Foraminiferal and Palynological Re Cords of the Late Badenian (Mid Dle Mio Cene) Trans Gres Sion in Podolia (Shchyrets Near Lviv, West Ern Ukraine)

Geo log i cal Quar terly, 2014, 58 (3): 465–484 DOI: http://dx.doi.org/10.7306/gq.1195

Foraminiferal and palynological re cords of the Late Badenian (Mid dle Mio cene) trans gres sion in Podolia (Shchyrets near Lviv, west ern Ukraine)

Danuta PERYT1, *, Przemys³aw GEDL2 and Tadeusz Marek PERYT3

1 Pol ish Acad emy of Sci ences, In sti tute of Paleobiology, Twarda 51/55, 00-818 Warszawa, Poland 2 Pol ish Acad emy of Sci ences, In sti tute of Geolog i cal Sci ences, Senacka 1, 31-002 Kraków, Poland 3 Pol ish Geo log i cal In sti tute – Na tional Re search In sti tute, Rakowiecka 4, 00-975 Warszawa, Poland

Peryt, D., Gedl, P., Peryt, T.M., 2014. Foraminiferal and palynological records of the Late Badenian (Middle Miocene ) trans - gres sion in Podolia (Shchyrets near Lviv, western Ukraine). Geo log i cal Quar terly, 58 (3): 465–484, doi: 10.7306/gq.1195

The Up per Badenian marly shales over ly ing gyp sum and the Ratyn Lime stone at Shchyrets, Ukraine, contain moder ately to well-preserved benthic (calcar e ous only) and plank tonic foraminifers, and palynofacies dom i nated by bisaccate pol len grains, pre sum ably trans ported by wind. Both foraminiferal and dinoflagellate cyst as sem blages in di cate an open ma rine envi ron ment with nor mal-ma rine sa lin ity and cool wa ters. The palaeodepth was ca. 50 m except for the upper most part of the sec tion stud ied, where a dis tinc tive deep en ing is in di cated by the dom i nance of Uvigerina in ben thic foraminiferal as sem- blages and a high P/B ra tio. The wa ter was ther mally strat i fied and the dif fer ences be tween the bot tom wa ter and the wa ter col umn show an up wards-in creas ing trend. Bulimina and Globocassidulina are the most com mon and dom i nant com po nent of ben thic foraminiferal as sem blages, ex cept for the up per most part where Uvigerina dom i nates the as sem blage. The compo si tion of ben thic foraminifer as sem blages and d13C val ues of foraminifers in di cate nu tri ent-rich wa ters and mesotrophic to eutrotrophic en vi ron ments in sur face wa ters, and low ox y gen a tion at the sea floor in the Ukrai nian Carpathian Foredeep Ba- sin dur ing the Late Badenian.

Key words: Paratethys, Carpathian Foredeep, Up per Badenian, foraminifers, dinoflagellate cysts, palaeoenvironment.

INTRODUCTION Carpathian fore land (Kudrin, 1966; Górka et al., 2012), and then, to wards the west, by rhodoid lime stones with mi nor in ter - ca la tions of marl and claystone (Gedl and Peryt, 2011; Fol low ing the mid-Badenian sa lin ity cri sis, which re sulted in Studencka et al., 2012); far ther to wards the south-west this car- the de po si tion of thick evaporite de pos its in var i ous bas ins of bon ate fa cies is re placed by clayey-sandy-car bon ate fa cies the Carpathian re gion (see Peryt, 2006 with ref er ences that, in turn, passes into sandy-clayey fa cies – the typ i cal Kosiv therein), the last ma rine flood ing in the Paratethys in the Late Suite. The sed i men tary fa cies changes are ac com pa nied by Badenian re sulted in the reconnection of the Cen tral and East- changes in foraminiferal as sem blages, and the most basin - ern Paratethys (Rögl, 1998). Dur ing this trans gres sion, which ward, clayey fa cies con tain chilostomellids, cassidulinids, buli - was dom i nantly con trolled by sea level changes out side the minids, and some plank tonic spe cies (Orbulina, Globigerina) Cen tral Paratethys realm (Kováè et al., 2007), outer and in ner (Bobrinskaya et al., 1998). neritic con di tions were es tab lished in the in ner and outer parts The Kosiv For ma tion con sists of silty grey clays which al ter - of the foredeep, and in the mar ginal part of the Carpathians nate with sep a rate interbeds of loose silts, sand stones, tuffs, (Oszczypko and Oszczypko-Clowes, 2012 with ref er ences and tuffites (Andreyeva-Grigorovich et al., 1997). It is com- therein). There are var i ous es ti mates of the trans gres sion start: posed of four lithologically dis tinc tive sub di vi sions: the from ca. 13.1 Ma (Œliwiñski et al., 2012) to ca. 13.54 Ma Verbovets, Prut, Kolomyia, and Kovalivka beds. (Hohenegger et al., 2014). De Leeuw et al. (2013) sug gested The Verbovets beds con tain sev eral lay ers of tuff and tuffite, that the end of the Badenian salinity crisis was at 13.36 Ma. and are char ac ter ized by nu mer ous Globigerina bulloides The Up per Badenian de pos its show car bon ate fa cies char - d’Orbigny, G. regularis d’Orbigny, Subbotina cognata (Pishva- ac ter ized by the oc cur rence of coralline al gae-vermetid reefs nova), and Velapertina indigena (£uczkowska). In ad di tion, and a va ri ety of bioclastic fa cies in the east ern part of the radio lar ians oc cur in the lower part of the sub di vi sion, while pteropods of the ge nus Spiratella, and foraminifera, oc cur in its up per part (Pishvanova, 1969; Garecka and Olszewska, 2011). Foraminiferal as sem blages were as signed to the Globigerina * Corresponding author: [email protected] decoraperta Zone. Within the Prut beds, sand stones pre dom i - nate (Andreyeva-Grigorovich et al., 1997). The Prut beds are Received: August 13, 2014; accepted: September 24, 2014; first published online: October 7, 2014 char ac ter ized by the co-oc cur rence of ag glu ti nated and cal car- e ous foraminifera of the Bogdanowiczia pokutica and Bulimina- 466 Danuta Peryt, Przemys³aw Gedl and Tadeusz Marek Peryt

-Bolivina zones, with typ i cal Hyperammina granulosa yeva -Grigorovich et al., 1997). The for ma tion is over lain by the Venglinski, Bogdaniowiczia pokutica Pishvanova, Cyclammina Up per Badenian Kosiv For ma tion (10–150 m thick); the over - pleschakovi Pishvanova, and nu mer ous Bulimina elongata ly ing Sarmatian strata are in cluded in the Dashava For ma tion d’Orbigny (Pishvanova, 1969; Garecka and Olszewska, 2011). that is fur ther sub di vided into two parts; the lower part (up to The aim of this pa per is to char ac ter ize and in ter pret the en - 3500 m thick), and the upper part (up to 1500 m thick) (Kuro - vi ron men tal changes from the suc ces sion of foraminiferal as - vets et al., 2004). sem blages, palynofacies, and as sem blages of dinoflagellate Var i ous types of the Badenian depos its are ex posed nat u - cysts in the basal part of the Kosiv For ma tion at Shchyrets, near rally in the Shchyrets area (£omnicki, 1897; cf. Gerasimov et al., Lviv, that is one of key sec tions of the Up per Badenian in the 2005). In the gypsum quarry (not active at pres ent), clastic, lam- Ukrai nian Carpathian Foredeep, ow ing to its palaeo geographi - i nated, and rede pos ited gypsum of total thick ness of ca. 20 m, cal lo ca tion near the bound ary of mar ginal and basinal parts of with ca. 5 m thick brec cia in ter ca la tion and nu cle ation cones at the foredeep (Fig. 1). their base (Peryt, 1996), is over lain by the Ratyn Lime stone (ca. 0.9 m thick; Fig. 2). The Ratyn Lime stone shows mudstone and then peloidal and intraclastic wackestone-packstone tex ture GEOLOGICAL SETTING (Peryt and Peryt, 1994). Its iso to pic com po si tion sug gests that both ma rine fa cies (d18O val ues from –3 to +1‰; d13C val ues from ca. –9‰) and diagenetic ma te rial (d18O val ues from ca. –1 Shchyrets is lo cated north of the Rava Ruska Fault Zone to –5‰; d13C val ues from ca. –13.5 to –15.5‰) oc cur (Peryt that is com monly consid ered to rep re sent the southwest ern and Peryt, 1994: fig. 3; cf. Peryt et al., 2012). edge of the East-Euro pean Plat form. South of the Rava Ruska The Ratyn Lime stone is over lain by 5 m thick pale beige to Fault Zone, strata of the Bilche-Volytsia zone of the Carpathian pale ol ive hard, mas sive marly clays, with one 20 cm thick bed Foredeep occur. of carbonatized tuffite lo cated 1.5–1.7 m above the Ratyn Lime - The Bilche-Volytsia Unit shows diverse strati graphic se - stone, a 15 cm thick sand stone in ter ca la tion oc cur ring 2.9 m quences and var ied thick nesses of Mio cene de pos its above the Ratyn Lime stone, and a 35 cm thick bed of (Oszczypko et al., 2006). At the base of the Mio cene sec tion in carbonatized tuffite at the top (Fig. 2). In addi tion, there oc cur bore hole pro files of the Bilche-Volytsia Unit, var i ous silici - thin ner tufogenic in ter ca la tions; one of these, oc cur ring about clastic de pos its, com monly con glom er ates and brec cias, and 2.5 m above the gypsum, was radio met ri cally dated to 13.19 ± car bonate de pos its oc cur that are in cluded in the Sandy-Cal - 0.14 Ma (Nejbert et al., 2012). These marly clays contain car e ous Se ries of the Karpatian (Vashchenko et al., 2007) or foraminifers; Kudrin (1966: p. 140) men tioned that N. Boya- Early Badenian (Kotarba et al., 2011) age; in the lat ter case, rintse vaya found rare Textularia carinata d’Orbigny, Gyroidina they form part of the Bohorodchany For ma tion that is cov ered soldanii d’Orbigny, Uvigerina pygmea d’Orbigny, Bulimina by evaporites of Tyras For ma tion (Peryt et al., 2010). In the elongata d’Orbigny, B. buchiana d’Orbigny, Pullenia coryelli Carpathian fore land, the Tyras For ma tion in cludes evaporites White, Globigerina ex gr. bulloides d’Orbigny, and Miliolina sp.

and the Ratyn Lime stone (Petryczenko et al., 1994; Andre - in the “tuffaceous sand stones” of Shchyrets.

g u B 50 km Lviv

F O Shchyrets D R ni ste E r L C A Ternopil

A N h c

u R D r

b P Z

C EAST

A A t

T r

R e H P S A EUROPEAN I A T N H S IA CRATON N ~ ~ ~ F ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ Zone I+II O ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ gypsum R Ivano-Frankivsk ~ ~ ~ ~ ~ ~ ~ ~ facies E Zone III D ~ ~ ~ ~ ~ ~ ~ ~ E ~ ~ ~ ~ ~ ~ ~ ~ E ~ ~ ~ ~ ~ ~ ~ ~ anhydrite facies, P ~ ~ ~ ~ ~ ~ ~ ~ Zone IV local halite facies ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ marly facies ~ ~ ~ ~ ~Kudryntsi~ ~ ~ with rhodoids Dnister P ~ ~ ~ ~ ~ ~ ~ ~ ru sandy-clayey t ~ ~ ~ ~ ~ ~ ~ ~ facies Upper ~ ~ ~ ~ ~ ~ ~ ~ Badenian ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ M~ Medobory ~P ~ ~ ~ ~ ~ ~ ~ reefs Chernivtru~t ~si ~ ~ ~ ~ ~ ~ O ~ ~ ~ ~ ~ ~ ~ ~ L ~ ~ ~ ~ ~ ~ ~ ~ D ~ ~ ~ ~ ~ ~ ~ ~ . Fig. 1. Lo ca tion map show ing the mid-Badenian sul phate zones (af ter ~Pery~t, ~2006)~ ~ ~ ~ ~ and Up per Badenian facies in the Carpathian fore land (af ter Kudrin~ ~, 1966)~ ~ ~ ~ ~ ~ A N I A R U M Foraminiferal and palynological records of the Late Badenian... 467

The fol low ing taxa, pres ent in the mate rial stud ied, are in - cluded in the oxic group: Heterolepa dutemplei, Lobatula lobatula, Cibicidoides spp., Cibicides sp., Sigmoilinita tenuis. Oxic in di ces rep re sent epifaunally liv ing spe cies. Taxa tol er ant of suboxic en vi ron ments are: Lenticulina spp., Lagena spp., Porosononion granosum, Astrononion perfossum, Melonis pompilioides, Pullenia bulloides, P. miocenica, Sphaeroidina bulloides, and taxa tol er ant of dysoxic en vi ron ments are Bulimina spp., Bolivina spp., Uvigerina spp., Fursenkoina acuta, Praeglobobulimina pyrula and Globocassidulina sp. Foraminifers tol er ant of suboxic en vi ron ments rep re sent mostly shal low infaunally liv ing spe cies, while foraminifers tol er ant of dysoxic en vi ron ments rep re sent mostly deep infauna and spe - cies with op por tu nis tic be hav ior. They are commonly used as stress mark ers (e.g., van der Zwaan et al., 1999; van Hinsbergen et al., 2005). Since Emiliani (1955), d18O val ues of foraminifera are re - garded as an ex cel lent in di ca tor of tem per ature changes. To cal - cu late ab so lute wa ter tem per a ture, d18O ra tios of se lected foraminifer spe cies were used: plank tonic Globigerina spp. (in four sam ples, in two of them G. bulloides) and infaunal Bulimina elongata. In one case where the lat ter taxon was too rare to al low for iso to pic stud ies, Uvigerina peregrina was used in stead, as both have sim i lar en vi ron men tal re quire ments, and in an other sam ple both Bulimina elongata and Uvigerina peregrina were used. It is as sumed that the iso tope val ues for Globigerina and Fig. 2. Upper Badenian section Bulimina/Uvigerina are in dic ative of the sur face and deep- water at Shchyrets Quarry show ing iso tope com po si tion, re spec tively. Foraminifer tests were re - sam ple lo ca tions acted with 100% phos phoric acid at 75°C, us ing a KIEL IV online au to matic car bon ate prep a ra tion line con nected to the Finnigan MATERIAL AND METHODS Mat delta plus mass-spec trom eter at the Light Sta ble Iso topes Lab o ra tory of the In sti tute of Geo log i cal Sci ences, Pol ish Acad - emy of Sci ences, Warszawa. All isoto pic data was re ported in The sec tion ex posed in the Shchyrets Quarry was mea - per mil rel ative to VPDB re lated to NBS 19. The pre ci sion sured and sam pled in 1996. Nine sam ples were se lected for (reproducibility of rep li cate anal yses) of both car bon and oxy gen study of foraminifers, palynology and min er al og i cal com po si - iso tope anal yses was usu ally better than ±0.2‰. For the cal cu la - tion. The lo ca tion of sam ples stud ied is shown in Figure 2. tion of palaeotemperatures, var i ous equa tions have been gen er - Sam ples M-1 to M-8 are pale beige to pale ol ive hard, mas - ated, but all gen er ally follow Ep stein et al.’s (1953) orig i nal equa - sive marly shales, and sam ples M-10 to M-15 are mostly pale tion. In the pres ent work we use this orig i nal equa tion. Due to var - beige fine-split ting marly shales. i ous cor rec tions, the fi nal tem per a ture val ues for Late Badenian Washed res i dues for foraminiferal study were ob tained from Paratethyan water can dif fer sub stan tially (see Peryt, 2013: ap - the marls by disaggregation us ing Na2SO4. An aliquot of about pendix 3), al though the trends of tem per ature changes, based on 200–300 spec i mens of foraminifers from the 100–600 µm size cal cu la tions with var i ous equa tions, re main sta ble. frac tion was picked for the fau nal anal yses. Taxon omy of the The sam ples were pro cessed fol low ing stan dard foraminifers fol lows Loeblich and Tappan (1987), Odrzywolska- palynological pro ce dure, in clud ing 38% hy dro chlo ric acid (HCl) - Bieñkowa and Olszewska (1996) and Cicha et al. (1998). The treat ment, 40% hydro flu oric acid (HF) treat ment, heavy liquid fig ured spec i mens are de pos ited in the Insti tute of Paleo - 3 (ZnCl2+HCl; den sity 2.0 g/cm ) sep a ra tion, ul tra sound for biology, Polish Acad emy of Sci ences, War szawa (ZPAL F. 60). 10–15 s, and siev ing at 15 µm on a nylon mesh. No fum ing ni tric Foraminiferal taxa were al lo cated to morphogroups ac cord - acid (HNO3) treat ment was ap plied. The quan tity of rock pro - ing to Jones and Charnock (1985) and Corliss and Chen cessed equalled 20 g for each sam ple. The rock sam ples, (1988). The rel ative per cent ages of ben thic foraminifer spe cies palynological res i dues and slides are stored in the col lec tion of within the ben thic foraminiferal as sem blages, the rel a tive abun - the In sti tute of Geo log i cal Sci ences, Pol ish Acad emy of Sci - dance of infaunal, shal low infaunal and epifaunal forms (to in- ences, Kraków. form on trophic con di tions), and the per cent age of plank tonic Palynomorphs and phytoclasts were counted up to a to tal of foraminifers within to tal foraminiferal as sem blages (P/B ra tio) 1000. Among palynomorphs dinoflagellate cysts, sporomorphs were cal cu lated. Palaeobathymetry was es ti mated on the basis (spores and pol len grains), and Leiosphaeridia were dis tin - of ben thic fau nal char ac ter is tics and the P/B ratio. The guished, whereas palynodebris con sist in the ma te rial studied palaeoenvironmental in ter pre ta tion, based on foraminifers, ap - of cu tic u lar re mains, black opaque phytoclasts, dark brown plies the re quire ments of pres ent-day rep re sen ta tives of re - trans lu cent woody par ti cles and structureless debris. All corded taxa (see Peryt and Gedl, 2010: table 1). To es ti mate dinoflagellate cysts on a slide were counted. the level of oxy gen a tion of the sea floor, benthic foraminifera Sam ples were sub ject to X-ray Diffrac tion (XRD) study us - were grouped into oxic, suboxic, and dysoxic in di ca tors ac cord - ing a Philips X’Pert PW 3020 spec trom eter at the Cen tral ing to Thomas (1980), van der Zwaan (1982, 1983), Verhallen Chem i cal Lab o ra tory of the Pol ish Geo log i cal In sti tute – Na - (1991), Jorissen et al. (1992), Kaiho (1994), Loub¾re (1996, tional Re search In sti tute, Warszawa. The wave length used was 1997), Bernhard and Sen Gupta (1999), Kouwenhoven and K-Alpha1 and the peak search pa ram eter set was PC-APD. van der Zwaan (2006), and Kaminski (2012). 468 Danuta Peryt, Przemys³aw Gedl and Tadeusz Marek Peryt

RESULTS and their con tri bution to the as sem blage exceeds 75%; suboxic spe cies form 20% and oxic spe cies form only 5% (Fig. 7). Plank tonic foraminifera, rep re sented by small Globigerina spp. FORAMINIFERS and Globigerinoides spp., form 5% of the as sem blage. In sam ple M-8, the con tri bu tion of Bulimina drops to 30%; The de pos its ex am ined yielded mod er ately- to well-pre - Globocassidulina sp. dom i nates (53% of the as sem blage); served foraminifers (Figs. 3–5). Ben thic as sem blages are com - Sigmoilinita tenuis and Astrononion perfossum are com mon in posed en tirely of cal car eous forms (Figs. 3 and 4); agglu ti nated this as sem blage; rare com po nents are rep re sented by Lagena foraminifers were not re corded in the mate rial studied. Sim ple sp., Lenticulina sp., Reussoolina apiculata, Porosononion ben thic di ver sity is low to mod er ate. Thirty-eight spe cies of ben - martko bi, Bolivina spp., and Glandulina ovula (Fig. 6). In this thic and nine spe cies of plank tonic foraminifers were recorded. as sem blage dysoxic forms dom i nate, reach ing 86%; suboxic Bulimina is the most com mon and dom i nant com po nent of rep re sen ta tives drop to 10% and oxic ones form 4% (Fig. 7). ben thic foraminiferal as sem blages in al most the entire in ter val Plank tonic foraminifera are rare and do not exceed 5% of the stud ied, ex cept in the upper most part, where this group is com - as sem blage. pletely lack ing. In places, Uvigerina and Globocassidulina, at In sam ple M-10 Bulimina dom i nates (B. aculeata and the ex pense of Bulimina, ex ceed 50% and dom i nate as sem - Bulimina elongata are the most abun dant); Astrononion blages. Fursenkoina, Heterolepa dutemplei, and Sphaeroidina perfossum and Sigmoilinita tenuis exceed 13 and 10%, re spec - bulloides are also tem po rarily im por tant con tri bu tors, form ing tively (Fig. 6). In this as sem blage, the contri bu tion of dysoxic up to 25% of the as sem blages; Pullenia bulloides, Sigmoilinita forms is 68%, and of suboxic ones is 20%; oxic in di ces form tenuis, Astrononion perfossum are com mon in dif fer ent in ter - 12% (Fig. 7). Plank tonic forms are rep re sented by Globigerino - vals (Fig. 6). ides spp., Globigerina bulloides, G. praebulloides, and Globi - The con tri bu tion of plank tonic foraminifera is very low gerina sp.; their con tri bu tion to the as sem blage is <5%. (0–5%) ex cept in the up per most part of the sec tion, where the In sam ple M-12, the tax o nomic com po si tion of ben thic P/B ratio ex ceeds 50%. Globigerina and Globigerinelloides are foraminiferal as sem blage is very sim i lar to that of sam ple M-8, the most com mon; Tenuitellinata, Globigerinoita, Turborotalita, where Bulimina is com mon but not dom i nant (Fig. 6). Globo - and Velapertina? were also re corded (Fig. 5). cassidulina sp. dom i nates in this as sem blage. Mi nor com po - In sam ple M-1, the ben thic foraminiferal as sem blage is dom i - nents are Sphaeroidina bulloides, Lagena sp., Pullenia nated by Bulimina aculeata and Bulimina elongata; com mon are bulloides, Lenticulina sp., Reussoolina apiculata, Porosononion Sigmoilinita tenuis and Lagena sp.; Bolivina sp., Sphaero idina martkobi and Glandulina ovula. Dysoxic spe cies dom i nate and bulloides, Astrononion perfossum, Elphidium macellum, form 87% of the as sem blage, suboxic spe cies com prise 6%, Cibicidoides sp. and Praeglobobulimina sp. rarely occur (Fig. 6). and oxic forms make up 7% (Fig. 7). Plank tonic foraminifera are Dysoxic in di ces form 80% of the as sem blage and are com posed very rare and rep re sented by Globigerina spp. mainly of Bulimina spp.; Bolivina and Praeglo bobulimina are mi - In sam ple M-13, Bulimina spp. dom i nate and form 63% of nor con tri butors to this group; suboxic in di ces form 13% of the the as sem blage; Sigmoilinita tenuis is com mon and rep re sents as sem blage, and oxic ones only 7% (Fig. 7). Plank tonic fora - 10%; rare com ponents in this as sem blage are rep re sented by minifera are rare and are rep re sented by Globi gerina bulloides, Astrononion perfossum, Lagena sp., Lenticulina sp., G. praebulloides, Globigerina sp., and Globi geri noides sp. In ad- Reussoolina apiculata, Porosononion martkobi and Glandulina di tion, re worked Cre ta ceous foraminifera occur. ovula (Fig. 6). Dysoxic rep re sen ta tives form 63% of the as sem - In sam ple M-2, Bulimina, a dom i nant form in the preced ing blage, suboxic ones 29%, and oxic ones 8% (Fig. 7). Plank tonic sam ple, de creases in rel ative abun dance to 38% of the as sem - foraminifera do not ex ceed 5% of the as sem blage. blage (Fig. 6). Small thin-walled Lagena spp., Astrononion The ben thic foraminiferal as sem blage of sam ple M-14 is perfossum, Reussoolina apiculata, Lobatula lobatula, Cibici - sim i lar in tax o nomic com po si tion to that of sam ple M-12 and is doides sp., Eponides repandus, and Polymorphina? sp. are dom i nated by Globocassidulina sp. – 38% of the as sem blage. com mon. In this as sem blage the con tri bu tion of dysoxic forms Bulimina aculeata and Bulimina elongata are com mon and to - is the lowest in the en tire in ter val stud ied and reaches 38%; the gether con trib ute 24% to the as sem blage; com mon con tri bu - suboxic group is the larg est and forms 48% of the to tal, and oxic tors to the as sem blage are Sigmoilinita tenuis (9%) and forms com prise 14% (Fig. 7). The plank tonic foraminifera as - Astrononion perfossum (6%); rare com po nents are repre - sem blage is the same as in sam ple M-1. sented by Glandulina ovula, Lagena sp., Lenticulina sp., In sam ple M-5, Bulimina again is the main com po nent of the Reussoolina apiculata, and Pseudotriloculina consobrina (Fig. ben thic foraminiferal as sem blage (70% of the to tal). Bulimina 6). In the as sem blage dysoxic forms dom i nate – 71%, suboxic aculeata and B. elongata are the most abun dant. Heterolepa ones form 20%, and oxic ones 9% (Fig. 7). Plank tonic forms – dutemplei is also a very impor tant con trib utor and ex ceeds 25% Globigerina bulloides, G. praebulloides, Globigerina sp., and of the as sem blage. Mi nor com po nents are Astrononion per - Globigerinoides spp. – con sti tute <5% of the as sem blage. fossum, Reussoolina apiculata, Elphidium sp., Melonis pompili- It is nota ble that foraminiferal as sem blages dom i nated by oides, Uvigerina sp., and Sphaeroidina bulloides (Fig. 6). Globocassidulina (sam ples M-8, M-12, and M-14) are char ac - Dysoxic in di ces con trib ute 65% of the as sem blage; oxic ones ter ized by reduced test sizes. rep re sented mainly by Heterolepa dutemplei form 27%, and In sam ple M-15, the ben thic foraminiferal as sem blage is suboxic forms com prise 8% (Fig. 7). Plank tonic foraminifera are char ac ter ized by the to tal ab sence of Bulimina; Uvigerina dom i - lack ing. nates this as sem blage. Uvigerina pudica, U. brunnensis, U. In the fol low ing sam ple, M-7, Bulimina exceeds 50% of the semiornata, U. peregrina, and Uvigerina sp. form al most 57% of as sem blage, Fursenkoina acuta forms 25%, Astrononion the to tal as sem blage. An im por tant con trib u tor to this as sem - perfossum forms 16%, and Sigmoilinita tenuis makes up 5% blage is Sphaeroidina bulloides, which forms 25% of the to tal; (Fig. 6); in ad di tion rare Heterolepa dutemplei, Bolivina sp., com mon spe cies are Sigmoilinita tenuis (5%), Bolivina spp. (B. Sphaeroidina bulloides, Elphidium macellum, Cibicidoides sp., dilatata, B. plicatella and B. sp.) (5%), Pullenia bulloides (5%); Praeglobobulimina pyrula, Guttulina sp. and Glandulina ovula rare con tri bu tors are Globulina punctata, Melonis pompilioides, oc cur. Bulimina and Fursenkoina acuta are main dysoxic forms Cibicidoides sp. and Osangularia? sp. (Fig. 6). Dysoxic com po - Foraminiferal and palynological records of the Late Badenian... 469

Fig. 3. Benthic foraminifers from Shchyrets A, B – Uvigerina semiornata; C, D, E – Uvigerina peregrina; F – Uvigerina sp.; G – Uvigerina brunnensis; H – Bulimina sp.; I, N, Q – Bulimina elongata; J – Bulimina aculeata; K – Bulimina insignis; L, O, P – Bulimina schischkinskayae; R, S, U, V, W, X – Sigmoilinita tenuis; T – Sigmoilinita sp.; Z – Sigmoilinita tschokrakensis; Y – Lagena sp.; A1 – Bolivina dilatata; B1 – Bolivina sp.; C1 – Bolivina plicatella; D1, E1 – Fursenkoina acuta; F1 – Bolivina sp.; G1, G2, H1, H2 – Globocassidulina sp.; I1 – Glandulina sp.; J1, J2 – Astrononion perfossum; K1, K2 – Pullenia bulloides; L1, L2 – Melonis pompilioides; scale bars = 100 µm 470 Danuta Peryt, Przemys³aw Gedl and Tadeusz Marek Peryt

Fig. 4. Benthic foraminifers from Shchyrets A1, A2 – Sphaeroidina bulloides; B1, B2 – Cibicidoides sp.; C1, C2, D1, D2 – Rosalina nana; E1, E2 – Globocassidulina sp.; F1, F2, L1–L3, M1–M3 – Lobatula lobatula; G1, G2 – Porosononion martkobi; H1–H3, J1–J3 – Heterolepa dutemplei; K1, K2 – Pullenia miocenica; A1, A2, B1, B2, K1, K2 – sam ple M-15; C1, C2 – sam ple M-13; D1, D2, E1, E2 – sam ple M-8; F1, F2, G1, G2, L1–L3, M1–M3 – sam ple M-2; H1–H3 – sam ple M-7; I1, I3 – sam ple M-4; J1–J3 – sam ple M-5; scale bars = 100 µm Foraminiferal and palynological records of the Late Badenian... 471

Fig. 5. Planktonic foraminifers from Shchyrets A1, A2, E1, E2 – Globigerina bulloides; B1, B2 – Globigerinelloides trilobus; C1, C2 – Globigerinoides primordius?; D1, D2, L1, L2 – Tenuitellinata juvenilis; F1, F2 – Globigerinoita sp.; G1, G2 – Velapertina? sp.; H1, H2 – Globigerina praebulloides; I1, I2, K1, K2 – Turborotalita quinqueloba; J1, J2 – Globigerinoides quadrilobatus; A1, A2, B1, B2, C1, C2, E1, E2, F1, F2, G1, G2, H1, H2, J1, J2, L1, L2 – sam ple M-15; D1, D2 – sam ple M-7; I1, I2, K1, K2 – sam ple M-8; scale bars = 100 µm nents form 62% of the as sem blage, suboxic forms 31% and is –1.18 ± 0.62‰); they are simi lar. The range of d18O val ues for oxic forms 7% (Fig. 7). P/B is 57%. Very common are Bulimina and Uvigerina is from –0.39 to 2.54‰ (the mean is Globigerinoides spp., Globigerina bulloides, G. praebulloides, 1.72 ± 0.99‰), and for Globigerina from –0.07 to 0.59‰ (the and Globigerina sp. Rare oc cur rences of Tenuitella, Globi - mean is 0.18 ± 0.29‰) (Fig. 8). gerinoita, Turborotalita, and Velapertina are re corded. The ben thic d13C curve shows some fluc tu ation with the lowest val ues re corded in the bot tom part of the sec tion stud ied. Higher up in the sec tion the d13C val ues of ben thic foraminifers ISOTOPIC ANALYSES OF FORAMINIFERS grad ually increase up to ca. 0‰ near +2.5 m, then de crease to ca. –2‰ near +4.0 m and next, in the up per most part of the sec - Re sults of iso to pic anal y ses of foraminifers are shown in tion studied, show an in crease to ca. –0.5‰. The benthic d18O Fig ures 8 and 9. The range of d13C val ues for Bulimina and curve shows first an in crease of d18O val ues (from 0.94‰ to Uvigerina is from –0.21 to –2.72‰ (the mean is –1.13 ± 1.73‰) and then a dis tinct decrease (to –0.39‰ just above the 0.80‰), and for Globigerina is from –0.41 to 1.72‰ (the mean thick tuffite bed). Next, in the mid dle part of the sec tion they in - 472 Danuta Peryt, Przemys³aw Gedl and Tadeusz Marek Peryt

Fig. 6. Rel a tive abun dances of dom i nant and com mon ben thic foraminiferal species within assem blages in the marls above the Ratyn Lime stone at Shchyrets

Spe cies or groups of spe cies which at least in one sam ple exceed 5% are shown crease to 2.28‰ and the upper part of the sec tions shows fluc - All sam ples, ex cept for M-10, yielded dinoflagellate cysts; they tu ations in a small range (2.05–2.54‰). As far as the plank tonic are il lus trated in Fig ures 11 and 12, and their dis tri bu tion is foraminifers are con cerned, the num ber of sam ples ana lysed shown in Table 1 and Fig ure 13. was too low to de tect the di rec tion of changes in car bon and ox- Palynofacies of the lower most sam ple M-1 is dom i nated by ygen iso topes, but lim ited data in di cate the high est d13C val ues sporomorphs (mostly bisaccate pol len grains) – up to 70%; and the low est d18O val ues at the base and top of the sec tion, black opaque, dark brown phytoclasts and small-sized cu ti cles and much a smaller range of fluc tu ation of d18O val ues than of are sub or di nate – up to 15%; the ra tio of highly disin te grated d13C val ues (Fig. 8). There is a dis tinc tive, grad ual up wards in - structureless par ti cles is dif fi cult to eval u ate, it pre sum ably does crease in Dd18O, from 0.9‰ in the low est sam ple, to 2.2‰ in the not ex ceed 10%. Aquatic palynomorphs are rel atively rare: high est sam ple, how ever, this trend is based on only four sam - dinoflagellate cysts are 1–2%, in fre quent Leiosphaeridia occur. ples (Fig. 8). Dinoflagellate cysts are well-pre served; their as sem blage is When com pared to roughly coeval foraminifers from other dom i nated by Spiniferites spp. (over 70% of all cysts; mainly Up per Badenian bas ins of the Cen tral Paratethys, our data for Spiniferites ramosus). The re main ing part of the as sem blage Globigerina bulloides is sim i lar to data from the Vi enna Ba sin con sists of com mon Operculodinium spp., Lingulodinium (Fig. 9). As far as our data for benthic foraminifera, mostly machaerophorum, Melitasphaeridium pseudorecurvatum, M. Bulimina elongata, is con cerned, five of eight sam ples stud ied choano phorum, Labyrinthodinium truncatum, less frequent gave re sults iden ti cal or close to those char ac ter is tic of Systema tophora placacantha, Hystrichokolpoma rigaudiae, Uvigerina of the Vi enna Ba sin, but three sam ples show devi a - Nematosphaeropsis labyrinthus, and sin gle spec i mens of tions in d val ues that are smaller by 1–2‰ compared to the Vi - Impagidinium sp. and Systematophora cf. placacantha (Table 1). enna Ba sin (Fig. 9). Both the Shchyrets sec tion and sec tions Rare re worked spec i mens of rew orked Paleogene Cordo - from the Vi enna Ba sin show clearly higher d18O val ues and sphaeridium? funiculatum, and Wetzeliella sp. have been found. clearly lower d13C val ues that the Up per Badenian Uvigerina Sam ple M-2 con tains sim i lar palynofacies (Table 1). and plank tonic foraminifera from the Pannonian Ba sin (Fig. 9). Dinoflagellate cysts (2%) are also dom i nated by Spiniferites spp., al though not so pro nouncedly as in lower sam ple M-1 – 40%. Operculodinium spp. and Lingulodinium machaero - PALYNOLOGY phorum are very fre quent, whereas Melitasphaeridium pseudo - recurvatum, M. choanophorum, Nematosphaeropsis labyrin - All sam ples yielded palynological or ganic mat ter (Fig. 10). thus, Labyrinthodinium truncatum, Reticulatosphaera actino - How ever, its quan tity and qual ity dif fers in par tic ular sam ples. coronata, and Homotryblium floripes are less com mon (the lat - Foraminiferal and palynological records of the Late Badenian... 473

Fig. 7. Rela tiv e abundances of dysoxic, suboxic and oxic ben thic foraminifers in the Shchyrets sec tion

Fig. 8. Iso tope pro file of foraminifers from Shchyrets Quarry and their palaeotemperatures 474 Danuta Peryt, Przemys³aw Gedl and Tadeusz Marek Peryt

oc cur. A sin gle iso lated pro cess most likely rep re - sents part of a rew orked Paleogene spec i men of Adnatosphaeri dium. A sim i lar palynofacies oc curs in sam ple M-7: dom i nat ing pol len grains (over 70%), black and dark brown woody parti cles (10%), small cu ti cles (8%), and aquatic palynomorphs (10%) (Fig. 13). The lat - ter are repre sented mainly by dinoflagellate cysts, which are more tax onom i cally diverse than in the lower sam ple. Al though dom i nated by Spini ferites spp. (70%), they also in clude fre quent Oper culo - dinium spp. and Batiacasphaera sp. Moreover, rel a - tively fre quent spec i mens of Nematosphaerio psis labyrinthus, Labyrinthodinium truncatum, Systema- to phora placacantha, and Melitasphaeri dium Fig. 9. Plot of d13C and d18O val ues of Up per Badenian foraminifers choanophorum oc cur. Rare spec i mens of Hystri cho- from Shchyrets Quarry kolpoma salacia, Dapsilidinium sp., Imperfe - ctodinium septatum, Impagidinium cf. aculeatum, ter spe cies might be re worked from Paleogene strata; see Phelodinium sp., and Reticulatosphaera actino coro nata have Gedl, 2005 for dis cus sion). A sin gle spec i men of re worked been found. A few iso lated pro cesses have been found, which, Cerodinium (Up per Cre ta ceous–Paleocene) has been found. as in sam ple M5, presum ably repre sent frag ments of re worked The higher sam ple M-5 is dis tin guished by a higher ratio of Paleogene spec i mens. Aquatic palyno morphs in this sam ple are dinoflagellate cysts – up to 15% (pale-col oured and thin-walled also rep re sented by the acritarch Nannobarbophora. pol len grains form 60%, and highly disin te grated black phyto- The fol low ing two sam ples, M-8 (+285 cm) and M-10 clasts com prise 25%) (Fig. 13). Dinoflagellate cyst as sem blage (+300 cm), are char ac ter ized by very small amounts of is tax o nom i cally im pov er ished: it con sists of Spini ferites spp., palynological organic mat ter, which con sists al most ex clu sively and less frequent Systematophora placacantha, Lingulodinium of black opaque phytoclasts. Rare bisaccate pol len grains oc - machaerophorum, and Operculodinium spp. Sin gle spec i mens cur in both sam ples; sam ple M-8 ad di tion ally con tains rare dark of Hystrichokolpoma rigaudiae and Impagidinium cf. aculeatum brown cu ti cle frag ments, and sin gle spec i mens of Spiniferites

Fig. 10. Palynofacies of the Shchyrets suc ces sion A, B – palynofacies of sam ple M-1 char ac terized by domi nation of pol len grains; dinoflagellate cysts are in frequent; C – sam ple M-7 showing palynofacies dom i nated by pollen grains, but aquatic el ements (mainly dinoflagellate cysts) show rela tively high ratios; D – palynofacies of sam ple M-8 con sist ing al most ex clu sively of black opaque phytoclasts Foraminiferal and palynological records of the Late Badenian... 475

Ta ble 1

Dis tri bution of dinoflagellate cysts in the Shchyrets suc ces sion

Pre-Mio cene re worked species high lighted with an as terisk sp., Lingulo dinium machaerophorum, and Operculodinium The palynofacies of sam ple M-15 – the high est of the sam - centro carpum (cf. Fig. 13) ples stud ied – qual i ta tively re sem bles that of lower sam ples (Fig. The amount of palynological organic mat ter in creases in 13), but sig nif i cantly dif fers by much lower amounts of sam ple M-12, col lected 9 cm above sam ple M-10. Its palyno- palynological organic mat ter. Also, the dinoflagellate cyst as sem - facies consists of sporomorphs (50%, mainly bisaccate pol len blage tax o nom i cally gen er ally re sem bles ones from sam ples grains), black opaque phytoclasts (30%), and dino flagellate M-14 and M-12, but spec i mens are much rarer. It is dom i nated cysts (over 15%). The lat ter are dom i nated by Spini ferites spp. by Spiniferites spp., and less frequently by Operculodinium spp. and the mor pho log i cally sim i lar ge nus Achomo sphaera. The Rare or sin gle spec i mens of the fol low ing taxa oc cur: fol low ing taxa oc cur fre quently: Melitasphaeri dium pseudo - Lingulodinium machaerophorum, Achomosphaera sp., recur vatum, Operculodinium spp., M. choanopho rum, Syste- Melitasphaeridium choanophorum, Labyrinthodinium truncatum, ma tophora placacantha, and Lingulodinium machaero pho rum; Impagidinium sp., Hystrichokolpoma salacia, Pentadinium sp., less com mon are: Nematosphaeropsis labyrin thus, Impa - Nematosphaeropsis labyrinthus, and Batiacasphaera? sp. gidinium sp., Reticulatosphaera actinocoro nata, Penta dinium sp., and Hystrichokolpoma salacia. Rel a tively fre quent are spec i mens of re worked Paleogene MINERALOGY taxa: Homotryblium tenuispinosum, Hystrichosphaeridium tubi - ferum, fragmentarily pre served (mainly isolated pro cesses) The re sults of XRF anal ysis are shown in Table 2. In all Areosphaeridium (in clud ing A. diktyoplokum), and Cordo - sam ples stud ied cal cite, quartz and smectite were re corded, sphaeridium. and the lat ter mineral oc curs in greater pro por tion in sam ples A sim i lar palynofacies dom i nated by bisaccate pol len grains M-10 and M-12. The three miner als are ac com panied, in the and a rel atively high ra tio of dinoflagellate cysts (15%) oc curs in lower part of sec tion stud ied (sam ples M-1 and M-2), by gyp- sam ple M-14 (Fig. 13). Also the tax onom i cal com posi tion of the sum, feld spar, ze o lite, py rite, illite, and chlorite, and these min - dinoflagellate cyst as sem blage is sim i lar to the one from the er als (ex cept for gypsum) are pres ent in other sam ples in the lower sam ple: it is dom i nated by Spiniferites and, to a lesser de - sec tion. In the mid dle part of the sec tion, ar agonite and gree, by Systematophora placacantha. Achomosphaera spp., muscovite were identified (Table 2). Melitasphaeridium pseudorecurvatum, Operculodinium spp., M. choanophorum, Reticulatosphaera actinocoronata, and Lingulodinium machaerophorum, which all oc cur frequently; INTERPRETATION Nematosphaeropsis labyrinthus, Labyrinthodinium truncatum, and Batiacasphaera? sp. are less nu mer ous. Sin gle spec i mens of Impagidinium and Cordosphaeridium cantharellum have FORAMINIFERAL RECORD been found. In this sam ple, as in sam ple M-12, re worked Paleogene taxa oc cur: Deflandrea sp., Areosphaeridium sp., The dom i nant spe cies re corded in the in ter val rep re sented and Hystrichosphaeridium tubiferum. by samples M-1 to M-14 in di cate a depth of ca. 50 m (Fig. 14) as 476 Danuta Peryt, Przemys³aw Gedl and Tadeusz Marek Peryt

Fig. 11. Dinoflagellate cysts and acritarchs from Shchyrets A–D – Labyrinthodinium truncatum (A–C: same spec i men, var i ous foci, M-15; D: M-14); E, F – Pyxidiniopsis sp. (both spec i mens M-14); G, H – Impagidinium spp. (G: M-15, H: M-14); I–K – Melitasphaeridium choanophorum (I, J: same spec i men, var i ous foci, M-14; K: M-15); L–O – Nematosphaeropsis labyrinthus (L, M and N, O: same spec i mens, var i ous foci; both spec i mens: M-14); P – Reticulatosphaera actinocoronata (M-14); Q, R – Operculodinium piaseckii (same spec i men, var i ous foci, M-14); S – Spiniferites sp. (M-14); T, U – Nannobarbophora gedlii (T: M-7, U: M-14); V – Achomosphaera sp. (M-14); W – Spiniferites sp. (M-14); X – Batiacasphaera sp. (M-7); Y – Spiniferites ramosus (M-14) Foraminiferal and palynological records of the Late Badenian... 477

Fig. 12. Dinoflagellate cysts from Shchyrets A, B – Hystrichokolpoma rigaudiae (both spec i mens: M-7); C – Pentadinium laticinctum (M-12); D–F – Lingulodinium machaerophorum (D: M-14; E, F: same spec i men, var i ous foci, M-14); G – Operculodinium centrocarpum (M-15); H, I – Operculodinium spp. (both spec i mens: M-15); J – Spiniferites pseudofurcatus (M-15); K, L – Systematophora placacantha (K: M-15, L: M-14)

Bulimina elongata lives at depths of >15 m, Heterolepa Majewski and Bohaty, 2010). Globigerinoides in turn is a sur - dutemplei at depths of >40 m, and Globocassidulina at depths face-dweller com mon in warm, oligotrophic waters of the mixed of >50 m (Hohenegger, 2005). Very low P/B val ues (0–5%) in layer, with high est abun dances in re gions where there is a per - the in ter val and tax o nomic com po si tion of plank tonic foramini - ma nent ver ti cal strat i fi ca tion of the wa ter col umn (Hemleben et feral as sem blages also in di cate in ner shelf depths (Murray, al., 1989; Di Stefano et al., 2010). 1991). Plank tonic foraminifera, mostly Globigerina and rarely Deep ening of the sea is in ter preted for in ter val start ing Globigerinoides, in di cate a shal low cool sea. Globigerina from sam ple M-15 where Uvigerina dom i nates, which ac cord - bulloides is a mixed-layer, cold-water dweller adapted to more ing to Hohenegger (2005) lives not shal lower than 70 m. At the eutrophic waters, tol er ant of a wide range of typi cal oce anic sa - same level the P/B ratio sig nif i cantly increases and ex ceeds lini ties (Pujol and Vergnaud-Grazzini, 1995; Majewski, 2003; 50% (Fig. 14). 478 Danuta Peryt, Przemys³aw Gedl and Tadeusz Marek Peryt

Fig. 13. Palynofacies changes in the Shchyrets suc ces sion

In the lowest part of the in ter val, the fre quency of infaunal of oxic con di tions at the sea floor in the higher part of the sec tion Bulimina is very high and exceeds 80%. Very high domi nance (sam ple M-2) is shown by a low-dom i nance as sem blage, char - of Bulimina in di cates proba bly not only very low oxy gen lev els ac ter ized by a rela tively low abundance of dysoxic forms in fa - at the sea floor caus ing stress for ben thic life, but prob ably also vour of suboxic ones that are rep re sented mostly by nodo - in creased sa lin ity, as Bulimina is tol er ant of both dysoxia and sariids, nonionids, and Lobatula lobatula; Cibicidoides spp. rep - high bot tom-wa ter sa lin ity (Verhallen, 1991). The ame lio ra tion re sent oxic forms. Then, the de po si tion of thin tuffite bed at the sea bot tom, pos si bly the result of Trans carpa - Ta ble 2 thian vol ca nic ac tiv ity of Badenian age (see Bilonizhka et al., 2012 with ref er ences therein), Min er al og i cal com po si tion of sam ples stud ied exter mi nated the biota for a short time (cf. Hess et al., 2001; Zágoršek et al., 2012). Hess et al. Sam ple num ber M-1 M-2 M-5 M-7 M-8 M-10 M-12 M-14 M-15 (2001), by mon i tor ing the recolo nisation of the Sam ple lo ca tion Mt Pinatubo 1991 ash layer by ben thic above the Ratyn 0.75 1.05 1.71 2.35 2.85 3.0 3.09 3.89 4.29 foraminifera, dis cov ered that recolo nisation was Lime stone [m] very fast and took only a few years for a com - Cal cite + + + + + + + + + plete re cov ery of the foraminiferal benthic com - Quartz + + + + + + + + + mu ni ties. The steps of recolonisation were not Gypsum + + rec og nized in the ma te rial stud ied. The M-8 Feldspar + + + + + + sam ple over ly ing the tuffite bed con tains a ben - thic foraminiferal as sem blage re flect ing a Ze o lite + + + + mesotrophic en vi ron ment at sur face wa ters and Py rite + + + no oxy gen def i cit at the sea floor. The epifaunal Ar agon ite + + dweller Heterolepa dutemplei con sti tutes there Opal/cristoballite + >25% of the as sem blage. This as sem blage Smectite + + + + + ++ + ++ + con tains the high est oxic in di ces found in the Illite + + + + en tire sec tion stud ied. Mus co vite + + In the in ter val rep re sented by sam ples M-7 to M-14 deep infaunally liv ing foraminifera dom i - Mus co vite/illite + nate: dysoxic, or op por tu nis tic forms. Their con - Chlorite + + + + + + tri bution to the as sem blages var ies from 70 to Foraminiferal and palynological records of the Late Badenian... 479

Fig. 14. Palaeoenvironmental changes in the Late Badenian basin at Shchyretsi based on in ter pre ta tion of foraminifera and dinoflagellate cyst assem blages

80%, which in di cates mesotrophic/eutrophic en vi ron ments at blage to 62%, dom i nance of Uvigerina (mid dle shelf – bathyal sur face waters, and a large in flux of or ganic mat ter to the sea form), in creased di ver sity and a high P/B ra tio in di cates deep - bot tom, where a lot of oxy gen was con sumed for its deg ra dation. ening of the sea to mid dle shelf depth, a mesotrophic en vi ron - The benthic foraminiferal as sem blages are com posed ment at the sur face, a lower in flux of or ganic mat ter to the bot - mainly by Bulimina and Globocassidulina. How ever, their rel ative tom, and better oxy gen a tion at the sea floor (Fig. 14). abundances vary from sam ple to sam ple. In sam ples M-7, M-10, In gen eral, both benthic and plank tonic d13C val ues in di cate and M-13 Bulimina dom i nates form ing from 56 to 77% of the as - the nu tri ent-rich con di tions in the Ukrai nian Carpathian sem blages. The con tri bu tion of Globocassidulina in these sam - Foredeep Ba sin dur ing the Late Badenian, al though they are ples var ies from 15 to 25%. On the other hand in sam ples M-8, prob ably the most clearly ex pressed in the low est part of the M-12, and M-14 Globocassidulina dom i nates in ben thic fora - sec tion, pos si bly due to in creased in put of con ti nen tal or ganic miniferal as sem blages and its con tri bution to the as sem blages mat ter dur ing the trans gres sion. Neg a tive d13C val ues of exceeds 60%. Lev els where small Globocassidulina dom i nate Bulimina and Uvigerina in di cat ing nu tri ent-rich and 13C-de - may indi cate the high est def i cit of oxy gen at the sea floor. Small, pleted pore-wa ter con di tions cor re spond to the dom i nance of thin-walled foraminiferal tests are com mon in low-oxy gen envi - low-ox y gen ben thic foraminiferal in di ca tors, such as Bulimina ron ments where foraminifera must withstand the acidic con di - elongata (cf. Kováèová and Hudáèková, 2009). tions of ten as so ci ated with or ganic en rich ment (Bernhard, 1986). There are sev eral fac tors con trol ling foraminiferal d18O dis- Fursenkoina acuta, Astrononion perfossum, and Sigmoilinita tri bu tion, al though tem per a ture changes played a de ci sive role tenuis are im por tant con tri bu tors in these as sem blages. As sem - in the Carpathian Foredeep Ba sin as well as in the Vi enna Ba - blages where Bulimina pre vails are more di verse, which prob a - sin (see dis cus sion in Kováèová and Hudáèková, 2009). In turn, bly reflect s better oxy gen a tion at the sea floor (Fig. 14). strongly neg a tive d18O val ues mea sured in Late Badenian The rea son for change in the rel ative abun dances of plank tonic foraminifers (see Figs. 8 and 9) were inter preted by Bulimina and Globocassidulina in this in ter val re mains enig - Báldi (2006) as due to less sa line sur face water. In their study of matic. One of the pos si ble rea sons could be a change of type Badenian foraminifera from the Vi enna Ba sin, Kováèová et al. 18 and/or qual ity of food sink ing from the sur face waters (cf. Peryt (2009) as sumed a d Owater of 0‰, and cal cu lated that palaeo - et al., 2002). water tem per atures, if the equa tion of Epstein et al. (1953) is The ben thic foraminiferal as sem blage from the top most applied, would be 6.3–8.5°C for ben thic foraminifers (mostly sam ple (M-15) is also dom i nated by dysoxic forms, but there is Uvigerina) and 9.7 to 17.7°C for Globigerina. Those val ues are a com plete re or gani za tion of the as sem blage: Bulimina and sim i lar to those re corded by us (5.4–8.4°C for Globocassidulina are ab sent, and Uvigerina forms 57% of the Bulimina/Uvigerina if two anoma lous val ues of 11.5 and 17.1°C as sem blage. Sphaeroidina bulloides, a shal low infauna dweller, are ig nored, and 12.9–15.7°C for Globigerina). However, we 18 is the sec ond im por tant com ponent of this as sem blage. as sume that d Owater was higher, al though most prob ably be- Sigmoilinita tenuis and Pullenia bulloides reach 5% each of the low 1‰. to tal. A de creased con tri bu tion of dysoxic forms to the as sem - 480 Danuta Peryt, Przemys³aw Gedl and Tadeusz Marek Peryt

Palaeotemperatures cal cu lated from the ox ygen iso tope ra - shows the low est val ues in the basal part (sam ples M-1 to tios of foraminifers (Fig. 8) in di cate dif fer ences be tween the bot - M-7), which may reflect a rel atively shal low basin com pared to tom water and the water col umn (Fig. 8). The in crease in Dd18O the top most part (sam ples M-12 to M-15). (from 0.9‰ in sam ple 1 to 2.2‰ in sam ple M-15) clearly sug - gests an up wards-in creas ing trend in the strat i fi ca tion of the wa - ter col umn. Such an in creas ing strat i fi ca tion trend was ear lier re - MINERALOGY corded in other parts of the Cen tral Paratethys: in the Vi enna Ba - sin (Kováèová et al., 2009), the Up per Silesia Basin (Gonera et There is no ma jor vari a tion of min er al og i cal com po si tion in al., 2000), and in the Pannonian Basin (Báldi, 2006), pos si bly the sec tion studied (Table 2). Clay min eral com posi tion was due to mod i fi ca tion of ba sin cir cu la tion (Kováèová et al., 2009). strongly con trolled by pyroclastic ma te rial al ter ation that re - sulted in the com mon oc cur rence of smectite (cf. Bilonizhka et al., 2012). As al ready mentioned, thin tufogenic in ter ca la tions PALYNOLOGICAL RECORD abound at Shchyrets (Kudrin, 1966; Nejbert et al., 2012).

A char ac ter is tic of the de pos its stud ied is a palynofacies dom i nated by bisaccate pol len grains. This fea ture, as so ci ated DISCUSSION with rel atively com mon aquatic el ements, and an al most com - plete lack of large cu tic ular re mains, indi cates a hemipelagic Both foraminiferal and dinoflagellate cyst as sem blages in di - sed i men tary set ting de void of di rect, in tense ter res trial in flux. cate an open ma rine en vi ron ment with nor mal-ma rine sa lin ity Dom i nat ing pol len grains were pre sum ably trans ported by (Fig. 14). Foraminifers are rep re sented by both plank tonic wind. Ra tio changes of dinoflagellate cysts and pol len grains (mainly Globigerina and Globigerinoides) and ben thic forms. sug gest slightly variable sedimentary conditions (Fig. 14). Bulimina, Globocassidulina, Uvigerina, Sphaeroidina, Pullenia, Basal sam ples M-1 and M-2 con tain a rel atively low ra tio of Heterolepa, and Fursenkoina which are com mon to dom i nant in dinoflagellate cysts com pared to the over whelm ing pol len ben thic foraminiferal as sem blages are shelf-bathyal spe cies grains. This may reflect a proxi mal site in flu enced by an intense (Murray, 1991, 2006; Hohenegger, 2005). A low di ver sity of in flux of pol len grains (ei ther by wind or water cur rents). The ben thic foraminiferal as sem blages, with high dom i nance of higher sam ples M-5 and M-7 con tain a higher ratio of infaunal dysoxic forms, in di cates nu tri ent-rich sur face wa ters dinoflagellate cysts, pre sum ably result ing from a less in tense and a def i cit of oxy gen at the sea floor. Fluc tu ations in rel ative land in flux. This most likely reflect s a more off shore sed i men - abun dances of dom i nant infaunal taxa in di cate prob a bly not tary set ting in com par i son to the basal in ter val, al though only changes in the quan tity of or ganic mat ter sink ing from the changes in hy dro dy namic cir cu la tion or wind di rec tion can not sur face but also in its type and/or qual ity. Dinoflagellate cyst as - be excluded. The lat ter may be re spon si ble for the palynolo- sem blages from all sam ples stud ied are qual i ta tively sim i lar gical con tent of fol low ing two sam ples M-8 and M-10, which (except those of sam ples M-8 and M-10, which con tain no con tain very low amounts of palynological organic mat ter. Such spec i mens or very in fre quent ones). Be ing dom i nated by con tent may be related to a very shallow la goon en vi ron ment, Spiniferites, they are tax o nom i cally rel a tively di verse, point ing or an en vi ron ment char ac ter ized by high-en er getic hy dro dy - to a nor mal ma rine en vi ron ment dur ing de po si tion of the namic cur rent ac tiv i ties (Fig. 14). A gen eral shallowing at this Shchyrets suc ces sion. The lat ter feature is confirm ed by a vir- level may be suggested by fre quent oc cur rences of Batiaca - tual lack of spe cies tol er ant of hypersaline con di tions (e.g., sphaera in the un der lying sam ple M-7. This taxon com monly Polysphaeridium zoharyi; Wall and Dale, 1969; Dale, 1976; oc curs in shal low-wa ter Mio cene de pos its of the Carpathian Wall et al., 1977; Morzadec-Kerfourn, 1979, 1983; Brad ford and Foredeep (see Gedl, 1996, 1997). Wall, 1984; Ed wards and Andrle, 1992), which have been re - The high est part of the suc ces sion stud ied (sam ples M-12, cently de scribed from ap prox i mately co eval de pos its of M-14 and M-15) dis plays sim i lar palynofacies to the one repre - Kudryntsi (Gedl and Peryt, 2011). The only indi ca tion of stress sented by sam ples M-5 and M-7. Hence, a sim i lar sed i men - con di tions in the ma te rial stud ied, pre sum ably re lated to in - tary set ting may be re con structed: rel atively fre quent creased sa lin ity, is the very high domi nance of Bulimina and the dinoflagellate cysts, as so ci ated with pol len grains (presum - oc cur rence of in fre quent Leiosphaeridia in basal sam ple M-1 ably wind-trans ported), point to hemipelagic sed i men ta tion in (Fig. 14). This seem ingly prasinophycean alga (see Guy- a rather off shore set ting. The lat ter feature of sed i men tary set - Ohlson, 1996) is reported from var i ous en vi ron ments, but com - ting is also sup ported by the oc cur rence of Nemato - monly from hypersaline ones (e.g., Brugman et al., 1994). In the sphaeropsis labyrinthus and Impagidinium sp. Al though in fre - Carpathian Foredeep this ge nus oc curs in mid-Badenian quent, these taxa are be lieved to be in dic ative of off shore wa - evaporitic de pos its (Gedl, 1997; Gedl in Peryt et al., 1997) or in ters (e.g., Morzadec-Kerfourn, 1977; Wall et al., 1977; strata di rectly over lying them (Gedl, 1999). This is in con cert Harland, 1983; Dale, 1996; Rochon et al., 1999; Vink et al., with the ben thic and plank tonic d13C val ues clearly in di cat ing 2000), oc cur in al most all sam ples stud ied, and therefore may nutri ent-rich con di tions, es pe cially in the low est part of the sec - be symptom atic of the whole Shchyrets suc ces sion. Their per - tion, pos si bly due to an increased in put of con ti nental or ganic cent age, how ever, reaches the high est val ues in the up per mat ter dur ing the trans gres sion. part of the sec tion, above the bar ren sam ples M-8 and M-10, The Kosiv suite at Yaziv Field, located 44 km NNW of being the high est in the top most sam ple M-15. This may re- Shchyrets in a roughly sim i lar palaeo geo graphi cal lo ca tion, flect a slight deep ening of the ba sin, re corded in the up per - con sists of a 8.3 m thick sec tion of the Verbovets beds fol lowed most part of the sec tion studied. A sim i lar in ter pre ta tion may by a 3 m thick sec tion of the Prut and Kolomyia beds (Goretsky, be based on dinoflagellate cyst as sem blage di ver sity. This 1977). Goretsky (1977) re corded the first plank tonic fora - Foraminiferal and palynological records of the Late Badenian... 481 minifers (Globigerina bulloides) 5.1 m above the Ratyn Lime - 3. Bulimina and Globocassidulina are the most com mon stone, and a quite rich as sem blage of ben thic foraminifers and dom i nant com po nent of ben thic foraminiferal assem - (Cibicides, Bulimina, Neobulimina, Glandulina) oc curs in the in - blages, ex cept of the up per most part where they are lack ing ter val 5.8–8.3 m above the Ratyn Lime stone. At Shchyrets, and Uvigerina dom i nates the as sem blage. In the up per most both ben thic and plank tonic foraminifers appear much lower in part the P/B ratio is 57% in con trast to the rest of the sec tion, the strati graphic sec tion. This may be due to oxy gen ation and where it is <5%, and this in di cates deep en ing of the sea. The pro duc tiv ity changes in the mar ginal part of the Ukrai nian lat ter is recorded in the palynological record by the high est per - Carpathian Foredeep Ba sin, close to its basinal part af ter the cent age (over 16%) of off shore taxa (Nematospaheropsis Badenian sa lin ity cri sis. labyrinthus and Impagidinium) in the topmost sam ple, whereas it is 5% or lower in the remain ing part of the sec tion. 4. The com po si tion of ben thic foraminifer as sem blages as CONCLUSIONS well as both ben thic and plank tonic d13C val ues in di cate nu tri - ent-rich waters, mesotrophic to eutrophic en vi ron ments at the sur face, and low oxy gen ated en vi ron ments at the sea floor in 1. The marly shales over lying mid-Badenian gypsum and the Ukrai nian Carpathian Foredeep Ba sin dur ing the Late Ratyn Lime stone at Shchyrets con tain mod er ately- to well-pre - 13 Badenian. Neg a tive d C val ues of Bulimina and Uvigerina in di - served ben thic (only calcar eous) and plank tonic foraminifers; 13 cat ing nu tri ent-rich and C-de pleted pore-wa ter con di tions cor - thirty-eight spe cies of ben thic and nine spe cies of plank tonic re spond to the dom i nance of low-oxy gen ben thic foraminiferal foraminifers were re corded. The palynofacies is dom i nated by in di ca tors, such as Bulimina elongata. bisaccate pol len grains. Twenty-six taxa of dinoflagellate cysts 6. Palaeotemperatures cal cu lated from the ox ygen iso tope were noted; in fre quent re worked taxa from Up per Cre ta ceous ra tios of foraminifers in di cate dif fer ences be tween the bot tom and Paleogene were also re corded. Both foraminiferal and water and the water col umn and an up wards-in creas ing trend in dinoflagellate cyst as sem blages in di cate an open ma rine en vi - the strat i fi ca tion of the water column. ron ment with nor mal-ma rine sa lin ity. It was rather a shal low ma - rine ba sin with a lim ited in flux of ter res trial or ganic mat ter, ex- Ac knowl edge ments. The field work and anal yses were cept for pol len grains, pre sum ably transported by wind or water funded by research grant No. 6 P04D 009 11 (Com mit tee on currents. Sci en tific Re search) to T.M. Peryt and spe cial grant No. 2. Changes in the rel ative abun dances of dom i nant and Ukraina/193/2006 (Min is try of Sci ence and Higher Ed uca tion) com mon spe cies within ben thic foraminiferal as sem blages, of to M. Kotarba. We thank A.V. Poberezhskyy for his help in the dinoflagellate cysts, and of pol len grains in di cate slightly vari - field. The com ments and sugges tions given by the journal re - able sed i men tary conditions. view ers, N. Hud´èková and A. Poberezhskyy, are ap pre ci ated.

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