Sedimentological and palaeocological records of the evolution of the southwestern part of the Carpathian Foredeep (Czech Republic) during the early Badenian

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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

Slavomír NEHYBA, Pavla TOMANOVÁ PETROVÁ and Kamil ZÁGORŠEK

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. Warszawa.

The depositional en vi ron ment of the south ern part of the Carpathian Foredeep in the Czech Re pub lic was stud ied in two bore holes us ing sedimentological and palaeontological meth ods. Eight lithofacies were re cog nised within cores of the early Badenian de pos its, com pris ing two fa cies as so ci a tions, namely de pos its of a coarse-grained Gilbert delta and off shore de pos its. As sem blages of foraminifers doc u ment the early Badenian (Mid dle Mio cene age). Two types of as sem blages were re cog nised: (1) pri mary taphocoenoses re flect ing the orig i nal en vi - ron ment of sed i men ta tion, i. e. a rel a tively deep sublittoral (circalittoral) en vi ron ment with low to nor mal ox y gen bot tom con di tions and deep-wa ter euryoxibiont foraminifers, nu mer ous plank tonic foraminifers, ag glu ti nated foraminifers and mixed as sem blages of deep- and shal low-wa ter foraminifers, (2) sec ond ary taphocoenoses of shal lower sublittoral (infralittoral) con di tion re de pos ited into the ba sin by grav ity cur rents. These as sem blages con tain shal low-wa ter foraminifers cou pled with an abun dant and di verse bryo zoan fauna.

Slavomír Nehyba, In sti tute of Geo log i cal Sci ences, Masaryk Uni ver sity, Kotláøská 2, 611 37 Brno, Czech Re pub lic, e-mail:

slavek@sci.muni.cz; Pavla Tomanová Petrová, Czech Geo log i cal Sur vey, Leitnerova 22, 658 69 Brno, Czech Re pub lic, e-mail:

petrova@cgu.cz; Kamil Zágoršek, Na tional Mu seum, Václavské nám. 68, 115 79 Praha, Czech Re pub lic, e-mail:

kamil.zagorsek@nm.cz (re ceived: April 2, 2007; ac cepted: Jan u ary 29, 2008).

Key words: Carpathian Foredeep, early Badenian, sedimentology, palaeo ec ol ogy, depositional en vi ron ment, foraminifers, bryo zoans.

INTRODUCTION

The tran si tion from the Early to the Mid Mio cene co in cides with a sig nif i cant sea level fall (Haq et al., 1988, Hardenbol et al., 1998), a chang ing tec tonic re gime in the Al pine-Carpathian realm (Kováè et al., 2007) while ex ten sive ma rine trans gres - sion fol lowed dur ing the early Mid Mio cene (the early Badenian). All these fac tors di rectly in flu enced the evo lu tion of bas ins in the fore land of the Al pine-Carpathian thrust wedge. Al though the rul ing fac tors of de po si tion and ba sin de - vel op ment are widely ac cepted for the broad area of the Cen tral Paratethys (Kováè, 2000) opin ions about the de vel op ment of Early to Mid Mio cene sed i men tary suc ces sions in two ad ja cent fore land bas ins i.e., the Carpathian Foredeep and the Al pine Molasse Zone dif fer substantially. Many au thors (Cicha, 1995, 2001; Švábenická and Ètyroká, 1998, 1999; Ètyroká and Švábenická, 2000; Rögl et al., 2002; Švábenická, 2002; Æoriæ, 2003; Æoriæ and Švábenická, 2004; Æoriæ and Rögl, 2004;

Æoriæ et al., 2004) have pub lished var i ous state ments about the

evo lu tion, biostratigraphy, and chronostratigraphic cor re la tion of the in di vid ual sed i men tary pack ages. The prin ci pal aim of this ar ti cle is to pro vide new data and in ter pre ta tions of the depositional en vi ron ment and of its evo lu tion within the stud - ied part of the Carpathian Foredeep dur ing the early Badenian.

GEOLOGICAL SETTINGS

The Carpathian Foredeep (CF) is a pe riph eral fore land ba - sin de vel oped on the Eu ro pean plate mar gin due to the West ern Carpathian accretionary wedge overthrust and deep subsurface load. The west ern part of the Carpathian Foredeep is lo cated on the east ern mar gin of the Variscan Bo he mian Mas sif. The part of the Carpathian Foredeep stud ied is filled with Neo gene clastic de pos its. The sed i men tary re cord started in the late Egerian/Eggenburgian (20.00 Ma) and ter mi nated by the early Badenian (15.97 Ma) sensu Gradstein et al., 2004. The cen tral Paratethys re gional stages and their com par i son with nanno - plankton NN zones are given in Fig ure 1.

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Five 3rd-or der depositional se quences were rec og nized within the Carpathian Foredeep sed i men tary infill (Nehyba and Šikula, 2007). The fifth, up per most se quence is early Badenian in age (16.5–15.97 Ma). Their de pos its are lo cated in the cen tral parts of the ba sin, with the max i mum thick ness (800 m) sit u ated al most sym met ri cally along the axis of the Carpathian Foredeep.

The pre served early Badenian de pos its rep re sent only an ero - sional relic of the orig i nal ba sin. Its orig i nal ex tent is partly re - flected by the oc cur rence of iso lated rel ics of ma rine de pos its lo - cated on the Bo he mian Mas sif (Hladilová et al., 1998; Nehyba and Hladilová, 2004) and by their char ac ter is tics. Two fa cies of early Badenian de pos its strongly pre dom i nate in the Carpathian Foredeep. Grav els, sandy grav els and grav elly sands rep re sent the first of these, as signed as “mar ginal or basinal clastics” ac - cord ing to their po si tion. Their max i mum thick ness is about 175 m, but the area of their oc cur rence is re stricted. Ac cord ing to Krystek (1974) they rep re sent beach de pos its, but Nehyba (2001) in ter preted them as de pos its of coarse-grained Gilbert del tas. The sec ond dom i nant fa cies con sists of dark green, green-grey or brown-grey cal car e ous pelites/mudstones, that vary in their con tent of silt and clay, shell de bris and in ten sity of bioturbation. They are tra di tion ally as signed as “tegel” and have been in ter preted as shal low-ma rine (shelf) to deep-wa ter de pos - its (bathyal; Brzobohatý, 1989). These mudstones are al most uni formly dis trib uted across the en tire depositional area with a max i mum thick ness of about 600 m. The ar eal and vol u met ric dis tri bu tion of all other fa cies (sands, red al gal lime stones, dis tal airfall tephra, etc.) is re stricted. There is a re mark ably low oc cur - rence/pres er va tion of coastal and shal low-ma rine fa cies within the area stud ied.

Tec tonic ac tiv ity and eustatic sea level change were the dom i nant rul ing fac tors of ba sin for ma tion and de po si tion dur - ing the late Karpatian and early Badenian (Nehyba and Šikula, 2007). Com pres sion of the Carpathian orogenic wedge ori -

ented to wards the NNW and NW changed its ori - en ta tion to wards the NNE and NE dur ing the late Karpatian and early Badenian (Kováè, 2000). This shift led to the dom i nant for ma tion of ac com mo da - tion space (flex ural sub si dence) in the north ern part of the CF whereas its south west ern part (the one stud ied) was af fected by rel a tive up lift. Older ba sin infills (pre dom i nantly Karpatian in age) were eroded and de formed. A lon gi tu di nal de pres sion along the ba sin axes (i.e. NE–SW di rec tion) was formed (an in cised val ley). This led to the for ma - tion of Gilbert del tas along the ba sin mar gin with basinward trans port di rec tion and sources from both op pos ing NW and SE mar gins. Fi nal flood ing of the “en tire” ba sin was dom i nated by de po si tion of basinal pelites (Nehyba, 2001). This pro cess was com bined with eustatic sea level change (TB 2.3 of Haq et al., 1988; CPC 3 of Kováè, 2000). Two early Badenian transgressive phases of sea level rise have been iden ti fied in the CF (Brzobohatý and Cicha, 1993) with the lat ter prob a bly the most ex - ten sive. Stepwise flood ing of the en tire Pannonian Ba sin Sys tem dur ing two early Badenian trans gres - sions have also been in ferred (Kováè et al., 2007).

Detailed cor re la tions of in di vid ual early Badenian beds within the Carpathian Foredeep and a widely ac cepted lithostratigraphy for them are still lacking.

METHODS OF STUDY

Early Badenian de pos its are gen er ally poorly ex posed in the Carpathian Foredeep. Two bore holes, Ivaò IK-1 and Vranovice VK-1, were newly drilled in South Moravia, the Czech Re pub lic (Fig. 2) by the Czech Geo log i cal Sur vey (Brno branch). The bore holes were sit u ated close to the con tact of Early and Mid Mio cene de pos its as in di cated by geo log i cal map ping. They reached a depth of 60 m and were fully cored.

De tailed de scrip tion of the cores al lows rec og ni tion of lithofacies and a gen eral rec og ni tion of fos sil con tent. La ser par ti cle size anal y sis (CILAS 1064 L) was used for the de scrip - tion of the grain-size dis tri bu tion of the mudstones. Sam ples for grain-size study were taken for anal y sis of fa cies dis tri bu tion within the pro file. At least two sam ples were taken from each 1 m in ter val and al to gether 211 sam ples were stud ied. Distiled wa ter and ul tra sonic tech nol ogy were used for sam ple prep a ra - tion. Me dian (P50) grain-size, con tent of clay and sand in the sam ples stud ied along the bore hole, pro files are shown in Fig u - res 3 and 4. Peb ble com po si tion (5 anal y ses) was stud ied in the

>4 mm frac tion. Fur ther data (5 anal y ses) were ob tained from the study of the 2–4 mm frac tion. Heavy min er als (11 anal y ses) were stud ied in the 0.063–0.125 mm frac tion.

For micropalaeontological stud ies the sed i ment was soaked in warm wa ter with so dium car bon ate for dissaggregation. It was washed un der run ning wa ter through 0.063 mm mesh sieves. Ap prox i mately 200 spec i mens of foraminifers were iden ti fied with a WILD bin oc u lar mi cro scope. The ra tio of planktonics (p)/benthics (b)was counted as a per cent age of

46 Slavomír Nehyba, Pavla Tomanová Petrová and Kamil Zágoršek

Fig. 1. Cor re la tion of the Early and Mid Mio cene with the Cen tral Paratethys stages by Cicha et al. (1998) and Gradstein et al. (2004), mod i fied

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plank tonic spec i mens in the as sem blage i. e., p/(p + b) ´ 100 in per cents. In to tal 56 foraminifer as sem blages were stud ied.

Bryo zoans were stud ied from 19 sam ples, where frag - ments of macrofossils were rec og nized. Sam ples were washed and sieved as de scribed by Zágoršek and Vávra (2000) on the min i mum 0.09 mm mesh. Se lected bryo zoans were cleaned us ing ul tra sonic treat ment and stud ied un der the scan ning elec tron microscop Jeol JSM 6400; all mea sure - ments were made by SemAfore 3.0 pro Jeol soft ware at the in - sti tute of Palae on tol ogy in Vi enna Uni ver sity.

FACIES ANALYSES

Eight lithofacies were re cog nised within the stud ied cores of early Badenian de pos its (Ta ble 1, Fig. 3). The oc cur rence of in di vid ual fa cies within the bore hole suc ces sion and their thick ness vari a tion are shown in Ta ble 2. The lithofacies were dis tin guished on the ba sis of de scrip tive sedimentological cri te - ria. The ter mi nol ogy used fol lows Collinson and Thomp son (1982). Lithofacies are con sid ered to be the ba sic “build ing blocks” of the sed i men tary suc ces sion (Walker, 1984; Ilgar and

Fig. 2. Lo ca tion of the Ivaò IK-1 and Vranovice VK-1 bore holes and the po si tion of the area studied within the Carpatho-Pannonian re gion

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Fig. 3. Se lected ex am ples of lithofacies of stud ied early Badenian de pos its

A — fa cies M1 — cal car e ous mas sive or hor i zon tal lam i nated mudstone; B — fa cies M2 — mudstone with ir reg u lar or cha otic bed ding, scat tered small peb bles and an gu lar intraclasts; C — fa cies M3 — cal car e ous clayey silt, mas sive or hor i zon tal lam i na tion, ad mix ture of fine to very fine sand; D — fa cies M4 — mudstone with abun dant shell de bris; E — fa cies M5 — cal car e ous mudstone, strongly bioturbated; F — fa cies Sf — fine to me dium sand mas sive, rarely hor i zon tal lam i na tion or flaser bed ding; G — fa cies Sg — me dium to coarse sand with scat tered gran ules or small peb bles; H — fa cies G — peb bly gravel or con glom er ate, lo cally pre served cross-bed ding

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Fig. 4. Lithological pro file of the IK-1 Ivaò bore hole, dis tri bu tion of se lected grain-size pa ram e ters, dis tri bu tion of fa cies and the ra tio of plank ton/benthos (foraminifers)

Lithofacies sym bols are ex plained in Ta ble 1

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Nemec, 2005). They are in di cated in the bore hole logs (Figs. 4 and 5) and serve as the ba sis for in ter pre ta tion of the depositional pro cesses. Based on spa tial group ing and dis tri bu - tion of lithofacies, two fa cies as so ci a tions/depositional en vi - ron ments were re cog nised i.e., de pos its of coarse-grained Gilbert del tas and off shore de pos its. These fa cies as so ci a tions are de scribed and in ter preted with ref er ence to depositional en - vi ron ment to gether with micropalaeontological data.

DEPOSITS OF A COARSE-GRAINED GILBERT DELTA This facies as so ci a tion is formed by lithofacies G and Sg typ i cally with a highly vari able con tent of peb bles and sand.

Lithofacies G was found only in the basal parts of bore hole IK-1. A char ac ter is tic fea ture of lithofacies G is a tran si tion from clast-sup ported tex ture to sandy ma trix-sup ported grav els and a lack of silt and clay within the sandy ma trix. Mudstone intraclasts oc cur rel a tively of ten and are sig nif i cantly larger than extraclasts. The av er age di am e ter of peb bles var ies within the beds be tween 0.5 to 1 cm. The larg est peb ble is about 6 cm in di am e ter. Peb bles are gen er ally rounded to subrounded, though no re stric tion of or mark edly higher oc cur rence of spe - cific peb ble shape in var i ous lo cal i ties or beds was re cog nised.

Grav els are polymict with a high con tent of car bon ate rocks (lime stones, dolomites — 44.6–49.3%), metamorphics (gneiss es, quartzites, phyllites, mica schists — 20.8–23.8%) and quartz (12.5–18.2%). Peb bles of cherts, sand stones and

Fa cies De scrip tion In ter pre ta tion

M1 Light grey, grey ish green cal car e ous silty clay or clayey silt, mas - sive or hor i zon tal lam i na tion. Oc cur rence of shell de bris is rare.

Al ter na tion of de po si tion from hemipelagic and hemiturbidite/

hyperpycnal flows (con cen trated sus pen sion). En vi ron ment hos tile to bur row ers. Deeper depositional en vi ron ment

(dis tant from clastic input).

M2

Green gray clay, ir reg u lar or cha otic bed ding with scat tered subangular or suboval clasts (quartz, granitoids, quartzites — di am e ter up to 1 cm) or an gu lar intraclasts and de formed laminas of grey mud, silt or sand. Rarely small ad mix ture of shell debris.

Tex tural in ver sion — mix ing of de pos its of sev eral depositional en vi - ron ments. Grav i ta tional de for ma tion, bioturbation?

M3

Light grey cal car e ous clayey silt. Mas sive, hor i zon tal lam i na tion, oc ca sion ally grad ing con nected with pres ence of fine to very fine

sand on the base. Usu ally sharp base and the top of beds.

Rapid de po si tion from con cen trated sus pen sion (hemiturbidite, dis tal tempestites, hyperpycnal cur rents). Al ter na tion of pe ri ods of de po si -

tion and erosion.

M4 Grey or light grey mudstone with abun dant shell de bris (molluscs, bryo zoans, rarely cor als). Oc cur rence of rounded clasts (mainly

quartz, max. 3 mm in di am e ter) is very rare.

Ero sion and redeposition of shells in coastal and shal low-ma rine en vi - ron ments and their trans port off shore (sus pen sion clouds — gravity

cur rents?, tempestites). Rapid de po si tion.

M5

Grey to green grey cal car e ous silty clay or clayey silt with subvertical bur rows filled by light grey to whit ish fine sand. Bed

thick ness var ies be tween 0.05 m to 0.4 m (av er age 0.3 m).

Con di tion suit able for bot tom col o ni za tion (sed i ment in put, time, ox y - gen con tent). Ben thic re work ing of fa cies M1–M4. Fa cies also re flect mas sive ero sion of sandy beds (sand pre served only within burrows).

Sf

Fine rarely fine to me dium sand mas sive, hor i zon tal lam i na tion or flaser bed ding. Form laminas or thin beds within fa cies M3 or M1. Sharp (of ten loaded) base, top sharp or grad ual. Beds are of -

ten de formed. Bed thick ness var ies be tween 0.01 m to 0.5 m (av er age 0.1 m).

Hyperpycnal or fine-grained tur bid ity cur rents.

Sg Coarse rarely me dium to coarse sand some times with scat tered gran ules or small quartz peb bles (up to 0.7 cm in di am e ter). Beds

are of ten de formed.

De po si tion from the grav ity cur rents (de bris flows, high den sity tur - bid ity cur rents — dis tal part of coarse-grained delta) or tempesites

(outer shelf). Sharp base re veal the ero sion prior to de po si tion.

G Peb bly gravel or con glom er ate, lo cally pre served cross-bed ding.

Typ i cal is var ied but gen er ally high con tent of coarse sand. De po si tion of high con cen tra tion grav ity cur rents, de po si tion con - nected with foresets of coarse-grained Gilbert delta.

T a b l e 1 De scrip tion and in ter pre ta tion of the lithofacies M1, M2, M3, M4, M5, Sf, Sg and G

M1 M2 M3 M4 M5 Sf Sg G

VK-1 61.2 % 4.4 % 11.2 % 12.3 % 6.4 % 2.3 %

Bed thick ness range

[m] 0.1–5.2 0.05–0.4 0.1–0.7 0.05–1.0 0.05–2 0.05–0.5

Av er age thick ness

[m] 0.5 0.1 0.2 0.3 0.3 0.1

IK-1 35.7 % 6.8 % 18.8 % 2.1 % 3.0 % 0.2 % 0.7 % 35.2 %

Bed thick ness range

[m] 0.1–1.1 0.05–0.2 0.1–1.0 0.2–0.6 0.2–0.4 0.05 0.05–0.2 0.55–1.9

Av er age thick ness

[m] 0.4 0.1 0.3 0.4 0.4 0.05 0.1 1.32

T a b l e 2 Oc cur rence of se lected lithofacies within the bore holes and their thick nesses

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Fig. 5. Lithological pro file of the VK-1 Vranovice bore hole, dis tri bu tion of se lected grain-size pa ram e ters, dis tri bu tion of fa cies and the ra tio plank ton/benthos (foraminifers)

Ex pla na tions as in Fig ure 4

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granitoids were also re cog nised. The pres ence of clasts of black coal (xylitic) was noted. The prom i nent struc tural fea ture of fa - cies G is cross-bed ding in ter preted as ev i dence of foresets. The fa cies is iden ti cal with that of early Badenian grav els de scribed in the broader area (Krystek, 1974) where foresets of coarse-grained Gilbert del tas can be ob served.

The com po si tion of the coars est frac tion in fa cies Sg is slightly dif fer ent to that of fa cies G. It is char ac ter ized by a higher con tent of quartz, a lower con tent of car bon ates and the pres ence of authigenic py rite. These dif fer ences can be mainly ex plained by the slightly dif fer ent grain-size frac tion but gen er - ally the same source of gran ules and peb bles can be sup posed.

Gar net typ i cally dom i nates in the trans par ent heavy min eral spec tra form ing 64.5–83.3%. The oc cur rence of other min er als (tour ma line, epidote, monazite, pyroxene, am phi bole, zir con, sillimanite, rutile, ti tan ite and staurolite) is usu ally low, only sev eral per cent ex cept for staurolite, which amounts to more than 10% in some sam ples. Small dif fer ences only in the trans - par ent heavy min eral spec tra (data from both fa cies Sg and Sf) con firm the com mon source of the de pos its. Fa cies Sg forms thin interbeds within the mudstones and its oc cur rence is in ter - preted as the most dis tal high den sity grav ity flows gen er ated on the delta slopes into the off shore depositional en vi ron ment.

A sharp con tact with the off shore de pos its in su per po si tion re veals the sud den drown ing of the delta front due to rapid rel a - tive sea level rise. Drown ing of the coarse-grained de pos its at the base of the early Badenian suc ces sion is widely re cog nised and con nected with the early Badenian trans gres sion (Brzobohatý and Cicha, 1993). De pos its of Gilbert del tas may rep re sent lowstand sys tems tracts and ma rine flood ing sur faces can be lo cated at their top.

OFFSHORE DEPOSITS

The off shore fa cies as so ci a tion strongly dom i nates within the suc ces sions and con sists of lithofacies: M1, M2, M3, M4, M5 and Sf. De po si tion of thick mudstone suc ces sions con tain - ing ma rine fos sils is usu ally as so ci ated with a pe lagic en vi ron - ment, deeper depositional set tings, steady-state style of de po si - tion and an im por tant role of sus pen sion fall out. The prin ci pal ques tion is how the coarser ma te rial was emplaced into this en - vi ron ment. In the sam ples stud ied, the ad mix ture of silt and sand forms fine hor i zon tal lam i na tion, nor mally graded beds, cha otic bed ding and tex tural in ver sion (lithofacies M2, M3, M4 and M5) or it forms lithofacies Sf it self.

Sands of lithofacies Sf are gen er ally well-sorted, form prob a - bly ex ten sive sheet-like beds a few centi metres thick, with sharp, of ten ero sional bases. Tops of the lay ers are of ten gradational, de formed and rarely sharp. The beds show pla nar par al lel lam i - na tion or cross-lam i na tion. Sand oc cur rences on the bases of mudstone beds are as so ci ated with nor mal grad ing (lithofacies M3). Graded laminae can re sult from nepheloid layer trans port, tails of tur bid ity cur rents and hemipelagites from outflowing river floods (Scott et al., 2004). Ero sional bases, nor mal grad ing, and pla nar par al lel and cross-lam i na tion, all give ev i dence for the role of low-den sity tur bid ity cur rents (Lowe, 1982). The sandy and silty interbeds with sharp bases and tops may be also

as so ci ated with the ac tiv ity of storms (Dott and Bour geois, 1982;

Ilgar and Nemec, 2005). The gen er a tion of some of these flows can be traced on the slopes of coarse-grained del tas, where they can be trig gered ep i sod i cally by hyperpycnal stream ef flu ent (Nemec, 1990, 1995).

Pre served sed i men tary struc tures in the off shore de pos its stud ied are con sis tent with in flu ence by den sity flows/grav ity cur rents. De po si tion from sed i ment grav ity cur rents typ i cally oc curs in an ep i sodic fash ion against back ground de po si tion.

This in ter pre ta tion is sup ported by palaeontological data, mainly by stud ies of foraminifers. Hor i zon tal lam i na tion can be con nected with a pulsed na ture of sed i men ta tion. A combination of high-en ergy ben thic hy dro dy nam ics and suf fi - cient fine sed i ment sup ply can re sult in ex ten sive grav - ity-driven flows. The source of the mud ma te rial may be con - nected with the ma rine dis persal of flu vial sed i ments (Rotondo and Bentley, 2004). Abun dant shell de bris (lithofacies M4) also sug gest ero sion in the coastal area. Alternation of clay and silt lay ers can be caused by seg re ga tion of silt and mud from bound ary shear pro cesses (Scott et al., 2004). Lithofacies M1, which plays a dom i nant role in the suc ces sion, re veals lit tle in - flu ence of grav ity cur rents due to its typ i cal mas sive fab ric.

Bi o log i cal/ben thic ac tiv ity also played an im por tant role in the dis tri bu tion and pres er va tion of sandy ma te rial within the off shore de pos its (M5). Sands are of ten pre served only as bur row infills. Ab sence of the sandy interbeds above and be - low lithofacies M5 may be as so ci ated with the ero sional ac tiv - ity of grav ity cur rents. Gra da tion of laminites into bioturbated beds may re flect low sed i men ta tion pe ri ods. The rare pres - ence of lithofacies M5 and Sf within the off shore as so ci a tion in bore hole IK-1 com pared to VK-1 may in di cate rel a tive deeper depositional.

Ver ti cal fa cies or ga ni za tion in the off shore suc ces sion has been eval u ated with the use of em bed ded Markov-chain anal y sis (Harper, 1984). A con ven tional chi-square test of dif fer ence ma - trix in di cates a rel a tively low value of “depositional ten dency”, which means that the fa cies suc ces sion can not be con sid ered to be “cy clic” in sto chas tic terms. How ever some pre ferred ver ti cal fa cies tran si tions/small cy cles can be re cog nised. The bases of the cy cles are formed by lithofacies M1 with thin interbeds of M2. The up per part of the cy cle is formed by lithofacies M3 or M4. Lithofacies M5 and Sf, which are rel a tively rare (see Ta - ble 2), were re cog nised ei ther above lithofacies M4 or M3 or di - rectly above lithofacies M1. These tran si tions in di cate ep i sod i - cally stron ger or weaker in flu ence of grav ity cur rents in the en vi - ron ment rel a tively dis tant from their source.

PALAEONTOLOGICAL DATA

Foraminifers were stud ied from the VK-1 Vranovice and IK-1 Ivaò bore holes (Tomanová-Petrová and Švábenická, 2007). Tests of foraminifers are well pre served in spite of be ing car ried in sus pen sion. The as sem blages of foraminifers from the IK-1 bore holes doc u ment a low-ox y gen sea-floor in a deeper sublittoral (circalittoral) en vi ron ment. The plank - ton/benthos ra tio ranges be tween 60–92% and usu ally reaches about 80% (Fig. 4). The char ac ter of foraminiferal as sem blages

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of bore hole VK-1, as well as the plank ton/benthos ra tio vary ing be tween 0.45–85.20%, rap idly change across the en tirely pro - file (Fig. 5). In an in ter nal of sev eral centi metres there were re - corded dis tinc tive di ver gences in the plank ton/benthos ra tio and in the to tal char ac ter of as sem blages. As sem blages of foraminifers are lo cally cou pled with bryo zoan col o nies of well-ox y gen ated warmer wa ters of nor mal sa lin ity of a shal low sea (infralittoral) with high wave en ergy, as sem blages of a low-ox y gen sea-floor of deeper sublittoral (circalittoral) con di - tions, as sem blages with nu mer ous ag glu ti nated foraminifers in di cat ing a deeper colder sea (circalittoral to prob a bly up per bathyal) of nor mal sa lin ity with out dysoxic in di ca tors (Kaiho, 1994) and mixed as sem blages of shal low-wa ter and deeper- wa ter ben thic foraminifers (see Fig. 6).

Bryo zoans were re corded only from bore hole VK-1. Al to - gether 56 spe cies have been rec og nized from 19 sam ples (the list of spe cies is given in Ta ble 3).

The dom i nant spe cies in the en tire as so ci a tion are cyclo - stome (Hornera and Polyascosoecia), which show the pi o - neer char ac ter of the as sem blage (Zágoršek et al., 2005). The av er age num ber of spe cies var ies from 20–25, ex cept sam ple from the 32 metres depth, where 34 spe cies were de ter mined.

On the other hand, there are sam ples, where less than 10 spe - cies oc cur. Ac cord ing to the spe cies dis tri bu tion and dis tri bu - tion of the growth forms (Hagemman et al., 1997) three groups can be dis tin guished. The first as so ci a tion (A) oc curs in the sam ples from 6.3 metres to 27.5 metres depth and is char ac ter ized by a dom i nance of erect rigid forms (the num - ber of spe cies of erect growth forms is about 10–15, other growth forms are rep re sented by less than 5 spe cies). The sec - ond as so ci a tion (B) is the best de vel oped one, while al most 35 spe cies be ing de ter mined in the sam ples from 32.0 and 35.0 metres. The third as so ci a tion (C), is the most poorly de vel - oped one, and less than 15 spe cies have been dis tin guished in the sam ples from 51.2 to 58.0 metres. Fig ure 7 shows the dis - tri bu tion of the taxa de ter mined in the sam ples stud ied. No bryo zoans have been found in the other sam ples. Char ac ter is - tic bryo zoans are shown in Fig ure 8.

INTERPRETATION OF THE DEPOSITIONAL ENVIRONMENT

Re sults of study of sed i men tary struc tures, fa cies, changes in con tent of de tri tal silt and sand, the ra tio of plank ton/benthos in the foraminiferal as sem blages, in ten sity of bioturbation, sup - posed oxicity dur ing de po si tion, and con tent of py rite all al - lowed an in ter pre ta tion of the evo lu tion of depositional en vi - ron ments and con di tions (Almon et al., 2004).

Three in ter vals can be re cog nised within the suc ces sion of bore hole VK-1 (Fig. 5). The ris ing con tent of silt and sand, oc - cur rence and thick ness of lithofacies M5 can be seen in the depth in ter nal from about 57 m to about 42 m (in ter val I). This can be ex plained by a rel a tive shallowing of depositional en vi - ron ment. The num ber of bryo zoan spe cies is very low, which in di cates a change able en vi ron ment in shal low wa ter with a high con tent of terrigenous ma te rial in the wa ter col umn (McKinney and Jack son, 1989). In ter val II be tween the depths

42 to 32 m re veal vari able con di tions that can be con nected gen er ally with rel a tive deep en ing. The most di verse bryo zoan as so ci a tion has been found in this in ter val, which in di cates deep en ing or the in tro duc tion of cold wa ter (Zágoršek, 1996).

In ter val III be tween the depths of 32 m and 10 m re veals fur ther rel a tive deep en ing of the depositional en vi ron ment which can be ob served in the ris ing con tent of clay, de cline in the me dian grain-size, low oc cur rence of lithofacies M5, Sf and sand.

Bryo zoans are com mon in this in ter val and dom i nated by cyclostome gen era, which in di cates a chang ing en vi ron ment in a deep en ing ba sin and slope unstability (McKinney and Jack - son, 1989).

The foraminifers Praeorbulina sicana (de Stef.) and Praeorbulina glomerosa circularis (Blow) doc u ment the Mid - dle Mio cene, M5b Zone of plank tonic foraminifers sensu Berggren et al. (1995) that is cor re lated with the lower Badenian in Cen tral Paratethys re gional stages. From the palaeontological point of view we can see some trends in the trend of the ra tio of plank ton/benthos cou pled with the trend of oc cur rence of bryo zoans. 4 types of as sem blages were dis tin - guished: (1) mixed shal low-wa ter as sem blages with Asterigerinata planorbis (d`Orb.) and Amphistegina mammilla (Ficht.-Moll.) and deep-wa ter as sem blages with Melonis pompilioides (Ficht.-Moll.) and Pullenia bulloides (d`Orb.) ben thic foraminifers from the depths 4.6 m, 31.6 m and 46.45 m (VK-1; Fig. 6C); (2) dom i nance of plank tonic foraminifers (pre dom i nance of pyritized tests) ac com pa nied by Siphono - dosaria div. sp., Bolivina div. sp., Pyramidulina raphanistrum (L.) and Uvigerina div. sp. re flect ing a lower ox y gen sup ply in bot tom wa ter from the depths 6.1 m, 21.9 m, 22.2 m, 23.6 m, 30.55 m, 52.8 m (VK-1; Fig. 6D); (3) higher num bers of ag glu - ti nated foraminifers Semivulvulina pectinata (Rss.), S.

deperdita (dÒrb.), Textularia gramen dÒrb., T. pala Czjzk., Spirorutilus carinatus (dÒrb.) ac com pa nied by cal car e ous benthos with Melonis pompilioides, Pullenia bulloides and Heterolepa dutemplei (dÒrb.) at the depths 36.8 m, 37.2 m, 39.2 m, 47.5 m and 49.4 m (VK-1; Fig. 6E) in di cate colder wa - ters; (4) dom i nance of deep-wa ter euryoxybiont foraminifers Uvigerina macrocarinata Papp and Turn., U. semiornata dÒrb., Pappina breviformis (Papp and Turn.), Bolivina div.

sp., Bulimina div. sp., ac com pa nied by the deep-wa ter spe cies Melonis pompilioides and Pullenia bulloides, a higher num ber of plank tonic foraminifers, and by pyritized centric di a toms at the depths 5.4 m, 12.2 m, 21.9 m, 24.55 m, 24.7 m, 29.65 m, 49.2 m, 57.2 m, 57.8 m, 59.9 m, 60.0 m in di cates a low-ox y gen sea-floor, in deeper sublittoral en vi ron ments. We sup pose that these as sem blages rep re sent pri mary taphocoenoses and they doc u ment orig i nal en vi ron ment of sed i men ta tion.

On the other hand, the as sem blages from the depths 6.3 m, 12.6 m, 14.4 m, 39.8 m, 40.05 m, 52.2 m and 52.95 m with Amphistegina mammilla (Ficht. and Moll), Asterigerinata planorbis (dÒrb.), Am mo nia viennensis (dÒrb.) and also Semilvulina deperdita (dÒrb.) in di cate a shal low-wa ter depositional en vi ron ment and they may doc u ment non in situ as sem blages. The bryo zoans are highly di verse, the best sam ple be ing from the depth 35.0 m, where 34 spe cies were de ter - mined. The dom i nant spe cies are cheilostome, of the ge nus Reteporella, which lived in in ner shelf to outer shelf en vi ron - ments in high en ergy wa ter (Hageman et al., 1997).

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Fig. 6. Typ i cal as sem blages of the foraminifers in the VK-1 Vranovice and IK-1 Ivaò bore holes

Pri mary taphocoenoses: A — deep-wa ter as sem blage with dom i nance of plank tonic and euroxybiont foraminifers (IK-1; 12.55 m); B — deep-wa ter as - sem blage with globigerinas, globigerinoides and Melonis pompilioides (Ficht. and Moll), (IK-1; 46.95 m); C — as sem blage doc u ment ing mix ing of shal - low-wa ter and deep-wa ter as sem blages (VK-1; 4.6 m); D — deep-wa ter as sem blage with nu mer ous plank tonic spe cies and Siphonodosaria div. sp.

(VK-1; 6.1 m); E — as sem blage with nu mer ous ag glu ti nated spe cies (VK-1; 37.2 m); sec ond ary taphocoenoses: F — shal low-wa ter as sem blage with Amphistegina mammilla (Ficht. and Moll) and Asterigerinata planorbis (d`Orb.) (VK-1; 40.05 m)

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TAXA/depth of

bore hole [m] 6.3 6.4 7.0 12.5 12.6 16.8 26.5 27.5 28.8 29.7 30.7 31.5 32.0 35.0 51.2 51.4 51.9 54.8 58.0

Adeona sp.n. * * * * * *

Adeonella

polystomella * * * * * * * * * * * * * * *

Adeonellopsis

coscinophora * * * *

Bicrisina compressa * * * *

Callopra bobiesi * *

Cellaria fistulosa * * * * * * * * *

Cellaria

salicornoides * * * * *

Cellepora

globularis * *

Celleporaria

palmata *

Celleporina costazi * * * * * * * *

Ceriopora indet. * * * *

Cribellopora *

Crisia cf. leicointrei *

Crisia eburnea * * * *

Crisia haueri * *

Crisia hoernesi * * * * * * * * * *

Crisidmonea

foraminosa * * * * * * * * *

Diplosolen obelium * *

Exidmonea atlantica * * * * * * * * * * * * *

Exochella (?) new

ge nus * * * * * * * * * *

Frondipora

verrucosa * *

Hippopleurifera

hypsostoma *

Hornera cf.

simplicissima * *

Hornera

frondiculata * * * * * * * * * * * * * * * * * * *

Hornera striata * * * * * * * * * * *

Hornera verrucosa * * * * * *

Idmidronea

coronopus * * *

Iodictyum rubeschi * *

Margaretta

cereoides * * * * *

Mecynoecia

proboscidea *

Mecynoecia

pulchella * * * * * * * * * * * * * * * *

Metrarabdotos

mallecki * * * * * * * * * * * * *

Micropora

parvicella *

Monoporella

venusta * *

Myriapora truncata *

Oncousoecia biloba *

Onychocella * *

Pleuronea pertusa * * * * * * * * * * * * * *

Polyascosoecia

coronopus * * * * * * * * * * * * * * * * *

T a b l e 3 The list of all spe cies of bryo zoans in the VK-1 Vranovice bore hole

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TAXA/depth of

bore hole [m] 6.3 6.4 7.0 12.5 12.6 16.8 26.5 27.5 28.8 29.7 30.7 31.5 32.0 35.0 51.2 51.4 51.9 54.8 58.0

Porella cf. nuda * *

Pseudofrondipora

foramninosa * * * * *

Reteporella

beaniana * * * * * * * * * * * * *

Reteporella

cellulosa * * * * * * *

Reteporella

septentrionalis * * *

Reussirella

haidingeri * * * * * * *

Schizobrachiella (?) * *

Schizomavella

tenella * *

Schizoporella

geminipora * * *

Schizostomella

grinzingensis *

Smittina cervicornis * * *

Steginoporella

cuculata * * * * * * * *

Teichopora cf.

clavata * * * *

Tubulipora

dimidiata * * * * *

Turbicellepora

coronopus * * * * *

Umbonula

endlicheri *

Ybselosoecia typica * * * * * * * *

to tal num ber

of taxa 56 24 22 18 23 17 19 21 22 4 12 10 10 23 34 9 8 12 11 11

Tab. 3 cont.

Fig. 7. Dis tri bu tion of the de ter mined taxa of bryo zoans and se lected bryo zoan as so ci a tions (A, B, C) in the VK-1 Vranovice bore hole

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Four in ter vals can be re cog nised within the suc ces sion of bore hole IK-1 (Fig. 4). A ris ing con tent of clay, a de cline in me dian grain-size and in sand con tent, rapid al ter na tion from the fa cies as so ci a tion of a coarse-grained Gilbert delta to off - shore fa cies can be traced from the base of the pro file to the depth of about 39 m (in ter val I). This re flects a dra matic and con tin u ous deep en ing of the depositional en vi ron ment. In ter - val II be tween the depths of 39 and 27 m re veals var ied con di - tions with pos si ble rel a tive shallowing. In ter val III be tween the depths of 27 and 20 m re veals rel a tive deep en ing of the depositional en vi ron ment and the top in ter val IV be tween the depths of 20 to 10 m re flects var ied con di tions with pos si ble shallowing. Ini tial deep en ing and fi nal shallowing are also seen in the trend of plank ton/benthos (Fig. 3). The pos si ble in ter pre -

ta tion of these in ter vals within the con text of se quence stra tig - ra phy (TST, late TST, early HST, parasequences see Al mond et al., 2004) needs fur ther study in the broader con text. The foraminiferal as sem blages from the depths 12.47 m, 12.55 m, 20.05 m, 20.35 m, 23.9 m, 27.3 m, 34.2 m, 34.3 m, 34.8 m, 46.2 m, 46.7 m, 46.95 m, 47.1 m and 48.0 m are dom i nated by the deep-wa ter foraminifers Melonis pompilioides and Pullenia bulloides ac com pa nied by Siphonodosaria div. sp. and the euryoxybiont taxa Uvigerina div. sp., Bolivina div. sp., Bulimina div. sp. in di cat ing a low-ox y gen sea-floor of deeper sublittoral (circalittoral) con di tions sensu Kaiho (1994), and also a higher num ber of plank tonic foraminifers.

Fig. 8. Char ac ter is tic bryo zoan spe cies from the VK-21 Vranovice bore hole

A — erect rigid growth form of Steginoporella cucullata, which usu ally in di cates a trop i cal en vi ron ment, scale bar 100 µm; B — mas sive erect rigid Crisidmonea foraminosa, very com mon in the “B” as so ci a tion, scale bar 1 mm; C — frag ment of glob u lar free-liv ing Reussirella haidingeri, in di cat ing hard sea bot tom, scale bar 1 mm; D — Polyascosoecia coronopus, one of the com mon est bryo zoans from bore hole VK-1 Vranovice, here with de vel oped ovicell, scale bar 1 mm; E — Hornera frondiculata, one of the com mon est bryo zoans from the bore hole VK-1 Vranovice; F — Reteporella septentrionalis, char ac ter is tic rep re sen ta tive of reteporidea growth form in di cat ing tur bu lent wa ter, scale bar 100 µm

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DISCUSSION

De pos its of coarse-grained Gilbert del tas re veal the ex is - tence of prom i nent re lief and in cised val leys (Nehyba and Šikula, 2007). The localised po si tion of these de pos its, their con sid er able thick ness, vari a tions in their prov e nance, and abun dant oc cur rence of large intraclasts of older ba sin infill (Nehyba, 2006; Nehyba et al., 2006) all point to ex is tence of the val leys ori ented gen er ally per pen dic u lar to the ba sin axis (Dvoøák, 1995), which rep re sented im por tant sources of sed i - ment in put. De pos its close to the en try point into the ba sin were coarse-grained, while de pos its far ther away were mainly fine-grained (pelagic and hemipelagic sedimentation).

When rel a tive sea level rose, the Gilbert del tas and the val - leys were flooded, which led to ma rine in cur sion deep into the fore land (Hladilová et al., 1998), change in the flu vial style and re duc tion of the coarse-grained in put into the ba sin (Zaitlin et al., 1994). Ac cord ing to a palaeobathymetrical study (Brzobohatý, 1997) the cen tral parts of the ba sin were rel a - tively deep and the palaeodepth can reach more than 400 m.

Ma rine dis persal of flu vial sed i ments is di rected by sev eral pro cesses. Coarse sed i ment is de pos ited near the river mouth, whereas fine silts and clays can be trans ported fur ther sea ward in ei ther pos i tively (hypopycnal) or neg a tively (hyperpycnal) buoy ant plume. Fluid muds (high con cen tra tion near-bed sus - pen sions of fine-grained sed i ments) have been ob served in many estuarine, coastal and shelf en vi ron ments. The regime of the ba sin, es pe cially wave-cur rents, resuspensation and trans - port in the wa ter col umn (auto-sus pen sion of grav ity flow, loft - ing) can fur ther dis perse fine ma te rial along the ba sin (Rotondo and Bentley, 2004; Soyinka and Slatt, 2004, Tripsanas et al., 2004). Tests of foraminifers and frag ments of bryo zoans can be trans ported within these grav ity flows. Ris ing sea level and cli - ma tic changes may have also nar rowed the shelf area and af - fected the in flux of sed i ments into the river systems (Emmery and Myers, 1996).

The re sults given sug gest pos si bil i ties for the sub di vi sion of the “mo not o nous” pile of early Badenian basinal pelites (“tegel”) into seg ments with dis tinct po si tions within cy cles of rel a tive sea level change. This is cru cial for the ap pli ca tion of

high-res o lu tion se quence stra tig ra phy. More over the pres ence of tegel intraclasts within the de pos its of coarse-grained Gilbert del tas has re cently been re cog nised (Nehyba et al., 2006). Elu - ci da tion of the fa cies ar chi tec ture of the var ied seg ments of the ba sin infill can pro vide im por tant re sults for se quence stra tig ra - phy and lithostratigraphy.

CONCLUSIONS

Eight lithofacies have been re cog nised within cores of early Badenian de pos its and these form two fa cies as so ci a tions i.e., de pos its of a coarse-grained Gilbert delta and off shore de pos its.

The fa cies as so ci a tion of a coarse-grained Gilbert delta is framed by lithofacies G and Sg. A sharp con tact with over ly ing off shore de pos its re veals the sud den drown ing of the delta front due to rapid sea level rise. Off shore de pos its strongly pre dom i - nate in the sed i men tary suc ces sions stud ied and con sist of fa - cies M1, M2, M3, M4, M5 and Sf. The in flu ence of grav ity cur - rents on their de po si tion is sup ported by pre served sed i men tary struc tures and micropalaeontological data. Pri mary taphocoenoses of foraminifers were dis tin guished show ing an off shore en vi ron ment of sed i men ta tion, i.e. a deeper sublittoral en vi ron ment with low to nor mal ox y gen bot tom con di tions and sec ond ary taphocoenoses con tain ing foraminifers and nu mer - ous and di verse bryo zoans, doc u ment ing de pos its of a shal - lower sublittoral en vi ron ment re de pos ited into the ba sin by grav ity cur rents.

Ac knowl edge ments. This work was kindly sup ported by the Grant Agency of the Czech Re pub lic (pro ject No.

205/04/2142 “Eval u a tion of sed i ments on the Karpa - tian-Badenian bound ary in the south ern part of the Carpathian Foredeep”, pro ject leader Pavla Tomanová Petrová and 205/06/0637 “Mio cene Bryo zoan Event”, pro ject leader Kamil Zágoršek) and by the Re search Pro ject MSM 0021622412. We thank Dr. A. Wysocka and an anon y mous re viewer for their con struc tive re vi sion and com ments on ear - lier drafts of this pa per.

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