Early Miocene age of the Stare Bystre Formation based on calcareous nannofossils (Magura Nappe, Outer Carpathians, Poland)

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Early Miocene age of the Stare Bystre Formation based on calcareous nannofossils (Magura Nappe, Outer Carpathians, Poland)

Agata KACZMAREK1, *, Marta OSZCZYPKO-CLOWES1 and Marek CIESZKOWSKI1

1 Jagiellonian University, Institute o f Geological Science, O leandry 2a, 30-063 Kraków, Poland

K aczm arek, A., O szczypko-C low es, M., Cieszkow ski, M., 2016. Early M iocene age o f the Stare Bystre Form ation based on c alcareous nannofossils (M agura Nappe, O uter C arpathians, Poland). G eological Q uarterly, 60 (2): 3 4 1 -3 5 4 , doi:

10.7 30 6 /g q .1 277

The area o f invest igat ion is situated close to the contact zone betw een the Pieniny Klippen Belt, Krynica Subunit o f the M agura Nappe and the Neogene strata o f the O ra v a -N o w y Targ Intram ontane Basin (southern Poland). In the area studied, m arine depos its o f the Stare Bystre Form ation outcrop at the surface w here th e y em erge from beneath fresh w a te r and te r

restrial Neogene and Q uaternary deposits. Nannofossil a ssem blages from all sa m p le s are strongly dom inated by reworked species. The Early M iocene age (nN2) o f the Stare Bystre Form ation has been determ ined on the base o f the first o ccu r

rence o f S ph e n o lith u s disb e le m n o s a fter S hackleton et al. (2000). During the Late O ligocene (N P25/N N 1), the frontal part o f M agura Nappe w as th ru st northw ards on to the term inal Krosno flysch basin. The northw ards thrusting o f the M agura Nappe w as accom panied by the form ation o f the piggy-back basin on the M agura Nappe, filled with the synrorogenic tu rb id ite s be

longing to the Z aw ada, Kremna and Stare Bystre fo rm ations (NN2).

Key w ords: O uter Carpathians, M agura Nappe, Stare Bystre Form ation, nannofossils, biostratigraphy, reworking.

INTRODUCTION

The youngest depos its of the Magura Nappe in Podhale have long attracted interest and controversy (Cieszkowski and Olszewska, 1986; Birkenmajer and Dudziak, 1988; Cieszko

wski, 1992; Gedl, 1995) as the dat i ng of the youngest depos its from the Magura Nappe is important both for understanding the tecton i cs of the Outer Carpathians and for the interpretation of the final evo l u-ion of the Central Carpathians and the Pieniny Klippen Belt. The presence of Oligocene/Miocene deposits was con -irmed not only in the peri- Pieniny Klippen Belt in Po l and and Slovakia, but also in the more external facies zones of the Magura Nappe in Po l and (Oszczypko, 1999, 2006; Oszczypko and Oszczypko-Clowes, 2002, 2010b, 2014; Oszczypko et al., 2005a).

In the peri- Pieniny Klippen Belt in Poland and Slovakia and also in the Raca facies zone, the age of the youngest depostis from the Magura Nappe, determined on the basis of calcareous nannoplankton and planktonic foraminifers, is not older than Early Burdigalian and not younger than Late Burdigalian (Oszczypko, 1999, 2006; Oszczypko and Oszczypko-Clowes, 2002, 2010b, 2014; Oszczypko et al., 2005a). The exceptions are outcrops around Waksmund, Zaskale and Stare Bystre (margins of the O rava-N owy Targ Basin) where, in addition to

* C orresponding author, e-m ail: agata.kaczm arek@ uj.edu.pl Received: Septem ber 8, 2015; accepted: D ecem ber 31, 2015; first published online: February 12, 2016

the Lower Miocene, Middle Badenian and Sarmatian deposits were also initially documented (Cieszkowski et al., 1991;

Cieszkowski, 1992). In subsequent papers Cieszkowski (1995) and Cieszkowski and Struska (2009) linked the question of the youngest deposits from the Magura Nappe with the debatable presence of marine Middle Miocene deposits in the Ora

va-N ow y Targ Intramontane Basin, without additional biostratigraphic data. All these papers described and discussed the section exposed at Stare Bystre (sometimes under the name of Rogoźnik), first described by W atycha (1976) as the Turbacz beds of Paleocene-Early Eocene age.

The aim of our study was to consider the age of the deposits from the Stare Bystre section on the basis of analysis of calcar

eous nannofossil assemblages.

GEOLOGICAL SETTING

The Orava-N owy Targ Basin is an intramontane depres

sion located at the boundary belween the Inner and Outer Carpathians, filled with terrestrial and freshwater depos its of Neogene and Quaternary age (Watycha, 1976; Łoziński et al., 2015 w ith references therein; Fig. 1A). It overlies three older units: the Magura Nappe, the Pieniny Klippen Belt (PKB), and the Podhale sector of the Central Carpathian Paleogene Basin (Fig. 1B).

The Magura Nappe, the largest unit of the Outer Western Carpathians (Fig. 1B), is mainly composed of Upper Crete"

ceous to Eocene strata. The oldest Lower Cretaceous rocks are known from the peri-PKB area in Po l and and from a few local i - ties in Southern Moravia. On the base of facies variations with

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342 Agata Kaczm arek, Marta O szczypko-C low es and M arek Cieszkowski

F ig. 1A - g e o lo g ic a l m a p o f th e E a s t A lp in e -C a rp a th ia n -P a n n o n ia n b a s in s y s te m (a fte r P ic h a a n d P e te rs , 1998);

B - s k e tc h -m a p o f th e P o lis h C a rp a th ia n s a n d th e ir fo re d e e p (b a se d o n Ż y tk o e t a l., 1989, s u p p le m e n te d ) Su - Siary, Ru - Raca, Bu - Bystrica, Ku - Krynica facies zo n e s o f the M agura Nappe;

place o f investigation: black sta r w ith the name R ogoźnik on the map

regards to the Paleogene deposits, the Magura Nappe has been subdivided into four facies - tectonic zones namely: the Krynica (Orava), Bystrica (Nowy Sącz), Raca and Siary zones (Fig. 1; see also Koszarski et al., 1974). In the Pol i sh sector of the Magura Nappe (Fig. 1) the youngest depos its have been first documented as the Oligocene Malcov Formation from the Nowy Sącz area (Oszczypko, 1973; see also Oszczypko et al., 1999; Oszczypko and Oszczypko-Clowes, 2002). The same depos its were found in the area near Nowy Targ (Cieszkowski and Olszewska, 1986; Cieszkowski, 1992), and subsequently, the Kremna Formation (O ligocene-Early Miocene) in the Beskid Sądecki Range and the Lubovnianska Vrchovina Mts.

(Oszczypko-Clowes, 2001, 2012; Oszczypko et al., 2005a;

Oszczypko and Oszczypko-Clowes, 2010b), as well as near Humenne (Matasovsky and Andreyeva-Grigorovich, 2002) and Horna Orava (Oszczypko-Clowes et al., 2013) in Slovakia.

The Krynica facies Zone provides important insights as re

gards our understand i ng of the terminal history of the Magura Basin formation. This zone records facies links with post

-nappe, Late Eocene to Oligocene basins of the Central Carpathians: the Paleogene Basin and the PKB structure Zone (Fig. 2 ). In the southern part of the Krynica Zone, the youngest deposits belong to the Kremna Formation, established by Oszczypko et al. (2005a). The Kremna Formation (Oszczypko et al., 2005a; Oszczypko and Oszczypko-Clowes, 2010a) is composed of a succession of thin- to medium-bedded turbidites with intercalations of thick-bedded massive sandstone. The up

per part is dom i nated by thin-bedded turbidites. Locally the cal

careous flysch of the Kremna Formation is intercalated with grey marls of Łącko type. The age of the Kremna Formation is Early Miocene, NN2 Zone (Oszczypko et al., 2005a;

Oszczypko and Oszczypko-Clowes, 2010b; Fig. 2 ).

PREVIOUS WORK

The first reports of the Middle Miocene mar ine depos its (clays with gypsum) in the Podhale region was given at the end of the nineteenth cenl ury by Uhlig (1890). Few years later Friedberg (1906, 1912) described mar ine deposi ts of Middle Miocene age near Szaflary. This view was questioned by Birkenmajer (1951) who claimed that the find i ng of Middle Mio

cene strata in Szaflary by Friedberg (1906, 1912) was a result of confusion between samples. A t the same time, geo l og ical and palynological research in the Orava Basin confirmed the fresh

water character and Mio/Pliocene age of these deposits (Foetterle, 1851; Raciborski, 1892; Halicki, 1930; Szafer, 1946-1947; Birkenmajer, 1954, 1958; Szafer and Oszast, 1964; Oszast, 1970; Watycha, 1976, 1977). For the first time in the Magura Nappe, Oligocene depos its (Malcov Formation) were discovered in the Nowy Sącz Basin (Raca Zone), over ly

ing the Magura sandstones (Oszczypko, 1973). Similar depos

its were also documented by Cieszkowski and Olszewska (1986) near Nowy Targ. A few years later, with reference to the views of Friedberg (1906, 1920), Cieszkowski et al. (1991) sig-

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F ig. 2. L ith o s tr a tig ra p h ic ta b le o f th e P a le o g e n e /E a rly M io c e n e d e p o s its o f th e M a g u ra N a p p e a n d P ie n in y K lip p e n B e lt (a fte r O s z c z y p k o a n d O s z c z y p k o -C lo w e s , 2 0 0 9 )

LAN. - Langhian; S - Serravallian

nalled the possibility of the existence of Middle Miocene marine deposits in the O rava-N owy Targ Basin. Finally Cieszkowski (1992, 1995) distinguished four new lithostratigraphic units: the Waksmund, Stare Bystre, Kopaczyska and Pasieka units, younger than the Magura and Malcov formations.

The data oblained from the Nowy Targ PIG 1 borehole al

lowed determination of the age of the Malcov Formation, based on calcareous nannoplankton (Smagowicz in Paul and Poprawa, 1992) rang i ng from Late Eocene to Early Miocene age. According to Cieszkowski (1992), these beds (in the O rava-N owy Targ Basin) do not bel ong to the Malcov Forma

tion but to the deposits which are younger than the Malcov For

mation, and named the W aksmund Beds.

The Waksmund Beds seem to form a transitional sequence between the Malcov Formation (Cieszkowski and Olszewska, 1986) and the Miocene beds ly i ng above. The stratigraphic po

sit ion of these depos its was determined on the basis of their structural context, lithological analogy to the Malcov and/or Magura formations, as well as on micropalaeontological dating.

The W aksmund Beds contain foraminifers of a wide strath graphic range, representing mainly Paleogene or Eocene spe

cies (Cieszkowski, 1992). However, the nannoplankton assem

blages are abundant, characterized by the presence of: Sphe- nolithus conicus, Sph. heteromorphus, Sph. pseudoradians and Helicosphaera cf. ampliaperta, and al lowed an age deter

mination ...as the Upper Oligocene-Lower Miocene...

(Cieszkowski, 1992). Cieszkowski and Struska (2009) included the W askmund Beds in the Malcov Formation.

The Stare Bystre Formation, developed in flysch facies, is represented by soft marls and marly shales intercaiated with thin and medium-bedded calcareous sandstones (Fig. 3 C -E ).

The depos its, which contain rich microfaunal assemblages,

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F ig. 3. L o c a litio n o f th e s a m p le s - th e e x p o s u re o f th e S ta re B y s tre F o rm a tio n o n th e b o u n d a ry b e tw e e n th e v illa g e s o f R o g o ź n ik a n d S ta re B y s tre in 2006

A, B - general view o f the exposure; C, D, E - yell owi sh m arly sh a le s and so ft m arls w ith thin in te r ca la tion o f ca lca re o u s sandstone; the sm all fold form s the front part o f a sm all subm arine slum p w ithin the m arly shales

have been described from two local ities (Zaskale and Rogo

źnik/Stare Bystre). The nannoplankton assemblages are char

acterized by the presence of Discoaster druggii, Sphenolithus ciperoensis, Sph. heteromorphus, Sph. abies, Helicosphaera ampliaperta, H. recta, Reticulofenestra pseudoumbilica and Discoaster kugleri. Based on the nannofossil content, Sma- gowicz (in Cieszkowski et al., 1991) determined the age of

Stare Bystre Formati on as Middle Miocene. The foraminifer analysis was conducted by Olszewska (in Cieszkowski et al., 1991). The assemblage determined contained such species as:

Globorotalia miozea Finlay, Gl. ex gr. foshi Cushman, Gl.

praemenardi Cushman, Globigerina bolli Citta et Premoli Silva, G. druryi Akkers, G. diplostomata Reuss, Gl. explications Jen

kins and Gl. ex gr. languaensis Bolli. According to Olszewska

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(in Cieszkowski et al., 1991) such an association allows for the determination of a Middle Miocene age for the Stare Bystre For

mation. Gedl (1995), on the basis of a dinoflagellate associa

tion, described the age of the deposits from Rogoźnik as Middle Eocene (Rhombodinium draco Zone).

The Kopaszyska Beds were initially called the Zaskale lay

ers (see Cieszkowski, 1992). They consist of yel l owl sh, slightly cohesive, fine to medium, rarely coarse-grained and conglom

eratic sandstones, occasionally with the occurrence of shales and mudstone clasts. These depos its are poor in microlauna, and mostly represented by agglutinated foraminifers:

Rhabdammina sp. Tak i ng into account the stratigraphic posi

tion, i.e. above the Stare Bystre Formation, the age was esli- mated as Middle Miocene.

The youngest deposits described by Cieszkowski et al.

(1991) be l ong to the Pasieka Beds, developed as soft marls and clays, and also of Middle Miocene age. Age est imat ion of the youngest divisions was based on stratigraphic position, not confirmed by biostratigraphic data. According to Cieszkowski (1992) the upper part of these deposits are probably the Szaflary clays described by Friedberg (1906, 1909).

SECTION STUDIED

The area stud i ed is located belween the vil l ages of Stare Bystre and Rogoźnik. The section (Fig. 3A, B) was situated on the left bank of the Rogoźnik Wielki Creek (GPS coordinates:

N49 26.506, E19 55.836). Currently the sect ion is completely covered by fluvial depos its, probably as an effect of stream ex

pansion. For that reason the description be l ow is based on the available literature (Cieszkowski et al., 1991; Cieszkowski, 1992, 1995; Cieszkowski and Struska, 2009). The beds were observed in inverted position, the dip of the layers fac i ng to the NNW at an angle of 75-80° (330/75). The Stare Bystre Forma

tion is typically a flysch deposit. The main part of the profile con

sists of thick layers of marly shales and soft marls with intercala

tions of coarse-grained sandstones (calcareous, grey-blui sh with two types of lamination: cross- and parallel, with muscovite and plant fragments). The upper part of the beds consists of thin-bedded sandstones with shale intercalations and plant fragments (carbonized detritus) while the lower part comprises fine-grained non-calcareous grey sandstones (Cieszkowski, 1992). Within the marly sequence, slump units of mudstone with marl clasts and delrilus were reported. The top of the lithostratigraphic subdivision in the profile passes into coarse-, medium- and fine-grained, thick-bedded sandstones typ i cal of the Magura Formation with intercalations of marls and marly shales, of the Łącko type (Fig. 4 ).

METHODS AND MATERIALS

18 samples (col l ected by the third aut hor) for calcareous nannofossil analyses, were prepared us i ng standard smear slide techniques for light microscope (LM). The investigation was carried out us i ng a Nikon-Eclipse E 600 POL, microscope at a magnificat ion of 1000x us i ng paral i el and crossed polars.

Quantitative analyses were performed using counts of 300 spec i mens per slide. In order to ana i yse and calcu i ate the per

centage abundance of autochthonous and allochthonous as

semblages a 5% range error was accepted. The nominal values and percentages are shown in Appendix 1*.

The state of preservation of calcareous nannofossils was assessed using the criteria of Roth and Thierstein (1972), Roth (1973) and Bown (1998). These are: G (good preservat ion) - small dissolution of skeletons with minimum overgrowth, where recognition of species did not cause any prob I ems, M (moder

ate preservation) - specimens were mechanically broken but still easy to recognize, P (poor preservation) - sped mens showed mechanical fragmentation and also overgrowths, VP (very poor preservation) - where taxa were mostly in fragments.

Also an attempt to separate different stages of preservation and overgrowth was made. Fol I owI ng Roth and Thierstein (1972), Roth (1973) and Bown (1998), six groups were considered (3 of mechanical degradation and 3 of overgrowth):

Mechanical dissolution:

E1 - where delicate structures were destroyed, in cocco- lith species sertate out I i nes were recognized. Crosst -structures in Chiasmolithus sp. and also in species such as Pontosphaera, Rhabdosphaera were still observed;

E2 - where central structures were destroyed (such as the grill, or cross). More del I cate species were still ob

served (for example Sphenolithus and Helicosphaera);

E3 - only the most resistant species survived - Coccolithus, Discoasters, Reticulofenestrid etc.

Overgrowth:

01 - rays of Discoasters were thickened, some elet ments of placoliths are overgrown;

0 2 - rays were more thickened, ray tips were not recog

nized;

0 3 - individual species of Discoaster were not recogniz

able. Placoliths covered strongly by calcite, identification was difficult.

In the samples investigated, attempts to accurately deter

mine the conservation status of the species caused many diffi

culties, due to several sources of reworked material. In all sam

ples various states of preservation of each species were visible.

Therefore, in Appendix 1, the states of preservation were given in ranges.

In most samples the state of preservation of the species van ed from moderate to good takI ng into account the 1st and 2nd level of overgrowths.

After Bown and Young (1998), species abundance levels were divided into 5 groups:

1. Very high (VH) > 20 taxa per 1 field of view;

2. High (H) 10-20 taxa per 1 field of view;

3. Moderate (M) 5 -1 0 taxa per 1 field of view;

4. Low (L) 1 -5 taxa per 1 field of view;

5. Very low (L) <1 taxon per 1 field of view.

In most of samples, frequency of species occurrence reached level 1 (very high) to level 2 (high). The states of pres

ervation in individual samples are shown in Appendix 1.

RESULTS

DESCRIPTIO N OF THE NAN NO PLANKTO N AS SE M B LA G ES

All samples were ana Iysed under the microscope. Dun ng the analysis 128 species of calcareous nannofossils were de

termined Appendix 2 . The species identified were divided into three assemblages containing: autochthonous, reworked and long-rang I ng taxa (Fig. 5).

* Supplem entary data associated with this article can be found, in the online version, at doi: 10.7306/gq.1277

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F ig. 4. L ith o s tr a tig ra p h ic a l lo g s o f th e S ta re B y s tre F o rm a tio n (a fte r C ie s z k o w s k i, 1992)

AUTO C H TH O N O U S ASSEM BLAG ES

The autochthonous assemblage consists of 13 taxa. The highest share (8.1-13% ) of autochthonous species was ob

served in the samples 24/98/N, 20/98/N and 5/98/N.

Autochthonous species observed almost in all samples were:

Coronocyclus nitescens (Fig. 6E, F), Pontosphaera multipora, Spenolithus disbelemnos (Fig. 6 P -U ) and Sph. dissimilis (Fig.

6W, Y ). Other species, found only in some samples were:

Braarudosphaera bigelowii (Fig. 6A), Calcidiscus leptoporus (Fig. 6B), Discoasterdeflandrei (Fig. 6H), Helicosphaera carteri (Fig. 6 J -M ), H. obliqua, Reticulofenestra daviesii, R. minuta

and R. haqii. Percentages of the most abundant autochthonous taxa are shown in Figure 7.

The highest percentage of all taxa determined was of Coronocyclus nitescens. The highest rate of occurrence of this species was found in samples 6/98/N (2.2%) and 5/98/N (1.9%). Clacidiscus leptoporus is most abundant in samples 24/98/N and 8/98/N (2.2%). However, this species was not ob

served in 5 samples, making its overall percentage smaller than that of other two species from that group. The percentage of Pontosphaera multipora was signifi cantly higher than that of Calcidiscus leptoporus (Appendix 1), the highest rate o foccur- rence of this species being found in samples 16/98/N and

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F ig . 5. T he p e rc e n ta g e o f a u to c h th o n o u s , re w o rk e d a n d lo n g -ra n g in g ta x a in th e s a m p le s c o lle c te d fr o m th e S ta re B y s tre s e c tio n

19/98/N (2.5%) (Fig. 7). Other species in the autochthonous group were observed in smaller quantities; in most cases they did not reach 6%, with two exceptions: Reticulofenestra minuta (8.6%) and Sphenolithus conicus (Fig. 6P, R), which almost reached 10% (9.8% in total percentage; Appendix 1).

REW O RKED AS SE M B LA G ES

In all samples 112 reworked taxa were recognized. These were mainly Paleogene and Eocene species.

In almost all samples species of the genus Fasciculithus were identified. In reworked assemblages, some Cretaceous species were also observed, which because of their low amounts were not determined to species level. The samples also included representatives of the genus Ericsonia the size of which did not allow species-level identification. In Appendix 1 these spec i mens were described as “small Ericsonia". The greatest species diversity in the reworked assemblages was observed in the genera Chiasmolithus, Discoaster or Spheno

lithus. The variabil ity of the percentage of each species within the genus is shown on the Figure 8.

The highest content of the genus Chiasmolithus was ob

served in sample 19/98/N (almost 3.5% - Fig. 8 ). The most common species is Chiasmolithus grandis, the percentage of all samples reach i ng 7.3% (Appendix 1), m ostfrequently rep

resented in the samples 8/98/N and 19/98/N. Other frequently occurred species within the genus included Chiasmolithus solitus (3.8%), most numerous in sample 8/98/N and Chias

molithus expansus (3.5%), most frequent in sample 19/98/N (Appendix 1).

The highest content of the genus Discoaster was observed in sample 16/98/N (almost 10.8% - Fig. 8). The most common species in the genus Discoaster was Discoaster barbadiensis, the percentage of its appearances in all samples be i ng 12.7%

(Appendix 1); it was most often observed in sample 16/98/N.

The highest content of the genus Sphenolithus was observed in sample 6/98/N (Fig. 8).

Within the genus Sphenolithus the most common species was Sph. radians, the sum of the percentage occurtences of that species in all samples amounting to 20.3% (Appendix 1). It was most widely represented in the samples 6/98/N, 8/98/N and 19/98/N. Another frequently observed species was Sph. editus (8.55%), its highest share of species be i ng in sample 8/98/N (Appendix 1).

Among reworked assemblages in each sample, Blackites spinosus, Ericsonia formosa, Semihololithus kerabyi, Toweius callosus, T. magnicrassus, T. rotundus, Zygrhablithus bijugatus and numerous Transversopontis pulcher and Tribrachiatus orthostylus were also observed. The highest contribution of re

worked taxa in samples from the profile in Stare Bystre amounted to 79.5% in sample 6/98/N (Fig. 9). The most numer

ous species rep tesented in the allochthonous assemblages were Zygrhablithus bijugatus, Toweius rotundus, T. callosus and Blackites spinosus (Fig. 9). The percentage of Zygrha- bilitus bijugatus in three samples (18/98/N, 13/98/N and 15/98/N) is >15% (Fig. 9). The percentage of Toweius rotundus in three samples (11/98/N, 6/98/N and 7/98/N) is >15% and in the sample 20/98/N the species is absent (Fig. 9). The percent

age of Blackites spinosus vary, the highest percentages be i ng observed in samples 9/98/N and 16/98/N, while this species was not observed in samples 15/98/N and 19/98/N (Fig. 9). The smallest percentage in described parts of the reworked assem

blages comprised Toweius callosus, identified in all samples studied (Fig. 9).

LO NG -RANG IN G TAXA

In all samples considered, besides a signifi cant level of re

depos i ted taxa, species with very long stratigraphic ranges, were also observed. For this reason, they were not included in autochthonous or reworked assemblages, and have been sep- a tated as a group of long-rang i ng taxa. These species are mostly cosmopolitan and also resistant to poor environmental

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F ig. 7. T he v a ria b ility o f th e p e rc e n ta g e o f th e m o s t a b u n d a n t a u to c h th o n o u s ta x a in s a m p le s fro m th e S ta re B y s tre s e c tio n

F ig . 8. T he p e rc e n ta g e o f v a ria b ility o f in d iv id u a l s p e c ie s w ith in th e g e n u s S p hen olithu s, D is c o a s ter a n d Chiasm olithu s in s a m p le s fr o m th e S ta re B y s tre v illa g e e x p o s u re

F ig. 6. LM m ic ro p h o to g r a p h s o f c a lc a re o u s n a n n o fo s s ils fro m s a m p le s fro m th e S ta re B y s tre F o rm a tio n

A - B ra arudosphaera b ig e lo w ii (Gran and Braarud, 1935) D eflandre (1947) sam ple11/98/N (xN); B - C a lcidiscus le p to po ru s (M urray and Blackm an, 1898) Loeblich and Tappan (1978) sam ple 24/98/N (xN); C - C occolithus p e la g icu s (W allich, 1877) S ch iller (1930) sam ple 14/98/N (xN); D - C occolithus p e la g icu s (W allich, 1877) S chiller (1930) sam ple 14/98/N (1 N); E - C oronocyclus nite sce ns (Kam ptner, 1963) Bram lette and W ilcoxon (1967) sam ple 20/98/N (xN); F - C oronocyclus n ite sce ns (Kam ptner, 1963) Bram lette and W ilcoxon (1967) sam ple 20/98/N (1N); G - C yclica rg o lithu s lu m in is (Sullivan, 1965) Bukry (1971) (xN); H - D isc o a s te r defla nd re i (Bram lette and Riedel, 1954) sa m  ple 5/98/N (1N); I - D is c o a s te r lo d o e n sis (Bram lette and Riedel, 1954) sam ple 8/98/N (1N); J - H e licosphaera ca rteri (W allich, 1877) K am ptner (1954) sam ple 4/98/N (xN); K - H e licosphaera ca rte ri (W allich, 1877) K am ptner (1954) sam ple 4/98/N (1N); L - H elicosphaera c a rteri (W allich, 1877) Kam ptner (1954) sam ple 24/98/N (xN); M - H e licosphaera ca rteri (W allich, 1877) K am ptner (1954) sam ple 24/98/N (1N); N, O - S ph e n o lith u s co n icu s (Bukry, 1971) sam ple 5/98/N (xN); P -U - Sph e n o lith u s disb e le m n o s (Fornaciari and Rio, 1996) sam ple 21/98/N (xN); W, Y - Sph e n o lith u s d issim ilis (Bukry and Percival, 1971) sam ple 6/98/N (xN); Z - S ph e n o lith u s m orifo rm is (Brönnim ann and S tradner, 1960) Bram lette and W ilcoxon (1967) sam ple 12/98/N (xN); Z - Z ygrh a b litu s b iju g a tus (D eflandre in: D eflandre and Fert, 1954) D eflandre (1959) and S em ih o lo lith us ke ra b yi (Perch-N ielsen, 1971) (xN); I. - Z ygrh a b litu s bijugatus, II. - S e m ih o lo lith us kerabyi; 1 N - plane parallel polars, xN - crossed polars

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Blackites spinosus □ Toweius callosus ■ Toweius rotundus □ Zygrhabilitus bijugatus

F ig. 9. T he p e rc e n ta g e o f th e m o s t a b u n d a n t a llo c h th o n o u s s p e c ie s in th e a s s e m b la g e s fr o m th e S ta re B y s tre s e c tio n

conditions. Among the group of heterococcoliths, two species in the genus Coccolithus were distinguished: C. pelagicus (Fig.

6C, D) and C. eopelagicus (range of occurrence from Danian to recent), and two species from the genus Cyclicargolithus: Cy.

floridanus (Eocene to Miocene) and Cy. abisectus (Oligocene to Early Miocene). In that group one species of Sphenolithus - Sph. moriformis (Fig. 6Z ; Eocene to Late Miocene) was noted and also one species from the nannolith fam i ly: Braarudo- sphaera bigelowii (Fig. 6A ) - which occurs in the oceans to the present day, associated with a neritic environment (Gran and Braarud, 1935).

INTERPRETATION

BIOSTRATIG RAPHY

The age of the Stare Bystre Formation was established as Early Miocene - NN2, us i ng standard nannoplankton zonation (Martini and Worsley, 1970). The age was determined on the ba

sis of the co-occurrence of Cyclicargolithus floridanus, Helicosphaera carteri, Sphenolithus conicus, Sph. dissimilis and Sph. disbelemnos. According to Fornaciari and Rio (1996) and Young (1998) Sph. disbelemnos is typ i cal of the NN2 Zone (Fig.

10). An astronomical age for Sph. disbelemnos was proposed by Shackleton et al. (2000; see also Raffi et al., 2005). The species appears at 22.67 Ma and it is shown to be an important datum level for the Paratethys region (Rogl and Nagymarosy, 2004;

Oszczypko-Clowes in: Oszczypko et al., 2005a).

At the same time Dictyococcites bisectus, Cyclicargolithus abisectus and Zygrhablithus bijugatus are absent from this as

sociation. According to Perch-Nielsen (1985), Berggren et al.

(1995), Fornaciari et al. (1996) and Young (1998) the LO of Dictyococcites bisectus detines the base of NN1. Thus, one can assume that the age of the Stare Bystre Forma tion is not older than NN2 (Aquitanian/Burdigalian).

AG E OF THE REW O RKED AS SE M B LA G ES

Redeposited species can help to decipher both the history of terrestrial erosion around the basin area, as well as the direction and intensity of the transport of eroded material. In the Magura succession, within the area investigated, flysch deposition was

F ig. 10. B io s tr a tig ra p h ic p o s itio n o f th e S ta re B y s tre F o rm a tio n (g re y fie ld )

mainly observed, involving turbidity currents from a continental slope. Biostratigraphical stud ies have shown the very high util ity of calcareous nannoplankton in turbidites. This is the result of the small size of nannofossils with at the same time large numbers of vari ous taxa preserved in a small portion of rock (Siesser, 1993).

Calcareous nannoplankton are ideally preserved in mud-clay mate tial, which forms a natu tal shield to the small nannofossil skeletons, protecting them from degradation during transport (Mikes et al., 2008; Oszczypko-Clowes, 2012). In the samples exam i ned, the proportion of reworked taxa reaches >50% of all observed species. The age of the reworked assemblages varies across a wide time range. In the material stud t ed, Cretaceous, Paleocene, Eocene and Oligocene taxa were observed, though with noticeable, significant predominance of Paleogene taxa over Cretaceous ones (Fig. 11).

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The contribution of Cretaceous species in reworked assem

blages does not exceed 5.07% (sample 24/98/N), whereas the Paleogene species can reach >80% of all species in the sam

ples investigated (Fig. 6 ).

The assemblages are mixed with species from different time intervals:

- The Lower Eocene assemblage is represented by Discoaster multiradiatus (range: NP9-11), Discoaster lodoensis (NP12-14; Fig. 6I) and Tribrachiatus ortho

stylus or Toweius crassus.

- The presence of the Middle Eocene (NP15 zone) could be dated by the Chiasmolithus gigas zonal marker or by Nanotetrina quadrata.

- Long-ranging species, spanning from the Mid Eocene to the Early Oligocene, include: Discoaster tanii nodifer (NP16-22), Helicosphaera bramlettei (NP14-23), Lan- ternithus minutus (NP16-22), Reticulofenestra umbilica (NP16-22), Discoaster barbadiensis (NP10-20), Dictyo- coccites bisectus (NP17-24), Discoaster saipanensis (NP14-23) and Ismolithus recurvus (NP19-22).

- In addition, typical Oligocene taxa include: Sphenolithus ciperoensis (FO), Pontosphaera latelliptica, Transverso- pontis fibula and, very rarely, Sph. capricornutus and Sph. calyculus.

DISCUSSION

The age of the Stare Bystre Formation was assigned to the Early Miocene - Aquitanian/Burdigalian (NN2 Zone). The age determination was made on the presence of Sphenolithus disbelemnos in almost all samples (Fig. 6 P -U ) which according to Young (1998) is an index species for the lower part of the NN2 nannoplankton zone. Such age deferminafion is in conf trast to the previous works describ i ng the age of Stare Bystre

Formation as Middle Miocene (Badenian/Sarmatian) (Ciesz

kowski et al., 1991; Cieszkowski, 1992, 1995). The age of the deposits in previous works was based on the presence of Discoaster drugii, Sphenolithus ciperoensis, Sph. heteromor- phus, Sph. abies, Helicosphaera ampliaperta, H. recta, Reti

culofenestra pseudoumbilica and Discoaster kugleri (Smago- wicz in Cieszkowski et al., 1991). Accord i ng to the previous works considering the standard zonation of Martini (1971) and Mar- ini and Wors I ey (1970), the first occur-ence of Reticulo

fenestra pseudoumbilica takes place in NN5, however, this taxon was reported by Marunteanu (1991) from the lower limit of NN2, while Holcova (2013) also questioned the Middle Miocene age of Reticulofenestra pseudoumbilica. Holcova (2013) di

vided the reticulofenestrid group on the basis of their size and also noticed differences between the first appearances of these species in the global ocean and in the Cen-ral Paratethys, in which the larger species appear a lit- le ear! i er. Accord i ng to Holcova (2013), the smallest species (i.e. R. haqii <4 pm) has a FO (first occurrence) in zone NP25 in the Paratethys, whereas in the global ocean it was in zones NN1/NN2. Similarly the spe

cies of R. pseudoumbilicus >5 pm first reportedly appeared at the end of the Oligocene. Holcova (2013) also suggested that different sizes in the R. haqii-pseudoumbilicus group depended on the seasonal -y in the ocean (smaller species in winter and larger in the summer). Larger taxa of Reticulofenestrid >7 pm (Holcova, 2012) appear in the NN4 Zone and >8 pm in the NN5 Zone. Cieszkowski et al. (1991) did not men-ion the size of Reticulofenestra pseudoumbilicus and therefore a reference to this species will not be considered.

In our opin j on, the most important species men-ioned by Smagowicz (in Cieszkowski et al., 1991), which determined the age of the Stare Bystre Formation are: Sphenolithus abies, the first appearance of which is in the NN6 Zone (Sarmatian, Tortonian) (Perch-Nielsen, 1985; Bown, 1998), and Discoaster kugleri, which is an index taxa for the NN7 Zone (Sarmatian) in the standard zonation (Martini, 1971).

F ig . 11. C o m p a ris o n o f th e p e rc e n ta g e o f C re ta c e o u s a n d P a le o g e n e s p e c ie s in in d iv id u a l s a m p le s fro m th e S ta re B y s tre p ro file

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Species such as: Discoaster drugii, Sphenolithus ciperen- sis, Sph. heteromorphus, Sph. abies, Helicosphaera amplia- perta, H. recta, Reticulofenestra pseudoumbilica and Disco

aster kugleri are not present. In such cases the Middle Miocene age of Stare Bystre Formation cannot be supported.

The autochthonous assemblage shows mostly temperate and warm-wa-er taxa, typ - cal of the gradual Early Miocene in

crease in surface wa-er tempera-ure. These include Spheno

lithus species such as Sph. conicus (Fig. 6N, O), Sph. disbele- mnos (Fig. 6 P -U ) and Sph. dissimilis (Fig. 6W, Y ). Also, the fol

lowing species were observed in all samples: D. deflandrei (Fig.

6H ), H. carteri and H. obliqua. In the long-rang i ng group there was also noticeable Cyclicargolithus floridanus which is an indi

cator of temperate water (Wei and Wise, 1990).

From the lithological point of view the Stare Bystre Forma

tion is characterized by the occurrence of Magura-type sand

stones and thin-bedded flysch layers with the Łącko type of marlstones. Considering the age, qualitative and quantitative composition of nannoplankton assemblages and also litho- facies compositions, a strong correlation between the Stare Bystre Forma-ion and the Kremna and Zawada formations is noticeable (cf. Oszczypko et al., 1999, 2005a; Oszczypko and Oszczypko-Clowes, 2002; Oszczypko-Clowes, 2012).

Within reworked assemblages a significant predominance of Paleogene species over Cre-aceous ones was observed, from which one can infer that they were transported with the mass of sediment in gravity flows. All Paleogene species within the reworked assemblages were better preserved than indige

nous or Cre-aceous ones, and have a much larger size sug

gesting a good resistance to mechanical damage during trans

port. With the growth of the accretionary prism, eroded older material (from Cretaceous deposits) also appeared. In the sam

ples within the reworked assemblages younger Oligocene taxa were also observed, suggesting the presence of another source of material. This could have been the products of ero

sion of younger deposits from the bottom of the basin, probably related to the presence of mud volcanoes, which in combination of dehydration of the material led to extraction and erosion from the bottom of the basin. This type of process is characteristic of the dynami cs of an accretionary prism (Mikes et al., 2008;

Oszczypko-Clowes, 2012). A similar degree of redeposition were described in the Miocene turbid rty depos rts from the PKB and also other Magura Nappe zones: Krynica, Tylicz and Bystrica, e.g. within the Kremna Formation (Oszczypko-Clowes in: Oszczypko et al., 2005a) or Zawada Forma-ion from the Lubovnianska Vierchovina sections (Oszczypko and Oszczy

pko-Clowes, 2002). Duringthe Late Oligocene (NN25/NN1)the frontal part of the Magura Nappe thrust northwards onto the ter

minal Krosno flysch basin. The northwards thrusting of the Magura Nappe was accompanied by the formation of the piggy

b a c k basin on the Magura Nappe, filled with the synorogenic turbidites be - ong - ng to the Zawada (Oszczypko et al., 1999), Kremna (Oszczypko at al., 2005a) and Stare Bystre formations (NN2). Duri ng the Early/Middle Miocene, the Magura Nappe was finally folded and flatly thrust northwards over the Fore-Magura Group of Nappes and, together with these, upon the Silesian Nappe.

CONCLUSIONS

1. On the basis of calcareous nannoplankton, the age of the Stare Bystre Format ion was assigned to the Burdigalian age (NN2 Zone).

2. Nannofossil analyses did not confirm a Badenian-Sar- ma tian age for the Stare Bystre For ma tion.

3. The nannofossil assemblages show high contents of re

worked species which are mostly of Eocene and Oligocene age.

4. On the basis of lithological and biostratigraphical similari

ties, the Stare Bystre Formafion can be corfe I ated with the Kremna and Zawada formations.

Acknowledgem ents. The aufhors express their profound gratifude to all the reviewers of this work (K. Holcova, Anony

mous and D. Ghita) for their insightful comments, important suggesfions and help in the process of writ f ng, and to the ed f tors, T.M. Peryt and E. Dqbrowska-J^drusik, for their editorial as sis tance.

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