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Geo log i cal Quar terly, 2012, 56 (2): 269–284

Lo cal ca tas tro phe caused by tephra in put near Pøemyslovice (Moravia, Czech Re pub lic) dur ing the mid dle Mio cene

Kamil ZÁGORŠEK, Slavomír NEHYBA, Pavla TOMANOVÁ PETROVÁ, Šárka HLADILOVÁ, Maria Aleksandra BITNER, Nela DOLÁKOVÁ, Juraj HRABOVSKÝ and Vladimíra JAŠKOVÁ

Zágoršek K., Nehyba S., Tomanová Petrová P., Hladilová Š., Bitner M. A., Doláková N., Hrabovský J. and Jašková V. (2012) – Lo cal ca -tas tro phe caused by tephra in put near Pøemyslovice (Moravia, Czech Re pub lic) dur ing the mid dle Mio cene. Geol. Quart., 56 (2):269–284. Warszawa.

Col o ni za tion by ma rine or gan isms such as foraminifers, molluscs, bryo zoans, brachi o pods and red al gae dur ing the mid dle Mio cene(early Badenian) trans gres sion near Pøemyslovice (Carpathian Foredeep) was ini tially af fected by a cool wa ter cur rent of un clear or i gin.How ever, shortly af ter wards, fall out of vol ca nic ma te rial caused a to tal ter mi na tion of the biota. Af ter this ca tas tro phe, the biota startedrecolonize the area. The suc ceed ing as so ci a tion, adopted to warm-wa ter in put, is char ac ter is tic of the cli ma tic op ti mum dur ing the earlyBadenian and is com pa ra ble with those of other sec tions re ferred to this in ter val in the Carpathian Foredeep (such as Kralice nadOslavou, Podbøežice, and Hluchov).

Kamil Zágoršek, De part ment of Palae on tol ogy, Na tional Mu seum, Václavské námìstí 68, CZ-115 74 Prague, e-mail:[email protected]; Slavomír Nehyba, Nela Doláková and Juraj Hrabovský, In sti tute of Geo log i cal Sci ences, Masaryk Uni ver sity,Kotláøská 2, 611 37 Brno, Czech Re pub lic; Pavla Tomanová Petrová, Czech Geo log i cal Sur vey, Leitnerova 22, 658 69 Brno, Czech Re -pub lic; Šárka Hladilová, De part ment of Bi ol ogy, Fac ulty of Ed u ca tion, Palacký Uni ver sity, Purkrabská 2, 771 46 Olomouc, Czech Re -pub lic; Maria Aleksandra Bitner, In sti tute of Paleobiology, Pol ish Acad emy of Sci ences, Twarda 51/55, 00-818 Warszawa, Po land;Vladimíra Jašková, Muzeum Prostìjovska v Prostìjovì, námìstí T. G. Masaryka 2, 796 01 Prostìjov, Czech Re pub lic. (re ceived: May11, 2011; ac cepted: Feb ru ary 3, 2012; first pub lished on line May 28, 2012).

Key words: mid dle Mio cene, Carpathian Foredeep, Moravia, Czech Re pub lic, tephra fall out, suc ces sion of biota.

INTRODUCTION

Sed i ment sup ply has long been rec og nized as a key fac torin the creation and de struc tion of ac com mo da tion space andthus in se quence stra tig ra phy (Catuneanu, 2006). The in put ofclastic ma te rial also af fects the qual ity and quan tity of biota byaf fect ing eco log i cal con di tions. Sud den in creases in clastic in -put can have a se ri ous af fect on the biota. Vol ca nic pro cessesare known for “sud den” in puts of large amount ofclastic/volcaniclastic ma te rial into depositional en vi ron ments(Fisher and Schmincke, 1984). Tephra beds are also re cordedin the Neo gene de pos its of the Carpathian Foredeep es pe ciallyin the early Badenian when fall out tephra form ba sin-wide de -pos its typ i cally sev eral centi metres thick and ex cep tion allyreach ing sev eral metres (Nehyba, 1997). These tephra beds areof use in cor re la tion (Nehyba and Roetzel, 1999; Nehyba andStráník, 2005), but their po ten tial ef fect on eco log i cal con di -tions has not yet eval u ated. Boreholes through this in ter val near

Pøemyslovice (Moravia, Czech Re pub lic) have pro vided ussuch a pos si bil ity. De tailed analysis of the re ac tion of var i ousplank tonic and ben thic biotas to in tense tephra in put into thedepositional en vi ron ment is the main topic of this pa per.

GEOLOGICAL SETTING

The Neo gene de pos its stud ied are a part of the CarpathianForedeep (CF). The CF is a pe riph eral fore land ba sin that de -vel oped from subsurface load ing of the Al pine-Carpathianorogenic belt on the pas sive mar gin of the Bo he mian Mas sif(Picha et al., 2006). De po si tion be gan in Egerian–earlyEggenburgian times and con tin ued in the area of the Czech Re -pub lic up to the late Badenian (Brzobohatý and Cicha, 1993).Dur ing the early mid dle Mio cene the CF ge om e try was re-or -ga nized, be cause the NNW- and NW-ori ented com pres sion ofthe Carpathian orogenic wedge changed to wards NNE- andNE-ori ented com pres sion. The max i mum thick ness of the

lower Badenian de pos its is more than 700 m. De pos its ofcoarse-grained Gilbert del tas, coastal and la goonal de pos itsand deeper-ma rine de pos its have all been rec og nized (Nehyba,2000). The deeper-ma rine de pos its (“Tegel”) com prisemudstones with silts, clays and shell de bris and pre dom i nate inthe infill of the ba sin. They have been in ter preted as outer shelfde pos its or hemipelagites (Nehyba et al., 2008). Coastal, la -goonal de pos its as well as oc cur rences of al gal and bryo zoanlime stones, cal car e ous sand stones and beds of dis tal airfalltephra (Nehyba, 1997; Dolakova et al., 2008) are re strictedboth areally and in thick ness. Iso lated rel ics of lower Badeniande pos its can be found far to the west of the pres ent ex tent of theba sin (Nehyba and Hladilová, 2004). Such var ied Neo gene de -pos its have been rec og nized also in cen tral Moravia, aroundProstìjov (Fig. 1).

The Mio cene deposits of the north west ern part of the CFnear the vil lage of Pøemyslovice were stud ied for the first timeby Schwarz (1946). A new in ves ti ga tion was ini ti ated byJašková (1998) af ter find ing rich bryo zoan-bear ing deposits inthe vi cin ity of Pøemyslovice. Be cause no sec tions were avail -able close to these lo ca tions, we de cided to drill shal low bore -holes to examine the sed i men tary suc ces sion. Pre lim i narybore holes were drilled in 2006 (Zágoršek and Holcová, 2009).

Re gion ally, Pre cam brian crys tal line base ment is cov ered bylower Car bon if er ous (Culmian) clastic de pos its of the DrahanyHigh land unit (Mísaø et al., 1985). De pos its of the Rozstání Fm.(Visean), com posed of al ter nat ing fine-grained greywackes,siltstones and shales, form the pre-Neo gene sub strate aroundPøemyslovice (Otava et al., 1995). NW–SE ori ented faults (theHaná fault belt), which were ac tive dur ing the Variscan orog enyand were re ac ti vated dur ing the Al pine orog eny, played an im -por tant role in the cre ation of depositional space dur ing the Neo -gene. A com pli cated re lief of fault-bounded steep, nar row de -pres sions and intrabasinal highs was formed, dip ping at a high

an gle to wards the cen tral part of the ba sin (Zapletal, 2004). Theold est Neo gene ma rine de pos its are Karpatian in age (Vysloužil,1981; Bubík and Dvoøák, 1996). A dom i nant role in the Neo -gene sed i men tary suc ces sion is played by the lower Badeniande pos its (Fig. 2), which of ten di rectly over lie the pre-Neo genesub strate. They reach their great est thick ness (more than 100 m)in the Prostìjov and Lutín de pres sions. Nu mer ous iso lated rel icsof Neo gene de pos its in the Drahany High land rep re sent pro lon -ga tion of the Prostìjov de pres sion to wards the NW (Kalabis,1961; Novák, 1975; Jašková, 1998; Zapletal et al., 2001;Zapletal, 2004). These de pos its, up to a few metres thick, areusu ally formed red al gal lime stones and sands whereas con -glom er ates and clays are rare.

270 Kamil ZÁGORŠEK et al.

Fig. 1. Geo graph ical sketch of the po si tion of the bore holes stud ied

Fig. 2. Strati graphic po si tion of the sec tion stud ied

METHODS

Re cently, three new shal low bore holes, PY5–7, have beendrilled near Pøemyslovice (GPS lo ca tion 49°34.169 N and016°57.928 E) called PY5 to PY7 (Fig. 1). Here, we pro videdetailed anal y sis of the bore hole logs.

Com bined siev ing and la ser meth ods were used for grainsize anal y sis. The Retch AS 200 siev ing ma chine ana lysed thecoarser grain frac tion (4–0.063 mm, wet siev ing), a Cilas 1064la ser dif frac tion granulometer be ing used for the finer frac tions(0.0004–0.5 mm). Ul tra sonic dis per sion, dis tilled wa ter andwash ing in so dium polyphosphate were used prior to anal y ses inor der to avoid floc cu la tion of the par ti cles ana lysed. The av er age grain size is dem on strated by the graphic mean (Mz) and the uni -for mity of the grain size dis tri bu tion/sort ing via the stan dard de -

vi a tion (sI) (Folk and Ward, 1957). Lithofacies anal y sis wasdone fol low ing Tucker (1988), Walker and James (1992) andNemec (2005). The shape and round ness of the coars est grainfrac tion (>4 mm – sieve sep a ra tion) were es ti mated vi su ally us -ing the method of Pow ers (1982). Heavy min er als were stud iedin the grain size frac tion 0.063–0.125 mm. The min eral com po -si tions of se lected heavy min er als were de ter mined us ing theCameca SX 100 elec tron microprobe at the Joint Lab o ra tory ofElec tron Mi cros copy and Microanalyses of the Masaryk Uni ver -sity and the Czech Geo log i cal Sur vey, Brno.

Ground pen e trat ing ra dar (GPR) scan ning em ployed aPulse Ekko Pro ra dar, man u fac tured by the Ca na dian com panySen sor & Soft ware, at a fre quency of 50 MHz with an an tennadis tance of 3 m. The mea sure ment in ter val was 0.5 m. TheAcme An a lyt i cal Lab o ra to ries Ltd. (Van cou ver) pro ducedchem i cal anal y ses of se lected sam ples by stan dard an a lyt i calmeth ods.

Sed i ments were soaked in warm wa ter with so dium car -bon ate for one day for dissaggregation, and then washed un derrun ning wa ter through 0.063 mm mesh sieves. Foraminiferswere picked from the frac tion, and iden ti fied with a WILD bin -oc u lar mi cro scope.

Groups of ag glu ti nated foraminifers, deep- and shal -low-wa ter foraminifers and euryoxybiont foraminifers were in -ter preted ac cord ing to the palaeo eco logi cal stud ies of Kaiho(1994), Spezzaferri and Æoriæ (2001), Spezzaferri et al. (2004)and Murray (2006). Biostratigraphic data were cor re lated withplank tonic foraminiferal zones by Berggren et al. (1995). Rec -og ni tion of cen tral Paratethys re gional stages and thebiostratigraphic eval u a tion of plank tonic foraminifers fol lowed Cicha et al. (1998).

The bryo zoans were stud ied from the frac tion larger than

200 mm. A few sam ples from more lithified rock sam ples were“lab o ra tory weath ered” and/or treated with ace tic acid as de -scribed by Zágoršek and Vávra (2000). Fi nally the sam pleswere cleaned in an ul tra sonic bath. The de tailed de ter mi na tionand anal y ses of skel e ton pres er va tion were car ried out with ascan ning elec tron mi cro scope (SEM) (JSM-6400 Jeol) in thePalaeontological De part ment of Vi enna Uni ver sity and aHitachi S3700N in the Paleontological De part ment of Na tionalMu seum Prague.

Al to gether fif teen sam ples of three taxa (Smittinacervicornis, Exidmonea sp. and celleporids) were se lected forgeo chem i cal stud ies. The sam ples se lected came from the same depth (bore hole PY7 depth 2.3 m – just above the tephra lay -ers). More than 50 mg of skel e tal ma te rial was re quired for geo -chem i cal anal y sis. The bryo zoan skel e tons were man u ally sep -a rated from the en clos ing rocks, cleaned in an ul tra soniccleaner and pul ver ized. Cathodolu mi nes cence was used toeval u ate pos si ble diagenetic al ter ation. The anal y ses of sta bleiso topes were per formed by the Lab o ra tory of the Czech Geo -log i cal Sur vey, Prague. Ox y gen and car bon iso tope mea sure -ments were per formed on a Finnigan MAT-251. The car bon

and ox y gen iso to pic ra tios are ex pressed in d no ta tion.The molluscs were stud ied from washed sam ples (PY5 – 11

sam ples, PY6 – 14 sam ples, PY7 – 16 sam ples). Al to gether twelve sam ples were used for palynological

stud ies. They were treated with cold HCl (35%) and HF (70%),re mov ing car bon ates and sil ica. Sep a ra tion of thepalynomorphs from the rest of the res i due was car ried out us ing ZnCl2 (den sity = 2g/cm3).

RESULTS

GEOPHYSICS

Two georadar pro files were mea sured at the lo cal ity. Thepo si tion of the pro files is shown in Fig ure 1. De ter mi na tion ofthe re lief of the un der ly ing pre-Neo gene bed rock and the shapeof the body of the early Badenian de pos its were the main ob jec -tives of this sur vey.

In ter pre ta tion of the geo phys i cal pro files is shown in Fig -ure 3. The pro files in di cate that the early Badenian deposits rest on a highly ir reg u lar and in clined re lief. The thick ness of Neo -gene de pos its is only few metres and is controlled by the re liefmor phol ogy, with greater thick nesses in de pres sions and thin -ning up slope. Neo gene de pos its rest here on weath ered Culmsed i men tary rocks. The thick ness of the pack age of weath eredsub strate rocks is approx. 4–6 m. The base ment re lief is af -fected by tec tonic struc tures/dis lo ca tions.

FACIES ANALYSIS

Sed i men tary fa cies are con sid ered to be the ba sic “build ingblocks” of the sed i men tary suc ces sion (Harms et al., 1975;Walker and James, 1992; Read ing, 1996). Lithofacies here arede fined ac cord ing to their pe trog ra phy, grain size and pre servedsed i men tary struc tures. Lithofacies de scrip tions are shown inTa ble 1 and their oc cur rence in lithostratigraphic logs (Fig. 4).

Lithofacies have been com bined, based on their spa tialgroup ing and depositional ar chi tec ture, with thepalaeontological con tent of the beds. Such an ap proach has ledto the rec og ni tion of four depositional units (A, B, C and D)within the sed i men tary suc ces sion studied. The oc cur rences ofthe units can be fol lowed in Figure 4. The units rep re sent theba sis for an in ter pre ta tion of the var i ous modes of sed i mention(see de scrip tion of the units later in the text).

Local catastrophe caused by tephra input near Pøemyslovice (Moravia, Czech Republic) during the middle Miocene 271


Fig. 3. In ter pre ta tion of georadar pro files at the Pøemyslovice lo cal ity

Sl Light green ir reg u larly lam i nated fine sand (Mz = 4.6–5.6f , sI = 2.3–2.9f).

SfLight grey-green fine sand, whit ish mot tled. Par al lel lam i na tion to flaser bed ding. Laminae and thin lay ers of sand stones (up to 3 cm thick) are sep -

a rated by laminae of grey ish mudstone. Shell de bris and gran ules and small peb bles of Culmian rocks along sharp base (up to 0.5 cm).

Mz = 5.9f , sI = 2.9f.

Mg Light grey-green mudstone – muddy gravel with an gu lar clasts of Culmian rocks (up to 10 cm). Mz = 2.5f , sI = 4.3f.

Mi Light green to whit ish green mudstone with an gu lar intraclasts of green clay up to 2 cm, cha otic fab ric, dis torted sandy laminae.

Ms Light green to grey-green sandy mudstone.

Hl Al ter na tion of flaser beds of cal car e ous sand and cal car e ous clay – flaser-wavy bed ding. Sharp base.

Lg Whit ish cal car e ous sand stone to sandy lime stone, sharp base, rare an gu lar intraclasts of yel low ish mudstone (up to 1 cm), fossiliferous. An gu larclasts of Culmian rocks at the base (up to 10 cm).

Vl Whit ish very fine cal car e ous tephra, pla nar lam i na tion. Mz = 3.9–4.7f , sI = 1.8–2.4f.

ViWhit ish grey to white cal car e ous tephra with ad mix ture of an gu lar intraclasts of grey-green to light grey mudstone (up to 5 cm).

Mz = 4.6–4.7f, sI = 1.9–2.1f.

T a b l e 1

List of lithofacies re cog nized in the stud ied Neo gene de pos its of Pøemyslovice

GEOCHEMISTRY

Two clear clus ters were dis tin guished in geo chem i cal anal -y sis (Fig. 5). One clus ter shows d13C from –0.1 to –0.8‰ whilethe sec ond one has val ues d13C from –2.1 to –2.9‰. Sim i larly,d18O val ues show sep a ra tion into two clus ters (one from 1.6 to1.3‰, the sec ond from 0.7 to 1.1‰). These clus ters do not re -flect tax on omy, as all fos sil groups ana lysed include sam ples

be long ing to both clus ters. There are no dif fer ences be tweenCheilostomata and Cyclostomata, nor as re gards the sizes of the col o nies. Shift in d13C re corded in the nearby sec tion ofPodbøežice (Nehyba et al., 2008) was not ev i dent. There fore,we as sume that this sharp dis tinc tion may in di cate two dif fer ent orig i nal en vi ron ments.

The palaeotemperature cal cu lated from O iso topes rangesbe tween 16.5 and 18.2oC for the first clus ter and 14.4 and


Fig. 4. Sub di vi sion of the sed i men tary and palaeontological suc ces sion in the bore holes stud ied in lithostratigraphic logs

A – PY5, B – PY6, C – PY7

15.7oC for the sec ond clus ter. The pro posed higher d18O valuefor Badenian sea wa ter (+l‰ SMOW), due to evap o ra tion, wasac cepted (sim i larly Latal et al., 2006; cf. Peryt and Gedl, 2010)for the cal cu la tion of palaeotemperatures. The iso to picpalaeotemperatures were cal cu lated from the d18O val ues us ing the equa tion: t (oC ) = 16.9 – 4.2 (dc – dw) + 0.13 (dc – dw)2,where dc de notes the d18O value of the sam ple rel a tive to thePDB stan dard and dw de notes the d18O value of sea wa ter rel a -tive to the SMOW stan dard. These re sults are in agree mentwith a pro posed sub trop i cal cli mate for the early to mid dleMio cene of Cen tral Eu rope based on ectothermic ver te brates(Böhme, 2003) and fishes (Schultz, 2003).

PALAEONTOLOGY

FORAMINIFERS

As sem blages from the bore holes stud ied con tain the lowerBadenian in dex fos sil – Uvigerina macrocarinata. Rarely, the Karpatian re worked spe cies Pararotalia canui and Pappinabreviformis were found. Pappina breviformis also be longs tothe low est Badenian sensu Cicha et al. (1998). Benthos dom i -nates; plank tonic spe cies are very rare, ag glu ti natedforaminifers were iden ti fied spo rad i cally.

We dis tin guish two foraminiferal as sem blages:– Amphistegina as sem blage (AA) – mod er ately large tests

of Amphistegina mammilla and/or Elphidium div. sp.cou pled with the taxa Asterigerinata planorbis andQuinqueloculina div. sp. Amphistegina is a shal low-wa -ter ge nus in hab it ing warm wa ters of the in ner shelf0–130 m deep (win ter min i mum is about 15oC, in sum -mer over 20oC), epifauna in hab it ing coral reefs, la -goons, of ten cou pled with Elphidium div. sp. – i. e. ma -rine spe cies of the in ner shelf to 70 m, which can in habitbrack ish to hypersaline marshes and la goons (all af terMurray, 2006).

– Lenticulina as sem blage (LA) – larger and smaller testsof Lenticulina div. sp., and also Heterolepa spp. cou pled with small tests of deep-wa ter foraminifers in hab it ingcolder wa ter. Lenticulina af ter Murray (2006) is a ma -rine ge nus, in hab it ing cold wa ter of outer shelf tobathyal depths; Pullenia bulloides, Melonispompilioides and nu mer ous Heterolepa dutemplei havesim i lar characteristics.

BRYOZOA

Bryo zoans oc cur in al most all sam ples stud ied and com -pose the larg est part of the fos sil con tent in washed residua(more than 80 wt.% of all fos sils found be long to bryo zoans onav er age). The as so ci a tion is very di verse, more than 100 spe -cies be ing de ter mined al to gether; the list of bryo zoans de ter -mined is given in Appendix (sup ple men tary file*).

Vol u met ri cally dom i nant in the as so ci a tion are celleporidglob u lar col o nies, which are, how ever, un de ter min able to ge -nus level. Very com mon also are rigid erect col o nies of the spe -cies Smittina cervicornis, Metrarabdotos maleckii andCrisidmonea foraminosa, fol lowed by an as so ci a tion of op por -tu nis tic spe cies such as Hornera cf. frondiculata, Onychocellaangulosa, Pleuronea pertusa, Reteporella sp. andTetrocycloecia dichotoma.

Two as so ci a tions may be dis tin guished in the bore holes

stud ied. The older one shows lower di ver sity (£40 spe cies)with a dom i nance of cyclostomatous spe cies (Crisidmoneaforaminosa, Tervia irregularis, Exidmonea atlantica,Mecynoecia pulchella) and the up per one con tains a more di -verse as so ci a tion (about 50–60 spe cies) dom i nated bycheilostomatous col o nies such as Adeonella polystomella,Smittina cervicornis and Metrarabdotos maleckii.

The bryozoan as so ci a tion from Pøemyslovice is one of themost di verse within the CF. The most sim i lar is the as sem blagefrom Podbøežice where 112 spe cies were de ter mined(Zágoršek, 2010a), and from Kralice nad Oslavou where 97spe cies were found (Zágoršek et al., 2009). There is no largedif fer ence in spe cies com po si tion with the CF bryo zoans as so -ci a tions de scribed pre vi ously (Zágoršek, 2010a, b), ex cept inthe pres ence of Poricella areolata which has not been found inany other sec tion.


Fig. 5. Re sults of sta ble iso tope anal y ses of bryo zoan skel e tons

* Supplementary files are available on website: www.gq.pgi.gov.pl

BRACHIOPODA

The in ves ti gated brachi o pods from Pøemyslovice are rareand of low di ver sity; only four spe cies have been de ter mined:the large, smooth terebratulide Terebratula sp. and threemicromophic megathyrid spe cies Megathiris detruncata,Argyrotheca cuneata, and Joania cordata (Fig. 6), A. cuneatadom i nat ing in the ma te rial stud ied.

Re cent rep re sen ta tives of the spe cies de scribed here have avery wide depth range, from a few metres to more than 800 m,thus not be ing good depth in di ca tors. In shal low wa ter theMegathyrididae oc cupy shel tered cryp tic hab i tats such ascaves, crev ices and overlongs (Jack son et al., 1971; Lo gan,1977; Rich ard son, 1997). The pres ence of a suit able sub strateis con sid ered to be one of the most im por tant fac tors con trol -ling the dis tri bu tion of brachi o pods. All spe cies rec og nized inthe sam ples stud ied have a func tional pedicle open ing and lived at tached to a firm sub strate by the pedicle.

RED ALGAE

Red al gae (Rhodophyta, Corallinaceae, Sporolithaceae) are pres ent in two bore holes (PY7 and PY6) in the depth in ter val2.2 to 0.5 m (Ta ble 2). They of ten form rhodoliths with erodedand bro ken sur faces, or thin crusts over grow ing bryo zoans, or

frag ments of these two forms. Spe cies of coralline al gae pres ent of Pøemyslovice are listed in Ta ble 2. Sam ples of rhodolithsand nod ules were col lected from dif fer ent depths in the bore -holes. Though many nod ules were pres ent at dif fer ent depthlev els, most of these were bryo zoan col o nies over grown by thin crusts of coralline al gae. Rhodoliths are ex ten sively bored withIchnoreticulina elegans, an ichnofacies of epi/endolithic greenalga Ostreobium quekettii (Fig. 7). Traces of Ichnoreticulinaworld-wide are dis trib uted in the shal low ma rine en vi ron mentto depths of more than 90 m (Kornmann and Sahling, 1980;Chazottes et al., 2009; Aponte and Ballentine, 2001).

MOLLUSCS

All the bore holes stud ied are mark edly dom i nated by bi -valves (with frag ments of Pectinidae and Ostreidae gen er allypre vail ing), whereas sca pho pods and gas tro pods (Fig. 7) aremuch more scarce both as in di vid u als and spe cies (Appendix).

PALYNOLOGY

All stud ied sam ples were nearly ster ile and con tained al -most no or ganic de bris; only spo radic bleached and de gradedpalynomorphs were ob served.


Fig. 6. Brachi o pods found in Pøemyslovice

A, B – Argyrotheca cuneata; C, F – Joania cordata; D, E – Megathiris detruncata, scale bar – 1 mm

276 Kamil ZÁGORŠEK et al.2

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yrtem

oiB

ax

at la

gla

der fo


Fig. 7. Ex am ples of al gae and molluscs found in the sam ples stud ied

A – Neogoniolithon sp.; B – Phymatolithon calcareum; C – Sporolithon sp.; D – Mesophyllum sancti-dionysii; E – Lithophyllum sp. 1; A– D – scalebars – 1 mm; F – Macrochlamis sp., G – Turritella sp.

UNITS A–D AND THEIR PALAEONTOLOGICAL CONTENT

UNIT A

Unit A lies di rectly on the weath ered pre-Neo gene sub -strate. It com prises only one lithofacies, Mg. The thick ness ofthe unit var ies be tween 0.6 and 1.4 m. The de pos its are poorlysorted (sI = 4.3) and a sig nif i cant pres ence of gran ules andpeb bles is typ i cal (graphic mean Mz = 2.5 f). The con tent ofpsephitic ma te rial is higher to wards the base of the unit wherean gu lar to subangular cob bles (A~10 cm) were recognized.The pe trog ra phy of the peb bles (frac tion above 4 mm) in di -cates prov e nance from the di rect sub strate. Peb bles (spher i calor bladed, rarely discoidal) of Culmian greywackes or shalesstrongly dom i nate. The peb bles are mostly subrounded orrounded, with subangular ones less com mon. A few per centof the peb bles is formed by milky quartz. Gar net, disthene,zoisite and ap a tite were re cog nized among the trans par entheavy min er als.

The de pos its are poor in macrofossils, only a few cor roded,de formed and pyritised frag ments be ing iden ti fied. Some sam -ples con tain only round ish traces re sem bling cysts ofdinoflagellates. The lower, rel a tively diverse, foraminiferal as -sem blages con sist of cold and deep-wa ter taxa dom i nated byMelonis pompilioides, Heterolepa dutemplei, Hoeglundinaelegans and Pullenia bulloides. Be sides these, only oxidisedtraces of dinoflagellates and rare frag ments of indeterminedpectinids were found in this in ter val.

The up per part of the unit con tains a mixed foraminifer as -so ci a tion. Shal low and warm-wa ter el e ments with a dom i nance of Asterigerinata planorbis, Amphistegina mammilla andElphidium div. sp. were oc curred cou pled with deep, cold andeuryoxibont taxa such as Melonis pompilioides, Pulleniabulloides, Heterolepa dutemplei and Lenticulina div. sp. (sensuMurray, 2006). Deep-wa ter spe cies (with spines) were notdam aged, while spec i mens of Heterolepa spp. were usu allycor roded. Ad di tional biota is lim ited to cyclostomatous bryo -zoans (Hornera, Tervia and Ceriopora), very low di ver sitycheilostomes (mainly Reteporella), rare molluscs (Pectinidaeindet., oys ters) and si li ceous spicules per haps from sponges.

UNIT B

Unit B is formed of three lithofacies (Sf, Vi, Vl), with fa cies Vl strongly dom i nant. The thick ness of the unit var ies be tween0.8 and 2.3 m. This unit can be sub di vided into two sub units.Siliciclasic sub unit B1 is com posed of fa cies Sf and was re cog -nised only in bore hole (PY7) above unit A. The volcaniclasticsub unit B2 was re cog nised in all bore holes and is formed by fa -cies Vi and Vl. Volcaniclastic sub unit lies above ei ther unit Aor sub unit B1.

De pos its of siliciclastic sub unit B1 are poorly sorted

(sI = 2.9). The silt frac tion dom i nates form ing 56.9%, with sub -or di nate sand (20.2%) and clay (19.6%) (graphic mean

Mz = 5.9 f). A small ad mix ture of gran ules and small peb bles(max. 1 cm) was also doc u mented. The pe trog ra phy of the peb -bles (frac tion above 4 mm) is sim i lar to that in unit A. Peb bles

(spher i cal or discoidal in shape) of Culmian greywackes orshales dom i nate. The peb bles are mostly subrounded or roundedwhereas subangular ones are less com mon. Peb bles of milkyquartz are rare whereas bro ken cal car e ous shells are fre quent.

A high con tent of silt and very fine sand is typical of thevolcaniclastic sub unit B2. The con tent of heavy min er als isvery low. Zir con, gar net and ap a tite dom i nate among trans par -ent heavy min er als. Zir cons show al most ex clu sively (over


Fig. 8 Trace el e ment dis crim i na tion di a grams for the volcaniclasticrocks clearly dem on strat ing that these are com pa ra ble with earlyBadenian tephra known from the CF that orig i nate from ex plo siveerup tions of rhyolitic to rhyodacitic magmas

90%) an euhedral shape. Such a shape is of ten con sid ered to in -di cate first-cy cle de tri tus, with no pre vi ous depositional his tory and to be ev i dence of a mag matic or vol ca nic or i gin(Poldervaart, 1950; Lihou and Mange-Rajetzky, 1996). Zonedzir cons with older cores were not rec og nized. In clu sions wereob served in all zir cons. Zir con typology (Pupin, 1980, 1985)was used for cor re la tion of Neo gene volcaniclastics in the CF(Nehyba, 1997; Nehyba and Roetzel, 1999; Nehyba andStráník, 2005). Ty po logi cal dis tri bu tion of zir con pop u la tionwas based on the study of 45 grains. The ma jor ity of the zir cons stud ied (63.6%) com prised sub types P1, P2, P3. Sub types P4,S5, S8, S13, S14, S15, S18 and S22 were less com mon. Suchzir cons dom i nated also in vol ca nic zir cons rec og nized withinearly Badenian tephra beds of the ba sin (Nehyba, 1997). Fur -ther ev i dence of the vol ca nic prov e nance of zir cons is the pres -ence of crys tals with a length to width ra tio of more than 3. Theav er age elon ga tion was 2.9 and zir cons with an elon ga tionvalve over 4 form 16%, and over 3 form 40%, in the zir conspec tra stud ied. These value also re flects the high role of vol ca -nic fall out and lim ited redeposition of the tephra (Zimmerle,1979). Zoned zir cons with older cores were not rec og nized. All zir cons stud ied show a high pro por tion of in clu sions. A smallamount of vol ca nic bi o tite was also re cog nized. Bulk dis taltephra anal y ses suf fer es pe cially from postdepositionalchanges and for this rea son they are not very suit able fortephrostratigraphy. Better re sults can be ob tained by im mo bilemi nor and trace el e ments (Winchester and Floyd, 1977;Nehyba, 1997). Se lected di ag nos tic di a grams are shown in Fig -ure 8 and clearly dem on strate that the volcaniclastic rocks stud -ied are com pa ra ble with other early Badenian tephra knownfrom the CF and orig i nate from ex plo sive erup tions ofrhyolitic to rhyodacitic vol ca noes (see Nehyba, 1997). This de -posit can be in ter preted as dis tal air fall tephra partly re de pos -ited. The ex tent of redeposition var ied be tween dif fer ent bore -holes and af fected mainly the up per parts of the unit. Scat teredquartz gran ules and chem i cal vari a tions re flect the im pact ofredeposition. The con tents of Al2O3, Fe2O3 and CaO risewhereas the con tents of SiO2, Na2O and K2O de crease up wards in unit B. More over chem i cal com po si tion of the up per parts ofunit B is sim i lar to that of the basal unit A (Fig. 8).

The de pos its gen er ally con tain few fos sils, com pris ing rarefrag ments of foraminifers, molluscs, the brachi o podMegathiris detruncata, sponges, frag ment of the algaMesophyllum sancti-dionysii over grow ing bryo zoans anddinoflagellates. All these frag ments show long trans port andare prob a bly re worked.

Gen er ally op por tu nis tic (pi o neer) com mu nity with the spe -cies Corbula gibba and Gouldia min ima, op ti mally adapted to un sta ble con di tions, oc curs in the bore holes PY5 (2.1 m) andPY7 (4.5 m). These bi valves are typ i cal rep re sen ta tives of theinfauna, namely sus pen sion or sed i ment feed ers, shal lowlybur row ing in muddy bot toms of intertidal/subtidal to bathyaldepths (Mandic and Harzhauser, 2003).

Sev eral de ter mi na ble pol len grains were ob served in (only)this unit. Grains of Pinus, Myrica, cf. Quercus, themorphospecies Tricolporopollenites liblarensis,Chenopodiaceae and a sin gle cyst of ma rine Dinophyta werefound in sam ples from the 3.7 m depth in bore hole PY7.

UNIT C

Unit C is formed of the siliciclastic lithofacies Sl, Hl, Msand Mi. The thick ness of the unit var ies be tween 0.3 and 0.8 m.Al though silt and very fine sand rep re sent the dom i nant grainsize frac tion in this unit, an ad mix ture of small peb bles andgran ules was also rec og nized. The graphic mean Mz var ies be -tween 3.9 and 4.8 f and the sort ing sI var ies be tween 1.7 and2.3 f. Psephitic frac tion is mostly ab sent or its con tent is verylow. Spher i cal, bladed or discoidal rounded to subroundedgran ules of greywacke and shale dom i nate, form ing 50.8% ofthe peb bles. Bro ken shells are pres ent, with an gu lar tosubangular milky quartz as a few per cent. Psephitic clasts wererec og nized mainly at the base of the unit.

Fos sil as sem blages rep re sent re peated col o ni za tions (as inunit A) and may be di vided into two as so ci a tions, lower and up -per one. At the bound ary be tween these as so ci a tions, a fewfrag ments of Culmian rocks were recognized.

The lower as so ci a tion (sub unit C1) is char ac ter ised by aricher as so ci a tion of plank ton than benthos, a mod er ate di ver -sity of bryo zoans and molluscs, and si li ceous sponge spicules.The foraminifers show a mix ture of AA and LA as sem blageswith plank tonic forms mar gin ally prev a lent and also theeuryoxybiont gen era Uvigerina and Bulimina. The small testshave well-pre served sculp tures and are not dam aged, whilelarger foraminifers are dam aged with abraded sur faces. Thebryo zoan as so ci a tion started with pi o neer gen era(Crisidmonea, Tervia and Mecynoecia), later sup planted bycheilostomate gen era (Reteporella, Celleporaria, Onychocellaand Porella). Other taxa are also com mon; the to tal num ber ofspe cies iden ti fied var ies from 44–55. Brachi o pods are rare, rep -re sented by only one spe cies, Argyrotheca cuneata. Di verse as -so ci a tions of molluscs are char ac ter ized by the pres ence ofAnomia, Aequipecten cf. macrotis and Crassadomamultistriata, to gether with ostreids and un de ter min able bi -valves (mostly epibionts liv ing on hard sub strates in a shal -low-wa ter en vi ron ment with strong cur rents). Al gal re mainsare abun dant, dom i nated by Lithothamnion cf. valens,Lithophyllum, Neogoniolithon sp., Mesophyllumsancti-dionysii, Lithoporella sp. and Phymatolithoncalcareum. Al gae are pres ent as rhodoliths or frag ments ofrhodoliths.

The up per as so ci a tion (sub unit C2) is characterized by a cli -max as so ci a tion. Fos sils are di verse, and the en vi ron men talcon di tions were ideal for rapid col o ni za tion.

The foraminifers rep re sent a mix ture of AA and LA with aslight prev a lence of the lat ter and plank ton dominanted byAmphistegina mammilla, Asterigerinata planorbis andElphidium div. sp., rarely with Heterolepa dutemplei andMelonis pompilioides. Larger tests are abraded, with out anyvis i ble sculp tures on the sur face. Bryo zoans are very diverse,up to 60 spe cies be ing de ter mi na ble, dom i nated bycheilostomatous encrusters (Onychocella, Puellina,Umbonula) and also large erect col o nies as (Smittina,Phoceana, Cellaria, Adeonella). Brachi o pods are rep re sentedby Terebratula sp., Megathiris detruncata and Argytothecacuneata; the lat ter spe cies dom i nates. Molluscs and al gae aredi verse; Aequipecten macrotis, Crassadoma multistriata andPetaloconchus intortus dom i nate among molluscs. Com mon


al gal re mains in clude Lithothamnion, Lithophyllum,Neogoniolithon, Mesophyllum and Lithoporella, a few spe cieseven form ing rhodoliths (Phymatolithon). Later, rhodophytesbe came com mon (Lithothamnion philippi, L. cf. valens, L. sp.,Phymatolithon calcareum, Neogoniolithon sp., Mesophyllumsancti-dionysii, M. obsitum, Lithophyllum, Sporolithon sp.) of -ten over grow ing bryo zoans or form ing rhodoliths.

UNIT D

Unit D is formed of fa cies Lg and sub or di nate Mg. Thebase of the as so ci a tion is sharp and ero sive, with an gu lar andsubangular peb bles of Culm rocks (fa cies Mg) rec og nizedabove it. The thick ness of the as so ci a tion var ies be tween 0.7 mand 1.55 m. The de pos its are poorly sorted with a high CaCO3

con tent, com pris ing mostly calcarenite or calcilutite with somesiliciclastic con tent. Shell de bris dom i nates in the psephiticfrac tion. Small peb bles and gran ules of greywackes are pres -ent, dom i nantly rounded to subrounded and spher i cal ordiscoidal in shape. The gravel and mud con tent is usu ally lower than in the basal fa cies as so ci a tion.

This part of the sec tion con tains the most di verse and richforaminiferal fauna with less plank ton and more abraded AA.Shal low and warm-wa ter foraminifers such as Elphidiumfichtelianum, E. crispum, Asterigerinata planorbis,Amphistegina mammilla, Quinqueloculina div. sp. pre dom i -nate. Cold (deep) wa ter spe cies are less com mon than in units A and C. Among bryo zoans Smittina and Metrarabdotos dom i -nate. No large celleporids oc cur, only smaller ones of ten over -grown by red al gae such as Lithothamnion sp., Mesophyllumsancti-dionysii, Mesophyllum sp., with Lithophyllum form ingrhodoliths. Brachi o pods con tain three spe cies, in clud ingJoania cordata not found in other units. The mol lusc as so ci a -tion is di verse; the most com mon frag ments be long to Ostreaand Aequipecten, the pres ence of wood bor ers (Teredinidae)be ing no ta ble (in bore holes PY5, PY6).

DISCUSSION

The suc ces sions stud ied show flood ing of the ir reg u lar andweath ered base ment of the Bo he mian Mas sif by the earlyBadenian sea. Sed i men ta tion started (unit A) by de po si tion ofre worked lo cal rocks in a rel a tively deep en ing sec tion of thecoastal area. The dinoflagellates and other fos sils sug gest ma -rine conditions.

The first true ma rine fauna is rep re sented by foraminifersdom i nated by Melonis pompilioides, Heterolepa dutemplei,Pullenia bulloides, fol lowed later (unit A) by cyclostomatousbryo zoans and molluscs. The as so ci a tions as a whole are char -ac ter ized by op por tu nis tic and/or pi o neer bryo zoan spe ciessuch as Reteporella, Tervia and Polyascosoecia, sim i lar to thepi o neer as so ci a tion de scribed in the Kralice sec tion (Zágoršeket al., 2009) and in other lo cal i ties in the CF (Holcová andZágoršek, 2008). The foraminiferal as sem blage in di catesdeep-wa ter conditions, un ex pected dur ing trans gres sion. Thepres ence of these deep-wa ter in di ca tors may be, how ever, ex -plained by a cooler en vi ron ment: a cool wa ter cur rent along the

sea shore may have carried deeper wa ter foraminifers to theshal low ma rine ba sin. A similar re gime of in flowing of coolwa ters has been de scribed from the Eocene of Slovakia(Zágoršek, 1996) and Hun gary (Zágoršek, 1993).

The cool wa ter cur rent (an upwelling re gime) may ex plainthe fau nal changes, evoking con di tions re sem bling those ofdeeper wa ter. The shal low-wa ter fauna still flour ished in ar easbe yond the in flu ence of the upwelling current. The orig i nalhab i tats of these dif fer ent fau nas were close to each other, sothe re sult ing strata in clude both el e ments of the fauna. Thissug ges tion is con sis tent with the pres ence of two dif fer ent geo -chem i cal clus ters of bryo zoan spe cies as shown in Fig ure 5.

In flow of the cold wa ters may have been con nected with asteep slope to wards the ba sin floor, are ir reg u lar coast line,strong along-coast cur rents and pos si bly also wind ac tion.These pro cesses may be de tected in di rectly by the re de pos itedna ture of a sig nif i cant part of the suc ces sion, by the thickvolcaniclastic bed and the mix ing of fos sils from dif fer ent eco -log i cal hab i tats. A rel a tively deep-wa ter en vi ron ment of theearly Badenian sea within the broader sur round ings of the areaun der study was pro posed by Brzobohatý (1997). Cold-wa terin flux may be also sup ported by the dom i nant east ern wind di -rec tion in Cen tral Eu rope dur ing the mid dle Mio cene Cli ma ticOp ti mum (17 and 14.5 Ma) as de scribed by Shevenell et al.(2004) and Costeur and Legendre (2006). Such winds wouldhave sup ported upwelling on east ern slopes of the ba sin, as onthe mar gin of the CF on the Bo he mian Mas sif, where thePøemyslovice sec tion is sit u ated. Sim i lar con di tions have beende scribed from older sed i men tary se quences of the Cen tralParatethys Sea (Grunert et al., 2010a, b).

The pres ence of al gae from the sub-fam ily Melobesioideaemay in di cate deep wa ter with a tem per ate cli ma tic belt. Ac -cord ing to Aguirre et al. (2000) the subfamily Melobesioideaeoc cu pies deeper and/or cooler en vi ron ments while thesubfamilies Mastophoroideae and Lithophylloideae pre dom i -nantly oc cur in shal low-wa ter set tings of warm and tem per atecli ma tic belts re spec tively. The fam ily Sporolithaceae con tainsal gae grow ing in deep-wa ter set tings in sub trop i cal to trop i calcli ma tic belts. In this con cept a pre dom i nance ofMelobesioideae al gae to gether with the low oc cur rence andabun dance of the al gal subfamilies Mastophoroideae andLithophylloideae may in di cate deeper-wa ter set tings in tem per -ate warm cli mate con di tions or shal low- and deep-wa ter set -tings in a tem per ate cli mate belt. Rhodoliths from Pøemyslovice may show a suc ces sion of en vi ron ments which starts withlithophylloid and mastophoroid al gae in cen tral parts, and endswith melobesioid al gae, or en tire rhodoliths com posed ofmelobesioid al gae. This sug gests rel a tive deep en ing or cool ing, of on en vi ron ment oc cu pied by al gae.

How ever, the south ern emer gence of the ge nus Sporolithon has been lo cated the very shal low and cool cli ma tic con di tionsof South ern Is land of New Zea land (Basso et al., 2009). Thus,in fer ences from the al gal com mu nity from Pøemysloviceshould be cor re lated with those from other or gan isms to in ter -pret the palaeo ec ol ogy correctly.

One might also spec u late about pos si ble in put of rel a tivecooler wa ter due to com mu ni ca tion of the early Badenian fore -land ba sin to wards the north with the Pol ish CF.


The on set of vol ca nic ac tiv ity sharply re duced the di ver sity offos sils in the se quence, with sponge spicules dominanting. Unit Brep re sents a con tin u a tion of the trans gres sion and rel a tive deep en -ing, with sig nif i cant in put of fall out tephra into the area stud ied.Redeposition of volcaniclastic ma te rial from a wider area liklyplayed an im por tant role, be cause the thick ness of tephra bedshere is greater com pared to cen tral/deeper parts of the ba sin(Nehyba, 1997). This layer of volcaniclastics may cor re late intoother CF sec tions, such as Kralice (Zágoršek et al., 2009).

The rapid redeposition of volcaniclastic ma te rial severely,and lo cally catastrophically af fected the biota. Fol low ing theap pear ances of pi o neer bryo zoans, op por tu nis tic molluscs anda rich as so ci a tion of foraminifers, the de pos its con tain al mostno fos sils at all. Volcanic ma te rial has also been de scribed from other ar eas, but its fall out was not so cat a strophic for the ma rine biota. This may be be cause the trans gres sion in Pøemyslovicehad just started and the ba sin was very shal low. There fore thevol ca nic ma te rial filled the ba sin quickly, and killed of thebiota, while elsewhere the bas ins were deeper, the vol ca nic ma -te rial spread over a larger area and only the ben thic biota wasaffected. Zágoršek et al. (2008, 2009) doc u mented an in ter rup -tion in the de vel op ment of the bryo zoan as so ci a tion at Kralice,where foraminifers were lit tle af fected.

Re newed siliciclastic shal low-ma rine de po si tion is rep re -sented by unit C, when trans gres sion prob a bly reached its max -i mum (and so this might be re garded as a max i mum flood ingsur face). The biota was quickly re stored af ter ter mi na tion of the in put of vol ca nic ma te rial (sub unit C1). A short pe riod of pi o -neer com mu ni ties was quickly re placed by a di verse as sem -blage of foraminifers, bryo zoans and molluscs char ac ter is tic of very shal low wa ter. A mixture of AA and LA with a dom i -nance of warm and shal low-wa ter el e ments to gether witheuryoxibiont taxa sug gests a slight de crease in ox y gen levels.Later, cur rents be came stron ger per haps sug gest ingshallowing, with Culm clasts ap pear ing within the Neo gene se -quence. Input of coarse ma te rial into the ba sin may have beencon nected with storms and/or rel a tive shal lowing.

The up per part (sub unit C2) prob a bly rep re sents a newflood ing cy cle in a rel a tively shal low ba sin. The fos sil as so ci a -tion once more shows pi o neer fea tures, quickly re placed bytyp i cal shal low-ma rine as sem blages within eutrophic con di -tions in warm (sub trop i cal) con di tions. The bryo zoan as so ci a -tion (Zágoršek, 2010b) in cludes fewer cool el e ments and in di -cates stron ger cur rents. A char ac ter is tic mix ture of shal low-and deep-wa ter foraminifers is in ter preted as in put of shal -low-wa ter el e ments from the shore to the deep en ing ba sin.

A chang ing en vi ron ment re flected in red al gal nod ules hasbeen widely dem on strated (Basso, 1998; Pisera and Studencki,1989). Growth zones in rhodoliths in di cate chang ing pe ri ods of trans por ta tion and ero sion of the sur face layer and pe ri ods ofgrowth and encrustation commonly marked by microborings.Such pe ri ods of high in ten sity and low fre quency may be re -garded as re flect ing storms (Bassi, 2005) or ep i sodic cur rents(Lund et al., 2000). Checconi et al. (2010) de scribed rhodoliths from the middle Mio cene of South ern Apennines, big ger butwith sim i lar abraded sur faces, as re de pos ited and trans portedbasinwards from shal low to deeper set tings. The small amountof al gae and rhodoliths at Pøemyslovice to gether with theirmostly bro ken na ture sup port this sug ges tion.

A reduction in siliciclastic in put and de po si tion of sandycar bon ates (red-al gal lime stones) is char ac ter is tic of unit D. Avery shal low en vi ron ment is sug gested also by abun dant over -growths of bryo zoans by Lithothamnion. Shal low andwarm-wa ter foraminifers such as Elphidium fichtelianum, E.crispum, Asterigerinata planorbis, Amphistegina mammilla,Quinqueloculina div. sp. predominated, cool- (deep-)wa ter el e -ments oc curring only spo rad i cally. Strong wa ters or cur rentsmay be in di cated by the fre quent oc cur rence of abradedforaminifer tests.

The scar city and deg ra da tion of palynomorphs and or -ganic de bris most prob a bly re flects taphonomy the bore holesstud ied. Pol len deg ra da tion be gins with ox i da tion of the exine (Brooks et al., 1971). The marked deg ra da tion is a func tion of well-ox y gen ated sed i ments and high rates of fun gal and bac -te rial ac tiv ity. Ac cord ing to Hart et al. (1994) the less ter res -trial or ganic mat ter is de liv ered to the shelf dur ing trans gres -sion. The ter res trial or ganic mat ter de pos ited dur ing trans -gres sion is re worked from be low, spends more time at the sed -i ment-wa ter in ter face, and/or is ex posed to morebiodegradation dur ing trans port.

SUMMARY

The sed i men tary suc ces sion stud ied near Pøemysloviceshows ev i dence of ma rine flood ing of the Bo he mian Mas sifdur ing the early Badenian. The sed i men tary pro file has beensub di vided into four depositional units (A, B, C and D). Thebasal unit A lies di rectly on the ir reg u lar and weath eredpre-Neo gene base ment and rep re sents the start of the trans gres -sion. Unit B is formed of siliciclasic sub unit B1 andvolcaniclastic sub unit B2 and rep re sents a fur ther land wardshift of the coast line and sig nif i cant in put of fall out tephra intothe ba sin. Re newed siliciclastic shal low ma rine de po si tion isre corded in unit C and re duc tion of siliciclastic in put and de po -si tion of sandy car bon ates (red-al gal lime stones) is char ac ter is -tic of unit D.

Col o ni za tion by ma rine biota dur ing trans gres sion of theearly Badenian sea has been pro posed. At first (unit A) a coolwa ter cur rent reached the area, but shortly af ter the biota was ex -ter mi nated by in put of vol ca nic ma te rial (unit B). Sub se quently,the biota re cov ered, once more oc cu py ing the area (unit C), thefi nal as so ci a tion (unit D) re flected warm wa ter con di tions char -ac ter is tic of the cli ma tic op ti mum dur ing this time. While othersec tions such as Kralice (Zágoršek et al., 2009) in clude vol ca nicma te rial, only in the Pøemyslovice area did the in put cause eco -log i cal ca tas tro phe. Nev er the less, the ter mi nal as so ci a tion(unit D) is very sim i lar to that of other sec tions. The bi otic di ver -sity is com pa ra ble with that of other sec tions such as Podbøežice,Holubice or Židlochovice (Zágoršek, 2010a, b).

Ac knowl edge ments. The fi nan cial sup port of the GrantAgency of the Czech Re pub lic (pro ject No. TOP/08/E014, pro -ject leader J. Francù) and 205/09/0103 is grate fully ac knowl -edged. We thank M. Harzhauser and T. M. Peryt for valu ablere marks and com ments in their re views.


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