The specimens with symbols “MK” and “A-13” were found in the Upper Berriasian deposits of the Kapuœnica II section of the Pieniny Limestone Formation. Specimen £-36/3 was found in the Valanginian limestones of the Pieniny Limestone Formation in the £ysonka section. The species Neolissoceras grasianum (d’Orbigny) is known from the Berriasian of Mediterranean Europe (Immel, 1987) and Valanginian–Lower Hauterivian of south-east France. This taxon disappears in the Late Hauterivian (Reboulet, 1995).

Neolissoceras desmoceratoides (Wiedmann, 1966) (Fig. 20: 1) 1994 Haploceras (Neolissoceras) desmoceratoides Wiedmann; Vašíèek et al., p. 56-57, pl. 8, fig. 3 2002 Neolissoceras desmoceratoides Wiedmann; Vašíèek, p. 188, pl. 2, fig. 3 Material: One specimen (2K-100). Dimensions:

No D (mm) H (mm) O (mm) H/D (%) O/D (%) 2K-100 40 19 8.5 47 21

Description: Shell medium-size, moderately involute, with subrectangular whorl section and flat sides without ornamentation. Ventral side and umbilical margin rounded. Umbilical wall inclined. Umbilicus moderately wide. Suture line obscured. Remarks: The specimen from the Pieniny Klippen Zone agrees well with description and figures presented by Vašíèek et al. (1994) and Vašíèek, 2002 (with synonymy). Occurrence: The specimen was found in the uppermost part of the Kapuœnica II section (Pieniny Limestone Formation, Hauterivian). The species Neolissoceras desmoceratoides (Wiedmann) was cited from the Late Valanginian of Spain and Rumanian Carpathians, Late Valanginian and Hauterivian of Bul- garia, and basal Hauterivian of the Pieniny Klippen Belt (Vašíèek, 2002).

Neolissoceras salinarium (Uhlig, 1888) (Fig. 17: 9) 1987 Haploceras (Neolissoceras) salinarium Uhlig; Immel, p. 67, pl. 3, fig. 2 1995 Neolissoceras salinarium (Uhlig); Reboulet, p. 164, pl. 34, figs 1-14 Material: One incomplete specimen (£-23-32). Dimensions:

No D (mm) H (mm) O (mm) H/D (%) O/D (%) £-23-32 15 7 3.5 46 23

Description: Shell small-sized, moderately involute with sub-rectangular whorl section and slightly convex sides. Ventral margin rounded. Venter side narrow, 182 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI rounded, with clear keel in middle part. Umbilical margin slightly rounded. Umbilical wall inclined. Umbilicus narrow, deep. Ornamentation absent. Remarks:. Specimen is consistent with descriptions and illustrations as given in the synonymy. Occurrence: The specimen was found in the interval between the limestone beds £-23 and 32 at £ysonka section (Pieniny Limestone Formation). The species Neolissoceras salinarium (Uhlig) occurs in Early Valanginian (Pertransiens and Campylotoxus Zones), sometimes is present also at base of Late Valanginian (Verrucosum Zone – see Reboulet, 1995).

Suborder Ancyloceratina Meek, 1876 Family Ancyloceratidae Gill, 1871 Genus Leptoceras Uhlig, 1883 Type species: Leptoceras brunneri (Ooster, 1860)

Leptoceras ex. gr. jelevi Nikolov, 1956 (Fig. 19: 1) ex gr. 1939 Leptoceras sp. ind.; Mazenot, p. 295, pl. 40, fig. 2 1967 Protoleptoceras jelevi jelevi Nikolov; Dimitrova, p. 34, pl. 12, fig 2, 3 1977 ?Leptoceras (Protoleptoceras) cf. jelevi (Nikolov, 1967); Myczyñski, p. 153, pl. 4, fig. 6 Material: One fragmentarily preserved specimen 2K-09 (10a); H = 5 mm. Description and remarks: One fragment of whorl with oval cross-section and strong, simple, perpendicular ribs. Inter ribs spaces wider than ribs. Our specimen is similar to the species Leptoceras jelevi Nikolov, 1956 described and illustrated in the synonymy; its fragmentary preservation does not permit its specific identification without reservation. Wiedmann (1973 p. 310) suggested that the genus Protoleptoceras proposed by Nikolov (1966) ought to be included to Protancyloceras Spath, 1927, but Avram (1999, p. 31) identified Nikolov’s genus as younger synonym of the genus Leptoceras Uhlig, 1883. Occurrence: Our specimen was found in the lower part of the Pieniny Limestone Formation at Kapuœnica II section (see Fig. 5A). The species Leptoceras jelevi Nikolov, 1956, was described from the Berriasian of Southern France and Bulgaria (Dimitrova, 1967). MICROFOSSIL AND NANNOCONID STRTIGRAPHY 183

Superfamily Perisphinctaceae Steinmann, 1890 Family Berriasellidae Spath, 1922 Subfamily Berriasellinae Spath, 1922 Genus Berriasella Uhlig, 1905 Subgenus Berriasella Uhlig, 1905 Type species: Ammonites privasensis Pictet, 1867

Berriasella (Berriasella) cf. callisto (d’Orbigny, 1847) (Fig. 20: 3) cf. 1967 Berriasella callisto (d’Orbigny); Dimitrova, p. 101, pl. 48, fig. 6 1982 Berriasella callisto (d’Orbigny); Nikolov, p. 58, pl. 11, figs 5, 6; pl. 12, figs 1-6; pl. 13, figs 1-3 1985 Berriasella callisto (d’Orbigny); Tavera, p. 255, pl. 35, figs 7-7; Text-fig. 11/N 1999 Berriasella (Berriasella) callisto (d’Orbigny); Vašíèek et al., p. 632, pl. 3, fig. 3 Material: One incomplete specimen, 2K-09c (H = 12, O = 14). Description and remarks: Shell of small size, with wide and shallow umbilicus, with moderately rapid increment of whorls. Sides slightly convex. Ornamentation consists of slightly prorsiradiate, bifurcate and trifurcate ribs. Ribs weak, dense on the internal whorls, robust and separate on external ones. Form of whorls and ornamentation are similar to the species Berriasella (Berriasella) callisto (d’Orbigny) as presented in the synonymy. Poor and fragmentary preservation of our specimen precludes its exact specific identification. Occurrence: The specimen was found in the lower part of the Pieniny Limestone Formation at Kapuœnica II section (cf. Fig. 5A). The species Berriasella (Berriasella) callisto (d’Orbigny) is known from Late Berriasian (Fauriella boissieri Zone) of Southern France, Spain, Italia, Bulgaria, and from base of the Tirnovella otopeta Zone of Southern France (see Tavera, 1985 and Vašíèek et al., 1999).

Berriasella (Berriasella) ex gr. moreti Mazenot, 1939 (Fig. 18: 2) ex gr. 1939 Berriasella moreti n. sp. Mazenot, p. 61, pl. 5, figs 2 a-c, 3a-c 1979 Berriasella (Berriasella) moreti Mazenot; Sapunov, p.174, pl. 55, fig. 4 1985 Berriasella (Berriasella) moreti Mazenot; Tavera, p. 249, pl. 34, figs 6-7, text-fig. 19-I Material: One incomplete specimen, £-17 (H = 12 mm; O = 10 mm). Description and remarks: Small fragment of whorl with slightly convex sides. The whorl ornamentation makes it similar to Berriasella (Berriasella) moreti Mazenot, as described and illustrated by authors cited in the synonymy. 184 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI

Occurrence: The specimen was found in the Pieniny Limestone Formation at £ysonka section (sample £-17 in Fig. 6). The species Berriasella (Berriasella) moreti Mazenot is known from the Berriasella jacobi Zone (Tavera, 1985).

Genus Elenaella, Nikolov, 1966 Type species: Berriasella cularensis Mazenot, 1939

Elenaella cf. subcularense Nikolov, 1982 (Fig. 17: 3) cf. 1982 Dalmasiceras (Elenaella) subcularense sp. n.; Nikolov, p. 108, pl. 27, figs 1-4 1999 Elenaella subcularense Nikolov; Vašíèek et al., p. 634, pl. 2, figs 5, 6 Material: One fragmentarily preserved specimen, 10b/2K-1 (H = 15). Description and remarks: One fragment of whorl with flattened side. Ornamen- tation consists of slightly prorsiradiate, bifurcate and trifurcate robust ribs swollen at furcating points. The form of whorls and ornamentation of our specimen are similar to those of the species Elenaella subcularense Nikolov, 1982 (see the synonymy), but fragmentary preservation precludes its exact specific identification. Occurrence: The specimen was found in the lower part of the Pieniny Limestone Formation at Kapuœnica II section (Fig. 5A). The species Elenaella subcularense Nikolov is known from the Late Berriasian of Bulgaria and Early Valanginian of Austria (see Vašíèek et al., 1999).

Genus Tirnovella Nikolov, 1966 Type species: Berriasella alpillensis Mazenot, 1939

Tirnovella cf. otopeta Thieuloy, 1979 (Fig. 19: 4) cf. 1999 Thurmanniceras cf. otopeta Thieuloy; Vašíèek & Faupl, p. 599, pl 1, fig. 7 1999 Tirnovella cf. otopeta Thieuloy; Vašíèek et al., p. 648 Material: Fragment of whorl, 2K-9 (H = 13 mm) Description and remarks: Small fragment of whorl. Sides slightly flattened. Ribs slightly prorsiradiate on umbilical margin rather strong on ventral part, simple and biplicate, with a tendency to fuse on umbilical margin. Our specimen resembles the species Tirnovella cf. otopeta Thieuloy as described and illustrated by Vašíèek and Faupl (1999). Occurrence: The specimen was found in the lower part of the Pieniny Limestone Formation at Kapuœnica II section. Tirnovella otopeta Thieuloy is known from the Late Berriasian of Spain and France (Vašíèek & Faupl, 1999). MICROFOSSIL AND NANNOCONID STRTIGRAPHY 185

Genus Dalmasiceras Djanelidze, 1921 Type species: Ammonites dalmasi Pictet, 1867 Dalmasiceras cf. djanelidzei Mazenot, 1939 (Fig. 17: 7) cf. 1939 Dalmasiceras djanelidzei n. sp.; Mazenot, p. 161, pl. 25 figs 1a-d, 4 (non figs 2ab, 3abc – see Tavera, 1985) 1979 Dalmasiceras djanelidzei Mazenot; Sapunov, p. 180, pl. 58, fig. 1 1982 Dalmasiceras djanelidzei Mazenot; Nikolov, p. 95, pl. 24, fig. 1 Material: One incomplete specimen, £-17/5 (H = 25). Description and remarks: Shell medium-sized, moderately evolute, with rapid increment of the whorls. Cross-section flattened with maximal width in umbilical region. Sides slightly convex, inclined towards ventral area. Ornamentation consists of lengthen periumbilical tubercles and weak prorsiradiate ribs which disappear above middle part of whorl. Our specimen is similar to the species Dalmasiceras djanelidzei Mazenot as described and illustrated by the authors presented in the synonymy. Its poor preservation precludes specific identification without reservation. Our specimen resembles also the species Dalmasiceras dalmasi (Pictet, 1867) as described and illustrated by Nikolov, (1982 p. 100, pl. 25, fig. 1), but differs from it by higher whorls. Occurrence: Our specimen was found in the Pieniny Limestone Formation at £ysonka section (see Fig. 6). The species Dalmasiceras djanelidzei Mazenot is known from the Berriasella jacobi Zone of France, Tunisia, Bulgaria and Spain (see Nikolov, 1982; Tavera, 1985).

Family Neocomitidae Salfeld, 1921 Subfamily Neocomitinae Salfeld, 1921 (= Endemoceratidae Schindewolf 1966; Leopoldiinae Thieuloy, 1971) Genus Criosarasinella Thieuloy, 1977 Criosarasinella furcillata Thieuloy, 1977 (Fig. 17: 1, 5, 6, 8, 13) 1977 Criosarasinella furcillata Thieuloy, p. 109, pl. 1, fig. 5; pl. 5, figs 3, 5? (non fig. 4) 1995 Criosarasinella furcillata Thieuloy, Reboulet, p. 75, pl. 17, fig. 5; pl. 18, figs 1-8; pl. 19, figs 1-6; pl. 20, figs 2-6 Material: Two incmplete specimens: ZK-8/2, ZK-8/3, and three whorl fragments – ZK-8/3a (H = 20 mm); ZK-8/3b (H = 16 mm); ZK-8/3c (H = 15 mm). Dimensions: No D (mm) H (mm) O (mm) H/D (%) O/D (%) R/2 r/2 ZK-8/2 52 19 19 37 37 27 ZK-8/3 68 22 26 32 38 186 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI

Description: Shell medium-sized, evolute with subrectangular cross-section of whorl and flat sides. Umbilicus wide, shallow. Ornamentation of inner part of shell consists of dense, flexuous and bifurcate ribs. On the outer part of the shell, strong ribs bifurcate atmbilical margin where small tubercles are present. Suture line is not preserved. Remarks: The species Criosarasinella furcillata Thieuloy, in Reboulet’s (1995) opinion includes micro and macroconchs. The specimen ZK-8/2 probably repre- sents a microconch, and ZK-8/3 – a macroconch. Both specimens agree well with descriptions and illustrations of the species Criosarasinella furcillata Thieuloy as presented in the synonymy. Occurrence: The specimens described here were found in the Pieniny Limestone Formation (ZK-8 bed) of the Zaskale section. The species Criosarasinella furcillata Thieuloy is known from the C. furcillata Zone of Late Valanginian age (cf. Reboulet, 1995; Hoedemaeker et al., 2003).

Genus Teschenites Thieuloy, 1971 Type species: Hoplites neocomiensiformis Uhlig, 1901

Teschenites subflucticulus Reboulet, 1995 (Fig. 19: 2) 1977 Neocomites (Teschenites) flucticulus Thieuloy; Thieuloy, p. 98, pl. 3, fig. 9 (non pl. 3, figs 7, 8, 10-11 = Teschenites flucticulus Thieuloy) 1995 Teschenites subflucticulus Reboulet n. sp.; Reboulet, p. 106, pl. 8, figs 1-9 (holotype – fig. 5) Material: One incomplete specimen preserved as internal cast (found in scree). Dimensions:

No D (mm) H (mm) O (mm) H/D (%) O/D (%) R/2 r/2 MK-1 37.5 16 9.5 25 43 16 26

Description: Shell medium-sized, moderately involute with slightly convex sides, and wide very shallow umbilicus. Umbilical margin slightly rounded. Umbilical wall almost vertical. Ornamentation of initial whorls consists of dense, short, strongly prorsiradiate primary ribs beginning at umbilical margin. Primary ribs on the last whorl prorsiradiate and falcate. Dense secondary ribs tilting forward, bifurate and trifurcate. Small tubercles appear on umbilical margin. Inter-rib spaces deep, twice as wide as the ribs. Primary ribs short and tilting forwards. Constric- tions with prominent collar. Remarks: The specimen from the Pieniny Klippen Belt agrees well with description and ammonites listed in the synonymy. It differs from the similar species Teschenites flucticulus Thieuloy by wide umbilicus and stronger ribs. Occurrence: The specimen was found in a loose, Radiolaria-bearing limestone MICROFOSSIL AND NANNOCONID STRTIGRAPHY 187 fragment, in the middle part of the Pieniny Limestone Formation at Kapuœnica II section (Fig. 5A). The species Teschenites subflucticulus Reboulet is known from Late Valanginian and basal part of the Acanthodiscus radiatus Zone of Early Hauterivian (Reboulet, 1995). Radiolarian assemblage, identified by the first author (A. P.) in thin section, suggests a Valanginian age of the limestone fragment.

Teschenites cf. subflucticulus Reboulet, 1995 (Fig. 18: 12) Material: One incomplete specimen, £-36-1. Dimensions:

No D (mm) H (mm) O (mm) H/D (%) O/D (%) R/2 r/2 £-36-1 28 12 6 42 21 16 28

Description and remarks: Shell small-sized, moderately involute, with slightly convex sides and narrow, very shallow umbilicus. Umbilical margin slightly rounded. Umbilical wall almost vertical. Ornamentation consists of small tubercles on umbilical margin from which begin dense, strongly prorsiradiate primary ribs bifurcating and trifurcating slightly above mid-part of whorls. Secondary ribs falcate, dense, tilted forwards. The specimen from the Pieniny Klippen Belt agrees with description and ammonites illustrated by Thieuloy (1977, p. 98, pl. 3, fig. 9) and Reboulet (1995, p. 106, pl. 8, figs 1-9). By narrow umbilicus and thinned ribs it differs from the species Teschenites flucticulus Thieuloy (see Thieuloy, 1977, p. 98-100, pl. 3, figs 7, 8, 10, 11; Vašíèek et al., 1994, p. 58, pl. 17, fig. 8; Reboulet, 1995, p. 110, pl. 9, figs 1-13; pl. 10, fig.14). Fragmentary preservation of our specimen precludes its more precise identification. Occurrence: The specimen was found in the uppermost part of the Pieniny Limestone Formation (£-36 in Fig. 6) exposed at £ysonka section. The species Teschenites subflucticulus Reboulet was described from the Criosarasinella furcillata horizon of Late Valanginian and basal part of the Acanthodiscus radiatus Zone of Early Hauterivian (Reboulet, 1995). The species Teschenites flucticulus Thieuloy is known from the Acanthodiscus radiatus Zone of Early Hauterivian (Reboulet, 1995).

Family Olcostephanidae Haug, 1910 Subfamily Olcostephaninae Haug, 1910 Genus Olcostephanus Neumayr, 1875 Subgenus Olcostephanus (Olcostephanus) Neumayr, 1875 Type species: Ammonites astierianus d’Orbigny, 1840

Olcostephanus (Olcostephanus) densicostatus (Wegener, 1909) (Fig. 18: 3) 1995 Olcostephanus (Olcostephanus) densicostatus (Wegener); Reboulet, p. 153, pl. 29, figs 3-5; pl. 30, figs 1-9; pl. 32, figs 1-5. 188 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI

Material: One incomplete specimen ZK-10-14 (found in scree). Dimensions:

No D (mm) H (mm) O (mm) H/D (%) O/D (%) ZK-10-14 c. 100 25 c. 39 c. 25 c. 38

Description: Medium-sized ammonite with slightly convex sides and wide, shallow umbilicus. Ornamentation consists of slightly prorsiradiate, prominent primary ribs, terminating in periumbilical tubercles, moreover slightly triangular, falcate and dense secondary ribs. They are tilted forwards, becoming irregularly bifurcate and trifurcate above tubercles and disappearing in the middle of shell flank. Inter-rib spaces deep, twice as wide as ribs. In the last whorl, the primary ribs are short tilting forward. Constrictions with prominent collar. Remarks: The specimen from the Pieniny Klippen Belt agrees well with description of the ammonite listed in the synonymy. It differs from similar species of the subgenus Olcostephanus (Olcostephanus) Neumayr, 1875, by weaker ornamentation. Occurrence: The specimen was found in the Pieniny Limestone Formation at the Zaskale section (Fig. 7). The species Olcostephanus (Olcostephanus) densicostatus (Wegener) occurs in Late Valanginian to Early Hauterivian (Reboulet, 1995).

APTYCHI

Genus Punctaptychus Trauth, 1927

Punctaptychus cinctus Trauth, 1935 (Fig. 19: 7) 1994 Punctaptychus cinctus Trauth; Vašièek et al., p. 70, pl. 23, fig. 2 (cum syn.) 1999 Punctaptychus cinctus Trauth; Boorova et al., p. 310, pl. 14, figs 4, 5 Material: One specimen, £-21/22 (long valve = 22 mm). Description: Valve long, with very shallow lateral depression. Articulate ribs strong, preserved only in apical part of valve. Inter ribs spaces as wide as ribs. Remarks: The specimen agrees with the forms cited in the synonymy. Occurrence: The specimen was found in the Pieniny Limestone Formation at £ysonka section. Punctaptychus cinctus Trauth was reported from the latest Tithonian to Middle Berriasian (Boorova et al., 1999). Our specimen was, however, found in the Upper Berriasian £ysonka Marl Bed (Fig. 6). MICROFOSSIL AND NANNOCONID STRTIGRAPHY 189

Genus Lamellaptychus Trauth, 1927

Lamellaptychus trauthi Renz & Habicht, 1985 (Fig. 18: 8) 1995 Lamellaptychus trauthi Renz et Habicht; Michalík et al., p. 290, fig. 5 1999 Lamellaptychus cf. trauthi Renz et Habicht; Vašíèek et al., p. 630, pl. 1, fig. 4 Material: One specimen, £-17 (long valve = 19 mm). Description: Valve long, with very shallow lateral depression. Articulate ribs, slightly curved, bend at right angle to the symphysal margin and arch towards terminal apex. Inter rib spaces as wide as ribs. Remarks: The specimen agrees with the forms cited in the synonymy. Occurrence: The specimen was found in the Lower Berriasian part of the Pieniny Limestone Formation at £ysonka section (Fig. 6). Lamellaptychus trauthi Renz et Habicht is known from Late Berriasian and Early Valanginian of Switzerland, and Early Valanginian of the West-Carpathian area (see Michalík et al., 1995).

Lamellaptychus ex. gr. herthae (Winkler, 1868) (Fig. 17: 12) Material: One internal mould, £-18. Description and remarks: Valve medium-sized (16 mm long), with shallow lateral depression and weakly marked ribs. Our specimen is similar to Lamellaptychus herthae (Winkler) as described and illustrated by Vašíèek et al. (1994, p. 71, pl. 23, fig. 8) and Vašíèek and Faupl (1999, p. 613. pl. 1, fig. 2). Poor preservation precludes its more precise identification. Occurrence: The specimen was found in the Lower Berriasian part of the Pieniny Limestone Formation, at £ysonka section. Lamellaptychus herthae (Winkler) was reported from Middle Berriasian to Late Valanginian (see Vašíèek & Faupl, 1999).

BELEMNITES

Order Belemnitida Zittel, 1895 Suborder Belemnitina Zittel, 1895 Family Belemnitidae d’ Orbigny, 1845 Subfamily Duvaliinae Pavlow, 1914 Genus Pseudobelus Blainville, 1827 Type species: Pseudobelus bipartitus Blainville, 1827

Pseudobelus ex gr. bipartitus Blainville, 1827 (Fig. 20: 4) ex gr. 1958 Pseudobelus bipartitus Bainville; Krimholz, p. 161, pl. 68, figs 7 a, b 190 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI

1960 Pseudobelus bipartitus Bainville; Kabanov, p. 366, pl. 1, figs 12 a, b Material: Four incomplete specimens (ZK-3; ZK-13; £-34/35; 2K-82). Description and remarks: Rostrum thick, long, cylindrical, oval in cross-section. Lateral grooves not visible. The specimens are similar to the forms cited in the synonymy; their lateral grooves are not visible. Occurrence: The specimens ZK-3 and ZK-13 were found in the Zaskale section, £-34/35 – in the £ysonka section, and 2K-82 – in the Kapuœnica II section, all in the Pieniny Limestone Formation. The species Pseudobelus bipartitus Blainville is known from the Valanginian of the Crimea, Caucasus and West Europe (Kabanov, 1960).

FINAL REMARKS AND CONCLUSIONS The studied sections of the Tithonian–Hauterivian deposits of the Branisko Suc- cession in the Polish part of the Pieniny Klippen Belt yielded micro- and macrofossils, which allowed to elaborate a more detailed stratigraphy of these strata, especially in their lowermost Cretaceous interval. (1) In the Kapuœnica I section (Fig. 3), presence of Malmica and Chitinoidella Zones, recognised already by Nowak (1976) in the Upszar Limestone Member, is confirmed herein. In the studied section, this member seems to be exclusively of Ti- thonian age. The Chitinoidella Zone occurs in the upper part of the Upszar Lime- stone Member, and could be 1.8 to 2.4 m thick in the Kapuœnica klippe. Interest- ingly, this zone is at least 1.7 m thick in the Brodno section of the Pieniny Limestone Fm. in Slovakia (cf. Houša et al., 1999). (2) The Upper Tithonian deposits of the Crassicollaria Standard Zone are missing in the section at the level presently accesible for stratigraphic analysis, due to tectonic shearing between the Czorsztyn and Pieniny Limestone Formations (see Fig. 4). Nevertheless, previous data and observations (Nowak, 1976; Birkenmajer, 1977; Obermajer, 1987) indicate that the Upper Tithonian limestones of the Crassi- collaria Zone were present in the lowermost part of the Pieniny Limestone Forma- tion. This is in accordance with the published data from the Brodno section in Slo- vakia, although there only the basal strata of the Pieniny (Limestone) Formation, about 1 m (Michalík et al., 1990) or 2.5 m (Houša et al., 1999) thick, were assigned to the Upper Tithonian. The limestones of the entire Upper Tithonian Crassicol- laria Zone are 2 to 2.7 m thick in this section (Michalík et al., 1990; Houša et al., 1999). Consequently, their sedimentation rate can be estimated at between 1.5 and 2 m/Ma. This value is similar to that obtained for the deposits assigned to magneto- zone CM19 in the Brodno section by Houša et al. (1999), between 2.17 and 2.19 m/Ma (Grabowski & Pszczó³kowski, 2002, tab. 2). (3) The incomplete Early Berriasian Calpionella alpina Subzone includes limestones about 9 m thick in the £ysonka section, further subdivided on the basis of the Nannoconus assemblages (see Tab. 4). The ammonites found in the Nannoconus steinmannii steinmannii Zone indicate the Beriasella jacobi Zone. The Alpina Sub- MICROFOSSIL AND NANNOCONID STRTIGRAPHY 191 zone seems to be complete in the Brodno section, where the limestones assigned to this subzone are about 3.5 m thick (Michalík et al., 1990). In the Kapuœnica I section, the sedimentation rate of the limestones assigned to the Elliptica Subzone was about 1.3 m/Ma. This value cannot be compared directly with the corresponding data from the Brodno section, as there the upper boundary of the Elliptica Subzone was not recognised. (4) The Upper Berriasian Simplex Subzone of the Calpionellopsis Standard Zone is fragmentarily represented in the £ysonka section, only. The Oblonga Sub- zone of this zone (sensu Remane et al., 1986) is better developed in the studied sections. In the £ysonka section, the Simplex/Oblonga subzonal boundary agrees with a change in lithology at the base of the £ysonka Marl Bed (Fig. 6). The Oblonga Subzone coincides with the marly deposition episode represented by two lithologic units – £ysonka Marl Bed (Birkenmajer, 1977) and (unnamed) marly and thin- bedded micritic limestones, separated by a limestone 1.2 m thick. The £ysonka Marl Bed is assigned to the lower interval of the Oblonga Subzone (sensu Remane et al., 1986). This bed corresponds, therefore, mainly to the Oblonga Subzone as defined by Grün and Blau (1997). In spite of terrigenous sediment influx, the overall sedimentation rate during the Late Berriasian Oblonga Subzone (s. l.) was low (about ~1.7 m/Ma). In contrast, marly deposits were not observed in the coeval strata of the Kapuœnica II section (Fig. 5A). However, the lower boundary of the Oblonga Subzone (Remane et al., 1986) was not recognised in this section. Pres- ence of the Tirnovella otopeta Zone was documented in the Kapuœnica II and £ysonka sections (see Tab. 5). This ammonite zone correlates with the uppermost part of the Calpionellopsis Zone (Blau & Grün, 1997; Aguado et al., 2000). (5) The radiolarian-calpionellid limestones of the Early Valanginian Calpionel- lites Zone are 8.3 m and about 1.6 m thick, in the Kapuœnica II and £ysonka sections, respectively. This difference in thickness may be partly due to a tectonic reduction in the latter section, although no clearly visible deformation of limestones was recognised in the discussed interval. In the £ysonka section, the Lower Valang- inian limestones differ from more marly Upper Berriasian deposits. In the Ka- puœnica II section, at the Berriasian/Valanginian boundary, there is a change in col- our of limestones only. Near the top of the zone, redeposited calpionellids occur indicating reworking of Upper Tithonian–Lower Berriasian sediments. In this section, the minimum value of sedimentation rate of the limestones assigned to the Calpionellites Standard Zone is about 4.1 m/Ma. (6) The Tintinnopsella Zone (latest Early Valanginian–Hauterivian) is represented by a limestone succession about 51 m thick in the Kapuœnica II section (Fig. 5A, B). The LateValanginian part of this calpionellid zone is documented by the ammonite Lytoceras lepidum (d’Orbigny) collected from scree; in the £ysonka section, this taxon was found in the limestone bed (see Fig. 6). In the latter section, the Upper Valanginian limestones are probably older than the Echinata Zone represented, however, in the Zaskale section. In the Zaskale outcrop, some ammonites are indicative of the Late Valanginian Criosarasinella furcillata Zone (sensu Hoe- demaeker et al., 2003 – see Fig. 7 and Tab. 5). The Upper Valanginian deposits ex- 192 A. PSZCZÓ£KOWSKI & R. MYCZYÑSKI posed in this section (Fig. 2: 4) are more marly than the coeval limestones from the Kapuœnica II section, and also the older Late Valanginian strata exposed in the £ysonka section. Moreover, the deposits at Zaskale (see Fig. 7) are richer in benthonic bioclasts in comparison with the coeval limestones from the Kapuœnica II section. (7) The ammonite findings are too sparse to designate precisely the Valangin- ian–Hauterivian boundary in the Kapuœnica II section. Infrequent calpionellids do not help to resolve this problem, as these microfossils are represented mainly by one taxon (Tintinnopsella carpathica). In this section, a few radiolarian taxa suggest the Hauterivian age of the sampled limestone beds numbered 2K-62 throughout 66; however, their age may still be Upper Valanginian, as explained above. The age of strata exposed in the upper part of the Zaskale section is ambiguous, although presence of the radiolarian taxon Ristola cretacea Jud (Fig. 12: 10) in sample ZK-16 is compatible with a Late Valanginian age of these deposits. (8) The Hauterivian limestones of the Tintinnopsella Zone are exposed in the upper part of the Kapuœnica II section (see Fig. 5B). The ammonites Olcostephanus sp. and Neolissoceras desmoceratoides (Wiedmann) were found only 4.5 m below the top of this section. This fauna indicates that the sparsely fossiliferous limestones are still Early Hauterivian in age (see Tab. 5). The high position of the discussed ammonites indicates that the Upper Hauterivian deposits, if present, are probably less than four metres thick in the studied section of the Pieniny Limestone Forma- tion. Presence of the Upper Hauterivian limestones is suggested by radiolarians found in thin section from grey radiolarian limestone exposed at the top of the section. These Radiolaria-bearing limestones, however, are very poor in calcareous microplankton.

Acknowledgements This work was done as a statutory research at the Institute of Geological Sciences, Polish Academy of Sciences. We would particularly like to thank Professor K. Birkenmajer for his advice and valuable information concerning location of outcrops of the Pieniny Limestone Formation, and constructive editorial remarks. We are grateful to the Director of the Pieniny National Park at Kroœcienko for permission to work in the nature reserves in the Polish part of the Pieniny Klippen Belt. We are also grateful to the Managers of the Reservoirs in Czorsztyn-Niedzica-Sromowce Wy¿ne S.A. for permission to access the Kapuœnica klippe during our field work. Thanks are due to Mrs E. Deput for making thin sections from samples used for this study, to Dr R. Or³owski for his technical assistance with the SEM, and to Mr Marian Dziewiñski for photographs of macrofauna.

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