Geo log i cal Quar terly, 2017, 61 (4): 697–722 DOI: http://dx.doi.org/10.7306/gq.1359

The po si tion and age of flysch de pos its in the Cri mea Moun tains (South ern Ukraine)

Nestor OSZCZYPKO1, *, Andrzej ŚLĄCZKA1, Ihor BUBNIAK2, Barbara OLSZEWSKA3 and Małgorzata GARECKA3

1 Jagiellonian Uni ver sity, In sti tute of Geolog i cal Sci ences, Gronostajowa 3a, 30-001 Kraków, Poland 2 Ivan Franko Na tional Uni ver sity of Lviv, Geolog i cal Fac ulty, Hrushevsky 4, Lviv 79005, Ukraine 3 Polish Geo log i cal In sti tute – Na tional Re search In sti tute, Skrzatów 1, 31-560 Kraków, Po land

Oszczypko, N., Ślączka, A., Bubniak, I., Olszewska, B., Garecka, M., 2017. The po si tion and age of flysch de pos its in the Cri- mean Moun tains (South ern Ukraine). Geo log i cal Quar terly, 61 (4): 697–722, doi: 10.7306/gq.1359

The Crimean Moun tains (CM) are regarded as part of the Al pine-Himalaya orogenic belt related to the col li sion of the Eur- asian and Af ri can plates. Our research in the CM has al lowed con firm ing the ex is tence of at least two flysch for ma tions of dif fer ent ages: the Taurida Flysch For ma tion (Up per Tri as sic/Lower–? Mid dle Ju ras sic) and the Sudak For ma tion (up per- most Ju ras sic/Lower Cre ta ceous) in the western and east ern sec tors of the CM, re spec tively. Af ter the Mid dle Ju ras sic vol- canism, the fresh wa ter claystones with coal-bear ing in ter ca la tions, as well as lo cal al lu vial fan con glom er ates were de pos ited. Then, follow ing the Oxfordian/Kimmeridgian ma rine trans gres sion, three sepa rated Tithonian/Berriasian car bon- ate plat forms de vel oped: Baydarska, Chatyr-Dag and Demerji/Karabi. At the turn of the Late Ju ras sic, the deep-water Sudak Ba sin (east ern sec tor of the CM) began to develop in the east ern pe riph ery of the Demerji/Karabi car bon ate plat form. This ba sin, dom i nated by turbiditic de po si tion, was prob a bly con nected with the Great Cau ca sus sed i men tary sys tem. Fi nally, dis tal flysch sed i men ta tion in the Sudak Basin was fol lowed by de bris-flow de pos its, with huge blocks of Up per Ju ras sic lime- stones. These blocks were derived from de struc tion of the Karabi car bon ate plat form. Dur ing the Berriasian/Valanginian, the east ern sec tor of the CM began to sub side. As a result, both carbon ate platforms (western CM) and the debris flow fans of the Sudak Ba sin (east ern CM) were over lain by marly shales and/or dis tal turbidites. This type of de po si tion lasted until the Aptian/Albian. In the post-Albian pe riod, the Alushta-Salgir tec tonic zone was trans formed into a SE-dip ping thrust fault with at least 10 km am pli tude of overthrusting.

Key words: Ukraine, Crimean Mts., stra tig ra phy, micropalaeontology, flysch.

INTRODUCTION Tak ing into ac count our ex pe ri ence in study ing the Outer Carpathians flysch, we be came in ter ested in the ex pla na tion of the con tro versy re lated to the Tauric Flysch. With this in mind, Flysch sed i ments, known al ready for more than 150 years we have con ducted our stud ies in the years 2010–2013, dur ing (from Dubois de Montpereaux, 1837), play an im por tant role in the three short, but in tense field work campaings. Our in ter est the geo log i cal struc ture of the Cri mean Mts. These de pos its has been fo cused on the fol low ing main ques tions: were tra di tion ally re garded as the Tauric Flysch of Late Tri as- – litho- and biostratigraphic stud ies of the Tauric Flysch; sic/Early Ju ras sic age (Muratov et al., 1969; Muratov, 1972). – its re la tion ships to over ly ing lithostratigraphic units; This age has been chal lenged by Popadyuk and Smirnov – lat eral and lon gi tu di nal spatial vari abil ity of the Tauric (1991), who con cluded Early Cre ta ceous age. This sparked a Flysch, es pe cially along the west-east di rec tion. lively dis cus sion (e.g., Popadyuk et al., 2010, 2013a, b, 2014; We started from the lo cus typicus of the Tauric Flysch: the Oszczypko et al., 2012b, c) un til Sheremet et al. (2014, 2016a), Alma and Bodrak val leys and along the Black Sea coast, be - on the basis of cal car e ous nannoplanton anal y ses of flysch-like tween the Cape of Sarych in the west and the vil lage of de pos its in the east ern sec tor of the CM, in cluded both the Rybache in the east (Oszczypko et al., 2012b, c). Then, we tried Tauric For ma tion and the Lower Cre ta ceous flysch de pos its of to rec og nize the re la tion ship be tween the Tauric Flysch and the the east ern sec tor of the Cri mea into the Tauric Group. Ju ras sic?/Early Cre ta ceous flysch of the east ern sec tor of the CM (Oszczypko et al., 2012c). In Rus sian pub li ca tions, the Me so zoic flysch is known as the Tavricheskaya svita, se ries, group or sim ply Taurica. We sug - gest in tro duc ing a new term – the Taurida Flysch For ma tion * Corresponding author, e-mail: [email protected] (TFF), which is more con sis tent with the for mal litho stra ti graphic Received: July 20, 2016; accepted: March 16, 2017; first published stan dards, rec om mend ing a geo graph ical noun. In this case it online: May 10, 2017 will be the Taurida – an an cient Greek name of the Crimean Peninsula. 698 Nestor Oszczypko, Andrzej Ślączka, Ihor Bubniak, Barbara Olszewska and Małgorzata Garecka

GEOLOGICAL SETTING First de tailed in for ma tion on tec tonic de for ma tions of the Tauric and Eski-Orda se ries, in the Bodrak Val ley, was given by Koronovsky and Mileev (1974). These authors de scribed in The Cri mean Mts. are part of the south ern, de formed places the highly deformed com plex, with south-vergent fold - bound ary of the East Eu ro pean Plat form, lo cated be tween the ing and thrust ing, re lated to the Early Cim mer ian phase. An in- Scythian Plate (which belongs to the Eur asian con ti nent) and ter est ing view on the struc tural evo lu tion of the Cri mean the Black Sea (Figs. 1 and 2). This moun tain chain is ~50 km orogen was pre sented by Kruglov and Tsypko (1988), who wide and ~150 km long (Figs. 3 and 4; cf. Ap pen dix 1*). It is high lighted two Cim mer ian orogenic phases: the older (Li- arch-shaped, with E–W struc tural trends in the west, and assic/Bathonian) one in the NW sector of the CM, and the NE–SW in the east. Tra di tion ally, the CM are re garded as the youn ger (Valan ginian/Hauterivian) one in the SE sector of the Cim mer ian/Al pine orogen (Muratov, 1960, 1969; Koronovsky CM. The early orogenic phase took place in the outer (exter - and Mileev, 1974; Byzova, 1980; Kruglov and Tsypko, 1988; nal) part of the basin, where the fold ing of TFF was pre ceded Mileev et al., 1997, 2006, 2009; Nikishin at al., 2015a, c). by pre-fold ing vol ca nism. This is well-doc u mented (Kruglov

Fig. 1. Struc tural sketch-map of the Alpine Orogen System of SE Eu rope and Middle East sensu lato af ter Sosson at al. (2010), sim pli fied

Po si tion of the Crimea Mts. is shown as a red rect an gle

* Supplementary data associated with this article can be found, in the online version, at doi: 10.7306/gq.1359 The po si tion and age of flysch de pos its in the Cri mean Moun tains (South ern Ukraine) 699

and Tsypko, 1988) by re sults of the Kacha 2 bore - hole (40 km SW of Simferopol). This bore hole drilled to the fi nal depth of 4032 m re vealed in - tensely folded sed i ments TFF (T3-J1) with numer - ous in tru sions (dykes, sills and pillow lavas of diabases, picritic diabases, andesites and ba- salt-andesites) in the 2270–3930 m depth in ter - val. Hurskiy and Kruglov (2007) dis tin guished the fol low ing stru c tural com plexes: – autochthonous (Aptian/Albian), fragmen - tarily pre served in the Salgir and Tonas val- leys; – allo chtho nous com plex with two nappes: lower – the Tauric Nappe, and up per – the Yayla Nappe (car bon ate plat forms); – Ceno manian/Eocene post-nappe com plex (Fig. 2). In the Simferopol 1 bore hole, be neath the Tauric Nappe, Lower Cre ta ceous de pos its were pierced at a depth of ~4 km (Yudin, 2005, 2013). The in ter pre ta tion of Kruglov and Tsypko (1988) clearly shows that sed i men ta tion of the TFF in the ex ter nal (NW) part of the basin ended up in the Mid dle Ju ras sic, and con tin ued through the Valanginian/Hauterivian in the in ner (SE) ba sin. In the Cri mea Ba sin, this de for ma tion took place in close re la tion with the begining of the clo sure of the Neo-Tethys Ocean (Kazmin et al., 2000; Golonka, 2004). However, there was also con se quent Al - Fig. 2. Tec tonic map of the Cri mea Moun tains pine de for ma tion (dur ing the Paleogene), re lated (Hurskyi and Kruglov, 2006) to the Ara bia-Eur asia con ver gence and to the evo -

Fig. 3. Sim pli fied geo log i cal map of the Cri mea Moun tains based on Muratov (1960), Pivovarov and Derenyuk (1984) and Popadyuk et al. (2013a), with lo ca tion of the most re cent micropalaeontological data presented by Popadyuk et al. (2013a) and Sheremet et al. (2014, 2016a), and of our study sections (WP) in 2011–2013 700 Nestor Oszczypko, Andrzej Ślączka, Ihor Bubniak, Barbara Olszewska and Małgorzata Garecka

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. g i F The po si tion and age of flysch de pos its in the Cri mean Moun tains (South ern Ukraine) 701 lu tion of the Neo-Tethys (Bocaletti et al., 1974; Letouzey et al., ceous trans gressive for ma tions in the NW, and under the Mid- 1977; Adamia et al., 1981; Zonen shain and Le Pichon, 1986). dle/Up per Ju ras sic de pos its in the SW and SE (Fig. 4). The As far as the polyphase struc tural evo lu tion of the Cri mea is south ern re gion of the TFF, which is up to 100 km long and only con cerned, there is some con tro versy about the major struc- a few kilo metres wide, is sit u ated along the Black Sea coastal tures, es pe cially re lated to the vergence of thrust sheets and zone, be tween the Sarych Cape in the west and the Sudak area the ages of their de vel op ment. Mileev et al. (1997) con sid ered in the east (Figs. 3 and 4). In the north, the TFF adjoins the Main the thrust sheet de vel op ment as Berriasian in age with a south Ridge of the CM along the ver ti cal walls of the Late Ju ras sic car- and south-east vergence (N160–N120° in az i muth). Popadyuk bon ate plat form. The nature of this con tact is not clear. and Smirnov (1991) as sumed that the thrust ing in Cri mea was The TFF is di vided by Pivovarov and Derenyuk (1984) into gen er ally north-vergent and had oc curred dur ing the Austrian the Up per Tri as sic and Up per Tri as sic/Lower Ju ras sic mem- phase (Mid dle Cre ta ceous). Galkin et al. (1994) con cluded that bers. In the Lozove and Bodrak ar eas, these mem bers are sep - the allochthonous Up per Ju ras sic rocks of the Chatyr Dagh a rated by thick-bedded quartzitic sand stones with imprints of Mas sif thrust to the west over the Albian de pos its. Ac cord ing to Sinemurian ammonites and blocks of Pa leo zoic and Me so zoic Shcherba (1978), the allochtho nous com plex (Late Ju ras sic lime stones (e.g., the Eksi-Orda Fm.; Panov et al., 2001). In the ter ranes) was dis placed to the south in Late Cre ta ceous-Early coastal zone betw een Hurzuf and Alushta, the TFF is in truded Paleogene times, and the de tach ment sur face was re ac ti vated by Mid dle Ju ras sic vol ca nic bod ies: gab bro-diabases, ande - dur ing the Plio-Qua ter nary. Kazantsev (1982) and Kazantsev sites, bas alts, diorites and plagiogranites (Pivovarov and et al. (1989) re ported that the struc tural com plexes are in volved Derenyuk, 1984; Kruglov and Tsypko, 1988; Bilecki, 2006b; in north -vergent thrust sheets in clud ing rocks aged from the Pa- Yudin, 2009; Solov’ev and Rogov, 2010; Meijers et al., 2010). In leo zoic to Sarmatian. the NW sector of the CM, the TFF is transgressively over lain by Panek et al. (2009) applied an ap a tite fis sion -track thermo - Lower Cre ta ceous, mainly Hauterivian de pos its (Figs. 3 and 4). chronology (AFT) to in ves ti gate the low-tem per a ture ther mal Un clear sit u a tion is near the town of Dobre (south of Simfero- evo lu tion of the CM. The vast ma jor ity of the sam ples taken pol), where the TFF is cov ered by red con ti nen tal con glom er - from Ju ras sic sed i men tary and mag matic rocks re vealed AFT ates re garded by Pivovarov and Derenyuk (1984) as Callo- ages in the range of 51–32 Ma (Eocene). These stud ies sho - vian/Oxfordian, and by Popadyuk et al. (2013) as Neo gene? wed that the moun tain range ex pe ri enced a ther mal over print Along the Black Sea coast, be tween the Cap of Sarych and af ter the Late Cim mer ian orog eny: at least 4 km of burial by the Pryvitne, a prom i nent po si tion is oc cu pied by the Titho - Early Cre ta ceous/Late Eocene plat form was fol lowed by Mid dle nian/Berriasian car bon ate plat form (Fig. 4), up to 2000 m thick Plio cene up lift, flu vial ero sion and large -scale land slides. (Krajewski and Olszewska, 2007; Dorotyak, 2008; Krajewski, Sheremet et al. (2014, 2016a), based on new micro- 2010). This plat form is un der lain by the Oxfordian and Kimme- palaeontological data, pro posed Up per Tri as sic to Mid dle Ju - ridgian con glom er ates, sand stones an lime stones (Pivovarov ras sic and Lower Early Cre ta ceous ages of the Tauric Group in and Derenyuk, 1984), and it lies below the Tri as sic/Ju ras sic the east ern CM, as so ci ated with mag matic ac tiv ity. In this area, flysch de pos its. This se quence is well exposed be neath the they also sug gested the Early Cre ta ceous phase of ex ten sion Baydar Yalta-Chatyr-Dag and Demerji yaylas (Figs. 3 and 4). A and short en ing pe ri ods dur ing the Paleocene -Early Eocene, sim i lar re la tion ship be tween the TFF and the Up per Ju ras - be fore the main Mid dle Eocene un con formity. Sheremet et al. sic/Berriasian lime stone se quences con tin ues east ward (Ka - (2016b), on the basis of two in te grated transects from the east - rabi Yayla) as far as the Arpat Creek in Pryvitne. Ac cord ing to ern CM to the Sorokin Trough (north of the east ern BS; Fig. 2), Lalomov (2007), the Up per Ju ras sic Con glom er ate For ma tion doc u mented the Early Paleocene to Plio cene short en ing (UJCF) un con form ably over lies the TFF in this area, and cre- phases linked with the Neo-Tethys clo sure and uplift of the ates a kind of “lenses” at the base of the Up per Ju ras sic lime - Great Cau ca sus. This sce nario has been sup ported by Sosson stones. In this in ter pre ta tion, the UJCF is tri par tite and reaches et al. (2016) who re con structed the palaeogeographic po si tion 750 m in thickness (e.g., Demerji area). The lower mem ber of of the Black Sea Cau ca sus area from the Titho nian to Early this for ma tion (up to 300 m thick) is com posed of boul der/peb - Paleocene. ble con glom er ates with sandy clayey matrix. The mid dle mem - ber, up to 250 m thick, is rep re sented by me dium- to well- -rounded boul der/peb ble con glom er ates with me dium-sorted CURRENT VIEWS ON THE AGE ma trix. The upper mem ber of the UJCF, up to 200 m thick, is OF THE TAURIDA FLYSCH FORMATION dom i nated by me dium/fine-grained sand stones with gravel and small pebbles. In this in ter pre ta tion, the de bris-flow de pos its of Dis tri bu tion of the TFF in the CM is well-il lus trated on sev- the UJCF were trans ported to the basin from the NW. This is eral gen eral geo log i cal maps 1:200,000 (Muratov, 1969; Pivo- con firmed by the gran ite boul ders de rived from the Ukrai nian varov and Derenyuk, 1984; Yudin, 2009), and on se rial geo log i - Shield (see Lalomov, 2007). cal maps 1:200,000: Eupatoria-Sevastopol and Simferopol - In the Sevastopol area, the up per most part of the UJCF -Yalta sheets (Bilecki, 2006a, b). could be partly cor re lated with the Hurzuf For ma tion (~50 m The TFF is tra di tion ally re garded as the old est sed i men tary thick), com posed of al gal lime stones, sands and con glom er - for ma tion of the CM, ex posed in two sep a rate, north ern and ates (Bilecki et al., 2006a). Prob a bly, a sim i lar po si tion is occu - south ern folded belts (Figs. 3 and 4). The north ern one, known pied by the Sukhoriche For ma tion (Oxfordian/Kimmeridgian), as the Kacha Uplifted Zone (Kruglov and Tsypko, 1988), is up com posed of con glom er ates, sand stones and biohermal lime - to 50 km long and up to 25 km wide. In this re gion, the tec toni - stones, up to 500 m thick (Bilecki, 2006a). cally mul ti plied thick ness of the TFF reaches a few kilo metres Along the shore line, east of the mouth of the Salgir River up (e.g., at least 2299 m in the Kacha 2 bore hole, and 4032 m in to Morskie vil lage the TFF occurs in a nar row zone ta per ing to - the Kacha 4 bore hole – see Bilecki, 2006a). In the east, this re- ward the E. In this area, the TFF is lo cally overlain by patches of gion ad joins the Late Ju ras sic car bon ate plat form of the Dolho - the Aalenian/Bajocian gravelithes with coal in ter ca la tions (Pivo- rukovska Yayla along the Alushta/Salgir transversal fault varov and Derenyuk, 1984). In the Morske vil lage the TFF dis - (Kruglov and Tsypko, 1988; Fig. 4). Tow ards the SW, the out - ap pears un der a cover of Bathonian/Callovian silty-sandy sed i - crops of the TFF nar row and dis ap pear un der the Lower Cre ta - ments (Pivovarov and Derenyuk, 1984). 702 Nestor Oszczypko, Andrzej Ślączka, Ihor Bubniak, Barbara Olszewska and Małgorzata Garecka

Ac cord ing to Yudin (2009) the con tacts of the TFF with plankton. In course of their pro ject, they col lected 224 sam ples, older and youn ger for ma tions are mainly tec tonic and accom - of which only 52 al lowed con clud ing about their age. These pos - pa nied by wide zones of tec tonic mélanges. The TFF is i tive sam ples have been picked up from marly shales, lime - transgressively over lain by Lower Cre ta ceous de pos its only be- stones, flysch and flysch-like de pos its of the east ern sec tor of tween the Salgir and Bodrak rivers. In the rest of the CM, the the CM, be tween Simferopol in the west and Feodosia in the con tacts of the TFF with both the younger and older for ma tions east. The ages of these de pos its are not younger than Valan - are tec tonic. ginian in the east and Aptian/Albian in the west. In turn, in the Un til re cently, the Late Tri as sic/Early Ju ras sic age of the west ern sec tor of the CM (W of the Salgir Val ley), and along the TFF was rel a tively poorly doc u mented by biostratigraphic, litho - coastal area betw een Alushta and Morske, where the TFF is stratigraphic and sedimentological stud ies. The strati graphic dom i nant, all sam ples were empty. How ever, these re sults po si tion of the TFF is based on few find ings of ammonites have not been cor re lated with any lithostratigraphic units shown (Astakhova, 1968a, b, 1971, 1972, 1976), cri noids, the Up per in geo log i cal maps (Pivovarov and Derenyuk, 1984; Bilecki, Tri as sic bi valve Monotis salinata (Klikushyn, 1988; Okay et al., 2006a, b; Yudin, 2009) and, more over, sam ples col lected from 2015), and palynological data (Bolotov et al., 2004 and ref er - the un ques tion able TFF de pos its have been usu ally barren. In ences therein). However, when we crit i cally ana lyse these an other pub li ca tion, Sheremet et al. (2016a) give ad di tional dates, we should take into ac count the fact that turbidite sed i - micropalaeontological data (e.g., from Berehove and Yalta) and ments con tain usu ally rew orked fos sils and palynological ma te - pro vide a new in ter pre ta tion of the struc tural evo lu tion of the CM rial (e.g., Oszczypko et al., 2004, 2012a). Re work ing proceses (Fig. 3). dur ing the de po si tion of the TFF are con firmed by the pres ence of nu mer ous blocks of both sed i men tary rocks with fossils, and plutonic and vol ca nic rocks (Muratov, 1960; Albov, 1964; Ippo - METHODS litov et al., 2008; Yudin, 2009). Popadyuk (2011) re ferred to a for got ten pub li ca tion of Dekhtyareva et al. (1978) where, in ad- di tion to the Car bon if er ous, Perm ian, Tri as sic to Mid dle Ju ras - For our stud ies, we used the geo log i cal map 1:200,000 sic, and Up per Tri as sic to Lower Ju ras sic fos sils in the exotic (Pivovarov and Derenyuk, 1984), ed ited by the Ukrai nian Geo - blocks of the Eksi-Orda For ma tion near Simferopol, also the log i cal Sur vey. This map well-il lus trates the main lithostrati - Barremian-Aptian ammonites have been found. Tak ing into ac - graphic units of the CM (Fig. 4) and shows that the Up per Tri as - count these data, Popadyuk (2011) ques tioned the Aptian - sic-Lower Ju ras sic flysch de pos its of the TFF are dis trib uted in -Albian age of the TFF, while the age of the post-tec tonic sed i - two ar eas: west of the Salgir River (Kacha Uplift) and along the men tary cover of the CM should be not older than Ceno manian. sea shore, be tween the Sarych Cape in the west and the vil lage Tak ing into ac count the in ter de pen dence of vol ca nism and of Morske in the east (Figs. 3 and 4). sed i men ta tion of the TFF (see Kruglov and Tsypko, 1988), the Ini tially (2011–2012), our in ter est was fo cused on stud ies of de tri tal zir cons from out crops lo cated near Simfe- lithostrati graphical stud ies and sam pling of the TFF in its lo cus ropol and along the Black Sea coast betw een Yalta and Alushta typicus area, lo cated west of the Salgir River (Fig. 4) and along as well as from the Kastel Massif (west of Alushta) sup plied im - the Black Sea coast, be tween the Sarych Cape in the west and por tant in for ma tion (Solov’ev and Rogov, 2010). They pro vide the vil lage of Pryvitne in the east (Oszczypko et al., 2012b, c). the fol low ing dates (in Ma): 220.1 ±12 and 169.9 ±8.6 in the Later (2013), these stud ies were extended on the Ju ras - north, 193.6 ±13.1, 167.1 ±12.1 and 154.0 ±10.2 on the sea - sic/Lower Cre ta ceous flysch of the east ern sec tor of the CM. shore, and 149.0 ±10.9 in the Kastel Massif, thus show ing that Our re search was car ried out along the main road and six se- the age of de tri tal zir con cor re spond ing to the in ter val be tween lected lo cal i ties. The stud ied and sam pled sec tions were doc - the Late Tri as sic to Mid dle Ju ras sic and the Oxfor dian/Kimme - u mented by GPS way-points (WP) and pho to graphs. Dur ing ridgian (Late Ju ras sic) is sim i lar to the usu ally accepted age of field work, we col lected 98 sam ples for biostratigraphic study, the TFF, and sug gests synchrony of vol ca nism (Late Tri as- of which 48 sam ples ap peared bar ren. In the re main ing sec - sic–Mid dle/Late Ju ras sic) and flysch sed i men ta tion. tions (50 sam ples col lected from 37 sites; Figs. 3 and 4) the Meijers et al. (2010) doc u mented the pres ence of two age de ter mi na tion was based on microfossils (foraminifera groups of vol ca nic rocks in the Cri mea Mts.: older – Aalenian to and cal car e ous nannoplankton). Microfacies types have also Oxfordian (~172–158 Ma in the area of the Bodrak Val ley and been de ter mined. In the lab o ra tory, stan dard pro cess ing near Simferopol) and younger – Tithonian–Berriasian meth ods were applied to iso late the foraminifera and dinocysts (~151–142 Ma in Karadag). from shales and mud stones. In general, the sam ples from The pre lim i nary re sults of our geo log i cal and micro palaeo - shales and mudstones of the TFF con tained scarce fora - nto logical stud ies (Oszczypko et al., 2012b, c) on the TFF in the minifera and dinocysts. Ad di tion ally, both microfacies and cal- Bodrak area and along the Black Sea coast con firmed its Up per car e ous nannoplankton were analysed in thin-sec tions from Tri as sic-Mid dle Ju ras sic age in these lo cal i ties. They also doc - sev eral lime stone sam ples. u mented that the Mid dle/Up per Ju ras sic Flysch is trangressi - vely overlain by the Up per Oxfordian/Kimmeridgian ma rine de - pos its near Laspi. Popadyuk et al. (2013) pub lished a new geo- STUDIED SECTIONS log i cal map of the CM (1:200,000) based on de ter mi na tion of 51 foraminifer spe cies and re vi sion of 163 sec tions (Fig. 3), and pointed out the Aptian/Albian age in the west ern part of the CM. WESTERN SECTOR OF THE CM The other area of oc cur rence of the Aptian/Albian de pos its is in the east ern part of the CM be tween Sudak and Feodosia. Un for tu nately, in places of typ i cal oc cur rence of the TFF, sam- Our re search focused on stratotype ar eas of the TFF near ples were barren. Prokhladne, south of Simferopol, and along the coast from Re cently, Sheremet et al. (2014) pub lished im por tant pa - Rybache in the east to the Sarych Cape in the west (Figs. 3 pers con cern ing large-scale stud ies of of cal car e ous nanno - and 4). The po si tion and age of flysch de pos its in the Cri mean Moun tains (South ern Ukraine) 703

Bodrak val leys. Both the TFF and Eksi-Orda Beds are locally transgressively over lain by lobes of Lower Cre ta ceous de pos - its, mainly of Albian age (Marcinowski and Najdin, 1976). Bolotov et al. (2004), based on palynofossils and the Norian bi - valve Monotis sp., doc u mented the Toarcian-Aalenian age of the TFF in the Bodrak River sec tions. Thin-bed ded flysch, sim i- lar to that described above, we have observed and sam pled also in sev eral ex po sures along the Black Sea coast, be tween Rybache in the east and Alushta and the Laspi Bay in the west. In the poor foraminifera as sem blage iden ti fied in WP 7, 8, 10–13 (Fig. 5), one spe cies, Thuramminoides metensis (Terquem) (Fig. 7), is char ac ter is tic for the Mid dle Tri as sic, and an other one, Thalmannammina canningensis Tappan, is also re ported from the Tri as sic–Lower Ju ras sic. Pre lim i nary stud ies of or ganic dinocysts from the Bodrak sec tion (WP 7–17) in di - cated poorly pre served Lower Ju ras sic dino cysts: Phallocysta sp., Wallodinium and Nannoceratopsis sp. Nanno ceratiopsis senex and N. gracilis have been oc ca sion ally ob served, in di cat - ing a Late Pliensbachian-Early Bajocian age (Oszczypko et al., 2012c). Laspi area (Figs. 8, 9 and 10). To the west of Yalta (Figs. 3 and 4), along the coast line, and near Laspi we observed well-ex posed flysch. On the geo log i cal map of Bilecki (2006a; Fig. 8) these flysch de pos its have been in cluded into the upper part the Taurida For ma tion (T3–J1) and the Aalenian/Bajocian flysch (J2ml) with tuffite in ter ca la tions and small subvolcanic diabase veins of Mid dle Ju ras sic age. In com par i son with the flysch of the Prokhladne sec tions, turbidites of this area differ in col our and show less in tense tectonisation of beds. West of Yalta, in Berehove along the Black Sea coast, we found well-ex- posed flysch de pos its (WP 39; Fig. 8). Pre vi ously, these depos - its were re garded by Pivovarov and Derenyuk (1984) and Yudin Fig. 5. Geolog i cal sketch-map of the Prokhladne area, (2009) as the TFF (T3-J1). These out crops dis play N-dipping based on Bilecki (2006b) (360/35) dark grey thin- to me dium-bed ded turbidites with thick- en ing- and coars en ing-up ward se quences (Fig. 9A–C). In gen- Prokhladne area. This area of good out crops, lo cated on eral, the flysch de pos its from Berehove are sig nif i cantly dif fer - hills betw een the rivers of Bodrak and Alma (Figs. 5 and 6A–E), ent from that of the Bodrak Val ley and coastal zones east of is re garded as lo cus typicus of the Taurida Flysch For ma tion of Alushta, in both the col our and degree of tec tonic de for ma tion Up per Tri as sic–Lower Ju ras sic age (e.g., Muratov, 1960; Levi - of beds. tskiy, 1974; Marcinowski and Najdin, 1976; Muratov et al., In the Berehove sec tion (WP 39), a rel a tively rich Early Ju- 1984; Baraboshkin, 1997). In Prokhladne, re mains of ammo- rassic foraminiferal as sem blage has been iden ti fied in grey nites (Dactilioceras sp.) and bel em nites (Mesoteuthis quen- siltstones (Figs. 8 and 9A–C, 10; Ap pen dix 1). A thin-sec tion of stetdti) were found at the top of the TFF, which point to the the same sam ple also re veals the pres ence of Up per Ju ras sic Toarcian/Aalenianian age of this for ma tion (Levitskiy, 1974). In foraminifera. Ad di tion ally, from the same lo cal ity (Bere ho - the same po si tion, di rectly be low Hauterivian transgresive de- ve/Kas tro pol, sam ple 40 lo cated at 225 m, az i muth 75 from WP pos its, Levitskiy (1974) doc u mented the pres ence of Palaepo - 39), Sheremet et al. (2016a) re ported the pres ence of lycheles crymensis. Mod ern rep re sen ta tives of this fam ily be- Hauterivian-Early Barremian cal car e ous nannoplankton. Early long to the ma rine benthos, oc cur ring at depths of up to 2000 m. Cre ta ceous (Up per Valanginian–Lower Barremian) cal car e ous Car to graphic po si tion of the TFF in this area is pre sented on nannoplankton has also been doc u mented in a sam ple from geo log i cal maps of Pivovarov and Derenyuk (1984), Bilecki Yalta (Sheremet et al., 2016a:, sam ple 42). (2006a, b) and Yudin (2009). The first group of ex po sures (WP Go ing to the west along the road H-19 to the lo cal ity of Laspi, 7–12) dis plays dark grey non-cal car e ous, fine to very fine, thin- we observed and sam pled the shaly fa cies prob a bly be long ing to to me dium-bed ded turbiditic sand stones with shaly and the upper part of the TFF (WP 40; Ap pen dix 1). In the dark beige mudstone in ter ca la tions, si der it ic con cre tions and rare thick mudstones, a rel a tively rich Up per Tri as sic- Lo wer/Mid dle Ju ras - sand stone beds (Fig. 6A–D). Few flute casts of me dium-bed - sic foraminiferal as sem blage has been doc u mented. ded turbiditic sand stone in di cate palaeotransport from NW to To the NW of the Sarych Cape, above the road H-19, the SE (300°). Green ish-brown shales are cov ered with red - up per shaly fa cies of the TFF (WP 40) are transgressively over - dish/black patina of Fe/Mn min er als (Fig. 6C, E). Subvertically lain by poorly ce mented fine gravel, 10–15 m thick, with clay - dip ping beds are folded and many of them are over turned. stone (WP 42, 43; Fig. 8). These Up per Ju ras sic clayey-sandy Some pack ages of strongly tectonized beds can be re garded de pos its, with clasts of rhodoid lime stones, up to 5 cm across, as a kind of “bro ken for ma tion” (Fig. 6F). About 1.8 km to the con tain (WP 43) a rel a tively rich foraminiferal as sem blage (Ap- north (WP 14, 15; Fig. 5) we found steeply NW-dip ping (340/60) pen dix 1) ac com pa nied by ostracods, echinoids, spikes and thin-bed ded turbidites with two diabase sills (0.5 and 4 m thick, cal ci fied radio lar ians. Its likely age is Early/Mid dle Oxfordian. A see Meijers et al., 2010) show ing ther mal con tacts (Fig. 6D). thin-sec tion (WP 43, thin-sec tion 1) revealed the pres ence of There is a nar row, up to 1 km wide, NE–SW-ori ented syncline mi cro bial bind stone con tain ing few foraminifera: Textularia sp., of the Eksi-Orda Beds (Lower Ju ras sic) be tween the Alma and Bullopora sp., Nubeculariidae, ac com pa nied by Polychaeta – 704 Nestor Oszczypko, Andrzej Ślączka, Ihor Bubniak, Barbara Olszewska and Małgorzata Garecka

Fig. 6. Taurida Flysch For ma tion of the Bodrak Val ley A – thin-bed ded turbidites dom i nated by dark grey non-cal car e ous shales and mudstones with rare in ter ca la tions of thin-bed ded sand stones, with rust-col oured weath er ing crust (sam ple WP 7); B – sill of Mid dle Ju ras sic volcanites; C – shaly lithofacies of TFF with few centi metres thick in ter ca la tions of very fine sand stones (WP 8); D – strongly tectonized shaly lithfacies of TFF (WP 9); E – coars en ing- and thick en ing-up ward se quence, up per part of TFF; F – details of above photo graphed sequence

Terebella lapillo ides Mun ster, and lo cal ac cu mu la tions of spon - ous nannoplankton (Nannoconus stein mannii) in di cat ing Late ge spi cules. This as sem blage points to Late Ju ras sic age. Sim i- Ju ras sic-Early Cre ta ceous age. Sam ple WP 74 has also larly, a thin-sec tion (WP 43, thin-sec tion 2) from micritic lime - yielded a cal car e ous nanno plankton as sem blage with Cycla- stone con tained poor, but stratigraphically im por tant micro - gelo sphaera argoensis and C. margerelli Noel, which in di cates fossils (Ap pen dix 1). The age cor re sponds to late Early–Mid dle Late Ju ras sic to Early Cre ta ceous age (Ap pen dix 1). Oxfordian. Chatyr-Dag Yayla (Figs. 11 and 12). In the Salgir River Val- In 2012, along the road to Laspi, above sam ples WP 42–43, ley, near Dobre (a few kilo metres south of Simferopol), we sam ples from the Late Ju ras sic car bon ate plat form of the turned off the main road and con tin ued mov ing up the lo cal road Baydarska (e.g., WP 65; Ap pen dix 1) were col lected. These to wards the Chatyr-Dag Massif (1527 m a.s.l.). In the road side sam ple con tains abun dant microfossils in di cat ing Late Ju ras sic ex po sures, red thick-bed ded con glom er ates with the red to Early Cre ta ceous age. The lime stones ex posed along the sandy -clayey ma trix oc cur. These NW-dip ping con ti nen tal de - road from Laspi to Sokolyne (sam ple WP 71) con tain cal car e - pos its stretch along the road for a few hundred metres (Fig. The po si tion and age of flysch de pos its in the Cri mean Moun tains (South ern Ukraine) 705

Fig. 7. Mi cro pho to graphs of foraminifers from TFF (Late Tri as sic–Early Ju ras sic), obtained by wa ter mac er a tion A – Kechenotiske cf. maurikensis Haig and Mc Cartain, WP 39, side view; B – Palustrella exigua (Schwager), WP 18, side view; C – Astacolus cf. varians (Bornemann), WP 40, side view; D – Textularia aff. haeusleri Kaptarenko Chernousova WP 18"2011", side view; E – Ammobaculites cf. rhaeticus Kristan-Tollmann, WP 23, side view; F – Thuramminoides metensis (Terquem), WP 8, side view; G – Trochammina sp., WP 39, apertual view; H – Verneuilinoides cf. liasina (Terquem and Berthelin), WP 39, side view 706 Nestor Oszczypko, Andrzej Ślączka, Ihor Bubniak, Barbara Olszewska and Małgorzata Garecka

Fig. 8A – geo log i cal sketch-map of the Laspi area, based on Bilecki (2006a), with lo ca tion of sampled sections; B – simpli fied lithostratigraphic pro file with lo ca tion of sampled sites

Fig. 9. Re la tion ship of TFF to the Late Ju ras sic car bon ate platfom of Baydarska Yayla near Laspi A – lo ca tions of sam ples WP 38/39; B – WP 42/43, poorly ce mented, coarse-grained sand stones, con glom er - ates and lime stone con cre tions in sandy ma trix of the Upper Oxfordian/Kimmeridgian, at the base of hard lime- stones (Tithonian/Berriassian, see Oszczypko et al., 2012b, c); C – fine grav els and sands (sam ple WP 42); D – Tithonian/Berriasian lime stone The po si tion and age of flysch de pos its in the Cri mean Moun tains (South ern Ukraine) 707

Fig. 10. Foraminifers of the Cri mea Mts. found in thin-sec tions A – Anchispirocyclina lusitanica (Egger), S.6/WP 71, equa to rial cross-sec tion, Late Ju ras sic (Tithonian); B – Anchispirocyclina lusitanica (Egger), S.6/WP 71, oblique cross-section, Late Ju ras sic (Tithonian); C – “Vidalina” martana Farinacci, WP 70a, equa to rial and oblique cross-section, Lias; D – Involutina cf. liasica (Jones), WP 70a, axial cross-sec tion, Early Ju ras sic; E – Pseudomarssonella osoviensis (Bielecka and Styk), WP 70a, axial cross-sec tion, Mid dle Ju ras sic; F – Siphovalvulina variabilis Septfontaine, WP 70a, ax ial cross-sec tion cut ting, Mid dle Ju ras sic; G – Protopeneroplis striata Weynschenk WP 70a, cut cross wise, ax ial cross-sec tion, Mid dle Ju ras sic; Sudak-Feodosia transect; H – Quinqueloculina cf. occulta Antonova, WP 70a, cut cross wise, axial cross-sec tion, Mid - dle Ju ras sic; Sudak-Feodosia transect 708 Nestor Oszczypko, Andrzej Ślączka, Ihor Bubniak, Barbara Olszewska and Małgorzata Garecka

Fig. 11A – geo log i cal sketch-map of the Chatyr-Dag-Alushta area, based on Bilecki (2006b), with lo ca tion of sampled sections; B – simpli fied lithostratigraphic pro file with lo ca tion of sampled sites

11A). The con glom er ates have been in cluded by Pivovarov spines of sea ur chins in sam ple WP 107 (Figs. 11 and 12E), and Derenyuk (1984) into the Callovian/Oxfordian, by Yudin clearly in di cat ing Early Cre ta ceous (Neocomian) age. In a (2009) into the Lower Cre ta ceous, and by Popadyuk et al. thin-sec tion, fora minifera not older than Kimmeridgian were (2013) into the Neo gene. Go ing up to the east, on a steep hill- also ob served. Sim i lar flysch occurs near WP 108. In this case, side, the var ie gated con glom er ates are fol lowed by thick beds the beds (dip ping at 310/30) are exposed in a mor pho log i cal de - of Oxfordian grey con glom er ates (Fig. 12C). These con glom er - pres sion lo cated be tween the Chatyr-Dag (1527 m a.s.l.) and ates are over lain by highly tectonized dark grey marly shales Demerji (1350 m a.s.l.; Fig. 12F) lime stone mas sifs. This sit u a - that con tain mainly pyritized microfossil pseudo morphs, not tion gives an im pres sion that these flysch strata dip beneath the older than Albian (WP 101; Ap pen dix 1). The Albian shales are car bon ate plat forms (cf. Popadyuk and Smirnov, 1991). An in- overthrust by the Tithonian/Berriasian grey lime stones (Fig. ter est ing re sult was pro vided by sam ple WP 80 col lected close 12), steeply dip ping to the east (85/51). Higher up, along the to Yalta from grey cal car e ous mudstones. These de pos its were road to Mramorna Pechera (WP 99/100 and WP 88), karstified re garded by Pivovarov and Derenyuk (1984) as the up per most lime stones of the Chatyr-Dag car bon ate plat form are exposed. part of the Tauride Flysch (T3-J1) lo cated be neath the car bon ate These lime stones contain Tithonian -Berriasian microfossils plat form. Sam ple WP 80 con tains cal car e ous nanno plankton (Ap pen dix 1). It needs to be high lighted that marly shales from (Ap pen dix 1), in clud ing Watznaueria barnesae (Black) WP 101 clearly cor re late with the Albian (K1al1-2) clays with Perch-Niel sen, which could be in ter preted as not older than fos sils and siderites (Pivovarov and Derenyuk, 1984). These Mid dle Ju ras sic and not younger than Early Cre ta ceous. de pos its are exposed also in the Salgir River Val ley on the Re sults of sam pling along the road cross-sec tions. In west ern mar gin of the Demerji Yayla car bon ate plat form. A few ad di tion to the pre vi ously de scribed ex po sures, our re search kilo metres to the SE in the val ley sep a rat ing Demerji and cov ered also the out crops lo cated along the roads in the west - Chatyr-Dag yaylas, at the petrol sta tion (WP 107; Figs. 11 and ern part of the CM (Figs. 3 and 4). In these ar eas, we rec og - 12E) in a cross-cut of a road, we found the south-dip ping nized, among oth ers, the Up per Ju ras sic/Lower Cre ta ceous (190/40) dark grey thin-bed ded flysch clas si fied by Pivovarov microfacies (WP 71, 80, 81) typ i cal of the car bon ate plat form and Derenyuk (1984) as the upper part of the TFF (T3-J1). How- (Ap pen dix 1) NE of Yalta. In the Alushta re gion, we have ac - ever, we found rel a tively abun dant microfossils, ostracods and quired data on the Up per Tri as sic/Lower Ju ras sic TFF (WP 31, The po si tion and age of flysch de pos its in the Cri mean Moun tains (South ern Ukraine) 709

Fig. 12. Rela tion of the Late Juras sic car bonate platform (Chatyr-dag Yayla) to its sed i men tary base ment A – red con ti nental con glom erates of TFF (Middle Ju ras sic?), WP 106; B – Oxfordian/Kimmeridgian? red dish and grey con glom er ates, WP 105; C – brec cia of the Aptian dark grey marly shales with blocks of Oxfordian/Kimmeridgian(?) con glom er ates; D – Tithonian/Berriasian lime stones of Chatyr-Dag Yayla, WP 99; E – Lower Creta ceous turbidites regarded as the Upper Trias sic/Lower Ju ras sic de pos its of TFF, Demerji Stream, near a petrol sta tion, WP 107; F – Late Ju ras sic carbon ate plat form of Demerji Yayla – view from the west

32, 34, 35), lo cated be low the car bon ate plat form of the Demerji ceous (Hauterivian, see Sheremet et al., 2016a: point 43) Yayla, and on the north ern mar gin of the Dolhorukovska Yayla. thin-bed ded flysch. In WP 170, we have doc u mented a 4 m East ern sec tor of the CM. Be tween the Sudak Bay and the thick basalt sill that con cor dantly in ter ca lated flysch de pos its. In Meganom Pen in sula, along the shore line and di rectly to the the Sudak area, we found Up per Ju ras sic/Lower Cre ta ceous north, N-dip ping, dark grey, thin- to me dium-bed ded turbidites foraminifera (in WP 153; Ap pen dix 1) and the Up per Ju ras - are well-ex posed (Figs. 3, 4 and 13). Tow ards the north, near sic/Lower Cre ta ceous bioclastic grainstone near Kurortne (WP Solnechna Dolyna, a range of hills exposes thin- to thick-bed - 158; Ap pen dix 1). The foraminifera de ter mi na tions con firm ded turbidites (Fig. 13D) over lain by con glom er ates (Fig. 13E). strati graphic data of Sheremet et al. (2014) and Popadyuk et al. The folded thick-bedded turbidites are also exposed near (2013). The thin-bed ded flysch passes upw ards into thick-bed - Feodosia (Fig. 13F). Further to the east, near Ordzhonikidze, ded turbidites and de bris-flow con glom er ates with huge blocks the steep ma rine cliffs re veal a thick se ries of Lower Cre ta - of Up per Ju ras sic reef lime stones, up to 2 km across (e.g., 710 Nestor Oszczypko, Andrzej Ślączka, Ihor Bubniak, Barbara Olszewska and Małgorzata Garecka

Fig. 13. Lithostratigraphic and sed i men tary de vel op ment of the Sudak Flysch For ma tion and over ly ing thick-bed ded turbidites and con glom er ates A – Black Sea shore east of Sudak, com posed of the Up per Ju ras sic/Lower Cre ta ceous flysch for ma tions, view to wards the Meganon Pen in sula; B – steeply dip ping me dium- and thick- bed ded flysch de pos its; C – huge expo - sures of the Ju ras sic/Cre ta ceous flysch, view to wards the NE; D – large con glom er ate and sand stone ex po sures north of Solnechna Dolyna; E – a packet of thin-bed ded flysch over lain by thick-bed ded sand stones and con glom - er ates; ex am ple of a thin ning- and fin ing-up ward turbidite se quence; F – thick- and me dium-bed ded turbidites near Feodosia

Khart-Kaya; see Yudin, 2009). These de pos its are exposed be - Morske-Vesele-Novyi Svit sectio ns (Figs. 14–17). These tween Pryvitne in the west and the Cap Kuuk-Atlama in the sec tions are lo cated along the road P 29 from Morske to Sudak east, over a dis tance of at least 70 km. The width of the out - (Figs. 3 and 4). The Vesele sec tion be gins with the strongly crops of these beds ranges betw een 2 km near Pryvitne to folded flysch of Lower Ju ras sic (Pivovarov and Dere nyuk, 1984) ~30 km at the Meganom me rid ian. These coarse clastic cone, or Mid dle Ju ras sic (Bilecki, 2006b) age. These flysch de pos its un der lain by dis tal turbidites in the south, is over lain by Lower are well-ex posed in the right side (S) of the road cross-cut (Figs. Cre ta ceous marls and lime stones in the north. 14 and 16). They are rep re sented by se ries of dark shales and The age of this for ma tion is Lower Cre ta ceous, not younger micaceous mudstones with in ter ca la tions of NW-dip ping, thin- to than Valanginian (Sheremet et al., 2016a). me dium-bed ded turbiditic sand stones which dis play palaeo- transport from the E (Fig. 16A–C). These de pos its prob a bly ex- The po si tion and age of flysch de pos its in the Cri mean Moun tains (South ern Ukraine) 711

fos sils come from re de pos ited ma te rial, their pre - cise age can not be de ter mined. North of Vesele, in the pass near the cross- roads to wards Sudak (Fig. 13; WP 18), there is a large block (5 x 3 m) of volcanites (Fig. 15F). This is a kind of Mid dle Ju ras sic or Up per Ju ras - sic/Lower Cre ta ceous vol ca nic sill as a mona - dnock or olistolith block de rived from the Up per Ju ras sic con glom er ates. This block is un der lain and over lain by dark grey mudstones which con - tain Up per Tri as sic/Lower Ju ras sic foraminifera at the base – WP 18 (Ap pen dix 1) – and Up per Ju ras sic microfacies and cal car e ous nanno - plankton at the top – WP 18A (Ap pen dix 1). From the Vesele sec tions, Sheremet et al. (2014, 2016a) re ported the Lower Cre ta ceous nanno - plankton, not younger than Valanginian, col lected from marly shales (points Nos. 59–61) lo cated 50–60 m east (az i muth 81) of WP 18A. In the Vesele sec tion, along the north ern side of the road, there are well-ex posed dif fer ent types of con glom er ates and thick-bedded turbidites (Fig. 15A, B), ma trix-sup ported de bris flows (Fig. 15C), and cha ot i cally or ga nized con glom er ates (Fig. 15D). In this sec tion, we rec og nized de pos - its of dif fer ent ages: both Up per Tri as sic-Lower Ju ras sic and Up per Ju ras sic/Lower Cre ta ceous (WP 23, WP 18 and 18A). There is sim i lar sit u a - Fig. 14A – geolog i cal sketch-map of the Vesele and Novyi Svit area tion with sec tion WP 39 (Berehove). This doc u- (based on Yudin, 2009) with lo ca tion of the stud ied and sam pled sec tions; B – simpli fied lithostratigraphic sec tion with loca tion of sampled sites mented that dur ing the Late Ju ras sic/Early Cre ta - ceous de po si tion the Late Ju ras sic/Early Cre ta - ceous de bris flows and turbiditic cur rents eroded tend south wards to the Perchem -Kaya (576 m a.s.l.) with very the Lower Ju ras sic flysch sed i ments and trans ported to the thick, NW-dip ping flysch se ries (Fig. 16D). Sudak Ba sin to gether with re worked microfossils. The sam ple col lected in WP 22 (Fig. 14) was bar ren. Fur - From the Vesele sec tion (WP 18), we con tin ued our ob ser va - ther to the west, within grey and beige micaceous mudstones tions along the road to Novyi Svit (Fig. 17). North of the road we ex posed along the N side of the road, one of the sam ples (Fig. passed the Khart-Kaya (375 m a.s.l.), a very large block (1 km 13E; WP 23) con tained foraminifera that sug gest Late Trias - across) of Up per Ju ras sic lime stones. Ac cord ing to Yudin (2009) sic–Early Ju ras sic age (see Ap pen dix 1). A few hun dred metres the block is in cor po rated into mélange (m2). It is highly prob a ble fur ther to the east, these flysch de pos its are over lain by a thick that this block is one of the many large olistoliths in the Up per Ju - con glom er ate com plex ex posed on the left (N) side of the road ras sic/Lower Cre ta ceous de bris-flow con glom er ates. De pos its (Fig. 15E) and dip ping to wards the NE. The age of these con - with huge olistoliths are well exposed on a cliff edge to wards glom er ates has been dif fer ently in ter preted: as Up per Callo - Novyi Svit (e.g., the Koba-Kaya cliff; Fig. 17A) – see the vian -Early Oxfordian by Pivovarov and Derenyuk (1984) and Callovian/Oxfordian car bon ate reef massif (Nikishin et al., Bilecki (2006b) and as Mid dle Ju ras sic sand stones, mudstones 2015b), and on the cliff close to the light house in Novyi Svit (Fig. and argilites with the Up per Ju ras sic reef lime stone olistolith by 17B). On the south ern slope of the massif, along the road, and di - Yudin (2009). rectly be low the con glom er ates, car bon ate sed i men tary brec cia Ac cord ing to our ob ser va tions, these de pos its con sist of (Fig. 17C) is exposed. The lime stone block con tains large thick-bed ded, graded, channelized con glom er ates, peb bly Pecten shells (Fig. 10D), and ammo nite (Fig. 17E) and ?stro - mud stones, and sed i men tary brec cias. They con tain peb bles matoid casts. This sug gests that they can rep re sent a re de pos - and large blocks of lime stones with macrofossils and frag ments ited biohermal fa cies. One of the sam ples taken from grey shale of brachi o pods. This coarse-grained com plex shows a thin - in ter ca la tions (sam ple WP 115) yielded a rel a tively rich assem - ning-up ward se quence with more sand stone in ter ca la tions up - blage of Lower Cre ta ceous (Neo comian) foraminifera (Ap pen dix per in the sec tion. The ex act char ac ter is tics of the thick-bedded 1). Just be low the road, there are strongly dis turbed grey-green - turbidites and de bris-flow con glom er ates with lime stone blocks ish mudstones de void of microfossils and frag ments of lime - is shown in Fig ure 14B. stones, which prob a bly rep re sent sed i men tary brec cias, with out The con glom er ates are com posed of var i ously sized Up per mesostructures char ac ter is tic for brec cias of tec tonic or i gin. Ju ras sic lime stone blocks and boul ders, sup ported by gra - From this sec tion, Sheremet et al. (2016a) re ported Up per Ju ras - vel/san dy/clay ma trix. Towards the east, there are sev eral very sic/Valanginian cal car e ous nanno plankton (points 66 and 67). large lime stone olistoliths, up to 1 km across (Fig. 13; see also Pryvitne-Krasnolisia transect (Figs. 18 and 19). In this Yudin, 2009). Thin-sec tions of these lime stones from the lower - area, our re search was car ried out along a lo cal road over a most part of the con glom er atic com plex con tain the Oxfordian dis tance of ~10 km. The cross-sec tion be gins ~7 km from the and Kimmeridgian microfossil as sem blages (Ap pen dix 1). It coast line of the Black Sea and runs north ward through sug gests that these con glom er ates can not be older than Pryvitne to wards the main ridge of the CM, up to Krasnolisia Kimmeridgian and younger than Berriasian. However, since the (Bilohirsk di rec tion). Ac cord ing to pre vi ous stud ies in this lo ca - 712 Nestor Oszczypko, Andrzej Ślączka, Ihor Bubniak, Barbara Olszewska and Małgorzata Garecka

Fig. 15. Rela tion of the Early Cre taceous debris flow conglom er ates to their flysch bedrock in the Vesele sec tion A – view from the road on the south ern slope of Perchem-Kaya (576 m a.s.l.) with very thick, NW-dip ping flysch se ries of TFF?; B – thin- to me dium-bed ded turbidites of TFF, roadcut; C – dark grey cal car e ous mudstones (sam ple WP 23); D – ver ti cally dip ping me dium-bed ded fine-grained sand stone, view on the lower surface with flute marks; E – ?Middle Juras sic /?volca ni c olistolith (a few metres across) within dark grey shales (sam ples WP 18 and 18A); F – graded debris-flow conglom erates and thick-bedded sand stones of the basal part of the Up per Ju ras sic/?Lower Cre ta ceous transgressive se ries, north ern side of road tion (Pivovarov and Derenyuk, 1984; Bilecki, 2006b; Mileev et TFF, fol lowed by a nar row zone of the Mid dle Ju ras sic sand - al., 2006; Afanasenkov et al., 2007; Yudin, 2009), the coastal stone/claystone flysch (J2). plain, up to 8 km wide, is com posed mainly of the TFF. Ac cord- In this place, our transect (Fig. 18) starts with strongly ing to Pivovarov and Derenyuk (1984), Up per Tri as sic-Lower tectonized black and dark grey shales, mudstones and thin- to Ju ras sic flysch depos its in this area are over lain by the Mid dle me dium-bed ded sand stones (Figs. 18 and 19A, B). These beds Ju ras sic flysch with in ter ca la tions of gravelites and lenses of are sub stan tially sim i lar to the upper part of the TFF (T3-J2) and coal. After Yudin (2009) the costal band of the TFF (T3-J2), bar ren in microfossils (WP 122). In a con glom er ate layer of WP ~3–4 km wide, is lim ited from the S and N by melange zones 125 (Figs. 18 and 19C), we rec og nized a block of dark rudstone com posed of the lower (T3-J1) and upper (T3-J2) parts of the with the spe cies of Troglotella incrustans Wernli and Fookes The po si tion and age of flysch de pos its in the Cri mean Moun tains (South ern Ukraine) 713

Fig. 16. Up per Ju ras sic/Lower Cre ta ceous con glom er ate se ries in the Vesele road section A – fine con glom erates at the base of sub-ver ti cally dip ping thick-bedded turbidite sand stones; B – thick-bed ded sand stone and lam i nated mudstones at the base of a few metres-thick se quence of chan nel de pos its; C – sub ma - rine slump conglom erates capped by lami nated mudstones; D – ma trix-supported debris flow with well-rounded cob bles; E – poorly sorted ma trix-sup ported con glom er ates; F – chaot i cal ly orga nized matrix-sup ported conglom - erate and microproblematic Koskinobullina socialis (Cherchi and de bris-flow de pos its (debrites with large olistostromes of Up per Schroeder) sug gest ing an age not older than Kimmeridgian. Ju ras sic micritic lime stones), as well as thick-bedded turbidites, Up per Aptian cal car e ous nannoplankton has re cently been re- which com monly display channelization. Con glom er atic se - ported from a site lo cated ~2 km to the east of WP 125 (see quences are sep a rated by few turbiditic se quences with me- Sheremet et al., 2016a: points 22 and 23, ta ble 3). Higher up dium- to thick-bed ded sand stones and dark grey mudstones or along our transect, folded dark flysch with in ter ca la tions of con - shales, which are few metres thick. The Pryvitne con glom er ate glom er ates is observed up to WP 134 (Fig. 18), where the com plex is over lain by a se quence of thin- and me dium-bed ded flysch de pos its are over lain by a very thick com plex, up to sand stones, sev eral tens of metres thick, with thin in ter ca la tions 1000 m thick, of sed i men tary brec cias and con glom er ates of shales (Figs. 18 and 19F). Microfossils iden ti fied in the in ves - build ing up the main range of the moun tains (Fig. 19D–E). They ti gated sam ples (WP 100 and 149) sug gest a Tithonian - rep re sent mainly var i ous types of sub ma rine slump de pos its, -Berriasian age or more likely Berriasian age (see Ap pen dix 1). 714 Nestor Oszczypko, Andrzej Ślączka, Ihor Bubniak, Barbara Olszewska and Małgorzata Garecka

Fig. 17. De bris-flow thick-bed ded con glom er ates and olistoliths of Upper Juras sic reef limestones along the cliff in Novy Svit A – sea shore cliff along a road to Novyi Svit; SW-dip ping con glom erates with sev eral huge blocks of rocks at the top (Koba-Kay – Callovian reef lime stones; see Nikishin at al., 2015b); B – western view of the Novyi Svit sea shore cliff, the Novyi Svit light house, and a thick series of channelized Ju ras sic/Lower Creta ceous con glom erates; C – lime stone block with a cast of brachi opod shell; D – cast of a Ju ras sic ?ammonite in a large lime stone boul der of Ju ras sic/Lower Creta ceous con glom erates

Fig. 18. Geo log i cal cross-sec tion Pryvitne-Bilohirsk The po si tion and age of flysch de pos its in the Cri mean Moun tains (South ern Ukraine) 715

Fig. 19. Typi cal lithofacies along the Pryvitne-Bilohirsk transect A – thin- to me dium-bed ded flysch of ?Taurida type, a nar row strongly deformed anticline (WP 123); B – ?Taurida-type flysch at the base of de bris-flow con glom erates; C – thick-bed ded con glom erates with boul ders and blocks of lime stones; D – fin ing-up ward conglom erate se quence near the pass; E – well-imbricated boul ders and cob bles of con glom erates with sandy/gravelly matrix; F – Creta ceous flyschoid depos its with lime stone in ter- ca la tions, di rectly above the top of conglom erates, be hind the pass (WP 149)

Fur ther along the pro file there is a se quence of thin- to Up per Barremian – sam ple WP 99b; Ap pen dix 1). Further to- thick-bed ded turbiditic sand stones and dark grey mudstones wards the north, the next sam ples WP 151a and b, taken from a with spo radic in ter ca la tions of very thick channelized con glom - re de pos ited con glom er ate block within grey mudstones, con - er ates. On the map of Pivovarov and Derenyuk (1984) these tain a foraminiferal as sem blage of Tithonian age (Ap pen dix 1). de pos its are re garded as Tithonian/Berriasian. Re cently, It ought to be stressed that these sam ples rep re sent re de pos - Shere met et al. (2014, 2016a) in cluded these beds into the Up- ited ma te rial and the Tithonian age is re lated to the primary age per Ju ras sic/Valanginian. Our sam ples (WP 99a and b) confirm of sed i ments be fore sub se quent re work ing. the Lower Cre ta ceous age (Lower Berriasian – sam ple 99a; 716 Nestor Oszczypko, Andrzej Œl¹czka, Ihor Bubniak, Barbara Olszewska and Ma³gorzata Garecka

Fig. 20. Corre la tion of Me sozoic sedi ments along the Black Sea coast

A – south ern termi na tion of the Kacha Uplift; B – Laspi Area; C – Ay-Petri and Yalta mas sifs, Dimerji Yayla; D – Karabi Yayla; E – east ern sec tor of the CM, east of Pryvitne; F – east ern sec tor of the CM, Vesele-Novyi Svit-Sudak

INTERPRETATION Be tween Yalta and Alushta, along the shore line, the TFF again re veals nu mer ous in tru sions of the Mid dle Jurasic volca- nites. The larg est in tru sion (3 x 4 km) of gab bro/bas alts is lo- RELATIONSHIP OF THE TFF cated near Hurzuf (Ayu-Dag, see Bilecki, 2006b; Yudin, 2009). TO THE YOUNGER DEPOSITS OF THE CM There are also large Mid dle Ju ras sic in tru sions of gab bro/dia - bases and plagiogranites in this area (e.g., Kastel; Bilecki, Our ob ser va tions and published data on the re la tion ship of 2006b; Solov’ev and Rogov, 2010). the TFF with youn ger de pos its in di cate that in the NW sector of In the post-Albian period, the Alushta-Salgir tec tonic zone the CM (Kacha Uplift) up to the Alushta-Salgir-Simferopol Fault was trans formed into the SE-dip ping thrust fault that moved the Zone, the TFF is transgressively over lain by the Lower Cre ta - Chatyr Dag Massif by at least 10 km to the west. East of this ceous, mainly Hauterivian, de pos its (Pivovarov and Derenyuk, fault zone, the TFF nar rows and then com pletely dis ap pears 1984; Bilecki, 2006b; Yudin, 2009, Sheret et al., 2014, 2016a; near the vil lage of Morske (Pivovarov and Derenyuk, 1984; see also Figs. 3 and 4). It sug gests that this area was emerged Bilecki, 2006b; Yudin, 2009). Be tween the Sarych Cup and and in tensely eroded dur ing the Late Ju ras sic/Berriasian. A dif - Alushta the TFF is over lain by the Mid dle Ju ras sic silt - fer ent sit u a tion is ob served along the west ern coastal part of the stone/claystone for ma tions, 250–300 m thick (Fig. 20; see also CM (Figs. 3, 4 and 20). Be tween the Sarych Cap and Bere hove, Bilecki, 2006a, b). The lower part of the se quence be longs to strongly de formed TFF, fol lowed by Mid dle Ju ras sic de pos its the Belbek Fm. (S mar gin of the Kacha Uplift) and the on the el e va tion up to 250–300 m a.s.l.; oc curs in a nar row Melaskaya Fm. (Laspi and Yalta/Ay-Petri sec tions), whereas zone. In some places, there are small sub-vol ca nic dykes and the top of the se quence is in cluded in the Ay-Vasil For ma tion. sills, re lated to the Mid dle Ju ras sic vol ca nism (Bilecki, 2006a). East of Alushta, the po si tion of the Mid dle Ju ras sic se ries is In this area, the TFF is over lain by the Mid dle Ju ras sic Melask oc cu pied by the Up per Ju ras sic con glom er ates, up to 800 m Fm. fol lowed by the Oxfordian/Kimmeridgian cor re la tive ho ri - thick (Lalomov, 2003, 2007). These con glom er ates dis cor - zon, ~50 m thick (see Oszczypko et al., 2012b, c). This unit dantly over lie the TFF and are cov ered by Tithonian/Berriasian could be partly cor re lated with both the Hurzuf (Bilecki, 2006a) car bon ate plat forms of the Demerji Yayla (cf. Bilecki, 2006b). and Sudak corelation ho ri zons (see Leshchukh et al., 1999). Sim i lar con glom er ates, de scribed by Bilecki (2006b) as the To wards the east, in the Berehove-Yalta uplifted block, we Tapshan (J2h3tp) or Khutoran beds (J3ht), are also found be low rec og nized the Up per Ju ras sic flysch (Lower Cre ta ceous ac - the Chatyr-Dag and Karabi-Yayla car bon ate plat forms (Fig. 20). cord ing to Sheremet et al., 2016a), overthrust by the Up per Ju - In both sec tions, the lower, red part of the con glom er ates is of ras sic car bon ate de pos its of the Ay-Petri-Yalta Massif (Kra- con ti nen tal or i gin. These de pos its prob a bly rep re sent al lu vial jewski and Olszewska, 2007; Krajewski, 2010). river system cones derived from the NW (granitoids from the Ukrai nian Shield, see Lalomov, 2007). Up per in the sec tion the The po si tion and age of flysch de pos its in the Cri mean Moun tains (South ern Ukraine) 717 red con glom er ates are re placed by grey de bris-flow con glom er - sian car bon ate plat form (Zhabina, 2008; Zhabina and Anike- ates de pos ited in a sub ma rine coastal fan delta (Lalomov, yeva, 2008) is re garded as a re gional cor re la tive ho ri zon of the 2007) or a Gilbert-type delta (Baraboshkin and Piskunov, Main Ridge of the CM, transgressively over lain by the Valan gi - 2010). The Demerji fan delta is a kind of half-graben cut by the nian/Haute rivian de pos its. Near the vil lage of Pryvitne, the Simferopol/Alushta Fault from the west, and edged to the east Korabi car bon ate plat form dis ap pears. On the map of Pivo- (Nikishin et al., 2015b). varov and Dere nyuk (1984), this boundary can be in ter preted Along the coast line, be tween the Sarych Cap in the west as a NW-SE scissor fault. In this in ter pre ta tion, the NW wing of and Pryvitne in the east, the TFF (T3-J1), fol lowed by Mid dle faults is oc cu pied by the Valanginian-Hauterivian car bon - Ju ras sic and Oxfordian/Kimmeridgian de pos its, are over lain ate/marly de pos its, while in the SE wing of the fault, the Ju ras - by the Tithonian/Berriasian car bon ate plat form. The thick ness sic/Cre ta ceous con glom er ates and flysch occur. In a sim i lar of this plat form ranges from ~500 m in the west (Sarych, way, the map of Yudin (2009) can be in ter preted. In the in ter - Laspi), ~800 m in the Ay-Petri Massif, ~1300 m in Demerji, pre ta tion of Sheremet et al. (2016a), the fault zone has a and ~500 m in Karabi yaylas in the east. The Titho nian/Berria - NE–SW di rec tion.

Fig. 21. The Late Tri as sic palaeotectonic po si tion and lithofacies of the south ern mar gin of Eur asia

Based on Golonka (2004, supple mented) 718 Nestor Oszczypko, Andrzej Ślączka, Ihor Bubniak, Barbara Olszewska and Małgorzata Garecka

PALAEOGEOGRAPHICAL RECONSTRUCTION with clastic ma te rial de rived from ero sion of the uplifted Scythian Platform (Lalomov, 2003, 2007). The width of this Dur ing the Late Tri as sic/Early Ju ras sic (plate po si tion at cone, could reach 50 km. Dur ing the Oxfordian ma rine trans - 225 Ma), the Taurida Flysch basin was lo cated in the back-arc gres sion from the south, the al lu vial cone in the north was po si tion (Golonka, 2004). This ba sin oc cu pied the south ern grad u ally trans formed into a ma rine fan delta. Dur ing the slope of the Scythian plat form and the Pontide deep-water ba - Kimme rid gian/Titho nian, this trans gres sion re sulted in the de- sin (Fig. 21). The mea sure ments of palaeotransport di rec tions vel op ment of an ex ten sive sea bay. Northw ards (Demerji - in the Bodrak Val ley show sup ply of clastic ma te rial from the -Zuya), this bay might have reached a width of 60 km. Tow ards NW. Dur ing the Early Juras sic (Nikishin, 2015b), marly/clay the west the bay prob a bly nar rowed to ~20 km. A car bon ate sed i ments were de pos ited in the north ern, shal low-wa ter part of plat form de vel oped in this bay and in the ad ja cent shelf area. the basin, lo cally follow ed by the ac cu mu la tion of Lower/Mid dle High sub si dence rate of this area in the period ~15 My al lowed Ju ras sic mudstones and claystones with coal-bear ing in ter ca la - the de po si tion of car bon ate se quence, up to 1500 m thick. At tions (Pivovarov and Derenyuk, 1984; Bilecki, 2006a; Ver- the same time, the pres ent-day Kacha Uplift was prob a bly still gelska, 2016). This was fol lowed by the Mid dle Ju ras sic fold ing, emerged and eroded. up lift and vol ca nic ac tiv ity in the north ern sec tor of the CM. Ac - It is unclear what happened at that time in the east ern sec - cord ing to Kruglov and Tsypko (1988), the fold ing and uplift tor of the CM. Per haps, dur ing the Mid dle Ju ras sic, par al lel were con nected with the Early Cim mer ian phase and took place with the uplift of the north-western sec tor of the CM, the re sid - only in the outer (WW) part of the Cri mea Ba sin, while in the in- ual flysch basin moved eastwards of the Pryvitne, to the Sudak ner (SE) part of this ba sin, deep-wa ter sed i men ta tion per sisted Trough. It was fol lowed by the Late Ju ras sic/Early Cre ta ceous to the Early Cre ta ceous. rift ing (Stovba et al., 2013) and in tense sub si dence in the east - In the north west ern, folded and uplifted part of Cri mea, ern sec tor of the CM, which obtained a con nec tion with the ero sion pro cesses con trolled the de vel op ment of the river net - sed i men tary area of the Great Cau ca sus (Fig. 22). Si mul ta- work, which sup plied the Chatyr-Dag-Demerji al lu vial cone, neously, a new source area appeared on the NW mar gin of the

Fig. 22. The Late Juras sic-Early Cre taceous palaeotectonic posi tion and lithofacies of the south ern mar gin of Eur asia

Based on Golonka (2004, sup ple mented) The po si tion and age of flysch de pos its in the Cri mean Moun tains (South ern Ukraine) 719

Sudak Trough. Dur ing the Late Ju ras sic and Early Cre ta - A def i nitely dif fer ent geo log i cal and strati graphic in ter pre ta - ceous, that area sup plied the basin with a huge amount of tion of the Prokhladne area was pre sented by Popadyuk et al. clastic ma te rial trans ported by turbidite and debris flows. At (2013) who, based on small foraminifera, in cluded the TFT of the same time, an active fault zone de vel oped at the bound ary the Bodrak Val ley into the Albian. That paper also pro vides in - be tween the east ern mar gin of the car bon ate plat form and the for ma tion about a find ing of the Albian-Cenomanian foraminifer Sudak Trough. This zone gen er ated sig nif i cant land falls of Gumbelina cenomanica Agal in the Mender bore hole at Up per Ju ras sic lime stones de rived to the Sudak Through as Prokhladne, at a depth of 94–200 m (Yanin, 1976). With this in olistoliths and olistostromes. This re sulted in pro gres sive mind, we want to re call that Marcinowski and Najdin (1976) re- west ward nar row ing of the east ern sec tor of the car bon ate ported the Up per Albian ammonites from sev eral sec tions near plat form, at least over a dis tance of ~10 km. De struc tion of the Prokhladne and gave in for ma tion about a bore hole drilled in the car bon ate plat form was ter mi nated with the be gin ning of the train ing cen tre MGU (Geo log i cal Fac ulty of Mos cow Uni ver sity). Valanginian/Hauterivian ma rine trans gres sion. In this drill ing, Up per Albian red marly mudstones occur down to a depth of 85 m, un der lain by Lower Ju ras sic de pos its of the Taurida For ma tion at a depth of 85–90 m. DISCUSSION East of the Karabi Yayla and north of Pryvitne, our in ves ti - ga tions have con firmed the pres ence of an other youn ger sub - ma rine con glom er atic fan sys tem (Tithonian) de pos ited by dif - Our re sults in di cate the ex is tence of at least two flysch for- fer ent den sity cur rents, which can rep re sent a coarse flysch se- ma tions in the CM: the Up per Tri as sic-Lower/?Mid dle Ju ras sic quence. The base of these con glom er ates is clearly vis i ble in and the Up per Ju ras sic/Lower Cre ta ceous ones. In ad di tion, both the Pryvitne and Vesele sections. the Aptian/Albian flysch-like de pos its might have been locally In the Privitne sec tion, the con glom er atic se quence, not de pos ited. The old est foraminiferal as sem blages that con tain youn ger than Berriasian, is un der lain by strongly de formed dark the spe cies Thuramminoides metensis (Terquem) and rare grey thin- to me dium-bed ded flysch, sim i lar to the TFF but not Thalmannammina canningensis Tappan were found in sev eral older than Kimmeridgian (WP 122–125). Pre vi ously-men tioned sam ples of brown and dark grey ferruginous siltstones in ter ca - flysch is re garded as Mid dle Ju ras sic (Pivovarov and Derenyuk, lated by turbiditic sand stones from the Bodrak Val ley, com - 1984) or Late Tri as sic-Early Ju ras sic in age (Yudin, 2009). Sim- monly regarded as be long ing to the TFF. These spe cies are i larly, we can in ter pret the po si tion of the vol ca nic block (WP 18) known only from the Late Tri as sic/Early Ju ras sic. No younger from the Vesele sec tion, un der lain and over lain by dark spe cies have been found. Sam ples of the TFF also show no siltstones, as Lower Ju ras sic at the base (WP 18) and Up per traces of re worked spe cies. Two sam ples (WP 11, 12) from this Ju ras sic/Lower Cre ta ceous (WP 18A; Ap pen dix 1) at the top. lo cal ity con tain stratigraphically sig nif i cant cal car e ous dino - These siltstones are sep a rated by a vol ca nic block. In such sit u- cysts: Nannoceratiopsis senex and N. gracilis, which in di cate a tion the Lower/Mid dle Ju ras sic foraminifera at the base of Early Juras sic age. There is also one sam ple (WP 16) that con - volcanites (WP 23 and 18) should be re garded as re worked. tains Wallodinium laganum, char ac ter is tic for the Late In the Novyi Svit sec tion, at the base of con glom er ates with Toarcian–Early Aalenian (see Oszczypko et al., 2012c). large blocks of Up per Ju ras sic reef lime stone, there are Lower To the south-east of the Kacha Up lift, three TFF sam ples Cre ta ceous dark marly shales (WP 115) sim i lar to that of the (WP 32, 34, 35) of brown and dark grey ferrugineous siltstones Sudak Flysch. The age of the Pryvitne and Vesele con glom er - con tain Thuramminoides metensis (Terquem) of Late Tri as- ates, over lain by the Lower Cre ta ceous shaly flysch fa cies (WP sic/Early Ju ras sic age. A sim i lar as sem blage with Thalmanna - 149, 99 and 151), may be es ti mated as Titho nian/Berriasian, mmina canningensis Tappan and Hyperammina aff. pediformis while the Novyi Svit con glom er ates may be long to the Lower Scherp was found near the Husynyi Ho tel (WP 39). This fora - Cre ta ceous. miniferal as sem blage sug gests an Early Juras sic age. Rocks of At sev eral lo cal i ties in the east ern sec tor of the CM, cal car e - the same age were found also to the east, in the Vesele sec tion ous nannoplankton not younger than Valanginian has re cently (WP 18 and 23), within beige micaceous mudstone re garded as been de ter mined (Sheremet et al., 2014, 2016a). The same a Lower Ju ras sic part of the TFF. youn ger dates (Hauterivian and Barremian) were ob tained by Near Sanatorne and Laspi, along the west ern part of the Pivovarov and Derenyuk (1984). Black Sea coast, we found dark grey flysch, sig nif i cantly dif fer - There are at least two flysch se quences within the CM: (1) ent from that of the Bodrak Val ley. In this area (WP 39/40; Figs. up per Tri as sic–Lower/Mid dle Ju ras sic, known from the west ern 1, 2 and 3B) the foraminiferal as sem blages typ i cal of Late Tri - sec tor of the CM as the TFF, and (2) Up per Ju ras sic/Lower Cre - as sic and Early Ju ras sic in cluded Hyperammina aff. pediformis ta ceous, de vel oped east of the Pryvitne-Bilohirsk line and typ i- Scherp (WP 39) in di cat ing Toarcian age. In ad di tion, the TFF is cal for the east ern sec tor of the CM. The Up per Ju ras sic/Lower over lain in this area by the Mid dle Ju ras sic flyschoid for ma tions Cre ta ceous flysch of the Sudak For ma tion passes up wards into (Ay-Vasil and Belbek) with a to tal thick ness of up to 500 m (Fig. a thick unit of con glom er ates and sand stones with blocks and 20; see also Bilecki, 2006a, b, 2007). The above-de scribed se- large olistoliths of Up per Ju ras sic lime stones, de pos ited by sub - quence of flysch and flyschoid sed i ments is over lain by the ma rine av a lanches and high-den sity turbiditic cur rents (Khart - Oxfordian/Kimmeridgian transgressive de pos its, iden ti fied at -Kaya Fm.). This se quence is ter mi nated by the Lower Cre ta - the base of the Tithonian/Berriasian car bon ate plat form ceous flyschoid marly deposits. (Oszczy pko et al., 2012b, c). This con firms un equiv o cally the Un clear is the geotectonic po si tion oc cu pied by a com plex Up per Tri as sic-Lower/Mid dle Ju ras sic po si tion of the TFF in of dark marly claystones and turbidites, ex posed along the road this part of the CM. To the east of Yalta, the Mid dle Ju ras sic from Simferopol to Alushta. In the north ern part of the area, flyschoid de pos its are re placed over a dis tance of ~25 km by a Pivovarov and Derenyuk (1984) dis tin guished the Albian clay- large sub ma rine con glom er atic fan (Fig. 20; see Up per Ju ras sic stones that oc cu pied a nar row ing to the south bay (see also Con glom er atic For ma tion, UJCF of Lalomov, 2007) of un cer - Marcinowski and Najdin, 1976). Re cently, in the south ern ex- tain age, but re cently re garded as Oxfordian and Kimme- ten sions of this bay, Popadyuk et al. (2013a, b) doc u mented the ridgian -Tithonian (Baraboshkin and Piskunov, 2010). Albian de pos its, and Sheremet et al. (2014, 2016a) found Up- 720 Nestor Oszczypko, Andrzej Ślączka, Ihor Bubniak, Barbara Olszewska and Małgorzata Garecka per Aptian-Lower Barremian rocks. Further to the south, at the zon has been doc u mented. It is partly an equiv a lent of the north ern edge of the Chatyr-Dag Yayla (WP 101) and along a Hurzuf and Sudak horizons. road (WP 107), we found the Albian dark marls and turbidites, 4. At the base of the Late Ju ras sic car bon ate plat form for merly re garded as the TFF (Pivovarov and Derenyuk, 1984; (Chatyr-Dag, Demerji and Karabi) and above the TFF, there are Bilecki, 2006b; Yudin, 2009). In our opin ion, the Aptian/Albian the Mid dle/Up per Ju ras sic al lu vial and delta fan con glom er ates de pos its re cently found in the TFF area along the west ern edge de rived from the NW. of the Dolhorukovska Yayla could be re lated to the 5. Dur ing the Late Ju ras sic/Early Cre ta ceous, the deep-wa - Aptian/Albian ma rine trans gres sion onto the TFF (Kacha Uplift, ter Sudak Ba sin de vel oped to the east of Pryvitne, sup plied with see Marcinowski and Najdin, 1976; Pivovarov and Derenyuk, coarse-grained de pos its sourced from the NW. These sed i - 1984). A sim i lar strati graphic po si tion is oc cu pied by the Up per ments were trans ported by de bris and den sity turbiditic flows. It Aptian-Albian de pos its near Zelenohorye, and by the Barre- is not ex cluded that the de pos its could pro vide the slope fa cies mian-Hauterivian rocks in Berehove, Yalta, and close to the of the flysch basin. Demerji Yayla (Sheremet et al., 2016a). 6. The ba sin was si mul ta neously sup plied with large blocks (olistoliths) of Up per Ju ras sic lime stones, de rived from de struc - tion of the east ern edge of the Karabi car bon ate platform. CONCLUSIONS 7. Ma jor ity of melanges dis tin guished in the CM, due to the ho mo ge ne ity of their ma te rial, are not true melanges, but rather strongly tectonized “bro ken for ma tions”, olistostromes and so- 1. At least two flysch for ma tions are found in the Cri mea -called “cha otic” sed i men tary deposits. Mts.: the Taurida (Up per Tri as sic to Lower/?Mid dle Ju ras sic) of the west ern sec tor of the CM, and the Up per Ju ras sic to Lower Acknow ledge m ents. Our re search in the Cri mea Mts. was Cre ta ceous flysch of the Sudak For ma tion (east ern sec tor of con ducted un der a grant of the Pol ish Na tional Sci ence Cen tre, the CM). The Up per Ju ras sic/Lower Ju ras sic flysch de pos its ti tled “Po si tion and age of the “Black Flysch” in the Carpa - has been also rec og nized near Berehove, the west of the Yalta. thian-Al pine orogen and the Cri mea Mts.” (N N 307 256139). Dr These de pos its prob a bly are pro longed along the shore line to- A. Murovska (Kiev, Ukraine), Prof. M. Sosson (Valbonne, wards the east. France) and an anon y mous re viewer pro vided crit i cal com- 2. Ad di tion ally, the Mid dle Ju ras sic flyschoid de pos its were ments on the early ver sions of the text. Dr E. Gedl (Kraków, Po- also ac cu mu lated (e.g., the Belbek and Ay-Vasil for ma tions) in land) de ter mined cal car e ous dino cyts. Thanks are also due to the west ern sec tor of the CM. Prof. J. Golonka (Kraków, Po land) for dis cus sions, and Dr Y. 3. Along the Black Sea be tween Sevastopol and Alushta, Volfman (Yalta, Ukraine) for dis cus sion and or ga ni za tion of above the TFF and be neath the Late Ju ras sic car bon ate plat - field work (2011). form, the Up per Oxfordian/Kimmeridgian Laspi cor re la tive ho ri -

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