Geo log i cal Quar terly, 2016, 60 (4): 943–958 DOI: http://dx.doi.org/10.7306/gq.1305
Palynology of Lower Oligocene brown coal and low er most Mid dle Mio cene sand de pos its from the £ukowa-4 bore hole (Carpathian Foredeep, SE Po land)
– im pli ca tions for palaeo geo graphi cal re con struc tions
Przemys³aw GEDL1, *, El¿bieta WOROBIEC2 and Barbara S£ODKOWSKA3
1 Pol ish Acad emy of Sci ence, Re search Cen ter in Kraków, In sti tute of Geo log i cal Sci ence, Senacka 1, 31-002 Kraków, Po land
2 Pol ish Acad emy of Sci ences, W. Szafer In sti tute of Bot any, Lubicz 46, 31-512 Kraków, Po land
3 Pol ish Geo log i cal In sti tute – Na tional Re search In sti tute, Rakowiecka 4, 00-975 Warszawa, Po land
Gedl, P., Worobiec, E., S³odkowska, B., 2016. Palynology of Lower Oligocene brown coal and low er most Mid dle Mio cene sand de pos its from the £ukowa-4 bore hole (Carpathian Foredeep, SE Po land) – im pli ca tions for palaeo geo graphi cal re con - struc tions. Geo log i cal Quar terly, 60 (4): 943–958, doi: 10.7306/gq.1305
Brown coal and over ly ing sand strata from the £ukowa-4 bore hole, lo cated in the north east ern sec tor of the Carpathian Foredeep in Po land, were stud ied for palynology. These strata are un der lain by Up per Eocene sands, and cov ered by Mid dle Mio cene rocks. Coal beds yielded in fre quent sporomorphs and fresh wa ter al gae Botryococcus. The pres ence of the lat ter in - di cates that these de pos its ac cu mu lated in a fresh wa ter en vi ron ment whereas sporomorph as sem blages point to the pres - ence of mixed for ests with a sig nif i cant por tion of thermophilous taxa. Age of the coal beds has been es tab lished based both on the pres ence of spe cies that ap pear for the last time in the Early Oligocene, and on the sim i lar ity with sporomorph spec tra from the Lower Oligocene of the Pol ish Low lands. Over ly ing sands yielded ma rine dinoflagellate cysts, which point to a ma - rine sed i men tary set ting, and fre quent sporomorphs. The lat ter in di cate the pres ence of mixed mesophytic for ests, bush swamps, swamp for ests, and ri par ian for ests in the vi cin ity of lac us trine en vi ron ments. Strati graphic anal y sis of dino - flagellate cyst and sporomorph as sem blages sug gests that the sands ac cu mu lated in early stages of Mio cene trans gres sion in the Carpathian Foredeep in the lat est Early–early Mid dle Mio cene. Our cli ma tic in ter pre ta tion of the sporomorph spec tra sug gests that the cli mate dur ing de po si tion of the strata was rel a tively warm, al though less fre quent thermophilous taxa re - corded in the Mio cene sands sug gest a slightly cooler cli mate than that de ducted from the spec tra yielded by the un der ly ing Lower Oligocene coal beds. Cor re la tion of Lower Oligocene coal beds with neigh bour ing co eval ma rine sands sug gests di - verse mor pho log i cal con di tions in the Carpathian fore land at that time, partly cov ered by a sea, and partly emerged. A sim i - lar, mor pho log i cally di verse base ment in the Carpathian fore land fa voured ac cu mu la tion of Lower Mio cene phytogenic de pos its. A sim i lar strati graphic po si tion of both Lower Oligocene and Lower Mio cene coal beds in the Carpathian Foredeep may re sult in a false cor re la tion of these strata de void of fos sils, which are com monly re garded as Mio cene.
Key words: sporomorphs, dinoflagellate cysts, palynostratigraphy, palaeoenvironment, Oligocene–Mio cene, Carpathian Foredeep.
INTRODUCTION
Brown-coal de pos its are wide spread at the base of the Mio - cene suc ces sion in the Carpathian Foredeep Ba sin (e.g., Kasiñski and Piwocki, 1994). They oc cur in two main ar eas along its north ern mar gin of the Pol ish sec tor (Fig. 1): in Silesia (Kêdzierzyn-KoŸle–Gliwice area) where they have been dis tin - guished as the K³odnica For ma tion (see e.g., Alexandrowicz, 1963, 1970; Alexandrowicz et al., 1982) and in north ern part (be tween Chomentów and Trzydnik) known as the Trzydnik
For ma tion (e.g., Czarnocki, 1932, 1933; Konior, 1948; Bie - lecka, 1957; Kowalewski, 1958; Radwañski, 1969, 1973; Szy - ma nko and Wójcik, 1982; Paw³owski et al., 1985). Most of these phytogenic de pos its were ac cu mu lated in a sys tem of la goonal - -lac us trine set tings that stretched along the north ern mar gin of the Carpathian Foredeep be fore ma rine trans gres sion that started in the Mid dle Mio cene (Kasiñski and Piwocki, 1994; for cor re la tion of over ly ing ma rine strata see e.g., Olszewska, 1999). Con ti nen tal set tings of their ac cu mu la tion is ev i denced by the in fre quent, but oc ca sional mass oc cur rence of ter res trial (gas tro pods He lix and Succinea), fresh wa ter (gas tro pods, e.g., Lymnaea and Planorbis, and bivalvia Congeria), and/or brack - ish to hypersaline (gas tro pods Hydrobia and Potamides, bi - valve Modiola, and foraminifera Am mo nia beccarii) fos sils (Kasiñ ski and Piwocki, 1994). Al though their old est oc cur ren - ces are known mostly from the Paleogene–Neo gene, but some show lon ger strati graphic ranges (e.g., A. beccarii is known since the Late Cre ta ceous; Brooks, 1967); this makes that ac -
* Corresponding author, e-mail: ndgedl@cyf-kr.edu.pl
Received: May 5, 2016; accepted: June 14, 2016; first published online: July 18, 2016.
cu rate ages of the host strata have never been es tab lished – they are most com monly re ferred to the Lower Mio cene, mainly on the ba sis of the age of the over ly ing youn ger ma rine strata, which are Mid dle Mio cene in age (Garecka et al., 1996; Gare - cka and Jugowiec, 1999; Olszewska, 1999).
Some of these sites were stud ied for palynology; sporo - morph as sem blages al lowed their dat ing as Lower Mio - cene–lower Mid dle Mio cene (Karpatian; Worobiec in Kr¹piec et al., 2011). Ac cu rate dat ing of these brown-coal de pos its is es - sen tial not only for palaeogeographic re con struc tions but also for in ter pre ta tion of tec tonic pro cesses in the Mio cene in this part of Po land, which led to sig nif i cant changes due to fold ing and overthrusting of the Carpathian orogen. The oc cur rence of Mio cene brown coal was used as a tool for cor re la tion of Carpathian Foredeep strata that oc cur in var i ous tec tonic po si - tions, like the el e vated Roztocze and the low ered cen tral Carpathian Foredeep area (e.g., Kr¹piec et al., 2011). In the
last two de cades, how ever, some of the brown coals of the Carpathian Foredeep yielded sporomorph as sem blages that might in di cate an older, Paleogene age of these phytogenic de - pos its (S³odkowska in Myœliwiec and Œmist, 2006). These dis - cov er ies ap peared at the same time when the first well-dated re cords of Paleogene ma rine strata un der ly ing the Mio cene suc ces sion in the east ern sec tor of the Carpathian Foredeep have been re ported (e.g., Gedl, 2000; Myœliwiec and Œmist, 2006). There fore, we un der took de tailed palynological stud ies of the avail able cores of brown coals and over ly ing strata from the £ukowa-4 bore hole (Fig. 2) lo cated in the north east ern sec - tor of the Carpathian Foredeep (Fig. 1). In this bore hole, phyto - genic de pos its oc cur at a depth of 804–807 m (Fig. 2); they rest on the Up per Eocene ma rine sandy de pos its, and are cov ered by cream-col oured sands of un cer tain age (Gedl, 2015); fol lo - wed by Mid dle Mio cene (Badenian) marly de pos its (Myœliwiec and Œmist, 2006).
944 Przemys³aw Gedl, El¿bieta Worobiec and Barbara S³odkowska
Fig. 1. Lo ca tion of the £ukowa-4 bore hole and a geo log i cal sketch-map of SE Po land show ing po si tions of main geo log i cal struc tures and lo cal i ties men tioned in the text (based on ¯ytko et al., 1989, from Oszczypko, 1996;
hatched ar eas of the coal de posit oc cur rences af ter Kasiñski and Piwocki, 1994)
GEOLOGICAL SETTING
The Carpathian Foredeep Ba sin was a ba sin sys tem de vel - oped at the front of north ward-mi grat ing Carpathian nappes.
They formed, due to over load of the overthrusting nappes and de flec tion of pre-Mio cene base ment, a ba sin sys tem that stretched arcuately over the dis tance of 1300 km from Aus tria, through the Czech Re pub lic, Po land and Ukraine to Ro ma nia (e.g., Ney et al., 1974; Kotlarczyk, 1985; Oszczypko et al., 2006). Ma rine strata that filled the foredeep ba sin reached a vari able thick ness, even up to 5 km in the Ukrai nian part. Their ac cu mu la tion started dur ing the Badenian (Langhian) cor re - lated with the NN5 Cal car e ous Nannoplankton Zone (NN4 in the wes tern most part of the Pol ish sec tor) and the M5 Plank - tonic Foraminifera Zone (Garecka et al., 1996; Garecka and Jugowiec, 1999; Olszewska, 1999; for zonal cor re la tion see Berggren et al., 1995).
The Badenian ma rine trans gres sion cov ered a geo log i cally di verse base ment, which caused that the basal in ter vals of the Mio cene suc ces sion rest upon rocks of var i ous ages in dif fer ent ar eas of the Carpathian Foredeep – from Pre cam brian to Up per Cre ta ceous (see e.g., Karnkowski and Ozimkowski, 2001: figs.
2, 3; Oszczypko et al., 2006: fig. 2). In the east ern part of the Carpathian Foredeep, iso lated sites with ma rine and con ti nen - tal Paleogene de pos its oc cur at the base of the Mio cene; they rep re sent rem nants of an Eocene and Oligocene cover eroded prior and/or dur ing early stages of the Badenian trans gres sion (e.g., Moryc, 1995; Gedl, 2000, 2012, 2015; Myœliwiec and Œmist, 2006). The pre-Mio cene base ment had been gen er ally ex posed to subaerial con di tions at least since the lat est Cre ta - ceous; later, it un der went long-last ing ero sional pro cesses that led to a highly di verse re lief, with over 1 km deep palaeovalleys (e.g., Karnkowski and Ozimkowski, 2001: figs. 1, 2). As a con - se quence, the ear li est de pos its of the Badenian trans gres sion, as well as pre ced ing con ti nen tal de pos its show high vari abil ity as they were de pos ited in a mor pho log i cally di verse area (see e.g., Bogacz, 1967; Radwañski, 1968; Oszczypko and Tomaœ, 1976, Kasiñski and Piwocki, 1994; Moryc, 1995). The mor pho - log i cally di verse base ment in cluded up lifted ar eas cov ered with veg e ta tion and de pres sions oc cu pied by lakes and/or bogs.
Par tic u larly suit able mor phol ogy con ve nient for phyto genic de - posit ac cu mu la tion ap peared along the north ern mar gin of the Carpathian Foredeep, where a gently in clined val ley sys tem oc - curred (e.g., Kasiñski and Piwocki, 1994). Main out lines of this mor pho log i cal sys tem ex isted pre sum ably al ready dur ing the short-last ing Mid dle–Late Eocene and Early Oligo cene trans - gres sions that cov ered at least the east ern part of the Carpathian Foredeep in Po land (e.g., Buraczyñski and Krzo - wski, 1994; Gedl, 2000, 2012, 2014, 2015). Hence, fre quent fa - cies changes can be ex pected in the Paleogene strata of this area, in clud ing interfingering of ma rine and con ti nen tal fa cies.
MATERIAL AND METHODS
The £ukowa-4 bore hole was drilled in the north east ern part of the Pol ish sec tor of the Carpathian Foredeep, near Tarno - gród (Fig. 1). It pen e trated the whole Mio cene suc ces sion that is 803 m thick in this area (see Myœliwiec and Œmist, 2006). Be - low, the 803–809 m depth core in ter val (Fig. 2) con sists of two dif fer ent lithologies. Me dium- to coarse-grained sands, non-cal - Palynology of Lower Oligocene brown coal and lowermost Middle Miocene sand deposits from the £ukowa-4 borehole... 945
Fig. 2. Li thol ogy and sam ple po si tion in the 803–823 m in ter val in the £ukowa-4 bore hole
car e ous and pale in col our (whit ish to beigish-brown), oc cur at the top of this in ter val (803.0–806.4 m). Six sam ples from these sands were stud ied (depths 803.0–803.2 m, 803.4–803.6 m, 804.1–804.2 m, 804.6–804.7 m, 805.2–805.3 m, 806.0–806.1 m). Be low, brown coal and coaly clay and sand oc cur (806.4–809.0 m); four sam ples from these phytogenic de pos its were stud ied (depths 806.4–806.5 m, 807.1–807.2 m, 807.8–807.9 m, and 808.9–809.0 m). The bound ary be tween coal and pale sand is sharp (Fig. 3). Be low, Up per Eocene glauconitic sands are un der lain by Mid dle Ju ras sic sandy de po - s its (Gedl, 2015; Fig. 2).
These sam ples were pro cessed in the micropalaeonto - logical lab o ra tory of the In sti tute of Geo log i cal Sci ences, Pol ish Acad emy of Sci ences, Kraków. The pro ce dure ap plied in cluded 38% hy dro chlo ric-acid (HCl) treat ment, 40% hy dro flu oric-acid (HF) treat ment, heavy-liq uid (ZnCl2 + HCl; den sity 2.0 g×cm–3) sep a ra tion, ul tra sound for 10–15 s and siev ing at 10 mm on a ny lon mesh. The quan ti ties of rock for anal y sis were vari able, de pend ing on the li thol ogy: 120–200 g for sand sam ples and 10 g for phytogenic sam ples. The same set of sam ples was used by Gedl (2015). Ad di tional slides were made and ana lysed for the pres ent study. Palynological slides were made us ing glyc er ine jelly as a mount ing me dium. These rock sam ples, their palynological res i dues and slides are stored in the col lec - tion of the In sti tute of Geo log i cal Sci ences, Pol ish Acad emy of Sci ences, Kraków.
Three ad di tional sam ples taken from brown coal (depths 806.25 m, 807.50 m and 808.50 m) were pro cessed at the Pol - ish Geo log i cal In sti tute – Na tional Re search In sti tute, Warsza - wa, us ing heavy-liq uid (CdJ2 + KJ; den sity 2.21 g·cm–3) sep a ra - tion. Then, the or ganic con tent was pro cessed ac cord ing to the mod i fied Erdtman’s acetolysis method (Moore et al., 1991).
Palynological slides were made from each sam ple, us ing glyc - er ine jelly as a mount ing me dium.
Tax on omy of dinoflagellate cysts fol lows Fensome et al.
(2008). The sporomorph taxa iden ti fied were clas si fied to an ap - pro pri ate palaeofloristical el e ment, mainly on the ba sis of the At las of Pol len and Spores of the Pol ish Neo gene (Stuchlik et al., 2001, 2002, 2009, 2014). The fol low ing palaeofloristical el e - ments were dis tin guished (Ap pen dix 1*): palaeotropical (P), in - clud ing: trop i cal (P1) and sub trop i cal (P2), as well as arctotertiary (A), in clud ing: warm-tem per ate (A1) and tem per - ate (A2).
Dinoflagellate cysts and other aquatic palynomorphs were pho to graphed (Figs. 4–7) us ing a Carl Zeiss Axiolab mi cro - scope with a Sony DSC-S75 cam era and Carl Zeiss Achroplan x100 oil lens. Mi cro pho to graphs of se lected sporomorphs (Fig.
8) were taken us ing a Nikon Eclipse mi cro scope fit ted with a Canon dig i tal cam era.
RESULTS OF THE PALYNOLOGICAL STUDY
Sam ples from the 803–809 m in ter val were stud ied for palynofacies and dinoflagellate cysts by Gedl (2015). This pa - per pres ents re sults of palynological study of the same set of sam ples stud ied for sporomorphs (EW), re sults of sporomorph stud ies from three ad di tional sam ples from coal beds (BS), and new re sults of dinoflagellate cyst stud ies from ad di tional slides from the sandy in ter val (PG).
DINOFLAGELLATE CYSTS AND OTHER AQUATIC PALYNOMORPHS
Coal beds (806.4–809 m). Phytogenic strata yielded no ma rine dinoflagellate cysts; fre quent forms of un cer tain or i gin, pos si bly fresh wa ter al gae (dinoflagellate cysts?) were found in a sam ple from 807.1–807.2 m depth (Gedl, 2015: fig. 9H–K).
Sandy in ter val (803.0–806.4 m). Dinoflagellate cysts oc cur in all five sam ples from this in ter val; their dis tri bu tion is shown in
946 Przemys³aw Gedl, El¿bieta Worobiec and Barbara S³odkowska
* Supplementary data associated with this article can be found, in the online version, at doi: 10.7306/gq.1305 Fig. 3. Li thol ogy of the up per part of the
coal beds and over ly ing sands in the
£ukowa-4 bore hole (from Gedl, 2015)
Palynology of Lower Oligocene brown coal and lowermost Middle Miocene sand deposits from the £ukowa-4 borehole... 947
Fig. 4. Dinoflagellate cysts from the sands at the 803.0–806.4 m depth in the £ukowa-4 bore hole
A, B – large, over 50 mm in di am e ter, spec i men of Batiacasphaera micropapillata; C, D, I–S – Batiacasphaera micropapillata; E–H – Nematosphaeropsis labyrinthus; T, U – Labyrinthodinium truncatum truncatum; V, W – Labyrin thodinium truncatum mo di cum; X, Y – Operculodinium sp.; Z – Impagidinium? sp.; Z1, Z2 – Reticulatosphaera actinocoronata; A–I, Z1, Z2: 803.0–803.2 m, J, X–Z: 803.4–803.6 m;
K, L, N–R: 804.1–804.2 m; M, S–W: 805.2–805.3 m
Ap pen dix 1 and the spec i mens are pre sented in Fig ures 4, 5 and 7. Dinoflagellate cysts are rare to very rare, be ing highly dis persed by ter res trial el e ments. The lat ter are main el e ments of palyno facies: all sam ples yielded a gen er ally uni form palyno - facies con sist ing of dark brown and black equidimensional phyto clasts and sporomorphs (mainly bisaccate pol len grains;
see be low). Their pro por tion may vary from sam ple to sam ple;
the high est pro por tions of black opaque phytoclasts and bisaccate pol len grains are in sam ples from 803.3–803.4 m and 806.0–806.1 m depths.
Dinoflagellate cyst as sem blages are the mix tures of var i - ously pre served forms. Gen er ally, they in clude very well-pre - served, pale-col oured spec i mens, and darker, much worse - -pre served, com monly in de ter min able forms. Un for tu nately, this di vi sion can not be sim ply cor re lated with var i ous ages, as it could be sus pected ac cord ing to the fol low ing scheme: darker, poorly pre served forms are re worked, whereas the pale-col - oured ones are in situ (see chap ter Age in ter pre ta tion).
Well-pre served forms in clude both spec i mens con sid ered to be in situ (i.e., spe cies with known strati graphic ranges not
948 Przemys³aw Gedl, El¿bieta Worobiec and Barbara S³odkowska
Fig. 5. Dinoflagellate cysts from the sands at the 803.0–806.4 m depth in the £ukowa-4 bore hole
A–D – Spiniferites spp.; E – Hystrichokolpoma rigaudiae; F–H – Spiniferites spp.; I – iso lated operculum of Cleistosphaeridium placacanthum; J – Palaeocystodinium golzowense; K – Spiniferites sp.; L – Cleistosphaeridium placacanthum; M – Cleistosphaeridium
?ancyreum; N, O – “Palaeocystodinium striatogranulosum”; scale bar in A is 25 mm and re fers to all pho to graphs; A, C–I, L, M:
805.2–805.3 m; B, J, N, O: 803.0–803.2 m; K: 806.0–806.1 m
Palynology of Lower Oligocene brown coal and lowermost Middle Miocene sand deposits from the £ukowa-4 borehole... 949
Fig. 6. Acritarchs and prasinophyceans from the sands at the 803.0–806.4 m depth in the £ukowa-4 bore hole A–D – Cymatiosphaera sp. 1; E–G – Nannobarbophora gedlii; H–O – rel a tively small chorate acritarchs, ?Micrhystridium; P, Q –
Cymatiosphaera sp. 2; R, S – rel a tively large chorate acritarch, ?Micrhystridium; T–V – Cymatiosphaera sp. 3; A–D, F, G, P–R:
803.0–803.2 m; E: 806.0–806.1 m; H–O, S–V: 805.2–805.3 m; scale bar in A is 25 mm and re fers to all pho to graphs
older than Early–Mid dle Mio cene), and spec i mens re worked from older strata (i.e., spe cies known to have ap peared for the last time be fore the Mio cene). Rep re sen ta tives of the first group are Eocene spe cies (e.g., Areosphaeridium diktyoplokum, Phthanoperidinium comatum; Fig. 7A, B) that most likely come from un der ly ing Eocene sands (Gedl, 2015; see also Gedl, 2012). Cre ta ceous spe cies are also well-pre served but in fre - quent and slightly darker than the Eocene ones (e.g., Cribro - peridinum sp., Surculosphaeridium? longifurcatum; Fig. 7C).
Spe cies in situ are Labyrinthodinium truncatum truncatum, L.
truncatum mo di cum, and “Palaeocystodinium striatogra nulo - sum” – all ap peared for the first time dur ing the Early Mio cene (e.g., Wil liams et al., 2004).
Their dis tinc tion is based solely on com par i son of their ranges, as the pres er va tion state is the same. This bears a prob lem in as sign ing the cor rect age to well-pre served spe cies with Paleogene–Neo gene age-range such as Batiacasphaera micropapillata, Cleistosphaeridium ?ancyreum, C. placacan - thum, Hystrichokolpoma rigaudiae, Impagidinium sp., Lingulo - dinium machaerophorum, Nematosphaeropsis labyrinthus, Oper culo dinium sp., Palaeocystodinium golzowense, Reticu - lato sphaera actinocoronata, and Spiniferites spp. They are treated ar bi trarily as in situ here. Some of these spe cies found in the pres ent ma te rial have bi modal state of pres er va tion (Li.
machaerophorum, R. actinocoronata, Spiniferites spp.) which sug gests that they may rep re sent both re worked (Paleogene) and in situ forms (Mio cene).
Poorly pre served forms, com monly in com plete and show - ing a higher de gree of ma tu rity, are ev i dently re worked; Wetze - liella sp. and Deflandrea sp. come from Paleogene strata; sev - eral oth ers, in de ter min able, may be also of Me so zoic age.
Dinoflagellate cysts are as so ci ated by well-pre served acri - tarchs and Cymatiosphaera (Prasinophycean al gae; Fig. 6).
Acritarchs are rep re sented by subspherical chorate spe cies, some at trib ut able to Nannobarbophora gedlii found in sam ples from 803.0–803.2 and 806.0–806.1 m depths (Fig. 6F, G). The other chorate forms are ques tion ably at trib uted to Micrhy - stridium, among which a sim ple di vi sion is made be tween
smaller (up to 25 mm di am e ter; Fig. 6H–O) and larger forms (Fig. 6R, S).
Cymatiosphaera is rep re sented by three spe cies that dif fer by size and height of their crests. Cymatiosphaera sp. 1 is a small form with high crests; its di am e ter does not ex ceed 25 mm (Fig. 6A–D). Cymatiosphaera sp. 2 is slightly larger with very short crests that form rel a tively large po lyg o nal fields (Fig. 6P, Q). The larg est is Cymatiosphaera sp. 3, which is over 30 m in di am e ter; low crests form a dense pat tern of smooth po lyg o nal fields (Fig. 6T–V); this spe cies re sem bles Cymatiosphaera sp.
B from the Mio cene of the Ukrai nian Carpathian Foredeep Ba - sin, which dif fer by pos i tive re lief on po lyg o nal fields (Gedl et al., 2016). It should be noted that Cymatiosphaera sp. 1 and Nannobarbophora gedlii oc cur in the Kortynica Clays (the lat ter as Svenkodinium versteeghii; Gedl, 1996).
SPOROMORPHS
Sporomorph as sem blages suit able for de tailed stud ies have been found in five sam ples (803.0–803.2 m, 803.4–803.6 m, 804.1–804.2 m, 804.6–804.7 m, and 805.2–805.3 m depths). Pol len grains and spores are very fre - quent in most of them, but their pres er va tion var ies from ex cel - lently pre served spec i mens to com pletely cor roded ones (es pe - cially bisaccate pol len grains) with highly dam aged struc ture.
Sam ples from the 806.0–806.1 and 807.10 m depths were bar - ren. Sam ples from the 806.4–806.5 m, 807.1–807.2 m, 807.8–807.9 m depths con tain no sporomorphs, how ever, col o - nies of Botryococcus al gae were en coun tered in these sam - ples. Al though the sam ples taken from brown coal (806.25 m, 807.50 m and 808.50 m depths) yielded only sparse pol len grains and spores, but they in cluded sev eral stratigraphically im por tant spe cies.
A to tal of 72 fos sil spe cies (in clud ing 16 spe cies of plant spores, 13 spe cies of gym no sperm pol len, and 43 spe cies of an gio sperm pol len) were iden ti fied (Fig. 8 and Ap pen dix 1). In all sam ples, pol len grains of co ni fers clearly pre vail (Ap pen -
950 Przemys³aw Gedl, El¿bieta Worobiec and Barbara S³odkowska
A B C
Fig. 7. Re worked dinoflagellate cysts from the sands at the 803.0–806.4 m depth in the £ukowa-4 bore hole
A – Areosphaeridium diktyoplokum; B – Phthanoperidinium comatum; C – Cribroperidinium sp.; A, B: 803.4–803.6 m, C: 803.0–803.2 m;
scale bar in A is 25 mm and re fers to all pho to graphs
dix 1). Some bisaccate pol len grains are in cluded into small bisaccates” group, which in cludes cor roded, dif fi cult to de ter - mine spec i mens, prob a bly, at least partly, re cy cled.
Coal beds (806.4–809 m). Sam ples taken from brown coal were pre pared us ing two dif fer ent meth ods, in clud ing heavy-liq -
uid sep a ra tion with two dif fer ent liq uids: ZnCl2 + HCl (den sity 2.0 g·cm–3) and CdJ2 + KJ (den sity 2.21 g·cm–3). Only sam ples pre pared with the later mix ture (depth 808.50–806.25 m) yiel - ded sparse sporomorphs. In these sam ples, Cupressaceae, Sciadopitys and bisaccate pol len grains of Pinaceae are rel a - Palynology of Lower Oligocene brown coal and lowermost Middle Miocene sand deposits from the £ukowa-4 borehole... 951
Fig. 8. Pol len grains from the sands at the 803.0–806.4 m depth in the £ukowa-4 bore hole
A, B – Zonalapollenites sp.; C – Cathayapollis sp.; D, E – Sciadopityspollenites serratus; F – Sequoiapollenites sp.; G – Inaperturopollenites sp.; H – Inaperturopollenites concedipites; I, J – Ericipites callidus; K – Ericipites sp.; L – Polyatriopollenites stellatus; M, N – Ulmipollenites undulosus; O – Intratriporopollenites sp.; scale bar in A is 25 mm and re fers to all pho to graphs; A, C, H, L, O: 805.2–805.3 m; B, F, G, I–K, M, N: 803.0–803.2 m; D, E: 804.6–804.7 m; H: 805.2–805.3 m
tively com mon. An gio sperms are rep re sented by pol len grains of fos sil spe cies Cupuliferoipollenites pusillus, Fususpollenites fusus, Momipites qui etus, Myricipites sp., Platanipollis ipelen - sis, Platycaryapollenites sp., Symplocoipollenites sp., Tricol - poro pollenites fallax, T. pseudocingulum, Ericaceae and Betu - la. Among spores, i.a., Cicatricosisporites dorogensis, Ci. para - do rogensis, and Neogenisporis neogenicus are re corded.
These sam ples con tain col o nies of Botryococcus and some al - gae of un cer tain tax on omy in a sam ple from 807.1–807.2 m depth, in ter preted by Gedl (2015) as pos si bly fresh wa ter dinoflagellate cysts.
Many fos sil spe cies re corded in the brown coal (spores of Cicatricosisporites dorogensis, Ci. paradorogensis and Neo - geni sporis neogenicus as well as pol len grains of Cupuliferoi - pollenites pusillus, Fususpollenites fusus, Momipites qui etus, Myricipites sp., Platanipollis ipelensis, Platycaryapollenites sp., Symplocoipollenites sp., Tricolporopollenites fallax and T.
pseudo cingulum) rep re sent palaeotropical (in clud ing trop i cal and sub trop i cal) and palaeotropical/warm-tem per ate palaeo - floristical el e ments (Ap pen dix 1).
Sandy in ter val (803.0–806.4 m). Most sam ples taken from the de pos its above the brown coal (depth 803.0–805.2 m) are rich in pol len grains and spores, but the pres er va tion of the sporomorphs var ies from ex cel lently pre served spec i mens to com pletely cor roded ones. In all sam ples from the up per most part of the £ukowa-4 bore hole, bisaccate pol len grains clearly pre vail. Among them, Pinus and Cathaya (fos sil spe cies Pinuspollenites labdacus, P. sp., Cathayapollis sp.) as well as Picea are most fre quent. In ad di tion, sin gle spec i mens of Abies pol len were en coun tered. Non-bisaccate pol len grains of co ni - fers are also fre quent in all these sam ples. Among them, pol len of Taxodium/Glyptostrobus (fos sil ge nus Inaperturopollenites), Sciadopitys, Tsuga as well as Se quoia and other mem bers of the Cupressaceae fam ily are most im por tant.
Among an gio sperms, trees and shrubs strongly dom i nate, whereas only a few pol len grains of herbs are pres ent. Pol len grains of Ericaceae, Ulmus, Alnus, Tricolporopollenites pseudo cingulum, Quercus (fos sil spe cies Quercoidites henrici and Quercopollenites sp.), Fagus, Myrica, Nyssa, Carya, Ptero carya, Betula, Castanea/Castanopsis (mainly fos sil spe - cies Cupuliferoipollenites pusillus), Carpinus, Acer, Masti xia - ceae (fos sil spe cies Cornaceaepollis satzveyensis), Euco - mmia, Trigonobalanus (fos sil spe cies Fususpollenites fusus), Malvaceae (fos sil ge nus Intratriporopollenites), and Engelhar - dia (fos sil spe cies Momipites punctatus) are most fre quent. In ad di tion, sin gle spec i mens of Fabaceae (fos sil spe cies Tricol - po ro pollenites liblarensis and T. fallax), Cyrillaceae/Clethra - ceae (fos sil spe cies Cyrillaceaepollenites exactus), Fraxinus, Juglans, Liquid ambar, Ilex, Sapotaceae, Zelkova, and cf.
Edmundi pollis sp. were re corded.
Cryp to gams are rep re sented mainly by spores of ferns (mainly fos sil spe cies Leiotriletes sp., Laevigatosporites sp., Neogenisporis neogenicus, Neogenisporis sp., Toroisporis sp., Baculatisporites sp.), Sphag num and mem bers of the fam ily Lycopodiaceae (fos sil spe cies Retitriletes sp., Camaro zono - sporites sp., and Selagosporis sp.).
In these sam ples, dinoflagellate cysts and acritarchs are pres ent as so ci ated by rare Prasinophyceae (Cymatiosphaera), whereas other al gae are al most ab sent (only one col ony of Botryococcus en coun tered). Fun gal spores are also very rare.
In ad di tion, in all sam ples from the up per most part of the
£ukowa-4 bore hole, some cor roded bisaccate pol len grains in - cluded into “small bisaccates” group, at least partly re cy cled, are pres ent. More over, in these sam ples other re cy cled pol len grains and spores are en coun tered. These spores are usu ally dark-col oured and have thick walls.
In all sam ples from the up per most part of the £ukowa-4 sec - tion, palaeotropical (in clud ing trop i cal and sub trop i cal) and palaeo tropical/warm-tem per ate palaeofloristical el e ments are pres ent (Ap pen dix 1). The palaeotropical and palaeotro - pical/warm -tem per ate el e ments are rep re sented by spores of, i.a., Camarozonosporites sp., Leiotriletes sp., Neogenisporis neogenicus, N. sp., and Toroisporis sp. as well as pol len grains of Inaperturopollenites concedipites, I. dubius, Cornaceaepollis satzveyensis, Cupuliferoipollenites oviformis, Cu. pusillus, Cyrilla ceae pollenites exactus, Fususpollenites fusus, Ilexpolle - nites margaritatus, Intratriporopollenites sp., Momipites pun - ctatus, Myricipites sp., Nyssapollenites sp., Oleoidearum polle - nites sp., Quercoidites henrici, Platycaryapollenites sp., Sapo - ta ceoidaepollenites sp., Tricolporopollenites pseudocin gulum, and T. staresedloensis.
RECONSTRUCTION OF PLANT COMMUNITIES AND PALAEOENVIRONMENT
Coal beds (806.4–809 m). The strata from this in ter val ac - cu mu lated in a ter res trial en vi ron ment (Fig. 9). The pres ence of col o nies of Botryococcus points to a fresh wa ter en vi ron ment, prob a bly shal low lakes or bogs with pe ri odic blooms of Botryo - coccus (Gedl, 2015). Rel a tively nu mer ous palaeotropical el e - ments sug gest warm cli mate dur ing sed i men ta tion of these lig - nite de pos its.
Al though the coal sam ples from the 808.25–806.50 m depth in ter val yielded only sparse pol len grains and spores, re sults of palynological anal y sis of these sam ples in di cate the pres ence of mixed for ests with a sig nif i cant por tion of thermo philous taxa.
In the vi cin ity there were also, i.a., mem bers of the fam ily Fagaceae (prob a bly from the gen era Trigonobalanus, Casta - nea and oth ers), Engelhardia, Platanus, Platycarya, Symplo - cos, Betula, mem bers of the fam i lies Myricaceae, Fabaceae, Ericaceae and oth ers. Co ni fers were im por tant el e ments of veg e ta tion. Mem bers of the fam i lies Pinaceae, Cupressaceae, and Sciadopitys were also pres ent. Cryp to gams were rep re - sented by thermophilous ferns from the fam i lies Schizaeaceae, Lygodiaceae and prob a bly Gleicheniaceae.
Sandy in ter val (803.0–806.4 m). The pres ence of ma rine dinoflagellate cysts in sands above the coal beds in di cates a ma rine sed i men tary set ting (Fig. 9). High pro por tion of sporo - morphs, in clud ing rel a tively fre quent spores (that are not as buoy ant as the pol len grains) may in di cate a nearshore ma rine set ting along a coast cov ered by veg e ta tion. The dinoflagellate cyst as sem blages them selves have a lim ited value for pre cise en vi ron men tal re con struc tion as their true tax o nomic com po si - tion is un cer tain (they con sist in part of re worked spe cies; see chap ter Dinoflagellate cysts and other aquatic palynomorphs).
How ever, if the pre sented in ter pre ta tion is ac cept able, then a dom i nance of Batiacasphaera micropapillata is out stand ing. Al - though palaeoenvironmental pref er ences of this spe cies are un known, but sim i lar Batiacasphaera-dom i nated as sem blages were de scribed from an ap prox i mately co eval nearshore fa cies of the Mid dle Mio cene strata of the Carpathian Foredeep. Com - mon oc cur rence of B. micropapillata (as so ci ated with fre quent B. sphaerica) was re ported from the nearshore Korytnica Clays (Gedl, 1996). Gedl (1995) com pared this nearshore as sem - blage with co eval as sem blages from off shore fa cies that are de void of this spe cies (they in clude fre quent Impagidinium, Unipontidinium aquaeductum and “Palaeocystodinium striato - granulosum”). Fre quent Batiacasphaera was re ported from basal strata of the Mio cene suc ces sion in the wes tern most part of the Carpathian Foredeep in Po land (Gedl, 1997).
952 Przemys³aw Gedl, El¿bieta Worobiec and Barbara S³odkowska
The re sults of pol len anal y sis of sam ples taken above the coal (803.0–805.2 m depth) in di cate the pres ence of mixed mesophytic for ests, bush swamps, swamp for ests, and ri par ian for ests (Fig. 9). The swamp for ests grew in the neigh bour ing area with a higher ground wa ter level and were com posed of Taxodium, Nyssa, and prob a bly also Glyptostrobus and Alnus.
Wet places in the vi cin ity were prob a bly over grown by ri par ian for ests com posed of Ulmus, Alnus, Carya, Pterocarya, Acer, Fraxinus, Liquid ambar, and oth ers.
The drier places were over grown by mesophytic for ests rich in thermophilous taxa. These mesophytic for ests were com posed, i.a., of trees and shrubs from the fam ily Fagaceae (prob a bly from the gen era Quercus, Castanea, Trigono - balanus, Fa gus, and oth ers), Betula, Carpinus, Engelhardia, Eucommia, Acer, and Zelkova, and mem bers of the fam i lies Mastixiaceae, Malvaceae, Fabaceae, and Sapotaceae, as well as co ni fers, ferns, and many oth ers. Some bisaccate pol - len grains from the Pinaceae fam ily (e.g., Pinus) pos si bly also come from plant com mu ni ties grow ing on el e vated ter rains, at a dis tance from the lo cal ity. Nev er the less, Cathaya, Pinus, Sciadopitys, Tsuga and Se quoia were most prob a bly im por - tant trees in the mixed for ests, or they formed their own plant com mu ni ties in the vi cin ity.
Mem bers of the fam i lies Ericaceae, Cyrillaceae, Clethra - ceae and Myricaceae were prob a bly com po nents of bush swamps.
Com po si tion of the palynological as sem blage from the up - per most part of the £ukowa-4 sec tion in di cates that the cli mate dur ing de po si tion of the sed i ment was rel a tively warm, al though less fre quent thermophilous taxa re corded in this in ter val sug - gest a lit tle cooler con di tions than de duced from the un der ly ing spec tra (Fig. 9).
AGE INTERPRETATION
Coal beds (806.4–809 m). Com po si tion of the spore-pol len as sem blage from the coal, in clud ing such fos sil spe cies as Cupuliferoipollenites pusillus, Fususpollenites fusus, Momipites qui etus, Platanipollis ipelensis, Symplocoipollenites sp., Tri - colpo ro pollenites fallax, T. pseudocingulum and Neogenisporis neogenicus, gen er ally points to Oligocene or Lower Mio cene age of the ma te rial. In ad di tion, two fos sil spe cies Cicatrico - sisporites dorogensis and Ci. paradorogensis were re corded among the spores. These two spe cies have their up per strati - graphic limit in the Early Oligocene (Grabowska, 1996b) and their pres ence, to gether with the whole com po si tion of the as - sem blage, in di cates that the age of the lig nite is most prob a bly Lower Oligocene (Fig. 9).
Sandy in ter val (803.0–806.4 m). Among dinoflagellate cyst spe cies con sid ered to be in situ (see chap ter Dinoflagellate cysts and other aquatic palynomorphs) two spe cies have rel a - tively short strati graphic ranges that al low dat ing of the sands above the coal beds. These are Labyrinthodinium truncatum truncatum, L. truncatum mo di cum, and “Palaeocystodinium striatogranulosum”. “P. striatogranulosum”, an in for mally de - scribed spe cies by Zevenboom and Santarelli (in Zevenboom, 1995) from the Mio cene of It aly, is be lieved to have a strati - graphi cal range lim ited to the Late Aquitanian–Early Tortonian (NN2–8 zones; Zevenboom, 1995; see also Wil liams et al., 2004). In the ma te rial stud ied, only a sin gle spec i men of this spe cies is noted (sam ple from 803.0–803.2 m depth); its scar - city may be as so ci ated with pos si bly off shore pref er ences of this spe cies as sug gested by Gedl (1995). Labyrinthodinium truncatum, as a spe cies, is given var i ous ages of its first ap -
pear ances de pend ing on lat i tudes (Wil liams et al., 2004): Late Aquitanian in high lat i tudes of the North ern Hemi sphere, Burdigalian/Langhian in ter val in mid-lat i tudes of the North ern Hemi sphere, and mid-Langhian in equa to rial ar eas (the two lat - ter ap pli ca ble to the po si tion of the ma te rial stud ied). The Langhian first ap pear ance of this spe cies was sug gested by, i.a., Piasecki (1980), Zevenboom (1995), Munsterman and Brinkhuis (2004); see also De Verteuil and Norris (1996) for dis - cus sion. The lat ter au thors sug gested a slightly lower the low est oc cur rence of the sub spe cies L. truncatum mo di cum in the NN4 Zone (i.e., pos si bly in the Up per Burdigalian; for cor re la tion see Berggren et al., 1995). The pres ence of both spe cies, but par tic - u larly Labyrinthodinium truncatum, shows that the sands that over lie coal beds in the £ukowa-4 bore hole are likely not older than Mid dle Mio cene (Fig. 9).
Com po si tion of the spore-pol len spec tra from the sands is gen er ally sim i lar to those from the Oligocene to Mid dle Mio cene palynofloras from Po land (see Dis cus sion). The as sem blage stud ied is rich in pol len grains of the Ulmaceae (fos sil ge nus Ulmipollenites) and Ericaceae fam i lies. In ad di tion, there are abun dant pol len of such co ni fers as Pinus, Sciadopitys, and Tsuga. The whole as sem blage is rel a tively poor in spe cies and dom i nated by arctoteriary el e ments. These fea tures of the spore-pol len spec tra are most sim i lar to the Early to Mid dle Mio - cene as sem blages from its cooler cli ma tic phases (see Piwocki and Ziembiñska-Tworzyd³o, 1997; Ziembiñska-Tworzyd³o, 1998), par tic u larly to palynofloras from cli ma tic phase IV – Ulmipollenites spore-pol len zone, Late Burdigalian in age. On the other hand, rel a tively sig nif i cant pres ence of palaeotropical and palaeotropical/warm-tem per ate el e ments is re corded (in - clud ing fos sil spe cies Camarozonosporites sp., Leiotriletes sp., Neogenisporis neogenicus, Neogenisporis sp., Toroisporis sp., Cornaceae pollis satzveyensis, Cupuliferoipollenites oviformis, Cu. pusillus, Cyrillaceaepollenites exactus, Fususpollenites fusus, Momipi tes punctatus, Quercoidites henrici, Platycarya - polle ni tes sp., Sapotaceoidaepollenites sp., Tricolporo polle - nites pseudo cin gulum, and T. staresedloensis). In this case, we can sus pect that the more re sis tant pol len grains (Ericaceae, Ulmus, Pinus) could be over-rep re sented and there fore the spore-pol len as sem blage from the sandy in ter val has only a lim - ited strati graphic sig nif i cance.
DISCUSSION
The dat ing of the coal beds from the £ukowa-4 bore hole sug gests that they ac cu mu lated dur ing the Early Oligocene.
Find ing of Lower Oligocene coal beds in the Carpathian Fore - deep adds im por tant data to palaeogeographic re con struc tions of the Carpathian fore land dur ing the Paleogene. It shows that there were some emerged ar eas in the Rupelian, al though most of the area was cov ered by the sea. The coal beds from the
£ukowa-4 bore hole can be cor re lated with ma rine sands de - scribed from neigh bour ing bore holes near Tarnogród (Gedl, 2000); they yielded dinoflagellate cysts such as Areoligera?
semicirculata, Chiropteridium ga lea, Ch. lobo spino sum, Penta - dinium laticinctum, Reticulatosphaera actinocoro nata, Rhom - bo dinium draco, Wetzeliella gochtii, and W. symme trica incisa.
Age of their as sem blages, as com pared with strati graphic ranges given by Wil liams et al. (2004), is Late Rupe lian–ear li est Chattian. A sim i lar age can be sug gested by com par i son with Oligocene dinoflagellate cyst as sem blages from epicontinental strata of cen tral and north ern Po land, de scribed by Grabowska (1974, 1987, 1996a), Grabowska and Wa¿yñ ska (1997), and S³odkowska (2004a, b). These as sem blages in cluded fre quent Palynology of Lower Oligocene brown coal and lowermost Middle Miocene sand deposits from the £ukowa-4 borehole... 953
Chiropteridium lobospinosum, as so ci ated with, i.a., Wetzeliella symmetrica and Rhombodinium draco.
This cor re la tion is fur ther sup ported by com par i son of sporomorphs from the up per part of the Lower Oligocene sec - tion in the Pol ish Low lands, which is rep re sented by the ma rine Rupel For ma tion (an equiv a lent of the Septarian Clays and Boom Clays from NW Eu rope; see Piwocki, 2004) and the Up - per Mosina For ma tion, as well as the con ti nen tal/brack ish Czempin For ma tion (for merly the Toruñ Clays; see Piwocki, 2004). The spore-pol len spec tra from these strata in clude, i.a., Cicatricosisporites dorogensis, Camarozonosporites heske ma - nsis, Boehlensipollis hohli, Cupanieidites eucalyptoides, Fusu - s polle nites fusus, Cupuliferoipollenites pusillus, Cu. oviformis, Edmun dipollis edmundi, Tricolporopollenites liblarensis, T.
fallax, T. staresedloensis, Quercoidites microhenrici, Momipites qui etus, Platycaryapollenites, Platanipollis ipelensis (e.g., Grabowska, 1965, 1983, 1987; Grabowska and Piwocki, 1975;
S³odkowska, 2009). Ac cord ingly, the com po si tion of the sporo - morph as sem blage from the brown coal in the £ukowa-4 bore - hole (806.4–809 m depth), par tic u larly the pres ence of Cicatricosiporites dorogensis, Ci. paradorogensis, Platanipollis ipelensis, Fususpollenites fusus and small tricolporate pol len grains, points to sim i lar ity of the above-men tioned as sem blage to the Lower Oligocene palynofloras from the Pol ish Low lands.
Our dis cov ery of Lower Oligocene phytogenic de pos its in the Carpathian Foredeep, and their cor re la tion with co eval ma - rine strata in the neigh bour hood, sug gest that the base ment of the Carpathian fore land dur ing the Early Oligocene was mor - pho log i cally di verse. The Rupelian ma rine trans gres sion in un - dated down-dropped ar eas, whereas on el e vated ar eas, phytogenic ter res trial ac cu mu la tion took place in con ti nen tal, fresh wa ter con di tions, most likely in a lac us trine en vi ron ment, as in di cated by the pres ence of Botryococcus. How ever, data scar city (the £ukowa-4 bore hole ma te rial is the only so-far dis -
954 Przemys³aw Gedl, El¿bieta Worobiec and Barbara S³odkowska
Fig. 9. Syn thetic com pi la tion of the Paleogene and basal Mio cene in ter val from the 803–823 m depth in the £ukowa-4 bore hole
cov ered trace of Early Oligocene ter res trial ac cu mu la tion in the Carpathian Foredeep) does not jus tify a fur ther-reach ing palaeogeographic re con struc tion. Moryc (1995) de scribed con - ti nen tal de pos its be low the Mio cene suc ces sion in the east ern part of the Carpathian Foredeep in the Rzeszów re gion, but the pre ci sion of the ear lier dat ing of those de pos its does not al low cor re la tion with the £ukowa-4 phytogenic se ries.
A sim i lar mor phol ogy was pos tu lated for early stages of the sub se quent Mio cene ma rine trans gres sion that cov ered the mor pho log i cally highly di verse base ment (e.g., Czarnocki, 1958; Radwañski, 1968; Oszczypko and Tomaœ, 1976, Kasiñ - ski and Piwocki, 1994; Moryc, 1995; Karnkowski and Ozimko - wski, 2001). At that time, sim i lar con ti nen tal to brack ish sed i - men tary set tings oc cu pied the north ern mar gin of the foredeep, where phytogenic ac cu mu la tion took place (e.g., Kasiñski and Piwocki, 1994). These coal beds are com monly un der lain by sandy de pos its of un cer tain, pre sum ably Paleo gene age (see ex am ple of the coal beds from Trzydnik; Kasiñ ski and Piwocki, 1994: figs. 3, 5a). The Lower Oligocene coal beds from the
£ukowa-4 bore hole oc cupy a sim i lar strati graphic po si tion (they are un der lain by the Up per Eocene in this bore hole). These sim i lar i ties may in di cate that some of the phytogenic de pos its of the Carpathian Foredeep, which are com monly de void of fos - sils (or con tain long-rang ing fresh wa ter/brack ish forms), are in fact Oligocene in age.
An other prob lem in palaeogeographic re con struc tions of Early Oligocene palaeoenvironments of the Carpathian fore - land re sults from the lack of cored ma te rial be low the coal beds in the £ukowa-4 bore hole (806.4–809 m depth), which does not al low trac ing the re la tion be tween the coal beds and un der ly ing strata. The coal beds in the £ukowa-4 bore hole are sep a rated from the Up per Eocene sands by an al most 10 m thick gap (Gedl, 2015). Lack of core ma te rial from this in ter val makes that it is not pos si ble to find out whether the coal beds rest upon the Oligocene ma rine sand (like that known from the nearby bore - holes at Tarnogród; Gedl, 2000; Myœliwiec and Œmist, 2006;
Fig. 1) and rep re sent a re cord of a shallowing ma rine ba sin that grad u ally be came brack ish and fresh wa ter, and the lac us trine phytogenic de po si tion is a re sult of a fi nal phase in a re gres sive cy cle, or the coal beds over lie older Eocene strata and they rep - re sent a fa cies lat er ally interfingering with ma rine sands.
Our age in ter pre ta tion of the coal beds in the £ukowa-4 bore hole is also im por tant for tec tonic stud ies of the Carpathian Foredeep, as these strata have been used as a cor re la tive level with some Mio cene phytogenic de pos its, e.g., at Siedliska and D¹brówka from the Roztocze area (e.g., Kr¹piec et al., 2011;
Fig. 1). How ever, the palynoflora in the lig nite from the
£ukowa-4 sec tion shows some sim i lar i ties to the Mio cene as - sem blages from Siedliska and D¹brówka. Brown coals from the two lat ter lo cal i ties were dated paly no logi cal ly to Early or Mid dle Mio cene (most prob a bly Karpatian; Worobiec in Kr¹piec et al., 2011). The spore-pol len as sem blage from the £ukowa coal, like both palynofloras from Roztocze, is rich in palaeotropical taxa.
Nev er the less, dif fer ent taxa dom i nate in par tic u lar as sem bla - ges. In both palynofloras from Siedliska and D¹brówka, nu mer - ous pol len grains of Edmundipollis sp., Cupuliferoi pollenites oviformis, Ilexpollenites margaritatus, I. propinquus, I. iliacus, Quercoidites henrici, Cyrillaceaepollenites exactus, Tricolporo - pollenites liblarensis, T. quisqualis, Cornaceaepollis satzveyen - sis, Platycaryapollenites sp., and Arecipites sp. were re corded.
In con trast, pol len of those spe cies is ab sent in the palynoflora from the £ukowa coal, but such spe cies as Platanipollis ipele n - sis, Cicatricosisporites dorogensis and Ci. paradoro gensis are re corded. These dif fer ences also sug gest that the £ukowa coal is most prob a bly older than the brown coal from Siedliska and D¹brówka.
Other sites with phytogenic de pos its in SE Po land are also youn ger than the coal beds from the £ukowa-4 bore hole. Lig - nite-bear ing de pos its in the Trzydnik area (north ern mar gin of the Carpathian Foredeep; Fig. 1) ac cu mu lated dur ing the lat est Karpatian and Early Badenian (Moravian) on the base ment com posed of Up per Cre ta ceous and Oligocene ma rine de pos - its (Kasiñski and Piwocki, 1994: fig. 5a). More north wards, in the low land area, an ap prox i mately 10 m thick sec tion of brown coal at the vil lage of Radawiec (about 20 km west of Lublin; Fig. 1) was dated as the Mid dle Mio cene (S³odkowska in Henkel and Danel, 2015).
Our in ter pre ta tion of the age of the sands that over lie coal beds in the £ukowa-4 bore hole, based on dinoflagellate cysts and sporomorphs, shows that they were ac cu mu lated most likely dur ing the lat est Early and ear li est Mid dle Mio cene (Late Karpatian–Early Badenian, i.e., Late Burdigalian–Early Lan - ghian). The sands have yielded no Unipontidinium aquaedu - ctum, the spe cies char ac ter is tic of Badenian strata un der ly ing the Badenian evaporites in the Carpathian Foredeep in Po land (e.g., Gedl, 1996, 1997, 1999, 2005; Peryt and Gedl, 2010).
This spe cies is known to have its first ap pear ance in the Mid dle or Late Langhian (Wil liams et al., 2004). The pres ence of Labyrinthodinium truncatum truncatum and L. truncatum mo di - cum sug gests Langhian age (see De Verteuil and Norris, 1996), al though lat est Burdigalian age can not be ex cluded as L.
truncatum shows diachronic first ap pear ances de pend ing on the lat i tude (Wil liams et al., 2004). There fore, the lack of U.
aquaeductum (if not caused by palaeoenvironmental fac tors) and the pres ence of L. truncatum in £ukowa-4 ma te rial may in - di cate that the sands ac cu mu lated dur ing early stages of the Langhian (Badenian) or slightly ear lier, dur ing the lat est Burdigalian (Karpatian). The lat ter pos si bil ity seems more re li - able when sporomorph dat ing is com pared, but dinoflagellate cyst data point rather at the lower Mid dle Mio cene age of the sands. A sim i lar as sem blage with fre quent Batiacasphaera micropapillata was de scribed from the Mid dle Mio cene strata of the Pol ish Low lands in Legnica (Gedl and Worobiec, 2005).
Com par i son of the spore-pol len spec tra from the sand that over lies the coal with those ex am ined pre vi ously in Paleogene and Neo gene de pos its of Po land (e.g., spore-pol len zones in Piwocki and Ziembiñska-Tworzyd³o, 1997) shows that the as - sem blage from the up per most part of the £ukowa-4 sec tion is gen er ally sim i lar to the Oligocene and Early to Mid dle Mio cene palynofloras. Un for tu nately, spore-pol len as sem blages from the Up per Oligocene–Lower Mio cene de pos its have no strongly dis tinc tive fea tures (Grabowska, 1996b). The spore-pol len as - sem blages are sig nif i cantly poorer in taxa than the older palynofloras, which is most prob a bly caused by a cli mate change. Those as sem blages are usu ally dom i nated by pol len grains of co ni fers from the fos sil gen era Pinuspollenites, Inaperturopollenites, Sequoiapollenites and, in some cases, Zonalapollenites (= Tsugaepollenites). Among an gio sperms, Cupuliferoipollenites pusillus (= Castaneoideaepollis pusillus), Tricolporopollenites liblarensis, Quercoidites microhenrici, Myricipites spp. and Cyrillaceaepollenites megaexactus (=
Tricolporopollenites megaexactus) are pres ent in the Late Oligocene–Early Mio cene as sem blages. Those fos sil taxa have rel a tively long strati graphic ranges and thus show a lim ited strati graphic sig nif i cance.
Com po si tion of the spore-pol len spec tra from the sands is sim i lar to that of the Early Mio cene as sem blages from its cooler cli ma tic phases (Piwocki and Ziembiñska-Tworzyd³o, 1997;
Ziembiñska-Tworzyd³o, 1998), par tic u larly to palynofloras from cli ma tic phase IV – Ulmipollenites spore-pol len zone. The as - sem blages of the Ulmipollenites spore-pol len zone are known from few lo cal i ties in the Fore-Sudetic Monocline and in the Pol - Palynology of Lower Oligocene brown coal and lowermost Middle Miocene sand deposits from the £ukowa-4 borehole... 955
ish Low lands (Ziembiñska-Tworzyd³o, 1998). Pol len grains of the Ulmaceae fam ily (fos sil ge nus Ulmipollenites) and the nu mer ous ac com pa ny ing Ericaceae are the in dic a tive pol len taxa for this phase. The whole as sem blage of the phase is poor in spe cies and dom i nated by arctotertiary el e ments, whereas palaeo - tropical el e ments are scarce and rep re sented mainly by sub trop i - cal taxa. In con trast, the spore-pol len spec tra from the up per - most part of the £ukowa-4 sec tion con tain rel a tively nu mer ous palaeotropical and palaeotropical/warm-tem per ate el e ments.
Tak ing into con sid er ation the whole com po si tion of the spec tra from the sands, an early Mid dle Mio cene age of the sands is most prob a ble.
CONCLUSIONS
A 10 m thick cored in ter val from the £ukowa-4 bore hole, for - merly im prop erly dated as Paleogene (re spec tively Up per Eocene?, Oligocene?, Lower Mio cene?; Gedl, 2015), yielded sporomorphs and dinoflagellate cysts that al low its more ac cu - rate dat ing.
We can as sume that the age of the £ukowa brown coal, based on sporomorph spec tra, is most prob a bly Lower Oligo - cene, whereas the over ly ing sands are Mio cene in age. Al - though the ab sence of sporomorphs that would un am big u ously
de fine the age of the sands and the pres ence of some re worked spec i mens do not al low for cer tain con clu sions about their age, but the pres ence of dinoflagellate cysts al low their dat ing as the ear li est Mid dle Mio cene. Thus, the sands rep re sent the ini tial stage of the Badenian (Mid dle Mio cene) trans gres sion, which pass up ward into marly strata of the Baranów Beds.
Our dis cov ery of the Lower Oligocene coal beds in the
£ukowa-4 bore hole may in di cate that some other phytogenic de pos its of the Carpathian Foredeep might be of sim i lar age.
This re fers to the phytogenic beds that oc cur in a sim i lar strati - graphic po si tion and con tain no age-di ag nos tic fos sil ev i dence, and their Mio cene age is based on the age of the over ly ing fossiliferous Miocene deposits.
Ac knowl edge ments. The Man age ment of Polskie Górnictwo Naftowe i Gazownictwo SA (PGNiG) is kindly ac - knowl edged for grant ing per mis sion to use their sam ples and to pub lish re search re sults. The study was partly sup ported by the W. Szafer In sti tute of Bot any, Pol ish Acad emy of Sci ences, Kraków, through stat u tory funds for E. Worobiec. We also thank G. Worobiec (W. Szafer In sti tute of Bot any, Pol ish Acad emy of Sci ences, Kraków) for his help in tak ing pho to graphs of pol len grains. M. Ziembiñska-Tworzyd³o and an anon y mous re viewer are kindly ac knowl edged for read ing the manu script and crit i cal com ments.
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