Fos sils from the Silesian-Subsilesian se ries of the Pol ish West ern Carpathians:
the im pli ca tions for changes in sea level and the ma rine en vi ron ment dur ing the Albian–Turonian
Andrzej SZYDŁO1, *, Małgorzata JUGOWIEC-NAZARKIEWICZ1 and Barbara OLSZEWSKA1
1 Pol ish Geo log i cal In sti tute – Na tional Re search In sti tute, Carpathian Branch, Skrzatów 1, 31-560 Kraków, Po land
Szydło, A., Jugowiec-Nazarkiewicz, M., Olszewska, B., 2015. Fos sils from the Silesian-Subsilesian se ries of the Pol ish West ern Carpathians: the im pli ca tions for changes in sea level and the ma rine en vi ron ment dur ing the Albian–Turonian.
Geo log i cal Quar terly, 59 (1): 215–228, doi: 10.7306/gq.1206
Foraminifera and cal car e ous nannoplankton, as well as other fos sils from the Albian-Turonian de pos its of the West ern Pol - ish Carpathians, are dis cussed in re la tion to changes in depositional en vi ron ments, which were con trolled by geotectonic ac - tiv ity, sea level changes, and anoxic and bi otic events. The dis tri bu tion and di ver sity of fos sils in the de pos its stud ied have been re lated to global sea level fluc tu a tions or lo cal sea level rise and fall. Dur ing the Albian to the Early Cenomanian, and in the Turonian, the lo cal sea level falls led to an in creased sup ply of coarse-grained ma te rial rich in si li ceous and some times cal car e ous fos sils and rock ma te rial. This cy clic pro cess has con trib uted to changes in the ma rine biota. In the Albian, monospecific foraminiferal as sem blages with a surficial infauna which col o nized bot tom wa ters af ter pe ri ods of or ganic in flux and ox y gen de fi ciency (OAE1b), evolved into more vari able as so ci a tions in clud ing deep infauna which in di cate more aer o bic con di tions. Un der these con di tions plank tonic and cal car e ous ben thic fos sils (tintinnids, cal car e ous nannoplankton, and foraminifera) were also pre served. Their pres ence was as so ci ated with the sup ply of terrigenous ma te rial from shal low-wa ter en vi ron ments and land, which were eroded dur ing re gres sions con trolled by lo cal tec tonic ac tiv ity. Dur ing the Albian- Turonian tran si tion, in tense sub si dence and vol ca nic ac tiv ity as so ci ated with a rel a tive sea level rise led to in creased pro - duc tiv ity of phytoplankton in the area stud ied. The sea-sur face pro duc tiv ity and en hanced upwelling re sulted in ex panded short-term ox y gen min ima at the end of the Albian (OAE1d) and the Cenomanian (OAE2). In the lat ter in ter val ben thic forms be came al most ex tinct while si li ceous and cal car e ous plank ton sur vived. In the Turonian, changes in sea level and sed i men - tary re gime led to re-col o ni za tion of the ba sin bot tom.
Key words: Cre ta ceous, fos sils, en vi ron ments, sea level, Pol ish Carpathians.
INTRODUCTION
Col li sion be tween the Af ri can and Eu ro pean-Asi atic plates led to im por tant changes in global palaeo ge ogra phy dur ing the mid-Cre ta ceous (e.g., Erbacher and Thurow, 1997; Hay et al., 1999; Golonka et al., 2000; Stampfli et al., 2001; Stampfli and Borel, 2002; Cavazza and Wezel, 2003). At that time, the Tethys Ocean was clos ing and vol ca nic ac tiv ity was un usu ally high. It was re spon si ble for changes in ocean cir cu la tion, sea level, the car bon cy cle, and sea-sur face pro duc tiv ity or pres er - va tion con di tions (Bralower and Thierstein, 1984; Haq et al., 1988; Vogt, 1989; Calvert and Pederson, 1992; Erbacher et al., 1999, 2001; Golonka and Krobicki, 2001; Herrle et al., 2003).
All these ex ter nal fac tors were re spon si ble for the green house con di tions in the mid-Cre ta ceous. At that time mas sive de po si - tion of or ganic mat ter in ma rine en vi ron ments re sulted in the for ma tion of or ganic-rich de pos its (black shales) (Schlanger
and Jenkyns, 1976; Ar thur et al., 1990). The wide spread dis tri - bu tion of black shales has been re garded as re flect ing Oce anic Anoxic Events (OAEs) (Schlanger and Jenkyns, 1976). Its im - pact on bi otic evo lu tion in the ocean was de pend ent on how rel - a tive sea level co in cided with the nu tri ent sup ply. The flood ing of neigh bour ing lands and the in put of nu tri ents dur ing a rel a tive rise of sea level led to in creased pro duc tiv ity and ex pan sion of the ox y gen min ima. Un der these dysa erobic con di tions, deep- dwell ing forms be came ex tinct. Shal lower dwell ing radio lar ians and plank tonic foraminifers sur vived (Leckie, 1987; Erbacher et al., 1999; Robaszyński et al., 2010). The de ter mi na tion of the ox y gen min ima has been cor re lated with the up lift of lands and rel a tive sea level falls, cor re spond ing with a de creased nu tri ent sup ply, which led to the de vel op ment of new deep hab i tats and to the ra di a tion of deep- dwell ing forms (Erbacher and Thurow, 1997; Erbacher et al., 1999).
The above-men tioned model al lows for the cor re la tion of micropalaeontological data and dif fer ent types of or ganic-rich shale, which re flect the OAEs and sea level fluc tu a tions in the ma rine en vi ron ment. It was used to ex plain the ex pan sion of the ox y gen min i mum zone (OMZ), which caused the ex tinc tion and ra di a tion of foraminifers and radio lar ians in the mid-Cre ta ceous and the Cenomanian-Turonian tran si tion in the North At lan tic and the west ern Tethys (Erbacher and Thurow, 1997; Erbacher
* Corresponding author, e-mail: andrzej.szydlo@pgi.gov.pl Received: Jan u ary 10, 2014, ac cepted: July 23, 2014; first pub lished on line: De cem ber 18, 2014
et al., 1999). An at tempt to ap ply this model to re con struc tions of the en vi ron men tal and sea level fluc tu a tions dur ing the Albian–Turonian in the West ern Outer Carpathian Ba sin has been pro posed. The north ern part of this area in cluded mar - ginal seas, which were es pe cially sen si tive to geotectonic in sta - bil ity and changes in sea level dur ing the mid-Cre ta ceous (Birkenmajer and Gasiński, 1992; Ślączka et al., 1999). In the Subsilesian and Silesian sub-bas ins the dy namic and rapid de - po si tion of siliciclastic sed i ments al ter nated with hemipelagic and pe lagic sed i men ta tion of or ganic-rich shales, which partly cor re spond to anoxic fa cies.
The for ma tion of or ganic-rich siliciclastic de pos its, which con tain nu mer ous and vari able min er al ised skel e tal parts or com po nents, and also crushed frag ments of skel e tons be long - ing to microfossils (foraminifers, radio lar ians, sponges, dino - cysts), macrofossils (bi valves, bel em nites, ammo nites) and nannofossils (cal car e ous nanno plankton), has been ana lysed in re la tion to chan ges in the ma rine en vi ron ment, sup plies of clastic ma te rial, and or ganic mat ter in the ba sin.
GEOLOGICAL AND BIOSTRATIGRAPHICAL SETTINGS
Rock ma te rial was sam pled from the Albian- Turonian de - pos its, in clud ing coarse-grained sand stone suc ces sions in ter - ca lated with shales or sep a rate for ma tions of dark green radio - larian and var ie gated shales, which oc cur in the Silesian- Subsilesian zone of the West ern Outer Carpathians in Po land.
The de pos its de scribed are ac ces si ble in pro files lo cated in the Beskid Śląski: Cisownica-3, Ustroń, Jaworze, Jasie nica; the Beskid Mały: Lipnik, Kozy, Bolęcin, Rzyki, Kaczyna, Buldo - nówka; Lanckorona Foot hills: Lusina, Woźniki, Klecza, Bugaj, Brody, Barwałd Górny, Lanckorona; the Beskid Średni: Bysina, Barnasiówka, Jasienica near Myśle nice, and also the Beskid Wyspowy: Rajbrot. With the ex cep tion of the Woźniki, Barwałd Górny, Lusina, Jasienica near Myślenice, and Rajbrot sec tions that con tain the Sub silesian Se ries, in the ex po sures listed only de pos its of the Silesian Unit oc cur (Fig. 1).
In the area stud ied, lo cated be tween the Olza and the Dunajec rivers, the de pos its sam pled be long to the Albian- Turonian Lgota and Gaize beds, the Turonian-low er most Turonian green radiolarian shales, and the Turonian Godula Beds and var ie gated marly shales (Ślączka et al., 1993; Bąk et al., 2001; Fig. 2). The so-called Lgota Beds in clude three lithostratigraphical units. There are coarse-grained sand stones of Early Albian age con tain ing car bon ate and mag matic rocks, spicule-rich sand stones in ter ca lated with dark, non-cal car e ous shales of the Mid dle-Late Albian age, and spongiolites of Late Albian-Turonian age (Koszarski and Nowak, 1960; Bieda et al., 1963; Geroch et al., 1967). The lower and up per most parts of the Lgota Beds oc cur only in the west ern part of the study area.
Sand stone se ries in ter ca lated with shales, that are typ i cal of the mid dle and partly up per part of this litho stratigraphical unit, are ex posed in the re main ing ar eas. The Lgota Beds are re placed lo cally by the Gaize Beds, con sist ing of sponge spicules in the north ern and spo rad i cally in the east ern up lifted parts of the Silesian Ba sin, which formed as the Subsilesian sub-ba sin in Cenomanian-Turonian time (Bieda et al., 1963; Geroch et al., Fig. 1. Lo ca tion of out crops stud ied in the con text of the tec tonic units
of the Pol ish Outer Carpathians (mod i fied from Żytko et al., 1989)
1 – Cisownica-3, 2 – Ustroń, 3 – Jasienica, 4 – Jaworze, 5 – Lipnik, 6 – Kozy, 7 – Bolęcin, 8 – Rzyki, 9 – Kaczyna, 10 – Woźniki, 11 – Klecza, 12 – Barwałd Górny, 13 – Bugaj, 14 – Brody, 15 – Lanckorona, 16 – Bysina, 17 – Barnasiówka, 18 – Lusina, 19 – Myślenice, 20 – Rajbrot
1967; Alexandrowicz, 1973). In the Cenomanian, ferro manga - nese and green radiolarian shales were typ i cal of open seas in the Silesian Ba sin while var ie gated biosiliceous marly shales and si lici fied marls and bioturbated lime stone oc curred in the Subsilesian zone. This suc ces sion, which is tra di tion ally known as the radiolarian beds, was partly as signed to the Barnasiówka Radiolarian Shale For ma tion by Bąk et al. (2001). The biosiliceous de pos its, in clud ing tuffites and bento nites, lo cally per sisted to the ear li est Turonian (Bąk, 2000), at which time the de po si tion of the Jasienica marls ceased (Liszkowa, 1972). In the Turonian, coarse clastic turbidites (Godula Beds) were de - pos ited again in the west ern part of the Outer Carpathian Ba sin, which was di vided into di verse zones of de po si tion (Silesian, Lanckorona and Wieliczka zones; Ksią żkiewicz, 1962). In the ini tial stage of this de po si tion, thick- bed ded sand stones dom i - nated (Silesian zone). The sand stone suc ces sion was in ter ca - lated with var ie gated cal car e ous shales, which be came the dom i nant fa cies in the cen tral part of the ba sin (Silesian zone) and at its north ern and east ern mar gins (Lanckorona and Wieliczka zones; Koszarski et al., 1959; Książkiewicz, 1962;
Słomka, 1995).
The Albian-Turonian se ries in clude biosiliceous and si li - ceous coarse-grained turbidites (Lgota Beds, Gaize Beds and Godula Beds) and also green and var ie gated shales and marls, which con tain nu mer ous sponge spicules, radio lar ians, fora - minifers, dinocysts, ben thic and nektonic macrofauna (bi valves, bel em nites and ammonites), and car bon ate and crys tal line blocks (Książkiewicz, 1962). Among them, fora minifers, radio - lar ians, and dinocysts are usu ally used for bio stratigraphy of the de pos its stud ied (Koszarski et al., 1959; Koszarski and Nowak, 1960; Geroch, 1966; Geroch et al., 1967; Geroch and Nowak, 1984; Olszewska, 1997; Bąk, 2000; Bąk et al., 2000, 2005;
Gedl, 2001, 2003).
MATERIAL AND METHODS
The pa per is partly based on the study of rock ma te rial taken mainly from si li ceous, marly, or limy shales, and some times bio- and si li ceous sand stones. The col lected shaly sam ples were dis - in te grated by boil ing and freez ing. The 63 mm frac tion was used for micropalaeontological anal y sis. The study of the se lected
microfossils (foraminifers, radio lar ians, and spo nge spicules) was per formed un der a ste reo scopic op ti cal mi cro scope (Zeiss Ste reo Dis cov ery.V12). In ad di tion, the smear - slides for cal car e - ous nannoplankton in ves ti ga tions and the thin-sec tions for micropalaeontological anal y sis (fora mini fers, tin tinnids, cal car e - ous dinocysts, and al gae) were an a lysed us ing po lar iz ing op ti cal mi cro scopes. Pho to graphic doc u men ta tion was per formed us ing op ti cal mi cro scopes made by Nikon and Zeiss.
The col lected mi cro- and nannofossils were de scribed with a spe cial fo cus on the re la tion ship be tween test mor phol ogy and liv ing or feed ing strat egy, and also eco log i cal pref er ences and fos sil isa tion po ten tial. These re sults are com pared with sea level and ox y gen a tion changes in the ma rine en vi ron ments.
RESULTS
The Albian-Turonian de pos its con tain di verse mi cro- and macrofossils. Foraminifers are the most wide spread group in the de pos its. This micro fauna in cludes pri mar ily autochthonous forms ag glu ti nated by sil ica, and also ones with cal car e ous ce - ment and plank tonic and cal car e ous ben thic forms (Huss, 1957; Geroch, 1966; Geroch and Nowak, 1984; Olszewska, 1997; Bąk et al., 2005; Szydło, 2008). Ag glu ti nated forms are nu mer ous, while cal car e ous forms oc cur in low num bers. Pe ri - od i cally si li ceous skel e tal el e ments of sponges and radio lar ians co-oc cur with them or re place them. These si li ceous micro - fossils are mainly com po nents of spongiolites, cherty mud - stones, and green radiolarian shales (Geroch, 1966; Geroch et al., 1967; Geroch and Nowak, 1984; Olsze wska, 1997; Górka and Geroch, 1998; Bąk, 2000). More over, the sil ica orig i nat ing from the dis so lu tion of these el e ments ce mented mainly sand - stones and con glom er ates, and some times marly shales be - long ing to the Lgota and the Godula beds. Sim i larly to the si li - ceous microfossils, dinocysts oc cur fre quently. These or - ganic-walled microfossils oc cur in the Albian- Turonian sand - stone se ries and also in the Cenoma nian- Turonian suc ces - sions (Gedl, 2001, 2003). Im por tant com po nents of fos sil as - sem blages are cal car e ous nano- and microflora and also macro fauna, which oc cur pe ri od i cally. Cal car e ous zoo plank ton (tintinnids) and phyto plankton (dinocysts) were de scribed for the first time in the de pos its stud ied while macrofauna (bi valves, Fig. 2. Li thol ogy and strati graphi cal po si tion of the stud ied se ries of the Silesian and Subsilesian units
ammonites and bel em nites) had been re ported ear lier (Kosza - rski et al., 1959; Kosza rski and Nowak, 1960).
The old est foraminiferal as sem blage that is dom i nated by nu mer ous spec i mens of Recurvoides pseudononioninoides Neagu (= Haplophragmoides aff. nonioninoides sensu Geroch, 1966; Neagu and Platon, 1994) is widely dis trib uted in the lower and mid dle part of the Lgota Beds of the Silesian and the Subsilesian units (comp. with Geroch, 1966; Szydło, 2008;
Figs. 3 and 4). The mass oc cur rence of this taxon is known from the un der ly ing Verovice Beds and cor re sponds with the ag glu ti - nated foraminiferal zone of Hpl. nonioninoides, dated to the Early Albian age (Geroch and Nowak, 1984; Olszewska, 1997;
Fig. 2). Ac cord ing to Szydło (2008), the rare taxa be long ing to gen era Jaculella, Hyperammina, Ammodiscus, Glomospira, Sa ccammina, Caudammina, Haplophragmoides, Thalma nna - mmina, Trochammina, Gaudryina, and Pseudobolivina are lo - cally ac com pa nied by the in dex spe cies in the lower part of the Lgota Beds (Cisownica-3, Jaworze, Lipnik, Kozy; Fig. 3).
In these suc ces sions few and poorly pre served radio lar ians be long ing mainly to the gen era Nasellaria, Dictyomitra, Sticho - capsa, Stichocampe, and some times Spumellaria, Cenellipsis, and Cenosphaera are also pres ent (Geroch, 1966; Górka and Geroch, 1989). In these de pos its macrofauna also oc curs. This is rep re sented by forms be long ing to Inoceramus, sin gle ammo nites re fer able to Acanthoplites bigoureti (Early Albian), and also nu mer ous bel em nite rostrae, which are cor re lated with the mass oc cur rence zone of Neohibolites minimus (Mid dle Albian; Figs. 3 and 4). In the west ern part of the Pol ish Outer Carpathians, this macrofauna is known from the Stra conka and Lipnik lo cal i ties in Beskid Mały (Koszarski and Nowak, 1960;
Szymakowska, 1980).
This macrofauna sug gests that the lower part of the Lgota Beds was mainly de pos ited in the Early Albian and partly also in the Mid dle Albian. At the time, tintinnids (Colomiella recta, C.
semiloricata; Fig. 5A, B) and cal car e ous dinocysts (Colomi - sphaera heliosphaera; Fig. 5C, see Ap pen dix 1*) lo cally oc cur in marls (Jasienica near Myślenice, Subsilesian Unit; Olsze - wska, 1997; Fig. 4). These de pos its were re garded as the Jasienica marls that lo cally per sisted into the lat est Turonian (Liszkowa, 1972).
In places, the as sem blage with R. pseudononioninoides sur - vived un til the end of the suc ces sion in low fre quency (Jaworze, Rzyki, Bysina, Barnasiówka lo cal i ties; Figs. 3 and 4). In the mid - dle and up per parts of the Lgota Beds, this as sem blage is usu ally re placed by the Late Albian as so ci a tion com posed of the spe cies P. alternans and R. imperfectus and G. filiformis (see Ap pen dix 1) in the Lipnik and Kaczyna lo cal i ties (Fig. 3). The as sem blage de scribed also con tains nu mer ous spec i mens of the gen era Plectorecurvoides and Thalma nnammina (Lipnik, Bolęcin; Fig.
3). This micro fauna cor re sponds to the P. alter nans Zone, which is cor re lated with the Mid dle Albian– Ceno manian by Geroch and Nowak (1984), or the Late Albian by Olszewska (1997) (Fig. 2).
In the lat ter cases, the up per part of the zone was marked by the first oc cur rence (FO) of Bulbo baculites problematicus to wards the end of the Early Cre ta ceous (Figs. 3 and 4). In Beskid Mały and in the Lanc korona Foot hills the Lgota Beds con tain arenaceous micro fauna, which are rep re sented by the spe cies Haplo phragmo ides falcato suturalis (Lipnik, Lanckorona – Geroch, 1966; bore hole Łodygowice IG-1 – Geroch and Nowak, 1980) and Areno bulimina chapmani (Kozy, Fig. 3; Brody, Fig. 4).
These Albian forms may still be pres ent in the Cenomanian. Sin - gle spec i mens of cal car e ous fora minifera of the gen era Lenticulina and Pseudonodosaria lo cally co-oc cur with them (Jaworze- Jasie nica area and Kozy; Fig. 3).
In the up per part of the Lgota Beds, si li ceous micro fauna is re placed by cal car e ous foraminifers, in clud ing plank tonic and ben thic forms. The first sim ple in flated forms be long to Hedber - gella delrioensis, H. infracretacea and Heterohelix moremani (Lipnik, Bolęcin, Barnasiówka; Fig. 3) and oth ers are rep re sented by the ge nus Rotalipora (Klecza Dolna, Fig. 4, see Ap pen dix 1).
The ben thic forms in clude Osangularia (O. brotzeni, O. schloen - bachi), Lenticulina, Gyroidinoides, Disco rbis, Cibi cides (Ciso - wnica-3, Lipnik, Bysina, Figs. 3 and 4; cf. with Geroch, 1966).
The cal car e ous fora minifer tests are of ten small and poorly pre - served, show ing traces of dis so lu tion and cor ro sion.
Nu mer ous spicules of sponges and very rare radio lar ians (Spumellaria) oc cur next to foraminifera in the de pos its dis - cussed. Radio lar ians and cal car e ous foraminifers are pre ser - ved usu ally as moulds com posed of py rite (Geroch, 1966; Bąk, 2000).
Ad di tion ally, or ganic-walled dinocysts oc cur in the Lgota Beds. Ac cord ing to Gedl (2003) these forms, oc cur ring above thick-bed ded sand stones, cor re spond to the Palaeohystricho - phora infusorioides Zone of Late Albian age and they are cor re - lated with the Albian-Turonian tran si tion (Epelidophaeridia spinosa Zone) in the up per part of the Lgota Beds (Gedl, 2003).
Gen er ally, palynofacies oc cur ring in the lower part of the Lgota Beds are dom i nated by forms be long ing to Pterodinium and by di ver si fied endocysts be long ing to the gen era Ovoidinium, Odonti chitina, Muderongia, Apteodinium, Canningia, Cyrculo - dinium, Pseudoceratinium, and also peridinioids (Lipnik; Gedl, 2001, 2003). Peridinioids also dom i nate in the up per part of the Lgota Beds. Along with the dom i nant Palaeohystrichophora infusorioides there co-oc cur nu mer ous black or ganic ob jects (phytoclasts) (Lipnik, Rzyki, Barnasiówka; Gedl, 2003). At the top of this suc ces sion blooms of Pseudoceratinium, Subtili - sphaera, and Ovoidinium are noted (Lipnik, Kozy, Rzyki).
In spicule-rich de pos its, which are as signed to the Gaize Beds, the num ber and di ver sity of the foraminifers dis tinctly de - crease. The micro fauna is rep re sented by cal car e ous ben thic foraminifera of the Albian–Turonian (Berthelina intermedia, B.
berthelini, Gyroidinoides infracretaceus, Valvulineria loetterlei, Patellina subcretacea). Part of them is poorly pre served. These forms be long to the gen era Lagena and Cibicides (Klecza- Babica and Woźniki lo cal i ties; Fig. 4) or Guttulina and Planularia (Barwałd; Fig. 4). Plank tonic fora minifers be long ing to Rotalipora co-ex ist with them (cf. Liszkowa, 1956; Huss, 1957). In these biosiliceous rocks, cal car e ous nannoplankton have been re - ported. In the vi cin ity of Barwałd Górny (Fig. 4), re worked Ju ras - sic spe cies oc cur (Watzna ueria barnesae, Poly podorhabdus escaigii, Ellipso gelosphaera bri tan nica, Zeugrha bdotus erec tus, Cretarhabdus conicus, Stephanolithion atme tos, C. crenulatus, Lotharingius hauffii, Crepido lithus granu latus, and spec i mens of Manivitella pemmatiodea; Fig. 6, see Ap pen dix 1) known from the Hauterivian; in ad di tion, cal car e ous ben thic foramini fers be - long ing to the gen era Guttulina, Planularia, and Lenti culina are de scribed. More over, cal car e ous nannoplankton in clud ing long-lived forms (Vagala pilla matalosa, Watznaueria barnesae, Glaukolithus diplogra mmus), and those from the Barremian (Gl.
com pac tus) and the Albian–Turonian (Pre disco sphaera columnata) are re ported from Woźniki (Figs. 4 and 6, see Ap pen - dix 1). The as sem blages de scribed cor re spond to in ter vals CC8 and the CC9. In the same sam ple, ag glu ti nated foraminifers be - long ing to B. problema ticus, the FO of which is lo cated in the high est Albian, were found.
In si lici fied var ie gated shales and marls, as op posed to spongiolites, there oc cur not only radio lar ians and sponge spicules but also plank tonic forms. The dom i nant com po nent of
* Supplementary data associated with this article can be found, in the online version, at doi: 10.7306/gq.1206
ees( lai re tam li ssof fo yt ilib airav dna noi tu bir tsid ehT .3 .giF1 xi dne ppAeht fo seli forp eht morf )naiseliSde iduts tinU su o era clac ,arefinimarof( lai re tam nwo rieht fo si sab eht no yduts siht fo sroh tua eht yb deli pmoc ataDnotknalponnan ,stsyconid ,sdinnitnit ) ( sna ira loidar no stlu ser dehsi lbup sa llew saakróGdna hcoreG0002 ,kąB ;9891 ,dna )stsyconid( ldeG)3002 ,1002 ,
plank tonic as so ci a tions is made of spher i cal skel e tons of radio - lar ians be long ing to the gen era Holocryptocanium and Hemi - cryptocapsa (Bąk, 2000), as well as smaller con i cal forms of Dictyomitra, which ap pear rarely in the Lgota Beds of the Silesian Unit (cf. Geroch, 1966; Górka and Geroch, 1989).
These forms, be long ing to the Nassellaria and the Spumellaria (Praeconocaryomma, Patellula), oc curred in the Late Cenoma - nian–Early Turonian (Bąk, 2000). In Albian-Cenomanian time, dinocysts and plank tonic foraminifers co-ex isted with them. The first are cal car e ous forms be long ing to the spe cies Ortho - pithonella sphaerica and O. ovalis (Fig. 5D, E; Rajbrot, Sub - silesian Unit; Olszewska, 1997), and or ganic-walled taxa (Silesian Unit; Bąk et al., 2000). Foraminiferal plank ton, which
are rep re sented by forms typ i cal of the Cenomanian (Schac - koina, Rotalipora) and the Cenomanian–Early Turonian (Prae - glo botruncana stephani), were de scribed in green shales of the Subsilesian Unit oc cur ring be tween and un der radio larites in Węglówka (Huss, 1957) and Tuchów, Targanice, and Czaniec Górny (Koszarski et al., 1959) re spec tively. In the green shales, which in clude radiolarites, plank tonic forms be long ing to the gen era Hedbergella, Guembelitria, Hetereholix (Fig. 5F–H) were also noted at Rajbrot (cf. Olszewska, 1997).
In the Cenomanian var ie gated shales of the Silesian Unit, in which si li ceous foraminifers are of ten lack ing (Kaczyna; Fig. 3) plank tonic foraminifers be long ing to the gen era Hedbergella and Heterohelix oc cur in low num bers (Barnasiówka; Fig. 4). In Fig. 4. The dis tri bu tion and vari abil ity of fos sil ma te rial from the pro files stud ied of the Subsilesian Unit
Data com piled by the au thors of this study, in clud ing their own re sults and the re sults on radio lar ians and dinocysts pub lished by Bąk (2000) and Gedl (2001, 2003) re spec tively; for other ex pla na tions see Fig ure 3
Fig. 5. Cal car e ous plank ton in clud ing tintinnids, dinocyst and foraminifers
Tintinnids: A – Colomiella recta Bonet, B – C. semiloricata Trejo (A, B – Jasienica n. Myílenice;
Subsilesian Unit); cal car e ous dinocysts: C – Colomisphaera heliosphaera (Vogler), Jasienica n.
Myílenice (Subsilesian Unit); D – Orthopithonella sphaerica (Kaufman); E – O. ovalis (Kaufman) (D, E – Rajbrot; Subsilesian Unit); foraminifers: F – Hedbergella delrioensis Carsey, G – Guembelitria cenomana Keller; H – Heterohelix moremani (Cushman) (F–H – Rajbrot; Subsilesian Unit)
Fig. 6. Cal car e ous nannoplankton
A – Watznaueria barnesae (Barwałd Górny, Gaize Beds, Subsilesian Unit); Ba, Bb – Cyclagelosphaera margerelii (Buldonówka, Godula Beds, Silesian Unit); C – Glaukolithus com - pac tus (Woźniki, Gaize Beds, Subsilesian Unit); D – Ellipsagelosphaera lucasii; E – E.
fossacincta; F – E. bri tan nica; G – Lotharingius hauffii (D–G – Barwałd Górny, Gaize Beds, Subsilesian Unit); Ha, Hb – Prediscosphaera columnata (Woźniki, Gaize Beds, Subsilesian Unit); I – Cretarhabdus crenulatus (Barwałd Górny, Gaize Beds, Subsilesian Unit); J – Cr.
conicus; Ka, Kb – Ephrolithus floralis (J, K – Buldonówka, Godula Beds, Silesian Unit); La, Lb – Vagalapilla sp. (Woźniki, Gaize Beds, Subsilesian Unit); M – Polypodorhabdus escaigii (Barwałd Górny, Gaize Beds, Subsilesian Unit); N – Ethmorhabdus gallicus (Buldonówka, Godula Beds, Silesian Unit); O – Stephanolithion atmetos; P – Crepidolithus granulatus; Ra, Rb – Manivitella pemmatoidea; S – Zeugrhabdotus erec tus (O–S – Barwałd Górny, Gaize Beds, Subsilesian Unit); T – Vagalapilla matalosa (Woźniki, Gaize Beds, Subsilesian Unit) (see Ap - pen dix 1)
(Lanckorona; Fig. 4). Its oc cur rence de ter mines the age of the var ie gated shales as be ing of the ear li est Cenomanian.
In the Turonian, these fa cies were re placed lo cally by thick- bed ded and coarse-grained sand stones, which are typ i cal of the bot tom of the Godula Beds (Słomka, 1995). In this part of the suc ces sion, macrofauna, in clud ing poorly pre served and crushed shells of ammonites and bi valves of the ge nus Ino - ceramus, oc curs lo cally (Koszarski et al., 1959). In other ar eas, var ie gated shales, which oc cur as in ter ca la tions in the glauco - nitic sand stones, con tain rare foraminifers. Sin gle spec i mens of the plank tonic Marginotruncana coronata, the FO of which cor - re sponds to the Late Turonian, ap pear in the Outer Carpathian re gion (Buldonówka; Fig. 3). In the same sam ple, mixed and re - worked cal car e ous nannoplankton be long ing to the spe cies W.
barnesae, E. gallicus, Cyclagelosphaera margerelii, Cretarha - bdus conicus and E. floralis are pres ent (Fig. 6, see Ap pen dix 1). The last form cor re sponds to the Aptian-Santonian in ter val (cf. Caron, 1985). In places, the Turonian Godula sand stones are in ter ca lated with var ie gated shales con tain ing ag glu ti nated foramini fers: N. excelsa, C. ovulum, G. lenis and U. jankoi (Fig.
4, see Ap pen dix 1; cf. Geroch et al., 1967).
CHANGES IN THE DEPOSITIONAL ENVIRONMENTS
In the Silesian-Subsilesian zone of the Outer Carpathian Ba - sin, biosiliciclastic sed i men ta tion pre vailed dur ing the Albian–Turonian. This sed i men tary pro cess was clearly re lated to geotectonic and vol ca nic ac tiv i ties, which re sulted in rel a tive sea level fluc tu a tions and anoxic or bi otic events (Książkiewicz, 1961, 1975; Gucwa and Wieser, 1980; Olsze wska, 1984;
Gucwa, 1990; Bąk et al., 2001, 2005; Olszewska and Malata, 2006; Bąk, 2007; Szydło, 2008; Olszewska and Szydło, 2012).
The avail abil ity of ox y gen and or ganic mat ter con tent in depo - sitional en vi ron ments was also con trolled by these set tings. All these fac tors had strong in flu ence on the evo lu tion and dis tri bu - tion of biotopes and on fos sili sa tion in the de pos its. The fos sils, es pe cially cal car e ous forms, are gen er ally poorly pre served in the de pos its stud ied, and are strongly af fected by diagenetic pro - cesses. Cal car e ous fos sils in clude ben thic and plank tonic fora - minifers, as well as nanno plankton, cal car e ous dinocysts, and the shells of bi valves and ammonites. Cal car e ous fos sils sim i lar to bel em nites, si li ceous skel e tal el e ments of radio lar ians and sponges and also or ganic dinocysts were re worked and mixed many times be fore they fi nally ac cu mu lated in the de pos its. Cal - car e ous or si li ceous skel e tons of ben thic forms orig i nated in shal low wa ter en vi ron ments, which were de stroyed dur ing the up lift of ar eas and the sea level fall ing, es pe cially in the Early Albian and the Early Turonian, and lo cally in the Late Albian. The oc cur rence of the or ganic-walled dinocysts, which are char ac ter - is tic of low sa lin ity (Ovoidinium, Odontichitina, Muderongia) and ter res trial (peridi nioids) en vi ron ments, co in cided with these events dur ing the Albian. These or ganic-walled cysts had thin and del i cate shells de void of com plex ap pend ages (Gedl, 2003).
Prob a bly tin tinnids be long ing to Colomiella as in dex fos sils for
Godula beds ac cu mu lated. These de pos its in clude the bro ken and crushed skel e tons of ben thic (bi valves) and nektonic (bel - em nites and ammonites) macrofauna, and also crys tal line (mag matic, meta mor phic) or car bon ate blocks char ac ter ized by a low de gree of weath er ing (Wieser, 1948; Koszarski and Nowak, 1960; Szymakowska, 1980). In ad di tion, the al most monospecific as sem blages of macrofauna con tained bel em - nites, which show ev i dence of wave ac tion (Lipnik; Koszarski, and Nowak, 1960).
The for ma tion of these de pos its was re lated to sud den brief trans port of sed i ments downslope over a short dis tance (Lee et al., 2007; Szydło, 2011). Cal car e ous bioclastic ma te rial was lo - cally sup plied. In di vid ual plank tonic forms, ac com pa nied by rare ben thic forms, were trans ported in long-dis tance sus pen - sion cur rents dur ing the Albian-Turonian tran si tion. In the up per part of the Lgota Beds con tain ing spongiolites (Albian- Turonian), ag glu ti nated micro fauna were oc ca sion ally re placed by cal car e ous foraminiferal as so ci a tions, which con sist of op - por tu nis tic plank tonic (Hedbergella, Heterohelix) or ben thic forms rep re sented by the gen era Osangularia, Lenticu lina, Gyroidinoides, Discorbis, Cibicides, and Dentalina (Ge roch, 1966; Bąk et al., 2005; Szydło, 2008). These cal car e ous forms in hab ited the near-shore en vi ron ments, and part of them ex - isted un der an aer o bic con di tions (Berhnard, 1986; Koutsoukos et al., 1990); they are usu ally pre served as moulds com posed of py rite (Geroch, 1966; Bąk, 2000). Sim i lar cal car e ous ben thic foraminifers and mostly re worked cal car e ous nannoplankton, and also plank tonic foraminifera and tintinnids, ap peared pe ri - od i cally dur ing the de po si tion of the Gaize Beds in the Albian- Turonian tran si tion and of the Godula Beds in the Early Turonian (Figs. 3, 4 and 7). Mas sive cor roded tests of deep- dwell ing plank tonic forms (Rotalipora) sen si tive to en vi ron men - tal changes (Gaize Beds; Liszkowa, 1956) or better pre served, epifaunal ben thic forms be long mainly to ac tive de posit feed ers (Berthelina, Gyroidinoides, Valvulineria, Patellina, Cibicides) that are ob served in the stud ied sam ples of these biosiliceous de pos its (Figs. 3 and 4). Ben thic foraminifera and cal car e ous nannoplankton were noted in hemipelagic de pos its form ing sand stone in ter ca la tions, while plank tonic fora minifera and tintinnids ap peared in hemipelagic and pe lagic de pos its, which formed as in de pend ent litho stratigraphic units. Their re la tion - ship was re lated to short- or long-last ing pe ri ods of low tec tonic ac tiv ity and mi nor eustatic changes, re spec tively.
Dur ing the sup ply of coarse-grained turbidities into the ba - sin, deep-wa ter cir cu la tion was re ac ti vated, the upwelling in - creased, and the nu tri ent sup plies were more fre quent and in - tense. These fac tors had an im pact on the spread on di verse ag glu ti nated as sem blages. In the Albian, as sem blages in - cluded mainly shal low and surficial epifauna (Plectorecurvo - ides, Recurvoides, Thalmannammina) ac com pa nied by a few deep infaunal forms such as Gaudryina, Bulbobaculites, and Arenobulimina (Figs. 3, 4 and 7). In the up per part of the Lgota Beds, bac te rial and de tri tus feed ers oc curred lo cally in high num bers (Haplophragmoides falcatosuturalis; Geroch, 1966;
Geroch and Nowak, 1984; Szydło, 2008). Nu mer ous and di - verse ag glu ti nated foraminifera, be long ing to shal low or deep infauna, were ob served in light grey and green shales of the
Lgota Beds as well as in the Cenomanian-Turonian var ie gated shales, which oc cur as in ter ca la tions in the lower part of the Godula Beds, or con sti tute a sep a rate lithological unit. Spec i - mens of shal low infauna (Recurvoides) are nu mer ous, while mo bile (Haplophragmoides) and deep infauna (Uvigerina - mmina, Falsogaudryinella, Gaudryina) rarely oc cur. The deep infauna (Gerochammina and Uvigerinammina), in clud ing ac tive de posit and bac te rial feed ers, dom i nated in var ie gated shales of the Turonian (Figs. 3, 4 and 7). The ac com pa ny ing epifaunal sus pen sion feed ers (Nothia) and forms at tached to ma rine plants (Ammodiscus) are rare. The sur face wa ters were col o - nized by deep-dwell ing plank tonic forms (Marginotruncana) at that time (Fig. 3). Dur ing the ho mo ge neous sed i men ta tion, an im pov er ished foraminiferal micro fauna ex isted un der the con di - tions of or ganic in flux and ox y gen de fi ciency, which dom i nated dur ing the rel a tive sea level rise. In the Early Albian, im pov er - ished ag glu ti nated foraminiferal as sem blages, sim i lar to those from the Verovice Shales, per sisted un der dysaerobic con di - tions (OAE1b) in the sep a rated parts of the ba sin. The mono - specific ag glu ti nated as sem blages known as biofacies B (Severin, 1983; Kuhnt and Kaminski, 1990), in clud ing mainly surficial infauna (Recurvoides), which are ac com pa nied by rare deep infauna (Gaudryina, Pseudobolivina) or scarce semi- infauna (Jaculella) and epifauna (Glomospira), ap peared in
black or ganic-rich de pos its (lower part of the Lgota Beds; Figs.
3 and 7). In this pe riod, plank ton, in clud ing cal car e ous dino - cysts and tintiniids (Colomiella), prob a bly ac cu mu lated in the sep a rated parts of the ba sin. In the Late Albian and Turonian, in tense sub si dence and vol ca nic ac tiv ity as so ci ated with a eustatic sea level rise in flu enced in creased phyto plankton pro - duc tiv ity and radiolarian blooms (CBTE). Si li ceous plank ton pro duc tiv ity and en hanced upwelling led to ex panded short-term ox y gen min ima in the Late Albian (OAE1d) and in the lat est Cenomanian (OAE2). In these pe ri ods of de fi cient ox - y gen lev els, ag glu ti nated foraminifers be came al most ex tinct in the bot tom wa ters, while plank tonic forms lo cally sur vived near the sur face (Hedber gella, Heterohelix, Guembelitria) and in sur - face wa ters (Rotalipora, Praeglobotruncana; Caron, 1985; Le - ckie, 1987; Leckie et al., 2002). The first forms oc curred in the up per part of the Lgota Beds, in clud ing spongiolites, and the lat - ter were noted in the var ie gated (green and red) shales be long - ing to the so-called radiolarian beds (Huss, 1957; Liszkowa, 1956). In these pe lagic de pos its of the Cenomanian–Turonian, the num ber of dinocysts spe cific for open ar eas (Pterodinium) in creased (Bąk et al., 2000). Forms of this type also oc curred pe ri od i cally in hemipelagic de pos its of the Albian (Lgota Beds).
This co in cided with changes in rel a tive sea level and phyto - plankton pro duc tiv ity at the time.
Fig. 7. Fau nal changes in ag glu ti nated foraminiferal as sem blages in re la tion to fa cies mod els and sea level fluc tu a tions, geotectonic ac tiv ity, and also oce anic anoxic and bi otic events
As sem blages with: 1 – surficial epifauna (Recurvoides), 1a – surficial epifauna (Recurvoides), semi-infauna (Jaculella) and rare deep infauna (Gaudryina, Pseudobolivina), 2 – surficial epifauna (Recurvoides) and shal low infauna (Plectorecurvoides), 3 – nu mer ous mo bile (Haplophragmoides) and very rare deep (Bulbobaculites, Arenobulimina) infauna, 4 – very rare deep infauna (Uvigerinammina, Gaudryina), 5 – surficial infauna (Recurvoides) or/and surficial infauna (Uvigerinammina, Gerochammina), 6 – sus pen sion (Nothia) and at tached epifauna (Ammodiscus)
level fluc tu a tions and anoxic and bi otic events. Ag glu ti nated foraminifers are re garded as autochthonous micro fauna and there fore are closely re lated to depositional en vi ron ments (e.g., Haig, 1979; Olszewska, 1984; Jones and Charnock, 1985;
Loubere, 1989; Kuhnt et al., 1989, 1992; Szydło, 2008). The sim pli fi ca tion of foraminiferal as sem blages may mainly be ob - served un der low ox y gen con di tions and high or ganic flux. Ag - glu ti nated foraminifers ex isted as bac te rial, de posit, and de tri - tus feed ers un der dysaerobic con di tions in the Early Albian (OAE1b) and the Late Albian (OAE1d). In the long per spec tive, de cay of the or ganic mat ter con trib uted to ox y gen con sump tion in the bot tom wa ters and fi nally led to the dis ap pear ance of ben - thic life. This was in ten si fied by vol ca nic ac tiv ity and a max i mal deep en ing of the ba sin dur ing pe lagic sed i men ta tion. The im - pov er ished as sem blages could also re flect the short sed i men - ta tion pe ri ods just af ter the sud den sup ply of coarse-grained ma te rial into the ba sin. In the long per spec tive, the sup ply of the sand stones con trib uted to the in crease of wa ter cir cu la tion and ox y gen a tion of the ba sin floor. Con se quently, these sed i men ta - tion ep i sodes fa voured nu mer ous and vari able deep wa ter morphotypes, which as sem bled the sec ond eco log i cal type of foraminiferal as sem blages.
Fau nal changes in the ag glu ti nated micro fauna co in cided with the sup ply of cal car e ous bioclastic ma te rial and caused phytoplankton pro duc tiv ity to fluc tu ate. This event was prob a - bly re corded for the first time in the Early Albian. It was cor re - lated with the oc cur rence of tintinnids (Colomiella), which are pre served in marly sed i ments of the Subsilesian Unit (Ol - szewska, 1997).
Ag glu ti nated foraminiferal as sem blages were pe ri od i cally re placed by plank tonic and cal car e ous ben thic foraminifers dur - ing the Albian-Turonian tran si tion. At the time of tec tonic in sta - bil ity and dy namic changes in sedimentation, cal car e ous nannoplankton, in clud ing mainly forms which were re sis tant to dis so lu tion, and lime stone of the Stramberk type had been sup - plied. Car bon ate rocks, in clud ing cal car e ous nannoplankton, orig i nated mainly from for mer Ju ras sic plat forms, which were up lifted and eroded in tensely in the sep a rated parts of the ba - sin. These events co in cided with the wide spread de struc tion of sponge “reefs”, which pro vided ma te rial for form ing the bio - siliceous de pos its (cherty mudstones and spongiolites). In these set tings, or ganic-walled dinocysts of lit to ral and low sa lin - ity en vi ron ments dom i nated.
These or ganic-walled cysts were re placed grad u ally by forms char ac ter is tic of open seas dur ing the Cenomanian. At that time, plank tonic si li ceous forms (radio lar ians) were wide - spread. The ex pan sion and ra di a tion of the phytoplankton was re lated to low tec tonic ac tiv ity and low-en ergy sed i men ta tion.
De po si tion of this type dom i nated in the Subsilesian Zone, while the sed i men ta tion of sponge-rich biosiliciclastic de pos its pre vailed in the Silesian Zone. Un der these con di tions spe cific plank tonic foraminifers sur vived. Their ex tinc tion was caused by the for ma tion of the OMZ in the sur face wa ters dur ing the Late Albian (OAE1d) and the lat est Cenomanian (OAE2).
Some of these, as eurytopic forms, had a wider eco log i cal tol er - ance (Heterohelix, Hedbergella, Guembelitria), and other ones,
anoxic wa ters into the sur face at the time.
Dur ing the Turonian, the evo lu tion of plank tonic foraminifera cor re lated with dy namic changes in depositional en vi ron ments, which were in duced by the re newed sup ply of terrigenous ma te - rial. This ma te rial mainly orig i nated from the east ern up lifted parts of the Silesian Ba sin, formed as the Subsilesian sub-ba - sin, in Cenomanian–Turonian time. The biogenic ma te rial, in - clud ing cal car e ous skel e tal el e ments of plank tonic forms, were lo cally sup plied in that time. These were cal car e ous nanno - plankton of the Ju ras sic and the Early Cre ta ceous, and fora - minifera of the Turonian–Santonian. Apart from new keeled plank ton be long ing to Marginotruncana, ag glu ti nated benthos that is rep re sented by forms be long ing to Uvigerinammina and Gerochammina oc cur in foraminiferal as sem blages. Fau nal changes in foraminiferal as so ci a tions were cor re lated with the de vel op ment of new niches dur ing the sed i men ta tion of var ie - gated cal car e ous de pos ition in the Turonian.
CONCLUSIONS
The se quences of the fos sils de scribed were clearly re - lated to sea level changes and also to phytoplankton pro duc - tiv ity dur ing the Albian–Turonian. The num ber, di ver sity, and pres er va tion of the fos sils dis cussed cor re spond with oce anic max i mum anoxic (OAE1b, OAE1d, OEA2) and bi otic (CTBE) events, which can be cor re lated with geotectonic and vol ca nic ac tiv ity in the Outer Carpathian Ba sin. Dur ing and af ter each type of event there oc curred sig nif i cant fau nal changes in foraminiferal as sem blages. Usu ally, the de creased vari abil ity and num ber of the micro fauna co in cided with dom i nant si li - ceous fos sils (spon ge spicules, radio lar ians) dur ing the Late Albian–Cenomanian or the Cenomanian–Turonian. In these in ter vals, such micro fossils were the pre dom i nant com po - nents of or ganic-rich de pos its (cherty mudstones, spongiolites and radiolarian shales). The spicule-rich de pos its in cluded also skel e tal el e ments of macro- and microfossils and also rock clasts from near shore en vi ron ments and land, which were up lifted and eroded at the time. The ac cu mu la tion of radiolarian skel e tons in large masses co in cided with a max i - mal sub si dence and eustatic sea level rise, which pre vi ously re sulted in radiolarian blooms (CTBE; Thurow, 1988; Bau - mgartner et al., 1992). Just be fore and dur ing this event, en - hanced vol ca nic ac tiv ity and upwelling were as so ci ated with an in creased sur face pro duc tiv ity and the de fi ciency of ox y gen in subsurface wa ters due to ox i da tion of or ganic car bon (Gucwa and Wieser, 1980; Vogt, 1989). This led to ex panded and in ten si fied ox y gen min ima, which co in cided with the elim i - na tion of life in bot tom (ag glu ti nated foraminifers) and then in sur face wa ters (foraminifers, radio lar ians and dinocysts). Dur - ing the Turonian, tec tonic re or ga ni za tion of the ba sin led to the re ac ti va tion of coarse-grained turbidites con tain ing re worked macrofossils and rock blocks sim i lar to those from the Lower Albian thick-bed ded de pos its, but in low num bers. Fi nally, coarse- grained de pos its were grad u ally re placed by hemipe -
lagic var ie gated shales dur ing the Turonian. At that time, di - ver si fied ag glu ti nated and sin gle plank tonic foraminifera rep - re sented mainly by deep-dwell ing forms ex isted in the bot tom or subsurface wa ters.
Ac knowl edge ments. We thank anon y mous re view ers for their con struc tive com ments on the manu script. We are grate ful
to Drs T. Malata, and to P. Nescieruk (Carpathian Branch of the Pol ish Geo log i cal In sti tute-Na tional Re search In sti tute) for his help dur ing field work and geo log i cal study. The re search was fi - nan cially sup ported by the State Com mit tee for Sci en tific Re - search grant No N307 005 32/0230 and by the PGI-NRI stat u - tory funds (pro jects 6.14.0009.00.0 and 6.14.0013.00.0).
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