Krzysztof Bąk, Marta Bąk, Marzena Cieśla & Zbigniew Paul

FORAMINIFERAL STRA TIG RA PHY OF PALAEOGENE

DEEP-WA TER RED FA CIES IN THE GORCE MOUN TAINS

(MAGURA NAPPE, POL ISH OUTER CARPATHIANS)

1

In sti tute of Ge og ra phy, Ped a gog i cal Uni ver sity of Cra cow, Podchor¹¿ych 2, 30-084 Kraków, Po land; e-mail: sgbak@cyf-kr.edu.pl

2

Fac ulty of Ge ol ogy, Geo phys ics and En vi ron men tal Pro tec tion, Uni ver sity of Sci ence and Tech nol ogy, Aleje Mickiewicza 30, 30-059 Kraków, Po land

3

In sti tute of Geo log i cal Sci ences, Jagiellonian Uni ver sity, Oleandry 2a, 30-063 Kraków, Po land 4

Pol ish Geo log i cal In sti tute, Carpathian Branch in Cra cow, Skrzatów 1, 31-560 Kraków, Po land B¹k, K., B¹k, M., Cieœla, M. & Paul, Z., 2013. Foraminiferal stra tig ra phy of Palaeogene deep-wa ter red fa cies in the Gorce Moun tains (Magura Nappe, Pol ish Outer Carpathians). Annales Societatis Geologorum Poloniae, 83: 201–212. Ab stract: The de po si tion of red and var ie gated mudstones and claystones char ac ter ized the an cient Tethys Ocean dur ing Cre ta ceous and Palaeogene times, in clud ing in its north-west ern part, the Al pine–Carpathian deep-wa ter bas ins. Palaeogene var ie gated sed i ments, con tain ing red mudstone and claystone lay ers, crop out in the Gorce Moun tains (Rosocha creek, near Lubomierz) in the Magura Nappe (Bystrica Sub unit) of the Pol ish Outer Carpa-thians. These sed i ments oc cur as lay ers 1–10 cm thick and as pack ages of lay ers 2–3 m thick that are as so ci ated with very thin-bed ded turbidites. The en tire suc ces sion is tec toni cally dis turbed and parts of it be long to the Ro-pianka, £abowa Shale and Beloveža For ma tions. The sed i ments stud ied con tain 27 gen era and 59 spe cies that be long to deep-wa ter ag glu ti nated foraminiferal (DWAF) as sem blages. Tu bu lar taxa, which are fre quent in va-r i ous Me so zoic–Ce no zoic flysch sed i ments ava-re va-rel a tively va-rava-re in the sec tion stud ied. The as sem blages ava-re mod e-r ately di vee-rse (3–20 taxa pee-r sam ple). Ex clud ing tu bu lae-r foe-rms, the most com mon taxa be long to Te-rochamminoi- Trochamminoi-des – ParatrochamminoiTrochamminoi-des spp., Saccammina pla centa, glomospirids, RecurvoiTrochamminoi-des – Recurvoidella spp. and karrerulinids. The old est part of the red sed i ments, re fer able to the Ropianka For ma tion, rep re sents the up per part of the Rzehakina fissistomata Zone (prob a bly the Up per Palaeo cene). The youn gest red sed i ments, form ing thin in ter ca la tions in the Beloveža For ma tion, rep re sent the acme of Reticulophragmium amplectens (mid dle Lute-tian). Ow ing to tec tonic dis tur bances, most of the Lower Eocene part of the var ie gated fa cies of the £abowa Shale For ma tion is not pre served in the sec tion stud ied. The up per part of it, a pack age 2 m thick, rep re sents the lower part of the Reticulophragmium amplectens Zone. The small thick ness (10–15 m) of the £abowa Shale For ma tion in the sec tion stud ied is sim i lar to other sec tions in the south ern part of the Bystrica Sub unit. It is prob a bly of a sed i men tary na ture, re flect ing a de creas ing num ber of mud-rich, grav i ta tional flows in the south ern part of the Magura Ba sin dur ing the Early Eocene. Nev er the less, the strong tec tonic dis tur bances that took place in this area dur ing the Oligocene–Mio cene fold ing and overthrusting in flu enced the re duc tion in thick ness of these sed i ments. Key words: Ag glu ti nated Foraminifera, red claystones and mudstones, Palaeo cene, Eocene, Magura Nappe, Pol ish Outer Carpathians, Gorce Moun tains.

Manu script re ceived 13 November 2013, ac cepted 23 December 2013

IN TRO DUC TION

The de po si tion of red and vari col oured (both red and green) mudstones and claystones was char ac ter is tic for the an cient Tethys Ocean dur ing Cre ta ceous and Palaeogene times (e.g. Hu et al., 2012). This was the case in the north-west ern part, which in cluded the Carpathian deep-wa ter ba-sins (cf., B¹k, 2002; Hu et al., 2005). In the Outer Carpa-thians, sed i men ta tion of these claystones and mudstones con tin ued up to the end of the Eocene (Ksi¹¿kiewicz, 1962; Jurkiewicz, 1967). It ended with the de po si tion of white cal

-car e ous pe lagic sed i ments of the Globigerina Marl (Lesz-czyñski, 1997). The red claystones and mudstones in the Cre ta ceous–Palaeogene de pos its of the Carpathians (e.g., Œl¹czka, 1963; Koszarski, 1966; Traczyk, 1978) re sem ble those from the At lan tic and Pa cific Oceans (Biscaye, 1965; Gleason et al., 2002). Nev er the less, the rate of sed i men ta -tion of these de pos its was strictly con trolled by grav i ta -tional flows, which were gen er ated on the slopes of the sur round -ing and intrabasinal ridges (cf., Leszczyñski and Uchman,

1991; Oszczypko and OszczypkoClowes, 2006). Con se quently, their thick ness and re stricted lat eral ex ten sion dif fer from one ba sin to an other, and even within the same ba -sin (sum mary in Oszczypko et al., 2006).

Rec og ni tion of the strati graphic po si tion of the var ie -gated fa cies in the Carpathians is dif fi cult, ow ing to the Oligocene–Mio cene thrust ing and fold ing, which were es pe -cially strong within mudstone-siltstone siliciclastic sed i -ments. More over, these sed i ments are de void of cal car e ous nanno- and microfossils, which are the most im por tant stra-tigraphic in di ca tors. In such cases, the only strati graphic data come from si li ceous microfossils, in clud ing radiolarian and ag glu ti nated foraminiferal as sem blages (e.g., B¹k M., 1995; Sanfilippo and Nigrini, 1998; B¹k and Barwicz-Pis-korz, 2005, 2006; Barwicz-Piskorz and Rajchel, 2012).

In the Outer Carpathians, the red-col oured fa cies, mainly claystones and mudstones, were char ac ter is tic of the Turo-nian–Campanian (Late Cre ta ceous) and the Early–Mid dle Eocene times in all tec tonic and fa cies units (sum mary in Oszczypko, 2006; Olszewska and Malata, 2006). This pa per pres ents the re sults of strati graphic stud ies of the Palaeo-gene red fa cies, be long ing to the Bystrica Sub unit of the Ma-gura Nappe, Pol ish Outer Carpathians, out crop ping in the Gorce Moun tains. These sed i ments were ac cu mu lated in the Magura Ba sin be low the CCD, as doc u mented by com po si tion of as sem blages of ben thic Foraminifera, which are de -void of cal car e ous forms (e.g., Olszewska and Malata, 2006). The sur round ing ridges were af fected by tec tonic ac tiv ity, which gen er ated grav i ta tional flows that spread across the basin floor. Con se quently, sed i men ta tion of the red claystones and mudclaystones was spo radic and re lated to the for ma tion of pack ages of siliciclastic (partly cal car e ous) thinbed -ded turbidites.

GEO LOG I CAL SET TING

The Palaeogene (mainly Lower–Mid dle Eocene) var ie -gated claystones in clud ing red lay ers, oc cur in all tec tonic-fa cies units in the Magura Nappe (sum mary in Oszczypko, 2006). The sec tion stud ied is in the Bystrica Sub unit, the sed i ments of which form the north ern foot of the Gorce Moun tains, one of the high est re gions in the Pol ish part of the Beskidy Range (Fig. 1). In this area, the ridges are built of thickbed ded sand stones, be long ing to the Magura For -ma tion (Fig. 1D), while the val leys are de vel oped along the

faults and within the thin- and mid dle-bed ded turbidites of the Ropianka, £abowa Shale and the Beloveža For ma tions. Red Palaeogene sed i ments oc cur in sev eral lithostratigra-phic units, but their thick ness is great est in the £abowa Shale For ma tion. The de tailed lithostratigraphy of this area (Tab. 1) was pre sented by Oszczypko et al. (2005).

Geo log i cal sec tion and lithostratigraphy

The sec tion stud ied lies along the Rosocha Creek, a left trib u tary of the Mszanka River, in the vi cin ity of the Lubo-mierz vil lage, about 50 km south of Kraków (Fig. 1B, C). The Rosocha val ley is on the north ern slopes of Mt. Kud³oñ (1274 m a.s.l.). In the mid dle part of this val ley (Fig. 1D), sed i ments be long ing to the Ropianka, the £abowa Shale and the Beloveža For ma tions are ex posed on both banks of the stream for a dis tance of about 150 m (Fig. 2). Four pack -ages with red claystones and mudstones oc cur within all of these for ma tions, in clud ing:

– red, poorly cal car e ous claystones and mudstones, as a thin (3–10 cm) in ter ca la tions in the turbiditic suc ces sion (ca 30 m thick) of the Ropianka For ma tion (pack age 1; Fig. 2). These turbidites con tain thin-bed ded (up to 4 cm) mudsto-nes and very fine-grained sand stomudsto-nes, par al lel- and cross-laminated, some of them with trace fos sils. The sand stones pass up wards into grey-blue cal car e ous shales. A sin gle, yel low layer of ben ton ite, 2 cm thick, also was found there; – red, non-cal car e ous claystones and mudstones, 3 m thick, rep re sent ing a part of the £abowa Shale For ma tion (package 2; Fig. 2). These red sed i ments are in tec tonic con tact with a suc ces sion of thickbed ded (0.7–1.0 m) sand -stones, 3 m thick;

– red, non-cal car e ous claystones and mudstones (1–3 cm thick), as in ter ca la tions in a turbidite suc ces sion, 4 m thick, which be longs to the Beloveža For ma tion (pack age 3; Fig. 2). The turbidites con tain very thin-bed ded mudstones (1–4 cm thick), in ter ca lated with the vari col oured claystones and mudstones, which pre dom i nate in this suc ces sion. The neigh -bour ing strongly folded pack ages of turbidites, de void of any in ter ca la tions of red shale, also be long to the Belo veža For -ma tion;

– red, poorly cal car e ous claystones and mudstones, in sed i men tary con tact with thick-bed ded sand stones (at least 1.5 m thick), sim i lar to those, which are in tec tonic con tact with pack age 2 (the £abowa Shale For ma tion), and to those in the mid dle part of the sec tion (pack age 4; Fig. 2). The red

Ta ble 1

Lithostratigraphy of Campanian–Mid dle Eocene sed i ments of the Bystrica Sub unit (Magura Nappe, Outer Carpathians) in the Gorce Moun tains and the Beskid Wyspowy Moun tains (sum ma rized af ter Oszczypko et al., 2005)

Stage Lithostratigraphic unit Thickness

Accumulation rate (m/Myr) (calculated from Oszczypko and

Oszczypko-Clowes, 2006)

Early–Middle Eocene Beloveža Formation 50–120 m 25–60

Early Eocene £abowa Shale Formation 200150 (? 200) m 3–20 (? 30) Maastrichtian-Palaeocene Ropianka Formation 80–100 m 15–20 Campanian-Maastrichtian Szczawina Sandstone Formation 20–350 m 5–65

sed i ments and sand stones form here a small anticline, which is in tec tonic con tact with the folded turbidites of the Belo-veža For ma tion. Most prob a bly these red sed i ments be long to the £abowa Shale For ma tion, cor re spond ing to pack age 2, which oc curs in the same strati graphic po si tion.

The sed i ments of the £abowa Shale For ma tion and sur -round ing units lie within the Konina–Lubomierz Thrust

Sheet that forms the south ern part of the Bystrica Sub unit in the Magura Nappe. This thrust sheet is in tec tonic con tact with the Krynica Sub unit at a dis tance of 2.2 km to the south of the sec tion stud ied. The Krynica Sub unit is com posed of a thick suc ces sion of Up per Cre ta ceous–Oligocene turbidi-tes in this area (Birkenmajer and Oszczypko, 1989).

Fig. 1. Lo ca tion of study area. A. Outer Carpathians (OC) against the back ground of a sim pli fied geo log i cal map of the Al pine orogens and their fore land; IC – In ner Carpathians, CF – Carpathian Foredeep, PKB – Pieniny Klippen Belt. B, C. Lo ca tion of study area in Pol ish part of Carpathians (B) with con tour map (C) of the sur round ings of Lubomierz vil lage (Gorce and Beskid Wyspowy Moun tains; Bryndal, 2011). D. Geo logic map of study area (af ter Oszczypko et al., 2005; sup ple mented) with lo ca tion of sec tion, stud ied at Rosocha Creek (black rect an gle)

MA TE RIAL AND METH ODS

Four sec tions, con tain ing red claystones and mudsto-nes, were sam pled dur ing the pres ent study (Figs 2, 3). The red sed i ments vary in the de tails of their li thol ogy, with re -gard to the cal cium car bon ate con tent (see Fig. 3), which was iden ti fied by its re ac tion with di lute hy dro chlo ric acid. The red claystones of the £abowa Shale and in the Beloveža for ma tions are cal cium car bon ate free.

The micropalaeontological stud ies were based on agg-lutinated foraminifers. Radio lar ians have not been found there. A stan dard pro ce dure for the prep a ra tion of micropalaeontological slides was em ployed. It in cluded the ex trac tion of mi -crofossils from 16 sam ples, weigh ing 20–300 g, which were dried and dis in te grated by re peated heat ing in a so dium car -bon ate so lu tion, dried, and then sieved, us ing a 63 µm mesh. The sam ples and the res i dues were weighed be fore and af ter the ex trac tion pro ce dure to mea sure the num ber of spec i mens in 1 gram of the sed i ment. All foraminiferal spec i -mens were picked and placed on microfaunal slides.

RE SULTS

The foraminiferal as sem blages in red claystones, presented in Ta ble 2, rep re sent only the deepwa ter ag glu ti -nated forms. Tu bu lar taxa, which are fre quent in the

hemi-pe lagic sed i ments of var i ous flysch bas ins (e.g., Kuhnt and Kaminski, 1989; Kaminski et al., 1996; B¹k, 2004), as dis -tinct from turbidite de pos its, are rel a tively rare in the sec tions stud ied. They are dom i nated by forms, be long ing to

Rhabda-mmina, Psammosiphonella, Nothia and Bathysiphon. Their

num bers in crease in the claystones of the fine-grained tur-bidites of the Beloveža For ma tion. The rel a tive abun dance of deep-wa ter ag glu ti nated foraminifera (DWAF) per gram of sed i ment, var ies from sam ple to sam ple, from 4 to 43 spec i -mens, de pend ing on the type of sed i ment. Most prob a bly, some sam ples with a very low di ver sity value in dex be long to a mixed layer of the Te part of the Bouma se quence from the mudstone part of the turbidite and the true hemipelagic layer, which are mac ro scop i cally dif fi cult to dif fer en ti ate.

27 gen era and 59 spe cies of DWAF were iden ti fied in sam ples from the red sed i ments and the sur round ing shales. The as sem blages are mod er ately di verse (be tween 3 and 20 taxa per sam ple). Ex clud ing tu bu lar forms, sim i lar as sem -blages char ac ter ize the red pack ages of all of the for ma tion (Fig. 4). The most com mon taxa be long to

Trochamminoi-des (Fig. 5P) – ParatrochamminoiTrochamminoi-des spp., Saccammina placenta, glomospirids, Recurvoides (Fig. 5M, N) – Re cur-voidella spp. and karrerulinids (Fig. 5H–L). Some spe cies

are char ac ter is tic for par tic u lar red shale pack ages. This re -lates to the more com mon oc cur rences of glomospirids in the £abowa Shale For ma tion and of Karrerulina conversa in the Ropianka For ma tion.

Fig. 2. Geo log i cal cross-sec tion along Rosocha val ley (Lubomierz area, Bystrica Sub unit, Magura Nappe), with lo ca tion of red and var ie gated claystones and mudstones from var i ous lithostratigraphic units; £SF – £abowa Shale For ma tion; num bers over the sec tion are re lated to sam ple lo ca tions

The fre quency of ag glu ti nated foraminiferal assembla-ges dif fers also be tween the red and the vari col oured clay-stones of the Beloveža For ma tion. The red sed i ments are en riched in spec i mens of Saccammina pla centa and Re

cur-voides – Recurvoidella, and are de pleted in ammodiscids

and in Karrerulina conversa.

Cer tain taxa oc cur only in the red fa cies of the Ropian-ka For ma tion (Remesella varians (Glaessner); Fig. 5C, D; Ta ble 2), while oth ers are char ac ter is tic only of the Ro-pianka and £abowa Shale For ma tions, e.g. rzehakinids (Fig. 5A, B; Ta ble 2), and oth ers were found only in the £abowa Shale and the Beloveža For ma tions (Fig. 5E–G; Ta ble 2), e.g. Reticulophragmium amplectens (Grzybowski).

Fig. 3. Palaeo cene and Eocene strati graphic sub di vi sions, geo mag netic po lar ity scale, zonation of cal car e ous nannofossils (Calc. Nan.), plank tonic foraminifera (Plank. For.) (Vandenberghe et al., 2012) and ag glu ti nated foraminifera (2 – Olszewska, 1997), deep-wa ter ag glu ti nated foraminifera acmes in West ern Tethys and North At lan tic (1 –Kaminski and Gradstein, 2005) with lith o logic logs of Rosocha sec tion (Bystrica fa cies, Magura Nappe, Outer Carpathians), plot ted against biostratigraphic mark ers and cal cium car bon ate con tent (in brack ets); (-) – car bon ate-free, (+) – traces of CaCO3, (++) low CaCO3 con tent

Ta ble 2

Dis tri bu tion of Palaeogene ag glu ti nated foraminifera at Rosocha Creek (Bystrica fa cies, Magura Nappe, Outer Carpathians); four frag ments of tu bu lar spe cies were cal cu lated as one in di vid ual

Package 1 Package 2 Package 3 P4

Ros-1 Ros-2 Ros-5 Ros-3 Ros-4 Ros-6 Ros-7 Ros-8 Ros-9 Ros-10Ros-11Ros-12Ros-13Ros-14Ros-15Ros-16

Ammobaculites aglutinans 1 Ammodiscus cretaceus 1 2 2 5 8 A. peruvianus 2 4 4 A. tenuissimus 1 Annectina grzybowskii 3 2 2 3 Aschemocella grandis 2 2 Bathysiphon microraphidus 2 1 1 3 3 Bathysiphon sp. 2 2 2 1 Caudammina ovulum 3 1 2 1 4 1 3 2 6 3 Cribrostommoides trinitatensis 2 1 C. subglobulosus 1 1 Dorothia sp. 1 1 Glomospira gordialis 1 1 2 2 4 3 G. irregularis 2 1 1 1 2 3 G. serpens 1 3 1 Haplophragmoides horridus 2 1 1 2 H. retroseptus 1 3 4 H. eggeri 1 1 H. suborbicularis 2 H. stomatus 1 Haplophragmoides sp. 1 1 Karrerulina conversa 13 1 25 K. horrida 2 1 11 Lituotuba lituiformis 2 Nothia excelsa 1 1 1 3 N. robusta 4 2 2 2 1 2 2 1 Paratrochamminoides heteromorphus 9 1 P. cf. mitratus 1 2 Paratrochamminoides sp. 1 Psammosiphonella cylindrica 1 3 3 Repmanina charoides 1 1 3 3 2 Rhabdammina linearis 5 1 1 1 1 2 1 1 Rhabdammina sp. 1 1 3 1 1 Recurvoidella lamella 4 3 2 2 1 1 Recurvoides contortus 3 6 1 1 R. nucleosus 1 1 R. retroseptus 1 1 1 2 1 Recurvoides sp. 2 1 Remesella varians 1 1 Reophax duplex 2 3 2 Reophax sp. 1 1 1 Reticulophragmium amplectens 7 4 R. intermedium 2 Rzehakina epigona 2 1 R. fissistomata 1 R. minima 1 1

Stra tig ra phy

The deep-wa ter ag glu ti nated foraminifers (DWAF), studied in four red claystone and mudstone pack ages, rep re -sent as sem blages of dif fer ent ages. The low er most pack age 1 (in the Ropianka Fm.) con tains spe cies, typ i cal for the Palaeocene (?Up per Palaeo cene), in clud ing forms, which be -long to the rzehakinids (Ta ble 2; Fig. 3), with R.

fissisto-mata (Grzybowski) and Remesella varians (Glaessner). Rzehakina fissistomata was used as the in dex spe cies in

sev eral zonations of the bathyal–abys sal sed i ments of the Outer Carpathians, which were based on ag glu ti nated taxa (Geroch and Nowak, 1984; Bubík, 1995; Olszewska, 1997; Bubík et al., 1999; B¹k, 2004; B¹k and Wolska, 2005). This zone cor re sponds to dif fer ent parts of the Palaeo cene or to the en tire Palaeo cene in these zonations. The FAD of R.

fis-sistomata is cor re lated with the Early Maastrichtian in

ba-thyal en vi ron ments of the South At lan tic (e.g., Koutsoukos, 2000). It ap peared later in abys sal sed i ments of the Carpa-thians, close to the Maastrichtian–Palaeo cene bound ary (Bubík et al., 1999). The LAD of this spe cies is not clearly de fined. It is marked be low the base of the DWAF as sem -blages with the Glomospira spp. acme that is cor re lated with the Palaeo cene–Eocene bound ary (cf. B¹k, 2004).

Remesella varians was de scribed from the up per most

Cretaceous–Palaeo cene in the NW Cau ca sus by Glaessner (1937). Af ter that, this spe cies was re ported from nu mer ous re gions of the West ern Tethys, North At lan tic and the Ca -rib bean re gion (sum mary in Kaminski and Gradstein, 2005), cor re spond ing to the Maastrichtian–Palaeo cene.

Two red claystone and mudstone pack ages, i.e. pack age 3 and pack age 4, con tain the DWAF as sem blages with a youn ger strati graphic marker, i.e. Reticulophragmium amp-

lectens (Grzybowski) (Ta ble 2; Fig. 3). Its first oc cur rence

(FO) is cor re lated with the Lower Eocene (mid dle Ypre-sian) in the Outer Carpathians, on the ba sis of cor re la tion with the nannoplankton zonal scheme by Olszewska and Smagowicz (1977; Zone NP12). In other bathyal and abys -sal sed i ments, its FO was de scribed above the Lower

Eo-cene Glomospira spp. acme. The LO of this spe cies is known from the vi cin ity of the Eocene–Oligocene bound ary (sum mary in Kaminski and Gradstein, 2005).

The thick est, non-cal car e ous red shale pack age 2 does not con tain strati graphic mark ers that rep re sent any DWAF spe cies (Tab. 2). Their fau nas re sem ble the as sem blages, de scribed from var i ous tec tonic-fa cies units of the Outer Carpathians from the Lower–Mid dle Eocene, be long ing to the £abowa Shale and Beloveža For ma tions (e.g., Geroch, 1960; Geroch et al., 1967; Jurkiewicz, 1967; Jednorowska, 1968; Morgiel and Szymakowska, 1978; Morgiel and Ol-szewska, 1981; Oszczypko et al., 1990, 1999, 2005; Bubík, 1995; B¹k et al., 1997; Waœkowska-Oliwa, 2001; Kender et

al., 2005; Golonka and Waœkowska, 2012). These are char

ac ter ized by an en hanced con tent of tu bu lar forms, as so ci -ated with large num bers of spec i mens of glomospirids, sac-camminids and the Trochamminoides – Paratrochamminoi-

des group.

DIS CUS SION

Biostratigraphic con text

On the ba sis of the oc cur rence of Rzehakina

fissisto-mata, a foraminifer char ac ter is tic for the Palaeo cene, the

sed i men ta tion of the red sed i ments started in the study area in the Late Palaeo cene. How ever, it is not pos si ble to elab o rate the de tailed stra tig ra phy, us ing only the DWAF as sem -blages.

The most char ac ter is tic fea ture of the youn ger red clay-stones and mudclay-stones in the Magura Nappe (also in other Outer Carpathian nappes), namely the Early Eocene ag glu -ti nated foraminifer as sem blage with abun dant Glomospira spp. (e.g., Morgiel and Olszewska, 1981; Olszewska, 1997), dis tin guished as the Glomospira Acme Zone, is not pre served in the sec tions stud ied. An other youn ger strati -graphic ho ri zon, i.e. the Saccamminoides carpathicus Zone, dis tin guished in many lo cal zonal schemes, on the ba sis of the DWAF as sem blages, is also ab sent in the sec tions stud

-Ros-1 Ros-2 Ros-5 Ros-3 Ros-4 Ros-6 Ros-7 Ros-8 Ros-9 -Ros-10-Ros-11-Ros-12-Ros-13-Ros-14-Ros-15-Ros-16

Saccammina grzybowskii 4 1 S. placenta 1 2 3 4 3 8 8 2 6 5 6 4 2 Spiroplectammina navarroana 3 Subreophax pseudoscalaria 1 Subreophax sp. 3 1 3 Trochammina spp. 2 2 1 1 2 2 Trochamminoides dubius 1 2 3 T. coronatus 3 12 T. grzybowskii 1 1 2 2 4 4 1 T. variolaris 3 2 T. proteus 1 1 2 6 6 1 3 7 2 T. subcoronatus 1 9 1 16 Trochamminoides sp. 2 2 2

ied. This in di cates a wide strati graphic gap within the suc ces sion of var ie gated fa cies in the study sec tion, due to tec -tonic dis tur bances (Fig. 3). Such an in ter pre ta tion is re lated to the tec tonic po si tion of the study area, i.e. within the nar row Konina – Lubomierz Thrust Sheet. This is mainly com -posed of thin- and me dium-bed ded turbidites that were fol-ded and thrusted be neath a thick suc ces sion of thick-bed fol-ded sandy turbidites of the Krynica Sub unit dur ing Oligocene– Mio cene time.

The youn gest red claystones, which crop out in the study sec tion, rep re sent the Reticulophragmium amplectens Zone. Ac cord ing to Olszewska (1997), the base of this zone is cor re lated with the base of the Mid dle Eocene (Lutetian). Tak ing into ac count the cor re la tion of the plank tonic fora-miniferal and cal car e ous nannoplankton zonations with the ben thic (ag glu ti nated) foraminiferal oc cur rences, pre sented by Kaminski and Gradstein (2005), the R. amplectens acme was cor re lated with the nannoplankton NP15 to early NP16 Zones. In the mod ern cor re la tion of the cal car e ous nanno-plank ton zonation with mag neto- and chronostratigraphy, this acme cor re sponds to the mid dle Lutetian (about 46–42 Ma; Vandenberghe et al., 2012).

The above data are in good agree ment with ear lier biostratigraphic stud ies within the Magura Nappe, in the Gorce and Beskid Wyspowy ranges (Oszczypko, 1991; Oszczypko et al. 1999, 2005), slightly ex tend ing the ranges of the red fa cies in the Gorce Moun tains area.

Lithostratigraphic con text

The Palaeogene var ie gated fa cies of the Bystrica Sub-unit (Magura Nappe) that oc cur in the Gorce and Beskid Wyspowy Moun tains have been in cluded to the £abowa Shale For ma tion (Oszczypko, 1991; Oszczypko et al., 1999, 2005). They con tain a few thick pack ages of non-cal car e ous shales and claystones, sev eral metres thick, in ter rupted ver -ti cally by ar gil la ceous turbidites with thin in ter ca la -tions of green and red shales. In the stud ied sec tion, the £abowa Shale For ma tion is rep re sented only by two thin pack ages (2–3 m thick) of the red claystones and mudstones. One of them (a part of the R. amplectens Zone), most prob a bly rep -re sents the up per most part of the £abowa Shale For ma tion. The po si tion of the sec ond one is un cer tain, ow ing to a lack of strati graphic mark ers. The char ac ter is tic fea ture of the £abowa Shale For ma tion in this area is the oc cur rence of a pack age of thick-bed ded sand stones, 2–3 m thick, with beds ex ceed ing 70 cm. It is not clear, if they rep re sent the same lithostratigraphic ho ri zon (tec toni cally di vided) or two sep -a r-ate ho ri zons. A sim i l-ar f-a cies -also w-as de scribed from the Porêba Wielka sec tion in the Gorce Moun tains (Oszczypko

et al., 2005), where two thick beds of sand stone oc cur near

the base of this for ma tion.

The to tal thick ness of the £abowa Shale For ma tion in the sec tion stud ied is dif fi cult to es ti mate, ow ing to strong tec tonic dis tur bances in this area. On the ba sis of fea tures of the sed i ments and a com par i son with neigh bour ing sec tions, the £abowa Shale For ma tion is prob a bly 10–15 m thick. This value is sim i lar to those, noted from other sec tions in the south ern part of the Bystrica Sub unit in the Gorce Mountains (Fig. 6), where it ranges from 20 to 30 m (Osz-czypko, 1991; Oszczypko et al., 2005), lo cally ex ceed ing 50 m. In the mid dle and the north ern parts of this sub unit, the £abowa Shale For ma tion to tal thick ness in creases grad -u ally -up to 150 m (M³yñczyska and Pó³rzeczki sec tions; Malata et al., 1996; Oszczypko et al., 2005). The sed i men -tary or i gin of the thick ness dif fer ences of the £abowa Shale For ma tion is taken into ac count, be cause of the nu mer ous ar gil la ceous turbidites in the mid dle part of this for ma tion, as de scribed in the Pó³rzeczki and M³yñczyska sec tions.

Fig. 4. Per cent age con tent of foraminiferal gen era in red fa cies of £abowa Shale For ma tion and Ropianka For ma tion against vari -col oured shales of Beloveža For ma tion

Fig. 5. Se lected deepwa ter ag glu ti nated foraminifers with strati graphic in dex spe cies (A–F) from Palaeo cene–Mid dle Eocene sed i -ments at Rosocha sec tion (Bystrica Sub unit, Magura Nappe, Outer Carpathians): A. Rzehakina min ima Cushman & Renz, sam ple Ros-1. B. Remesella varians (Glaessner), sam ple Ros-1. C–F. Reticulophragmium amplectens (Grzybowski), C – sam ple Ros-16, D–E – sam ple Ros-15. G. Karrerulina conversa (Grzybowski), sam ple Ros-14. H–K. Karrerulina horrida (Mjatliuk), H – sam ple Ros-11, I–K – sam ple Ros-11. L. Haplophragmoides eggeri Cushman, sam ple Ros-1. M. Recurvoides retroseptus (Grzybowski), sam ple Ros-1. N. Recurvoides nucleosus (Grzybowski), sam ple Ros-8. O. Trochamminoides subcoronatus (Grzybowski), sam ple Ros-14

The low ac cu mu la tion rate dur ing Palaeo cene–Early Eo-cene times in this part of the Magura Ba sin (3–20 m/Myr; Tab. 1), com pared to data from the neigh bour ing Raèa Sub -unit (15–110 m/ Myr; Oszczypko and Oszczypko-Clowes, 2006), may con firm this in ter pre ta tion.

CON CLU SIONS

1. Palaeogene red claystones and mudstones oc cur in the Ropianka, £abowa Shale and Beloveža For ma tions of the Gorce Moun tains (Rosocha sec tion), in the Bystrica Sub unit of the Magura Nappe, Outer Carpathians.

2. Deepwa ter ag glu ti nated foraminiferal (DWAF) as sem blages, oc cur ring in these strata, con tain forms that be long to 59 spe cies. Tu bu lar forms are rare in the red sed i -ments. The most com mon taxa be long to Trochamminoides – Paratrochamminoides spp., Saccammina pla centa, glo-mospirids, Recurvoides – Recurvoidella spp. and karreru-linids. The rel a tive abun dance of DWAF var ies from 4 to 43 spec i mens per sam ple in one gram of sed i ment, de pend ing on the type of sed i ment.

3. The stratigraphically old est part of the red sed i ments, oc cur ring as in ter ca la tions a few centi metres thick in the Ropianka For ma tion, rep re sents the up per part of the

Rze-hakina fissistomata Zone, cor re spond ing most prob a bly to

the Up per Palaeo cene.

4. The stratigraphically youn gest red claystones and mudstones in the sec tion stud ied, oc cur ring as in ter ca la tions a few centi metres thick in the Beloveža For ma tion, rep re -sent the acme of Reticulophragmium amplectens (ac cord ing to Kaminski and Gradstein, 2005). Us ing the

chronostrati-graphy of Vandenberghe et al. (2012), a cor re la tion of this acme with the cal car e ous nannoplankton of the NP15 to early NP16 Zones (Kaminski and Gradstein, 2005) shows that it cor re sponds to the mid dle Lutetian (about 46–42 Ma). 5. The Early Eocene red sed i ments of the £abowa Shale For ma tion are strongly tectonized in the study area. Their lower and mid dle parts, cor re spond ing to the Glomospira spp. Acme Zone and to the Saccamminoides carpathicus Zone, are not pre served there. The up per part of the £abowa Shale For ma tion, rep re sented by con tin u ous red shales 2 m thick, be longs to the lower part of the Reticulophragmium

amplectens Zone.

6. The small thick ness of the £abowa Shale For ma tion (10–15 m) in the sec tion stud ied is sim i lar to val ues, noted from other sec tions in the Konina – Lubomierz Thrust Sheet (Bystrica Sub unit). Com par i sons of the to tal thick ness of the £abowa Shale For ma tion of the Bystrica Sub unit (Gorce Moun tains) with that of the cor re spond ing sed i ments of the Raèa Sub unit (Beskid Wyspowy Moun tains) re veal that an in crease in thick ness of up to 150 m is prob a bly sed i men tary in na ture. It may be the re sult of an in creased num ber of mud-rich grav i ta tional flows in the north ern part of the Magura Ba sin dur ing the Early Eocene.

Ac knowl edge ments

This study was car ried out in part as an MSc pro ject by M. Cieœla at the In sti tute of Geo log i cal Sci ences, Jagiellonian Uni ver -sity of Kraków. The au thors would like to thank Wanda Barwicz-Piskorz (Kraków) for her help dur ing the field stud ies. This pa per bene fited con sid er ably from in sight ful com ments by Nestor Osz-czypko (Kraków) and an anon y mous re viewer. Spe cial thanks go Fig. 6. To tal thick ness of £abowa Shale For ma tion in var i ous sec tions of Bystrica fa cies (Magura Nappe, Outer Carpathians), Gorce Moun tains and Beskid Wyspowy Moun tains (based on Oszczypko, 1991; Malata et al., 1996; Oszczypko et al., 2005; this study)

and Tech nol ogy (AGH), awarded to K. B¹k (DS-UP-WGB-3) and to M. B¹k (DS-AGH – Uni ver sity of Sci ence and Tech nol ogy WGGiOŒ-KGOiG-No. 11.11.140.173).

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