The Dobrotiv For ma tion (Mio cene) in the Boryslav-Pokuttya and Sambir nappes of the Ukrai nian Carpathians: a re cord of sed i men tary en vi ron men tal change
in the de vel op ment of the Carpathian Foredeep Ba sin
Nestor OSZCZYPKO1, Al fred UCHMAN1, * and Ihor BUBNIAK2
1 Jagiellonian Uni ver sity, In sti tute of Geo log i cal Sci ences, Oleandry 2a, 30-063 Kraków, Po land
2 Geo log i cal Fac ulty, Ivan Franko Na tional Uni ver sity of Lviv, Hrushevskyi 4, 79005 Lviv, Ukraine
Oszczypko, N., Uchman, A., Bubniak, I., 2014. The Dobrotiv For ma tion (Mio cene) in the Boryslav-Pokuttya and Sambir nappes of the Ukrai nian Carpathians: a re cord of sed i men tary en vi ron men tal change in the de vel op ment of the Carpathian Foredeep Ba sin. Geo log i cal Quar terly, 58 (3): 393–408, doi: 10.7306/gq.1152
The up per Lower Mio cene Dobrotiv For ma tion, a 700–800-m-thick unit, was de pos ited in a sub sid ing plat form mar gin, which be come in volved in the mar ginal part of the Outer East ern Carpathian accretionary wedge. The sed i men tary suc ces sion from the Sloboda Con glom er ate up to the Dobrotiv For ma tion re cords a tran si tion from al lu vial fan through fan-delta to deltaic de - pos its, fol lowed by the flu vial plain-chan nel fa cies of the Stebnyk For ma tion. The deltaic de pos its are mud-dom i nated, with poorly de vel oped thick en ing-up pack ets of beds. Ef fi cient sed i ment ac cu mu la tion was bal anced by sub si dence caused by subsurface load ing. Emerged parts of the deltaic sed i men tary sys tem in clude tetrapod foot prints and rain drop im prints. The gen eral ab sence of mudcracks in the Dobrotiv For ma tion sug gests a hu mid cli mate. De pos its of the Sloboda, Dobrotiv and Stebnyk for ma tions form fin ing- and thin ning-up wards clastic wedge suc ces sions along the Ukrai nian Carpathians.
Key words: non-ma rine, deltaic sed i ments, molasse, mam mal and bird foot prints.
INTRODUCTION
A sed i men tary suc ces sion at least 2-km-thick of the rem nant to pe riph eral fore land ba sin of the Boryslav-Pokuttya and Sambir nappes (Vashchenko and Hnylko, 2002; Hnylko, 2012) in the mar ginal part of the East ern Carpathians in Ukraine (Fig. 1A, B) con tains, in its mid dle part, thick, non -ma rine de pos its. They are dis tin guished as the Sloboda Con glom er ate, Dobrotiv For ma tion and Stebnyk For ma tion (Fig. 1C, D). The Dobrotiv For ma tion, dom i nated by fine-grained de pos its, is known from spec tac u larly well-pre served mam mal and bird foot prints (Via lov, 1966). How - ever, there has been lit tle palaeo enviro nmental in ter pre ta tion of this unit. Its sed i men ta tion, which took place af ter coarse clastic de po si tion in the al lu vial fan and fan-delta of the Sloboda Con - glom er ate (Oszczypko et al., 2012), com menced with var ie gated marls, shales and sand stones of the Stebnyk For ma tion and re - cords a sig nif i cant change in depo sitional palaeoenvironment in the fore land ba sin. The course of the change re mains un known, but this prob lem can not be sat is fac to rily solved with out fa cies anal y sis of the Dobrotiv For ma tion.
The aim of this pa per is to de scribe and in ter pret the palaeoenvironment of the Dobrotiv For ma tion, in the con text of
the ba sin de vel op ment, on the ba sis of field re search in the Prut River sec tion, which is the best sec tion through this for ma tion.
PREVIOUS WORKS
The Dobrotiv For ma tion (orig i nally the Dobrotiv Beds) was dis tin guished by Paul and Tietze (1877). Later, it was stud ied by al most all the Pol ish and Ukrai nian ge ol o gists work ing on the fore land of the Ukrai nian Carpathians (e.g., Zuber, 1888, 1915, 1918; Teisseyre, 1927; Bujalski, 1930, 1934, 1938; Denisova, 1959, 1970; Fedushchak, 1962; Vialov, 1960, 1965, 1966 and ref er ences therein), who fo cused mainly on its strati graphic po - si tion, li thol ogy and palaeontological fea tures. Its fa cies coun - ter parts are in the Sub-Carpathian Unit in Ro ma nia are known as the Tescani Beds (Micu, 1982).
The most de tailed de scrip tions of the Dobrotiv For ma tion are given by Teisseyre (1927), Bujalski (1934) and Denisova (1970). Ac cord ing to Teisseyre (1927), de pos its of this for ma - tion are bi par tite and are char ac ter ized by dis tinct lower and up - per bound aries. Their lower part is dom i nated by sand stones, and the up per by claystones and marls. In gen eral, the Dobrotiv For ma tion dis plays a fin ing- and thin ning-up wards se quence.
Vialov (1965) agreed that the Dobrotiv For ma tion oc curs be - tween the Sloboda Con glom er ate and the Stebnyk For ma tion, and con sid ered that the Sloboda Con glom er ate and the Dobro - tiv For ma tion cor re late with of the lower and up per part of the Vorotyshcha Salt For ma tion, re spec tively. Vialov (1965) con -
* Corresponding author: alfred.uchman@uj.edu.pl
Received: October 23, 2013; accepted December 10, 2013; first published online: February 28, 2014
Fig. 1. Lo ca tion maps
A – po si tion of the study area in the Al pine-Carpathian sys tem (af ter Picha, 1996, mod i fied by Oszczypko et al., 2006); B – tec tonic map of the Ukrai nian Carpathians (af ter Œl¹czka et al., 2006, sim pli fied); CF – Carpathian Foredeep, SK – Skyba (Skole) Nappe, CZ – Chornohora Nappe, RA – Rakhiv Nappe, MR – Marmarosh Mas sif, MK – Marmarosh Klippen Zone, MA – Magura Nappe, PK – Pieniny Klippen Belt, WH – Vihorlat-Gutin Vol ca nic Mas sif, TC – Trans-Carpathian De pres sion; C – geo log i cal map of Deliatyn-Lanchyn-Nadvirna area (af ter Jankowski et al., 2007), show ing lo ca tion of the sec tion D; D – geo log i cal map along the Prut River show ing lo ca tion of the sec tions A–C
sid ered that the bound ary be tween the Dobrotiv and Stebnyk for ma tions is at the base of the first “rose marls”.
All in ves ti ga tors have noted the pres ence of well-pre served mam mal and bird foot prints (see Vialov, 1966) and rain-drop im prints (Teisseyre, 1927; Dimitriéva et al., 1962; Vialov, 1965;
Deni sova, 1972). The most de tailed lithological and sedimento - logical stud ies of the Dobrotiv For ma tion has been made by Denisova (1959). Based on anal y sis of the sed i men tary struc - tures, she pro posed a deltaic or i gin for the Dobrotiv For ma tion, the sed i ments of which, dom i nated by an over whelm ing pre - dom i nance of zir cons in the heavy min er als frac tion, were de - rived from the East Eu ro pean Plat form.
De tailed min er al og i cal study of the Dobrotiv For ma tion was car ried out by Tkachenko (1961), who showed that the heavy min eral frac tion of the sand stones is dis tinctly dif fer ent from that of other Lower Mio cene units by a high pre dom i nance of chlorite and zir con over other heavy min er als. Sim i larly, mud - stone in ter ca la tions show a dom i nance of chlorite with small amounts of hydromicas, while other Lower Mio cene units are dom i nated by hydromicas.
GEOLOGICAL SETTING AND SECTIONS INVESTIGATED
Along the mar ginal part of the Ukrai nian Carpathians, a wide zone of folded Mio cene strata be longs to the Boryslav - -Pokuttya and Sambir nappes (Fig. 1B, C). The Boryslav - -Pokuttya Nappe, known also as the Mar ginal Fold Unit or the Boryslav-Pokuttya Folds, is ex posed in a nar row (up to 10 km) belt lo cated be tween the Skyba and Sambir nappes. This nappe may be traced from Ro ma nia in the SE to the Pol ish bor - der in the NW. This nappe is built of a com plex set of su per im - posed thrust sheets (Koltun et al., 2005). The Boryslav - -Pokuttya Nappe, com posed of flysch and molasse de pos its is over lain by the fron tal Carpathian thurst, overthrust on the Sambir Nappe, which com prises ex clu sively molasse de pos its.
Some au thors (Burov et al., 1978; Smirnov et al., 2000) con - sider the Boryslav-Pokuttya and Sambir nappes as rep re sent - ing the in ner part of the Carpathian Foredeep. Both nappes are over thrusted onto the Mid dle Mio cene (Badenian and Sarma - tian) autochthonous de pos its of the Bilche-Volytsia Zone, which rests di rectly on the fore land plat form base ment.
BORYSLAV-POKUTTYA NAPPE
This nappe is sub di vided into the Deliatyn and Runhury Sloboda sub-nappes (Kulchytsky et al., 1997). The Deliatyn Sub-nappe is com posed of Cre ta ceous-Lower Mio cene flysch, which is sim i lar to that of the Skyba Nappe. The youn gest Lower Mio cene flysch suc ces sion be longs to the Polyanytsia For ma tion, which is over lain by the Vorotyshcha For ma tion (NN3–?NN4 Zone; Andreyeva-Grigorovich et al., 2008a). The Vorotyshcha For ma tion (Fig. 2), up to 700-m-thick, com posed of grey mudstones and siltstones in ter ca lated with coarse - -grained sand stones and con glom er ates, con tains large blocks of im pure ha lite and anhydrite (Gurzhyi, 1969; Andreyeva - -Grigo rovich et al., 2008a). Lo cally, the up per part of the Voroty - shcha For ma tion is re placed by the Sloboda Con glom er ate (Oszczy pko et al., 2012 and ref er ences therein).
The Deliatyn Sub-nappe is overthrusted upon the Runhury Sloboda Sub-nappe. The lat ter is built mainly of the Sloboda Con glom er ate, Dobrotiv For ma tion and Stebnyk For ma tion.
Sev e ral bore holes show that the Sloboda Con glom er ate is un - der lain by the Vorotyshcha For ma tion, while the flysch de pos -
its, mainly of the Lower Menilite For ma tion, are rep re sented by the olistoliths and olistostromes, and olistoplaques (Kolodiy et al., 2004).
On the south ern limb of the Runhury Sloboda Anticline, the Sloboda Con glom er ate is un der lain by the Menilite For ma tion shales (Oligocene), and on its north ern limb by the salt-bear ing clays of the Vorotyshcha For ma tion (To³wiñski, 1950). The Sloboda Con glom er ate (Fig. 2) con tains ex otic blocks, boul ders and cob bles of Up per Pro tero zoic-Lower Pa leo zoic green phyllite, black schist, do lo mite, Ju ras sic white lime stone, and rare flysch-de rived olistoliths and olistostromes (Fedushchak, 1962;
Oszczy pko et al., 2012). The thick ness of the Sloboda Con glom - er ate in creases from 450–500 m in the Nadvirna area up to 1400 m at Runhury Sloboda. The Sloboda Con glom er ate passes into the ?Ottnan gian Dobrotiv For ma tion, which is up to 800-m-thick. This for ma tion is over lain by the var ie gated mudstones, marls and sand stones of the Stebnyk For ma tion (Karpatian–Early Bade nian; see Andreyeva-Grigorovich et al., 1995, 1997, 2008a). On the north ern limb of the Runhury Sloboda Anticline at Jabloniv, gyp sum lay ers up to 100-m-thick are sandwiched be tween the Sloboda and Dobrotiv for ma tions (To³wiñski, 1950).
SAMBIR NAPPE
The Sambir Nappe, up to 24 km wide and com posed of sev - eral thrust-sheets (Fig. 1), is cor re lated with the Sub-Carpathian Unit in Ro ma nia and the Stebnik Nappe in Po land (Oszczypko et al., 2006, 2008). This unit is overthrusted upon the Badenian - -Sarmatian de pos its of the outer zone of the Carpathian Fore - deep (Kolodiy et al., 2004). The Sambir Nappe suc ces sion is com posed mainly of the thick suc ces sion of “lower” Mio cene molasse of the Stebnyk and Balych for ma tions. The litho strati - graphy of its basal part is still un der dis cus sion. Sev eral au thors (Koltun et al., 2005; Andreyeva-Grigorovich et al., 2008b and ref - er ences therein) re gard the Vorotyshcha For ma tion as the old est di vi sion of the Sambir Nappe suc ces sion. This opin ion is sup - ported by bore holes, e.g. Hvizd 1 near Nadvirna and Urizh 6 (NE of Boryslav), where the Vorotyshcha For ma tion was pen e trated (Andreyeva-Grigorovich et al., 1997, 2008a). At the same time, poorly de vel oped coarse clastic de pos its of the Sloboda Con - glom er ate and Dobrotiv For ma tion oc cur lo cally in this unit. The Dobrotiv For ma tion is fol lowed by var ie gated marls, mudstones and sand stones of the Stebnyk For ma tion (Late Karpatian–Early Badenian; NN4–NN5 zones; Andreyeva -Grigorovich et al., 1997, 2008a). The Stebnyk For ma tion passes up into green ish and grey clays, mudstones and poorly ce mented sand stones of the Balych For ma tion, re garded by Bujalski (1930) as the north ern fa cies of the up per part of the Stebnyk For ma tion (see also Vialov, 1965). In the vil lage of Sadzhavka, 2 km E of Lanchyn, Berlavsky (fide Vialov, 1965) dis tin guished a suc ces sion of mas - sive sand stones in the up per part of the Stebnyk For ma tion, which are 40-m-thick. Also two units of dacitic tuffite are known from the vil lages of Krasna and Seredniy Maydan near Lanchyn (Bujalski, 1938), each 40–45-m-thick (Vialov, 1965). More over, a num ber of brine springs re lated to the “youn ger” Mio cene salt de - pos its of the Stebnyk For ma tion are known from the area (Buja - lski, 1938).
In the Kalush area, the Stebnyk and Balych for ma tions are un di vided and they pass up wards into the Bohorodchany For - ma tion, com posed of 100–250-m-thick grey marly mudstones and sand stones, which con tain abun dant Badenian plank tonic foraminifera and cal car e ous nannoplankton of the NN5 Zone (Andreyeva-Grigorovich and Kulchytsky, 1985; Andreyeva - -Grigorovich et al., 2003). In the south ern sec tor of the Kalush area, the Bohorodchany For ma tion passes up into the evapo -
ritic salt se quence of the Kalush For ma tion, or gyp sum and salt de pos its of the Tyras For ma tion, which be long to the NN5–NN6 zones (Andreyeva-Grigorovich et al., 2003).
The youn gest de pos its be long ing to the Kosiv (Up per Bade nian) and Dashava (Sarmatian) for ma tions have been doc u mented near Dobromyl. These de pos its are ter mi - nated by the Radych Con glom er ate, which con tain flysch clasts and is dated to the NN6–NN9 zones (Andreyeva- Grigorovich et al., 2008a).
SECTIONS STUDIED
The sec tions stud ied crop out in the Prut River val ley (Fig. 1D), north of Deliatyn, be tween the vil lages of Zarich - chya and Lanchyn, where al most con tin u ous ex po sures are pres ent for about 8 km along the river banks. These ex po - sures dis play folded Mio cene de pos its of the Runhury Sloboda Anticline within the Boryslav-Pokuttya Nappe. The core of the anticline is formed by the Sloboda Con glom er ate, while the limbs are oc cu pied by the Dobrotiv and Stebnyk for - ma tions. More over, the tran si tion be tween the Sloboda Con - glom er ate and the Dobrotiv For ma tion was stud ied in the Nadvirna area, as shown in Oszczypko et al. (2012).
In the Prut val ley, the bound ary be tween the Boryslav- Pokuttya and Sambir nappes is not clear. Geo log i cal maps (Jankowski et al., 2007; see also Hnylko, 2012) show this bound ary within the Stebnyk For ma tion on the north limb of the Runhury Sloboda Anticline, ca. 6 km north of Deliatyn.
The sec tions stud ied of the Dobrotiv For ma tion in the Boryslav-Pokuttya Nappe are as fol lows (Fig. 1C, D):
– sec tion A – south ern limb of the Runhury Sloboda Anticline, south of the of the Oslava Stream in flow to the Prut River at Dobrotiv (GPS co or di nates: from N48°32.161’; E24°41.080’ to N48°32.156’;
E24°40.819’) to wards Deliatyn (GPS co or di nates:
from N48°32.049’; E24°38.854’ to N48°33.033’;
E24°45.282’). This sec tion dis plays a tran si tion of the up per most part of the Sloboda Con glom er ate into the Dobrotiv For ma tion and con tin ues through the Dobro - tiv For ma tion up to the Stebnyk For ma tion;
– sec tion B – right and left banks of the Prut River be - tween the Oslava Stream in flow to the Prut River to the ca ble bridge at Dobrotiv (GPS co or di nates: from N48°32.161’; E24°41.080’ to N48°32.336’; E24°43.461’).
– sec tion C – left bank of the Prut River at Lanchyn near the bridge (GPS co or di nates: N48°33.015’; E24°45.155’ to N48°33.117’; E24°45.117’). This sec tion dis plays a tran - si tion from the up per most part of the Vorotyshcha For ma - tion through the Sloboda Con glo m er ate and the Dobrotiv For ma tion type sand stones, which dis play strongly re - duced thick nesses, up to the base of the Stebnyk For ma - tion rep re sented by rose -col oured marly shales;
– sec tion D – cliffs along the left bank of the Bystrytsia Nadvirnanska River at Nadvirna (GPS co-or di nates:
N48°32.240’; E24°41.012’). A tran si tion from the Slobo da Con glom er ate to the Dobrotiv For ma tion can be ob - served here.
In ves ti ga tions of sec tions A and B en abled prep a ra tion of two sed i men tary logs of the Dobrotiv For ma tion on both limbs of the Runhury Sloboda Anticline. The log of the south ern limb is con tin u ous, cov er ing the pro file de scribed by Vialov (1965, p:
54–59). The log of the north ern limb of the anticline is com bined due to tec tonic dis place ment along the Prut River, where the sec tion is ob scured over a dis tance of 450 m (GPS co or di nates:
from N48°32.445’; E24°42.558’ to N48°32.407’; E24°42.876’).
This area is crossed by a trans verse NW–SE fault, which dis - places the limb of the anticline north wards by ap prox i mately 500 m. This re sulted in du pli ca tion of thick ness on the north ern limb for about 350 m.
Sec tion C dis plays the core of the Lanchyn Anticline, prob a - bly be long ing to the Sambir Nappe. The south ern limb of the anticline is com posed of grey brecciated mudstones of the Vorotyshcha For ma tion (see Andreyeva-Grigorovich et al., 2008a). This for ma tion is over lain by the Sloboda Con glom er - ate and Dobrotiv For ma tion of strongly re duced thick ness:
25–30 m and 22–25 m re spec tively. The Sloboda Con glom er - ate be gins with grey ma trix- and clast-sup ported me dium- grained con glom er ates with sharp-edged and semi-rounded clasts, 2–5 cm across, the beds of which dip subvertically to - wards the south. The clasts are com posed of grey sand stones and mudstones with small ad mix tures of quartz and car bon - ates. These con glom er ates, de pos ited by de bris flows, are 10–15-m-thick. They are over lain by a 15-m-thick suc ces sion of thick-bed ded (0.7–1.0 m) fine con glom er ates, with a muddy - -sandy ma trix. Their beds show a tran si tion to fine- to coarse - -grained sand stones, in beds 10–30-cm-thick. Lower sur faces of the con glom er ate beds are usu ally flat and only lo cally channelized. These beds are over lain by 10 m of, thick-bed ded, coarse-grained, structureless sand stones, which are fol lowed Fig. 2. Lithostratigraphic scheme of the Borislav-Pokuttya
and Sambir nappes (based on Andreyeva-Grigorovich et al., 2003, 2008a, b; Oszczypko et al., 2006, sup ple mented)
by 12 m of thin- to me dium-bed ded, fine-grained sand stones with in ter ca la tions of dark or grey mudstone, re sem bling these from the up per most part of the Dobrotiv For ma tion. Di rectly above the Dobrotiv For ma tion-type de pos its, grey and rose-col - oured shales of the basal por tion of the Stebnyk For ma tion are ex posed. Such a large re duc tion in thick ness of the Sloboda and Dobrotiv for ma tions in sec tion C can be caused by both tec tonic trun ca tion and sed i men tary pinch ing out.
Be neath the bridge, on the north ern limb of the anticline, the Vorotyshcha For ma tion is over lain by a sub-ver ti cal SW-dip - ping, over turned packet of blue-grey, non-cal car e ous shales with thin anhydrite lenses (GPS co or di nates: from N48°33.066’;
E24°45.375’ to N48°33.125’; E24°45.528’). This suc ces sion is known as the “Lanchyn blue com plex” (Vialov, 1965), which spo rad i cally con tains in ter ca la tions of thick-bed ded, coarse- grained, amal gam ated sand stones, with palaeotransport from the ESE (110°; see also Andreyeva-Grigorovich et al., 2008a).
FACIES CHARACTERISTICS
LITHOLOGY AND SEDIMENTARY STRUCTURES
The low est part of the Dobrotiv For ma tion (unit A in this pa - per) was re garded as a tran si tion from the Sloboda Con glom er - ate (Koliadnyi, 1951). It is 123-m-thick on the south ern limb of the Runhury Sloboda Anticline (Fig. 3), 90-m-thick on its north ern limb (Fig. 4) and at least 30-m-thick in the Nadvirna sec tion (Fig. 5). It con tains beds of grey or brown ish polymictic con glom - er ates of the same type as in the Sloboda Con glom er ate (for de - tails see Oszczypko et al., 2012), but mostly finer and com monly ma trix-rich. These beds are up to a few metres thick, and at Nadvirna up to 10-m-thick. There are also brown ish or grey, thin- to thick-bed ded, me dium- or coarse-grained, poorly-sorted, lo - cally muddy sand stones. Some cross-lam i nated beds dis play a tran si tion from con glom er atic sand stone or fine con glom er ate at the base to coarse-grained sand stone at the top. In verted graded bed ding (Fig. 6), from coarse- grained sand stone to fine- grained con glom er ate, is less com mon. Some of beds show large-scale (over 30 cm) cross-bed ding. Thicker sand stone beds are in ter ca lated with pack ets of grey or red dish, thin- to me - dium-bed ded, fine-grained, mas sive, par al lel- or rip ple-lam i nated sand stones, which are in ter ca lated with grey or red dish cal car e - ous mudstones.
The main part of the Dobrotiv For ma tion (unit B in this pa per or the lower part of the for ma tion in Koliadnyi, 1951) is 540-m-thick on the south ern limb of the Runhury Sloboda Anticline (Fig. 3), and 645 m or 690-m-thick on the north ern limb (Fig. 4). It dis plays mo not o nous light grey, cal car e ous de pos its.
A few sand stone beds and rare marlstone beds are yel low ish on weath ered sur faces. Three ba sic lithofacies of these de pos - its in clude (Fig. 7):
1 – very thin- and thin-bed ded mudstone-siltstone in ter ca la - tions, in which beds are 1–2 cm or 2–5-cm-thick;
2 – mudstone-siltstone in ter ca la tions interbedded with very fine- and fine-grained, thin-bed ded sand stones;
3 – very fine- and fine-grained, me dium- to thick-bed ded sand stones interbedded with mudstones and siltstones.
These lithofacies change through the sec tions, with grad ual tran si tions in most cases. More over, the higher part of the for - ma tion – south ern limb of the Runhury Sloboda Anticline (Fig.
3) con tains thin and me dium beds of marl stone (see also Vialov, 1966: fig. 9), which are com posed of marly silt or very fine-grained cal car e ous sand stone at the base and muddy pass ing up into grey marlstone at the top. The beds are yel low on weath ered sur faces.
Cross-sec tions and sur faces of beds dis play (Fig. 8) depo - sitional, ero sive, deformational and biogenic sed i men tary struc - tures (for their or i gin and clas si fi ca tion see Allen, 1982; D¿u -
³yñski, 1996, 2001). Many of these were rec og nized by Deni - sova (1959) and Vialov (1965, 1966) but de scribed us ing other no men cla ture. The sed i men tary struc tures are rep re sented mostly by par al lel or gently wavy lam i na tion, which is vis i ble in sand stones and finer de pos its. How ever, some beds are mac - ro scop i cally mas sive. Larger scale cross-bed ding is rare, rip ple lam i na tion is more fre quent.
Some up per bed ding sur faces dis play dif fer ent rip ple-marks (pre served also as casts; see Zuber, 1888, 1915; Teisseyre, 1927; Denisova, 1959; Dimitriéva et al., 1962), which can be sym met ri cal or asym met ri cal, with straight, wind ing or bi fur cat - ing crests. Linguloid rip ples are very rare. Vialov (1965, 1966) called the Dobrotiv For ma tion a “mu seum of rip ple-marks”. The sym met ri cal rip ples are in ter preted as wave rip ples. More over, in ter fer ence rip ples have been found, in clud ing com bi na tions of cur rent and wave rip ples.
Some sand stone dis play sharp lower bed ding sur faces, while oth ers show dif fuse tran si tions. Most sand stone beds grad u ally pass up into finer sed i ments. Al most all beds are tab - u lar at out crop scale (over a dis tance of up to 20 m). Ero sional struc tures are gen er ally rare. Small scour casts oc cur very rarely in the fine-grained, heterolithic de pos its as do shal low chan nel-fills at bed scale. The in fill ing sand stones pinch out and can con tain rip-up mud clasts.
Fine ero sional struc tures are rep re sented by groove marks (Fig. 8). Some of these dis play sec ond ary grooves along the main one. Rarely, flute casts have been ob served. These oc cur on lower bed ding planes of sand stones and in di cate trans port to the east.
Deformational struc tures (Fig. 9) are rep re sented pri mar ily by ball-and-pil low struc tures (called “rounded con cre tions” by Zuber, 1888, or curved and twisted bed ding by Vialov, 1966), which are pres ent in some thicker beds. Some sand stone pil - lows are dis mem bered and “float” in finer ma trix. Smaller load struc tures can be seen on some lower bed ding sur faces, oc ca - sion ally in as so ci a tion with groove marks and other ero sional struc tures. More over, a few beds of debrite (1–2-m-thick) oc cur in the mid dle part of the units. They are com posed mostly of muddy ma trix with float ing blocks of sand stone. Ball-and-pil low struc tures are re ferred mostly to load ing pro cesses (Allen, 1982), which can be trig gered by seis mic shock (e.g., Rodrí - guez-Pascua et al., 2000).
A few sand stone beds con tain muddy intraclasts and larger, car bon ized plant frag ments.
Finer deformational struc tures in clude rain drop im prints and their casts (see also Teisseyre, 1927; Koliadnyi, 1951; Deni - sova, 1959), which oc cur at sev eral ho ri zons, com monly in as - so ci a tion with in ver te brate and ver te brate trace fos sils.
The higher part of the Dobrotiv For ma tion passes into the Stebnyk For ma tion, that is char ac ter ized by red dish mudstones and fine-, me dium-, and coarse-grained sand stones, that are less well sorted than in those in the Dobrotiv For ma tion (Fig. 3).
The bound ary be tween the for ma tions is nor mal and may be placed at the base of the first red dish mudstone layer or the first coarse-grained sand stone bed. The lat ter is pre ferred, be cause the oc cur rence of the coarse-grained, poorly sorted sand stones in di cates an im por tant fa cies change, as so ci ated with sed i men - ta tion in flu vial chan nels. Such sand stones be gin in the grey and dark grey mudstones of Dobrotiv For ma tion type. The red dish mudstones can oc cur a few tens of metres above. More over, the top of the Dobrotiv For ma tion (ca. 100-m-thick) that is shale-dom i nated, con tains mudcracks, and a few beds of cross- bed ded, me dium-grained sand stone have been dis tin guished by Koliadnyi (1951) as within the up per part of this for ma tion.
TRACE FOSSILS
Ver te brate trace fos sils (Fig. 10) from the Dobrotiv For ma - tion have were noted and il lus trated by Koliadnyi (1951) and de - scribed in de tail by Vialov and Flerov (1952, 1953, 1954), Hizhniakov (1954), Denisova (1959, 1970) and Vialov (1960, 1966) and il lus trated by Dimitriéva et al. (1962). They in clude foot prints and trackways of ar tio dac tyl mam mals (one ichno - species of Gazellipeda Vialov, one ichnospecies of Cervipeda Vialov and two ichnospecies of Pecoripeda Vialov), angulate mam mals (one ichnospecies of Hippipeda Vialov), car niv o rous mam mals (two ichnospecies of Bestiopeda Vialov), and sev eral foot prints and trackways of birds (three ichnospecies of Avipe - da Vialov).
Dur ing the field work, sev eral mam mal foot prints (Gazellipe - da) and bird foot prints (Avipeda) have been found. They are pre - served on the up per sand stone sur faces of or as casts on their lower sur faces, com monly in as so ci a tion with rain drop im prints or their casts. More over, a low-di ver sity as sem blage of sim ple, hor i - zon tal in ver te brates bur rows has been found. The se were noted by Teisseyre (1927). All these trace fos sils are the sub ject of a sep a rate pa per in prep a ra tion.
BEDDING TRENDS
Long in ter vals of the sec tions stud ied are mo not o nous, with out dis tinct thick en ing or thin ning trends in the ar range ment of beds. In some in ter vals, only a few metres-thick, thick en - Fig. 3. Sed i men tary log of the Dobrotiv For ma tion along the Prut River, south ern limb
of the Runhury Sloboda Anticline (sec tion A)
ing-up or thin ning up trends can be ob served, as well as sym - met ri cal trends or iso lated, thicker beds with out any trend con - text. Al ter na tions of sets of thicker and thin ner beds can be also ob served, with out any or der.
How ever, there are a few ex cep tions. At the base of the for - ma tion (unit A), a thick en ing-up packet can be seen near the Oslava River in flow to the Prut River (Fig. 11). It is ca. 10-m -thick. Thick beds at the top dis play ero sional bases with shal - low in ci sion into the un der ly ing de pos its, pinch ing out, cross -
-bed ding and load struc tures. The tops of some beds are con - vex-up, while their bases are flat. This in ter val is capped by thin- and me dium-bed ded rhyth mic in ter ca la tions of sand stones and siltstones and mudstones.
An other thick en ing in ter val can be seen at 237–264 m of sec - tion A (N limb of the Runhury Sloboda Anticline; Fig. 4), where beds at the top dis play com mon ball-and-pil low struc tures. At some places, pack ets of sand stone about 10-m-thick rest on thin- or me dium bed ded strata with out any grad ual tran si tions.
Fig. 4. Sed i men tary logs of the Dobrotiv For ma tion along the Prut River, north ern limb of the Runhury Sloboda Anticline (sec tion B) and south ern limb of the Lanchyn Anticline (sec tion C)
VoF – Vorotyshcha For ma tion, SlCg – Sloboda Con glom er ate, DoF – Dobrotiv For ma tion, Steb. Fm. – Stebnyk For ma tion; df – delta front, dp – delta plain; for other ex pla na tions see Fig ure 3
DISCUSSION
SEDIMENTARY ENVIRONMENT
The sed i men tary en vi ron ment of the Dobrotiv For ma tion was de ter mined as deltaic by Denisova (1959), but with out anal y sis or dis cus sion.
In the lower part of the for ma tion (unit A), above the Slobo - da Con glom er ate, coarse-grained to fine-grained con glom er - atic sed i ments were de pos ited. The up per part of the con glom - er ate was de pos ited on an al lu vial fan and the top most part on a
Fig. 5. Sed i men tary logs of the Sloboda Con glom er ate – Dobrotiv For ma tion tran si tion,
along the Bystry tsia Nadvinanska River at Nadvirna (sec tion D) For ex pla na tions see Fig ure 3
Fig. 6. Ex am ples of fan-delta fa cies
A – bed show ing in verted graded bed ding from coarse-grained sand - stone to fine-grained con glom er ate; B – large-scale cross -bed ding in a bed of coarse-grained muddy sand stone; C – in the lower part, two fine-grained con glom er ate to coarse-grained sand stone beds show - ing cross-bed ding, which in di cate trans port from the south; D – in ter - ca la tion of sand stone and red dish-grey mudstones
Fig. 7. Ex am ples of deltaic fa cies
A – heterolithic de pos its – rhyth mic in ter ca la tions of mudstone, siltstone and very fine-grained sand stone; B – small chan nel-fill in heterolithic de pos its; C – in ter ca la tions of mudstone, siltstone and very fine-grained sand stone, thicker than in A or B; D – beds com posed of very fine-grained sand stone at the base with a tran si tion to marlstone at the top; E – packet of thick-bed ded fine-grained sand stone in ter ca - lated with thin ner-bed ded clastic de pos its; F – packet of thick-bed ded fine-grained sand stones in ter ca lated with thin ner-bed ded clastic de - pos its; note pinch ing out of two thin ner beds in ter ca lated be tween two thick beds; the higher thick bed trun cates the two thin ner beds; G – chan nel bed wedge, which con tains rip-up mudstone clasts
fan-delta (Oszczypko et al., 2012). The low est part of the for ma - tion, where coarse sed i ments can be found, was likely de pos - ited in a mor i bund fan-delta, with a well-de vel oped delta plain, in which tetrapod foot prints and rain drop im prints are pre served.
Fine con glom er ates and coarse sand stones were de pos ited in flu vial chan nels (as de bris flows?). In creas ing num bers of fine- grained rip pled sand stones and finer clastics point to de po si tion un der wa ter (sub aque ous part of the fan-delta).
The in ter pre ta tion of the main part of the Dobrotiv For ma tion (unit B) as deltaic sed i ments can be main tained. How ever, sev - eral de tails need to be clar i fied. The sed i men tary struc tures point to flow ing wa ter as the main mech a nism of sed i ment trans port and de po si tion, mainly in the lower flow re gime, in which sed i ment was trans ported by trac tion. These were oc ca - sional grav ity flows, which re sulted in the de po si tion of debrites.
Spo radic oc cur rences of sym met ri cal ripplemarks sug gest Fig. 8. Some bed ding-sur face struc tures
A – groove marks; B – groove marks, load struc tures and ferruginization af ter py rite con cre tions; C – flute casts;
D – load struc tures; E – in ter fer ence of cur rent (smaller) and wave (larger) rip ples; F – large wave rip ples; G – very small cur rent rip ples punc tu ated by ver ti cal bur rows; H – three sur faces (1–3) of dif fer ent cur rent rip ples show ing dif fer ent di rec tions of flow
wave ac tion in shal low wa ter. Thick en ing-up trends in bed sets from mudstone-dom i nated to sand stone-dom i nated pack ets, mostly 10–20-m-thick, though very rare, are typ i cal of deltaic sed i ments. They re flect a progradation of delta from prodelta to delta-front sands. The ball-and-pil low struc tures also are the char ac ter is tic fea ture of deltaic de po si tion (e.g., Hubert et al., 1972; Flores and Erbenbeck, 1981; Rajchl, 1999). Gen er ally, the delta-front sands are poorly rep re sented in the Dobrotiv For ma tion. Such a sit u a tion might be caused by ero sional trun - ca tion at the tops of thick en ing-up parasequences (Einsele, 2000), but this is not the case in the Dobrotiv For ma tion, be -
cause the thicker sand stone beds and their ad ja cent de pos its, in ter preted as delta-front sands, are capped by heterolithic de - pos its con tain ing mam mal foot prints and rain drop im prints in di - cat ing dry ing ter res trial con di tions, which can be re ferred to a delta plain. Some thicker sand stone beds on the delta plain are prob a bly flu vial chan nel fills and thin ner sand stone beds were likely de pos ited in cre vasse splays.
Soils did not de velop on the ex posed ar eas, prob a bly due fre quent ep i sodes of sed i men ta tion. We saw no signs of des ic - ca tion, such as mudcracks, though Vialov (1965: pl. 11) noted some in an unspec i fied part of the for ma tion. This in di cates a Fig. 9. Deformational struc tures
A – ball-and-pil low struc tures in a packet of thick-bed ded sand stones; B – a few lev els of ball-and-pil low struc tures in thick-bed ded sand - stones; C – ball-and-pil low struc tures; D – ini tial pil low ing on a bed ding sur face; up rooted pil lows in mudstone;
E – cha otic mudstone with de formed frag ments of sand stone beds – a slump
hu mid cli mate as shown by com mon rain drop im prints. The pres ence of struc tures re lated to ice crys tals (Vialov, 1965;
Denisova, 1970), sug gests a mod er ate cli mate.
The coastal part of the delta was prob a bly a mi gra tion path for her biv o rous mam mals. Abun dant plant de tri tus in di cates veg e tated ar eas be hind the site of de po si tion.
In ter est ingly, there is al most no ex it ing bioturbational dis tur - bance of the fine-grained sed i ments in ter preted as prodelta.
Sig nif i cant bioturbation of prodelta sed i ments, with the oc cur - rence of typ i cally ma rine trace fos sils such as Chondrites or Phycosiphon is com mon (Hovikoski et al., 2008). The most con vinc ing ex pla na tion is brack ish con di tions in the ba sin, and maybe ox y gen de fi ciency. It is sig nif i cant that ma rine micro -
fossils are al most ab sent from the Dobrotiv For ma tion. Only Koliadnyi (1951) noted poorly pre served and low-di ver sity fora - minifers but it is not clear if they are autochthonous or ex humed from older sed i ments. All the sam ples we col lected ap peared bar ren of foraminifers and nannoplankton.
The poor de vel op ment of the delta-front sands, with their mostly very fine- and fine-grained na ture, finer than in many mouth bars of dif fer ent types (com monly me dium- and coarse - -grained sand; cf. Field ing et al., 2005), in clud ing many lac us - trine del tas (e.g., Thomas et al., 2006), sug gests a mud-dom i - nated delta on a mud-dom i nated coast. Such depositional set - tings are still poorly un der stood, but known from re cent and fos - sil ex am ples (Augustinus, 1980; Hovikoski et al., 2008). Delta - Fig. 10. Raindrop struc tures and trace fos sils
A – rain drop casts; B – raindrop im prints; C – wind ing in ver te brate bur rows; D, E – bird foot prints;
F – Gazellipeda – mam mal foot print; G – mammal trackway Gazellipeda, bird foot prints, rain drop casts
-front fa cies in such del tas can be com posed mostly of mud (Tanabe et al., 2003). Del i cate sed i men tary struc tures, such as par al lel and cross-lam i na tion in mudstones and siltstones in the Dobrotiv For ma tion, re sem ble those from mud banks of the Su - ri nam coast (NE South Amer ica), where mud-dom i nated shelf sed i ments pre vail, though these are partly bioturbated (Rine and Ginsburg, 1985). Deltaic sed i ments that ac cu mu lated in shal low lakes, with very lim ited ac com mo da tion space, do not form typ i cal thick en ing-up trends (Tye and Coleman, 1989).
BASIN DEVELOPMENT CONTEXT
The intra-Burdigalian fold ing and up lift of the Outer Carpa - thians were re lated to the north-eastwards trans la tion of the Alcapa and Tisza-Dacia microplates in re sponse to the roll- back of the Carpathian subduction slab (Zoetemeijer et al., 1999; Ziegler et al., 2002; Rasser et al., 2008). This was ac com - pa nied by north- and north-east-di rected nappe trans port and the de vel op ment of the pe riph eral flex ural Carpathian Foredeep Fig. 11. Trends in bed ding
A – gen er ally thick en ing-up suc ces sion of beds in ter preted as a mouth bar; out let of Oslava; square in di cates de tail in B; B – de tail of A – con - cave-up lithosome of thick-bed ded sand stone; C – lat eral equiv a lent of A on the left side of the Prut River, op po site to the Oslava River out let;
top of the Sloboda Con glom er ate by ham mer; D – a suc ces sion of thin and me dium beds of sand stones in ter ca lated with mudstones and siltstones; here, mam mal foot prints, bird foot prints and rain drop im prints oc cur; this suc ces sion is in ter preted as of delta plain fa cies; thick sand stone at the top may be a river chan nel-fill; E – a suc ces sion of beds with out any dis tinct thick en ing or thin ning trends
along the ad vanc ing (mar ginal) part of the accretionary prism as well as on the plat form (Oszczypko, 1998, 1999; Oszczypko and Oszczypko-Clowes, 2012; Fig. 12).
In many cases, the es ti mated weight of the orogen thrust over load and foredeep de pos its (i.e. sur face and top o graphic loads) is not suf fi cient to ex plain the ob served flex ural bend ing of the fore land (lower) lithospheric plate (Royden, 1988). Flex - ural mod el ling stud ies for the Pol ish and Ukrai nian Carpathians (Royden and Burchfiel, 1989; Krzywiec and Jochym, 1997) sug gest that deep pro cesses and as so ci ated subsurface loads were most im por tant for the ob served pres ent-day flex ural bend ing of the fore land lithospheric plate in this orogenic belt (see also Kov«è et al., 1989; Oszczypko et al., 2006 and ref er - ences therein). The sub si dence of the ini tial (Ottnan - gian–Karpatian) fore land ba sin was re lated to the deep sub - surface load. At that time the rate of sub si dence at the front of the Ukrai nian Outer Carpathians reached at least 2000 m/Ma (Oszczypko, 1998). Such rapid sub si dence was com pen sated by a high rate of ac cu mu la tion as re flected by ter res trial and shal low-wa ter sed i men ta tion of the Sloboda Con glom er ate and the Dobrotiv and Stebnyk for ma tions.
De po si tion of the un der ly ing Sloboda Con glom er ate as an al - lu vial fan and fan-delta is re lated to high-re lief forebulge el e va tion that orig i nated at an early stage of Carpathian Foredeep de vel - op ment (Oszczypko et al., 2012). The tran si tion from al lu vial fans via a short fan-delta phase to fine-grained sed i men ta tion re flects a sig nif i cant change in sed i ment sup ply from coarse clastic to very fine clastic de pos its. This sug gests that the re lief in the source area be came much lower (Vialov, 1965: p. 80); how ever, the source area was still ef fi cient and sup plied the ba sin with fine and very fine sand, silt and clay, which may have de rived from eroded Carpathian flysch, though this is an open ques tion.
The ba sin was shal low, with com monly ex posed muddy sur - faces as in di cated by the tetrapod foot prints and rain-drop im - prints. The small wa ter depth and large ac com mo da tion space
may ex plain the poor de vel op ment of thick en ing-up deltaic cy - cles, which gen er ally re sult from progradation. The large ac com - mo da tion space was caused by tec tonic sub si dence which bal - anced sed i ment ac cu mu la tion. The sub si dence was prob a bly caused both by subsurface as well as by thrust up loading of ad - vanc ing Carpathian nappes dur ing the ini tial stage of de vel op - ment of the Carpathian Foredeep (Oszczypko et al., 2006); how - ever, the sub si dence may have been en hanced by lo cal load ing of the Sloboda Con glom er ate, which is up to 1400-m-thick, un - der lies the Dobrotiv For ma tion and is lim ited to the same area (Oszczypko et al., 2012). As a re sult of such stack ing thick se - quences (800 m) could ac cu mu late in a small area.
The delta of the Dobrotiv For ma tion passed into flu vial en vi - ron ments, which are rep re sented by the Stebnyk For ma tion. The lat ter dis plays well-de vel oped flu vial chan nel fa cies of coarse - -grained, poorly sorted sand stones oc cur ring within fine - grained overchannel sed i ments, which cover much larger ar eas than does the Dobrotiv For ma tion. Their red col our and the com mon pres ence of mudcracks in di cate a change to a drier cli ma tic. The first ma rine in gres sions are marked at the top of the Stebnyk For - ma tion by the oc cur rence of ma rine micro fossils.
A sim i lar though older suc ces sion of sed i ments is known from the Molasse Fore land Ba sin of the North ern Alps (Rasser et al., 2008). The Polyanytsia and Vorotyshcha for ma tions (Late Aquitanian–Burdigalian) cor re spond to the Lower Ma rine Mo - lasse (Rupelian), while the Sloboda Con glom er ate and Dobro tiv and Stebnyk for ma tions (Late Burdigalian–Early Lan ghian) may be re ferred to the Lower Fresh wa ter Molasse (Chattian–Aqui - tanian) in the Molasse Fore land Ba sin. In par tic u lar, the Sloboda Con glom er ate and Dobrotiv For ma tion form a clastic wedge which shows a fin ing and thin ning up wards mega sequence (Vialov, 1965), sim i lar to that of the Lower Fresh wa ter Molasse.
The strati graphic shift of this type of sed i men tary de vel op ment is con sis tent with west-east mi gra tion of fold ing and thrust ing of the Al pine-Carpathian orogens (Kováè et al., 1989).
Fig. 12. Late Ottnangian-?Karpatian palinspastic palaeo ge ogra phy of the fore land of the Pol ish and Ukrai nian Carpathian Foredeep (based on Oszczypko and Oszczypko-Clowes, 2003;
Oszczypko et al., 2006, 2012, sup ple mented)
CONCLUSIONS
The Dobrotiv For ma tion (up per Lower Mio cene Mio cene;
700–800- m- thick) is in ter preted as a deltaic suc ces sion show - ing a tran si tion from a fan-delta (top of the Sloboda Con glom er - ate) to a flu vial coastal plain (Stebnyk For ma tion). It was de pos - ited on sub sid ing, mar ginal part of the Outer East ern Carpa - thians. The delta was mud-dom i nated, with poorly de vel oped thick en ing-up trends, and de pos ited in shal low wa ter un der a hu mid cli mate. Ep i sodes of sed i ment emer gence are in di cated
by tetrapod foot prints and rain drop im prints. The un der ly ing Sloboda Con glom er ate, and the Dobrotiv and Stebnyk for ma - tions, form a clastic wedge of thin ning- and fin ing-up wards suc - ces sions.
Ac knowl edge ments. Field work was sup ported by the Jagiellonian Uni ver sity (DS funds). Y. Koltun (Lviv, Ukraine) and M. Kováè (Bratislava, Slo vak Re pub lic) pro vided use ful re - views and im prove ments.
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