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, doi: 10.7306/gq.1021
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 started recolonize 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 Early Badenian 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 nad Oslavou, 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:
kamil.zagorsek@nm.cz; 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: May 11, 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 tor in the cre ation and de struc tion of ac com mo da tion space and thus in se quence stra tig ra phy (Catuneanu, 2006). The in put of clastic ma te rial also af fects the qual ity and quan tity of biota by af 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 cesses are known for “sud den” in puts of large amount of clastic/volcaniclastic ma te rial into depositional en vi ron ments (Fisher and Schmincke, 1984). Tephra beds are also re corded in the Neo gene de pos its of the Carpathian Foredeep es pe cially in 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 ally reach ing sev eral metres (Nehyba, 1997). These tephra beds are of use in cor re la tion (Nehyba and Roetzel, 1999; Nehyba and Stráník, 2005), but their po ten tial ef fect on eco log i cal con di - tions has not yet eval u ated. Bore holes through this in ter val near
Pøemyslovice (Moravia, Czech Re pub lic) have pro vided us such a pos si bil ity. De tailed anal y sis of the re ac tion of var i ous plank tonic and ben thic biotas to in tense tephra in put into the depositional 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 Carpathian Foredeep (CF). The CF is a pe riph eral fore land ba sin that de - vel oped from subsurface load ing of the Al pine-Carpathian orogenic 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–early Eggenburgian 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 of the Carpathian orogenic wedge changed to wards NNE- and NE-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 of coarse-grained Gilbert del tas, coastal and la goonal de pos its and deeper-ma rine de pos its have all been rec og nized (Nehyba, 2000). The deeper-ma rine de pos its (“Tegel”) com prise mudstones with silts, clays and shell de bris and pre dom i nate in the infill of the ba sin. They have been in ter preted as outer shelf de 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 zoan lime stones, cal car e ous sand stones and beds of dis tal airfall tephra (Nehyba, 1997; Dolakova et al., 2008) are re stricted both areally and in thick ness. Iso lated rel ics of Lower Badenian de pos its can be found far to the west of the pres ent ex tent of the ba sin (Nehyba and Hladilová, 2004). Such var ied Neo gene de - pos its have been rec og nized also in cen tral Moravia, around Prostìjov (Fig. 1).
The Mio cene deposits of the north west ern part of the CF near the vil lage of Pøemyslovice were stud ied for the first time by Schwarz (1946). A new in ves ti ga tion was ini ti ated by Jašková (1998) af ter find ing rich bryo zoan-bear ing deposits in the 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 nary bore holes were drilled in 2006 (Zágoršek and Holcová, 2009).
Re gion ally, Pre cam brian crys tal line base ment is cov ered by lower Car bon if er ous (Culmian) clastic de pos its of the Drahany High 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 around Pøemyslovice (Otava et al., 1995). NW–SE ori ented faults (the Haná fault belt), which were ac tive dur ing the Variscan orog eny and 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). The old 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 Badenian de pos its (Fig. 2), which of ten di rectly over lie the pre-Neo gene sub 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 ics of 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, are usu 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 been drilled near Pøemyslovice (GPS lo ca tion 49°34.169’N and 016°57.928’E) called PY5 to PY7 (Fig. 1). Here, we pro vide de tailed anal y sis of the bore hole logs.
Com bined siev ing and la ser meth ods were used for grain-size anal y sis. The Retch AS 200 siev ing ma chine ana lysed the coarser grain frac tion (4–0.063 mm, wet siev ing), a Cilas 1064 la 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 and wash ing in so dium polyphosphate were used prior to anal y - ses in or 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 was done fol low ing Tucker (1988), Walker and James (1992) and Nemec (2005). The shape and round ness of the coars est grain frac 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 ied in 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 the Cameca SX 100 elec tron microprobe at the Joint Lab o ra tory of Elec 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 a Pulse Ekko Pro ra dar, man u fac tured by the Ca na dian com pany Sen sor & Soft ware, at a fre quency of 50 MHz with an an tenna dis tance of 3 m. The mea sure ment in ter val was 0.5 m. The Acme An a lyt i cal Lab o ra to ries Ltd. (Van cou ver) pro duced chem i cal anal y ses of se lected sam ples by stan dard an a lyt i cal meth 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 der run ning wa ter through 0.063 mm mesh sieves. Foraminifers were 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 with plank tonic foraminiferal zones by Berggren et al. (1995). Rec - og ni tion of cen tral Paratethys re gional stages and the biostratigraphic 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 ples were cleaned in an ul tra sonic bath. The de tailed de ter mi na tion and anal y ses of skel e ton pres er va tion were car ried out with a scan ning elec tron mi cro scope (SEM; JSM-6400 Jeol) in the Palaeontological De part ment of Vi enna Uni ver sity and a Hitachi S3700N in the Paleontological De part ment of Na tional Mu seum Prague.
Al to gether fif teen sam ples of three taxa (Smittina cervicornis, Exidmonea sp. and celleporids) were se lected for geo 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 sonic cleaner and pul ver ized. Cathodolu mi nes cence was used to eval u ate pos si ble diagenetic al ter ation. The anal y ses of sta ble iso 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 the palynomorphs 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. The po si tion of the pro files is shown in Fig ure 1. De ter mi na tion of the re lief of the un der ly ing pre-Neo gene bed rock and the shape of 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 de pos its 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 con trolled by the re lief mor 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 Culm sed i men tary rocks. The thick ness of the pack age of weath ered sub 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 ing blocks” of the sed i men tary suc ces sion (Harms et al., 1975;
Walker and James, 1992; Read ing, 1996). Lithofacies here are de fined ac cord ing to their pe trog ra phy, grain size and pre served sed i men tary struc tures. Lithofacies de scrip tions are shown in Ta ble 1 and their oc cur rence in lithostratigraphic logs (Fig. 4).
Lithofacies have been com bined, based on their spa tial group ing and depositional ar chi tec ture, with the palaeontological con tent of the beds. Such an ap proach has led to the rec og ni tion of four depositional units (A–D) within the sed i men tary suc ces sion stud ied. The oc cur rences of the units can be fol lowed in Fig ure 4. The units rep re sent the ba sis for an in ter pre ta tion of the var i ous modes of sedimention (see de - scrip tion of the units later in the text).
272 Kamil Zágoršek et al.
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).
Sf
Light 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 lar clasts 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
Vi Whit 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‰ while the 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 to 1.3‰, 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 in clude sam ples
be long ing to both clus ters. There are no dif fer ences be tween Cheilostomata and Cyclostomata, nor as re gards the sizes of the col o nies. Shift in d13C re corded in the nearby sec tion of Podbøežice (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 ranges be 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 value for Badenian sea wa ter (+l‰ SMOW), due to evap o ra tion, was ac cepted (sim i larly Latal et al., 2006; cf. Peryt and Gedl, 2010) for the cal cu la tion of palaeotemperatures. The iso to pic palaeotemperatures 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 the PDB 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 ment with a pro posed sub trop i cal cli mate for the Early to Mid dle Mio 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 Lower Badenian in dex fos sil – Uvigerina macrocarinata. Rarely, the Karpatian re worked spe cies Pararotalia canui and Pappina breviformis were found. Pappina breviformis also be longs to the low est Badenian sensu Cicha et al. (1998). Benthos dom i - nates; plank tonic spe cies are very rare, ag glu ti nated foraminifers 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 and Quinqueloculina div. sp. Amphistegina is a shal low-wa - ter ge nus in hab it ing warm wa ters of the in ner shelf 0–130 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 habit brack ish to hypersaline marshes and la goons (all af ter Murray, 2006).
– Lenticulina as sem blage (LA) – larger and smaller tests of Lenticulina div. sp., and also Heterolepa div. sp. cou - pled with small tests of deep-wa ter foraminifers in hab it - ing colder wa ter. Lenticulina af ter Murray (2006) is a ma rine ge nus, in hab it ing cold wa ter of outer shelf to bathyal depths; Pullenia bulloides, Melonis pompilioides and nu mer ous Heterolepa dutemplei have sim 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 on av 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 Ap pen dix (sup ple men tary file*).
Vol u met ri cally dom i nant in the as so ci a tion are celleporid glob 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 and Crisidmonea foraminosa, fol lowed by an as so ci a tion of op por - tu nis tic spe cies such as Hornera cf. frondiculata, Onychocella angulosa, Pleuronea pertusa, Reteporella sp. and Tetrocycloecia 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 (Crisidmonea foraminosa, 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 by cheilostomatous col o nies such as Adeonella polystomella, Smittina cervicornis and Metrarabdotos maleckii.
The bryozoan as so ci a tion from Pøemyslovice is one of the most di verse within the CF. The most sim i lar is the as sem blage from Podbøežice where 112 spe cies were de ter mined (Zágoršek, 2010a), and from Kralice nad Oslavou where 97 spe cies were found (Zágoršek et al., 2009). There is no large dif 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 in the pres ence of Poricella areolata which has not been found in any other sec tion.
274 Kamil Zágoršek et al.
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 rare and of low di ver sity; only four spe cies have been de ter mined:
the large, smooth terebratulide Terebratula sp. and three micromophic megathyrid spe cies Megathiris detruncata, Argyrotheca cuneata, and Joania cordata (Fig. 6), A. cuneata dom 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 a very 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 the Megathyrididae oc cupy shel tered cryp tic hab i tats such as caves, crev ices and overlongs (Jack son et al., 1971; Lo gan, 1977; Rich ard son, 1997). The pres ence of a suit able sub strate is 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 in the 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 val 2.2 to 0.5 m (Ta ble 2). They of ten form rhodoliths with eroded and 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 rhodoliths and 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 depth lev 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 with Ichnoreticulina elegans, an ichnofacies of epi/endolithic green alga Ostreobium quekettii (Fig. 7). Traces of Ichnoreticulina world-wide are dis trib uted in the shal low ma rine en vi ron ment to 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 ally pre vail ing), whereas sca pho pods and gas tro pods (Fig. 7) are much more scarce both as in di vid u als and spe cies (Ap pen dix).
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 graded palynomorphs 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
276Kamil Zágoršek et al. 2
e l b a T y
r t e m o i
B o fredal ga ltaxa
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 – scale bars – 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 of the unit var ies be tween 0.6 and 1.4 m. The de pos its are poorly sorted (sI = 4.3) and a sig nif i cant pres ence of gran ules and peb bles is typ i cal (graphic mean Mz = 2.5 f). The con tent of psephitic ma te rial is higher to wards the base of the unit where an 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 cal or bladed, rarely discoidal) of Culmian greywackes or shales strongly dom i nate. The peb bles are mostly subrounded or rounded, with subangular ones less com mon. A few per cent of the peb bles is formed by milky quartz. Gar net, disthene, zoisite and ap a tite were re cog nized among the trans par ent heavy 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 of dinoflagellates. The lower, rel a tively diverse, foraminiferal as - sem blages con sist of cold and deep-wa ter taxa dom i nated by Melonis pompilioides, Heterolepa dutemplei, Hoeglundina elegans and Pullenia bulloides. Be sides these, only oxidised traces of dinoflagellates and rare frag ments of indetermined pectinids 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 and Elphidium div. sp. were oc curred cou pled with deep, cold and euryoxibont taxa such as Melonis pompilioides, Pullenia bulloides, Heterolepa dutemplei and Lenticulina div. sp. (sensu Murray, 2006). Deep-wa ter spe cies (with spines) were not dam aged, while spec i mens of Heterolepa div. sp. were usu ally cor roded. Ad di tional biota is lim ited to cyclostomatous bryo - zoans (Hornera, Tervia and Ceriopora), very low di ver sity cheilostomes (mainly Reteporella), rare molluscs (Pectinidae indet., 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 tween 0.8 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 volcaniclastic sub 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 A or 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 or shales dom i nate. The peb bles are mostly subrounded or rounded whereas subangular ones are less com mon. Peb bles of milky quartz are rare whereas bro ken cal car e ous shells are fre quent.
A high con tent of silt and very fine sand is typ i cal of the volcaniclastic sub unit B2. The con tent of heavy min er als is very 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
278 Kamil Zágoršek et al.
Fig. 8 Trace el e ment dis crim i na tion di a grams for the volcaniclastic rocks clearly dem on strat ing that these are com pa ra ble with Early Badenian tephra known from the CF that orig i nate from ex plo sive erup tions of rhyolitic to rhyodacitic mag mas
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). Zoned zir cons with older cores were not rec og nized. In clu sions were ob 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 and Stráník, 2005). Ty po logi cal dis tri bu tion of zir con pop u la tion was 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. Such zir cons dom i nated also in vol ca nic zir cons rec og nized within Early 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. The av er age elon ga tion was 2.9 and zir cons with an elon ga tion valve over 4 form 16%, and over 3 form 40%, in the zir con spec 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 small amount of vol ca nic bi o tite was also rec og nized. Bulk dis tal tephra anal y ses suf fer es pe cially from postdepositional changes and for this rea son they are not very suit able for tephrostratigraphy. Better re sults can be ob tained by im mo bile mi 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 known from the CF and orig i nate from ex plo sive erup tions of rhyolitic 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 tered quartz gran ules and chem i cal vari a tions re flect the im pact of redeposition. The con tents of Al2O3, Fe2O3 and CaO rise whereas 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 of unit 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 rare frag ments of foraminifers, molluscs, the brachi o pod Megathiris detruncata, sponges, frag ment of the alga Mesophyllum sancti-dionysii over grow ing bryo zoans and dinoflagellates. All these frag ments show long trans port and are 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) and PY7 (4.5 m). These bi valves are typ i cal rep re sen ta tives of the infauna, namely sus pen sion or sed i ment feed ers, shal lowly bur row ing in muddy bot toms of intertidal/subtidal to bathyal depths (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, the morphospecies Tricolporopollenites liblarensis, Chenopodiaceae and a sin gle cyst of ma rine Dinophyta were found 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, Ms and 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 grain-size frac tion in this unit, an ad mix ture of small peb bles and gran 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 and 2.3 f. Psephitic frac tion is mostly ab sent or its con tent is very low. Spher i cal, bladed or discoidal rounded to subrounded gran ules of greywacke and shale dom i nate, form ing 50.8% of the peb bles. Bro ken shells are pres ent, with an gu lar to subangular milky quartz as a few per cent. Psephitic clasts were rec 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 in unit 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 few frag ments of Culmian rocks were recognized.
The lower as so ci a tion (sub unit C1) is char ac ter ised by a richer 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 blages with plank tonic forms mar gin ally prev a lent and also the euryoxybiont gen era Uvigerina and Bulimina. The small tests have well-pre served sculp tures and are not dam aged, while larger foraminifers are dam aged with abraded sur faces. The bryo zoan as so ci a tion started with pi o neer gen era (Crisidmonea, Tervia and Mecynoecia), later sup planted by cheilostomate gen era (Reteporella, Celleporaria, Onychocella and Porella). Other taxa are also com mon; the to tal num ber of spe 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 of Anomia, Aequipecten cf. macrotis and Crassadoma multistriata, 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 mains are abun dant, dom i nated by Lithothamnion cf. valens, Lithophyllum, Neogoniolithon sp., Mesophyllum sancti- dionysii, Lithoporella sp. and Phymatolithon calcareum. Al gae are pres ent as rhodoliths or frag ments of rhodoliths.
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 tal con di tions were ideal for rapid col o ni za tion.
The foraminifers rep re sent a mix ture of AA and LA with a slight prev a lence of the lat ter and plank ton dominanted by Amphistegina mammilla, Asterigerinata planorbis and Elphidium div. sp., rarely with Heterolepa dutemplei and Melonis pompilioides. Larger tests are abraded, with out any vis 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 by cheilostomatous encrusters (Onychocella, Puellina, Umbonula) and also large erect col o nies as (Smittina, Phoceana, Cellaria, Adeonella). Brachi o pods are rep re sented by Terebratula sp., Megathiris detruncata and Argytotheca cuneata; the lat ter spe cies dom i nates. Molluscs and al gae are di verse; Aequipecten macrotis, Crassadoma multistriata and Petaloconchus intortus dom i nate among molluscs. Com mon al gal re mains in clude Lithothamnion, Lithophyllum,
Neogoniolithon, Mesophyllum and Lithoporella, a few spe cies even form ing rhodoliths (Phymatolithon). Later, rhodophytes be came com mon (Lithothamnion philippi, L. cf. valens, L. sp., Phymatolithon calcareum, Neogoniolithon sp., Mesophyllum sancti-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. The base of the as so ci a tion is sharp and ero sive, with an gu lar and subangular peb bles of Culm rocks (fa cies Mg) rec og nized above it. The thick ness of the as so ci a tion var ies be tween 0.7 m and 1.55 m. The de pos its are poorly sorted with a high CaCO3
con tent, com pris ing mostly calcarenite or calcilutite with some siliciclastic con tent. Shell de bris dom i nates in the psephitic frac tion. Small peb bles and gran ules of greywackes are pres - ent, dom i nantly rounded to subrounded and spher i cal or discoidal 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 rich foraminiferal fauna with less plank ton and more abraded AA.
Shal low and warm-wa ter foraminifers such as Elphidium fichtelianum, 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., Mesophyllum sancti-dionysii, Mesophyllum sp., with Lithophyllum form ing rhodoliths. Brachi o pods con tain three spe cies, in clud ing Joania 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 Ostrea and 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 and weath ered base ment of the Bo he mian Mas sif by the Early Badenian sea. Sed i men ta tion started (unit A) by de po si tion of re worked lo cal rocks in a rel a tively deep en ing sec tion of the coastal area. The dinoflagellates and other fos sils sug gest ma - rine con di tions.
The first true ma rine fauna is rep re sented by foraminifers dom i nated by Melonis pompilioides, Heterolepa dutemplei, Pullenia bulloides, fol lowed later (unit A) by cyclostomatous bryo 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 cies such as Reteporella, Tervia and Polyascosoecia, sim i lar to the pi o neer as so ci a tion de scribed in the Kralice sec tion (Zágoršek et al., 2009) and in other lo cal i ties in the CF (Holcová and Zágoršek, 2008). The foraminiferal as sem blage in di cates deep-wa ter conditions, un ex pected dur ing trans gres sion. The pres 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 the
shal low ma rine ba sin. A similar re gime of in flowing of cool wa 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 plain the fau nal changes, evok ing con di tions re sem bling those of deeper wa ter. The shal low-wa ter fauna still flour ished in ar eas be yond the in flu ence of the upwelling cur rent. The orig i nal hab i tats of these dif fer ent fau nas were close to each other, so the re sult ing strata in clude both el e ments of the fauna. This sug 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 a steep 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 ited na ture of a sig nif i cant part of the suc ces sion, by the thick volcaniclastic 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 the Early Badenian sea within the broader sur round ings of the area un der study was pro posed by Brzobohatý (1997). Cold-wa ter in 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 tic Op ti mum (17 and 14.5 Ma) as de scribed by Shevenell et al.
(2004) and Costeur and Legendre (2006). Such winds would have sup ported upwelling on east ern slopes of the ba sin, as on the mar gin of the CF on the Bo he mian Mas sif, where the Pøemyslovice sec tion is sit u ated. Sim i lar con di tions have been de scribed from older sed i men tary se quences of the Cen tral Paratethys Sea (Grunert et al., 2010a, b).
The pres ence of al gae from the sub-fam ily Melobesioideae may 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 Melobesioideae oc cu pies deeper and/or cooler en vi ron ments while the subfamilies Mastophoroideae and Lithophylloideae pre dom i - nantly oc cur in shal low-wa ter set tings of warm and tem per ate cli ma tic belts re spec tively. The fam ily Sporolithaceae con tains al gae grow ing in deep-wa ter set tings in sub trop i cal to trop i cal cli ma tic belts. In this con cept a pre dom i nance of Melobesioideae al gae to gether with the low oc cur rence and abun dance of the al gal subfamilies Mastophoroideae and Lithophylloideae 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 with lithophylloid and mastophoroid al gae in cen tral parts, and ends with melobesioid al gae, or en tire rhodoliths com posed of melobesioid 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 tions of South ern Is land of New Zea land (Basso et al., 2009). Thus, in fer ences from the al gal com mu nity from Pøemyslovice should 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 tive cooler 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.
280 Kamil Zágoršek et al.
The on set of vol ca nic ac tiv ity sharply re duced the di ver sity of fos sils in the se quence, with sponge spicules dominanting. Unit B rep 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 likly played an im por tant role, be cause the thick ness of tephra beds here is greater com pared to cen tral/deeper parts of the ba sin (Nehyba, 1997). This layer of volcaniclastics may cor re late into other 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 the ap pear ances of pi o neer bryo zoans, op por tu nis tic molluscs and a rich as so ci a tion of foraminifers, the de pos its con tain al most no 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 Pøemyslovice had just started and the ba sin was very shal low. There fore the vol ca nic ma te rial filled the ba sin quickly, and killed of the biota, 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 was affected. 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 ing sur 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 with euryoxibiont taxa sug gests a slight de crease in ox y gen levels.
Later, cur rents be came stron ger per haps sug gest ing shallowing, with Culm clasts ap pear ing within the Neo gene se - quence. Input of coarse ma te rial into the ba sin may have been con nected with storms and/or rel a tive shal lowing.
The up per part (sub unit C2) prob a bly rep re sents a new flood 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 by typ 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 has been 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 of growth and encrustation com monly 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 Mid dle Mio cene of South ern Apennines, big ger but with sim i lar abraded sur faces, as re de pos ited and trans ported basinwards from shal low to deeper set tings. The small amount
of al gae and rhodoliths at Pøemyslovice to gether with their mostly bro ken na ture sup port this sug ges tion.
A reduction in 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. A very shal low en vi ron ment is sug gested also by abun dant over - growths of bryo zoans by Lithothamnion. Shal low and warm-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 rents may be in di cated by the fre quent oc cur rence of abraded foraminifer 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 holes stud 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 more biodegradation dur ing trans port.
SUMMARY
The sed i men tary suc ces sion stud ied near Pøemyslovice shows ev i dence of ma rine flood ing of the Bo he mian Mas sif dur ing the Early Badenian. The sed i men tary pro file has been sub di vided into four depositional units (A–D). The basal unit A lies di rectly on the ir reg u lar and weath ered pre-Neo gene base - ment and rep re sents the start of the trans gres sion. Unit B is formed of siliciclasic sub unit B1 and volcaniclastic sub unit B2 and rep re sents a fur ther land ward shift of the coast line and sig - nif i cant in put of fall out tephra into the ba sin. Re newed siliciclastic shal low ma rine de po si tion is re 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 the Early Badenian sea has been pro posed. At first (unit A) a cool wa 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), the fi 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 other sec tions such as Kralice (Zágoršek et al., 2009) in clude vol ca nic ma 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 Grant Agency 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 able re marks and com ments in their re views.
REFERENCES
AGUIRRE J., RIDING R. and BRAGA J. C. (2000) – Di ver sity of coralline red al gae: orig i na tion and ex tinc tion pat terns from the Early Cre ta ceous to the Pleis to cene. Paleobiology, 26: 651–667.
APONTE N. E. and BALLANTINE D. L. (2001) – Depth dis tri bu tion of al gal spe cies on the deep in su lar fore reef at Lee Stock ing Is land, Ba - ha mas. Deep-Sea Res., 48: 2185–2194.
BASSI D. (2005) – Larger foraminiferal and coralline al gal fa cies in an Up per Eocene storm-in flu enced, shal low-wa ter car bon ate plat form (Colli Berici, north-east ern It aly). Palaeogeogr. Palaeoclimatol.
Palaeoecol., 226: 17–35.
BASSO D. (1998) – Deep rhodolith dis tri bu tion in the Pontian Is lands, It - aly: a model for the paleoecology of a tem per ate sea. Palaeogeogr.
Palaeoclimatol. Palaeoecol., 137: 173–187.
BASSO D., NALIN R. and NELSON S. C. (2009) – Shal low-wa ter Sporolithon Rhodoliths from North Is land (New Zeeland). Palaios, 24: 92–103.
BERGGREN W. A., KENT D. V., SWISHER C. C., III. and AUBRY M. P.
(1995) – A re vised Ce no zoic geo chron ol ogy and chronostratigraphy.
SEPM Spec. Publ., 54: 129–212.
BÖHME M. (2003) – The Mio cene cli ma tic op ti mum: ev i dence from ectothermic ver te brates of Cen tral Eu rope. Palaeogeogr.
Palaeoclimatol. Palaeoecol., 195: 389–401.
BROOKS J., GRANT P. R., MUIR M., van GIJZEL P. and SHAW G.
(1971) – Sporopollenin. Ac a demic Press, Lon don–New York.
BRZOBOHATÝ R. (1997) – Paleobathymetry of the Lower Badenian (Mid dle Mio cene, Carpathian Foredeep, South Moravia) based on oto - liths. In: Dynamika vztahù marinního a kontinentálního prostøedí (ed.
Š. Hladilová): 37–45. Masarykova univerzita.
BRZOBOHATÝ R. and CICHA I. (1993) – Karpatská pøedhlubeò (in Czech). In: Geologie Moravy a Slezska (eds. A. Pøichystal, V. Obstová and M. Suk): 123–128. MZM, PøF MU.
BUBÍK M. and DVOØÁK J. (1996) – O nálezu karpatu (miocén) a dalších výsledcích vrtu Slatinky MH-10 (in Czech). Zpr. Geol. Výzk. v r.
1995: 20–21.
CATUNEANU O. (2006) – Prin ci ples of se quence stra tig ra phy. Elsevier, Ox ford.
CICHA I., RÖGL F., RUPP CH. and ÈTYROKÁ J. (1998) – Oligocene-Mio cene foraminifera of the Cen tral Paratethys. Abh.
Senckenberg. Naturforsch. Ges., 549: 1–325.
CHAZOTTES V., CABIOCH G., GOLUBIC S. and RADTKE G. (2009) – Bathymetric zonation of mod ern microborers in dead coral sub strates from New Cal edo nia – im pli ca tions for paleodepth re con struc tions in Ho lo cene cor als. Palaeogeogr. Palaeoclimatol. Palaeoecol., 280:
456–468.
CHECCONI A., BASSI D., CARANNANTE G. and MONACO P. (2010) – Re-de pos ited rhodoliths in the Mid dle Mio cene hemipelagic de pos - its of Vitulano (South ern Apennines, It aly): coralline as sem blage char ac ter iza tion and re lated trace fos sils. Sediment. Geol., 225:
50–66.
COSTEUR L. and LEGENDRE S. (2006) – Mam ma lian com mu ni ties doc - u ment a lat i tu di nal en vi ron men tal gra di ent dur ing the Mio cene cli ma - tic op ti mum in West ern Eu rope. Palaios, 23 (5): 280–288.
DOLÁKOVÁ N., BRZOBOHATÝ R., HLADILOVÁ Š. and NEHYBA S.
(2008) – The red-al gal fa cies of the Lower Badenian lime stones of the Carpathian Foredeep in Moravia (Czech Re pub lic). Geol. Carpath., 59 (2): 133–146.
FISHER R. V. and SCHMINCKE H. U. (1984) – Pyroclastic rocks.
Springer, Berlin.
FOLK R. L. and WARD W. (1957) – Brazos River bar: a study in the sig nif - i cance of grain-size pa ram e ters. J. Sed i ment. Petrol., 27: 3–26.
GRUNERT P., HARZHAUSER M., RÖGL F., SACHSENHOFER R., GRATZER R., SOLIMAN A. and PILLER W. E. (2010a) – Ocean o - graphic con di tions trig ger ing the for ma tion of an Early Mio cene (Aquitanian) Konservat-Lagerstätte in the Cen tral Paratethys Sea.
Palaeogeogr. Palaeoclimatol. Palaeoecol., 292: 425–442.
GRUNERT P., SOLIMAN A., HARZHAUSER M., MÜLLEGGER S., PILLER W. E. and RÖGL F. (2010b) – Upwelling con di tions in the
Early Mio cene Cen tral Paratethys Sea. Geol. Carpath., 61 (2):
129–145.
HARMS J. C., SOUTHARD J. B., SPEARING D. R. and WALKER R. G.
(1975) – Depositional en vi ron ments as in ter preted from pri mary sed i - men tary struc tures and strat i fi ca tion se quences. SEPM Short Course, 2: 1–161.
HART F., PASLEY M. A. and GREGORY W. A. (1994) – Par tic u late or - ganic mat ter, maceral fa cies mod els, and ap pli ca tion to se quence stra - tig ra phy. In: Sed i men ta tion of or ganic par ti cles (ed. A. Tra verse):
337–390. Cam bridge Uni ver sity Press.
HOLCOVÁ K. and ZÁGORŠEK K. (2008) – Bryozoa, foraminifera and cal car e ous nannoplankton as en vi ron men tal prox ies of the “bryo zoan event” in the Mid dle Mio cene of the Cen tral Paratethys (Czech Re pub - lic). Palaeogeogr. Palaeoclimatol. Palaeoecol., 267: 216–234.
JACKSON J. B., GOREAU T. and HARTMANN W. D. (1971) – Re cent brachi o pod-coralline sponge com mu ni ties and their paleoecological sig nif i cance. Sci ence, 173: 623–625.
JAŠKOVÁ V. (1998) – Novì objevené miocénní lo cal ity na Prostìjovsku.
Pøírodovìdné Studie Muzea Prostìjovska, 1: 133–139.
KAIHO K. (1994) – Ben thic foraminiferal dis solved-ox y gen in dex and dis solved-ox y gen lev els in the mod ern ocean. Ge ol ogy, 22: 719–722.
KALABIS V. (1961) – Historie výzkumu terciéru širšího okolí Prostìjova.
Sborník Vlastivìdného Muzea Prostìjov, oddíl pøírodovìdný: 59–75.
KORNMAN P. and SAHLING P. H. (1980) – Ostreobium quekettii (Codiales, Chlorophyta). Helgoländer Meeresunters, 34: 115–122.
LATAL Ch., PILLER W. E. and HARZHAUSER M. (2006) – Shifts in ox y - gen and car bon iso tope sig nals in ma rine molluscs from the Cen tral Paratethys (Eu rope) around the Lower/Mid dle Mio cene tran si tion.
Palaeogeogr. Palaeoclimatol. Palaeoecol., 231: 347–360.
LIHOU J. C. and MANGE-RAJETZKY M. A. (1996) – Prov e nance of the Sardona Flysch, east ern Swiss Alps: ex am ple of high-res o lu tion heavy min eral anal y sis ap plied to an ultrastable as sem blage. Sediment.
Geol., 105: 141–157.
LOGAN A. (1977) – Reef dwell ing ar tic u late brachi o pods from Grand Cayman. Proc. 3rd Internat. Coral Reef Sym po sium, Mi ami: 87–93.
LUND M., DAVIES P. J. and BRAGA J. C. (2000) – Coralline Al gal Nod - ules off Fra ser Is land, East ern Aus tra lia. Fa cies, 42: 25–34.
MANDIC O. and HARZHAUSER M. (2003) – Molluscs from the Badenian (Mid dle Mio cene) of the Gaindorf For ma tion (Al pine Molasse Ba sin, NE Aus tria) – Tax on omy, Paleoecology and Biostratigraphy. Ann. Naturhistor. Mus. Wien, 104A: 85–127.
MÍSAØ Z., DUDEK A., HAVLENA V. and WEISS. J. (1985) – Geologie ÈSSR, Èeský masív (in Czech). SPN Praha.
MURRAY J. (2006) – Ecol ogy and Ap pli ca tions of Ben thic Foraminifera.
Cam bridge Uni ver sity Press.
NEHYBA S. (1997) – Mio cene volcaniclastics of the Carpathian Foredeep in Czech Re pub lic. Vìstník Èeského Geologického Ústavu, 72 (4):
311–327.
NEHYBA S. (2000) – The cyclicity of Lower Mio cene de pos its of the SW part of the Carpathian Foredeep as the depositional re sponse to sed i - ment sup ply and sea-level changes. Geol. Carpath., 51 (1): 7–17.
NEHYBA S. and HLADILOVÁ Š. (2004) – Rel ics of the most dis tal part of the Neo gene fore land ba sin in SW Moravia. Bull. Geosc., 79:
113–120.
NEHYBA S. and ROETZEL R. (1999) – Lower Mio cene volcaniclastics in South west ern Moravia and Lower Aus tria. Jb. Geol. Bundesanstalt, 141 (4): 473–490.
NEHYBA S. and STRÁNÍK Z. (2005) – Vulkanoklastika v pavlovickém souvrství ždánické jednotky. Geologické výzkumy na Moravì a ve Slezsku v roce 2004, 12 (1): 37–41.
NEHYBA S., TOMANOVÁ-PETROVÁ P. and ZÁGORŠEK K. (2008) – Sedimentological and palaeocological re cords of the evo lu tion of the south west ern part of the Carpathian Foredeep (Czech Re pub lic) dur - ing the early Badenian. Geol. Quart., 52 (1): 45–60.
NEMEC W. (2005) – Prin ci ples of lithostratigraphic log ging and fa cies anal y ses. Institutt for geovitenskap, Universitat Bergen.
NOVÁK Z. (1975) – Spodnobadenské vápence karpatské pøedhlubnì. Un - pub lished PhD the sis. Fac ulty of Sci ence, Masaryk Uni ver sity Brno.
282 Kamil Zágoršek et al.
OTAVA J., ed. (1995) – Vysvìtlivky ke geologické mapì 1:50 000 list 24–21 Jevíèko. MS ÈGS.
PERYT D. and GEDL P. (2010) – Palaeoenvironmental changes pre ced ing the Mid dle Mio cene Badenian sa lin ity cri sis in the north ern Pol ish Carpathian Foredeep Ba sin (Borków Quarry) in ferred from foraminifers and dinoflagellate cysts. Geol. Quart., 54 (4): 487–508.
PICHA F. J., STRÁNÍK Z. and KREJÈÍ O. (2006) – Ge ol ogy and hy dro - car bon re sources of the Outer West ern Carpathians and their fore land, Czech Re pub lic. AAPG Mem., 84: 49–175.
PISERA A. and STUDENCKI W. (1989) – Mid dle Mio cene rhodoliths from the Korytnica ba sin (South ern Po land): environmenal sig nif i - cance and pa le on tol ogy. Acta Palaeont. Pol., 34: 179–209.
POLDERVAART A. (1950) – Sta tis ti cal stud ies of zir con as a cri te rion in granitization. Na ture, 165: 574–575.
POWERS M. C. (1982) – Com par i son chart for es ti mat ing round ness and sphe ric ity. AGI Data Sheet, 18.
PUPIN J. P. (1980) – Zir con and Gran ite Pe trol ogy. Contrib. Miner.
Petrol., 73: 207–220.
PUPIN J. P. (1985) – Mag matic zonic of Hercynian granitoids in France based on zir con typology. Schweiz. Miner. Petrogr. Mitt., 65: 29–56.
READING H. G., ed. (1996) – Sed i men tary en vi ron ments: pro cesses, fa - cies and stra tig ra phy. Blackwell Sci en tific Pub li ca tions, Ox ford.
REMEŠ M. (1933) – Dodatky ke geologické mapì okolí olomouckého a poznámky k nìkterým listùm sousedním. Zprávy Komitétu pro pøírodovìdné zkoumání Moravy, 12: 1–28.
RICHARDSON J. (1997) – Ecol ogy of ar tic u lated brachi o pods. In: Trea - tise on In ver te brate Pa le on tol ogy (ed. R. L. Kaesler), Part H.
Brachiopoda Re vised, 1: 441–462. Geo log i cal So ci ety of Amer ica and Uni ver sity of Kan sas, Boul der, Col o rado Law rence, Kan sas.
RÙŽIÈKA M., ed. (1995) – Vysvìtlivky ke geologické mapì 1:50 000 list 24–21 Olomouc. MS ÈGS. Praha.
SCHULTZ O. (2003) – The Mid dle Mio cene fish fauna (excl. otolithes) from Mühlbach am Manhartsberg and Grund near Hollabrunn, Lower Aus tria. Ann. Naturhist. Mus. Wien, 104A:185–193.
SCHWARZ R. (1946) – Pøíspìvek k poznání neogenu na listu Olomouc.
Vìstník Královské Èeské Spoleènosti Nauk, Tøída matematicko pøírodovìdná, 44: 1–20.
SHEVENELL A. E., KENNETT J. P. and LEA D. W. (2004) – Mid dle Mio - cene south ern ocean cool ing and Ant arc tic cryosphere ex pan sion. Sci - ence, 305 (5691): 1766–1770.
SPEZZAFERRI S. and ÆORIÆ S. (2001) – Ecol ogy of Karpatian (early Mio cene) foraminifers and cal car e ous nannoplankton from Laa an der Thaya, Lower Aus tria: a sta tis ti cal ap proach. Geol. Carpath., 52 (6):
361–374.
SPEZZAFERRI S., RÖGL F., CORIC S. and HOHENEGGER J. (2004) – Paleoenvironmental changes and ag glu ti nated foraminifera across the Karpatian/Badenian (Early/Mid dle Mio cene) bound ary in the Styrian Ba sin (Aus tria, Cen tral Paratethys). Grzybowski Found. Spec. Publ., 8: 423–459.
TUCKER M., ed. (1988) – Tech niques in Sedimentology. Blackwell Sci ence.
VYSLOUŽIL O. (1981) – Fauna spodního badenu na lokalitì Služín v karpatské pøedhlubní na Moravì. MS Mas ter The sis, MU Brno.
WALKER R. G. and JAMES N. P. (1992) – Fa cies mod els. Re sponse to sea level changes. Geo log i cal As so ci a tion Can ada.
WINCHESTER J. A. and FLOYD P. A. (1977) – Geo chem i cal dis crim i na - tion of dif fer ent magma se ries and their dif fer en ti a tion prod ucts us ing im mo bile el e ments. Chem. Geol., 20: 325–343.
ZÁGORŠEK K. (1993) – Changes in Bryozoa com mu nity in the Up per Eocene se quence of Mátyáshegy (Hun gary). Oeslenytáni Viták (Discussiones Paleontologicae), 39: 91–96.
ZÁGORŠEK K. (1996) – Paleoecology of the Eocene Bryo zoan Marl in the Al pine-Carpathian Re gion. In: Bryo zoans in Space and Time (eds.
D. P. Gordon et al.): 413–422. Na tional In sti tute of Wa ter and At mo - spheric Re search.
ZÁGORŠEK K. (2010a) – Bryozoa from the Langhian (Mio cene) of the Czech Re pub lic. Part I: Ge ol ogy of the stud ied sec tions, sys tem atic de - scrip tion of the or ders Cyclostomata, Ctenostomata and “Anascan”
Cheilostomata (Suborders Malacostega Levinsen, 1902 and Flustrina Smitt, 1868). Acta Mus. Nat. Pragae, Ser. B, Hist. Nat., 66 (1–2):
3–136.
ZÁGORŠEK K. (2010b) – Bryozoa from the Langhian (Mio cene) of the Czech Re pub lic. Part II: Sys tem atic de scrip tion of the suborder Ascophora Levinsen, 1909 and paleoecological re con struc tion of the stud ied paleoenvironment. Acta Mus. Nat. Pragae, Ser. B, Hist. Nat., 66 (3–4): 139–255.
ZÁGORŠEK K. and HOLCOVÁ K. (2009) – The old est Lower Badenian bryo zoan event in the Carpathian Foredeep from bore-holes in Pøemyslovice (PY-1 to PY-4). Pøírodovìdné studie Muzea Prostìjovska, 10–11: 171–182.
ZÁGORŠEK K. and VÁVRA N. (2000) – A new method for the ex trac tion of Bryo zoans from hard rocks from the Eocene of Aus tria. Jb. Geol.
Bundesanstalt, 142 (2): 249–258.
ZÁGORŠEK K., HOLCOVÁ K. and TØASOÒ T. (2008) – Bryo zoan event from Mid dle Mio cene (Early Badenian) lower neritic sed i ments from the lo cal ity Kralice nad Oslavou (Cen tral Paratethys, Moravian part of the Carpathian Foredeep). In ternat. J. Earth Sc., 97: 835–850.
ZÁGORŠEK K., HOLCOVÁ K., NEHYBA S., KROH A. and HLADILOVÁ Š. (2009) – The in ver te brate fauna of the Mid dle Mio - cene (Lower Badenian) sed i ments of Kralice nad Oslavou (Cen tral Paratethys, Moravian part of the Carpathian Foredeep). Bull. Geosc., 84 (3): 465–496.
ZAPLETAL J. (2004) – Con tri bu tion to paleogeographic evo lu tion of Lower Badenian sed i men ta tion in cen tral Moravia (Czech Re pub lic).
Scripta Fac. Sc. Nat. Univ. Masarykianae Brunensis, Ge ol ogy, 31–32:
87–98.
ZAPLETAL J., HLADILOVÁ Š. and DOLÁKOVÁ N. (2001) – Ma rine sed i ments of the Lower Badenian mar ginal fa cies in Olomouc. Scripta Fac. Sc. Nat. Univ. Masarykianae Brunensis, Ge ol ogy, 30: 75–86.
ZIMMERLE W. (1979) – Ac ces sory Zir con from Rhy o lite, Yel low stone Na tional Park (Wy o ming, U.S.A.). Z. dt. geol. Ges., 130: 361–369.
