DINOFLAGELLATE CYST, PALYNOFACIES AND FORAMINIFERAL
RECORDS OF ENVIRONMENTAL CHANGES RELATED
TO THE LATE BADENIAN (MIDDLE MIOCENE) TRANSGRESSION
AT 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: ndgedl@cyf-kr.edu.pl
2
In sti tute of Paleobiology, Pol ish Acad emy of Sci ences, Twarda 51/55, 00-818 Warszawa, Po land, e-mail: d.peryt@twarda.pan.pl
Gedl, P. & Peryt, D., 2011. Dinoflagellate cyst, palynofacies and foraminiferal re cords of en vi ron men tal changes re lated to the Late Badenian (Mid dle Mio cene) trans gres sion at Kudryntsi (west ern Ukraine). Annales Societatis Geologorum 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 at Kudryntsi (west ern Ukraine) in di cate that this suc ces sion was de pos ited in vari able en vi ron ments. The basal siliciclastic se ries shows a very low con tent of palynological or ganic mat ter and palynofacies, which in di cate a re 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 the over 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 cyst as 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 slightly in 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 ments dur 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 of sa lin ity is sup ported also by the suc ces sion of foraminiferal as sem blages, which un dergo grad ual changes from Elphidium 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 tains two spe cies com mon for the Sarmatian, i.e. Elphidium reginum and Elphidium koberi, the lat ter spe cies known so far 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 in west ern Ukraine, the ev i dently ma rine de pos its (lime stones and in ter ca lated marls with abun dant fau nal as sem blage) form ing the basal part of the Up per Badenian transgressive se 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 cal study of these pelites showed that they formed in re stricted en vi ron ments (Peryt & Peryt, 2009).
The aim of the pa per is to com pare the dinoflagellate cyst and foraminiferal re cords ob tained from the same set of
sam ples col lected from the Up per Badenian transgressive
sec tion that is cur rently ex posed at Kudryntsi gyp sum
quarry.
Dinoflagellates are uni cel lu lar, mainly autotrophic, or -gan isms in hab it ing al most all aquatic eco sys tems, from fresh wa ter to ma rine and hypersaline. Dur ing their lifecy -cle they pro duce rest ing cysts, which in some spe cies are fossilizable. 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 low for 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
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 of the Carpathian Foredeep (Gedl, 1996).
How ever, dinoflagellate cysts are not the only or ganic fos 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, and tis 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. They were also used for palaeoenvironmental re con struc tions of the 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 and palaeoenvironment 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 cent ben 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 good
bioindicators of ma rine en vi ron ment changes (Murray,
2006), es pe cially that some Mio cene foraminiferal spe cies still live in re cent seas.
GEO LOG I CAL FRAME WORK
The Kudryntsi gyp sum quarry is lo cated on the left side of the Zbruch River Val ley in the fore land of the Carpathian Foredeep Ba sin (Fig. 1). The stromatolitic gyp sum (ca. 23 m thick) 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 lain by thin basal brec cia that rests upon the Cenomanian (Peryt & Peryt, 2009). A unit of 4mthick fine siliciclastic de pos its with in ter ca la tions of lime stones and finegrained sand -stones (up to 15 cm thick) oc curs above the gyp sum (the Tyras Suite; Peryt & Peryt, 2009). In the north ern part of the Kudryntsi quarry this unit is per va sively gypsified (Peryt et
al., 2008).
This siliciclastic unit is over lain by a lime stone unit (1.3–1.4 m thick) com posed of lithoclastic and fossiliferous
lime 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 per Badenian rhodoid lime stones with mi nor in ter ca la tions of marls and claystones (Proniatyn fa cies of Teisseyre, 1900;
cf. Siplivyy et al., 1974). Eastwards, this car bon ate fa cies is
char ac ter ized by oc cur rence of coralline al gae-vermetid
reefs and a va ri ety of bioclastic fa cies (Kudrin, 1966).
These strata in the neigh bour hood of Kudryntsi are more than 10 m thick when not eroded (Siplivyy et al., 1974); in the 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 placed by the clayey-sandy-car bon ate fa cies that, in turn, passes
332
P. GEDL & D. PERYTFig. 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-car bon ate fa cies, 3 – sandyclayey 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
into sandy-clayey fa cies (Fig. 1) – a typ i cal Kosiv Suite. The bound ary be tween the car bon ate and clayeysandycar -bon ate fa cies is lo cated some 1.5 km SW of the Kudryntsi quarry (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 they
lie 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 or clays, brec cias and con glom er ates, as well as serpulidmi -crobialite reefs (Kudrin, 1966; Siplivyy et al., 1974; Jasio-nowski et al., 2003; JasioJasio-nowski, 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 into south east ern Po land and west ern Ukraine from the Med i ter -ra nean (Andreyeva-Grigorovich et al., 1997; Oszczypko et
al., 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 rine clay bed, which oc curs be low the lime stone unit con sid ered to be the Ratyn Lime stone, orig i nated in shal low subtidal en vi ron ments of nor mal ma rine sa lin ity and tem per ate to
warm wa ters as in di cated by re quire ments of Elphidium
crispum 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 the prog 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 (2.2 m thick) of the siliciclastic unit (the Tyras Suite), the lime -stone unit (1.3–1.4 m thick; the Ratyn Lime -stone) and the 3.7-m-thick se ries of rhodoid lime stones with in ter ca la tions of marls and claystones (the Kosiv Suite; Fig. 2). Nine teen sam ples col lected from the sec tion have been an a lysed for dinoflagellate cysts and palynofacies as well as foramini-fers, ex cept of sam ple O from which foraminifers have not been 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 greygreen ish, noncal car -e ous sandy mudston-e. Sam pl-e F, col l-ect-ed from organod-e- organode-trital lime stone com plex, is hard pale-beige mas sive marl be ing more cal car e ous than un der ly ing strata. Sam ple G rep re sents very hard pelitic creamy lime stone (highly cal -car e ous). Sam ple H is very poorly cal -car e ous soft darkbrown banded clay with rare fish re mains. Two sam ples col
-lected from con glom er atic slump layer rep re sent white
chalky lime stone (sam ple I) and darkbrown 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 stone
com plex rep re sent two va ri et ies. Sam ples M and O are
whit ish-creamy hard organodetrital lime stone, whereas the re main ing sam ples con sist of rhodoids with var i ous amount of 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 the
Micropalaeontological 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 for each 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 of the In sti tute of Geo log i cal Sci ences, Pol ish Acad emy of Sciences, Kraków.
Low fre quency of dinoflagellate cysts made that al most all 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 the lab 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 are de pos ited in the In sti tute of Paleobiology, Pol ish Acad emy of Sci ences, Warszawa (ZPAL F. 70). The palaeoenvironmen 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 ples A–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 wood par 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 and sin gle subspherical forms). A dif fer ent palynofacies oc curs in sam ple H taken from dark-brown clays: it con sists of highly dis in te grated small-sized par ti cles of structureless or ganic mat ter; no palynomorphs have been found ex cept of
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 amounts of very well pre served Late Cre ta ceous dinoflagellate cysts (ex cluded from fur ther stud ies in this pa per), and sam ple J
con 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 organodetrital limestone 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 ramosus
s. 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 most sam 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 to sev eral tens per cent. Palynofacies of sam ples from the rhodoid lime stone com plex shows re la tion to li thol ogy: sam -ples col lected from organodetrital lay ers (M, O) con tain a much higher amount of palynological or ganic mat ter than other sam ples from rhodoid lay ers. More over, the for mer
334
P. GEDL & D. PERYTFig. 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
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
336
P. GEDL & D. PERYTFig. 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 of structureless 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; large palynomorphs of un cer tain or i gin [zooclasts?] oc cur); F – sam ple R (palynofacies com posed of equidimensional black phytoclasts)
Fig. 6. Dinoflagellate cysts from Badenian se quence at Kudryntsi: A–D – Lingulodinium machaerophorum (A, B: spec i mens with scabrate 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)
con tain high ra tios of sporomorphs (mainly bisaccate pol len grains) and dinoflagellate cysts. The lat ter yielded mainly black phytoclasts (par tic u larly dom i nat ing in sam ples from up per part of rhodoid com plex: Q and R), ex cept of sam ple N, 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., Polysphaeridium subtile and Lingulodinium machaerophorum, and sin
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P. GEDL & D. PERYTFig. 7. Dinoflagellate cysts from Badenian se quence at Kudryntsi: A, B –Hystrichokolpoma rigaudiae (both spec i mens from sam ple P); C – Impagidinium sp. (sam ple P); D – Pyxidiniopsis sp. (sam ple K); E – Operculodinium sp. (sam ple M); F–I – Polysphaeridium subtile (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 from sam ple N); P, Q – Operculodinium sp. (both spec i mens from sam ple N)
gle specimens of Spiniferites sp. and Dapsilidinium pseudo-
colligerum.
A higher sam ple M (organodetrital lime stone layer) is
com posed of dom i nat ing sporomorphs (mainly bisaccate
pol 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 the ge 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 high ra tio of dinoflagellate cysts – up to 60%. Their as sem blage is 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., Lingulodinium 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 Pentadinium
sp. 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 by pol len grains (up to 60%). Dinoflagellate cysts (20%) from this 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 to 50%) and sporomorphs (30%; be side bisaccate grains, ge nus
Intratriporopollenites is com mon). Dinoflagellate cysts are
rel a tively com mon (app. 15%); their as sem blage con sists
mainly 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 tain
or 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 low
amounts of palynological or ganic mat ter. Their palynofa-cies is dom i nated by small-sized black phytoclasts (up to 90%). 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 Systematophora
placacantha and Lingulodinium machaerophorum; fur ther
-more, Spiniferites spp., Pentadinium sp., Polysphaeridium
subtile, 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 is char ac ter ized by lack of Spiniferites ramosus. Both sam ples con 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 and
fungi (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 shown in Fig ure 8 and se lected spe cies are shown in Fig ures 9 and 10. Sam ples from the siliciclastic unit yielded very rare and poorly 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 bly re worked and re de pos ited (Peryt & Peryt, 2009). One sam -ple (sam -ple A) yielded a quite rich as sem blage of Badenian foraminifers: 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, Cibicidoides pseudoungerianus, 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 is re 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 ing the Ratyn Lime stone (sam ple E; Fig. 8). This low di ver sity as sem blage is char ac ter ized by dom i nance of elphidiids (more than 60%) rep re sented mainly by Elphidium koberi and ?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 Astrononion perfossum 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. M-il-iol-ids are also im por tant con tri bu tors. Their ra tio ex ceeds 40%:
Triloculina spp. (25%), Quinqueloculina spp. (9%), Pyrgo
spp. (4%) and Articulina sp. (3%). Rare large spec i mens of
E. reginum are also re corded. Rosalina is com mon in this
as 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 by
miliolids (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).
340
P. GEDL & D. PERYT . 8 . gi F is t n yr d u K t a ec ne u qe s na i ne da B re p p U e ht ni hti w s p u or g ar efi ni ma r of f o se c na d n u ba e vi t al er d na s e ga l b me ss a l ar efi ni ma r of ci h t ne BFig. 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)
342
P. GEDL & D. PERYTFig. 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 – Guttulina communis (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)
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 lobaLoba-tula (8–10%) are also com mon. Elphidium is very
rare in this as sem blage (Fig. 8). The large tests are of ten dam aged and their sur faces are smoothed due to cur rent activity.
As sem blage VII has been found in the top most part of the rhodoid com plex (sam ples R and S). This as sem blage is char ac ter ized by the high est di ver sity, and by the com mon pres 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 ter the be gin ning of Late Badenian de po si tion char ac ter ized by trans 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 foraminif-ers, which oc cur in vari able ra tios within the Kudryntsi sec tion.Foraminiferal palaeoenvironmental pref er ences Elphidiids are very com mon com po nent of foraminife 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 that con 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 in shal low ma rine en vi ron ments (in ner shelf) with warm to
tem per ate and nor mal to hypersaline (35–70‰) wa ters
(Hay ward et al., 1997; Murray, 2006). Quinqueloculina is an epifaunal dweller, liv ing free or cling ing on plants or sed 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 ments pos sesses Triloculina, com monly oc cur ring in com bi na tion with 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 v-ated 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 Neoconorbina are 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 ganic mat ter. It con sists al most ex clu sively of var i ously pre served black phytoclasts (Fig. 4A); there are no dinoflagellate cysts. 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 for pres er va tion of palynomorphs. A rare oc cur rence of sporo-morphs seems to opt for the first pos si bil ity. These strata were 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 ing to 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, but these 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 is enig matic. One pos si ble ex pla na tion is that the siliciclastic unit 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 Badenian trans gres sion. How ever, other sam ples from this unit are bar ren (ex cept for the re de pos ited Cre ta ceous forms). The al 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 took place in a la goon, which was pe ri od i cally flooded by shortlived 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 ern
Betics, SE Spain, where scarce and poorly pre served
foraminifera are re corded in var i ous gyp sum units (Play´ et
al., 2000, ta ble 2); plank tonic foraminifera are scarce, small
and usu ally poorly pre served, and the ben thic foraminifera seem to have adapted to a wide range of sa lin ity (Play´ et
al., 2000, ta ble 2). The com po si tion of foraminifers in sam
-ple A strongly ar gues for redeposition from older Badenian strata. The Kudryntsi sec tion is lo cated very close to the orig i nal limit of the Badenian gyp sum ba sin (Peryt et al., 2004; Peryt & Peryt, 2009), and to wards the east the Up per Badenian rests upon the Lower Badenian strata (Siplivyy et
al., 1974).
A monospecific as sem blage I with Elphidium koberi from the clayey marly bed from the top most part of the siliciclastic 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 mal ma rine to slightly el e vated sa lin ity, and char ac ter ized by high 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 foraminiferal as sem blage II with Elphidium crispum and E. macellum (samples F, G, J).
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 sively of 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). Foraminiferal as 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 lowma 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 part of the organodetrital lime stone com plex (sam ple K) and in the 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 rine con 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 was rather lim ited, since dinoflagellate cysts are a sig nif i cant component of palynofacies, be ing in dic a tive for hemipe-lagic mode of sed i men ta tion. Such a change may be re lated to a grad ual wid en ing of the ba sin, pos si bly as so ci ated with deep 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 tion
and 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 and proximochorate spec i mens. The lack of peridinioids might be re lated ei ther to pri mary con di tions not suit able for this group of dinoflagellates (e.g. low nu tri ent con di tions of the sur face wa ter) but also un fa vour able syn- and post depositional 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 for their 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 of the rhodoid com plex. The majority of spe cies are typ i cal for shelf en vi ron ment. Some of them, like Polysphaeridium
zoharyi 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 in sam ples M and N (sin gle spec i men of Impagidinium oc curs also 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 in near-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 eral
au thors, these spe cies (es pe cially P. zoharyi) are typ i cal for lit 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. zoharyi
from low sa line en vi ron ments and suggested euryhaline
nature 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 the de po si tion of the low er most part of the rhodoid com plex, in shal 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. Dinoflagellate
cyst as sem blages from sam ples M–O con tain no
Poly-sphaeridium zoharyi: this change might be in ter preted as
tran si tion from higher sa line re gime dur ing de po si tion of the basal part of the rhodoid com plex, into nor mal ma rine en vi ron ment in its higher part. The oc cur rence of some off -shore taxa (Nematosphaeropsis labyrinthus and spe cies of
Impagidinium) 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 shore wa ters (e.g., Morzadec-Kerfourn, 1977; Wall et al., 1977; Harland, 1983; Brinkhuis, 1994). The other com mon spe cies in the mid dle part of the rhodoid com plex –
Operculodi-nium sp. (mainly O. centrocarpum) and LingulodiOperculodi-nium 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 lower sa line con di tions (e.g., Wall & Dale, 1973; Dale, 1996;
Elle-gaard, 2000): in our ma te rial spec i mens of L.
machaerophorum have rather long pro cesses, which may sug gest nor
-mal sa lin ity. Operculodinium centrocarpum, which is a very fre 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 of en 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 et
al., 1989; Ellegaard, 2000), but in Kudryntsi ma te rial spe cies
with “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 are
dom i nated by cos mo pol i tan spe cies Systematophora
placa-cantha and Lingulodinium machaerophorum. Qual i ta tive
fluc tu a tion of tax o nom i cal com po si tion may be re lated to wa ter depth: as sem blages with com mon or dom i nat ing
Operculodinium (sam ples M–O) may re flect slightly deeper
(off shore) en vi ron ment than the ones in hab ited by motile stages 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 from the in ner coastal zone with wa ter depth of 10–30 m, and
Operculodinium 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 mon
Operculodinium. How ever, com mon oc cur rence of Hystrichokolpoma rigaudiae in sam ple P may also in di cate off
shore con di tions since this ge nus, al though com monly be
lieved to be cos mo pol i tan (e.g., Brinkhuis, 1994) is re lated by 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 other en vi ron men tal changes like wa ter tem per a ture.
The foraminiferal as sem blages VI and VII oc cur ring in that part of the sec tion char ac ter ize the high est di ver sity and taxa pre fer ring tem per atewarm 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 rine en vi ron ments (Lobatula, Neoconorbina, Rosalina,
Poroso-nonion, Astrononion), con firms sug ges tions of low er ing of
sa lin ity to nor mal ma rine in the mid dle part of the rodoid com 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 REGINUM
OC CUR RENCE
We fo cused in this pa per on palaeoenvironmental as -pects of our micropalaeontological as sem blages from Kudryntsi. 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 Badenian succes 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 reginum oc curs in the Buglovian and Volhynian (Pishvanova, 1958; Krasheninnikov, 1960), but Krasheninnikov (1958, p. 296 and 302; 1960, fig. 6) noted that it ap pears al ready in the up -per most Badenian (his ho ri zon G). Szczechura (1982) also re ported sin gle spec i mens of this spe cies in the Badenian pro file of Józefów and Hamernia in Roztocze Hills (SE Po -land). Other typ i cally Sarmatian foraminifers ap pear ing in the Anomalinoides dividens Zone (e.g., Czepiec, 1996) are lack 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 have been very sim i lar to those in which the Sarmatian as sem -blages lived (cf. Szczechura, 1982). The same rea son ing may 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 E
and H in the Kudryntsi sec tion. Harzhauser and Piller
(2004b) re corded re worked corallinacean lime stone and
abundant corallinacean frag ments in the Lower Sarmatian deposits of the Vi enna Ba sin and in ter preted them as due to in 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 other outcrops in Aus tria and Hun gary in which the Badenian/ Sarmatian bound ary is ex pressed as hi a tus, and the ear li est Sarmatian de pos its are usu ally re worked Badenian coralli-nacean lime stone, which bear the en tire suite of Badenian taxa, 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 edly
there is some re work ing within the stud ied sec tion at
Kudryntsi, 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 strata and the in cor po ra tion of re worked rhodoids and molluscs di 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 tion above 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 of changes 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 of Late 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 at
highly 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 ergy shal low en vi ron ment (palynofacies of this part of sec tion con 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 warmtem per ate re stricted en vi ron -ment with in creased sa lin ity and chang ing hy dro dy namic in ten sity is sug gested for the top most siliciclastic unit and the 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 foraminiferal as sem blages II (with Elphidium crispum and E. macellum) and III (Elphidiids with spines, i.e. Elphidium aculeatum and E. koberi); the lat ter as sem blage char ac ter izes shal low wa 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 gave rise to anoxic bot tom con di tions as pre sumed from palynofa 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 for
foraminifera, but cru cial for dinoflagellates. The lat ter ap -peared for the first time in the top most part of the organodetrital 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 stone con 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 atewa 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 and the 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
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 der slightly re stricted con di tions re lated to slightly in creased wa 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 ter en 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 yielded a 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 microfossil groups, or bot tom wa ters in hab ited by foraminifera were char ac ter ized by in creased sa lin ity com pared to the sur face marine waters.
The higher part of the rhodoid com plex was de pos ited in ma rine, more off shore, but still rather nearshore en vi ron
-ment. Dinoflagellate cyst as sem blages from the rhodoid
com 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) and nor 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). The monospecific as sem blage V with Lobatula lobatula from the lower part of the rhodoid com plex (sam ple N) in di cates shal lowma 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 is
char 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 the high est tax o nom i cal di ver sity; they in clude taxa pre fer ring tem per atewarm 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 tic
fea 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. PERYTFig. 11. Con cep tual palaeoenvironmental changes in the Late Badenian ba sin at Kudryntsi based on in ter pre ta tion of dinoflagellate cyst and foraminifera as sem blages
may re flect some palaeoenvironmental vari a tion, pos si bly re lated to mi nor cool ing of ma rine wa ters as in duced from
foraminifera re cord (the as sem blage VI con sists of taxa
preferring temperate-warm shallow marine environments, whereas the assemblage VII suggests temperate to cold marine 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 may re flect a slight cool ing dur ing the Late Badenian, but it may be also linked to deep en ing of the ba sin and ap pear ance of colder bottom waters.
The foraminiferal as sem blages from Kudryntsi con tain
Elphidium reginum and Elphidium koberi com mon for the
Sarmatian; 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 cally
Sarmatian foraminifers of the Anomalinoides dividens Zone are lack ing and the oc cur rence of Elphidium reginum and
Elphidium koberi in the Up per Badenian of Kudryntsi is re
-lated to spe cific en vi ron men tal con di tions which were very sim 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 the manu script and crit i cal re marks. Spe cial thanks are due to Mathias Harzhauser 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 ried out 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 Zofia Dubicka for the field as sis tance.
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