Early Mio cene age of the Stare Bystre For ma tion based on cal car e ous nannofossils (Magura Nappe, Outer Carpathians, Po land)
Agata KACZMAREK1, *, Marta OSZCZYPKO-CLOWES1 and Marek CIESZKOWSKI1
1 Jagiellonian Uni ver sity, In sti tute of Geo log i cal Sci ence, Oleandry 2a, 30-063 Kraków, Po land
Kaczmarek, A., Oszczypko-Clowes, M., Cieszkowski, M., 2016. Early Mio cene age of the Stare Bystre For ma tion based on cal car e ous nannofossils (Magura Nappe, Outer Carpathians, Po land). Geo log i cal Quar terly, 60 (2): 341–354, doi:
10.7306/gq.1277
The area of in ves ti ga tion is sit u ated close to the con tact zone be tween the Pieniny Klippen Belt, Krynica Sub unit of the Magura Nappe and the Neo gene strata of the Orava–Nowy Targ Intramontane Ba sin (south ern Po land). In the area stud ied, ma rine de pos its of the Stare Bystre For ma tion out crop at the sur face where they emerge from be neath fresh wa ter and ter - res trial Neo gene and Qua ter nary de pos its. Nannofossil as sem blages from all sam ples are strongly dom i nated by re worked spe cies. The Early Mio cene age (NN2) of the Stare Bystre For ma tion has been de ter mined on the base of the first oc cur - rence of Sphenolithus disbelemnos af ter Shackle ton et al. (2000). Dur ing the Late Oligocene (NP25/NN1), the fron tal part of Magura Nappe was thrust north wards on to the ter mi nal Krosno flysch ba sin. The north wards thrust ing of the Magura Nappe was ac com pa nied by the for ma tion of the piggy-back ba sin on the Magura Nappe, filled with the synrorogenic turbidites be - long ing to the Zawada, Kremná and Stare Bystre for ma tions (NN2).
Key words: Outer Carpathians, Magura Nappe, Stare Bystre For ma tion, nannofossils, biostratigraphy, re work ing.
INTRODUCTION
The youn gest de pos its of the Magura Nappe in Podhale have long at tracted in ter est and con tro versy (Cieszkowski and Olszewska, 1986; Birkenmajer and Dudziak, 1988; Cieszko - wski, 1992; Gedl, 1995) as the dat ing of the youn gest de pos its from the Magura Nappe is im por tant both for un der stand ing the tec ton ics of the Outer Carpathians and for the in ter pre ta tion of the fi nal evo lu tion of the Cen tral Carpathians and the Pieniny Klippen Belt. The pres ence of Oligocene/Mio cene de pos its was con firmed not only in the peri- Pieniny Klippen Belt in Po land and Slovakia, but also in the more ex ter nal fa cies zones of the Magura Nappe in Po land (Oszczypko, 1999, 2006; Oszczypko and Oszczypko-Clowes, 2002, 2010b, 2014; Oszczy pko et al., 2005a).
In the peri- Pieniny Klippen Belt in Po land and Slovakia and also in the Rača fa cies zone, the age of the youn gest depostis from the Magura Nappe, de ter mined on the ba sis of cal car e ous nannoplankton and plank tonic foraminifers, is not older than Early Burdigalian and not youn ger than Late Burdigalian (Oszczypko, 1999, 2006; Oszczypko and Oszczypko -Clowes, 2002, 2010b, 2014; Oszczypko et al., 2005a). The ex cep tions are out crops around Waksmund, Zaskale and Stare Bystre (mar gins of the Orava–Nowy Targ Ba sin) where, in ad di tion to
the Lower Mio cene, Mid dle Badenian and Sarmatian de pos its were also ini tially doc u mented (Cieszkowski et al., 1991;
Cieszkowski, 1992). In sub se quent pa pers Cieszkowski (1995) and Cieszkowski and Struska (2009) linked the ques tion of the youn gest de pos its from the Magura Nappe with the de bat able pres ence of ma rine Mid dle Mio cene de pos its in the Ora - va–Nowy Targ Intramontane Ba sin, with out ad di tional biostrati - graphic data. All these pa pers de scribed and dis cussed the sec tion ex posed at Stare Bystre (some times un der the name of Rogoźnik), first de scribed by Watycha (1976) as the Turbacz beds of Paleocene–Early Eocene age.
The aim of our study was to con sider the age of the de pos its from the Stare Bystre sec tion on the ba sis of anal y sis of cal car - e ous nannofossil as sem blages.
GEOLOGICAL SETTING
The Orava–Nowy Targ Ba sin is an intramontane de pres - sion lo cated at the bound ary be tween the In ner and Outer Carpathians, filled with ter res trial and fresh wa ter de pos its of Neo gene and Qua ter nary age (Watycha, 1976; Łoziński et al., 2015 with ref er ences therein; Fig. 1A). It over lies three older units: the Magura Nappe, the Pieniny Klippen Belt (PKB), and the Podhale sec tor of the Cen tral Carpathian Paleogene Ba sin (Fig. 1B).
The Magura Nappe, the larg est unit of the Outer West ern Carpathians (Fig. 1B), is mainly com posed of Up per Cre ta - ceous to Eocene strata. The old est Lower Cre ta ceous rocks are known from the peri-PKB area in Po land and from a few lo cal i - ties in South ern Moravia. On the base of fa cies vari a tions with
* Corresponding author, e-mail: agata.kaczmarek@uj.edu.pl Received: September 8, 2015; accepted: December 31, 2015; first published online: February 12, 2016
re gards to the Paleogene de pos its, the Magura Nappe has been sub di vided into four fa cies – tec tonic zones namely: the Krynica (Orava), Bystrica (Nowy Sącz), Rača and Siary zones (Fig. 1; see also Koszarski et al., 1974). In the Pol ish sec tor of the Magura Nappe (Fig. 1) the youn gest de pos its have been first doc u mented as the Oligocene Malcov For ma tion from the Nowy Sącz area (Oszczypko, 1973; see also Oszczypko et al., 1999; Oszczypko and Oszczypko-Clowes, 2002). The same de pos its were found in the area near Nowy Targ (Cieszkowski and Olszewska, 1986; Cieszkowski, 1992), and sub se quently, the Kremna For ma tion (Oligocene–Early Mio cene) in the Beskid Sądecki Range and the Ľubovnianska Vrchovina Mts.
(Oszczypko-Clowes, 2001, 2012; Oszczypko et al., 2005a;
Oszczypko and Oszczypko-Clowes, 2010b), as well as near Humenné (Matašovsky and Andreyeva- Grigorovich, 2002) and Horna Orava (Oszczypko-Clowes et al., 2013) in Slovakia.
The Krynica fa cies Zone pro vides im por tant in sights as re - gards our un der stand ing of the ter mi nal his tory of the Magura Ba sin for ma tion. This zone re cords fa cies links with post - -nappe, Late Eocene to Oligocene bas ins of the Cen tral Carpathians: the Paleogene Ba sin and the PKB struc ture Zone (Fig. 2). In the south ern part of the Krynica Zone, the youn gest de pos its be long to the Kremna For ma tion, es tab lished by Oszczypko et al. (2005a). The Kremna For ma tion (Oszczypko et al., 2005a; Oszczypko and Oszczypko-Clowes, 2010a) is com posed of a suc ces sion of thin- to me dium-bed ded turbidites with in ter ca la tions of thick -bed ded mas sive sand stone. The up - per part is dom i nated by thin-bed ded turbidites. Lo cally the cal -
car e ous flysch of the Kremna For ma tion is in ter ca lated with grey marls of Łącko type. The age of the Kremna For ma tion is Early Mio cene, NN2 Zone (Oszczypko et al., 2005a;
Oszczypko and Oszczypko-Clowes, 2010b; Fig. 2).
PREVIOUS WORK
The first re ports of the Mid dle Mio cene ma rine de pos its (clays with gyp sum) in the Podhale re gion was given at the end of the nine teenth cen tury by Uhlig (1890). Few years later Friedberg (1906, 1912) de scribed ma rine de pos its of Mid dle Mio cene age near Szaflary. This view was ques tioned by Birkenmajer (1951) who claimed that the find ing of Mid dle Mio - cene strata in Szaflary by Friedberg (1906, 1912) was a re sult of con fu sion be tween sam ples. At the same time, geo log i cal and palynological re search in the Orava Ba sin con firmed the fresh - wa ter char ac ter and Mio/Plio cene age of these de pos its (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 de pos its (Malcov For ma tion) were dis cov ered in the Nowy Sącz Ba sin (Rača Zone), over ly - ing the Magura sand stones (Oszczypko, 1973). Sim i lar de pos - its were also doc u mented by Cieszkowski and Olszewska (1986) near Nowy Targ. A few years later, with ref er ence to the views of Friedberg (1906, 1920), Cieszkowski et al. (1991) sig -
342 Agata Kaczmarek, Marta Oszczypko-Clowes and Marek Cieszkowski
Fig. 1A – geo log i cal map of the East Al pine–Carpathian–Pannonian ba sin sys tem (af ter Picha and Pe ters, 1998);
B – sketch-map of the Pol ish Carpathians and their foredeep (based on Żytko et al., 1989, sup ple mented) Su – Siary, Ru – Rača, Bu – Bystrica, Ku – Krynica fa cies zones of the Magura Nappe;
place of in ves ti ga tion: black star with the name Rogoźnik on the map
nalled the pos si bil ity of the ex is tence of Mid dle Mio cene ma rine de pos its in the Orava–Nowy Targ Ba sin. Fi nally Cieszkowski (1992, 1995) dis tin guished four new lithostratigraphic units: the Waks mund, Stare Bystre, Kopaczyska and Pasieka units, youn ger than the Magura and Malcov for ma tions.
The data ob tained from the Nowy Targ PIG 1 bore hole al - lowed de ter mi na tion of the age of the Malcov For ma tion, based on cal car e ous nannoplankton (Smagowicz in Paul and Poprawa, 1992) rang ing from Late Eocene to Early Mio cene age. Ac cord ing to Cieszkowski (1992), these beds (in the Orava–Nowy Targ Ba sin) do not be long to the Malcov For ma - tion but to the de pos its which are youn ger than the Malcov For - ma tion, and named the Waksmund Beds.
The Waksmund Beds seem to form a tran si tional se quence be tween the Malcov For ma tion (Cieszkowski and Olszewska, 1986) and the Mio cene beds ly ing above. The strati graphic po -
si tion of these de pos its was de ter mined on the ba sis of their struc tural con text, lithological anal ogy to the Malcov and/or Magura for ma tions, as well as on micropalaeontological dat ing.
The Waksmund Beds con tain foraminifers of a wide strati - graphic range, rep re sent ing mainly Paleogene or Eocene spe - cies (Cieszkowski, 1992). How ever, the nannoplankton as sem - blages are abun dant, char ac ter ized by the pres ence of: Sphe - no lithus conicus, Sph. heteromorphus, Sph. pseudoradians and Helicosphaera cf. ampliaperta, and al lowed an age de ter - mi na tion …as the Up per Oligocene–Lower Mio cene…
(Cieszkowski, 1992). Cieszkowski and Struska (2009) in cluded the Waskmund Beds in the Malcov For ma tion.
The Stare Bystre For ma tion, de vel oped in flysch fa cies, is rep re sented by soft marls and marly shales in ter ca lated with thin and me dium-bed ded cal car e ous sand stones (Fig. 3C–E).
The de pos its, which con tain rich microfaunal as sem blages,
S N
?
KRYNICA BYSTRICA RAČA SIARY
?
MAGURA FACIES/TECTONIC ZONES TYLICZ
?
?
?
PIENINY KLIPPEN BELT
S
30 25 15
20
EARLYEARLYEARLYEARLYLATELATELATE PRIABO NIANRUPE LIANCHATTIANAQUITA NIANBURDIGA LIANLAN.BARTO NIANLUTETIANYPRESIANDANIANSELAN DIANTHANE TIAN
EOCENEOLIGOCENEMIOCENE
35
MIDDLEMIDDLE
a
a b
b c NP18
NP17
NP16
NP13
NP11 NP10 NP12
NP9 NP8 NP6 NP5
NP4
NP3 NP2 NP1 NP 15
NP 14 NP19-20
NP21 NP22 NP23
100 m
NP24 NP25 NN1 NN2 NN3 NN4 NN5
TIME SEA LEVEL
OSCILLATION (Haq et al., 1987)
EPOCH AGE NANNO ZONES
PALEOCENE
40
45
50
55
60
65
My
Malcov Fm.
Kremna Fm.
Szczawnica Fm.
Zarzecze Fm
Ropianka Fm.
Ropianka Fm.
Ropianka Fm.
Łabowa Fm.
Łabowa Fm.
Łabowa Fm.
Beloveza Fm.
Beloveza Fm.
Żeleźnikowa Fm.
Żeleźnikowa Fm.
Złockie Fm.
Łabowa Fm.
Jarmuta Fm.
Zawada Fm.
Malcov Poprad Fm.
Mb Poprad
Poprad Mb
Mb. Poprad
Mb.
Mniszek Mb. Mniszek Mb.
Piwniczna Mb.
Piwniczna Mb.
Maszkowice Mb.
Maszkowice Mb.
Życzanów Mb.
Krynica Mb.
Magura Fm.
Magura Fm
Magura Fm.
Magura Fm.
Magura Fm. Sub-Menilite
Glob. Marls
Variegated marls
Budzów Beds
Sub-Magura Beds
Wątkowa Sandstone Menilite Beds
Skawce Mb.
Pasierbiec Sandstone
Proč Jarmuta Fm.
oceanic variegated shales thin to thick-bedded calcareous sandstones, shales medium to thin-bedded sandstones, shales
Łącko type, massive marls
exotic conglomerates and thick-bedded sandstones,
thick-bedded glauconitic sandstones thick-bedded muscovitic sandstones
bituminous shales variegated marls
tuffites hornstones
Beloveza Fm.
Łosie Sandstone
PELAGITES AND HEMIPELAGITES TURBIDITIES
Fig. 2. Lithostratigraphic ta ble of the Paleogene/Early Mio cene de pos its of the Magura Nappe and Pieniny Klippen Belt (af ter Oszczypko and Oszczypko-Clowes, 2009)
LAN. – Langhian; S – Serravallian
have been de scribed from two lo cal i ties (Zaskale and Rogo - źnik/Stare Bystre). The nannoplankton as sem blages are char - ac ter ized by the pres ence of Discoaster druggii, Sphenolithus ciperoensis, Sph. heteromorphus, Sph. abies, Helicosphaera ampliaperta, H. recta, Reticulofenestra pseudoumbilica and Discoaster kugleri. Based on the nannofossil con tent, Sma - gowicz (in Cieszkowski et al., 1991) de ter mined the age of
Stare Bystre For ma tion as Mid dle Mio cene. The foraminifer anal y sis was con ducted by Olszewska (in Cieszkowski et al., 1991). The as sem blage de ter mined con tained such spe cies as:
Globorotalia miozea Finlay, Gl. ex gr. foshi Cushman, Gl.
praemen ardi Cushman, Globigerina bolli Citta et Premoli Silva, G. druryi Akkers, G. diplostomata Reuss, Gl. explicationis Jen - kins and Gl. ex gr. languaensis Bolli. Ac cord ing to Olszewska 344 Agata Kaczmarek, Marta Oszczypko-Clowes and Marek Cieszkowski
Fig. 3. Localition of the sam ples – the ex po sure of the Stare Bystre For ma tion on the bound ary be tween the vil lages of Rogoźnik and Stare Bystre in 2006
A, B – gen eral view of the ex po sure; C, D, E – yel low ish marly shales and soft marls with thin in ter ca la tion of cal car e ous sand stone; the small fold forms the front part of a small sub ma rine slump within the marly shales
(in Cieszkowski et al., 1991) such an as so ci a tion al lows for the de ter mi na tion of a Mid dle Mio cene age for the Stare Bystre For - ma tion. Gedl (1995), on the ba sis of a dinoflagellate as so ci a - tion, de scribed the age of the de pos its from Rogoźnik as Mid dle Eocene (Rhombodinium draco Zone).
The Kopaszyska Beds were ini tially called the Zaskale lay - ers (see Cieszkowski, 1992). They con sist of yel low ish, slightly co he sive, fine to me dium, rarely coarse-grained and con glom - er atic sand stones, oc ca sion ally with the oc cur rence of shales and mudstone clasts. These de pos its are poor in micro fauna, and mostly rep re sented by ag glu ti nated foraminifers:
Rhabdammina sp. Tak ing into ac count the strati graphic po si - tion, i.e. above the Stare Bystre For ma tion, the age was es ti - mated as Mid dle Mio cene.
The youn gest de pos its de scribed by Cieszkowski et al.
(1991) be long to the Pasieka Beds, de vel oped as soft marls and clays, and also of Mid dle Mio cene age. Age es ti ma tion of the youn gest di vi sions was based on strati graphic po si tion, not con firmed by biostratigraphic data. Ac cord ing to Cieszkowski (1992) the up per part of these de pos its are prob a bly the Szaflary clays de scribed by Friedberg (1906, 1909).
SECTION STUDIED
The area stud ied is lo cated be tween the vil lages of Stare Bystre and Rogoźnik. The sec tion (Fig. 3A, B) was sit u ated on the left bank of the Rogoźnik Wielki Creek (GPS co or di nates:
N49 26.506, E19 55.836). Cur rently the sec tion is com pletely cov ered by flu vial de pos its, prob a bly as an ef fect of stream ex - pan sion. For that rea son the de scrip tion be low is based on the avail able lit er a ture (Cieszkowski et al., 1991; Cieszkowski, 1992, 1995; Cieszkowski and Struska, 2009). The beds were ob served in in verted po si tion, the dip of the lay ers fac ing to the NNW at an an gle of 75–80° (330/75). The Stare Bystre For ma - tion is typ i cally a flysch de posit. The main part of the pro file con - sists of thick lay ers of marly shales and soft marls with in ter ca la - tions of coarse-grained sand stones (cal car e ous, grey-blu ish with two types of lam i na tion: cross- and par al lel, with mus co vite and plant frag ments). The up per part of the beds con sists of thin-bed ded sand stones with shale in ter ca la tions and plant frag ments (car bon ized de tri tus) while the lower part com prises fine-grained non-cal car e ous grey sand stones (Cieszko wski, 1992). Within the marly se quence, slump units of mudstone with marl clasts and de tri tus were re ported. The top of the lithostratigraphic sub di vi sion in the pro file passes into coarse-, me dium- and fine-grained, thick-bed ded sand stones typ i cal of the Magura For ma tion with in ter ca la tions of marls and marly shales, of the Łącko type (Fig. 4).
METHODS AND MATERIALS
18 sam ples (col lected by the third au thor) for cal car e ous nannofossil anal y ses, were pre pared us ing stan dard smear slide tech niques for light mi cro scope (LM). The in ves ti ga tion was car ried out us ing a Nikon-Eclipse E 600 POL, mi cro scope at a mag ni fi ca tion of 1000x us ing par al lel and crossed polars.
Quan ti ta tive anal y ses were per formed us ing counts of 300 spec i mens per slide. In or der to ana lyse and cal cu late the per - cent age abun dance of autochthonous and allochthonous as -
sem blages a 5% range er ror was ac cepted. The nom i nal val ues and per cent ages are shown in Ap pen dix 1*.
The state of pres er va tion of cal car e ous nannofossils was as sessed us ing the cri te ria of Roth and Thierstein (1972), Roth (1973) and Bown (1998). These are: G (good pres er va tion) – small dis so lu tion of skel e tons with min i mum over growth, where rec og ni tion of spe cies did not cause any prob lems, M (mod er - ate pres er va tion) – spec i mens were me chan i cally bro ken but still easy to rec og nize, P (poor pres er va tion) – spec i mens showed me chan i cal frag men ta tion and also overgrowths, VP (very poor pres er va tion) – where taxa were mostly in frag ments.
Also an at tempt to sep a rate dif fer ent stages of pres er va tion and over growth was made. Fol low ing Roth and Thierstein (1972), Roth (1973) and Bown (1998), six groups were con sid ered (3 of me chan i cal deg ra da tion and 3 of over growth):
Me chan i cal dis so lu tion:
E1 – where del i cate struc tures were de stroyed, in cocco - lith spe cies ser rate out lines were rec og nized. Cross - -struc tures in Chiasmolithus sp. and also in spe cies such as Pontosphaera, Rhabdosphaera were still ob served;
E2 – where cen tral struc tures were de stroyed (such as the grill, or cross). More del i cate spe cies were still ob - served (for ex am ple Sphenolithus and Helicosphaera);
E3 – only the most re sis tant spe cies sur vived – Coccolithus, Discoasters, Reticulofenestrid etc.
Over growth:
O1 – rays of Discoasters were thick ened, some el e - ments of placoliths are over grown;
O2 – rays were more thick ened, ray tips were not rec og - nized;
O3 – in di vid ual spe cies of Discoaster were not rec og niz - able. Placoliths cov ered strongly by cal cite, iden ti fi ca tion was dif fi cult.
In the sam ples in ves ti gated, at tempts to ac cu rately de ter - mine the con ser va tion sta tus of the spe cies caused many dif fi - cul ties, due to sev eral sources of re worked ma te rial. In all sam - ples var i ous states of pres er va tion of each spe cies were vis i ble.
There fore, in Ap pen dix 1, the states of pres er va tion were given in ranges.
In most sam ples the state of pres er va tion of the spe cies var ied from mod er ate to good tak ing into ac count the 1st and 2nd level of overgrowths.
Af ter Bown and Young (1998), spe cies abun dance lev els were di vided 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. Mod er ate (M) 5–10 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 sam ples, fre quency of spe cies oc cur rence reached level 1 (very high) to level 2 (high). The states of pres - er va tion in in di vid ual sam ples are shown in Ap pen dix 1.
RESULTS
DESCRIPTION OF THE NANNOPLANKTON ASSEMBLAGES
All sam ples were ana lysed un der the mi cro scope. Dur ing the anal y sis 128 spe cies of cal car e ous nannofossils were de - ter mined Ap pen dix 2. The spe cies iden ti fied were di vided into three as sem blages con tain ing: autochthonous, re worked and long-rang ing taxa (Fig. 5).
* Supplementary data associated with this article can be found, in the online version, at doi: 10.7306/gq.1277
AUTOCHTHONOUS ASSEMBLAGES
The autochthonous as sem blage con sists of 13 taxa. The high est share (8.1–13%) of autochthonous spe cies was ob - served in the sam ples 24/98/N, 20/98/N and 5/98/N.
Autochthonous spe cies ob served al most in all sam ples were:
Coronocyclus nitescens (Fig. 6E, F), Pontosphaera multipora, Spenolithus disbelemnos (Fig. 6P–U) and Sph. dissimilis (Fig.
6W, Y). Other spe cies, found only in some sam ples were:
Braarudosphaera bigelowii (Fig. 6A), Calcidiscus leptoporus (Fig. 6B), Discoaster deflandrei (Fig. 6H), Helicosphaera carteri (Fig. 6J–M), H. obliqua, Reticulofenestra daviesii, R. minuta
and R. haqii. Per cent ages of the most abun dant autochthonous taxa are shown in Fig ure 7.
The high est per cent age of all taxa de ter mined was of Coronocyclus nitescens. The high est rate of oc cur rence of this spe cies was found in sam ples 6/98/N (2.2%) and 5/98/N (1.9%). Clacidiscus leptoporus is most abun dant in sam ples 24/98/N and 8/98/N (2.2%). How ever, this spe cies was not ob - served in 5 sam ples, mak ing its over all per cent age smaller than that of other two spe cies from that group. The per cent age of Pontosphaera multipora was sig nif i cantly higher than that of Calcidiscus leptoporus (Ap pen dix 1), the high est rate of oc cur - rence of this spe cies be ing found in sam ples 16/98/N and
346 Agata Kaczmarek, Marta Oszczypko-Clowes and Marek Cieszkowski
Fig. 4. Lithostratigraphical logs of the Stare Bystre For ma tion (af ter Cieszkowski, 1992)
19/98/N (2.5%) (Fig. 7). Other spe cies in the autochthonous group were ob served in smaller quan ti ties; in most cases they did not reach 6%, with two ex cep tions: Reticulofenestra minuta (8.6%) and Sphenolithus conicus (Fig. 6P, R), which al most reached 10% (9.8% in to tal per cent age; Ap pen dix 1).
REWORKED ASSEMBLAGES
In all sam ples 112 re worked taxa were rec og nized. These were mainly Paleogene and Eocene spe cies.
In al most all sam ples spe cies of the ge nus Fasciculithus were iden ti fied. In re worked as sem blages, some Cre ta ceous spe cies were also ob served, which be cause of their low amounts were not de ter mined to spe cies level. The sam ples also in cluded rep re sen ta tives of the ge nus Ericsonia the size of which did not al low spe cies-level iden ti fi ca tion. In Ap pen dix 1 these spec i mens were de scribed as “small Ericsonia”. The great est spe cies di ver sity in the re worked as sem blages was ob served in the gen era Chiasmolithus, Discoaster or Spheno - lithus. The vari abil ity of the per cent age of each spe cies within the ge nus is shown on the Fig ure 8.
The high est con tent of the ge nus Chiasmolithus was ob - served in sam ple 19/98/N (al most 3.5% – Fig. 8). The most com mon spe cies is Chiasmolithus grandis, the per cent age of all sam ples reach ing 7.3% (Ap pen dix 1), most fre quently rep - re sented in the sam ples 8/98/N and 19/98/N. Other fre quently oc curred spe cies within the ge nus in cluded Chiasmolithus solitus (3.8%), most nu mer ous in sam ple 8/98/N and Chias - molithus expansus (3.5%), most fre quent in sam ple 19/98/N (Ap pen dix 1).
The high est con tent of the ge nus Discoaster was ob served in sam ple 16/98/N (al most 10.8% – Fig. 8). The most com mon spe cies in the ge nus Discoaster was Discoaster barbadiensis, the per cent age of its ap pear ances in all sam ples be ing 12.7%
(Ap pen dix 1); it was most of ten ob served in sam ple 16/98/N.
The high est con tent of the ge nus Sphenolithus was ob served in sam ple 6/98/N (Fig. 8).
Within the ge nus Sphenolithus the most com mon spe cies was Sph. ra di ans, the sum of the per cent age oc cur rences of that spe cies in all sam ples amount ing to 20.3% (Ap pen dix 1). It was most widely rep re sented in the sam ples 6/98/N, 8/98/N and 19/98/N. An other fre quently ob served spe cies was Sph. editus (8.55%), its high est share of spe cies be ing in sam ple 8/98/N (Ap pen dix 1).
Among re worked as sem blages in each sam ple, Blackites spinosus, Ericsonia formosa, Semihololithus kerabyi, Toweius callosus, T. magnicrassus, T. rotundus, Zygrhablithus bijugatus and nu mer ous Transversopontis pulcher and Tribrachiatus orthostylus were also ob served. The high est con tri bu tion of re - worked taxa in sam ples from the pro file in Stare Bystre amounted to 79.5% in sam ple 6/98/N (Fig. 9). The most nu mer - ous spe cies rep re sented in the allochthonous as sem blages were Zygrhablithus bijugatus, Toweius rotundus, T. callosus and Blackites spinosus (Fig. 9). The per cent age of Zygrha - bilitus bijugatus in three sam ples (18/98/N, 13/98/N and 15/98/N) is >15% (Fig. 9). The per cent age of Toweius rotundus in three sam ples (11/98/N, 6/98/N and 7/98/N) is >15% and in the sam ple 20/98/N the spe cies is ab sent (Fig. 9). The per cent - age of Blackites spinosus vary, the high est per cent ages be ing ob served in sam ples 9/98/N and 16/98/N, while this spe cies was not ob served in sam ples 15/98/N and 19/98/N (Fig. 9). The small est per cent age in de scribed parts of the re worked as sem - blages com prised Toweius callosus, iden ti fied in all sam ples stud ied (Fig. 9).
LONG-RANGING TAXA
In all sam ples con sid ered, be sides a sig nif i cant level of re - de pos ited taxa, spe cies with very long strati graphic ranges, were also ob served. For this rea son, they were not in cluded in autochthonous or re worked as sem blages, and have been sep - a rated as a group of long-rang ing taxa. These spe cies are mostly cos mo pol i tan and also re sis tant to poor en vi ron men tal Fig. 5. The per cent age of autochthonous, re worked and long-rang ing taxa in the sam ples col lected
from the Stare Bystre sec tion
348 Agata Kaczmarek, Marta Oszczypko-Clowes and Marek Cieszkowski
Fig. 6. LM mi cro pho to graphs of cal car e ous nannofossils from sam ples from the Stare Bystre For ma tion
A – Braarudosphaera bigelowii (Gran and Braarud, 1935) Deflandre (1947) sample11/98/N (xN); B – Calcidiscus leptoporus (Murray and Blackman, 1898) Loeblich and Tappan (1978) sam ple 24/98/N (xN); C – Coccolithus pelagicus (Wallich, 1877) Schiller (1930) sam ple 14/98/N (xN); D – Coccolithus pelagicus (Wallich, 1877) Schiller (1930) sam ple 14/98/N (1N); E – Coronocyclus nitescens (Kamptner, 1963) Bramlette and Wilcoxon (1967) sam ple 20/98/N (xN); F – Coronocyclus nitescens (Kamptner, 1963) Bramlette and Wilcoxon (1967) sam ple 20/98/N (1N); G – Cyclicargolithus luminis (Sullivan, 1965) Bukry (1971) (xN); H – Discoaster deflandrei (Bramlette and Riedel, 1954) sam - ple 5/98/N (1N); I – Discoaster lodoensis (Bramlette and Riedel, 1954) sam ple 8/98/N (1N); J – Helicosphaera carteri (Wallich, 1877) Kamptner (1954) sam ple 4/98/N (xN); K – Helicosphaera carteri (Wallich, 1877) Kamptner (1954) sam ple 4/98/N (1N); L – Helicosphaera carteri (Wallich, 1877) Kamptner (1954) sam ple 24/98/N (xN); M – Helicosphaera carteri (Wallich, 1877) Kamptner (1954) sam ple 24/98/N (1N); N, O – Sphenolithus conicus (Bukry, 1971) sam ple 5/98/N (xN); P–U – Sphenolithus disbelemnos (Fornaciari and Rio, 1996) sam ple 21/98/N (xN); W, Y – Sphenolithus dissimilis (Bukry and Percival, 1971) sam ple 6/98/N (xN); Z – Sphenolithus moriformis (Brönnimann and Stradner, 1960) Bramlette and Wilcoxon (1967) sam ple 12/98/N (xN); Z – Zygrhablitus bijugatus (Deflandre in: Deflandre and Fert, 1954) Deflandre (1959) and Semihololithus kerabyi (Perch-Niel sen, 1971) (xN); I. – Zygrhablitus bijugatus, II. – Semihololithus kerabyi; 1N – plane par al lel polars, xN – crossed polars
Fig. 7. The vari abil ity of the per cent age of the most abun dant autochthonous taxa in sam ples from the Stare Bystre sec tion
Fig. 8. The per cent age of vari abil ity of in di vid ual spe cies within the ge nus Sphenolithus, Discoaster and Chiasmolithus in sam ples from the Stare Bystre vil lage ex po sure
con di tions. Among the group of heterococcoliths, two spe cies in the ge nus Coccolithus were dis tin guished: C. pelagicus (Fig.
6C, D) and C. eopelagicus (range of oc cur rence from Danian to re cent), and two spe cies from the ge nus Cyclicargolithus: Cy.
floridanus (Eocene to Mio cene) and Cy. abisectus (Oligocene to Early Mio cene). In that group one spe cies of Sphenolithus – Sph. moriformis (Fig. 6Z; Eocene to Late Mio cene) was noted and also one spe cies from the nannolith fam ily: Braarudo - sphaera bigelowii (Fig. 6A) – which oc curs in the oceans to the pres ent day, as so ci ated with a neritic en vi ron ment (Gran and Braarud, 1935).
INTERPRETATION
BIOSTRATIGRAPHY
The age of the Stare Bystre For ma tion was es tab lished as Early Mio cene – NN2, us ing stan dard nannoplankton zonation (Mar tini and Wors ley, 1970). The age was de ter mined on the ba - sis of the co-oc cur rence of Cyclicargolithus floridanus, Helicosphaera carteri, Sphenolithus conicus, Sph. dissimilis and Sph. disbelemnos. Ac cord ing to Fornaciari and Rio (1996) and Young (1998) Sph. disbelemnos is typ i cal of the NN2 Zone (Fig.
10). An as tro nom i cal age for Sph. disbelemnos was pro posed by Shackle ton et al. (2000; see also Raffi et al., 2005). The spe cies ap pears at 22.67 Ma and it is shown to be an im por tant da tum level for the Paratethys re gion (Rögl and Nagymarosy, 2004;
Oszczypko-Clowes in: Oszczypko et al., 2005a).
At the same time Dictyococcites bisectus, Cyclicargolithus abisectus and Zygrhablithus bijugatus are ab sent from this as - so ci a tion. Ac cord ing to Perch-Niel sen (1985), Berggren et al.
(1995), Fornaciari et al. (1996) and Young (1998) the LO of Dictyococcites bisectus de fines the base of NN1. Thus, one can as sume that the age of the Stare Bystre For ma tion is not older than NN2 (Aquitanian/Burdigalian).
AGE OF THE REWORKED ASSEMBLAGES
Re de pos ited spe cies can help to de ci pher both the his tory of ter res trial ero sion around the ba sin area, as well as the di rec tion and in ten sity of the trans port of eroded ma te rial. In the Magura suc ces sion, within the area in ves ti gated, flysch de po si tion was
mainly ob served, in volv ing tur bid ity cur rents from a con ti nen tal slope. Biostratigraphical stud ies have shown the very high util ity of cal car e ous nannoplankton in turbidites. This is the re sult of the small size of nannofossils with at the same time large num bers of var i ous taxa pre served in a small por tion of rock (Siesser, 1993).
Cal car e ous nannoplankton are ide ally pre served in mud-clay ma te rial, which forms a nat u ral shield to the small nannofossil skel e tons, pro tect ing them from deg ra da tion dur ing trans port (Mikes et al., 2008; Oszczypko-Clowes, 2012). In the sam ples ex am ined, the pro por tion of re worked taxa reaches >50% of all ob served spe cies. The age of the re worked as sem blages var ies across a wide time range. In the ma te rial stud ied, Cre ta ceous, Paleocene, Eocene and Oligocene taxa were ob served, though with no tice able, sig nif i cant pre dom i nance of Paleogene taxa over Cre ta ceous ones (Fig. 11).
350 Agata Kaczmarek, Marta Oszczypko-Clowes and Marek Cieszkowski
Fig. 9. The per cent age of the most abun dant allochthonous spe cies in the as sem blages from the Stare Bystre sec tion
Fig. 10. Biostratigraphic po si tion of the Stare Bystre For ma tion (grey field)
The con tri bu tion of Cre ta ceous spe cies in re worked as sem - blages does not ex ceed 5.07% (sam ple 24/98/N), whereas the Paleogene spe cies can reach >80% of all spe cies in the sam - ples in ves ti gated (Fig. 6).
The as sem blages are mixed with spe cies from dif fer ent time in ter vals:
– The Lower Eocene as sem blage is rep re sented by Disco aster multiradiatus (range: NP9-11), Discoaster lodo ensis (NP12-14; Fig. 6I) and Tribrachiatus ortho - stylus or Toweius crassus.
– The pres ence of the Mid dle Eocene (NP15 zone) could be dated by the Chiasmolithus gigas zonal marker or by Nanotetrina quadrata.
– Long-rang ing spe cies, span ning from the Mid Eocene to the Early Oligocene, in clude: Discoaster tanii nodifer (NP16 -22), Helicosphaera bramlettei (NP14-23), Lan - ter ni thus minutus (NP16-22), Reticulofenestra umbilica (NP16 -22), Disco aster barbadiensis (NP10-20), Dictyo - coccites bisectus (NP17-24), Discoaster saipanensis (NP14-23) and Ismolithus recurvus (NP19-22).
– In ad di tion, typ i cal Oligocene taxa in clude: Sphenolithus ciperoensis (FO), Pontosphaera latelliptica, Transverso - pontis fib ula and, very rarely, Sph. capricornutus and Sph. calyculus.
DISCUSSION
The age of the Stare Bystre For ma tion was as signed to the Early Mio cene – Aquitanian/Burdigalian (NN2 Zone). The age de ter mi na tion was made on the pres ence of Sphenolithus disbelemnos in al most all sam ples (Fig. 6P–U) which ac cord ing to Young (1998) is an in dex spe cies for the lower part of the NN2 nannoplankton zone. Such age de ter mi na tion is in con - trast to the pre vi ous works de scrib ing the age of Stare Bystre
For ma tion as Mid dle Mio cene (Badenian/Sarmatian) (Ciesz - kowski et al., 1991; Cieszkowski, 1992, 1995). The age of the de pos its in pre vi ous works was based on the pres ence of Discoaster drugii, Sphenolithus ciperoensis, Sph. hetero mor - phus, Sph. abies, Helicosphaera ampliaperta, H. recta, Reti - culo fenestra pseudoumbilica and Discoaster kugleri (Smago - wicz in Cieszkowski et al., 1991). Ac cord ing to the pre vi ous works con sid er ing the stan dard zonation of Mar tini (1971) and Mar tini and Wors ley (1970), the first oc cur rence of Reticulo - fenestra pseudoumbilica takes place in NN5, how ever, this taxon was re ported by Marunteanu (1991) from the lower limit of NN2, while Holcová (2013) also ques tioned the Mid dle Mio cene age of Reticulofenestra pseudoumbilica. Holcová (2013) di - vided the reticulofenestrid group on the ba sis of their size and also no ticed dif fer ences be tween the first ap pear ances of these spe cies in the global ocean and in the Cen tral Paratethys, in which the larger spe cies ap pear a lit tle ear lier. Ac cord ing to Holcová (2013), the small est spe cies (i.e. R. haqii <4 mm) has a FO (first oc cur rence) in zone NP25 in the Paratethys, whereas in the global ocean it was in zones NN1/NN2. Sim i larly the spe - cies of R. pseudoumbilicus >5 mm first re port edly ap peared at the end of the Oligocene. Holcová (2013) also sug gested that dif fer ent sizes in the R. haqii-pseudoumbilicus group de pended on the sea son al ity in the ocean (smaller spe cies in win ter and larger in the sum mer). Larger taxa of Reticulofenestrid >7 mm (Holcova, 2012) ap pear in the NN4 Zone and >8 mm in the NN5 Zone. Cieszkowski et al. (1991) did not men tion the size of Reticulofenestra pseudoumbilicus and there fore a ref er ence to this spe cies will not be con sid ered.
In our opin ion, the most im por tant spe cies men tioned by Smagowicz (in Cieszkowski et al., 1991), which de ter mined the age of the Stare Bystre For ma tion are: Sphenolithus abies, the first ap pear ance of which is in the NN6 Zone (Sarmatian, Tortonian) (Perch-Niel sen, 1985; Bown, 1998), and Discoaster kugleri, which is an in dex taxa for the NN7 Zone (Sarmatian) in the stan dard zonation (Mar tini, 1971).
Fig. 11. Com par i son of the per cent age of Cre ta ceous and Paleogene spe cies in in di vid ual sam ples from the Stare Bystre pro file
Spe cies such as: Discoaster drugii, Sphenolithus ciperen - sis, Sph. heteromorphus, Sph. abies, Helicosphaera amplia - perta, H. recta, Reticulofenestra pseudoumbilica and Disco - aster kugleri are not pres ent. In such cases the Mid dle Mio cene age of Stare Bystre For ma tion can not be sup ported.
The autochthonous as sem blage shows mostly tem per ate and warm-wa ter taxa, typ i cal of the grad ual Early Mio cene in - crease in sur face wa ter tem per a ture. These in clude Spheno - lithus spe cies such as Sph. conicus (Fig. 6N, O), Sph. disbele - mnos (Fig. 6P–U) and Sph. dissimilis (Fig. 6W, Y). Also, the fol - low ing spe cies were ob served in all sam ples: D. deflandrei (Fig.
6H), H. carteri and H. obliqua. In the long-rang ing group there was also no tice able Cyclicargolithus floridanus which is an in di - ca tor of tem per ate wa ter (Wei and Wise, 1990).
From the lithological point of view the Stare Bystre For ma - tion is char ac ter ized by the oc cur rence of Magura-type sand - stones and thin-bed ded flysch lay ers with the Łącko type of marlstones. Con sid er ing the age, qual i ta tive and quan ti ta tive com po si tion of nannoplankton as sem blages and also litho - facies com po si tions, a strong cor re la tion be tween the Stare Bystre For ma tion and the Kremna and Zawada for ma tions is no tice able (cf. Oszczypko et al., 1999, 2005a; Oszczypko and Oszczypko-Clowes, 2002; Oszczypko-Clowes, 2012).
Within re worked as sem blages a sig nif i cant pre dom i nance of Paleogene spe cies over Cre ta ceous ones was ob served, from which one can in fer that they were trans ported with the mass of sed i ment in grav ity flows. All Paleogene spe cies within the re worked as sem blages were better pre served than in dig e - nous or Cre ta ceous ones, and have a much larger size sug - gest ing a good re sis tance to me chan i cal dam age dur ing trans - port. With the growth of the accretionary prism, eroded older ma te rial (from Cre ta ceous de pos its) also ap peared. In the sam - ples within the re worked as sem blages youn ger Oligocene taxa were also ob served, sug gest ing the pres ence of an other source of ma te rial. This could have been the prod ucts of ero - sion of youn ger de pos its from the bot tom of the ba sin, prob a bly re lated to the pres ence of mud vol ca noes, which in com bi na tion of de hy dra tion of the ma te rial led to ex trac tion and ero sion from the bot tom of the ba sin. This type of pro cess is char ac ter is tic of the dy nam ics of an accretionary prism (Mikes et al., 2008;
Oszczypko-Clowes, 2012). A sim i lar de gree of redeposition were de scribed in the Mio cene tur bid ity de pos its from the PKB and also other Magura Nappe zones: Krynica, Tylicz and Bystrica, e.g. within the Kremna For ma tion (Oszczypko-Clowes in: Oszczypko et al., 2005a) or Zawada For ma tion from the Lubovnianska Vierchovina sec tions (Oszczypko and Oszczy - pko -Clowes, 2002). Dur ing the Late Oligocene (NN25/NN1) the fron tal part of the Magura Nappe thrust north wards onto the ter - mi nal Krosno flysch ba sin. The north wards thrust ing of the Magura Nappe was ac com pa nied by the for ma tion of the piggy - -back ba sin on the Magura Nappe, filled with the synorogenic turbidites be long ing to the Zawada (Oszczypko et al., 1999), Kremná (Oszczypko at al., 2005a) and Stare Bystre for ma tions (NN2). Dur ing the Early/Mid dle Mio cene, the Magura Nappe was fi nally folded and flatly thrust north wards over the Fore-Magura Group of Nappes and, to gether with these, upon the Silesian Nappe.
CONCLUSIONS
1. On the ba sis of cal car e ous nannoplankton, the age of the Stare Bystre For ma tion was as signed to the Burdigalian age (NN2 Zone).
2. Nannofossil anal y ses did not con firm a Bade nian–Sar - ma tian age for the Stare Bystre For ma tion.
3. The nannofossil as sem blages show high con tents of re - worked spe cies which are mostly of Eocene and Oligocene age.
4. On the ba sis of lithological and biostratigraphical sim i lar i - ties, the Stare Bystre For ma tion can be cor re lated with the Kremna and Zawada for ma tions.
Ac knowl edge ments. The au thors ex press their pro found grat i tude to all the re view ers of this work (K. Holcová, Anon y - mous and D. Ghita) for their in sight ful com ments, im por tant sug ges tions and help in the pro cess of writ ing, and to the ed i - tors, T.M. Peryt and E. Dąbrowska-Jędrusik, for their ed i to rial as sis tance.
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