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Annales Societatis Geologorum Poloniae (2011), vol. 81: 331–349. DINOFLAGELLATE CYST, PALYNOFACIES AND FORAMINIFERAL RECORDS OF ENVIRONMENTAL CHANGES RELATED TO THE LATE BADENIAN (MIDDLE MIOCENE) TRANSGRESSION AT KUDRYNTSI (WESTERN UKRAINE) Przemys³aw GEDL 1 & Danuta PERYT 2 1 Institute of Geological Sciences, Polish Academy of Sciences, Senacka 1, 31-002 Kraków, Poland, e-mail: [email protected] 2 Institute of Paleobiology, Polish Academy of Sciences, Twarda 51/55, 00-818 Warszawa, Poland, e-mail: [email protected] Gedl, P. & Peryt, D., 2011. Dinoflagellate cyst, palynofacies and foraminiferal records of environmental changes related to the Late Badenian (Middle Miocene) transgression at Kudryntsi (western Ukraine). Annales Societatis Geologorum Poloniae, 81: 331–349. Abstract: Qualitative and quantitative characteristics of the palynological content of the Upper Badenian strata at Kudryntsi (western Ukraine) indicate that this succession was deposited in variable environments. The basal siliciclastic series shows a very low content of palynological organic matter and palynofacies, which indicate a restricted environment and/or unfavourable conditions for the palynomorph preservation. The presence of dinofla- gellate cysts (and composition of their assemblages) in the upper part of organodetrital limestones and the overlying rhodoid limestones indicates a typical shelf environment. Taxonomically variable dinoflagellate cyst assemblages from particular samples reflect gradual environmental changes – from environments of slightly increased salinity of seawater (strata overlying the siliciclastic series) to open marine, more remote environments during deposition of the upper part of the section examined. The gradual deepening of the sea and decrease of salinity is supported also by the succession of foraminiferal assemblages, which undergo gradual changes from Elphidium spp. assemblages, through Miliolidae assemblage, Lobatula lobatula assemblage, Neoconorbina spp. assemblage to Cibicidoides assemblage. The Late Badenian foraminiferal assemblage from Kudryntsi contains two species common for the Sarmatian, i.e. Elphidium reginum and Elphidium koberi, the latter species known so far from the Sarmatian. Key words: palaeoenvironment, dinoflagellate cysts, foraminifers, Upper Badenian, Middle Miocene, Paratethys, Carpathian Foredeep. Manuscript received 3 June 2011, accepted 3 November 2011 INTRODUCTION This paper deals with deposits related to the major Late Badenian transgression, which took place when the connec- tion of the Carpathian Foredeep Basin with other Parate- thyan basins was restored due to the sea level rise (Osz- czypko et al., 2006; Peryt, 2006). In places, as Kudryntsi in western Ukraine, the evidently marine deposits (limestones and intercalated marls with abundant faunal assemblage) forming the basal part of the Upper Badenian transgressive sequence are underlain by the pelites of the siliciclastic se- ries occurring above the Badenian gypsum deposits (Peryt & Peryt, 2009). The earlier foraminiferal and geochemical study of these pelites showed that they formed in restricted environments (Peryt & Peryt, 2009). The aim of the paper is to compare the dinoflagellate cyst and foraminiferal records obtained from the same set of samples collected from the Upper Badenian transgressive section that is currently exposed at Kudryntsi gypsum quarry. Dinoflagellates are unicellular, mainly autotrophic, or- ganisms inhabiting almost all aquatic ecosystems, from freshwater to marine and hypersaline. During their life-cy- cle they produce resting cysts, which in some species are fossilizable. Studies on Recent dinoflagellate cyst distribu- tion (e.g., Dale, 1976; Wall et al., 1977; Harland, 1983; McMinn, 1990; Edwards & Andrle, 1992; Rochon et al., 1999; Vink et al., 2000; Marret & Zonneveld, 2003) allow for relative precise palaeoecological interpretation of Mio- cene forms, which in major part are also known from Holo- cene deposits. Therefore, their presence makes possible ba- sic reconstructions of fossil material related to such factors

DINOFLAGELLATE CYST, PALYNOFACIES AND ......Dinoflagellate cyst, palynofacies and foraminiferal records of en vi ron men tal changes re lated to the Late Badenian (Mid dle Mio cene)

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Page 1: DINOFLAGELLATE CYST, PALYNOFACIES AND ......Dinoflagellate cyst, palynofacies and foraminiferal records of en vi ron men tal changes re lated to the Late Badenian (Mid dle Mio cene)

Annales Societatis Geologorum Poloniae (2011), vol. 81: 331–349.

DINOFLAGELLATE CYST, PALYNOFACIES AND FORAMINIFERAL RECORDS OF ENVIRONMENTAL CHANGES RELATED

TO THE LATE BADENIAN (MIDDLE MIOCENE) TRANSGRESSIONAT KUDRYNTSI (WESTERN UKRAINE)

Przemys³aw GEDL1 & Danuta PERYT2

1 In sti tute of Geo log i cal Sci ences, Pol ish Acad emy of Sci ences, Senacka 1, 31-002 Kraków, Po land,e-mail: [email protected]

2 In sti tute of Paleobiology, Pol ish Acad emy of Sci ences, Twarda 51/55, 00-818 Warszawa, Po land,e-mail: [email protected]

Gedl, P. & Peryt, D., 2011. Dinoflagellate cyst, palynofacies and foraminiferal re cords of en vi ron men tal changesre lated to the Late Badenian (Mid dle Mio cene) trans gres sion at Kudryntsi (west ern Ukraine). Annales SocietatisGeologorum Poloniae, 81: 331–349.

Ab stract: Qual i ta tive and quan ti ta tive char ac ter is tics of the palynological con tent of the Up per Badenian strata atKudryntsi (west ern Ukraine) in di cate that this suc ces sion was de pos ited in vari able en vi ron ments. The basalsiliciclastic se ries shows a very low con tent of palynological or ganic mat ter and palynofacies, which in di cate are stricted en vi ron ment and/or un fa vour able con di tions for the palynomorph pres er va tion. The pres ence of dinofla- gellate cysts (and com po si tion of their as sem blages) in the up per part of organodetrital lime stones and theover ly ing rhodoid lime stones in di cates a typ i cal shelf en vi ron ment. Tax o nom i cally vari able dinoflagellate cystas sem blages from par tic u lar sam ples re flect grad ual en vi ron men tal changes – from en vi ron ments of slightlyin creased sa lin ity of sea wa ter (strata over ly ing the siliciclastic se ries) to open ma rine, more re mote en vi ron mentsdur ing de po si tion of the up per part of the sec tion ex am ined. The grad ual deep en ing of the sea and de crease ofsa lin ity is sup ported also by the suc ces sion of foraminiferal as sem blages, which un dergo grad ual changes fromElphidium spp. as sem blages, through Miliolidae as sem blage, Lobatula lobatula as sem blage, Neoconorbina spp.as sem blage to Cibicidoides as sem blage. The Late Badenian foraminiferal as sem blage from Kudryntsi con tainstwo spe cies com mon for the Sarmatian, i.e. Elphidium reginum and Elphidium koberi, the lat ter spe cies known sofar from the Sarmatian.

Key words: palaeoenvironment, dinoflagellate cysts, foraminifers, Up per Badenian, Mid dle Mio cene, Paratethys, Carpathian Foredeep.

Manu script re ceived 3 June 2011, ac cepted 3 November 2011

IN TRO DUC TION

This pa per deals with de pos its re lated to the ma jor LateBadenian trans gres sion, which took place when the con nec -tion of the Carpathian Foredeep Ba sin with other Parate-thyan bas ins was re stored due to the sea level rise (Osz-czypko et al., 2006; Peryt, 2006). In places, as Kudryntsi inwest ern Ukraine, the ev i dently ma rine de pos its (lime stonesand in ter ca lated marls with abun dant fau nal as sem blage)form ing the basal part of the Up per Badenian transgressivese quence are un der lain by the pelites of the siliciclastic se -ries oc cur ring above the Badenian gyp sum de pos its (Peryt& Peryt, 2009). The ear lier foraminiferal and geo chem i calstudy of these pelites showed that they formed in re stricteden vi ron ments (Peryt & Peryt, 2009).

The aim of the pa per is to com pare the dinoflagellatecyst and foraminiferal re cords ob tained from the same set of

sam ples col lected from the Up per Badenian transgressivesec tion that is cur rently ex posed at Kudryntsi gyp sumquarry.

Dinoflagellates are uni cel lu lar, mainly autotrophic, or -gan isms in hab it ing al most all aquatic eco sys tems, fromfresh wa ter to ma rine and hypersaline. Dur ing their life-cy -cle they pro duce rest ing cysts, which in some spe cies arefossilizable. Stud ies on Re cent dinoflagellate cyst dis tri bu -tion (e.g., Dale, 1976; Wall et al., 1977; Harland, 1983;McMinn, 1990; Ed wards & Andrle, 1992; Rochon et al.,1999; Vink et al., 2000; Marret & Zonneveld, 2003) al lowfor rel a tive pre cise palaeo eco logi cal in ter pre ta tion of Mio -cene forms, which in ma jor part are also known from Ho lo -cene de pos its. There fore, their pres ence makes pos si ble ba -sic re con struc tions of fos sil ma te rial re lated to such fac tors

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like wa ter sa lin ity, tem per a ture, dis tance from shore, pro -duc tiv ity (e.g. Dale, 1996). Dinoflagellate cysts have al -ready been used for these pur poses in stud ies of Mio cene ofthe Carpathian Foredeep (Gedl, 1996).

How ever, dinoflagellate cysts are not the only or ganicfos sils that oc cur in sed i men tary rocks. Fossilizable are also

par tic u lar fresh wa ter and ma rine al gae, sporomorphs, andtis sue re mains of ter res trial plants. As so ci a tion of these or -ganic par ti cles is known as palynofacies (Combaz, 1964;see also Tyson, 1995; Bat ten, 1996). Anal y sis of palynofa -cies el e ment ra tios, com bined with sedimentological data,serves for fur ther in ter pre ta tion of en vi ron men tal fac tors,in clud ing in ten sity of land in flux and sa lin ity level. Theywere also used for palaeoenvironmental re con struc tions ofthe Mio cene of the Carpathian Foredeep (Gedl, 1997, 1999) be ing par tic u larly use ful in case of the Mid dle Mio cene(Badenian) evaporite de pos its (Gedl in Peryt et al., 1997).

Foraminifers are an other group of microfossils com -monly used in stud ies of the Mio cene biostratigraphy andpalaeoenvironment of the Carpathian Foredeep (e.g., Sub-botina et al., 1960; Pishvanova, 1969; Szczechura, 1982;Czepiec, 1996; Gruzman & Trofimovich, 1996; Czepiec &Kotarba, 1998; Gonera, 2001; Peryt & Gedl, 2010; Garecka& Olszewska, 2011). En vi ron men tal re quire ments of re centben thic foraminifera have been the sub ject of many stud ies(e.g. Jorissen, 1987; Hottinger et al., 1993; Langer, 1993;Hay ward et al.,. 1997; de Rijk et al., 1999; Chendes et al.,2004; Fiorini, 2004; Debeney et al., 2005; Abbene et al.,2006; Milker et al., 2009). This makes that they are goodbioindicators of ma rine en vi ron ment changes (Murray,2006), es pe cially that some Mio cene foraminiferal spe ciesstill live in re cent seas.

GEO LOG I CAL FRAME WORK

The Kudryntsi gyp sum quarry is lo cated on the left sideof the Zbruch River Val ley in the fore land of the CarpathianForedeep Ba sin (Fig. 1). The stromatolitic gyp sum (ca. 23 mthick) ex ploited in the quarry lies on the Cenomanian sand -stones or on the Lower Badenian biodetrital (usu ally cora-lline al gal) lime stones (2 m thick); the lat ter are un der lainby thin basal brec cia that rests upon the Cenomanian (Peryt& Peryt, 2009). A unit of 4-m-thick fine siliciclastic de pos -its with in ter ca la tions of lime stones and fine-grained sand -stones (up to 15 cm thick) oc curs above the gyp sum (theTyras Suite; Peryt & Peryt, 2009). In the north ern part of the Kudryntsi quarry this unit is per va sively gypsified (Peryt etal., 2008).

This siliciclastic unit is over lain by a lime stone unit(1.3–1.4 m thick) com posed of lithoclastic and fossiliferouslime stones with mi nor in ter ca la tions of clays and marls(10–30 cm thick; Fig. 2), which is con sid ered to be the ma -rine fa cies of the Ratyn Lime stone (Peryt & Peryt, 2009)typ i cally over ly ing the gyp sum de pos its in this re gion (Sip-livyy et al., 1974). This lime stone is cov ered by the Up perBadenian rhodoid lime stones with mi nor in ter ca la tions ofmarls and claystones (Proniatyn fa cies of Teisseyre, 1900;cf. Siplivyy et al., 1974). Eastwards, this car bon ate fa cies ischar ac ter ized by oc cur rence of coralline al gae-vermetidreefs and a va ri ety of bioclastic fa cies (Kudrin, 1966).These strata in the neigh bour hood of Kudryntsi are morethan 10 m thick when not eroded (Siplivyy et al., 1974); inthe Kudryntsi quarry the ex posed sec tion reaches 6 m. Far-ther to ward the south west this car bon ate fa cies is re placedby the clayey-sandy-car bon ate fa cies that, in turn, passes

332 P. GEDL & D. PERYT

Fig. 1. Lo ca tion map show ing the gen eral dis tri bu tion of Up per Badenian fa cies (af ter Kudrin, 1966 and Siplivyy et al., 1974); 1 –car bon ate fa cies, 2 – clayey-sandy-car bon ate fa cies, 3 – sandy-clayey fa cies. In ad di tion, fa cies zones (I–IV) of the Badenian sul -phate de pos its (af ter Peryt, 2006) and the pres ent NE gyp sum limit are shown. Ab bre vi a tion: MD – Re pub lic of Moldova

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into sandy-clayey fa cies (Fig. 1) – a typ i cal Kosiv Suite.The bound ary be tween the car bon ate and clayey-sandy-car -bon ate fa cies is lo cated some 1.5 km SW of the Kudryntsiquarry (Fig. 1; Siplivyy et al., 1974).

The Up per Badenian strata are cov ered by Lower Sar-matian strata that are clearly transgressive; farther east-wards they over lie the older Mid dle Mio cene strata or theylie di rectly upon pre-Mio cene sub strate (Siplivyy et al.,1974) (Fig. 1). The Lower Sarmatian de pos its com prise bi -valve coquinas, bioclastic or oolitic grainstones, marls orclays, brec cias and con glom er ates, as well as serpulid-mi -crobialite reefs (Kudrin, 1966; Siplivyy et al., 1974; Jasio-nowski et al., 2003; Jasionowski, 2006).

The ear lier study of the Kudryntsi sec tion doc u mented a ma jor en vi ron men tal change dur ing the Late Badenian(Peryt & Peryt, 2009), fol low ing the ma rine in va sion intosouth east ern Po land and west ern Ukraine from the Med i ter -ra nean (Andreyeva-Grigorovich et al., 1997; Oszczypko etal., 2006; Kovaè et al., 2007). The siliciclastic se ries over ly -ing the gyp sum was de pos ited in evaporitic la goon in flu -enced by large in flows of con ti nen tal wa ters. The ma rineclay bed, which oc curs be low the lime stone unit con sid eredto be the Ratyn Lime stone, orig i nated in shal low subtidalen vi ron ments of nor mal ma rine sa lin ity and tem per ate towarm wa ters as in di cated by re quire ments of Elphidiumcrispum as so ci a tion in re cent seas (Peryt & Peryt, 2009).

MA TE RIAL AND METH ODS

We have stud ied a new sec tion avail able due to theprog ress of the ex ploi ta tion in the quarry. The sec tion is lo -cated in the south-cen tral part of the Kudryntsi quarry(N48°37.185’, E26°19.261’). It in cludes the up per part (2.2m thick) of the siliciclastic unit (the Tyras Suite), the lime -stone unit (1.3–1.4 m thick; the Ratyn Lime stone) and the3.7-m-thick se ries of rhodoid lime stones with in ter ca la tionsof marls and claystones (the Kosiv Suite; Fig. 2). Nine teensam ples col lected from the sec tion have been an a lysed fordinoflagellate cysts and palynofacies as well as foramini-fers, ex cept of sam ple O from which foraminifers have notbeen stud ied; the lo ca tion of sam ples is shown in Fig ure 2.

The stud ied sam ples rep re sent var i ous lithologies. Sam -ples from the lower part of the sec tion (sam ples A, B, D, E)are pale-col oured (whit ish-creamy), fre quently banded,poorly cal car e ous light marly claystone. Sam ple C, col -lected from the same com plex, is grey-green ish, non-cal car -e ous sandy mudstone. Sam ple F, col lected from organode-trital lime stone com plex, is hard pale-beige mas sive marlbe ing more cal car e ous than un der ly ing strata. Sam ple Grep re sents very hard pelitic creamy lime stone (highly cal -car e ous). Sam ple H is very poorly cal car e ous soft dark-brown banded clay with rare fish re mains. Two sam ples col -lected from con glom er atic slump layer rep re sent whitechalky lime stone (sam ple I) and dark-brown ish hard lime -stone (sam ple J). Sam ple K (top of the organodetrital lime -stone) is dark-beige mas sive and hard lime stone with rho-doids.

Sam ples L–S col lected from the rhodoid lime stonecom plex rep re sent two va ri et ies. Sam ples M and O are

whit ish-creamy hard organodetrital lime stone, whereas there main ing sam ples con sist of rhodoids with var i ous amountof cal car e ous ma trix. Sam ples N, Q and R are purely rho-doid, whit ish-grey hard lime stone, while sam ples L, P and S con tain ad mix ture of grey ish-green (L, P) and wil low-green clay (S).

The sam ples for palynology were pro cessed in theMicropalaeontological Lab o ra tory of the In sti tute of Geolo- gical Sci ences, Pol ish Acad emy of Sci ences, Kraków. Stan-dard palynological pro ce dure was ap plied, in clud ing 38%hy dro chlo ric acid (HCl) treat ment, 40% hy dro flu oric acid(HF) treat ment, heavy liq uid (ZnCl2+HCl; den sity 2.0 g/cm3)sep a ra tion, ul tra sound for 10–15 s and siev ing at 15 µm on a ny lon mesh. No ni tric acid (HNO3) treat ment was ap plied.The quan tity of rock pro cessed was ap prox i mately 40 g foreach sam ple ex cept of sam ple 4, whose quan tity was 10 g.Mi cro scope slides were made from each sam ple us ing gly-cerine jelly as a mount ing me dium. The rock sam ples, paly-nological res i dues and slides are stored in the col lec tion ofthe In sti tute of Geo log i cal Sci ences, Pol ish Acad emy ofSciences, Kraków.

Low fre quency of dinoflagellate cysts made that al mostall re sid uum was used for slides, which have been scanned.Palynofacies were based on count ing up to 1,000 el e ments.

Sam ples for foraminiferal study were pro cessed in thelab o ra tory of the In sti tute of Palaeobiology, Pol ish Acad -emy of Sci ences, Warszawa. Washed res i dues were obtai-ned by disaggregation of sam ples us ing Na2SO4. An aliquot of about 200–300 spec i mens from the >100 µm size frac tion was used for the fau nal anal y ses. The fig ured spec i mens arede pos ited in the In sti tute of Paleobiology, Pol ish Acad emyof Sci ences, Warszawa (ZPAL F. 70). The palaeoenviron-men tal in ter pre ta tion based on foraminifers ap plies the re -quire ments of pres ent-day rep re sen ta tives of re corded taxa.

RE SULTS

Palynofacies and dinoflagellate cysts

All sam ples yielded palynological or ganic mat ter,which, how ever, dif fer in quan tity and qual ity (Figs 3, 4).The palynofacies are shown in Fig ure 5 and the rep re sen ta -tive dinoflagellate cysts are shown in Fig ures 6 and 7.Siliciclastic (basal) part of the Kudryntsi sec tion (sam plesA–E) con tains very low amounts rep re sented al most ex clu -sively by black, opaque phytoclasts (95%), and highly de -graded black and dark-brown, fre quently elon gated woodpar ti cles. There are al most no palynomorphs ex cept of in -fre quent sporomorphs and some pale-col oured subspherical forms of un cer tain or i gin (pos si bly Re cent con tam i na tion).Qual i ta tive dif fer ences re fer to shape of black woody par ti -cles, which par tic u larly in sam ples A and B are elon gated,be ing strongly dis in te grated in sam ple D.

Sam ples col lected from organodetrital lime stone ex -posed above (G and F) con tain only trace amounts of paly-nological or ganic mat ter (small-sized black phytoclasts andsin gle subspherical forms). A dif fer ent palynofacies oc cursin sam ple H taken from dark-brown clays: it con sists ofhighly dis in te grated small-sized par ti cles of structurelessor ganic mat ter; no palynomorphs have been found ex cept of

EN VI RON MEN TAL CHANGES DUR ING LATE BADENIAN TRANS GRES SION, UKRAINE 333

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a sin gle spec i men of pale-col oured dinoflagellate cyst Sys-tematophora placacantha.

Two sam ples from the con glom er atic slump layer yiel-ded dif fer ent palynofacies. Sam ple I con tains high amountsof very well pre served Late Cre ta ceous dinoflagellate cysts(ex cluded from fur ther stud ies in this pa per), and sam ple Jcon tains trace amounts of palynological or ganic mat ter(highly dis in te grated small-sized black phytoclasts).

Sam ple K from the top most layer of the organodetritallimestone com plex is the first sam ple, which con tains dino-flag el late cysts. It gen er ally con tains low amounts of paly-nological or ganic mat ter, which con sists chiefly of small-sized black phytoclasts (70%), and pale-col oured phyto-

clasts palynodebris (30%). Dinoflagellate cysts are very rare;these are Systematophora placacantha, Spiniferites ramosuss. l., Polysphaeridium subtile and Lingulodinium machaero-phorum, and a sin gle spec i men of Pyxidiniopsis? sp.

A char ac ter is tic fea ture of the rhodoid com plex is oc -cur rence of dinoflagellate cysts (ex cept of the up per mostsam ple S), which are ab sent or very rare in un der ly ing strata of the stud ied sec tion. Their ra tios range there from a few tosev eral tens per cent. Palynofacies of sam ples from the rho-doid lime stone com plex shows re la tion to li thol ogy: sam -ples col lected from organodetrital lay ers (M, O) con tain amuch higher amount of palynological or ganic mat ter thanother sam ples from rhodoid lay ers. More over, the for mer

334 P. GEDL & D. PERYT

Fig. 2. Li thol ogy and lithostratigraphy of the stud ied sec tion and sam ple po si tion; A – pho to graph of the up per part of the sec tion; B –pho to graph of the lower part of the sec tion

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EN VI RON MEN TAL CHANGES DUR ING LATE BADENIAN TRANS GRES SION, UKRAINE 335

Fig. 3. Dis tri bu tion of dinoflagellate cysts in Kudryntsi sec tion. Ab bre vi a tions: d.c. – dark clay; o.l. – organodetrital layer

Fig. 4. Palynofacies changes in Kudryntsi sec tion (Sam ple I with Cre ta ceous dinoflagellate cysts is ex cluded here). Ab bre vi a tions: d.c.– dark clay; o.l. – organodetrital layer

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336 P. GEDL & D. PERYT

Fig. 5. Palynofacies of Badenian de pos its from Kudryntsi (scale bar in F rep re sents 0.5 mm and re fers to all other pho to mi cro graphs):A – sam ple B (black and dark-brown elon gated wood par ti cles); B – sam ple H (palynofacies con sists of highly dis in te grated par ti cles ofstructureless or ganic mat ter); C – sam ple M (palynofacies with com mon bisaccate pol len grains and dinoflagellate cysts); D – sam ple N(palynofacies with high ra tio of dinoflagellate cysts); E – sam ple Q (palynofacies dom i nated by small-sized black palynodebris; largepalynomorphs of un cer tain or i gin [zooclasts?] oc cur); F – sam ple R (palynofacies com posed of equidimensional black phytoclasts)

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EN VI RON MEN TAL CHANGES DUR ING LATE BADENIAN TRANS GRES SION, UKRAINE 337

Fig. 6. Dinoflagellate cysts from Badenian se quence at Kudryntsi: A–D – Lingulodinium machaerophorum (A, B: spec i mens withscabrate cyst wall and long pro cesses, sam ple L; C: spec i men with rel a tively smooth cyst wall and 2P archaeopyle, sam ple R; D: spec i men with thick and scabrate cyst wall and rel a tively short pro cesses, sam ple R; E: spec i men with 5P archaeopyle, sam ple L); F–H –Pentadinium sp. (F: sam ple L; G, H: sam ple P); I – Systematophora placacantha (sam ple L); J, K – Spiniferites pseudofurcatus (J: sam ple O; K: sam ple N); L–N – Systematophora placacantha (L, M: sam ple N; N: sam ple L)

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con tain high ra tios of sporomorphs (mainly bisaccate pol len grains) and dinoflagellate cysts. The lat ter yielded mainlyblack phytoclasts (par tic u larly dom i nat ing in sam ples fromup per part of rhodoid com plex: Q and R), ex cept of sam pleN, which con tain high ra tio of dinoflagellate cysts.

The basal sam ple from the rhodoid com plex (L) con -tains low amounts of palynological or ganic mat ter dom i -

nated by small-sized black phytoclasts (70%). Pale-colou-red plant tis sue re mains, sporomorphs and palynomorphs of un cer tain tax o nom i cal po si tion (pre sum ably al gae) are sub -or di nate. Dinoflagellate cyst as sem blage (8%) is tax o nom i -cally im pov er ished; it con sists of four dom i nat ing taxa: Sys- tematophora placacantha, Pentadinium sp., Polysphaeri-dium subtile and Lingulodinium machaerophorum, and sin -

338 P. GEDL & D. PERYT

Fig. 7. Dinoflagellate cysts from Badenian se quence at Kudryntsi: A, B –Hystrichokolpoma rigaudiae (both spec i mens from sam pleP); C – Impagidinium sp. (sam ple P); D – Pyxidiniopsis sp. (sam ple K); E – Operculodinium sp. (sam ple M); F–I – Polysphaeridiumsubtile (all spec i mens sam ple R); J – Dapsilidinium pseudocolligerum (sam ple L); K, L – Spiniferites sp. (K: sam ple N, L: sam ple M); M– Systematophora placacantha (sam ple H); N – Impagidinium sp. (sam ple M); O – Systematophora placacantha (two spec i mens fromsam ple N); P, Q – Operculodinium sp. (both spec i mens from sam ple N)

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gle specimens of Spiniferites sp. and Dapsilidinium pseudo- colligerum.

A higher sam ple M (organodetrital lime stone layer) iscom posed of dom i nat ing sporomorphs (mainly bisaccatepol len grains – up to 60%) and aquatic palynomorphs rep re -sent ing dinoflagellate cysts (up to 20%), acritarchs and al -gae. The dinoflagellate cyst as sem blage is dom i nated by thege nus Spiniferites (app. 70%), rel a tively com mon are spec i -mens of Operculodinium spp., Systematophora placa-cantha and Lingulodinium machaerophorum. Rare Nema-tosphaeropsis labyrinthea, Impagidinium sp., and Pentadi-nium sp. oc cur. Note wor thy is pres er va tion of dinoflagellate cysts, which fre quently are wrin kled or torn-off.

Palynofacies of sam ple N is dis tin guished by very highra tio of dinoflagellate cysts – up to 60%. Their as sem blageis tax o nom i cally sim i lar to the one from sam ple B, but dif -fers qual i ta tively. It con sists of fre quent spec i mens of Syste- matophora placacantha, Operculodinium spp., Lingulodi-nium machaerophorum and Spiniferites spp. (the lat ter ge -nus is much less fre quent than in sam ple M). Nematosphae-ropsis labyrinthea, Achomosphaera spp. and Pentadiniumsp. are rep re sented by rare spec i mens.

Sam ple O yielded sim i lar palynofacies as sam ple M, an -other sam ple rep re sent ing organodetrital layer, dom i nated bypol len grains (up to 60%). Dinoflagellate cysts (20%) fromthis sam ple are also tax o nom i cally im pov er ished: their as-semblage is dom i nated by the ge nus Opercu- lodinium, and,to a lesser de gree, Systematophora placacantha and Lingulo- dinium machaerophorum. Rep re sen ta tives of the ge nus Spi-niferites are sub or di nate, sim i larly as Pyxidiniopsis? sp.

Palynofacies of sam ple P con tain ing low amount of paly- nological or ganic mat ter con sists of black phytoclasts (up to50%) and sporomorphs (30%; be side bisaccate grains, ge nusIntratriporopollenites is com mon). Dinoflagellate cysts arerel a tively com mon (app. 15%); their as sem blage con sistsmainly of Systematophora placacantha, Lingulodinium ma-chaerophorum and Spiniferites spp. An out stand ing fea ture is low ra tio of Operculodinium (fre quent in un der ly ing sam -ples) and nu mer ous oc cur rence of Hystrichokolpoma rigau-diae, which is ab sent in lower sam ples of the stud ied sec tion.Pentadinium sp., Polysphaeridium subtile and Polysphaeri-dium zoharyi are in fre quent. A sin gle spec i men of Impagi-dinium sp. has been found. Some palynomorphs of un cer tainor i gin, pos si bly al gae, have been found in this sam ple.

The two fol low ing sam ples Q and R con tain lowamounts of palynological or ganic mat ter. Their palynofa-cies is dom i nated by small-sized black phytoclasts (up to90%). Ad di tion ally, small-sized plant tis sue re mains, sporo- morphs (fre quent spores) and dinoflagellate cysts oc cur.The lat ter are rel a tively rare (a few per cent): their assembla- ges in both sam ples con sist of dom i nat ing Systematophoraplacacantha and Lingulodinium machaerophorum; fur ther -more, Spiniferites spp., Pentadinium sp., Polysphaeridiumsubtile, P. zoharyi are also pres ent. In fre quent small acri-tarchs oc cur in sam ple Q. As sem blage from sam ple R ischar ac ter ized by lack of Spiniferites ramosus. Both sam plescon tain no Operculodinium.

The topmost sam ple S, as the only one from the rhodoid com plex, con tains no dinoflagellate cysts. Its low amount of palynological or ganic mat ter con sists of small-sized black

phytoclasts, and pale-col oured plant tis sue re mains andfungi (the two lat ter groups, sim i larly as sin gle sporomor-phs, are pos si bly re cent contamination).

Foraminifers

The abun dance fluc tu a tions of foraminifers ares shownin Fig ure 8 and se lected spe cies are shown in Fig ures 9 and10. Sam ples from the siliciclastic unit yielded very rare andpoorly pre served foraminifers. Tax o nomic com po si tion and their state of pres er va tion sug gest that they were prob a blyre worked and re de pos ited (Peryt & Peryt, 2009). One sam -ple (sam ple A) yielded a quite rich as sem blage of Badenianforaminifers: sin gle spec i mens of Heterolepa dutemplei,Eponides repandus, molds of Quinqueloculina spp. and Tri- loculina spp. and other strongly dam aged tests. In ad di tion,the fol low ing taxa oc cur: keeled elphidiids (Elphidium fich-telianum, E. joukovi, E. macellum), Porosononion spp.,Astrononion perfossum, Lobatula lobatula, Cibicidoidespseudoungerianus, C. ungerianus, Semivulvulina sp., Buli-mina aculeate, Rosalina sp., Siphotextularia sp., Neoepo-nides sp. and rare spec i mens of plank tonic Globigerina bul-loides. Most of tests show very dis tinct ev i dences of redepo- sition; some of them, however, are well preserved.

The low est oc cur rence of in situ ben thic foraminifers isre corded in sam ple E (Fig. 8). Seven foraminiferal as sem -blages (I–VII) have been rec og nised in the in ter val com pris -ing samples E–S.

As sem blage I oc curs in a clayey-sandy bed un der ly ingthe Ratyn Lime stone (sam ple E; Fig. 8). This low di ver sityas sem blage is char ac ter ized by dom i nance of elphidiids(more than 60%) rep re sented mainly by Elphidium koberiand ?Elphidium sp. An other im por tant com po nent is Neo-conorbina sp., which ex ceeds 20%. Rare spec i mens of El-phidium aculeatum, Quinqueloculina sp. and Astrononionperfossum also occur.

As sem blage II is re corded in organodetrital lime stone(sam ples F, G, J). This as sem blage is dom i nated by thick-walled, large spec i mens of Elphidium crispum and E. mace- llum con trib ut ing 60–80% to the as sem blage (Fig. 8). Mi nor com po nents in these as sem blage are miliolids and Poro-sononion spp.

As sem blage III oc curs in dark-brown clays (sam ple H)and in top most layer of the organodetrital lime stone com -plex (sam ple K; Fig. 8). This as sem blage dif fers sig nif i -cantly from as sem blage II from organodetrital lime stones.Elphidium crispum is not pres ent in this as sem blage. In -stead, spiny elphidiids: E. aculeatum and E. koberi are dom -i nant taxa. They form to 50% of the as sem blage. Miliolidsare also im por tant con tri bu tors. Their ra tio ex ceeds 40%:Triloculina spp. (25%), Quinqueloculina spp. (9%), Pyrgospp. (4%) and Articulina sp. (3%). Rare large spec i mens ofE. reginum are also re corded. Rosalina is com mon in thisas sem blage too. The tests show slightly dam aged or na men -ta tion possibly caused by bottom currents.

As sem blage IV oc curs in basal sam ples from the rho-doid com plex (L and M). The as sem blage is dom i nated bymiliolids (60–70%); com mon are Porosononion spp.,Guttulina spp. and Glandulina spp. in sam ple L, and Elphi-dium crispum and E. macellum in sam ple M (Fig. 8).

EN VI RON MEN TAL CHANGES DUR ING LATE BADENIAN TRANS GRES SION, UKRAINE 339

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340 P. GEDL & D. PERYT

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EN VI RON MEN TAL CHANGES DUR ING LATE BADENIAN TRANS GRES SION, UKRAINE 341

Fig. 9. Foraminifers from Badenian se quence at Kudryntsi (scale bars = 200 µm): A – Elphidium fichtelianum (d’Orbigny) (sam ple S);B – Elphidium rugosum (d’Orbigny) (sam ple J); C – Elphidium crispum (Linné) (sam ple J); D – Elphidium joukovi Serova (sam ple N); E– Elphidium fichtelianum (d’Orbigny) (sam ple P); F – Elphidium aculeatum (d’Orbigny) (sam ple K); G – Reussella pulchra Cushman(sam ple L); H – Elphidium reginum (d’Orbigny) (sam ple K); I–K – Elphidium aculeatum (d’Orbigny) (sam ple K); L – Virgulinopsis sp.(sam ple L); M – Globulina spinosa d’Orbigny (sam ple L); N – ?Elphidium sp. (sam ple H); O, P – Elphidium koberi Tollmann (sam ple H); Q – Elphidium macellum (Fichtel & Moll) (sam ple S); R – Elphidium crispum (Linné) (sam ple J); S – Schackoinella imperatoria(d’Orbigny) (sam ple K)

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342 P. GEDL & D. PERYT

Fig. 10. Foraminifers from Badenian se quence at Kudryntsi (scale bars = 200 µm): A – Rosalina obtusa d’Orbigny (sam ple L); B, C –Astrononion perfossum (Clodius) (sam ple L); D – Porosononion martkobi (Bogdanowicz) (sam ple L); E – Lobatula lobatula (Walker &Ja cob) (sam ple S); F – Lobatula lobatula (Walker & Ja cob) (sam ple N); G – Cibicidoides pseudoungerianus (Cushman) (sam ple S); H –Neoconorbina sp. (sam ple S); I – Siphotextularia concava (Karrer) (sam ple S); J – Pseudotriloculina consobrina (d’Orbigny) (sam ple L);K, M, N – Triloculina gibba d’Orbigny (sam ple K); L – Triloculina sp. (sam ple K); O – Glandulina sp. (sam ple L); P – Guttulinacommunis (d’Orbigny) (sam ple L); Q – Guttulina gibba (d’Orbigny) (sam ple L); R – Quinqueloculina buchiana d’Orbigny (sam ple K); S– Quinqueloculina sp. (sam ple K)

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As sem blage V has been dis tin guished in sam ple N from the rhodoid com plex. This al most monospecific as sem blage is in 70% com posed of Lobatula lobatula. Mi nor com po -nents are keeled elphidiids and miliolids (Fig. 8).

As sem blage VI oc curs in sam ples P and Q of the rho-doid com plex. In this as sem blage, Neoconorbina spp. (35–40%) and Astrononion perfossum (18–22%) dom i nate. Ro-sa lina spp. (11–14%), Porosononion spp. (11%) and Loba-tula lobatula (8–10%) are also com mon. Elphidium is veryrare in this as sem blage (Fig. 8). The large tests are of tendam aged and their sur faces are smoothed due to cur rentactivity.

As sem blage VII has been found in the top most part ofthe rhodoid com plex (sam ples R and S). This as sem blage ischar ac ter ized by the high est di ver sity, and by the com monpres ence of Cibicidoides spp., which is ab sent in other as -sem blages; Neoconorbina is much less abun dant (10%)than in as sem blage VI; Elphidium spp., Baggina sp., Rosa-lina spp., Astrononion perfossum are also common (Fig. 8).

IN TER PRE TA TION AND DIS CUS SION

A car bon ate plat form ex isted in west ern Ukraine (sim i -larly as in a few places within the Cen tral Paratethys) af terthe be gin ning of Late Badenian de po si tion char ac ter ized bytrans gres sion and for ma tion of a nor mal ma rine en vi ron -ment (Schmid et al., 2001; Vrsaljko et al., 2006). Qual i ta -tively and quan ti ta tively di ver si fied palynological and fora-miniferal con tents of the Badenian strata ex posed in the Ku- dryntsi sec tion lo cated near the sea ward mar gin of that plat -form in di cate vari able en vi ron men tal con di tions. In ter pre ta -tion of these changes are sup ported by en vi ron men tal pref -er ences of par tic u lar gen era of foraminifers, which oc cur invari able ra tios within the Kudryntsi sec tion.

Foraminiferal palaeoenvironmental pref er ences

Elphidiids are very com mon com po nent of foramini-fe ral as sem blages re corded in the Kudryntsi sec tion. Sa lin -ity and wa ter depth are im por tant eco log i cal fac tors thatcon trol abun dance of this group. Par tic u lar Elphidium spe -cies show also re la tion to wa ter depth and the de gree of ex -po sure to high wave and cur rent en ergy (Langer, 1993;Hayward et al., 1997). Keeled morphotypes, which are pre-sent in the de scribed as sem blages, are mostly her biv o rous,epifaunal dwell ers pre fer ring sandy sed i ment, oc cur ring inshal low ma rine en vi ron ments (in ner shelf) with warm totem per ate and nor mal to hypersaline (35–70‰) wa ters(Hay ward et al., 1997; Murray, 2006). Quinqueloculina isan epifaunal dweller, liv ing free or cling ing on plants orsed i ment, pre fer ring shal low nor mal ma rine to hypersaline(32–65‰) en vi ron ments. Sim i lar ecologic re quire mentspos sesses Triloculina, com monly oc cur ring in com bi na tionwith Elphidium and Quinqueloculina (Murray, 1991, 2006). The Quinqueloculina spp. as so ci a tion oc curs in re cent Med -i ter ra nean Sea in shal low en vi ron ments (2–65 m), tem per -ate to warm wa ters (10–25°C) and slightly el e vated sa lin ity(37–39‰). Lobatula lobatula is an epifaunal dweller, usu -ally at tached and im mo bile, es pe cially in high en ergy; pre -

fer ring tem per ate – warm shal low nor mal ma rine en vi ron -ments (Murray, 1991, 2006). Rosalina and Neoconorbinaare epifaunal dwell ers, pre fer ring tem per ate – warm shal -low nor mal ma rine en vi ron ments (Murray, 1991, 2006). Ci- bicidoides and Astrononion are an epifaunal dwell ers, pre -fer ring cold nor mal ma rine en vi ron ments (shelf – bathyal;Murray, 1991, 2006).

Palaeoenvironment re con struc tion

The siliciclastic part of the ex po sure (sam ples A–E;Fig. 2) con tains very low amounts of palynological or ganicmat ter. It con sists al most ex clu sively of var i ously pre served black phytoclasts (Fig. 4A); there are no dinoflagellatecysts. Such palynofacies may re flect ei ther re stricted en vi -ron ment, un fa vour able for aquatic phytoplankton (e.g.dinoflagellates), or spe cific sed i men tary set ting crit i cal forpres er va tion of palynomorphs. A rare oc cur rence of sporo-morphs seems to opt for the first pos si bil ity. These stratawere pre sum ably de pos ited in very shal low en vi ron ments,char ac ter ized by high hy dro dy namic con di tions. Ac cord ingto Bat ten (1996, p. 1033 and ref er ences therein), a high ra tio of black phytoclasts is as so ci ated with prox i mal, high en -ergy en vi ron ments (it also oc cur in deep sea fa cies, butthese can be ex cluded in case of Kudryntsi de pos its).

The pres ence of foraminifers in the siliciclastic unit ca.2 m be low the un doubt edly ma rine de pos its lime stone isenig matic. One pos si ble ex pla na tion is that the siliciclasticunit re lated so far with the fi nal stage of evaporite de po si -tion in the Carpathian Foredeep Ba sin (Peryt & Peryt,2009), should be rather as so ci ated with the Late Badeniantrans gres sion. How ever, other sam ples from this unit arebar ren (ex cept for the re de pos ited Cre ta ceous forms). Theal ter na tive ex pla na tion is that dur ing ter mi nal stages of eva-poritic ba sin, the de po si tion of the siliciclastic unit tookplace in a la goon, which was pe ri od i cally flooded by short-lived ma rine in gres sions. Sim i lar sit u a tion has been de -scribed from the Up per Mio cene evaporites of the East ernBetics, SE Spain, where scarce and poorly pre servedforaminifera are re corded in var i ous gyp sum units (Play´ etal., 2000, ta ble 2); plank tonic foraminifera are scarce, smalland usu ally poorly pre served, and the ben thic foraminiferaseem to have adapted to a wide range of sa lin ity (Play´ etal., 2000, ta ble 2). The com po si tion of foraminifers in sam -ple A strongly ar gues for redeposition from older Badenianstrata. The Kudryntsi sec tion is lo cated very close to theorig i nal limit of the Badenian gyp sum ba sin (Peryt et al.,2004; Peryt & Peryt, 2009), and to wards the east the Up perBadenian rests upon the Lower Badenian strata (Siplivyy etal., 1974).

A monospecific as sem blage I with Elphidium koberifrom the clayey marly bed from the top most part of thesiliciclastic unit (sam ple E) in di cates a very re stricted ma -rine en vi ron ment; prob a bly with el e vated salinity.

Shal low wa ter en vi ron ments (0–20 m deep) of nor malma rine to slightly el e vated sa lin ity, and char ac ter ized byhigh hy dro dy namic con di tions, are sug gested for de po si tion of organodetrital car bon ates char ac ter ized by foraminiferalas sem blage II with Elphidium crispum and E. macellum(samples F, G, J).

EN VI RON MEN TAL CHANGES DUR ING LATE BADENIAN TRANS GRES SION, UKRAINE 343

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The oc cur rence of dark-brown clay with fish re mains(sam ple H) may in di cate a pe riod of a calm, stag nant en vi -ron ment – palynofacies of this sam ple con sists ex clu sivelyof structureless or ganic mat ter, which is typ i cal for the bac -te rial de cay of or ganic mat ter in the ox y gen de pleted, es pe -cially anoxic en vi ron ments (Bat ten, 1996). Foraminiferalas sem blage III with dom i nant elphidiids with spines, i.e.Elphidium aculeatum and E. koberi and com mon miliolids,char ac ter izes shal low-ma rine en vi ron ment with low hy dro -dy namic con di tions and slightly in creased sa lin ity.

Oc cur rence of dinoflagellate cysts in the top most partof the organodetrital lime stone com plex (sam ple K) and inthe over ly ing rhodoid lime stone in di cates a change of en vi -ron ment that might be re lated to the ap pear ance of ma rinecon di tions fa vour able for motile stages of dinoflagellates,or it may re flect a change of sed i men tary set ting re spon si ble for the pres er va tion of ter res trial and aquatic palynomorphs. A high ra tio of sporomorphs and cu ti cles points at a ter res -trial in flux into the ma rine ba sin. The in flux in ten sity wasrather lim ited, since dinoflagellate cysts are a sig nif i cantcomponent of palynofacies, be ing in dic a tive for hemipe-lagic mode of sed i men ta tion. Such a change may be re latedto a grad ual wid en ing of the ba sin, pos si bly as so ci ated withdeep en ing, and the ap pear ance of more off shore, less dyna-mic, quiet bot tom en vi ron ment, which led to ac cu mu la tionand pres er va tion of both ter res trial and ma rine palyno-morphs. Dinoflagellate cyst as sem blages are rather taxono-mically not di ver si fied. They con sist ex clu sively of gonyau- lacoids, which in ma jor ity are rep re sented by chorate andproximochorate spec i mens. The lack of peridinioids mightbe re lated ei ther to pri mary con di tions not suit able for thisgroup of dinoflagellates (e.g. low nu tri ent con di tions of thesur face wa ter) but also un fa vour able syn- and post depo-sitional con di tions re lated to aer o bic con di tions at the bot -tom and in the sed i ment, which are par tic u larly hos tage fortheir pres er va tion (see e.g., Zonneveld et al., 1997).

A gen eral com po si tion of dinoflagellate cyst as sem -blages sug gests ma rine en vi ron ment dur ing de po si tion ofthe rhodoid com plex. The majority of spe cies are typ i cal for shelf en vi ron ment. Some of them, like Polysphaeridium zo-haryi and P. subtile, are char ac ter is tic for in ner shelf or la -goonal en vi ron ments, be ing tol er ant to in creased sa lin ity.How ever, these spe cies never oc cur as dom i nant in the stud -ied ma te rial. On the other hand, rare spec i mens of taxa typ i -cal for off shore, oligotrophic wa ters have been found insam ples M and N (sin gle spec i men of Impagidinium oc cursalso in sam ple P). Their pres ence may in di cate ei ther in flu -ences of off shore wa ters, lim ited nu tri ent avail abil ity innear-shore surface waters, or deepening of the basin.

Foraminiferal as sem blages from the rhodoid com plex(IV–VII) also sup port ma rine en vi ron ments of their orig i na -tion.

A dif fer ent com po si tion of dinoflagellate cyst as sem -blages in par tic u lar sam ples re flects pre sum ably slightly di -verse en vi ron men tal con di tions. Sam ple L con tains Poly-sphaeridium zoharyi and P. subtile. Ac cord ing to sev eralau thors, these spe cies (es pe cially P. zoharyi) are typ i cal forlit to ral embayment in trop i cal to sub trop i cal set tings and are tol er ant for in creased sa lin ity (Wall & Dale, 1969; Dale,1976; Wall et al., 1977; Morzadec-Kerfourn, 1979, 1983;

Brad ford & Wall, 1984; Ed wards & Andrle, 1992). How -ever, Marret and Zonneveld (2003) re ported P. zoharyifrom low sa line en vi ron ments and suggested euryhalinenature of this species.

The as sem blage IV with Miliolidae (sam ples L and M)sup ports the in ter pre ta tion of el e vated sa lin ity dur ing thede po si tion of the low er most part of the rhodoid com plex, inshal low wa ter en vi ron ment. The next, monospecific as sem -blage V with Lobatula lobatula (sam ple N) sug gests shal -low-ma rine, very high-en ergy en vi ron ment. Dinoflagellatecyst as sem blages from sam ples M–O con tain no Poly-sphaeridium zoharyi: this change might be in ter preted astran si tion from higher sa line re gime dur ing de po si tion ofthe basal part of the rhodoid com plex, into nor mal ma rineen vi ron ment in its higher part. The oc cur rence of some off -shore taxa (Nematosphaeropsis labyrinthus and spe cies ofImpagidinium) in the mid dle part of the rhodoid com plex(sam ples M and N) co in cides with the high est ra tio of dino-flag el late cysts (up to 60% in sam ple N). Both N. laby-rinthus and Impagidinium are treated by sev eral au thors as“oce anic” spe cies, which motile stages in hab ited off shorewa ters (e.g., Morzadec-Kerfourn, 1977; Wall et al., 1977;Harland, 1983; Brinkhuis, 1994). The other com mon spe ciesin the mid dle part of the rhodoid com plex – Operculodi-nium sp. (mainly O. centrocarpum) and Lingulodinium ma-chaerophorum are cos mo pol i tan spe cies (e.g., Marret & Zon- neveld, 2003). Lingulodinium machaerophorum is a euryha-line spe cies, which may pos sess shorter pro cesses in lowersa line con di tions (e.g., Wall & Dale, 1973; Dale, 1996; Elle-gaard, 2000): in our ma te rial spec i mens of L. machaero-phorum have rather long pro cesses, which may sug gest nor -mal sa lin ity. Operculodinium centrocarpum, which is a veryfre quent spe cies in sam ples M–O, is re garded a cos mo pol i tan spe cies, which motile stage can flour ish in a wide range ofen vi ron ments. Also in case of this spe cies a pro cess length re -duc tion re lated to lower sa lin ity was sug gested (de Ver nal etal., 1989; Ellegaard, 2000), but in Kudryntsi ma te rial spe cieswith “nor mal” pro cesses pre dom i nate.

Sam ples P–R from the higher part of the rhodoid com -plex con tain dinoflagellate cyst as sem blages, which aredom i nated by cos mo pol i tan spe cies Systematophora placa-cantha and Lingulodinium machaerophorum. Qual i ta tivefluc tu a tion of tax o nom i cal com po si tion may be re lated towa ter depth: as sem blages with com mon or dom i nat ingOperculodinium (sam ples M–O) may re flect slightly deeper (off shore) en vi ron ment than the ones in hab ited by motilestages of Lingulodinium machaerophorum and Systemato-phora placacantha (sam ples P–R). Pos si bly sim i lar changes were de scribed by Morzadec-Kerfourn (1983) who de -scribed Lingulodinium machaerophorum As so ci a tion fromthe in ner coastal zone with wa ter depth of 10–30 m, andOperculodinium centrocarpum-O. israelianum As so ci a tion from the deeper outer coastal zone (30–50 m wa ter depth).More prox i mal en vi ron ment for sam ples P–R may be sup -ported by the oc cur rence of Polysphaeridium in these sam -ples, and the ab sence of this ge nus in sam ples sug gests more off shore en vi ron ment for sam ples M–O with com monOperculodinium. How ever, com mon oc cur rence of Hystri-chokolpoma rigaudiae in sam ple P may also in di cate off -shore con di tions since this ge nus, al though com monly be -

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lieved to be cos mo pol i tan (e.g., Brinkhuis, 1994) is re latedby some au thors as an off shore one (e.g., Rassmussen et al.,2003). On the other hand, it can not be ex cluded that ap pear -ance of H. rigaudiae in our ma te rial is as so ci ated with otheren vi ron men tal changes like wa ter tem per a ture.

The foraminiferal as sem blages VI and VII oc cur ring inthat part of the sec tion char ac ter ize the high est di ver sity and taxa pre fer ring tem per ate-warm to cold shelf to bathyal nor -mal ma rine en vi ron ments. The as sem blage VI, com posed of taxa pre fer ring tem per ate – warm shal low nor mal ma rineen vi ron ments (Lobatula, Neoconorbina, Rosalina, Poroso-nonion, Astrononion), con firms sug ges tions of low er ing ofsa lin ity to nor mal ma rine in the mid dle part of the rodoidcom plex. The as sem blage VII with Cibicidoides and Lo-batula, Neoconorbina, Rosalina, Baggina, Porosononion,Elphidium and Astrononion sug gests tem per ate to cold nor-mal marine shelf environment.

A NOTE ON ELPHIDIUM REGINUMOC CUR RENCE

We fo cused in this pa per on palaeoenvironmental as -pects of our micropalaeontological as sem blages from Kud-ryntsi. How ever, one biostratigraphical as pect, which is an -nounced here, de serves a sep a rate dis cus sion. It re fers to the oc cur rence of Elphidium reginum in the Up per Badeniansucces sion at Kudryntsi. This spe cies is re garded as the in -dex spe cies of the Lower Sarmatian biozone (Grill, 1941;£uczkowska, 1972; Czepiec, 1996; Harzhauser & Piller,2004a; Toth et al., 2010). In Podolia, Elphidium reginumoc curs in the Buglovian and Volhynian (Pishvanova, 1958;Krasheninnikov, 1960), but Krasheninnikov (1958, p. 296and 302; 1960, fig. 6) noted that it ap pears al ready in the up -per most Badenian (his ho ri zon G). Szczechura (1982) alsore ported sin gle spec i mens of this spe cies in the Badenianpro file of Józefów and Hamernia in Roztocze Hills (SE Po -land). Other typ i cally Sarmatian foraminifers ap pear ing inthe Anomalinoides dividens Zone (e.g., Czepiec, 1996) arelack ing and there fore we re late the ap pear ance of Elphidium reginum in the Up per Badenian of Kudryntsi to spe cific en -vi ron men tal con di tions which in that par tic u lar area havebeen very sim i lar to those in which the Sarmatian as sem -blages lived (cf. Szczechura, 1982). The same rea son ingmay be ap plied to Elphidium koberi, an other elphidiid spe -cies that so far was de scribed from the Sarmatian strata(Tollmann, 1955; Brestenska, 1974; Papp & Schmid, 1985;Cicha et al., 1998; Görür et al., 2000; Paruch-Kulczycka,2007; Schütz et al., 2007) and which oc curs in sam ples Eand H in the Kudryntsi sec tion. Harzhauser and Piller(2004b) re corded re worked corallinacean lime stone andabundant corallinacean frag ments in the Lower Sarmatiandeposits of the Vi enna Ba sin and in ter preted them as due toin tense re work ing of Badenian de pos its. In ad di tion, Harz-hauser (writ ten in for ma tion, 2011) has seen sev eral otheroutcrops in Aus tria and Hun gary in which the Badenian/Sarmatian bound ary is ex pressed as hi a tus, and the ear li estSarmatian de pos its are usu ally re worked Badenian coralli-nacean lime stone, which bear the en tire suite of Badeniantaxa, in clud ing molluscs (this kind of de pos its has an own

lithostratigraphic term in Aus trian ge ol ogy re ferred to as de -tri tal Leitha Lime stone). How ever, al though un doubt edlythere is some re work ing within the stud ied sec tion atKudryntsi, we do not see the con vinc ing ar gu ments in fa -vour of the mas sive re work ing of the Up per Badenian strataand the in cor po ra tion of re worked rhodoids and molluscsdi ag nos tic for the Badenian into the Sarmatian suc ces sion in the case of the Kudryntsi out crop.

SUM MARY

Di ver si fied palynological and foraminiferal as sem -blages re corded in strata ex posed in the Kudryntsi sec tionabove the gyp sum in di cate vari able en vi ron men tal con di -tions dur ing the Late Badenian trans gres sion. Anal y sis ofchanges of mi crofossil as sem blages sug gests re stricted en -vi ron ment dur ing be gin ning of the trans gres sion, and grad -ual pas sage into ma rine en vi ron ment dur ing later stages ofLate Badenian de po si tion (Fig. 11).

The basal part of the Up per Badenian suc ces sion (silici- clastic com plex) at Kudryntsi is bar ren – this points athighly re stricted en vi ron men tal con di tions not suit able nei -ther for dinoflag el late cysts (ab sent) nor foraminifera (rare – pre sum ably re worked). It was pre sum ably high-en ergyshal low en vi ron ment (palynofacies of this part of sec tioncon tains fre quent elon gated woody par ti cles), pos si bly as -so ci ated with hypersaline con di tions as in di cated by forami- nifera as sem blage from top most part of the siliciclastic unit(As sem blage I).

A shal low subtidal warm-tem per ate re stricted en vi ron -ment with in creased sa lin ity and chang ing hy dro dy namicin ten sity is sug gested for the top most siliciclastic unit andthe organodetrital lime stone. The for mer yielded a mono-spe cific foraminiferal as sem blage I with Elphidium koberi,whereas the organodetrital lime stone con tains foraminiferalas sem blages II (with Elphidium crispum and E. macellum)and III (Elphidiids with spines, i.e. Elphidium aculeatumand E. koberi); the lat ter as sem blage char ac ter izes shal lowwa ter ma rine en vi ron ment with low hy dro dy namic con di -tions and slightly el e vated sa lin ity. The low er ing hy dro dy -namic con di tions that pe ri od i cally ap peared in Late Bade-nian sea dur ing de po si tion of organodetrital com plex gaverise to anoxic bot tom con di tions as pre sumed from palyno-fa cies (sam ple H). En vi ron men tal con di tions dur ing de po si -tion of the organodetrital lime stone were suf fi cient forforaminifera, but cru cial for dinoflagellates. The lat ter ap -peared for the first time in the top most part of the organode-trital com plex. Their ap pear ance is re lated with fur ther sa -lin ity de crease (al though in fre quent dinoflagellate cyst as -sem blage from the top most part of organodetrital lime stonecon tains rare spec i mens typ i cal for hypersaline en vi ron -ments) and grad ual remoting of the sed i men tary set ting ex -posed at Kudryntsi, which led to slightly deeper set ting,with nor mal ma rine sa lin ity and tem per ate-wa ter en vi ron -ment dur ing de po si tion of the rhodoid com plex. How ever,ap pear ance of dinoflagellate cysts may be re lated to sedi-mentological fac tors re flect ing in crease of wa ter depth andthe ap pear ance of less dy namic, quiet bot tom en vi ron ment,which led to ac cu mu la tion and pres er va tion of both ter res -

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trial and ma rine palynomorphs. The be gin ning of the de po -si tion of the rhodoid com plex was pre sum ably still un derslightly re stricted con di tions re lated to slightly in creasedwa ter sa lin ity (as sem blage IV in the basal part of the rho-doid com plex with Miliolidae – typ i cal for shal low wa teren vi ron ment with slightly in creased sa lin ity); in ter est ingly,this part of the sec tion yielded dinoflagellate cyst as sem -blage typ i cal for nor mal sa lin ity re gime. Sam ple M yieldeda dinoflagellate cyst as sem blage dom i nated by Spiniferites,and sin gle spec i mens of an off shore ge nus Impagidinium.This may in di cate var i ous sen si tiv ity of both microfossilgroups, or bot tom wa ters in hab ited by foraminifera werechar ac ter ized by in creased sa lin ity com pared to the sur facemarine waters.

The higher part of the rhodoid com plex was de pos itedin ma rine, more off shore, but still rather near-shore en vi ron -ment. Dinoflagellate cyst as sem blages from the rhodoidcom plex sug gest the tran si tion from slightly higher sa line

re gime char ac ter is tic for the de po si tion of its basal part(sam ple L – oc cur rence of Polysphaeridium subtile) andnor mal ma rine en vi ron ment in its higher part (sam ples M–R – tax o nom i cally rich and di ver si fied as sem blages). Themonospecific as sem blage V with Lobatula lobatula fromthe lower part of the rhodoid com plex (sam ple N) in di catesshal low-ma rine en vi ron ment with nor mal sa lin ity, but char -ac ter ized by very high-en ergy hy dro dy namic con di tions.Dinoflagellate cyst as sem blage from the same sam ple ischar ac ter ized by high fre quency and rel a tive di ver sity – this points at op ti mal liv ing con di tions re lated to shelf wa ters.The foraminiferal as sem blages VI and VII char ac ter ize thehigh est tax o nom i cal di ver sity; they in clude taxa pre fer ringtem per ate-warm to cold shelf to bathyal ma rine en vi ron -ments. As so ci ated dinoflagellate cysts from the same in ter -val (sam ples P–R) are gen er ally di ver si fied; a char ac ter is ticfea ture of their as sem blages is lack of Operculodinium,which com monly oc cur in un der ly ing strata. This change

346 P. GEDL & D. PERYT

Fig. 11. Con cep tual palaeoenvironmental changes in the Late Badenian ba sin at Kudryntsi based on in ter pre ta tion of dinoflagellate cystand foraminifera as sem blages

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may re flect some palaeoenvironmental vari a tion, pos si blyre lated to mi nor cool ing of ma rine wa ters as in duced fromforaminifera re cord (the as sem blage VI con sists of taxapreferring temperate-warm shallow marine environments,whereas the assemblage VII suggests temperate to coldmarine shelf environment).

The lat ter in ter pre ta tion of changes of foraminiferal as -sem blages is re lated to wa ter tem per a ture de cline. This mayre flect a slight cool ing dur ing the Late Badenian, but it maybe also linked to deep en ing of the ba sin and ap pear ance ofcolder bottom waters.

The foraminiferal as sem blages from Kudryntsi con tainElphidium reginum and Elphidium koberi com mon for theSarmatian; Elphidium reginum is re garded as the in dex spe -cies of the Lower Sarmatian biozone, al though it was ear lier re ported from the up per most Badenian. Other typ i callySarmatian foraminifers of the Anomalinoides dividens Zone are lack ing and the oc cur rence of Elphidium reginum andElphidium koberi in the Up per Badenian of Kudryntsi is re -lated to spe cific en vi ron men tal con di tions which were verysim i lar to those char ac ter is tic for the Sarmatian.

Ac knowl edge ments

We would like to thank Barbara S³odkowska for read ing themanu script and crit i cal re marks. Spe cial thanks are due to MathiasHarzhauser for his help ful com ments and in spir ing sug ges tions. The re search was un der taken as a re search pro ject No. UKRAINA/193/2006 of the Min is try of Sci ence and Higher Ed u ca tion car riedout at the AGH Uni ver sity of Sci ence and Tech nol ogy and the Pol -ish Geo log i cal In sti tute – Na tional Re search In sti tute and was fi -nanced from the sci en tific fund of 2007–2010. We thank ZofiaDubicka for the field as sis tance.

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