Coal-bear ing sub ma rine slump sed i ments from Oligocene–Mio cene tran si tion of the East ern Outer Carpathians (Bieszczady Moun tains, SE Po land)
Krzysztof B¥K1, *, Anna WOLSKA1, Magdalena ZIELIÑSKA3 and Marta B¥K2
1 Ped a gog i cal Uni ver sity of Cra cow, In sti tute of Ge og ra phy, Podchor¹¿ych 2, 30-084 Kraków, Po land
2 AGH Uni ver sity of Sci ence and Tech nol ogy, Fac ulty of Ge ol ogy, Geo phys ics and En vi ron men tal Pro tec tion, al. A. Mickie - wicza 30, 30-059 Kraków, Po land
3 Uni ver sity of Silesia, Fac ulty of Earth Sci ences, Bêdziñska 60, 41-200 Sosnowiec, Po land
B¹k, K., Wolska, A., Zieliñska, M., B¹k, M., 2015. Coal-bear ing sub ma rine slump sed i ments from Oligocene–Mio cene tran si - tion of the East ern Carpathians (Bieszczady Moun tains, SE Po land). Geo log i cal Quar terly, 59 (2): 300–315, doi:
10.7306/gq.1224
The pa per pres ents a new find ing of lus trous coal par ti cles in the youn gest flysch sed i ments of the Silesian Nappe, East ern Outer Carpathians, out cropped in the Bieszczady Moun tains. The coal ma te rial oc curs in a 1 m thick sub ma rine slump layer in the Kiczera Dydiowska Sand stones that be long to the youn gest part of the Krosno Beds. Coal par ti cles are nu mer ous (up to 16%) in a mas sive sand stone of the slump layer. The siliciclastic par ti cles in these sed i ments are clas si fied as ma te rial de - rived from weath ered rocks of a con ti nen tal block or they have been re cy cled from post-orogenic sed i ments. Lus trous coal rep re sents coaly, mostly ho mo ge neous plant frag ments rep re sent ing macerals of the vitrinite group. The ran dom vitrinite reflectance var ies from 0.52 to 0.57%, which cor re sponds to high vol a tile bi tu mi nous rank. Some coal peb bles dis play a tree struc ture, typ i cal of gelified xylites, due to im preg na tion of cell walls by resinite. Its oc cur rence in this ma te rial in di cates ter - res trial plants pro duc ing waxes and res ins. Some of the gelified plant de bris shows ev i dence of pyritisation that, in the ab - sence of inertinite macerals in coal, may in di cate dysoxic con di tions dur ing the first de com po si tion pro cesses of or ganic mat ter un der an aque ous en vi ron ment. The coaly-bear ing slump moved down most prob a bly from the SE dur ing Oligocene–Mio cene tran si tion time. This shows that an intrabasinal ex otic mas sif, as an up lifted frag ment of ?Pre cam brian craton, which sup plied a large amount of siliciclastic ma te rial to the Silesian–Subsilesian ba sin dur ing the Early–Mid dle Oligocene, still ex isted at the end of the Oligocene.
Key words: coal peb bles, sub ma rine slump, foraminifera, Oligocene–Mio cene tran si tion, East ern Outer Carpathians, Bieszczady Mts.
INTRODUCTION
Cre ta ceous through Paleogene flysch sed i ments of the In - ner and Outer Carpathians con tain nu mer ous exotics of the Up - per Car bon if er ous coal and thin lay ers or lenses of autochthonous lus trous coal (for sum mary see Kotlarczyk, 1979; Matl, 1991; Wag ner, 1996). The Up per Car bon if er ous de tri tal ma te rial was sup plied by grav i ta tional flows mainly to the mar ginal parts of the Carpathian realm within the Silesian–Subsilesian and Skole–Tarèau bas ins. The coal exotics oc cur in var i ous frac tions of turbidites, show ing vari able petrographic and microfossil com po si tion (e.g., Bukowy, 1957;
Kotlarczyk and Œliwowa, 1963; Ladyzenski and Sawkiewicz, 1968; Turnau, 1970; Frankiewicz, 1974). They have been found in var i ous lithostratigraphic units. Most of them be long to
the Beriasian–Aptian strata in the West ern Outer Carpathians, and Berriasian to the Maastrichtian–Oligocene turbidite sed i - ments in the East ern Outer Carpathians (Kotlarczyk, 1979).
Sup ply of the allochthonous (ex otic) coal was pos tu lated based on microfloristic and petrographic stud ies. Most prob a bly, this ma te rial was sup plied as coal de tri tus to the West ern Outer Carpathian bas ins from the Up per Silesia Coal Ba sin and its con tin u a tion to the south, and to their east ern part from other Up per Car bon if er ous bas ins, re cently oc cur ring un der the nappes of the East ern Outer Carpathians (Bukowy, 1957;
Kotlarczyk and Œliwowa, 1963). Ac cord ing to Turnau (1970), both these ar eas may have formed a sin gle Precarpathian Coal Ba sin near the south ern mar gin of the Eu ro pean Plat form. It is also pos si ble that some of the so-called Up per Car bon if er ous coal lay ers oc cur ring in the flysch suc ces sions could be an ef - fect of carbonisation of much youn ger or ganic mat ter mixed with Car bon if er ous spores, as was doc u mented from the Maastrichtian–Paleocene and Oligocene sec tions in the Skole Nappe of the Outer Carpathians by Kotlarczyk (1979), and from the so-called “black flysch” in the Pieniny Klippen Belt (Birkenmajer and Turnau, 1962), dif fer ently dated as Early Ju - ras sic (e.g., Horwitz, 1937; Birkenmajer, 1957; Birkenmajer et
* Corresponding author, e-mail: sgbak@cyf-kr.edu.pl
Received: September 19, 2014; accepted: December 12, 2014; first published online: February 27, 2015
al., 2008) or Early Cre ta ceous (Sikora, 1962; Ksi¹¿kiewicz, 1972; Oszczypko et al., 2004, 2012).
How ever, autochthonous de tri tal coal which has been de - scribed mainly from mudstones and claystones as coalified de - bris oc curs also in var i ous frac tions of flysch sed i ments (Kotlarczyk, 1979; Matl, 1991; Wag ner, 1980). Ad di tion ally, it may cre ate lenses and thin lay ers, and co-oc cur with tree trunks or their frag mented stems (Zuber, 1918; D¿u³yñski and Œl¹czka, 1958; Kotlarczyk, 1979; Wag ner, 1980). This coaly or - ganic mat ter oc curs mostly in the Oligocene turbidites of the In - ner Carpathians (Podhale Flysch) and in the Eocene–Mid dle Mio cene of the East ern Outer Carpathians (Horwitz and Doktorowicz-Hrebnicki, 1932; Go³¹b, 1959; B¹kowski, 1967;
Frankiewicz, 1974; Kotlarczyk, 1979; Lipiarski and Peszat, 1984; Ladyzenski and Sawkiewicz, 1968; Zieliñska, 2010;
Wag ner, 2011, 2013). It was also found in the Mid dle Mio cene sed i ments of the Carpathian Foredeep and within intra-moun - tain de pres sions (Sarjusz-Makowski, 1947; Frankiewicz and Wag ner, 1982; Szafran and Wag ner, 1999). Coaly or ganic mat - ter is char ac ter ized by vari able coal rank from dull and bright brown coal to bi tu mi nous coal (Wag ner, 1980, 1992, 1996, 2011, 2013; Lipiarski and Peszat, 1984; Zieliñska, 2013).
Higher rank coal is com pared with ortho-lig nite (Wag ner, 2013).
Most of the Cre ta ceous–Eocene or ganic mat ter is the autochthonous coal de rived from the north ern mar gin of the Outer Carpathian bas ins, as was sug gested based on flute casts of turbidite lay ers. A much rarer source of bi tu mi nous coal is re - lated to emerged intra-basinal cor dil leras from which it was trans - ported by grav i ta tional flows to more in ter nal parts of the Outer Carpathian bas ins (e.g., Kotlarczyk, 1978; Zieliñska, 2013).
This study pres ents a new find ing of lus trous coal peb bles from the Oligocene–Mio cene tran si tion flysch sed i ments of the Silesian Nappe, East ern Outer Carpathians, out cropped in the Bieszczady Moun tains (Fig. 1). We dis cuss sed i men tary and petrographic fea tures of the coal-bear ing layer, petrographic fea tures of coal par ti cles and strati graphic po si tion of sed i ments con tain ing the coal-bear ing layer.
GEOLOGICAL SETTING
The Silesian Nappe, one of tec tonic units of the Outer Carpathians, con sists of a suc ces sion of Up per Ju ras sic through Mio cene flysch sed i ments. The coal-bear ing sed i - ments have been found in the south east ern part of the Silesian Nappe, out cropped in the Bieszczady Moun tains. It is rep re - sented only by the youn gest se ries, Oligocene–Mio cene in age.
These sed i ments, dis tin guished as the Krosno Beds, are com - posed of a 3.2 km thick flysch suc ces sion. In the Pol ish part of the Bieszczady Moun tains, the Krosno Beds have been sub di - vided into three in for mal lithostratigraphic units (Fig. 2), named as the lower, mid dle and up per di vi sions (¯ytko, 1968). De tailed geo log i cal map ping of the Bieszczady Moun tains al lowed rec - og ni tion of sed i men tary fea tures and stra tig ra phy of this suc - ces sion (Haczewski et al., 2007, 2015a, b). The lower di vi sion, up to 700 m thick, con sists of me dium- and thin-bed ded sand - stones and marlstones. The mid dle di vi sion, up to 1300 m thick, con sists of thick (up to 80 m) pack ages of thick-bed ded polymictic sand stones, the so-called Otryt Sand stones. The up - per di vi sion, up to 1200 m thick, con sists mostly of non-fis sile marlstones with con vo lute- and cross-lam i nated, thin-bed ded sand stones. The mid dle part of this di vi sion in cludes two ho ri - zons with coccolith lime stone bands, the Jas³o and the Zagórz lime stones, which are widely used as isochronous re gional mark ers within the Oligocene suc ces sions of the Outer
Carpathians (e.g., Jucha, 1958, 1969; Koszarski and ¯ytko, 1961; Jucha and Kotlarczyk, 1961; Haczewski, 1984, 1989).
The up per most part of the up per di vi sion con sists also of two len tic u lar pack ages (130 m and 25 m thick) of thick-bed ded low- to me dium-grained, mas sive, rarely cross- to par al lel-lam i nated sand stones, clas si fied as the Kiczera Dydiowska Sand stones (Haczewski et al., 2007).
LOCALITY OF THE COAL-BEARING LAYER
The out crop of sed i ments con tain ing lus trous coal peb bles and ac com pa ny ing coal de tri tus lies in a lo cal road cross ing the vil lage of Procisne, within the San River val ley in the Bieszczady Moun tains, Po land, close to the Pol ish/Ukrai nian bor der (Fig. 1). Struc tur ally, this sed i men tary suc ces sion is lo - cated on the NE limb of the DŸwiniacz Górny Syncline (Haczewski et al., 2007, 2015a). With re gard to the ge ol ogy of the area, the coal-bear ing layer oc curs in a turbidite suc ces sion, ca. 550 m above the Zagórz Lime stone (Fig. 2), a coccolith lime stone, rec og nized in this area by Haczewski (1972). The sed i ments are part of the sec ond pack age of the Kiczera Dydiowska Sand stones, which con sists here of two types of thick-bed ded sand stones (Fig. 3). The first of them con sists of thin- to me dium-grained sand stones with clayey-cal car e ous ce - ment in clud ing coal peb bles and clayey/silty clasts. The sec ond one is rep re sented by fine-grained, par al lel-, cross- and con vo - lute-lam i nated micaceous sand stones with cal car e ous ce ment.
METHODS
In ad di tion to field sed i men tary ob ser va tions, mi cro scopic anal y ses have been made dur ing this study, in clud ing: (1) micropalaeontological study of the coal-bear ing suc ces sion, (2) min er al ogy and pe trog ra phy of the coal-bear ing layer, and (3) pe trog ra phy of coal.
Six sam ples were col lected from the Procisne sec tion for microfossil study. Microfossils were ex tracted by re peated heat - ing up and dry ing in so dium car bon ate so lu tion. Res i dues were dried, and washed through 63 µm mesh sieves. Foraminiferal and di a tom spec i mens were man u ally picked up from the frac - tion 0.063–1.5 mm.
The petrographic study of the coal-bear ing sand stone layer was per formed on three thin sec tions us ing a NICON YM-EPI Eclipse E600POL op ti cal mi cro scope. The modal min er al ogy of the sed i ment was ob tained by count ing at least 700 points with a ZEISS au to matic coun ter in each thin sec tion. The frame work com po si tion (modal anal y sis) was quan ti fied us ing the point-coun ter method de scribed by Dickinson (1985). In con trast to the Gazzi-Dickinson method (Ingersoll et al., 1984), min er als
>63 µm within lithoclasts were counted as rock-form ing min er als of the lithoclast com po si tion (Decker and Helmold, 1985).
The petrographic study of coal is based on three sam ples.
The anal y ses were car ried out on pol ished sur faces of lump sam ples in clud ing de ter mi na tion of maceral com po si tion of coal us ing re flected white and flu o res cent blue light, un der mag ni fi ca - tion 400´. In or der to de ter mine the de gree of or ganic mat ter coalification, ran dom vitrinite reflectance was ex am ined. All mea - sure ments were ob tained in ac cor dance with ICCP (In ter na tional Com mit tee for Coal and Or ganic Pe trol ogy) re quire ments.
The re sid ual rock sam ples used in the petrographic stud ies and microfossil slides are housed at the In sti tute of Ge og ra phy, Ped a gog i cal Uni ver sity of Cra cow (col lec tion of K. B¹k).
Fig. 1A – the Outer Carpathians on the background of simplified geological map of Alpine orogens and their foreland; B, C – position of the study area in relation to main morphological (B) and geological units (C) (after Oszczypko, 2004 and Bryndal, 2014);
D, E – detailed geological maps of the Procisne region (after Haczewski, 1972; Haczewski et al., 2007, 2015a) with the location of study section
C.F. – Carpathian Foredeep, I.C. – Inner Carpathian, PKB – Pieniny Klippen Belt, S.N. – Subsilesian Nappe
RESULTS
LITHOLOGY AND STRUCTURE OF THE COAL-BEARING SUBMARINE SLUMP
The sec ond pack age of the Kiczera Dydiowska Sand stones ex posed at the vil lage of Procisne con tains a 22 m thick turbidite suc ces sion, in clud ing a 1 m thick de formed layer, which re sem bles a sub ma rine slump (Figs. 3 and 4). A three metres long ex po sure of this layer dis plays its spe cific in ter nal struc ture. The layer is com posed of wedge- and ball-shaped bod ies of co her ently to semicoherently folded al ter nat ing sand - stone, mudstone and thin claystone beds show ing folded or tilted in ter nal bed ding (Fig. 4). Mac ro scop i cally, the wedge- and ball-shaped bod ies con sist of poorly ce mented fine- to me - dium-grained mas sive sand stones, grey-yel low on weath ered sur faces due to fer rous com pounds in clayey-cal car e ous ma - trix. They con tain con torted lenses of lam i nated very fine- and fine-grained sand stones and mudstones, and slubs of shales or claystones. Claystones and shales in this layer are cal car e ous and grey in col our, oc cur ring as thin beds within folds and as rip-up clasts of var i ous di men sions in mas sive sand stone within wedge-shaped bod ies. The shales also form small ir reg u lar lenses con tain ing small rounded, ball-shaped lam i nated sand - stones and mudstones (Fig. 3). In ad di tion to claystone clasts, nu mer ous scat tered lus trous black coal par ti cles, from peb bles to de tri tus in shape, are pres ent in the wedge-shaped sand - stone bod ies of the slump layer (Fig. 5). The di men sions of coal peb bles vary be tween 1 and 3 cm (mid dle axis).
Slump folds are iso cli nal. In ter nal bed ding of lam i nated sand stone and mudstone pieces is dis cor dant, re sem bling imbricated slabs. The bot tom of the slump layer is sharp, and the top is mounded to flat.
PETROGRAPHY OF COAL-BEARING SLUMP SANDSTONES
The coal-bear ing mas sive sand stones from the slump layer in the Procisne sec tion rep re sent fine- to me dium-grained (0.21–0.063 mm and 0.63–0.21 mm) subarcos es/sublithare - nites us ing Folk’s clas si fi ca tion (Q–F–RF di a gram; Fig. 6). Most of min eral and lithoclast grains range from 0.2 to 0.5 mm in size, oc ca sion ally to 0.9 mm. The frame work grains are rounded and subrounded ac cord ing to the ter mi nol ogy af ter Pettijohn (1975).
The sand stones are mod er ately to well-sorted. Quartz is the dom i nant min eral in these sed i ments (Ta ble 1 and Fig. 7), with its a con tent vary ing be tween 48 and 61%. It com monly oc curs as “mo saic” and undulose grains (up to 50%; Fig. 8A). Coal par - ti cles are the sec ond ma jor com po nent of the sand stones (up to 16%). Nu mer ous grains are rep re sented by feld spar ac count ing for 9%. The ma jor ity of feld spar grains (4.5%) are strongly al - tered (seritised, kaolinised). Among the un al tered feld spars, K-feld spars (as orthoclase perth ite; Fig. 8B), microcline (Fig. 8C) and plagioclases (Fig. 8D) oc cur. Frag ments of phyllosilicate flakes oc cur in sub or di nate amounts, in clud ing white mica (Fig. 8A; up to 7%) and bi o tite (up to 3%). Bi o tite is of ten al tered show ing dif fer ent stages of the chloritisation pro - cess (Fig. 8B). Small chlorite flakes are also ob served. The sand stones con tain also heavy min er als, up to 0.2%. Trans par - ent heavy min er als are rep re sented by very sta ble min er als, Fig. 2. Lithostratigraphic subdivision and lithologic log of the
Silesian Nappe in the Bieszczady Mountains (Poland; after B¹k, 2005; Haczewski et al., 2015b)
Fig. 3. Detailed lithological log of the upper division of the Krosno Beds at Prosisne (Silesian Nappe, Polish Outer Carpathians, Bieszczady Mountains) with the position of samples
and photographs of submarine slump layer
Fig. 4. Slump layer exposed along a road at Procisne, Silesian Nappe, Polish Outer Carpathians, Bieszczady Mountains cl – calcareous claystone, ls – laminated fine-grained sandstone and mudstone, m – massive fine- to medium-grained sandstone,
sh – calcareous shale
Fig. 5. Coal particles (c), clay clast (cl) and coal detritus (cd) in sandstone from slump layer at Procisne, Silesian Nappe, Polish Outer Carpathians, Bieszczady Mountains
Fig. 6. Quartz–Feldspars–Rock fragments (Q–F–RF) discrimination diagram (after Folk, 1974) of massive sandstone from slump layer at Procisne, Silesian Nappe,
Polish Outer Carpathians, Bieszczady Mountains Samples: 1 – Proc-13a, 2 – Proc-13b, 3 – Proc-14
Fig. 7. Pie charts of modal composition of massive sandstone from slump layer at Procisne, Silesian Nappe, Polish Outer Carpathians, Bieszczady Mountains
Sam ples
Proc-13a Proc-13b Proc-14b
subarcose* sub-litharenite* subarcose*
%
Quartz
“mo saic” grains 49.5 35.4 44.8
undulose grain 1.1 2.0 2.9
non-undulose grain 10.8 10.3 13.1
Feld spars
plagioclases 2.0 2.0 2.7
K-feld spars
2.5 0.9 2.4
strongly al tered feld spars 4.5 4.2 2.9
Other min er als
withe mica
4.4 6.9 4.0
bi o tite/al tered bi o tite
2.1 2.9 2.4
chlorite
1.3 1.9 1.0
trans par ent heavy min er als 0 0.1 0.2
non trans par ent heavy min er als 1.1 1.7 1.3
Lithoclasts
gneiss es 1.8 1.6 1.9
gra nitic gneiss es/gran ites 1.7 1.4 1.8
schists 1.6 1.4 0.2
slates/phyllites 0 1.0 0.6
si li ceous rocks/chert 0.2 0.6 0.9
brown car bon ates 0.7 0.9 0.8
mudstones 0.1 0 0
vol ca nic rocks 0 0.4 1.0
Bioclasts coal macerals 8.2 15.8 1.1
Ce ment car bon ates + clay min er als 6.4 8.6 14.0
To tal con tent 100.0 100.0 100.0
* – names of the rocks af ter the clas si fi ca tion of Folk (1974)
T a b l e 1 Modal min er al ogy of mas sive sand stone from the slump coal-bear ing layer in the Procisne
sec tion, Silesian Nappe, Pol ish Outer Carpathians, Bieszczady Moun tains
Fig. 8. Microphotographs of grains and lithoclasts in sandstone from slump layer at Procisne, Silesian Nappe, Polish Outer Carpathians, Bieszczady Mountains
A – “mo saic” quartz grain and white mica flake (left), sam ple Proc-14b; B – pertithic orthoclase grain and al tered bi o tite flake (above), sam ple Proc-13a; C – microcline grain with char ac ter is tic tar tan-type twinning, sam ple Proc-14b; D – plagioclase grain (right) show ing mul ti ple lamellar al bite twinning, and mudstone lithoclast (left), sam ple Proc-13a; E – augen gneiss lithoclast, sam ple Proc-14b; F – gra nitic gneiss lithoclast, sam ple Proc-14b; G – gran ite lithoclast, sam ple Proc-14b; H – schist lithoclast, sam ple Proc-14b; I – si li ceous rock lithoclast, sam - ple Proc-14b; J – slate/phyllite lithoclast, sam ple Proc-14b; K – sid er ite lithoclast, sam ple Proc-14b; L – vol ca nic rock lithoclast (pum ice-rich tuff ?), sam ple Proc-14b; all pho to graphs un der crossed polars; scale bar for all pho to graphs is shown in A
such as tour ma line, rutile, zir con, and opaque min er als (2%) – an hy drous and hy drated iron ox ides.
The to tal con tent of rock frag ment grains var ies be tween 6 and 7%. The con tent of lithoclasts of meta mor phic rocks is vari able (Ta ble 1). They are rep re sented mainly by rocks of low- and me dium-grade re gional meta mor phism, such as gneiss es (Fig. 8E), gra nitic gneiss es (Fig. 8F), gran ites (Fig. 8G), schists (Fig. 8H), and slates/phyllites (Fig. 8I). Other grains, in clud ing si li ceous rocks (Fig. 8J), siderites (Fig. 8K), vol ca nic rocks (Fig. 8L) and mudstones (Fig. 8D), are less com mon (Ta ble 1).
The slump layer sand stones con tain pre dom i nantly the con - tact-po rous type of car bon ate ce ment (6–14%) with a mix ture of clay ma te rial. Some parts of the sand stones also con tain a ma - trix (up to 5%).
MICROFOSSILS FROM THE KICZERA DYDIOWSKA SANDSTONES
Six sam ples of cal car e ous shales from the Procisne sec tion (Fig. 3) re veal a poorly di ver si fied foraminiferal as sem blage (Ta ble 2) and un de ter min able radiolarian and di a tom moulds.
Among plank tonic foraminifers, four spe cies have been de ter - mined, in clud ing Globigerina praebulloides (Fig. 9B–D), Tenuitella munda (Fig. 9A), T. liverovskae and Tenuitellinata angustiumbilicata (Fig. 9E, F). The as sem blages of ben thic foraminifers con sist of well-pre served, partly pyritised, orig i nally cal car e ous, smooth-walled hyaline forms. Most nu mer ous are
Virgulinella chalkophila (Fig. 9H) and Nonionella liebusi (Fig. 9L), ac com pa nied by Virgulinella karagiensis (Fig. 9I), Chilostomela ovoidea (Fig. 9K), Fursenkoina mustoni (Fig. 9G), Praeglobobulimina pyrula, P. bathyalis (Fig. 9J), Am mo nia beccari, Cibicidoides lopjanicus, Stilostomella sp. and ag glu ti - nated forms, such as Bathysiphon sp. and Saccammina sp.
Large pyritised di a toms are a sig nif i cant com po nent in these sed i ments (Ta ble 2). Most of them are gonioid di a toms, an gu lar in out line, rep re sented by tri an gu lar spec i mens of Triceratium sp. (Fig. 9O) and el lip ti cal frustules of Odontella?
sp. (Fig. 9P). There are also dis coid di a toms (Fig. 9M, N) and spec i mens with long lin ear-el lip ti cal valves (Pyxilia? sp.;
Fig. 9R). Many spher i cal micronodules, over grown by large py - rite crys tals re sem bling radiolarian moulds, are a sub or di nate com po nent in the microfossil as sem blages.
PETROGRAPHY OF COAL PEBBLES
Coal peb bles from the Procisne sec tion oc cur as vitrain particules. Ran dom vitrinite reflectance mea sure ments dis play a range from 0.52 to 0.57%, in di cat ing the rank of high vol a tile bi tu mi nous coal (Tay lor et al., 1998).
Or ganic mat ter is rep re sented mostly by the vitrinite group.
Collotelinite, which is dom i nant among the main macerals, forms very thin lenses (1–3 mm) at tain ing a length of 8–10 mm (Fig. 10A, B). The lenses are dis trib uted par al lel to each other
Pr-1 Pr-2 Pr-4 Pr-5 Pr-6 Pr-7
Bathysiphon sp. 1
Saccammina sp. 1 1
Stilostomella sp. 1
Globigerina praebulloides Blow 3 3
Tenuitella liverovskae (Bykova) 1
Tenuitella munda (Jenkins) 2 4
Tenuitella sp. 3
Tenuitellinata angustiumbilicata (Bolli) 2 2
Praeglobobulimina bathyalis (Reiser) 2
Praeglobobulimina pyrula (d’Orbigny) 2 1
Fursenkoina mustoni (Andreae) 2
Virgulinella chalkophila (Hagn) 20 4
Virgulinella karagiensis Mikhailova 4 1 1
Virgulinella sp. 7
Nonionella liebusi Hagn 7 1
Chilostomella ovoidea Reuss 3 1
Am mo nia beccari (Linne) 1
Cibicidoides lopjanicus (Myatlyuk) 1
Cibicidoides sp. 1 1
Diatomae – Triceratium sp. 2 5
Diatomae – dis coid morphotype 8 5
Diatomae – ?Odontella sp. 17
Diatomae – ?Pyxilia sp. 3
Spher i cal pyritysed moulds of ?radio lar ians 5 1 8
Echinoid spines 3 1 1
T a b l e 2 Microfossils in rock sam ples from the Procisne sec tion,
Silesian Nappe, Pol ish Outer Carpathians, Bieszczady Mts.
Fig. 9. SEM photomicrographs of foraminifers and diatoms from the Procisne section, Kiczera Dydiowska Sandstones of the Krosno Beds, Silesian Nappe, Polish Outer Carpathians, Bieszczady Mountains
A – Tenuitella munda (Jenkins), sam ple Proc-6; B–D – Globigerina praebulloides Blow: B – sam ple Proc-6, C, D – sam ple Proc-5; E – Tenuitellinata angustiumbilicata (Bolli), sam ple Proc-5; F – Tenuitellinata cf. angustiumbilicata (Bolli), sam ple Proc-5; G – Fursenkoina mustoni (Andreae), sam ple Proc-1; H – Virgulinella chalkophila (Hagn), sam ple Proc-2; I – Virgulinella karagiensis Mikhailova, sam ple Proc-2; J – Praeglobobulimina bathyalis (Reiser), sam ple Proc-2; K – Chilostomella ovoidea Reuss, sam ple Proc-6; L – Nonionella liebusi Hagn, sam ple Proc-4; M, N – Diatomae indet gen sp., sam ple Proc-2; O – Triceratium sp., sam ple Proc-7; P – Odontella sp., sam ple Proc-2;
R – diatomae indet gen sp., sam ple Proc-2; scale bar is 100 µm
(Fig. 10C). Colotellinite is also vis i ble as dis persed re mains around vitrain lenses (Fig. 10D). The sec ond com po nent of the vitrinite group is tellinite, both with empty win dow cells (Fig. 10E) and im preg nated with resinite (Fig. 10F). In wide vitrain lenses, a grad ual tran si tion from tellinite (oc cur ring in the cen tral part) to colotellinite (in the mar ginal part) is vis i ble. The sec ond maceral group of the coal peb bles is the liptinite group rep re sented by resinite char ac ter ized by or ange col our un der blue flu o res cent light.
An other char ac ter is tic min eral com po nent in coal is py rite oc cur ring around or ganic re mains and fill ing the inter gra nu lar space. The py rite is also ob served as framboids that are dis trib - uted in collotelinite (Fig. 10G) and scat tered in the min eral frac - tion of mas sive sand stone (Fig. 10H).
DISCUSSION
STRATIGRAPHY OF THE SUCCESSION WITH COAL-BEARING SLUMP LAYER
Biostratigraphy of the Oligocene in the Outer Carpathians ren ders some prob lems. Plank tonic foraminiferal spe cies, usu - ally poorly pre served, oc cur as sin gle spec i mens, or they are ab sent (e.g., Olszewska, 1984a, b, 1997, 1998; B¹k, 1999, 2005).
Plank tonic forms from the stud ied sec tion are typ i cal of the Oligocene in the Outer Carpathians, but they do not con strain the age of these sed i ments. Con se quently, the strati graphic po - si tion of the sed i ments is here sug gested based on a com par i - son with sec tions from the area lo cated a few kilo metres to the SE of Procisne in the same tec tonic unit, the DŸwiniacz Górny Syncline. Biostratigraphy of these sed i ments has been stud ied in both the syncline limbs by B¹k (2005). They rep re sent the up - per part of the Tenuitella munda and Globigerinoides primordius plank tonic foraminiferal zones there, cor re spond ing to the up per part of the NP24 through NN1 cal car e ous nannoplankton zones (Garecka in Haczewski et al., 2015b).
Due to the po si tion of the coal-bear ing slump layer within the up per most part of the Kiczera Dydiowska Sand stones, its strati - graphic po si tion may roughly cor re spond to the Oligocene–Mio - cene tran si tion.
PARENT ROCKS OF MINERAL GRAINS IN SLUMP LAYER
The ra tios of feld spars, quartz and lithic grains, pre sented for the sand stones in ter nary di a grams (Fig. 11), in di cate that their min er als could orig i nate from rocks of a con ti nen tal block or they have been re cy cled from post-orogenic sed i ments (Dickinson, 1985). Such or i gin may be con firmed by a low con tent of feld - spars and vol ca nic rocks within the min eral as sem blages (cf.
Dickinson and Suczek, 1979). The oc cur rence of undulose and
“mo saic” quartz grains in un struc tured sand stones within the slump layer im plies their or i gin from low- and me dium-grade meta mor phic rocks, such as slates, gra nitic gneiss es, gneiss es or schists. On the other hand, the pres ence of subrounded and rounded grains, and the oc cur rence of very sta ble heavy min er -
Fig. 10. Microphotographs of coaly organic matter from slump layer at Procisne, Silesian Nappe, Polish Outer Carpathians, Bieszczady Mountains
A, B – typical collotelinite (ct) impregnated with pyrite (S); C – collotelinite lenses parallel to each other; D – idspersed remains of collotelinite; E – telinite (Tl) with empty window cells; F – telinite impregnated with resinite (Re); G – collotelinite impregnated with pyrite
(S); H – pyrite framboids in mineral setting; all photographs under reflected light, with oil immersion, and at the same scale (Figure H) Fig. 11. F–Qt–L (A) and F–Qm–Lt (B) ternary discrimination diagrams of sandstone from slump layer at Procisne, related to different tectonic provenances (after Dickinson et al., 1983) F – to tal feld spar, L – to tal lithic frag ments in clud ing extrabasinal car bon ate lithic frag ments, Lt – to tal lithic frag ments in clud ing extrabasinal car bon ate lithic frag ments plus polycrystalline quartz, Qm – monocrystalline quartz, Qt – to tal monocrystalline and polycrystalline chert; sam ples: 1 – Proc-13a, 2 – Proc-13b, 3 – Proc-14
als (rutile, tour ma line, zir con) within the sand stones show, long re cy cling pro cesses of the pri mary rocks.
ORIGIN OF COAL MATERIAL
Lus trous coal par ti cles found in the slump layer do not rep - re sent an ex otic Car bon if er ous ma te rial. Lam i nar struc ture char ac ter is tic of the ex otic Car bon if er ous coal peb bles has not been de tected in coal of the stud ied ma te rial. Nu mer ous coaly plant frag ments found in these sed i ments are the re sult of post-diagenetic pro cesses of land-de rived or ganic mat ter, which was semi-con tem po ra ne ous with the slump layer.
Petrographic com po nents of coaly or ganic mat ter are mostly ho mo ge neous and be long to the vitrinite group. Vitrinisation of or ganic mat ter oc curred within the sed i ment af ter fi nal de po si - tion at the ba sin floor. It is con firmed by in ter me di ate val ues of vitrinite reflectance (ca. 0.5%) with their low range sug gest ing sim i lar diagenetic and catagenetic changes of organic matter particles.
The or i gin of or ganic mat ter is re lated to the com po si tion of tis sue plant com po nents dif fer ing in the gelification and frag - men ta tion ex tent. The plant frag ments with well-pre served cel - lu lar struc ture, which is re flected in the pres ence of telinite, and com pletely gelified plant frag ments in di cate var i ous plant re sis - tance lev els to bio chem i cal de com po si tion due to both mi cro or - gan ism ac tiv ity and me chan i cal dis in te gra tion, in clud ing drag - ging and fric tion. Part of the coaly ma te rial with grad ual tran si - tion from tellinite (in the cen tral part) to colotellinite (in the mar - ginal part) in wide vitrain lenses is ev i dence of set back gelification processes after burial within the sediment.
Some coal peb bles dis play well-pre served tree struc ture, typ i cal of gelified xylites, due to im preg na tion of cell walls by resinite. Fur ther more, the oc cur rence of resinite in this ma te rial in di cates a spe cific type of ter res trial plants pro duc ing waxes and resins.
The oc cur rence of py rite framboids in coaly or ganic mat ter, which is pro duced dur ing de com po si tion of plant ma te rial by bac te ria un der spe cific re dox con di tions (e.g., Can field, 1989;
Wilkin et al., 1996; Wilkin and Barnes, 1997), in the ab sence of inertinite macerals in the coal peb bles, which in turn may in di - cate oxi dis ing con di tions in the pri mary en vi ron ment, sug gests that the first de com po si tion of or ganic mat ter with its gelification took place in a wa ter en vi ron ment un der dysoxic con di tions.
Most of the gelified plant de bris do not show ev i dence of pyritisation. It means that they had stayed for a long time in a wa ter col umn be fore they were bur ied in the sed i ment.
PROVENANCE OF SUBMARINE SLUMP
Axes of the larg est slump folds are ori ented SW–NE with the vergence in di cat ing the slump moved down to the NW. The trend of axes of small-scale folds is ir reg u lar. On the other hand, palaeocurrent data from turbidite sand stone lay ers of the Kiczera Dydiowska Sand stones (Haczewski et al., 2007, 2015b) sug gest that tur bid ity cur rents flowed from the NW, most likely from the south ern slope of the Eu ro pean Plat form. Tak ing into ac count the ori en ta tion of fold struc tures, we can care fully sug gest that the slump moved down from the SE (Fig. 12).
The li thol ogy of the slump layer, which con tains frag mented lay ers of fine-rhyth mic cross- and wavy-lam i nated fine-grained sand stones and mudstones, shows that these pack ages are more likely to have been de pos ited from tur bid ity cur rents on a ba sin floor rather than on a slope, and af ter their par tial
lithification they have been in volved into the slump. On the other hand, the pe trog ra phy of me dium-sized min eral grains, in clud ing lus trous coal par ti cles of var i ous sizes, which are com po nents of mas sive sand stones, points to ma te rial de rived from a shal low part of the ba sin. Hence, the ini tial stage of slump ing could rep re - sent a mo tion of a muddy-silty flow from the up per part of the slope. Whereas, dur ing the sub se quent stages of move ment, ero sion with dis rup tion and fold ing of the par tially con sol i dated turbidites took place. Such a slump ing mech a nism was also sug - gested by D¿u³yñski and Œl¹czka (1958) for other sub ma rine slump ing lay ers from the an cient Silesian Ba sin. These au thors pre sented the ex am ples of sim i lar in con sis tences be tween trans - port di rec tions of turbidites al ter nat ing the slump lay ers within the Oligocene suc ces sion of the Krosno Beds, and the vergencies of folds within those slumps. The fine-rhyth mic turbidites orig i nated from var i ous di rec tions cor re spond ing mostly to the lon gi tu di nal ex ten sion of the Silesian Ba sin, whereas ma te rial of the slump lay ers and coarse-grained turbidites (in clud ing the Otryt Sand - stones) came from the S and SE.
PALAEOGEOGRAPHIC IMPLICATIONS
Dur ing the Oligocene, a synorogenic ba sin (as part of the Cen tral Paratethys Sea) was formed and filled with a thick turbidite se ries of the or ganic-rich Menilitic Shales fol lowed by micaceous cal car e ous sand stones with grey marlstones, known as the Krosno Beds in the West ern and East ern Carpathian realm (e.g., Opolski, 1933; Ksi¹¿kiewicz, 1962).
The stud ied slump sed i ments of the Kiczera Dydiowska Sand - stones rep re sent the youn gest part of the Krosno Beds, cor re - Fig. 12. Lo ca tion of the ex otic ridge as a source of or ganic par ti - cles sup plied within the slump sed i ments to the Silesian Ba sin (a part of the Menilite–Krosno Ba sin) dur ing Oligocene–Mio - cene tran si tion time, based on sim pli fied palaeogeographic map af ter Oszczypko and Oszczypko-Clowes (2006, sup ple - mented)
spond ing to the Oligocene–Mio cene tran si tion. Their re cent tec tonic po si tion in the Silesian Nappe (within the DŸwiniacz Górny Syncline) points to an al most cen tral po si tion within the Silesian–Subsilesian ba sin dur ing the Late Oligocene–Early Mio cene. The cen tral part of this subbasin was a main depocentrum of turbidite sed i men ta tion at that time, dom i nated at the be gin ning by de po si tion of fine-rhyth mic micaceous turbidites and fol lowed by thick-bed ded sand stones with vari - able min eral com po si tion, con tain ing nu mer ous mus co vite, weath ered feld spar grains and lime stone clasts (Opolski, 1933;
¯ytko, 1968). The lat ter sed i ments are clas si fied as the sand - stones of the Lesko fa cies, in clud ing among oth ers the Kiczera Dydiowska Sand stones. The change in type of ma te rial trans - ported to the ba sin floor was re lated to changes in their source ar eas. Dur ing the Late Oligocene, tur bid ity cur rents flowed from the NW along the ba sin axis, most prob a bly from the mar ginal part of the Eu ro pean Plat form (D¿u³yñski and Œl¹czka, 1958;
Haczewski et al., 2007). Later, other sources were of greater im por tance. Flute casts on soles of thick-bed ded sand stones in di cate vari able trans port di rec tions from the north-west, north and south (Opolski, 1933; D¿u³yñski and Œl¹czka, 1958;
Haczewski et al., 2015b). The lat ter di rec tions were dom i nant dur ing the Early–Mid dle Oligocene in this area, when the thick suc ces sion of thick-bed ded Otryt Sand stones was de pos ited there (Haczewski et al., 2007). The petrographic com po si tion of mas sive sand stone from the slump layer, char ac ter ized by a vari able con tent of quartz grains (mainly “mo saic” meta mor phic quartz) and nu mer ous lithoclasts of meta mor phic rocks is sim i - lar to that from the Otryt Sand stones, which ad di tion ally con tain olistostromes in clud ing di ver si fied meta mor phic rocks (e.g., Œl¹czka and Wieser, 1962; Tokarski, 1975; Ziemianin and Wolska, 2014). It may sug gest that a part of an intrabasinal mas sif, as the up lifted frag ment of ?Pre cam brian craton, still ex - isted at the end of the Oligocene. It sup plied a large amount of siliciclastic ma te rial to the south ern part of the Siles - ian–Subsilesian ba sin dur ing the Early–Mid dle Oligocene. Ac - cord ing to Œl¹czka (1963), B¹k et al. (2001) and Haczewski et al. (2007), this intrabasinal mas sif could rep re sent a NW ex ten - sion of the Marmarosh or Rachov mas sifs. In an other palaeogeographic in ter pre ta tion pro posed by Oszczypko and Oszczypko-Clowes (2006), there oc cur an un named intrabasinal ridge be tween the Magura pig gy back ba sin and the Silesian–Subsilesian–Skole Ba sin, ly ing in the same basinal po si tion as the Silesian Ridge (Fig. 12). Ir re spec tive of the name as signed, the au thors ac cept the lat ter in ter pre ta tion which takes into ac count the pres ence of a sub merged source of ter res trial or ganic ma te rial, lo cated to the south of the Silesian–Subsilesian–Skole Ba sin dur ing the lat est Oligocene–ear li est Mio cene.
CONCLUSIONS
Coaly or ganic mat ter com monly oc curs in the Cre ta - ceous–Neo gene flysch sed i ments of the Carpathians. It is char - ac ter ized by vari able coal rank from dull and bright brown coal to bi tu mi nous coal. The pres ent pa per con tains data on coal par ti cles from the youn gest turbidite sed i ments of the Silesian Nappe (Pol ish Outer Carpathians), lat est Oligocene–ear li est Mio cene in age, based on plank tonic foraminiferal data, where lus trous coal par ti cles oc cur in sand stones of the sub ma rine slump layer. Such oc cur rence of coal of fers an op por tu nity for in ter pre ta tion of the fea tures of the source area of or ganic mat - ter and siliciclastic ma te rial sup plied to the deep ba sin floor from other di rec tions than most of turbidites in the same area. This is sug gested based on the vergence of folds within the stud ied slump layer, which is dif fer ent than the trans port di rec tions in ter - preted from flute casts of the sur round ing turbidite beds.
If the di rec tion of slump move ment is cor rectly in ter preted (from SE to NW), the source ar eas of ter res trial ma te rial pre - served in the slump layer could rep re sent an intrabasinal cor dil - lera (ridge) be tween the Magura pig gy back ba sin to the south and the Menilite–Krosno Ba sin to the north, which was vari ably ac tive (up lifted) dur ing the whole Oligocene. Tak ing into ac - count the min eral com po si tion of the slump layer sand stones, this ridge was built mainly of meta mor phic rocks as so ci ated by cal car e ous sed i men tary strata. It seems that these sed i men tary rocks were strongly eroded ear lier, i.e. dur ing the Early–Mid dle Oligocene, and trans ported by grav ity cur rents (in clud ing olistostromes) to the Silesian–Subsilesian Ba sin.
Lus trous coal peb bles from the slump layer rep re sent coalified or ganic mat ter of Late Oligocene–Early Mio cene veg e - ta tion. Their fea tures in di cate the ex is tence of coastal plains or la goons within the shelf zone of an intrabasinal ridge. Ter res trial or ganic mat ter, in clud ing plants that pro duced waxes, could be partly de graded there un der oxic/dysoxic con di tions with out burial, where it was sub ject to quick gelification. None the less, most of the or ganic ma te rial un der went the gelification pro cess at the deep ba sin floor af ter trans port and burial, partly un der dysoxic con di tions, which is in ter preted from the oc cur rence of py rite framboids in or ganic par ti cles.
Aknowledgements. This pa per was sup ported by Funds of Ped a gog i cal Uni ver sity of Cra cow and AGH Uni ver sity of Sci ence and Tech nol ogy, awarded to K. B¹k (DS-UP WGB No 6n) and to M. B¹k (DS-AGH WGGiOŒ-KGOiG No 11.11.140.173). We are grate ful to Y.V. Koltun (Ukrai nian Acad emy of Sci ences, Lviv), N.
Oszczypko (Jagiellonian Uni ver sity, Kraków), and J. Soták (Slo - vak Acad emy of Sci ences, Banská Bystrica). Thanks also go to T.
Peryt (Pol ish Geo log i cal In sti tute – Na tional Re search In sti tute, Warszawa) for use ful ed i to rial cor rec tions. Spe cial thanks go to K.
Leszczyñski for im prov ing the Eng lish text.
REFERENCES
B¹k, K., 1999. Late Oligocene Foraminifera from the Krosno Beds in the San val ley sec tion (Bieszczady Moun tains); Silesian Unit, Pol ish Outer Carpathians. Annales Societatis Geologorum Poloniae, 69: 195–217.
B¹k, K., 2005. Foraminiferal biostratigraphy of the Egerian flysch sed i ments in the Silesian Nappe, Outer Carpathians, Pol ish part
of the Bieszczady Moun tains. Annales Societatis Geologorum Poloniae, 75: 71–93.
B¹k, K., Rubinkiewicz, J., Garecka, M., Machaniec, E., Dziubiñska, B., 2001. Exotics-bear ing layer in the Oligocene flysch of the Krosno Beds in the Fore-Dukla Zone (Silesian Nappe, Outer Carpathians), Po land. Geologica Carpathica, 52:
159–171.
B¹kowski, Z., 1967. Phoe nix szaferi sp. nov. z górnego eocenu Podhala oraz zarys historii rodzaju Phoe nix L (in Pol ish). Prace Muzeum Ziemi, 10: 169–213.
Birkenmajer, K., 1957. Sed i men tary char ac ter is tics of the Flysch Aalenian in the Pieniny Klippen Belt (Cen tral Carpathians). Bul - le tin de l’Académie Po lo naise des Sci ences, 5: 451–456.
Birkenmajer, K., Turnau, E., 1962. Car bon if er ous micro spores as sec ond ary de posit in the Aalenian flysch of the Pieniny Klippen Belt. Bul le tin de l’Académie Po lo naise des Sci ences, Série des Sci ences Géologiques et Géographiques, Varsovie, 10: 99–103.
Birkenmajer, K., Gedl, P., Myczyñski, R., Tyszka, J., 2008. “Cre ta - ceous black flysch” in the Pieniny Klippen Belt, West Carpathians: a case of geo log i cal mis in ter pre ta tion. Cre ta ceous Re search, 29: 535–549.
Bryndal, T., 2014. A method for iden ti fi ca tion of small Carpathian catch ments more prone to flash flood gen er a tion based on the ex am ple of south-east ern part of the Pol ish Carpathians.
Carpathian Jour nal of Earth and En vi ron men tal Sci ences, 9:
109–122.
Bukowy, S., 1957. Wêgiel kamienny w Karpatach brze¿nych (in Pol ish). Przegl¹d Geologiczny, 5: 577–578.
Can field, D.E., 1989. Sul fate re duc tion and oxic res pi ra tion in ma - rine sed i ments: im pli ca tions for or ganic car bon pres er va tion in euxinic en vi ron ments. Deep Sea Re search A, 36: 121–138.
Decker, J., Helmold, K.P, 1985. The ef fect of grain size on de tri tal modes: a test of the Gazzi-Dickinson point-count ing method – dis cus sion. Jour nal of Sed i men tary Pe trol ogy, 55: 618–620.
Dickinson, W.R., 1985. In ter pret ing prov e nance re la tions from de - tri tal modes of sand stones. NATO ASI Se ries C, Math e mat i cal and Phys i cal Sci ences, 148: 333–363.
Dickinson, W.R., Suczek, C.A., 1979. Plate tec ton ics and sand - stones com po si tions. AAPG Bul le tin, 63: 2164–2182.
Dickinson, W.R., Beard, G.R., Brakenridge, G.R., Erjavec, J.L., Frrguson, R.C., Inman, K.F., Knepp, R.A., Lindberg, F.A., Ryberg, P.T., 1983. Prov e nance of North Amer i can Phanerozoic sand stones in re la tion to tec tonic set ting. GSA Bul - le tin, 94: 222–235.
D¿u³yñski, S., Œl¹czka, A., 1958. Di rec tional struc tures and sed i - men ta tion of the Krosno beds (Carpathian flysch). Rocznik Polskiego Towarzystwa Geologicznego, 28: 205–260.
Folk, R.L., 1974. Pe trol ogy and Sed i men tary Rocks. Aus tin TX, Hemphill Press.
Frankiewicz, J., 1974. Znaleziska eoceñskiej flory we fliszu podhalañskim grzbietu guba³owskiego (in Pol ish). Sprawozda - nia z Posiedzeñ Komisji Nauk Geologicznych PAN, Oddzia³ w Krakowie, 18: 321–323.
Frankiewicz, J., Wag ner, M., 1982. Brown coal de pos its in Grudna Dolna; char ac ter of coal and pos si bil i ties of its ex ploi ta tion (in Pol ish with Eng lish sum mary). Zeszyty Naukowe AGH, Geologia, 4: 67–88.
Go³¹b, J., 1959. On the ge ol ogy of the West ern Podhale Flysch area (in Pol ish with Eng lish sum mary). Biuletyn Instytutu Geologicznego, 149: 225–239.
Haczewski, G., 1972. Badania geologiczne miêdzy Smolnikiem a Mucznem w Bieszczadach (in Pol ish). Kwartalnik Geologiczny, 16: 488–489.
Haczewski, G., 1984. Cor re la tion of laminae in chronohorizons of Jas³o lime stone and Zagórz lime stone (Outer Carpathians) (in Pol ish with Eng lish sum mary). Kwartalnik Geologiczny, 28:
675–688.
Haczewski, G., 1989. Coccolith lime stone ho ri zons in the Menilite–Krosno se ries (Oligocene, Carpathians) – iden ti fi ca - tion, cor re la tion and or i gin (in Pol ish with Eng lish sum mary).
Annales Societatis Geologorum Poloniae, 59: 435–523.
Haczewski, G., Kukulak, J., B¹k, K., 2007. Ge ol ogy and re lief of the Bieszczady Na tional Park (in Pol ish with Eng lish sum mary).
Wydawnictwo Naukowe Uniwersytetu Pedagogicznego w Krakowie.
Haczewski, G., B¹k, K., Kukulak, J., Mastella, L., Rubinkiewicz, J., 2015a. Szczegó³owa Mapa Geologiczna Polski, 1:50 000,
arkusz Ustrzyki Górne (1068) (in Pol ish). Pañstwowy Instytut Geologiczny, Warszawa.
Haczewski, G., B¹k, K., Kukulak, J., Mastella, L., Rubinkiewicz, J., 2015b. Objaœnienia do Szczegó³owej Mapy Geologicznej Polski, 1:50 000, arkusz Ustrzyki Górne (1068) (in Pol ish).
Pañstwowy Instytu Geologiczny, Warszawa.
Horwitz, L., 1937. La faune et l’âge des couches á Posidonomyes, Zone Piénine des Klippes, Karpates Po lo naises. A. Partie génerale. Sprawozdania Pañstwowego Instytutu Geologicz - nego, 8: 69–127.
Horwitz, L., Doktorowicz-Hrebnicki, S., 1932. O wêglu w Szczawnicy i okolicach (in Pol ish). Posiedzenia Naukowe Pañstwowego Instytutu Geologicznego, 33: 65–68.
Ingersoll, R.V., Bulard, T.F., Ford, R.L., Grimn, J.P., Pickle, J.P., Sares, S.W., 1984. The ef fect of grain size on de tri tal modes: a text of the Gazzi-Dickinson Point Count ing method. Jour nal of Sed i men tary Pe trol ogy, 54: 103–116.
Jucha, S., 1958. Con tri bu tions on Jas³o shaly lime stones in the Pol - ish Carpathians. Bul le tin de l’Académie Po lo naise des Sci - ences, Série des Sci ences Géologiques et Géographiques, Varsovie, 6: 681–688.
Jucha, S., 1969. Les schistes de Jas³o, leur im por tance pour la stratigraphie et la sédimentologie de la série ménilitique et des couches de Krosno; Carpathes flyscheuses (in Pol ish with French sum mary). Prace Geologiczne, 52: 1–128.
Jucha, S., Kotlarczyk, J. 1961. La série des couches à menilite et des couches de Krosno dans le flysch des Karpates (in Pol ish with French sum mary). Prace Geologiczne, 4: 1–155.
Koszarski, L., ¯ytko, K., 1961. Jas³o shales in the Menilite-Krosno se ries in the Mid dle Carpathians (in Pol ish with Eng lish sum - mary). Biuletyn Instytutu Geologicznego, 166: 87–232.
Kotlarczyk, J., 1979. Oc cur rence of coal in the Carpathian flysch – some sedimentological ob ser va tion. Annales Societatis Geologorum Poloniae, 49: 135–154.
Kotlarczyk, J., Œliwowa, M., 1963. On knowl edge of the pro duc tive Car bon if er ous for ma tions in the sub stra tum of the east ern part of the Pol ish Carpathians (in Pol ish with Eng lish sum mary).
Przegl¹d Geologiczny, 11: 268–272.
Ksi¹¿kiewicz, M., ed., 1962. Geo log i cal At las of Po land. Instytut Geologiczny, Warszawa.
Ksi¹¿kiewicz, M., 1972. Karpaty. In: Budowa geologiczna Polski, vol. 4. Tektonika, cz. 3 (in Pol ish). Wyd. Geol., Warszawa.
Ladyzenski, G.N., Sawkiewicz, S.S., 1968. O mineralogii iskolayemykh smol iz Skibovoy zony Sovyetskikh Karpat (in Rus sian). Mineralogicheskii Sbornik, 22: 410–413.
Lipiarski, I., Peszat, C., 1984. Charakterystyka petrograficzna wyst¹pieñ wêgla w „piaskowcach otryckich z kamienio³omu Sêkowiec” (oligocen pasma Otrytu) (in Pol ish). Materia³y VII Sympozjum Geologia formacji wêglonoœnych Polski, AGH Kraków, 18–21.
Matl, K., 1991. Braunkohlen und exotische Steinkohle im Bereich der polnischen Karpaten. Archiv für Lagerstattenforschung der Geologischen Bundesanstat, Wien, 13: 87–100.
Olszewska, B., 1984a. Biostratigraphy of the Menilite-Krosno se - ries in the vi cin ity of Przemyœl (Skole Unit, Pol ish Ex ter nal Carpathians) (in Pol ish with Eng lish sum mary). Biuletyn Instytutu Geologicznego, 340: 45–87.
Olszewska, B., 1984b. Some re marks on ac com pa ny ing foraminifer as sem blages in Jas³o lime stones in the Pol ish Outer Carpathians. Kwartalnik Geologiczny, 28: 689–700.
Olszewska, B., 1997. Foraminiferal biostratigraphy of the Pol ish Outer Carpathians: a re cord of ba sin geohistory. Annales Societatis Geologorum Poloniae, 67: 325–337.
Olszewska, B., 1998. The Oligocene of the Pol ish Carpathians.
Abhandlungen der Senckenbergischen Naturforschenden Gesellschaft, 549: 23–28.
Opolski, Z., 1933. Stratygrafia warstw kroœniañskich (in Pol ish).
Sprawozdania Pañstwowego Instytutu Geologicznego, 7:
565–636.
Oszczypko, N., 2004. The struc tural po si tion and tectonosedimentary evo lu tion of the Pol ish Outer Carpathians.
Przegl¹d Geologiczny, 52: 780–791.
Oszczypko, N., Oszczypko-Clowes, M., 2006. Rozwój basenu magurskiego (in Pol ish). In: Rozwój paleotektoniczny basenów Karpat zewnêtrznych i pieniñskiego pasa ska³kowego (eds. N.
Oszczypko, A. Uchman and E. Malata): 133–164. Instytut Nauk Geologicznych UJ, Kraków.
Oszczypko, N., Malata, E., Švábenická, L., Golonka, J., Marko, F., 2004. Ju ras sic-Cre ta ceous con tro ver sies in the West ern Carpathian Flysch: the ‘‘black flysch’’ case study. Cre ta ceous Re search, 25: 89–113.
Oszczypko, N., Olszewska, B., Malata, E., 2012. Cre ta ceous (Aptian/Albian-?Cenomanian) age of “Black Flysch”and ad ja - cent de pos its of the Grajcarek Thrust-Sheets in the Ma³e Pieniny Mts. (Pieniny Klippen Belt, Pol ish Outer Carpathians).
Geo log i cal Quar terly, 56 (3): 411–440.
Pettijohn, F.J., 1975. Sed i men tary Rocks. Harper & Row, New York.
Rögl, F., 1998. Paratethys Oligocene-Mio cene strati graphic cor re la - tion. Abhandlungen der Senckenbergischen Naturforschenden Gesellschaft, 549: 3–7.
Sarjusz-Makowski, A., 1947. Brown coal in cen tral Po land (in Pol - ish with Eng lish summary). Biuletyn Pañstwowego Instytutu Geologicznego, 40: 15–65.
Sikora, W., 1962. New data on the ge ol ogy of the Pieniny Klippen Belt. Bul le tin of the Pol ish Acad emy of Sci ences, Earth Sci - ences, 10: 203–211.
Szafran, S., Wag ner, M., 1999. Charakter petrograficzny uwêglonego materia³u organicznego w mioceñskich osadach wschodniej czêœci zapadliska przedkarpackiego (in Pol ish).
Zeszyty Naukowe Politechniki Œl¹skiej, Górnictwo, 243:
131–138.
Œl¹czka A., 1963. Couches de Krosno inférieures de Roztoki Dolne – Karpates Po lo naises Orientales (in Pol ish with French sum - mary). Annales de la Société Geologique de Pologne, 33:
181–187.
Œl¹czka, A., Wieser, T., 1962. Shales with exotics from the Krosno Beds in Baligród (in Pol ish with Eng lish sum mary). Kwartalnik Geologiczny, 6: 662–667.
Tay lor, G.H., Teichmüller, M., Da vis, A., Diessel, C.F.K., Littke, R., Rob ert, P., 1998. Or ganic Pe trol ogy. Gerbrüder Borntraeger, Berlin.
Tokarski, A., 1975. Ge ol ogy and geo mor phol ogy of the Ustrzyki Górne area (Pol ish East ern Carpathians). Studia Geologica Polonica, 48: 1–90.
Turnau, E., 1970. Plant microfossils and palaeo ge ogra phy of the Car bon if er ous coal de pos its in Pol ish Carpathians. Biuletyn Instytutu Geologicznego, 235: 163–244.
Wag ner, M., 1980. Coal mat ter in the Flysch of the Magura nappe be tween Jordanów and Nowy S¹cz. Annales de la Société Geologique de Pologne, 51: 99–117.
Wag ner, M., 1992. Studium petrologiczne wêgla karpackiego równowiekowego z utworami fliszowymi, jako Ÿród³a generowania gazu ziemnego. Gospodarka Surowcami Mineralnymi, 8: 803–816.
Wag ner, M., 1996. Pet ro logic stud ies of ter res trial or ganic mat ter in Carpathian flysch sed i ments, south ern Po land. In ter na tional Jour nal of Coal Ge ol ogy, 29: 259–272.
Wag ner, M., 2011. Pet ro logic stud ies and diagenetic his tory of coaly mat ter in the Podhale flysch sed i ments, south ern Po land.
Annales Societatis Geologorum Poloniae, 81: 173–183.
Wag ner, M., 2013. The geo log i cal as pects of meta-lig nite and sub-bi tu mi nous coal oc cur rences in Po land within the con text of de pos its and un eco nomic oc cur rences in Eu rope. Gospodarka Surowcami Mineralnymi, 29: 25–46.
Wilkin R.T., Barnes H.L., 1997. For ma tion pro cesses of framboidal py rite. Geochimica at Cosmochimica Acta, 61: 323–339.
Wilkin, R.T., Barnes, H.L., Brantley, S.L., 1996. The size dis tri bu - tion of framboidal py rite in mod ern sed i ments: an in di ca tor of re - dox con di tions. Geochimica at Cosmochimica Acta, 60:
3897–3912.
Zieliñska, M., 2010. Petrographic struc ture of ter res trial or ganic mat ter in Po land’s West ern Flysch Carpathians (in Pol ish with Eng lish sum mary). Kwartalnik AGH – Geologia, 36: 567–584.
Zieliñska, M., 2013. Pet ro logic study of dis persed or ganic mat ter in the West ern Flysch Carpathians (in Pol ish with Eng lish sum - mary). Ph.D. the sis, AGH Uni ver sity of Sci ence and Tech nol ogy.
Ziemianin, K., Wolska, A., 2014. Min er al og i cal and pet ro log i cal char ac ter is tics of ex otic schist cob bles from the Krosno Beds (Silesian Unit, Bieszczady Mts., south-east Po land). Nafta-Gaz, 2014/10: 659–670.
Zuber, F., 1918. Flisz i Nafta (in Pol ish). Prace naukowe Towarzystwa Naukowego we Lwowie, 2: 1–381.
¯ytko, K., 1968. Budowa geologiczna Karpat miêdzy dorzeczem Strwi¹¿a a Wetlin¹ w Bieszczadach (in Pol ish). Archiwum Oddzia³u Karpackiego Pañstwowego Instytutu Geologicznego.
