TWO AMMONITES FROM THE EARLY CRETACEOUS DEEP-SEA
SEDIMENTS OF THE SILESIAN NAPPE, POLISH CARPATHIANS,
AND STRATIGRAPHIC PROBLEMS RESULTED FROM
MICROPALAEONTOLOGICAL DATING OF THEIR SITES
Zdenìk VAŠÍÈEK1, El¿bi eta GEDL2, Mari usz KÊDZIER SKI2 & Al fred UCH MAN2
1
In sti tute of Geon ics, ASÈR, Stu dent ská 1768. CZ- 708000 Ostrava- Poruba, Czech Re pub lic, e- mail: zde nek.va sicek@vsb.cz
2
In sti tute of Geo logi cal Sci ences, Jagiel lo nian Uni ver sity, Ole an dry 2a, 30- 063 Kraków, Po land, e- mail: ela.gedl@uj.edu.pl; mari usz.kedzier ski@uj.edu.pl; al fred.uch man@uj.edu.pl
Vašíèek, Z., Gedl, E., Kêdzier ski, M. & Uch man, A., 2010. Two am mon ites from the Early Cre ta ceous deep- sea sedi ments of the Sile sian Nappe, Pol ish Car pa thi ans, and stra tigraphic prob lems re sulted from mi cro pa lae on to lo-gi cal dat ing of their sites. An nales So cie ta tis Ge olo go rum Po lo niae, 80: 25–37.
Ab stract: Two am mon ites Tes chenites sub fluc ticu lus Re bou let and Crio sara si nella man dovi Thieuloy have been found for the first time in the Flysch Car pa thi ans. They oc cur in the so far poorly dated Early Cre ta ceous flysch de pos its of the Sile sian Nappe at Pozna chowice Dolne, in the Up per Ci eszyn Shale and the Hra dištì (Grodziszcze) beds litho types, re spec tively. Tes chenites sub fluc ticu lus points to Late Valang in ian (Fur cil lata Zone), but nan no -plank ton points to Late Hau terivian–Late Bar re mian and dino cysts to Late Hau terivian, all ana lyzed from the same sam ple. Crio sara si nella man dovi points also to Late Valang in ian (Fur cil lata Zone), what is not in con tra -dic tion with the nan no plank ton as sem blage (Early Valang in ian–Early Bar re mian) ana lyzed from the same bed, but dino cysts sug gest Late Hau terivian. Pres er va tion of the am mon ites and sedi men tary fea tures of their host beds ex clude re de po si tion. The dif fer ence in age by al most 3 Ma years be tween the am mon ites and mi cro fos sils can not be sat is fac to rily ex plained ac cord ing to the cur rent knowl edge on their bi os tra tigraphic mean ing; it is left as it is as a di lemma.
Key words: am mon ites, nan no plank ton, dino cysts, bi os tra tigra phy, Lower Cre ta ceous, Flysch Car pa thi ans. Manu script re ceived 26 March 2009, ac cepted 5 No vem ber 2009
IN TRO DUC TION
Macrofossils are very rare in the deep-sea, mostly flysch de pos its of the Carpathians. How ever, the Early Cre -ta ceous dark sed i ments of the Silesian Nappe con tain among oth ers rare ammonites, which are known since the 19th cen tury. Vi en nese ge ol o gist Lud wig Hohenegger men tioned as so ci a tion of ammonites from pelitic de pos its des ig -nated by him as the Wernsdorfer Schichten (re cent Veøo-vice beds). These ammonites were elab o rated by Uhlig (1883) and dated to the Barremian–Early Aptian. Later, Uhlig (1902) stud ied an other cephalopod col lec tion of Hohenegger, which came only with some ex cep tions from the Oberen Teschener Schichten (re cent Up per Cieszyn beds). They rep re sent rare find ings of the Valanginian age. Fre quent Barremian–Early Aptian ammonites were an a -lyzed by Kokoszyñska (1949), Szymakowska (1965, 1977, 1981) and Vašíèek (1972, 1975, 2008).
Most of the so far de scribed am mon ites were found in the west ern part of the Sile sian Nappe, where the Lower
Cre ta ceous crops out in larger area and where its lithos tra tigra phy and bi os tra tigra phy are bet ter rec og nized. Lithos -tra tigra phy and bi os -tra tigra phy of the Lower Cre ta ceous of the Sile sian Nappe in the area south and south east of Kra-ków is much less rec og nized, mostly ow ing to gen er ally poor ex posure. How ever, in the re gion of Pozna chowice Dolne (Fig. 1), the Lower Cre ta ceous is well ex posed. Two am mon ites were found in situ in two out crops of that re gion. They be long to taxa, which so far were not found in the Flysch Car pa thi ans. The am mon ites en able dat ing of their sites. A cal care ous nan no plank ton and dino cyst analy sis from these sites al low com pare the bi os tra tigraphic data ob -tained in dif fer ent ways, and what is, be side de scrip tion of the am mon ites, the main aim of the pa per.
GEO LOG I CAL SET TING
The Lower Cre ta ceous of the Poznachowice Dolne re -gion be longs to the Silesian Unit, which con sti tutes a large
Fig. 1. Lo ca tion maps and lithostratigraphic scheme of the Silesian Nappe. A. Gen eral maps; P.K.B. – Pieniny Klippen Belt. B. Lithostratigraphic scheme of the Silesian Nappe; the shaded units oc cur in the study area; the Veøovice beds of Pol ish ge ol o gists in lighter col our; com piled from G¹siorowski (1960); Szymakowska (1977); Œl¹czka & Kaminski (1998), B¹k et al. (2001), Gedl (2001, 2003), Cieszkowski et al. (2003), Golonka et al. (2008), Olszewska et al. (2008), and ref er ences therein. C. De tailed lo ca tion map; S-1 and S-2 re fer to sites of Teschenites subflucticulus and Criosarasinella mandovi, re spec tively
com plex nappe in the Ukrai nian, Pol ish and Czech Flysch Carpathians. This nappe con tains thick, di verse Kimme-ridgian to the early Mio cene de pos its, mostly flysch, which ac cu mu lated in the deep-sea Silesian Ba sin, which is lately called also the Severin-Moldavidic Ba sin, or the ProtoSilesian Ba sin for the Early Cre ta ceous stage of de vel op -ment (e.g., Œl¹czka et al., 2006; Golonka et al., 2008). This ba sin, a part of the West ern Tethys, was at least a few tens of kilo metres wide and a few hun dreds of kilo metres long. De pos its of the Silesian Ba sin were folded and thrust north -ward dur ing the Mio cene (e.g., Œl¹czka et al., 2006). Litho-stra tig ra phy of the Lower Cre ta ceous of the Silesian Unit is a mat ter of dis cus sion and runs to for mal iza tion and uni fi ca -tion by Golonka et al. (2008).
The Cre ta ceous in the study area was men tioned by KuŸniar (1923, 1924). Tec tonic frame work and stratigra-phic scheme of the area was pro vided by Bur tan (1978, 1984). Ap pli ca tion of the lat est lithos tra tigraphic propo si -tions for the Lower Cre ta ceous (Golonka et al., 2008) in the study area is highly pre ma ture, but an ap prox i mate scheme can be given.
The old est sedi ment of the study area are re ferred to the Up per Ci eszyn beds (Valang in ian–Hau terivian), which are pro posed as the Cisownica Shale Mem ber with the low er -most part of Hra dištì For ma tion (Golonka et al., 2008). How ever, ac cord ing to Olszewska et al. (2008), sedi men ta -tion of the Ci eszyn Lime stone was con tin ued at least un til the end of Valang in ian, what sug gests that sedi men ta tion of the Up per Ci eszyn beds started not ear lier than the Hau -terivian. It is domi nated by dark- grey marly mud stones alternating with regu larly thin- bedded, cal care ous sand -stones. In the west ern part of the Sile sian Unit, it is about 300 m thick.
The Up per Ci eszyn beds are over lain or partly re placed by the Hra dište (Grodziszcze) beds (Up per Hauterivian– Lower Ap tian). In the Bielsko- Bia³a re gion, depo si tion of the Hra dište beds ends in the mid dle Bar re mian (Gedl, 2003). They are rep re sented by grey marly shales al ter nat ing with thin cal care ous sand stone beds and marl stones. Lo cally, pack ages of thick bedded cal care ous sand stones oc -cur. Tra di tion ally, they are dis tin guished as the Grodziszcze Sand stone, which are now pro posed as the Piechówki Sand -stone Mem ber within the Hra dište For ma tion, which in -cludes also the more shaly parts of the Hra dište beds (Golonka et al., 2008). In the study area, Bur tan (1978) re -ferred the Grodziszcze beds only the thick- bedded flysch oc cur ring as lenses within the Up per Ci eszyn beds. They con tain con glom er ates and ex otic blocks, which can be in -ter preted as debris- flow de pos its. Age of these de pos its is older than the Bar re mian Piechówki Sand stone Mem ber (Golonka et al., 2008) and was as sumed as the Hau terivian (G¹sior owski, 1960). Most proba bly, these de pos its as well as the Grodziszcze Sand stone (Lower Ap tian) from Stêpina in the east ern part of the Pol ish Car pa thi ans (Szy makowska, 1977) rep re sent three dif fer ent litho somes (Fig. 1B), which de serve a sepa ra tion in lithos tra tigra phy (be yond scope of this pa per). In the west ern part of the Sile sian Unit, the Hra -dište beds are 95–140 m thick.
The Veøovice Shale (in Po land Barremian–Lower Albian) con tain black shales, mudstones interbedded with
rare crosslam i nated thin sand stone beds and si der it ic con -cre tions. Their low est part is cal car e ous and up the sec tion, they are non-cal car e ous. In the west ern part of the Silesian Unit, they are con fined to the Up per Aptian and dis tin -guished as the non-cal car e ous Veøovice For ma tion, which is 200–500 m thick (Golonka et al., 2008). How ever, dif fer -ent age and thick nesses of these de pos its are known in the Po- lish Carpathians. Ac cord ing to S³omka et al. (2006), thick ness of the Veøovice Shale is sta ble and ranges from 180 to 250 m. In the Moravian Carpathians, the Veøovice Shale is dated to the Late Aptian (Skupieñ, 2003; Golonka et al., 2008). In the Pol ish Carpathians, the Veøovice Shale is dated to the Barremian–Aptian (e.g., Szymakowska, 1981; Olszewska, 1997) and Barremian–ear li est Albian (e.g., Geroch & Nowak, 1963; Szyd³o, 1997). In the Andrychów re gion, sed i men ta tion of the Veøovice Shale ter mi -nated in the Early Albian; in the Bielsko-Bia³a re gion it ranges from the Late Barremian–Late Aptian (Gedl, 2003). Golonka et al. (2008) pro posed a limi ta tion of the Veøo- vice For ma tion to non- calcareous black shales con fined to the up per Ap tian. Ac cord ing to these authors, the older at least partly cal care ous black shales in the Pol ish Carpa-thians con sid ered so far as the Veøovice Shale should be ascribed to the Hra dište For ma tion. In the Pozna chowice Górne re gion, the Veøovice Shale is tec toni cally re duced.
The Lhoty (Lgota) beds (Al bian–Mid dle Ce no ma nian) is com posed mainly of thin bed ded sand stone tur bid ites and non- calcareous grey- greenish spotty shales, which are about 300 m thick. It is pro posed as the Lhoty For ma tion (Golonka et al., 2008), which in cludes the Mikuszowice Chert Mem ber in the up per most part. The Lhoty beds are poorly ex posed in the stud ied area.
In the study area, the Up per Ci eszyn beds and the bedded fa cies of the Hra dište beds are dif fi cult to sepa ra tion in the field. There fore, they are un di vided on the geo logi cal maps by Bur tan (1954, 1966a, b, 1974). They oc cur in sev eral small im bri cated thrust slices close to the north ern mar -gin of the Wiœn iowa tec tonic win dow, which be long to the Sub sile sian Unit. In places, the beds are strongly tec toni cally dis turbed. Bur tan (1978) pro vided the only closer de -scrip tion of these de pos its and as cribed them col lec tively to the Lower Cre ta ceous. Their pa lae on tol ogy, bi os tra tigra phy and in ter nal lithos tra tigra phy are poorly rec og nized. Su per -po si tion of beds be tween the thrust slices is im -pos si ble at this stage of re search. There fore, we re fer to litho types of the Up per Ci eszyn beds or the Hra dište beds rather than to these units sensu stricto.
G¹sior owski (1960) de scribed Early Cre ta ceous La mel -lap tychus from the Grodziszcze Sand stone (thick- bedded sandstones in the Hra dište beds) at Wiœn iowa and Racie-chowice-Wolica. Bur tan (1978, p. 25) cited G¹sior owski (1960) in de scrip tion of the Up per Ci eszyn Shale and in di cated that the ap tychae found by him point to the Hau -terivian. Kra jewski and Ur ba niak (1964, p. 120) men tioned the oc cur rence of Ap tychus in the Hra dište beds at Pozna -chowice Dolne in a tribu tary stream of the Krzy wor zeka River and un de ter mined An tho zoa and an am mon ite of the ge nus Crio ceras from the Hra dište beds on an un named hill in feet of the Grodzisko Mount. Szy makowska (1981) showed a few sites with am mon ites in the Pozna chowice
Dolne re gion on a gen eral geo logi cal map of the Pol ish Car pa thi ans but un for tu nately with out any closer data on the lo -cali ties and de ter mi na tions.
THE AMMONITES
The ammonites were found in two dif fer ent out crops along the Krzyworzeka River be long ing to two dif fer ent thrust slices. Teschenites subflucticulus Reboulet was found by Mariusz Hoffmann and Al fred Uchman in very thin-beded muddy turbidites with in ter ca la tions of very thin sandtone beds (GPS co-or di nates: N49°49’24.34”; E20°07’08.66”±5 m) as cribed pro vi sion ally to the Up per Cieszyn Shale ac cord ing to Burtan’s (1978) de scrip tion.
Crio sara si nella man dovi Thieuloy was found by El¿bi eta W³odarc zyk in steeply dip ping beds as cribed to the Hra -dište Beds (GPS co- ordinates: N49°49’49.05”; E20°07’ 12.05”±6 m). They are thin- bedded cal care ous tur biditic sand stones in ter ca lated with grey marly shales and rare medium- bedded sand stones. The tur biditic rhythms are here thicker (com monly more than 5 cm) than in the former lo -cal ity (sin gle cen ti me tres).
By anal ogy to the lithostratigraphy in the west ern part of the Silesian unit, the beds bear ing Teschenites subflucti-culus should be older than the beds bear ing Criosarasinella mandovi. How ever, there is no di rect ev i dence of su per po si -tion of these beds.
The ammonites are pre served as in com plete im pres -sions (Teschenites subflucticulus) or de formed in ter nal moulds (Criosarasinella mandovi). With re gard to the in com plete ness of shells, only ex cep tion ally some of di men sional pa ram e ters were mea sured, namely: D = shell di am e -ter, H = last whorl height, U = um bi li cus width. In the brack ets af ter di men sions in mm, val ues of H/D and U/D ra -tios are stated. The whorl width cannot be measured in any case.
SYS TEM ATIC DE SCRIP TION
The clas si fi ca tion at higher than ge nus level is based on the new edi tion of Trea tise of In ver te brate Pa le on tol ogy, part L (Wright et al., 1996). The ex cep tion is the ge nus Criosarasinella, which is as cribed to the suborder Ancylo-ceratina (Vašíèek, 2005).
Suborder AMMONITINA Hyatt, 1889 Superfamily PERISPHINCTOIDEA Steinmann, 1890
Fam ily NEOCOMITIDAE Salfeld, 1921 Subfamily NEOCOMITINAE Salfeld, 1921
Ge nus Teschenites Thieuloy, 1971
Type spe cies Teschenites flucticulus Thieuloy, 1977 (in Busnardo et al., 2003)
Teschenites subflucticulus Reboulet, 1996 Fig. 2
1977. Neocomites (Teschenites) flucticulus n. sp.: Thieuloy, p. 98, pl. 3, fig. 9.
v 1994. Neocomites (Teschenites) flucticulus Thieuloy: Vašíèek et al., p. 58, pl. 17, fig. 8.
* 1996. Neocomites subflucticulus n. sp.: Reboulet, p. 106, pl. 8, figs. 1-9.
1996. Neocomites flucticulus (Thieuloy): Reboulet, pl. 9, fig. 9.
2005. Neocomites (Teschenites) subflucticulus (Reboulet): Klein, p. 320 (cum syn.)
Ma te rial: An in com plete im print of the last whorl in grey mudstone. The im print be longs to a rather large, flat de formed shell with the non-pre served ven tral side. Poznachowice Górne, lithotype of the Up per Cieszyn beds. INGUJ 203P1.
De scrip tion: An im print of semi-in vo lute shell with high, slightly vaulted whorls and a rather wide um bi li cus. The de scrip tion of sculp ture, prob a bly in the vi cin ity of tran si tion of the phra-gmocone into the body cham ber, cor re sponds to the best pre served part of the im print. There, the shell is densely ribbed with rather thin, proverse, S-shaped ribs. The ribs be gin at the line of coil ing in in dis tinct bulges and con tinue to um bil i cal tu ber cles. From these tu ber cles, two, lo cally even three ribs run. In the case of two ribs, one of them may bi fur cate in the lower third of whorl. Oc ca -sion ally it is clear that be tween the bun dles of ribs run ning from the tu ber cles, one sim ple rib with the be gin ning closely above the um bil i cal tu ber cles can oc cur. All the ribs end in faint mar ginal tu -ber cles on the ven tral side.
Mea sure ments: The max i mal di am e ter of the shell is es ti mated at about 85–90 mm, it means that this is a macroconch. At the only mea sur able whole shell di am e ter D = 57 mm, H = 24.0 (0.42) and U = 17.5 (0.31).
Re marks: With re gard to the den sity of rib bing, but es pe cially to a rather wide um bi li cus, the de scribed im pres sion cor re sponds best to the di ag no sis of T. subflucticulus. The spe cies is close to T. Fig. 2. Teschenites subflucticulus Reboulet, INGUJ 203P1.
flucticulus, which dif fers by hav ing the nar rower um bi li cus (af ter Reboulet, 1996, U/D ranges from 0.22 to 0.28). Busnardo in Busnardo et al. (2003, p. 44) ex presses doubts about dis tin guish -ing T. flucticulus from T. subflucticulus as in di vid ual spe cies when only their dif fer ent strati graphic po si tions are taken into ac count, al though it is true that T. flucticulus de vel oped from the pre vi ous spe cies, and tran sient forms be tween them ex ist; how ever, the um -bi li cus width is a good di ag nos tic fea ture in this case. Forms with mark edly wider um bi li cus (T. subflucticulus) are stratigraphically older in the West ern Carpathians.
Dis tri bu tion: Ac cord ing to Reboulet (1996), T. subflucticulus oc -curs as sur edly only in France, from the Late Valanginian to the basal Hauterivian (ammonite Furcillata Zone to the base of Radia-tus Zone). On the ba sis of biostratigraphical re searches done in the sec tion of the Butkov quarry (Vašíèek et al., 1994; Vašíèek, 2005), T. subflucticulus oc curs in the Slo vak West ern Carpathians merely in the Late Valanginian (Furcillata Zone), whereas T. flucticulus oc curs as late as the Early Hauterivian.
Suborder ANCYLOCERATINA Wiedmann, 1960 Superfamily ANCYLOCERATOIDEA Gill, 1871
Fam ily ANCYLOCERATIDAE Gill, 1871 Subfamily CRIOCERATITINAE Gill, 1871
Ge nus Criosarasinella Thieuloy, 1977 Type spe cies Criosarasinella furcillata Thieuloy, 1977
Criosarasinella mandovi Thieuloy, 1977 Fig. 3
* 1977. Criosarasinella mandovi n. sp.: Thieuloy, p. 110, pl. 5, figs. 6, 7.
1996. Criosarasinella mandovi Thieuloy: Reboulet, p. 78, pl. 16, fig. 4;, pl. 20, figs. 1, 7; pl. 21, figs. 1, 3-7. v 2005. Criosarasinella mandovi Thieuloy: Vašíèek, p. 249,
figs. 3.2, 3.3.
Ma te rial: The only large, heavily de formed in ter nal mould hav ing poorly pre served in ner whorls, and with a rather fa vour ably pre served last halfwhorl. The fa vour ably pre served part of shell be -longs, ac cord ing to su tures, to the phragmocone, the pre vail ing
re main ing part be longs then to the body cham ber. The spec i men dis plays an unique, prob a bly taphonomic fea ture: the last half-whorl is sep a rated from the more ju ve nile evolute half-whorls so that the spec i men ap pears to be a shell with free coiled last whorl (for taphonomic in ter pre ta tion see Dis cus sion). Lithotype of the Hra-dište beds, Poznachowice Górne, INGUJ 203P2.
De scrip tion: An orig i nally evolute shell is dem on strated by in ter -nal whorls. The poorly pre served in ner whorls are cov ered with ribs of uni form type. Poorly vis i ble, del i cate tu ber cles are vis i ble through out the um bi li cus. The zone of tran si tion of phragmocone into the body cham ber and the body cham ber dis play S-shaped main ribs. They are cov ered by three rows of tu ber cles: um bil i cal, ventrolateral and mar ginal ones. Be tween the main ribs, two or three mark edly thin ner ribs with out tu ber cles are in serted. At the fi nal half-whorl, 14–15 main ribs are lo cated.
Mea sure ments: In the poorly pre served shell, which is heavily flat de formed, the morphometric pa ram e ters of the last but one whorl can be mea sured along sev eral rays: the diame ter D = 155 mm, H = 53.- (0.34) and U = 70.- (0.45). At the di am e ter of the shell D = 120 mm, H = 38. (0.32) and U = 54. (0.45). If we the o -ret i cally at tach the sec ond arily sep a rated last whorl to the line of coil of the for mer whorl, we must add two rel e vant heights of the last whorl to the di am e ter. At the di am e ter of the shell of 155 mm, whorl at the end of phragmocone is about 80 mm high of and about 105 mm high in the vi cin ity of shell peri stome. In the sum, the max i mum di am e ter of the shell (in flu enced by de for ma tion) at -tains about 340 mm. The bound ary be tween the phragmocone and the body cham ber is lo cated at the di am e ter of 160–165 mm. Re marks: The spec i men falls to the cat e gory of the Late Valanginian macroconchs, which are rather rare. Their body cham bers dis -play con sid er ably sim i lar or na men ta tions in shape of trituber-culate main ribs, be tween which in serted ribs with out tu ber cles are grad u ally re duced or fade away. Their main rep re sen ta tives are Neocomites (Varlheideites) peregrinus Raw son et Kemper, Rodi-ghieroites cardulus Com pany and Criosarasinella mandovi Thieuloy. For their ac cu rate iden ti fi ca tion and ge neric clas si fi ca -tion, the sculp ture and the coil ing of in ner whorls play a de ci sive role. In V. peregrinus, the in ner whorls over lap each other par tially, and thus the coil ing can be taken as semievolute. Ac cord -ing to Reboulet (1996, p. 95), the H/D ra tio of most V. peregrinus Fig. 3. Criosarasinella mandovi Thieuloy, INGUJ 203P2. Lithotype of the Hradište Beds, Poznachowice Górne. A. gen eral view of the lower side. B. De tail of A
macro- conchs ranges broadly from 0.35 to 0.40 (mode 0.38) and the U/D ra tio ranges from 0.35 to 0.40 (mode 0.36). Ribs on the in -ner whorls are thin and dense, of the so-called neocomitid type. R. cardulus dis plays all the whorls evolutely coiled, in which main and sub sid iary ribs can be dif fer en ti ated even on the in ner whorls. The main ribs are trituberculate. The in ner as well as adult whorls of C. mandovi are evolute to such an ex tent that the whorls are only in con tact. In the larg est spec i men of Reboulet (1996, p. 78), the shell di am e ter at tains 215 mm, with the ra tios H/D = 0.31 and U/D = 0.49. Close pa ram e ters were mea sured in the stud ied spec i -men from Poznachowice Górne. Other small dif fer ences can be ob served in the or na men ta tion of body cham bers of macroconchs. Each of trituberculate ribs of V. peregrinus and R. cardulus are ac -com pa nied by a sim ple rib along their fron tal sides. The ribs are sep a rated from each other by a con stric tion. At the case of C. mandovi, paired ribs ac com pa nied by a con stric tion are miss ing. Ac cord ing to the lit er a ture, the great est macroconchs reach the di -am e ter of 150–185 mm in of V. peregrinus and about 130 mm in R. cardulus. C. mandovi is up to 215 mm. The de scribed fea tures, es -pe cially the coil ing of in ner whorls, the s-pec i men can be as cribed C. mandovi. The spec i men at tains more than 300 mm in di am e ter. How ever, it can be slightly over es ti mated be cause of de for ma tion. Dis tri bu tion: C. mandovi oc curs in the Late Valanginian in the ammonite Furcillata Zone. It is known fore most from the
Vocon-tian Trough in France and from the Manín Unit of Slo vak West ern Carpathians. Fur ther more, it is known from Bul garia and a sin gle find ing co mes from the Koœcieliska Marl For ma tion of the Pol ish part of the Tatra Moun tains (Lefeld, 1974).
STRATI GRAPHIC EVAL U A TION
OF THE AMMONITES
Teschenites subflucticulus and Criosarasinella man-dovi are known mainly from the Late Valanginian of the Vocontian Trough in France. Ac cord ing to Reboulet (1996), Teschenites subflucticulus oc curs in the ammonite Furcillata Zone and reaches as far as the base of Hauterivian (Radiatus Zone). Criosarasinella mandovi oc curs in the ammonite Furcillata Zone (ammonite zones ac cord ing to Reboulet, 1996 and Reboulet et al., 2006). Both the men -tioned spe cies have also been found in sec tions in the But-kov quarry in the Slo vak Cen tral Carpathians, in the same strati graphic po si tion (Vašíèek, 2005). They are known merely from to the Med i ter ra nean warm-wa ter bioprovince. They are found for the first time in the Outer Carpathians.
CAL CAR E OUS NANNOPLANKTON
Two mi cro scope slides were pre pared from the cal car e -ous mudstone of ad hered to the ammonites us ing the rou tine sim ple smear-slide tech nique. They were in ves ti gated un der the light mi cro scope at mag ni fi ca tion ×1000 in bright and cross-po lar ized light as well as phase-con trast. The slides con tain mod er ately pre served nannofossil as sem blages with an av er age abun dance of 1 spec i men of nannofossil per 1 to 10 fields of view, al though as sem blage com ing from the T. subflucticulus bed (slide S-1) is a lit tle more abun dant and slightly better pre served than from the C. mandovi bed (slide S-2). State of pres er va tion of the stud ied as sem blages can be es ti mated as a slightly etched, e.g. E-1 for slide S-1 and E-2 for slide S-2 us ing Roth’s (1983) scale.
The stud ied as sem blages (Fig. 4) are poorly tax o nom i cally di ver si fied (Tab. 1). Only a few taxa have been rec og -nized. The most pop u lar spe cies is Watznaueria barnesiae, which dom i nates in both slides. The next taxon com monly found is W. fossacincta and as well as ge nus Retecapsa spp. in slide S-1.
The most re cent strati graphic nannoplankton zonation for Lower Cre ta ceous is given by Bown et al. (1998), who con cluded that the best nannofossils for biostratigraphy de -rive from NW Eu rope sec tions. They pre sented bo real nannoplankton zonation (BC zones) cor re lated against the bo real ammonite chronostratigraphy. The BC zones were also cor re lated with the Tethyan nannoplankton zonation (NC zones) pre vi ously es tab lished by Roth (1978, 1983), Bralower (1987) and Bralower et al. (1993).
In gen eral, the stud ied nannofossils are typ i cal of the Neocomian as sem blages with dom i nance of W. barnesiae, W. fossacincta or Rhagodiscus asper and Micrantholithus hoschultzii. The most im por tant spe cies for this study is the in dex spe cies Calcicalthina oblongata, which is pres ent in slide S-2. It is a typ i cal Tethyan spe cies, which ranges from
Fig. 4. Cal car e ous nannoplankton in cross-po lar ized light. A. Cretarhabus conicus, slide S-1; B. Rhagodiscus sp., slide S-2; C. Zeugrhabdotus embergeri, slide S-1; D. Watznaueria fossacincta, slide S-1; E. Micrantholithus sp., slide S-2; F. Calcicalathina sp., S-2. Length of scale bar is 1 µm
the low er most Valanginian to the up per part of lower Barremian (Bown et al., 1998). Micrantholithus hoschultzii (both slides) is known from the low er most Berriasian up to the Aptian, with two acme zones in the up per Hauterivian and in the lower Barremian. More over, the stud ied slides do not con tain Haysites irregularis or Eprolithus floralis, which have their FO in the Up per Barremian and in the Lower Aptian, re spec tively. Based on these cal car e ous nannoplankton zonal marker spe cies, the age of the stud ied ma te rial could be de ter mined as Lower Berriasian through Up per Barremian for S-1 (T. subflucticulus), and Lower Valanginian–Lower Barremian for S2 (C. mandovi). How -ever, slide S-2 (T. subflucticulus) con tains also Zeugrha-bdotus scutula, which hith erto re ported FO is in the lower part of Up per Hauterivian (see also Bown et al., 1998). In re gard to that strati graphic range, slide S-2 (T. subflucticu-lus) might rep re sent Up per Hauterivian–Up per Barremian.
DINOCYSTS AND PALYNOFACIES
The same sam ples as for cal car e ous nannoplankton were used for study of dinocysts: sam ple AmI is an equiv a -lent of slide S-1 (ammonite T. subflucticulus) and sam ple Am-II is an equiv a lent of slide S-2 (ammonite C. mandovi). 15 g of mudstone from each sam ple were pro cessed for palynological anal y sis: dis solv ing in 38% HCl and, then, in 40% HF, heavy liq uid sep a ra tion (ZnCl2), siev ing with a
15 µm sieve, and cen tri fug ing to con cen trate the re sid uum. Three gel a tineglyc er ine slides for each sam ple were pre -pared and stud ied un der transfluent light mi cro scope.
Palynofacies anal y sis were done on the ba sis of groups of com po nents (cf. Tyson, 1995; Bat ten, 1996): black woody par ti cles, brown woody par ti cles, sporomorphs, dinocysts, foraminifera test lin ings, and amor phous or ganic mat ter. Three slides for each sam ple were searched to ob tain strati graphic data on the ba sis of dinocysts.
In sam ple Am-I (Teschenites subflucticulus), palyno-fa cies are com posed of black woody phytoclasts (20.2%), brown woody phytoclasts (12.6%), cuticules (0.2%), sporo- morphs (33%), dinocysts (19.8%), amor phous or ganic mat -ter (12.8%) and foraminifera linnings (1.4%). Dinocysts of var i ous stage of pres er va tion, from well (es pe cially Circu-lodinium sp.) to very bad pre served cysts, are pres ent (Fig. 5). They in clude Achomosphaera neptunii, Avellodinium falsificum, Batioladinium jaegaerii, Batioladinium mi cro-podum, Circulodinium distinctum, Cymososphaeridium validum, Hystrichodinium pulchrum, Hystrichosphaerina schindewolfii, Kiokansium polypes, Kleithriasphaeridium corrugatum, Lithodinia stoverii, Nelchinopsis kostromien-sis, Oligosphaeridium com plex, Phoberocysta neocomica, Pseudoceratium cf. solocispinum, Pseudoceratium pellife-rum, Tanyosphaeridium regulare, Valensiella re tic u late, and Wallodinium krutzschii.
Achomosphaera neptunii has been re ported from the north-west Eu rope and North Sea wells from the up per Ryazanian to up per Aptian (Heilmann-Clausen, 1987), but usu ally is noted from the Hauterivian to the Barremian (e.g., Prössl, 1995). The pres ence of Lithodinia stoverii (FO in
Lower Hauterivian – Costa and Davey, 1992, or in up per Lower Hauterivian – Leereveld, 1995), Nelchinopsis kostromiensis (LO in Up per Hauterivian; Costa & Davey, 1992) and Cymososphaeridium validum (LO in Up per Hauterivian; Leereveld, 1995) in di cate Hauterivian. Cooc -cur rence of these cysts with Batioladinium jaegeri, taxon known from rocks not older than Late Hauterivian (e.g., Duxbury, 1977; Prössl, 1990) sug gests the Late Hauterivian age.
The pres ence of com mon Batioladinium jaegeri, and, less com mon, Avellodinium falsificum, B. micropodum, Discorsia nanna, and Hystrichosphaerina schindewolfii sug gests a con nec tion with the Bo real Prov ince; in the Tethys Prov ince those cysts are usu ally re cog nised as bo real im mi grants (cf., Leereveld, 1995).
Sam ple Am-II (Criosarasinella mandovi) con tains pa-lynofacies com posed of black woody phytoclasts (41.5%), brown woody phytoclasts (15%), sporomorphs (18.5%), dinocysts (17%), amor phous or ganic mat ter (1%), foramini- fera linnings (1.5%) and acritarchs (0.5%). Dinocysts (Fig. 5) are rather badly pre served, me chan i cally de stroyed, with py rite sphaeroids. They in clude: Avellodinium falsifi-cum, Cymososphaeridium validum, Dingodinium albertii, Discorsia nanna, Gonyaulacysta helicoidea, Kiokansium unituberculatum, Lithodinia pertusa, Muderongia staurota, Oligosphaeridium com plex, Phoberocysta neocomica, Pseudoceratium pelliferum, Pseudoceratium cf. retusum, Rhombodella vesca, Spiniferites sp., Subtilisphaera terrula, Systematophora cretacea, Systematophora syliba, Tanyo-sphaeridium magneticum, and Valensiella magna.
Ta ble 1 Cal car e ous nannoplankton in slide S-1 (T.
subflucticulus-bear ing bed) and S-2 (C. mandovi-subflucticulus-bear ing bed);
S-1 S-2
Biscutum constans (Górka) x
Calcicalathina oblongata (Worsley) x
Cretarhabdus conicus (Bramlette & Martini) x
Cretarhabdus sp. Bramlette & Martini x
Micrantholithus hoschulzii (Reinhardt) x x
Nannoconus sp. Kamptner x
Percivalia fenestrata (Worsley) x
Rhagodiscus asper (Stradner) x
Retecapsa octofenestrata (Bralower) x Retecapsa surirella (Deflandre & Fert) x
Retecapsa sp. Black x
Stradnelithus sp. Black x
Tranolithus gabalus (Stover) x
Watznaueria barnesiae (Black) x x
Watznaueria fossacincta (Black) x
Zeugrhabdotus embergeri (Noël) x
Zeugrhabdotus scutula (Bergen) x
Fig. 5. Se lected dinocysts. A, D, F–H and K from sam ple Am-I (T. subflucticulus); B, C, E, I and J from sam ple Am-II (C. mandovii). A. Pseudoceratium pelliferum; B. Cymososphaeridium validum; C. Phoberocysta neocomica; D. Batioladinium jaegeri; E. Come-todinium habibi; F. Circulodinium distinctum; G. Nelchinopsis kostromiensis; H. Lithodinia stoveri; I. Subtilisphaera terrula; J. Discorsia nanna; K. Kiokansium sp. Length of scale bar is 10 µm and it re fers to all pic tures
The first oc cur rence data (FAD) of Muderongia stau-rota are known from both Tethyan and Bo real prov inces at Early Hauterivian (A. radiatus and E. amblygonium ammonite zones, re spec tively; Leereveld, 1995). The first oc cur -rence of Subtilisphaera terrula at Late Hauterivian is known both from Tethyan and Bo real prov inces (cf. Davey, 1979, 1982; Leereveld, 1995). Lithodinia pertusa dis ap pear at Late Hauterivian, ac cord ing to Leereveld, 1995. These data sug gest Late Hauterivian age of the sam ple Am-II (Criosarasinella mandovi). The pres ence of Avellodinium falsificum, Discorsia nanna and Valensiella magna im pli -cates con nec tion with the Bo real Prov ince; in the Tethys Prov ince those cysts are re cog nised as bo real im mi grants (cf. Leereveld, 1995).
Both sam ples are rich in palynomorphs (50% in Am-I and 35% in Am-II). The pres ence of foraminifera lin ings and, oc ca sion ally, cu ti cles in sam ple Am-I in di cates rather shal low ma rine prov e nance of the sed i ment, which was trans ported into deeper en vi ron ment. Com par ing palyno-fa cies of these two sam ples, sam ple Am-II rep re sents more dis tal en vi ron ment than sam ple Am-I: cu ti cles are ab sent, sporomorphs less fre quent and among dinocyst Dingo-dinium sp. oc curs (outer neritic group; Leereveld, 1995). How ever, beds are thicker around sam ple Am-II than around sample Am-I.
DIS CUS SION
Ammonites are con sid ered as the most valu able strati graphic in di ca tors es pe cially for the Ju ras sic and the Cre ta ceous. The ammonite spec i mens from this study show a nar -row strati graphic range re stricted to the Late Valanginian (the ammonite Furcillata Zone in both cases) in con trast to the wide ranges ob tained from dinocyst and mark edly wider from the cal car e ous nannoplankton in ves ti ga tions (Fig. 6). More over, the ranges of the dif fer ent groups of fos sils are not syn chro nous.
In the case of Teschenites subflucticulus, nannoplank-ton as sem blage com prises three nannoplanknannoplank-ton zones from the base of Valanginian to the Lower Barremian and dino-cyst as sem blage rep re sents only Up per Hauterivian against the Up per Valanginian based on the T. subflucticulus. In the case of Criosarasinella mandovi, nannoplankton as sem -blage in di cates at least Up per Hauterivian based on the first oc cur rence of Z. scutula, which is con sis tent with the strati -graphic po si tion based on the dinocyst as sem blage, but still dif fers from the date based on the ammonite (Late Valan-ginian).
Thus, there is no con flict in age de ter mi na tion based on the cal car e ous nannoplankton and dinocysts, but the age based on them is dif fer ent from the age based on the
ammonites by about 3 Ma years. The sit u a tion is not easy to ex plain. As a rea son, the redeposition of older ammonites and mi gra tion of biota can be considered.
The stud ied ammonites oc cur in very thin-bed ded (Teschenites) or thin- to me dium-bed ded (Criosarasinella) pack age of beds. The pack ages dis play al ter na tions of sand -stones and shale sed i ments, in which the sand stone beds were de pos its by weak turbidites or bot tom cur rents (rip ple mark phase). Teschenites was found in a thin marly shale layer, which was de pos ited by even weaker cur rents. Criosarasinella shell was laid flat in a marly shale and its first cham bers were filled by sand stone (Fig. 7A). The firsts sand stone layer fill ing pro tected the shell. Its un pro tected parts, in clud ing umbiculus and part of the in ner whorls were dis solved and or col lapsed (Fig. 7B, D). Than the next sand -stone layer (sec ond sand -stone layer was de pos ited), which filled the de pres sion af ter col lapse and dis so lu tion of the ammonite shell. It dis play dis tinct rip ple cross lam i na tion and slightly ero sive base. The first and the sec ond sand stone beds are welded and ap pear as one bed. The first sand stone layer shell fill ing form the in ter nal mould of the lower part of the shell (Fig. 7D), which dis plays cast of ribs, frag ments of shell and cast of lobe line. The pres er va tion style is sim i -lar to the so-called half ammonites (Seilacher et al., 1976; Maeda & Seilacher, 1996).
Such a pres er va tion and the sed i men tary fea tures of the bear ing strata point that the ex hu ma tion of the Late Valangi- nian ammonites and their redeposition af ter al most more than 3 Ma years dur ing the Late Hauterivian is very lit tle prob a ble. Af ter such a time (like from Plio cene to re cent), the shells should be bur ied and filled with sed i ment. Rede-po si tion of heavy (in case of large Criosarasinella sev eral ki lo grams), sed i ment-filled shells by weak cur rents is not re li able. The closed shell can not be filled with crosslam i nated sed i ment. There is also no ev i dence of lon ger nonde -po si tion. Thus, the ammonites should in di cate an age of the beds in which they were found.
It should be stressed, that strati graphic ranges of the nannoplankton taxa from this study were es tab lished by Bown et al. (1998) in ref er ence to the bo real ammonite zonation, so some dif fer ences in chronostratigraphic po si -tion of strati graphic ranges can not be ex cluded for Tethyan realm. The study area rep re sents a tran si tional do main with in flu ence of bo real dinocysts but Tethyan ammonites, where such dif fer ences can be also expected.
Some nannoplankton taxa ap pear ear lier in the Tethyan Prov ince than in the Bo real one. For in stance, Bown (1992) is of opin ion that the old est nannoplankton taxa from the Late Tri as sic evolved within the Tethys first and then spread into the new eco log i cal niches out side, for in stance into the Bo real Prov ince. Such pat tern seems to be re peated fur ther for the other taxa, though the op po site pref er ences are also ob served, e.g. or i gin of taxa in the sub po lar (highlat i tude) re gions and mi gra tion through the time to the trop i -cal bioprovince. The best known Cre ta ceous spe cies with such pref er ences is Nephrolithus frequens, coolwa ter in di -ca tor which mi grated through the al most all Maastrichtian to the warmer re gions (Thierstein, 1981; Bur nett, 1998). There fore, biostratigraphic zonation of cal car e ous nanno-plank ton zones or the age of rock sam ple based on that group of fos sils can not be es tab lished with out ref er ence to palaeobiogeography. Ac cord ingly, chronostratigraphic po -si tion of the first oc cur rence of Z. scutula given in Fig. 6
Fig. 7. Model of pres er va tion of Criosarasinella mandovi Thieuloy. A–C – Taphonomic stages; 1 and 2 in C re fer to the first and sec ond sand stone lay ers, re spec tively. D – Lower part of the spec i men; 1 – in ter nal mould filled with the first sand stone layer; sh – shell frag ments; lo – area of lobe line pres er va tion; 2 – sec ond sand stone layer with cross lam i na tion, 3 – area of com plete shell dis so lu tion filled with the sec ond sand stone layer, 4 – con cave col -lapsed part of shell with casts of shell frag ments, 5 – umbiculus part com pletely dis solved and filled the second sandstone layer
may be dif fer ent in the Tethyan Prov ince and, prob a bly, lower than in Bo real Prov ince. This can ex plain dif fer ences in age based on the ammonite Criosarasinella mandovi and on the nannoplankton zonation. Dinocyst ranges (FAD) of M. staurota and S. terrula in Early and Late Hauterivian re -spec tively are well known and al most co eval both from the Tethyan and Bo real prov inces (Davey, 1979, 1982; Leereveld, 1995). Batioladinium jaegerii (FAD in Late Hauterivian) is usu ally treated as bo real im mi grant in the Tethyan prov ince. In the Pol ish Carpathians, this spe cies was noted be fore from Veøovice beds (Silesian Unit) near Bielsko-Bia³a (Gedl, 2003) from Up per Barremian. Batio-ladinium jaegerii was also noted in the Pieniny Lime stone For ma tion, in Lower Barremian sam ple (Gedl, 2007).
None of the ex pla na tions of the dif fer ences in age de -ter mi na tion on the ba sis of ammonites, cal car e ous nanno-plank ton and dinocysts is sat is fac tory. There fore, we would like to left this prob lem as a di lemma. Prob a bly, age de ter -mi na tions based on dif fer ent tax o nomic groups in other Carpathian flysch sec tions will bring sim i lar prob lems, which solv ing should en hance biostratigraphic schemes.
Apart from the dif fer ences in dat ing the all groups of fos sils point to more or less the same age of both sites, which were as cribed to two dif fer ent lithotypes, which are typ i cal of gen er ally older Up per Cieszyn Shale and gen er -ally youn ger Hradište beds. How ever, these lithostratigraphic units interfinger and are partly co eval. The stud ied sec -tion con firms such a sit u a -tion.
CON CLU SIONS
1. Tethyan ammonites Teschenites subflucticulus Reboulet and Criosarasinella mandovi Thieuloy have been indentified for the first time in the Flysch Carpathians, in the Lower Cre ta ceous of the Silesian Unit.
2. The ammonites point to Late Valanginian (Furcillata Zone), but nannoplankton and dinocysts from their sites point to Late Hauterivian.
3. Pres er va tion of the ammonites and sed i men tary fea -tures of the host beds ex clude redeposition of the ammo-nites.
4. The 3 Ma years dif fer ence in age in dat ing by the ammonites and microfossils is un re solved di lemma; maybe mi gra tions be tween bioprovinces in flu ence strati graphic ranges of these fossils.
Ac knowl edge ments
Criosarasinella mandovi was found by El¿bieta W³odarczyk dur ing her field work for M.Sc. The sis. Mariusz Hoffmann as so ci -ated with found ing of Teschenites subflucticulus. Prof. Barbara Olszewska (Pol ish Geo log i cal In sti tute, Carpathian Branch, Kraków) and Prof. Andrzej Wierzbowski (Uni ver sity of War saw) pro vided help ful com ments and im prove ments.
Ap pen dix
Al pha betic list of dinocyst taxa from sam ples Am-I and Am-II (for tax o nomic ci ta tion see Wil liams et al., 1998).
Achomosphaera neptunii (Eisenack, 1958) Davey and Wil liams, 1966
Avellodinium falsificum Duxbury, 1977
Batioladinium jaegaerii (Al ber ti, 1961) Brideaux, 1975
Batioladinium micropodum (Eisenack & Cookson, 1960) Bride-aux, 1975
Circulodinium distinctum (Deflandre & Cookson, 1955) Janso-nius, 1986
Cymososphaeridium validum Davey, 1982b Dingodinium? albertii Sarjeant, 1966
Discorsia nanna (Davey, 1974) Duxbury, 1977, emend. Khowaja- Ateequzzaman et al., 1985
Gonyaulacysta helicoidea (Eisenack & Cookson, 1960) Sarjeant, 1966
Hystrichodinium pulchrum Deflandre, 1935 Hystrichosphaerina schindewolfii Al ber ti, 1961
Kiokansium polypes (Cookson and Eisenack, 1962) Be low, 1982 Kiokansium unituberculatum (Tasch in Tasch et al., 1964) Stover
& Evitt, 1978
Kleithriasphaeridium corrugatum Davey, 1974 Lithodinia pertusa Duxbury, 1977
Lithodinia stoverii (Millioud, 1969) Gocht, 1976
Muderongia staurota Sarjeant, 1966c, emend. Monteil, 1991b Nelchinopsis kostromiensis (Vozzhennikova, 1967) Wiggins,
1972, emend. Har ding, 1996
Oligosphaeridium com plex (White, 1842) Davey & Wil liams, 1969
Phoberocysta neocomica (Gocht, 1957) Millioud, 1969, emend. Helby, 1987
Pseudoceratium cf. retusum Brideaux 1977
Pseudoceratium cf. solocispinum (Davey 1974) Har ding 1990 Pseudoceratium pelliferum Gocht, 1957, emend. Dörhöfer &
Davies, 1980
Rhombodella vesca Duxbury, 1980 Spiniferites sp.
Subtilisphaera terrula (Davey, 1974) Lentin & Wil liams, 1976; emend. Har ding, 1986
Systematophora cretacea Davey, 1979 Systematophora syliba Davey, 1979 Tanyosphaeridium magneticum Davies, 1983 Tanyosphaeridium regulare Davey & Wil liams, 1966 Valensiella magna (Davey, 1974) Courtinat, 1989 Valensiella reticulata (Davey, 1969) Courtinat, 1989
Wallodinium krutzschii (Al ber ti, 1961) Habib, 1972 emend. Poulsen, 1996
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