Eustatic and tec tonic con tr ol on late Eocen e fan … et al 2012.pdfRastislav Vojtko , De part men t of Ge ol ogy and Palae on tol ogy, Fac ul ty of Nat u ral Sci enc es, Comeni

Geo log i cal Quar terly, 2012, 56 (1): 67–84

Eustatic and tec tonic con trol on late Eocene fan delta de vel op ment(Orava Ba sin, Cen tral West ern Carpathians)

Dušan STAREK, Ľubomír SLIVA and Rastislav VOJTKO

Starek D., Sliva Ľ. and Vojtko R. (2012) – Eustatic and tec tonic con trol on late Eocene fan delta de vel op ment (Orava Ba sin, Cen tralWest ern Carpathians). Geol. Quart., 56 (1): 67–84.

The evo lu tion of the Cen tral Carpathian Paleogene Ba sin (CCPB) re flects an im por tant role of rel a tive sea level changes on a tec toni cally ac tive ba sin mar gin. Af ter the ini tial up per Lutetian/Bartonian trans gres sion, the next re gres sive-transgressive cy cle played a key role ina for ma tion of the late Eocene fan delta fa cies as so ci a tions in the south ern Orava re gion of North ern Slovakia. De tailed sed i men tary anal -y sis al lowed the sep a ra tion of the fol low ing three fa cies as so ci a tions which rep re sent dis tinct depositional en vi ron ments: al lu vial fan(subaerial fan delta; Unit 1); sub aque ous fan delta (Unit 2); and prodelta/slope and ba sin (Unit 3). The first stage of delta de vel op ment iscon nected with eustatic sea level fall at the Bartonian/Priabonian bound ary, ac com pa nied by subaerial ex po sure, flu vial in ci sion and de -po si tion of al lu vial fan sed i ments. Subaerial de po si tion was char ac ter ized by a va ri ety of mass flow con glom er ates with a red muddy ma -trix, interfingering with stream or sheetflood de pos its. The next stage of the delta cor re sponds to high-am pli tude trans gres sion re lated torapid tec tonic sub si dence along the CCPB mar gins dur ing the Priabonian. The ver ti cal ar range ment of fa cies sug gests ret ro grade deltade vel op ment that shows rapid sub mer gence of the subaerial parts and onlap of sub aque ous mass flow con glom er ates, of ten re worked bywaves or wave-in duced shal low-ma rine cur rents. Con tin u ous deep en ing of the depositional en vi ron ment dur ing the latePriabonian/early Rupelian led to the rel a tively rapid su per po si tion of prodelta/slope and ba sin fa cies as so ci a tions by slowly ac cu mu latedhemipelagic deposis.

Dušan Starek, Geo log i cal In sti tute, Slo vak Acad emy of Sci ences, Dúbravská cesta 9, 841-04 Bratislava, Slovakia, e-mail:[email protected]; Ľubomír Sliva, NAFTA a.s., Votrubova 1, 821-09 Bratislava, Slovakia, e-mail: [email protected];Rastislav Vojtko, De part ment of Ge ol ogy and Palae on tol ogy, Fac ulty of Nat u ral Sci ences, Comenius Uni ver sity, Mlynská dol ina G,842-15 Bratislava, Slovakia, e-mail: [email protected] (re ceived: June 3, 2011; ac cepted: De cem ber 12, 2011).

Key words: Paleogene, Orava, West ern Carpathians, fan delta, mass flow de pos its, coarse-grained delta.

INTRODUCTION

Fa cies as so ci a tions of al lu vial fan del tas (sensu Nemec,1990a) can pre serve de tailed strati graphic re cords and pro -cesses at ba sin mar gins. The term “fan delta” de notescoarse-grained del tas, typ i cally fed by al lu vial fan feed ers, de -vel oped along steep top o graphic gra di ents where al lu vial fanshave prograded di rectly into a stand ing body of wa ter(McPherson et al., 1987; Nemec, 1990b). Fan del tas there forerep re sent the in ter ac tion be tween sed i ment-laden al lu vial fansand ma rine or lac us trine pro cesses (Nemec and Steel, 1988).Delta styles and ar chi tec ture are mainly con trolled by tec tonicmove ment (e.g., Gordon and Bridge, 1987; Dabrio, 1990;Frostick and Steel, 1993); sea level fluc tu a tion (e.g.,Posamentier and Vail, 1988; Gal lo way, 1989; van Wag oner etal., 1990; Bardaji et al., 1990; Dart et al., 1994; Postma, 1995),

and cli ma te change (Monecke et al., 2001; Postma, 2001; Deband Chaudhuri, 2007).

This pa per de scribes sedimentological stud ies of thecoarse-grained se quences which are well-known from out crops in the south ern Orava re gion of Slovakia and which form partof the Cen tral Carpathian Paleogene Ba sin fill. These se -quences which were named the Pucov con glom er ates (Gross etal., 1982), and later cat e go rized as the Pucov Mem ber (Gross et al., 1984); they have been stud ied by sev eral au thors (Bieda,1957; Maheľ et al., 1964; Andrusov, 1965; Gross et al., 1982).The lat est, gen er ally ac cepted in ter pre ta tion of the Pucov Mem -ber is con nected with deep ma rine can yons and fans (Gross etal., 1982, 1993). The aim of this pa per is the sedimentologicalre in ter pre ta tion of the Pucov Mem ber based on new field ob -ser va tions. Herein, we pres ent a new al lu vial and fan deltadepositional model, where the de po si tion was con trolled byboth eustatic changes and tec ton ics. Sed i men ta tion was mainlyin flu enced by a re gres sive-transgressive cy cle in the late

Bartonian to early Priabonian pe riod. The sed i men tary fa ciessug gests deltaic subaerial to sub aque ous mass-flow de po si tion, wave-re work ing, and de po si tion by hyperpycnal andhypopycnal flows on the delta slope and in the prodelta andbasinal en vi ron ments.

GEOLOGICAL SETTING

The CCPB lies within the West ern Carpathian Moun tainchain (Fig. 1A) and it de vel oped in the basinal sys tem of thePeri- and Paratethys. The ba sin ac com mo dated a forearc po si -

tion on the de struc tive Al pine–Carpathian–Panonnian(ALCAPA) microplate mar gin and at the hin ter land of theOuter West ern Carpathian accretionary prism (Soták et al.,2001). The ba sin is mainly filled with flysch-like de pos its witha thick ness of up to a thou sand metres and they over lap thePalaeoalpine, pre-Senonian nappe struc ture. The age of thesed i men tary fill ranges from Bartonian (e.g., Sam uel andFusán, 1992; Gross et al., 1993) to lat est Oligocene (cf. Soták et al., 1996, 2001, 2007; Soták, 1998; Olszewska and Wieczorek,1998; Gedl, 2000).

The de pos its of the CCPB are pre served in many struc turalsub-bas ins (Fig. 1B), in clud ing the Žilina, Rajec, Turiec,Orava, Liptov, Podhale, Poprad and Hornád de pres sions. The

68 Dušan Starek, Ľubomír Sliva and Rastislav Vojtko

Fig. 1A – lo ca tion of study area within the Al pine-Carpathian orogen; B – Cen tral Carpathian Paleogene Ba sin sys tem with struc turalsub-bas ins, base ment and sur round ing units; C – geo log i cal sketch of the Orava re gion (af ter Gross et al., 1993; Biely et al., 1996, mod i fied)

C – lo ca tion of stud ied sec tions: a – N 49°13’14’’, E 19°22’17’’; b – N 49°13’5’’, E 19°21’18’’; c – N 49°12’8’’, E 19°19’9’’; d – N 49°15’14’’, E 19°9’43’’; e – N 49°15’12’’, E 19°9’57’’; f – N 49°15’12’’, E 19°10’11’’

CCPB sed i ments in the study area are bounded by thePalaeoalpine late Pa leo zoic to Me so zoic units in the south,while the north ern bound ary is rep re sented by the PieninyKlippen Belt (Fig. 1) which rep re sents a transpressionalstrike-slip shear zone re lated to a plate bound ary (Csontos etal., 1992; Ratschbacher et al., 1993; Csontos, 1995; Potfaj,1998). The CCPB was formed on the up per plate above thesubducting oce anic slab at tached to the Eu ro pean Plat form(e.g., Royden and Baldi, 1988).

The CCPB de pos its are com monly di vided into fourlithostratigraphic for ma tions (Gross et al., 1984; Fig. 2A). The

low er most, Borové For ma tion con sists of basal ter res trial de -pos its linked to al lu vial fan and flu vial sys tems (Marshalko,1970; Baráth and Kováè, 1995; Filo and Siráòová, 1998) andshal low-ma rine transgressive de pos its (Kulka, 1985; Gross etal., 1993; Filo and Siráòová, 1996; Bartholdy et al., 1999). This for ma tion is over lain by the Huty For ma tion, which mainly em -braces var i ous mud-rich, deep ma rine de pos its (e.g., Janoèkoand Jacko, 1999; Soták et al., 2001; Starek et al., 2004). Theover ly ing Zuberec and Biely Potok for ma tions are com posedof fa cies as so ci a tions of sand-rich sub ma rine fans (Soták,1998; Janoèko et al., 1998; Starek et al., 2000; Starek, 2001;

Eustatic and tectonic control on late Eocene fan delta development (Orava Basin, Central Western Carpathians) 69

Fig. 2A – de scrip tive lithostratigraphy of the CCPB; no men cla ture of the for ma tions ac cord ing to Gross et al. (1984, adapted); biostratigraphy isbased on the data pub lished by Olszewska and Wieczorek (1998), Starek et al. (2000), Starek (2001), and Soták et al. (2001, 2007); B – rep re sen ta -tive logs of al lu vial fan delta de pos its (a, b – Pucov sites; c – Medzihradné site; d–f – Èremoš sites); for map lo ca tion and GPS po si tion data see Fig -ure 1C; C – rep re sen ta tive frag ment of the in di vid ual fa cies as so ci a tions

For more de tails see Fig ures 3, 4, 7

Soták et al., 2001). The Pucov Mem ber in the Orava Ba sin isgen er ally in cised into the Borové For ma tion and Me so zoicbase ment. It is over lain by the Huty For ma tion and even tu allyits de po si tion dis ap pears in the low er most part of Huty For ma -tion (Gross et al., 1982). Nev er the less, the def i ni tion of thePucov Mem ber de pos its (sensu Gross et al., 1984) is un der -stood to be a lithotype rep re sent ing coarse-grained in put to thedeeper parts of the ba sin and oc cur ring in all lithostratigraphicfor ma tions. It ex ists in al most all re gions of the CCPB.

The con glom er ates of the Pucov Mem ber have their mainout crops near the village of Pucov and these have been in ter -preted in sev eral ways. Orig i nally, they were re garded as“basal” transgressive lithofacies (Bieda, 1957; Maheľ et al.,1964; Andrusov, 1965), but Gross et al. (1982) later showedthat this coarse-grained se quence is not a basal com po nent ofthe transgressive suc ces sion – the Borové For ma tion (cf., Gross et al., 1984). They were con sid ered to be con glom er ates trans -ported by can yons of sub ma rine val leys 5–10 km to wards thenorth where the sed i ments formed a 210–270 m thick sub ma -rine fan (Gross et al., 1982, 1993).

The con glom er ates stud ied oc cur at sev eral sites in theOrava Ba sin. How ever, only six ex po sures were ap pli ca ble tothis study be cause of the poor ex po sure (Fig. 1C). The mostcom plex data are de rived from a more than 250 m thick sed i -men tary suc ces sion near Pucov. The con glom er ates are ex -posed in cliffs 150 m high. The low er most part of the suc ces -sion was doc u mented by an ex plo ra tion bore hole (Gross,1979). The sed i men tary se quence at the bot tom be gins withred dish mas sive boul der-size con glom er ates which are themost abun dant de pos its at the Pucov sec tion (Fig. 2B, sec -tion a). The red dish col our dis ap pears grad u ally at higher lev -els, where sand stone and finer con glom er atic beds start to oc -cur. The up per most part of the Pucov sec tion mainly con sists of siltstone, marlstone, and sand stones with scarce, iso lated con -glom er atic beds. This is re ferred to as the Huty For ma tion(sensu Gross et al., 1993), and more pre cisely to theGlobigerina and Submenilite beds (cf. Soták et al., 2007).

No biostratigraphical data could be ob tained from the mas -sive con glom er ates. How ever, the late Bartonian to earlyPriabonian time span of the de po si tion has been de ter minedfrom their po si tion above the Bartonian Num mu lit ic lime stones of the Borové For ma tion (Bieda, 1957; Sam uel and Salaj,1968; Gross et al., 1984, 1993) and from the first oc cur rence ofthe lower Priabonian (Zone P 15) fossiliferous marls in the up -per most part of the con glom er atic suc ces sion (Soták et al.,2007; Soták, 2010).

RESULTS

SEDIMENTARY FACIES

The clas si fi ca tion is mainly based on de scrip tive pa ram e -ters such as grain-size, round ing, sort ing and grain fab ric, sup -ple mented by other pa ram e ters in clud ing sed i men tary struc -tures, shape, oc cur rence of biogenic re mains and bioturbationstruc tures. Herein, grain-size and tex tural clas si fi ca tion wasused ac cord ing to Blair and McPherson (1999). The

coarse-grained fa cies eval u ated show wide vari a tion in theirround ness and here the stan dard in dex of Pow ers (1953) wasap plied. The de pos its that com prise ex clu sively, or mostly,very an gu lar to subangular clasts are termed brec cias (Fa ciesB1, B2). Those that con sist of subrounded to well-roundedclasts are re ferred to as con glom er ates (Fa cies C). The sand -stones are re ferred to as Fa cies S and mudstones/marlstones asFa cies M. Al though the fa cies are also eval u ated by ma trix col -our, as in red dish and grey con glom er ates, dif fer ences be tweenma trix colours are not used as pa ram e ters to di vide the sep a ratefa cies. Herein, 13 in di vid ual fa cies with their pos si ble hy dro dy -namic in ter pre ta tion were dis tin guished, as de picted in Ta ble 1.

The oc cur rence and ar range ment of fa cies de fined in ver ti -cal suc ces sion al lowed as to sep a rate the fol low ing three mainunits (Fig. 2C) that rep re sent fa cies as so ci a tions, spe cific of dis -tinct depositional en vi ron ments.

FACIES ASSOCIATION OF UNIT 1

De scrip tion: the de pos its of Unit 1 are gen er ally thick-bed -ded, mas sive, un sorted or poorly sorted ma trix- to clast-sup -ported con glom er ates of Fa cies C (Fig. 3B, D–G) or rarelybrec cias of Fa cies B, mainly at the Čremoë lo cal ity (Fig. 3C).The beds are sheetlike, non-ero sive or with in sig nif i cant basalero sion. The thick ness of in di vid ual beds is vari able but itmainly ranges from less than 1 m to 2.5 m. Con glom er atesrange from tex tur ally polymodal to bi modal, with clast sizerang ing from peb bles to large boul ders. The max i mum size ofthe boul ders is of ten more than 1 m in long axis and lo cally iso -lated “over sized clasts” up to 2.5 m across can oc cur. These areev i dently larger than the com mon large boul der size in the bedsand they of ten equal the bed thick ness. Al though clasts are ran -domly ar ranged, subhorizontal and flow-par al lel clasts are rel a -tively com mon. There is wide vari a tion in the char ac ter of ma -trix but, gen er ally, it com prises poorly sorted grav elly, red dishsandy mud (Fig. 3I). Some con glom er ates have a pre dom i -nantly sandy ma trix, while oth ers are more muddy (Fig. 3D).Marked size dif fer ences in clast round ness are ob serv able inFa cies C1–3 at the Pucov lo cal ity. The larger, cob ble- to boul -der-size clasts are of ten subrounded or rounded, while thesmaller clasts are gen er ally less rounded and more subangularor an gu lar. The in verse grad ing in the con glom er ates (Fa ciesC3, Fig. 3F) is marked by a grad ual in crease in larger cob blesand boul ders which oc cur mainly in the up per most part of thebed leav ing the bulk of the peb ble/cob ble-size con glom er atever ti cally un changed. Less fre quently, there is a pro gres sive in -crease in the size of all clasts through out the bed. Thethick-bed ded con glom er ates are oc ca sion ally interbedded withmas sive, red dish sandy mudstones with spo radic scat teredclasts (Fa cies M1).

Some de pos its of Unit 1 gen er ally form thin ner beds, from a few decimetres to a metre thick, and they usu ally have an ero -sive base. They are of ten len tic u lar and pinch out over a dis -tance of a few metres (Fig. 3A). Clasts size here range fromgran ules to cob bles, typ i cally with clast-sup ported fab ric andcrude gra da tion (Fa cies C4). How ever, they oc ca sion ally showsigns of crudely de vel oped strat i fi ca tion in the up per parts ofbeds (Fa cies C6). The clasts usu ally show hor i zon tal ori en ta tion and signs of imbrication. The sort ing and round ness of these



T a b l e 1

De scrip tion and in ter pre ta tion of dom i nant sed i men tary fa cies in the late Eocene al lu vial fan delta se quence (the Pucov Mem ber)of the south ern Orava re gion

Fa cies Oc cur rence Char ac ter is tics In ter pre ta tion

Fa cies B1 – mas sive,clast sup ported brec cia

sub or di nate

clast-sup ported fab ric, un graded, very an gu lar to subangular, poorly to very poorly sorted, coarse peb ble to me dium boul der-size clasts, sandy muddyma trix, slightly or ga nized – par al lel-ori ented large clasts, some ver ti cal

clasts, sheet-like lat er ally con tin u ous beds, bed thick ness from decimetresto sev eral metres

lam i nar shear flow, co he sionless de bris flow,

hyperconcentrated flow

(Allen, 1981; Lowe, 1982;Shultz, 1984; Postma, 1986)

Fa cies B2 – mas siveto crudely strat i fied,ma trix sup portedbrec cia

sub or di nate

ma trix-sup ported fab ric, very an gu lar to subangular, poorly sorted, verycoarse peb ble to coarse cob ble-size clasts oc ca sion ally with some iso lated�out sized” clasts (me dium boul ders), gravely (fine peb ble), sandy muddy

ma trix, dis or ga nized to slightly or ga nized – clasts ar range ment showspar al lel-ori en ta tion to bed ding but many of clasts are ran domly ori ented

(much more than in fa cies B1); usu ally sheet-like beds gen er ally not ex ceed 1 m in the thick ness; spo radic thin in verse grad ing at the base

de bris flow, (lam i nar shear to plug flow)

(Naylor, 1980; Nemec and Postma, 1993)

Fa cies C1 – mas sive,clast sup ported con glom er ates

main

clast-sup ported fab ric, subrounded to rounded (rare also well-rounded),poorly to mod er ately sorted, un graded (some times thin in verse grad ing at

the base), peb ble to me dium boul der-size clasts (usu ally not ex ceed70–80 cm in long axis); sand/fine gravel ma trix with the lo cal markedin creas ing of mud por tion, dis or ga nized to slightly or ga nized (par al lel-ori ented large clasts, some ver ti cal clasts); lat er ally con tin u ous beds,non-ero sive base, beds thick ness from decimetres to sev eral metres

cohesionless de bris flow

(Nemec et al., 1980;Lowe, 1982; Massari, 1984)

Fa cies C2 – mas sive,ma trix sup ported con glom er ates

main

ma trix-sup ported fab ric, subrounded to rounded (rare also well-rounded),poorly sorted, un graded (spo radic thin in verse grad ing at the base), verycoarse peb ble to coarse boul der-size clasts, the iso lated “out sized” clasts

can reach very coarse boul der size (up to 2.5 m in long axis), vari ablegran ule/sand-muddy to sandy fine peb ble grav elly ma trix; dis or ga nized to

slightly or ga nized (ran domly- to par al lel-ori ented large clasts), usu allysheet-like beds, from decimetres to sev eral metres in thick ness,

non-ero sive base

de bris flow, dom i nant co he sivestrength sup port, dis perse

pres sure at clast in ter ac tions can oc cur

(John son, 1970; Hampton, 1979; ;Lowe, 1979, 1982)

Fa cies C3 – in verselygraded con glom er ates

sub or di nate

to

rare

vari ably clast- to ma trix-sup ported (clast-sup ported fab ric pre vail),subrounded to rounded, poorly sorted, graded (the in versely gra da tion isof ten less-dis tinc tive and may form all the bed or just part of the bed),peb ble to fine boul der-size clasts, sandy muddy ma trix, beds thick nessare ap prox i mately 50–250 cm, the lower bound aries are usu ally flat;

the up ward coars en ing clast-sup ported gran ule to cob ble con glom er ates,some times with ero sive base, usu ally up to 80 cm thick beds

de bris flows (Lowe, 1982; Nemec

and Steel, 1984; Postma, 1986; )

chan nel bar de pos its (Nemec and Postma, 1993)

Fa cies C4 – nor mallygraded con glom er ates

sub or di nate

to rare

clast-sup ported fab ric, subrounded to rounded, poorly to mod er ately sorted, graded, gran ule to fine boul der-size clasts, sandy muddy to sandy ma trix,

vari able bed thick ness from 20–100 cm, usu ally ero sional lower bound ary,oc ca sion ally with the coarse to very coarse grained poorly sorted

sand stones in the up per most part of the fa cies

gravely high-den sity turbidite;fluidal sed i ment flow, wa ter-laid de pos its/stream flow, de bris fall

de pos its

(Lowe 1979, 1982; Nemec,1990; Nemecand Postma, 1993)

Fa cies C5 – in versely-to-nor mally graded con glom er ates

rare

vari ably clast- to ma trix-sup ported, subrounded to rounded, poorly to mod -er ately sorted, peb ble to fine boul der-size clasts, graded (lower in verselygraded part is usu ally ma trix-sup ported, nor mally graded part tend to beclast-sup ported), poorly to well-sorted pre dom i nantly sandy ma trix, bedsthick ness up to 250 cm, the lower bound aries are usu ally flat and sharp

debris flow, high-den sity tur bid ity cur rent

(Lowe, 1982; Nemec and Steel,1984; Kim et al., 1995)

Fa cies C6 – strat i fiedcon glom er ates andsand stones

sub or di nate

clast-sup ported fab ric, subrounded to well-rounded, mod er ately towell-sorted peb ble to cob ble-size con glom er ates (�out size” fine

boul der-size clasts are pres ent) interstratified with coarse to very coarsegrained peb ble sand stones and gran ule-size con glom er ates with occurenceof cross-bed ding and par al lel lam i na tion, com monly bi modal or polymodaltex tures, beds thick ness are about 20–150 cm, dis tinc tive lower bound aries,

oc ca sion ally ero sive

de po si tion in the shoreface zoneun der wave ac tion

(Reineck and Singh, 1980;stream flow

(Rust, 1978; Nemec and Steel, 1984)

Fa cies C7 –well-sorted,imbricated con glom er ates

sub or di natemas sive, close-packed, well-sorted, well-rounded, rod/spher i cal to

disc/blade shaped peb ble-size (rare cob ble-size) clasts, well-sorted sandyma trix, up to 1 m thick lat er ally dis con tin u ous beds with ero sive bases

shoreface or beachface with rip chan nels

(Bluck, 1967; Gruszczyński etal., 1993; Hart and Plint, 1995;

Da vis and Fitz ger ald, 2004)

Fa cies S1 – mas siveto graded sand stones sub or di nate

me dium to very coarse sand stones, few centi metres to sev eral decimetres in thick ness, can form iso lated beds or can be part of larger suc ces sion,

nor mal grad ing usu ally in the basal part; well to poorly sorted, some timeswith dis persed gran ule to peb ble-size clasts; strong vari abil ity in grain

shap ing (from an gu lar to rounded); oc ca sion ally large amount of well tomod er ately pre served fos sil re mains (mainly large foraminifers) – dis persed

or con cen trated at the base; rare bioturbation

tur bid ity cur rents, wan ing trac tion cur rents, re turn storm

flows

(Lowe, 1982; Brenchley, 1985;Myrow and Southard, 1996)

Fa cies S2 – lam i natedsand stones andsiltstones

sub or di nate

me dium sand stones to fine siltstones, vari able in thick ness from sev eralcenti metres to few metres; some times con tin u ing from fa cies S1 or fa cies

C4; mainly thick beds show fin ing – up ward ten dency in grain size(from sand stones to very fine siltstones); pos si ble cur rent rip ples;

com monly over lain by fa cies M2

hyperpycnal flows, sus pen sionset tling (hypopycnal flows);

low-den sity tur bid ity cur rents

(Bouma, 1962; Middle tonand Hampton, 1976)

Fa cies M1 – mas sive,red dish mudstones rare

unstructuralised mudstones, poorly sorted, oc ca sion ally with scat tered clasts and var ied con tent of sand; decimetres

to max i mal 2 m thick interbeds

the re sult of set tling of fines af ter flood ing

(Bardaji et al., 1990), mud flow

Fa cies M2 – ho mo ge neousmudstones/marlstones

mainvari able con tent of a silty com pound; ran dom bioturbation, rich on

microfossils (foraminifers, dinoflagellates, cal car e ous nannoplankton), rare oc cur rence of thin tuffite ho ri zons and lam i nated lime stones; thin to very

thick (few centi metres to sev eral metres)

hemipelagic set tling

(Pickering et al., 1986)


de pos its vary con sid er ably from be ing well-sorted and hav ingrel a tive tex tural ma tu rity to poorly sorted con glom er ates andbrec cias with an un sorted red dish ma trix. The con glom er ateslo cally ex hibit tex tural bimodality with openwork grav els filled with fines of – clay and fine silt/sand (cf. Frostick et al., 1984).

No fos sil re mains were found within Unit 1 and the clastcom po si tion re flects the source ar eas formed by the Choč andKrížna nappes (cf. Gross et al., 1984). Oc ca sion ally, at theČremoš lo cal ity, flowstone clasts (Fig. 3H) were found.

In ter pre ta tion: the in ter nal char ac ter is tics of the fa cies ofthe Unit 1 in di cates that de po si tion could range from slow- mov ing, high-strength/vis cos ity de bris flows to more wa ter --rich fluidal flows with in tense shear ing and pos si bly tur bu -lence.

Un graded, poorly sorted beds with ran dom fab ric may in di -cate high shear-strength or high vis cos ity, and these can be in -ter preted as “co he sive de bris flows” with the de vel op ment of a“semi-rigid plug” (John son, 1970; Naylor, 1980). Thissemi-rigid plug usu ally forms in the thicker, up per part of thebed over ly ing the basal high-shear layer (e.g., Hubert andFilipov, 1989), and it can form al most the en tire bed thick ness,of ten with thin in verse grad ing re stricted to the basal few centi -metres (shear zone; Fig. 3E). The larger boul ders tend to moveup wards in the flow and out of the shear ing layer, thus pro duc -ing the in verse grad ing seen at the base of the beds (Hubert andFilipov, 1989). Al though in verse grad ing through out the bedhas been ex plained by dispersive pres sure in the flow, so thatthe larger clasts move up wards through the flow to equal ize thestress gra di ent (e.g., Bagnold, 1954; Nemec and Steel, 1984),later lab o ra tory ex per i ments pro posed a mech a nism known aski netic siev ing. This pro cess in volves small grains pass ingthrough the in ter stices be tween the larger par ti cles through ag i -ta tion, thus dis plac ing the larger par ti cles up wards (Middle ton,1970; Naylor, 1980; Gray and Thorn ton, 2005).

The trend of size dif fer ences in clast round ness can be ob -served al most ex clu sively in those fa cies with a red dish ma trix(Unit 1). This may be a re sult of more ef fec tive abra sive pro -cesses for large clasts over a short trans port dis tance, or al ter na -tively it may in di cate redeposition of older fluvio-al lu vialdeposits.

The nor mal grad ing in con glom er ates (Fa cies C4) withsigns of basal ero sion most likely oc curred as a re sult of de po si -tion from more wa tery fluidal sed i ment flows (e.g., Law son,1982). A trans verse clast align ment (Fig. 3G) sug gests de vel -

op ment from more fluidal flow with a sig nif i cant trac tionalcom po nent (Pierson, 1981; Law son, 1982).

Mas sive, red dish, sandy mudstone interbeds (Fa cies M1)are rare, and these may re flect the set tling of fines fol low ingflood ing (Bardaji et al., 1990) or a redeposition of fine-grainedma te rial re worked from de bris flow de pos its or bedload-dom i -nated de pos its.

Wa ter-laid de pos its (Bull, 1972), are rep re sented by streamand sheetflood de pos its. They rep re sent fluid-grav ity flows,with fluid tur bu lence sup port ing clasts in New to nian flu ids,and they are char ac ter ized by a lack of shear or yield strength(Costa, 1988). The thin ner ero sive con glom er ate beds may rep -re sent chan nel-fill de pos its or broad shal low scour fills, thelarg est clasts at the base likely be ing bed-load ma te rial de pos -ited af ter ero sion in the max i mum stage of flood ing as chan -nel-floor lags.

The spo radic up ward coars en ing char ac ter of the clast-sup -ported con glom er ates (Fig. 3A) oc curs in as so ci a tion withchan nel-floor lags and these can most likely be in ter preted aschan nel bar de pos its (Nemec and Postma, 1993).

The pres ence of the up ward-fin ing sandy cap ping (Fa -cies S1), lo cally with an ero sive base, and signs of strat i fi ca tion,may re sult from tur bu lent fluid flow or al ter na tively fromheavily sed i ment-laden stream flow fol lowed by de bris flow(Nemec and Steel, 1984). Some beds are more lat er ally ex ten -sive with slight strat i fi ca tion and they can rep re sent sheetfloods de pos its. Sheetflood con glom er ates can be de pos ited from ex -tremely heavy but short-lived floods (Blair and McPherson,1994). In con trast to streams, these form shal low, un con finedflows cov er ing a large sur face.

The fa cies as so ci a tion of Unit 1 com prises sed i men tary fa -cies which are pre dom i nantly in volved in mass flow de pos itsinterfingering with fluid-grav ity flow de pos its (Fig. 3A).

Mas sive, dis or ga nized to slightly or ga nized con glom er ates(Fa cies C1, C2) in clud ing mas sive to crudely strat i fied brec cias(Fa cies B1, B2) are the most fre quent fa cies in Unit 1. These fa -cies com monly show strong ver ti cal vari a tions, and clast-sup -ported con glom er ates of ten pass to or are interbedded with ma -trix-sup ported con glom er ates (Fig. 3D). How ever, some bedsex hibit better or ga ni za tion with in versely graded con glom er -ates be ing rel a tively abun dant (Fa cies C3) and, in a few iso latedcases, nor mally graded con glom er ates (Fa cies C4) with an ero -sional base oc cur. The de bris flow-type con glom er ates in thelower parts of Unit 1 are oc ca sion ally interbedded with mas -sive, red dish mudstones (Fa cies M1). This fa cies has been doc -


Fig. 3A – de tailed sec tion of the al lu vial fan fa cies as so ci a tion (Unit 1) spe cific in mass-flow de pos its interfingering with stream de pos its; B – ma -trix-sup ported, well-rounded boul der con glom er ates with red dish sand-clayey ma trix (Fa cies C2, Pucov site); C – clast-sup ported red dish brec -cias (Fa cies B1, Čremoš site); D – surg ing de bris flow de pos its with ver ti cal vari a tion in char ac ter of the ma trix from red dish muddy ma trix of thema trix-sup ported con glom er ates (Fa cies C2, lower part) to the sandy ma trix of the clast-sup ported con glom er ates (Fa cies C1, up per parts); E –un graded, poorly sorted, de bris flow con glom er ates (Fa cies C1) with slightly or ga nized to ran dom fab ric (“semi-rigid plug” flow de po si tion) withthin in verse grad ing re stricted to the basal few centimetres (shear zone); F – in versely graded con glom er ates (Fa cies C3); G – trans verse align -ment of clasts in more fluidal flow with a sig nif i cant trac tional com po nent; H – rare flowstone clasts in de bris flow con glom er ates at the Čremošsite in di cate karstification the source area; I – brec cia with poorly sorted sand-clayey red dish ma trix (Čremoš site, mi cro scopic view)

A: DF – de bris flow, SF – stream flow, FSF – fluidal sed i ment flow, g – gran ule, p – peb ble, c – cob ble, b – boul der

u mented only by bore hole in ves ti ga tion (Gross, 1979). Streamand sheetfloods de pos its oc cur in far fewer por tions as massflow de pos its.

The fa cies as so ci a tion of Unit 1 rep re sents the subaerialpor tion of a coarse-grained fan delta. Subaerial mass-flow de -pos its are note wor thy for their red dish col our and they form the ver ti cally most ex ten sive suc ces sion with a max i mum thick -ness of ap prox i mately 150 m (Gross, 1979; Fig. 2B, sec tion a).


De scrip tion: the de pos its of Unit 2 are gen er ally thick-bed -ded, mas sive, ma trix- to clast-sup ported con glom er ates (Fa cies C; Fig. 4A) with a grey ish-to-yel low ish poorly to mod er atelysorted grav elly/sand to sandy ma trix (Fig. 4D). The beds areusu ally sheet-like, non-ero sive, with bed thick nesses rang ingfrom less than 1 m to sev eral metres. Al though the bed bound -aries are lo cally in dis tinct and amal gam ated, they are gen er allymuch better de fined than those in Unit 1. These con glom er atesare un graded, with some beds ex hib it ing better or ga ni za tionwith in verse grad ing of Fa cies C3 (Fig. 4G). Nor mal grad ing(Fa cies C4, Fa cies S1 – in the case of sandy cappings) or rare in -verse-to-nor mal grad ing (Fa cies C5) oc ca sion ally oc curs. Theclasts vary from gran ule- to boul der-size up to 80 cm.

Some lat er ally dis con tin u ous beds have an ero sive base(Fig. 5A), and they are formed by close-packed, well-sorted,of ten imbricated, rod/spher i cal (Fig. 5A1) to disc/blade(Fig. 5A2) shaped peb bles (Fa cies C7). A bedset of well- tomod er ately sorted, well-strat i fied coarse-grained peb bly sand -stones and peb ble- to cob ble-size con glom er ates (Fa cies C6;Fig. 4A – up per part) oc cur within Unit 2. These beds have dis -tinc tive and oc ca sion ally ero sive lower bound aries and lat er -ally they show sig nif i cant persistance.

The clast com po si tion is al most iden ti cal to that of theUnit 1 de pos its, but in the up per most parts of Unit 2 some peb -bles of mid dle Eocene car bon ate sand stones from the BorovéFm. also oc cur (Gross et al., 1982, 1993).

In ter pre ta tion: the char ac ter is tics of the de pos its of Unit 2(Fig. 4F) are gen er ally sim i lar to those of Unit 1, and they in di -cate de po si tion within high shear-strength or high vis cos ityflows (“rigid plug” flow de po si tion – with ran dom fab ric andsome clasts pro jected above the bed), strongly sheared, lam i nar flows with pre ferred clast ori en ta tion fab ric, and more wa -ter-rich fluidal flows (nor mal grad ing, signs of basal ero sion).The scarce in verse-to-nor mal grad ing of Fa cies C5 may re flectthe ten dency of sub aque ous de bris flows to re duce flow den sity and fric tional/vis cous re sis tance and to evolve into high-den -sity tur bid ity cur rents (Lowe, 1982; Nemec and Steel, 1984).

Good sort ing and lack of inter gra nu lar mud within Fa -cies C7 re veal that the depositional pro cesses were ef fec tive inwash ing and sort ing the sed i ment (Clifton, 1973; Bluck, 1999). Close-packed, well-sorted, well-rounded con glom er ates of tenrep re sent wave-re worked tops of de bris-flow con glom er atesand they can be at trib uted to a wave ravinement sur face.Sharply bounded tab u lar gravel beds may be in ter preted aswave lag de pos its with storm-re lated ero sional sur faces. Smallchan nels and cross-lam i na tion (Fig. 5B, C) may have beenformed by ei ther waves or along shore cur rents (Hart and Plint,1995). The chan nels and scours can rep re sent both along shore

troughs and rip chan nels (Gruszczyński et al., 1993). How ever, the clast imbrication shown in Fig ure 6A is sim i lar to theimbrication in the un der ly ing de bris flow de pos its in Fig ure 6B, and this points rather to rip chan nel fea tures.

As for the de pos its of the Unit 1, those of Unit 2 were pre -dom i nantly sup plied as mass-flow de pos its (Fig. 4A) andsubordinately as wave-re worked de pos its that form lat eral dis -con tin u ous interbeds rang ing from a few decimetres up to ametre thick in side de bris-flow de pos its, or they form bedsets up to 6 m thick spo rad i cally al ter nat ing with thin ner de bris-flowcon glom er ates.

How ever, there are gen er ally some tex tural and struc turaldif fer ences be tween the mass flow de pos its in Units 1 and 2.Un like in Unit 1, the max i mum clast size here is con sid er ablysmaller and the mass flow de pos its gen er ally ex hibit betterround ing of all par ti cles (Fig. 4D, E); better sort ing; an ab senceof inter gra nu lar mud; a more fre quent oc cur rence of gran -ule/sandy cappings, and more beds that show an up wards in -crease in their ma trix con tent.

Fos sil re mains oc cur in Unit 2 (Fig. 4B) to gether with rarebioturbation (Fig. 4C), wave-re worked de pos its (Fig. 5), andspo radic thin mudstone interbeds rich in microfossils (Soták etal., 2007). These char ac ters sug gest that the fa cies as so ci a tionof Unit 2 re flects de po si tion in the sub aque ous part of acoarse-grained fan delta. Sub aque ous coarse-grained fan deltade pos its oc cur at Pucov, Čremoš, and most likely also atMedzihradné. The lim ited out crop and mo not o nous, grey mas -sive con glom er ates at this lat ter lo cal ity do not al low un am big -u ous in ter pre ta tion of the depositional set ting.


De scrip tion: the de pos its of Unit 3 are well-doc u mented asan ap prox i mately 50 m thick se quence at the Pucov sec tion(Fig. 2B, sec tion a). The se quence is char ac ter ized by de creas -ing con glom er ate vol ume, while sand stones and siltstones (Fa -cies S1, S2) are dom i nant and the mudstone pro por tion (Fa ciesM2) is mark edly higher (Fig. 7B).

The bed thick ness ranges from a few cm to more than 1.5 m. Thin ner beds of up to 20 cm in the lower parts of Unit 3 formiso lated granu lites to sand stones with dis tinct bot toms and tops(Fa cies S1). Most of the sand stones con tain a rel a tively largenum ber of re de pos ited fos sil re mains, pre dom i nantly those oflarge foraminifers (Fig. 7C), and these sand stones are sep a rated by decimetre-thick mudstones.

In fre quent, well-de fined, iso lated, and non-con tin u ousbeds up to 1 m in thick ness oc cur here (Fig. 7D). These areformed by nor mally graded fine boul der- to peb ble-size con -glom er ates (Fa cies C4) pass ing up wards to very coarse peb blysand stones (Fa cies S1) and to a thin in ter val of lam i nated finesand stones and siltstones (Fa cies S2).

Oc ca sion ally, there are also com pos ite beds more than 1 mthick (Fig. 7F) with mas sive, clast-sup ported con glom er ates atthe base (Fa cies C1). These con glom er ates are over lain by nor -mally-graded beds (from base up ward Fa cies C4, S1, and S2)and also by ho mog e nous mudstones (Fa cies M2).

The up per por tion of Unit 3 is mainly rep re sented byfine-grained marlstones rich in microfossils (Fa cies M2), andinterbedded with thin sand stones (Fa cies S2) as well as with


lam i nated lime stones (Fig. 7G) and thin ocherous brown tuffite ho ri zons (Fig. 7H). The up per most part of Unit 3 at the Pucovand Čremoš sec tions shows oc cur rences of a thick iso latedsand stone bed.

In ter pre ta tion: a rel a tively thick peb ble to boul der size,usu ally nor mally graded con glom er ate can be in ter preted as the

de posit of a hyperconcentrated flow (Costa, 1988) or de -bris-fall av a lanche (Nemec, 1990b). The me dium peb ble sizecon glom er ates to sand stones fa cies of S1 and S2 in the top ofthese beds may re flect de po si tion rang ing from grav ellyhigh-den sity tur bid ity cur rents (Lowe, 1982) to low-den sitytur bid ity cur rents (Bouma, 1962). The coarse-grained iso lated


Fig. 4A – de tailed sec tion of the sub aque ous fan delta fa cies as so ci a tion (Unit 2) spe cific in mass-flow de pos its interfingering with wave-re workedde pos its; oc cur rence of fos sil re mains (B – large foraminifers) and bioturbation (C) in the sub aque ous fan delta de pos its; ma trix-sup ported con -glom er ates (Fa cies C2) (D) and clast-sup ported con glom er ates (E) with rel a tively well-sorted and rounded par ti cles (Fa cies C6); F – mass-flowcon glom er ates (Pucov); G – in versely graded beds (Fa cies C3)

DF – de bris flow, WR – wave re worked; v c – v. coarse, for other ex pla na tions see Fig ure 3


Fig. 5A – wave-re worked top of de bris-flow con glom er ates (Fa cies C7); A1 – close-packed, well-sorted,imbricated, rod/spher i cal shaped peb bles; A2 – imbricated peb bles be hind the large boul der (rel ict of de -bris-flow de po si tion); B, C – cross-lam i nated fine-grained con glom er ates and sand stones formed by wavesor shal low-ma rine (wave in duced) cur rents (Fa cies C6, S1)

DF – de bris flow, d/b – disc/blade, s/r – rod/spher i cal

Fig. 6. Mea sure ments of in clined clasts from de bris-flow con glom er ates of Unit 1 (A) and ripchan nels of Unit 2 (B) pre sented by Rose di a gram of dip di rec tion

Data is ro tated to orig i nal po si tion; gen eral palaeotransport is to ward the NW to W;n – num ber of mea sure ments

granu lites to sand stones with dis tinct tops sug gest in com pleteturbidites (“top cut-out” beds) that may re flect the downslopeby pass ing of most of the fine-grained sus pended load (Nemec,1990b). The fine-grained, usu ally lam i nated sand stones andsiltstones (Fig. 7E) may re flect dis charge from a flood-stagestream with a high con cen tra tion of sed i ment de pos ited byhyperpycnal flows (Bates, 1953; Wright et al., 1988; Mulderand Syvitski, 1995) or by flows of hyperconcentrated bedload(Prior and Bornhold, 1989) that reached the prodelta and slope.The fine-sed i ment frac tions may also be de rived from in tensefall out from the sus pen sion plume blan ket ing large sub aque ous ar eas with a dense, mo bile sus pen sion which could evolve intoa sheet-like un der flow (cf. Hay et al., 1982; Wright et al., 1986; Syvitski and Far row, 1989).

The fa cies as so ci a tion in the lower parts of Unit 3 sug gestsde po si tion in a prodelta and slope en vi ron ment and forms theup per most part of the delta fan suc ces sion. An in creas ing trendin the pro por tion of com plete me dium- to fine-grainedturbidites (low-den sity tur bid ity cur rents; cf. Bouma, 1962;Middle ton and Hampton, 1976), the con tri bu tion ofhemipelagic mudstones/marlstones fa cies (M2), and an oc cur -rence of lam i nated lime stones are mainly ev i dent in the higherparts of Unit 3. These com po nents may re flect dis talprodelta/slope de po si tion and a basinal fa cies (Fig. 7A).

DISCUSSION

BOUNDARY BETWEEN SUBAERIAL AND SUBAQUEOUS FAN DELTA ENVIRONMENTS

The subaerial and sub aque ous de pos its of the Pucov sec tion are rel a tively sim i lar and it dif fi cult to pre cisely dis tin guishtheir in ter face be cause of their mass flow coarse-grained char -ac ter (cf. Nemec and Steel, 1984). How ever, in ad di tion to thepres ence of fos sil re mains, rare bioturbation and wave re work -ing in the up per part of Unit 2, there are other dif fer encesamong the mass flow de pos its in these units. In Unit 2, a largenum ber of grey ish con glom er atic beds tend to be better or ga -nized and sandy cappings be ing are more com mon. This mayre flect the ten dency of the sub aque ous de bris flows to evolveto wards high-den sity tur bid ity cur rents (Lowe, 1982). How -ever, beds with an up wards in crease in their ma trix con tent aremore fre quent. A red dish muddy ma trix, com mon in Unit 1, iscom pletely miss ing in the Unit 2 con glom er ates, which also ex -hibit better sort ing and round ing of par ti cles and an ab sence ofcon glom er ate in ter sti tial mud. This may sug gest a redepositionof sed i ments which were re worked on the sea shore as well ascan ni bal ism of the shal low-ma rine units of pre vi ous cy cles(Borové For ma tion). The coarse-grained fa cies ana lysed showa pos i tive cor re la tion be tween bed thick ness and max i mumclast size (Fig. 8). This could be used to sup port the idea ofmass-flow de po si tion of the con glom er ates (e.g., Larsen andSteel, 1978; Porębski, 1981; Nemec and Steel, 1984; Nemec,1990b). Al though boul der-size clasts are fre quent in Unit 2, the max i mum av er age size is less than those in Unit 1. This dis tinc -tion is also ex pressed in the dif fer ent re gres sion line gra di ent ofthe MPS/BTh di a gram in Unit 2 (Fig. 8), which may re flect arel a tive de crease in de bris-flow com pe tency af ter pass ing into

wa ter, due to ad mix ing of wa ter into the flow, which re ducestheir den sity, vis cos ity and con cen tra tion (Larsen and Steel,1978; Nemec and Steel, 1984). How ever, the MPS/BTh di a -gram shows a rel a tively wide dis per sion of data and a low cor -re la tion co ef fi cient. This may have been due to the small num -ber of beds ana lysed and to the im pos si bil ity of de ter min ingbed in ter faces be tween the mas sively tex tured sed i ments. Ad -di tion ally, even if it were pos si ble to de fine such in ter faces,they may rep re sent breaks be tween sed i ments de pos ited bymul ti ple dis crete flows rather than breaks be tween in di vid ualflows (Mayor, 1997). Other fac tors in flu enc ing MPS/BTh cor -re la tion in clude (cf. Nemec, 1990b):

– in ac cu rate def i ni tion of flow com pe tence due to theredeposition of pre-sorted de bris (seem ingly lower com -pe tence),

– ero sion of the up per most parts of de bris flow de pos its, – the ad di tion of large clasts to freez ing de bris flows by

de bris-fall pro cesses (seem ingly higher com pe tence). More over, later stud ies on ex per i men tal de bris flows by

Mayor (1997) and Inverson (2003) cast doubt on the suit abil ityof the MPS/BTh an a lytical method. These ex per i ments re -vealed that mas sively tex tured, un sorted de bris-flow de pos itscan of ten re sult from pro gres sive in cre men tal de po si tion which can ac cu mu late with out ob vi ous strati graphic con tact. This canpar tic u larly oc cur where there is a short time in ter val be tweenevents, or sim i lar source ma te ri als, or small travel dis tances.Ver ti cal ac cre tion of sed i ment from surges can pro duce bedsthat ap pear to “sup port” over sized par ti cles which wereemplaced rather than be ing tractional bedloads (Mayor, 1997).Since the above men tioned prob lems ad versely af fect the es ti -ma tion of flow prop er ties em a nat ing solely from MPS/BThanal y sis, this cor re la tion was uti lized herein only as ad di tionalsup port in dis tin guish ing the Unit 1 and Unit 2 deposits.

The bor der line be tween Units 1 and 2 was de fined as thatpar ti tion in the sed i men tary sec tion where the red dish muddyma trix dis ap pears from the de pos its and the grey ish con glom er -ates bear ing the above men tioned signs appear.

TECTONIC AND EUSTATIC CONTROLS ON SEDIMENTATION

Tec ton ics and eustasy played an im por tant role in the for -ma tion of the up per Eocene al lu vial fan delta fa cies as so ci a -tions in the south ern Orava re gion.

Af ter the ini tial trans gres sion of the CCPB (TA 3.5–3.6third-or der Ex xon cy cles), de po si tion changed from subaerialto sub aque ous (Baráth and Kováč, 1995), with the de po si tionof the shal low ma rine Bartonian fa cies of the Borové Fm. Dur -ing the highstand, most of the coarse sed i ments of the fan del tas were stored ad ja cent to hin ter land, thus re strict ing the ar eal ex -tent of the subaerial fans. The marked eustatic low er ing of sealevel in the early Priabonian, at the be gin ning of the TA4supercycle, led to re gres sion ac com pa nied by subaerial ex po -sure and the ero sion of de pos its of pre vi ous sed i men tary cy cles. Rare flowstone clasts (Fig. 3H) in the de bris flow con glom er -ates can in di cate karstification in the source area. The ex posedshelf was prone to de vel op ing in cised val leys as a re sult of flu -vial in ci sion (e.g., Vail et al., 1984; Porębski and Steel, 2003).Con se quently, the red dish nonfossiliferous mass-flow dom i -



nant con glom er ates (al lu vial fan de pos its/subaerial fan delta;Unit 1) filled the in cised val leys. The flu vial in ci sion into theun der ly ing de pos its of the Borové For ma tion and the Me so zoic base ment units is well-marked at the Čremoš lo cal ity and it cor -re sponds to a se quence-stra tig ra phy bound ary (SB1). This in ci -sion in creased from the mar gin to wards the cen tral part of thePucov con glom er ates, with only the cen tral part of this val leyin cised into the Me so zoic base ment be ing over lain by theUnit 1 and 2 de pos its. The in ci sion at the mar ginal ar eas ter mi -nated in de pos its of the Borové For ma tion. Val ley flanks hereare over lain by more wide-spread de pos its of Unit 2 as a con se -quence of backstepping of fan del tas.

The con glom er ates of Unit 1 are no ta ble for their red dishma trix. We as sume that this red pig ment is he ma tite formed byma ture hy drated fer ric ox ides en ter ing the al lu vial sed i ments asfinely di vided soil-weath er ing prod ucts (Tay lor, 1982), fol low -ing their trans port and de po si tion by rivers (e.g., McPherson,1980). The red pig men ta tion may also have been in creased bydis in te gra tion of red and vi o let sed i men tary rocks of the Me so -zoic units (Gross et al., 1982). A sub se quent rise in the rel a tivesea level ac com pa nied by rel a tively rapid tec tonic sub si dence(Soták et al., 2001) along the CCPB mar gins dur ing thePriabonian led to ex ten sive trans gres sion and the grad ual over ly -ing of subaerial al lu vial de pos its by the sub aque ous fan delta fa -cies as so ci a tion of Unit 2. The on set of trans gres sion is markedby wave-re worked con glom er ates and by the onlap of de pos itsof Unit 2 onto the in cised val ley walls, where the transgressivesur face co in cides with the SB1 se quence bound ary. Ero sive fea -tures filled by wave-worked con glom er ates may rep re sentravinement sur faces. The sub aque ous en vi ron ment of delta fansshows a rel a tively high coarse-grained in put which is mainly due to mass flow move ment. How ever, this en vi ron ment is char ac -ter ized by het er o ge ne ity of the fa cies se quences, which can re -flect in ter play be tween pro cesses. These in clude vary ing dis -charges of sed i ment dur ing in di vid ual flood events or the ef fectsof wave, tide and cur rent pro cesses. Wave-re worked seg mentsin the Unit 2 may in di cate a “tran si tion zone” (Wescott andEthridge, 1982) where coarse-grained del tas are in flu enced bywave and tides (Postma, 1984; Colella, 1988).

A sub se quent con tin ual rel a tive sea level rise re sulted in adeep en ing depositional en vi ron ment which is doc u mented bythe gen er ally up wards-fin ing trend in par ti cle size be tweenUnit 2 and 3. This re flects the rel a tively rapid tran si tion from ashal lower-wa ter fa cies to a prodelta/slope and basinal fa cieswith slow hemipelagic set tling. Max i mum flood ing oc curred in

Unit 3 abreast of de po si tion of the Globigerina Marls (Soták etal., 2007).

How ever, it is dif fi cult to es ti mate the in di vid ual con tri bu -tions of eustatic fluc tu a tions and tec tonic ef fects to the rel a tivesea level changes (e.g., Schlager, 1993; Massari et al., 1999).While re gres sion at the Bartonian/Priabonian bound ary ap pearsto be cou pled rather with a eustatic sea level fall, the in flu ence oftec tonic ac tiv ity at the sources can not be ex cluded. This is due tothe very coarse-grained sed i ments which in di cate a steep gra di -ent in the depositional area which is typ i cal of tec toni cally con -trolled ba sin mar gins. Ad di tion ally, the fol low ing trans gres sionand rel a tively rapid deep en ing of the depositional en vi ron mentsug gest a sig nif i cant ef fect of tec tonic sub si dence in the Oravare gion of the CCPB. The con tin u ous rel a tive sea level rise mayhave in flu enced the delta front to re treat to wards the land. Aban -don ment of the delta slope and the prodelta re sulted in ahemipelagic drape on the sub sid ing fan delta lobes in Unit 2.

The rel a tively small lat eral ex tent of in di vid ual deltaic bod -ies, the vari able dis charge com pe tence, and the lim ited trans -port dis tance as in di cated by the scarce ness of sta ble con stit u -ents and the dom i nance of im ma ture de bris; all sug gest a smallfan delta sys tem with a small drain age ba sin and a short feedersys tem. The for ma tion of such del tas re flects a rapid re sponseto cli ma tic and tec tonic changes (Postma, 1990). The ar chi tec -ture of the Pucov suc ces sion cor re sponds to a shal low-wa tercoarse-grained al lu vial delta, gen er ally dom i nated by gravel,with a steep gra di ent of the A-feeder type sys tem (sensuPostma, 1990). It is char ac ter ized by ephem eral, un con finedstreams in volv ing mass flows. Due to rapid tec tonic sub si dence along the CCPB mar gins, this ini tial shoal-wa ter delta stagechanged dur ing the Priabonian and de po si tion re flects thedeep en ing en vi ron ment af fect ing the fan del tas’ ar chi tec ture.This caused the land ward shift ing of coarse-grained fa cies withclasts trapped on the shore, while dis tal parts of the fan deltawere de ac ti vated by the su per po si tion of basinal marlstones,lime stones and thin turbidites.

SEDIMENTOLOGICAL INTERPRETATION AND SPATIALOCCURRENCE OF THE PUCOV MEMBER

The in ter pre ta tion of the Pucov Mem ber pre sented in thispa per dif fers from that pro vide by Gross et al. (1982, 1993).From a sedimentological view point, there are at least three rea -sons for this dif fer ent in ter pre ta tion.


Fig. 7A – de tailed sec tion of the dis tal prodelta/slope and ba sin fa cies as so ci a tion (up per part of Unit 3) show ing mainly its fine-grainedhemipelagic de po si tion and turbidites (Pucov); B – rhyth mic de po si tion of siltstones and mudstones with thin turbiditic sand stones in prodelta(Fa cies M2, S2); C – mi cro scopic view of car bon ate sand stones (Fa cies S1) with com mon re de pos ited fos sil re mains (mainly large foraminifers:Num mu lites sp., Alveolina sp.); D – iso lated, thick bed of nor mally-graded con glom er ates (Fa cies C4) underbeded with Fa cies M2 and over lappedby thin in ter val of Fa cies S2 with Fa cies M2 (prodelta/slope enviroment); E – fine-grained, lam i nated sand stones and siltstones (Fa cies S2) de pos -ited by hyperpycnal flows; F – thick com plex bed formed (bot tom up wards) by peb ble to fine cob ble de bris-flow con glom er ates at the base (Fa ciesC1), over lain by a turbidite unit of mas sive to nor mally-graded coarse peb ble con glom er ates with ero sive base (Fa cies C4), coarse peb ble sand stone (Fa cies S1) and pla nar-strat i fied sand stones to siltstones (Fa cies S2) con tin u ous pass ing into mudstones (Fa cies M2); G – lam i nated lime stones; H –thin tuffite ho ri zon

m – mudstone, s – siltstone, sand. – sand stone

Firstly, if the Pucov con glom er ates form a deep-wa terdepositional fan in the lower part of the Huty For ma tion, thepres ence of an un der ly ing Eocene basinal/deep-wa ter fa ciescan be pre sumed. How ever, such a basinal/deep-wa ter fa cieswas not con firmed by field map ping and by an ex plo ra tionwell. It was es tab lished that only other shal low-wa ter de pos itsof the Borové For ma tion or the Cre ta ceous sed i men tary base -ment of the Krížna Nappe are pre served in the stud ied sec tions.

Sec ondly, sed i men tary fea tures, such as the col our andcom po si tion of the ma trix, the ab sence and up wards in crease of fos sil rem nants, and the oc cur rence of wave re worked seg -ments, all sug gest de po si tion chang ing from a subaerial to ashal low ma rine en vi ron ment rather than a deep ma rine one(e.g., Dabrio, 1990).

Thirdly, the to tal ab sence of fos sils in the rare fine-grainedfa cies as so ci ated with the red con glom er ates is more in keep ing with al lu vial fan mod els rather than with deep-wa ter can yonsor ter mi nal fan mod els, where interbed ding with hemipelagicmudstone drapes which are of ten rich in microfossil con tent,and also more sandy ho ri zons, are typ i cal (e.g., Wright et al.,1988; Prior and Bornhold, 1990; Gardner et al., 2003).

With re gard to cri te ria such as fa cies as so ci a tions,depositional palaeoenvironment, and strati graphic po si tion, the Pucov Mem ber can be de fined as the fan delta fa cies as so ci a -tion which re flects the change from subaerial to sub aque ousdepositional en vi ron ments dur ing the late Bartonian to earlyPriabonian re gres sive-transgressive cy cle. The sed i men tary re -cord for the sep a rate lo ca tions in the Orava Ba sin (Fig. 2B) rep -

re sents co eval equiv a lents within the fandelta sys tem that changed dur ing evo lu tionof the ba sin.

How ever, con glom er ate de pos itsmarked as the Pucov Mem ber are doc u -mented in dif fer ent strati graphi cal lev els invar i ous parts of CCPB (sensu Gross et al.,1984). These are of ten con nected with un -re lated events and depositionalpalaeoenvironments dur ing evo lu tion ofthe CCPB (e.g., Tokáreň con glom er ates onthe east ern slope of the High Tatra Mts.;Janočko and Jacko, 1999; Janočko et al.,2000). That they share the name the PucovMem ber is con fus ing (cf. Sliva et al., 2004;Soták et al., 2007).

Sed i men tary fa cies, sim i lar to thePucov Mem ber with red to grey coarseclastic de pos its of ter res trial to shal low ma -rine or i gin, are pre served at dif fer ent strati -graphic lev els in sev eral CCPB out crops.The most dis tinct of these are on the north -ern flanks of the High Tatra Mts. (HrubyRegiel), where pre-transgressive de pos itsof red to grey con glom er ates and brec ciasare over lain by the shal low ma rine stratacom pris ing sand stones and lime stones ofthe Borové For ma tion (Sokołowski, 1959). A partly sim i lar sit u a tion oc curs at the east -ern part of the CCPB, in the Hornád Mem -ber as de scribed by Filo and Siráňová

(1998). Pre-transgressive de pos its near Markušovce vil lagehave been in ter preted as a ter res trial flu vial val ley fill to the fandelta (Marschalko, 1970; Baráth and Kováč, 1995; Prekopováand Janočko, 2005). The fa cies as so ci a tion of the Pucov con -glom er ates is also sim i lar to the Vajsková con glom er ates in theLopejská kotlina De pres sion (Biely and Sam uel, 1982), but de -spite this sim i lar ity, their strati graphi cal po si tion re mains un -clear be cause of poor ex po sure area.

Re newal of a suc ces sion of pre-transgressive char ac ter (de -vel oped on the base of the Borové For ma tion) in the ter mi nalpart of the Borové For ma tion (Pucov Mem ber) sug gests a newre gres sive cy cle at the bound ary be tween the Bartonian andPriabonian. Iden ti fi ca tion of this re gres sive event in other partsof the CCPB is un clear.

This may be es tab lished by the pres ence of strata rich inplant frag ments in the ter mi nal part of the Borové For ma tion(Num mu lit ic Eocene in Po land; Sokołowski, 1959; Głazek and Zastawniak, 1999). Soták et al. (2007) sug gested that thePucov con glom er ates could be in di rectly cor re lated with al lu -vial and fluviolimnic de pos its such as the fresh wa ter Odorínlime stones in the Spiš area or with the fresh wa ter and brack ishclays at the top of the Paleogene coral ho ri zon of the Buda Ba -sin (Seneš, 1964). These were de pos ited dur ing re gres sion andsubaerial ero sion at the end of the mid Eocene and pre ceded the new ma rine trans gres sion at the be gin ning of the late Eocene.

How ever, in ac cor dance with the strati graphi cal po si tionand fa cies fea tures of the Pucov Mem ber, it cur rently ap pearsthat its oc cur rence is lim ited to the Orava re gion.


Fig. 8. MPS/BTh re la tion ship in de bris flows from subaerial (Unit 1) and sub aque ous (Unit 2) de pos its of the al lu vial fan and fan delta

CONCLUSION

The Cen tral Carpathian Paleogene Ba sin evo lu tion re flectsthe im por tant role of rel a tive sea level changes on a tec toni cally ac tive ba sin mar gin. Af ter the ini tial up per Lutetian/Bartoniantrans gres sion with shal low-ma rine de po si tion, the next re gres -sive-transgressive cy cle played a key role in the for ma tion oflate Eocene al lu vial fan delta fa cies as so ci a tions in the south ern Orava re gion.

The first stage of delta de vel op ment is con nected with there gres sion which cor re sponds well with the marked globaleustatic low er ing of sea level at the Bartonian/Priabonianbound ary. This sea level low er ing was most likely the mainrea son for subaerial ex po sure and in ci sion of pre vi ous sed i -men tary suc ces sions and also for the con sis tent de po si tion ofcoarse-grained al lu vial fans. The subaerial de po si tion, ac com -pa nied mainly by thick boul der-rich con glom er ates with a red -dish clayey ma trix, sug gests a mass-flow-dom i nated al lu vialdelta with a va ri ety of de pos its re flect ing a range of slow-mov -ing, high strength/high-vis cos ity de bris flows to more wa -ter-rich fluidal flows, likely show ing a tran si tion to sed i -ment-laden stream flows. The al lu vial fans ad join the sub aque -ous en vi ron ment dis tally where the mass flow de pos its wereof ten sub ject to re work ing by waves or wave-in duced shal -

low-ma rine cur rents and they were also sub ject to fur therresedimentation.

How ever, the ver ti cal ar range ment of the fa cies as so ci a -tions shows a ret ro grad ing delta sys tem which sug gests thathigh-am pli tude trans gres sion re sulted in a rel a tively rapid sub -mer gence of the subaerial and shal low wa ter parts of the thecoarse-grained al lu vial delta with ac com pa ny ing su per po si tionof prodelta/slope and ba sinal fa cies as so ci a tions. Dur ing therapid in crease in sea level, the ar eal ex tent of the subaerial fanswas re stricted and the dis tal parts of the fan delta be came in ac -tive. Al though this trans gres sion re sponded to the grad ualeustatic sea level rise dur ing the Priabonian and at the be gin -ning of the Rupelian, we pro pose that rapid tec tonic sub si dence(Soták et al., 2001) along the CCPB mar gins dur ing thePriabonian was the main agent lead ing to this trans gres sion and to the marked deep en ing of the depositional en vi ron ment.

Ac knowl edge ments. This work was sup ported by the sci -en tific grant agency of the Slo vak Re pub lic (Vega 0140) andSlo vak Re search and De vel op ment Agency un der the con tractNo. APVV-0465-06. We thank D. Ventra and anon y mous re -viewer for the de tailed re view of this pa per and con struc tivecomments.

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Eustatic and tec tonic con tr ol on late Eocen e fan … et al 2012.pdfRastislav Vojtko , De part men t of Ge ol ogy and Palae on tol ogy, Fac ul ty of Nat u ral Sci enc es, Comeni