A new Lower Coniacian fauna from the Jerzmanice Zdrój region of the North Sudetic Basin, SW Poland

Ge olo gia Sudetica, 2008, 40: 33–50.

A new Lower Co nia cian fauna from the Jerz manice Zdrój re gion of the North Sudetic Ba sin, SW Po land

Alina Chrz¹stek

In sti tute of Geo log i cal Sci ences, Wroc³aw Uni ver sity, Maksa Borna 9, 50-204 Wroc³aw, Po land, e-mail: alina.chrzastek@ing.uni.wroc.pl

Key words: Lower Coniacian, Up per Cre ta ceous, North Sudetic Ba sin, inoceramids, bi valves, palaeoenvironment, West Sudetes.

Ab stract

Manu script re ceived 5 June 2008, ac cepted 20 De cem ber 2008

IN TRO DUC TION

The Jerz manice Zdrój area oc curs in the south ern part of the North Sudetic Syn cli nor ium (¯elaŸniewicz & Alek - sandrowski, 2008) in which there is the Leszc zyna–Jerz - manice half- graben that con tains Ce no ma nian–Co nia cian (lower Up per Cre ta ceous) de pos its (Chrz¹stek, 1995) (Figs 1, 2). Within the Jerz manice Zdrój area there is an out crop near the vil lage of Jerz manice Zdrój of Lower Co nia cian sedi ments (Figs 1, 2, 3A) from which a rich fos sil as sem - blage (Tab. 1) can be ex tracted. This as sem blage com prises some 16 taxa, mainly bi valves, and in cludes a frag ment of prob able am mon ite and also a shark’s tooth from the fam - ily Cre toxyr hini dae (?Cre toxyr hina man telli, Agas siz, 1843). Such shark’s teeth were pre vi ously un known from the Lower Co nia cian of the North Sudetic Ba sin, though teeth of Cre toxyr hina man telli have been de scribed from the Ce no ma nian and Tu ro nian near Lwówek Œl¹ski (Scu - pin, 1912–13; Kühn & Zim mer mann, 1919). In the Ce no - ma nian and Tu ro nian of the North Sudetic Ba sin, teeth of

6 shark spe cies have been rec og nised (Scu pin, 1912–13;

Kühn & Zim mer mann, 1919). Scu pin (1912–13) de scribed Lower Co nia cian bi valves from other parts of the North Sudetic Ba sin, mostly in the vi cin ity of Warta Boles³a- wiecka, and men tioned only 3 taxa from Jerz manice Zdrój: Pec ten cu lus ge initzi d’Or bigny, 1843–47, Cu cul laea sp., and Inoce ra mus la tus Man tell, 1822. Palaeo geo graphic re con struc tions, based on de tailed lithos tra tigraphic and bi os tra tigraphic analy ses of the Up per Cre ta ceous de pos - its, were given by both Scu pin (1912–13) and, later, by Mile wicz (1958; 1967; 1973a, b; 1979; 1997; 1998) who en - vis aged two is lands in the Late Cre ta ceous sea de liv er ing de tri tus into the North Sudetic Ba sin. This pa per re ports on new macro- and mi cro fauna as sem blages from the marly sand stones of the Jerz manice Zdrój sec tion, con - firms an Early Co nia cian age for these de pos its, and of fers a palaeo geo graphic re con struc tion of the sedi men tary en - vi ron ment of these rocks.

GEO LOG I CAL SET TING

The North Sudetic Syn cli nor ium oc curs at the NE rim of the Bo he mian Mas sif in the west ern part of the Fore- Sudetic Block. The base ment of this syn cli nor ium com prises the ?Edia ca ran to Mis sis sip pian low- grade meta - mor phic rocks of the Kac zawa Com plex (Ba ra nowski et al., 1990; Chrz¹stek et al., 2004), on which rest in com plete suc ces sions of Up per Pa laeo zoic (Car bon if er ous (Penn syl - va nian) and Per mian), Meso zoic (Tri as sic and Up per Cre -

ta ceous) and Ce no zoic plat form sedi ments. These plat - form sedi ments were gen tly folded and faulted dur ing the Palaeo gene when the North Sudetic Ba sin un der went tec - tonic in ver sion to pro duce the present- day North Sudetic Syn cli nor ium.

Tri as sic de pos its para con forma bly un der lie the Up per Cre ta ceous suc ces sion (Mile wicz, 1997). In the south ern part of the ba sin, it is the Lower and Mid dle Bunt sand -

Fig. 1. Geo log i cal map of the North Sudetic Ba sin (mod i fied af ter Sawicki, 1995).

LOWER CONIACIAN FAUNA, JERZMANICE ZDRÓJ

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Fig. 2. Geo log i cal sketch map of the Jerzmanice Zdrój area of the North Sudetic Ba sin (mod i fied af ter Milewicz & Jerzmañski, 1956–57).

stein, whereas in the north ern part Röt and Muschel kalk rocks are in evi dence at the non con form ity. Lo cally, in the Wleñ Trough, the Up per Cre ta ceous sedi ments cover the Rot lieg en des and meta mor phic rocks of the Kac zawa Com plex (Gorczyca- Ska³a, 1977; Œli wi ñski et al., 2003).

The Up per Cre ta ceous of the North Sudetic Ba sin is di vided into 3 for ma tions: the Ra kowice Wiel kie For ma - tion (Ce no ma nian–Co nia cian), Czerna For ma tion (San to -

nian) and Wêgliniec For ma tion (San to nian) de scribed by Mile wicz (1997), Œli wi ñski et al. (2003), Chrz¹stek et al.

(2004).

In the North Sudetic Ba sin, Late Cre ta ceous sedi men - ta tion oc curred from the Cenomanian to the San to nian (Mile wicz, 1973a, b; 1997). The thick ness of the Up per Cre ta ceous de pos its ranges be tween 600 m and 1,100 m, the Co nia cian de pos its them selves be ing up to ~310 m thick (Mile wicz, 1973a, b; Ba ra nowski et al., 1990). In the bore hole known as Wêgliniec IG 1, lo cated in the west ern part of the North Sudetic Ba sin, Lower Co nia cian rocks

~130 m thick were drilled (Mile wicz, 1988). The Up per Cre ta ceous sedi ments of the Ce no ma nian, Tu ro nian and Co nia cian of the North Sudetic Ba sin are mostly sand - stones and marls, whereas the San to nian sedi ments are of mud stones and sand stones with in ter ca la tions of clay - stones and coals (Ba ra nowski et al., 1990; Chrz¹s- tek, 2002; Œli wi ñski et al., 2003; Leszc zyñski & Cho dowska, 2008). Sand stones domi nate in the east ern part of the North Sudetic Ba sin, whereas mud stones and marls domi - nate its west ern part (Œli wi ñski et al., 2003). As a re sult of the axis of the North Sudetic Syn cli nor ium plung ing to - ward the WNW, the young est sedi ments now out crop in the north west part of the ba sin (Mile wicz, 1997). Co nia - cian marly sand stones from the North Sudetic Ba sin have been de scribed by Mile wicz (1997, 1998). The lower part of the Lower Co nia cian suc ces sion con tains fine- grained sand stones, the up per part con tains me dium-grai- ned sand stones (Mile wicz, 1998), and all the sand stones pass lat er ally into car bon ate de pos its. Ac cord ing to Mile wicz (1997, 1998), the Lower Co nia cian sand stones con tain the small est grain- size sand (0.2 mm) of all the Cre ta ceous sand stones in the North Sudetic Ba sin.

LITHOSTRATIGRAPHY AND BIOSTRATIGRAPHY

The biostratigraphic sub di vi sion of the Up per Cre ta - ceous of the North Sudetic Ba sin is based on inoceramids (Milewicz, 1997). Ac cord ing to Milewicz (1997), the Lower Coniacian be longs to the Inoceramus koeneni ho ri - zon. The di vi sion of the Up per Cre ta ceous sed i ments of Po land, Ger many, Eng land, Cen tral Eu ro pean Rus sia and the United States has been fur ther re fined by Walaszczyk (1992), Walaszczyk & Wood (1998), Walaszczyk &

Cobban (2004), Tröger & Wejda (1998), Tröger (2004), Walaszczyk et al. (2004) and Wood et al. (2004).

At the bound ary be tween the Turonian and Coniacian in Po land and Ger many, Walaszczyk & Wood (1998) claim that the bi valves Mytiloides and Inoceramus are re placed by Cremnoceramus, the lat ter be ing most com mon in the up per most Turonian and Lower Coniacian. Ac cord ing to Walaszczyk & Wood (1998), the bound ary be tween the Turonian and the Coniacian is the base of the Cremnoceramus deformis erec tus Zone and is marked by the first ap pear ance of Cremnoceramus deformis erec tus Meek, 1877. The Turonian–Coniacian bound ary in Po land cor re sponds to the for mer Cremno-

ceramus brogniarti Zone (Walaszczyk, 1992), Cremnocera- mus deformis erec tus Meek, 1877 be ing a syn onym of Cremnoceramus rotundatus Zone (Walaszczyk & Wood, 1998; Walaszczyk & Cobban, 1998). The bound ary be - tween the Turonian and the Lower Coniacian in other parts of Eu rope – Sax ony (Ger many), Eu ro pean part of Rus sia, Eng land and the United States – is marked by the lower bound ary of the Cremnoceramus deformis erec tus Zone (Tröger & Wejda 1998; Walaszczyk & Cobban, 1998; Walaszczyk & Wood, 1998; Walaszczyk et al., 2004;

Wood et al., 2004). The base of the Cremnoceramus rotun- datus Zone in Ja pan, how ever, is equiv a lent to the base of the Cremnoceramus deformis erec tus Zone (Noda & Matsu- moto, 1998).

Inoce ra mids pro vide the ba sis for the sub di vi sion of the Lower Co nia cian into 5 zones (Wa laszc zyk & Wood, 1998; Wood et al., 2004), which are as fol lows: Crem noce - ra mus de formis erec tus; Crem noce ra mus wal ters dor fen sis han novren sis; Crem noce ra mus cras sus in con stans; Crem - noce ra mus cras sus + Crem noce ra mus de formis de formis;

and Inoce ra mus gib bo sus.

Ta ble 1 Fos sil taxa in the Lower Coniacian at Jerzmanice Zdrój

(North Sudetic Ba sin)

No Taxa

1 Anatina (Cercomya) lanceolata Geinitz, 1871-75 2 Crasatella arcacea Roemer, 1841

3 Cremnoceramus deformis erec tus Meek, 1877

4 Cremnoceramus waltersdorfensis waltersdorfensis Andert, 1911 5 Cucullaea sp.

6 Cytherea sp.

7 Granocardium cf. drescheri Böhm, 1911 8 Inoceramus latus Mantell, 1822 9 Inoceramus lusatiae Andert, 1911 10 Inoceramus sp.

11 ?Lima haidingeri Zittel, 1878

12 Ostrea (Alectryonia) sudetica Scupin, 1912-13 13 Panopea depressa Scupin, 1912-13

14 Panopea muelleri Scupin, 1912-13 15 Tellina strigata Goldfuss, 1834-40 16 ?Cretoxyrhina mantelli Agassiz, 1843

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Fig. 3. The Lower Coniacian sec tion in Jerzmanice Zdrój, North Sudetic Ba sin. (A) Rock ex po sure at Jerzmanice Zdrój; (B–D) Foraminifer Ammodiscus cre ta ceous Reuss, 1845; (E) Foraminifer Gaudryina laevigata Franke, 1914; (F, G) Foraminifer Gavelinella ammonoides Reuss, 1845. In B–G the photo height is 2 mm.

LOWER CONIACIAN IN JERZMANICE ZDRÓJ

The Lower Co nia cian sedi ments of the Ra kowice Wiel kie For ma tion in the Jerz manice Zdrój sec tion are fine- grained grey ish marly sand stones with in ter ca la tions of sandy lime stone. Thin sec tions of the marly sand stones show that grain size var ies from 0.05 mm to 0.2 mm; that there is a pre domi nance of sub rounded quartz grains, only a mi nor ity be ing suban gu lar to an gu lar; that glau co nite is pres ent; and that there are a few pla gio clases and some iso - lated flakes of mus co vite. The marly sand stones con tain 10–20% car bon ate; clay min er als, such as kao lin ite, can also be ob served. Pre sent through out the Lower Co nia - cian se quence are mi cro crys tal line SiO₂, some Fe and Ti ox ides and phos phates, such as col lo phane: the heavy min - er als ru tile and zir con are rare. The ce ment (ma trix) for these sand stones is a carbon- rich clay, the clay min er als them selves con sti tut ing up to 50% of the ma trix. In agree - ment with classification of sed i men tary rocks (Lorenc, 1978; Manecki & Muszyñski, 2008), the ma jor ity of the Lower Co nia cian rocks may be clas si fied as marly sand - stones.

A mi nor ity of the Lower Co nia cian rocks, how ever, should be clas si fied as sandy lime stones. Thin sec tions of these sandy lime stones dem on strate that car bon ates, mostly in the form of sparite ce ment, domi nate over quartz (20–25%,) and clay min er als (about 10%). Some - times the sandy lime stones show di rec tional tex tures and clear lami na tions, which are marked by the hori zon tal ori - en ta tion of lon gi tu di nal skele tal ele ments.

It is the marly sand stones of the Jerz manice Zdrój sec - tion that con tain the fos sils de scribed in this pa per: the inoce ra mid bi valves, the prob able frag ment of am mon ite,

and the Cre toxyr hini dae shark's tooth (?Cre toxyr hina man telli Agas siz, 1843) (Tab. 1). Thin sec tions of the marly sand stone re veal the abun dant fo ra mini fers and some less com mon gas tro pods (Tab. 2).

SYS TEM ATIC PALAE ON TOL OGY OF FOS SILS

This sec tion pres ents the sys tem atic palae on tol ogy of the newly found inoceramids and the ver te brate re mains from the Lower Coniacian Jerzmanice Zdrój out crop (Ta - ble 1). Other fos sil taxa are only briefly men tioned. Fos sils de scrip tions are based on pa pers by Scupin (1912–13);

Andert (1934); Gawor-Biedowa (1980); Cappetta (1987);

Walaszczyk (1988, 1992): Tarkowski (1991); Teisseyre (1992); Noda & Matsumoto (1998);Walaszczyk & Wood (1998); Cicimurri (2001a, b); Walaszczyk et al., (2004);

Wiese et al., (2004); Wood et al., (2004) and Zonova &

Yazykowa (1998). All the de scribed spec i mens (cat a logue num bers start ing MGU.Wr) are de pos ited in the col lec - tions of the Geo log i cal Mu seum of the Uni ver sity of Wroc³aw.

Ge nus Cremnoceramus Cox, 1969 Cremnoceramus deformis erec tus Meek, 1877

Fig. 4H–I MGU.Wr – 5442s

1988 Cremnoceramus rotundatus Fiege, 1930; Walasz- czyk; Pl. 7, figs 1-6.

1992 Cremnoceramus brongniarti Mantell, 1822; Walasz- czyk; p. 48–52, Pl. 22, figs 1–2; Pl. 23, figs 1–5; Pl.

24, figs 1–5; Pl. 25, figs 1–5; Pl. 30, fig. 2.

Ta ble 2 Foraminifers in the Up per Cre ta ceous of the North Sudetic Ba sin.

LOWER CONIACIAN FAUNA, JERZMANICE ZDRÓJ

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Fig. 4. Foraminifers, gas tro pod and inoceramids from Jerzmanice Zdrój. (A–C) Foraminifer Gavelinella moniliformis Reuss, 1845; (D, E) Foraminifer Globotruncana bulloides Vögler, 1941; (F) Foraminifer Heteroxelix striata Ehrenberg, 1840; (G) Gas tro pod in a thin sec - tion; (H, I) Inoceramid Cremnoceramus deformis erec tus Meek, 1877 (MGU.Wr – 5442s); (J, K) Inoceramid Cremnoceramus waltersdorfensis waltersdorfensis Andert, 1911 (MGU.Wr – 5443s). In A–G the photo height is 2 mm.

1998 Cremnoceramus deformis erec tus Meek, 1877;

Walaszczyk & Wood; p. 415–416; Pl. 5, fig. 14; Pl.

6, figs 1–6, 8; Pls 7–8; Pl. 9, figs 1, 3–6; Pl. 10, figs 1–4, 6; Pl. 11, figs 1, 3, 5–7; Pl. 13, fig. 1; Pl. 15, fig. 6.

2004 Cremnoceramus deformis erec tus Meek, 1877; Wood et al.; Pl. 3, figs 6, 10.

2004 Cremnoceramus deformis erec tus Meek, 1877;

Walaszczyk et al.; fig. 4.7.

Ma te rial: One spec i men of a sin gle shell, ven tral part dam - aged.

De scrip tion: Very con vex, av er age size, strong beak. Beak an gle 125°. Ax ial length can not be es tab lished be cause shell is bro ken. Sec ond ary axis is 2.2 cm. An te rior mar gin is about 1 cm, slightly con vex. Pre served ven tral mar gin is gently rounded. Hinge line not eas ily vis i ble. Or na men ta - tion of the shell con sists of con cen tric and reg u lar rugae (lines and ribs). The spec i men does not dif fer from sim i lar spec i mens de scribed by Walaszczyk & Wood (1998) and Wood et al. (2004).

Oc cur rence: In the Lower Coniacian, the Rakowice Wiel- kie For ma tion, at Jerzmanice Zdrój (North Sudetic Ba sin).

Cremnoceramus deformis erec tus Meek is known from the Lower Coniacian of Eu rope, North Amer ica, and Ja pan (Walaszczyk & Wood, 1998). Wood et al. (2004), Walasz- czyk et al. (2004) re ported C. deformis erec tus from the low - er most Coniacian of Eng land and Rus sia.

Cremnoceramus waltersdorfensis waltersdorfensis Andert, 1911

Fig. 4J, K MGU.Wr – 5443s

1991 Inoceramus waltersdorfensis waltersdorfensis Andert, 1911; Tarkowski, p. 117–118, Tab. 16.4.

1992 Cremnoceramus waltersdorfensis Andert, 1911;

Walaszczyk, p. 41–46, Pls 16–17, Pl. 18, figs 1–3.

1998 Cremnoceramus waltersdorfensis waltersdorfensis Andert, 1911; Walaszczyk & Wood, p. 413–414; Pl.

5, figs. 1, 3–7, 9–13, 15–18; Pl. 15, figs 1–3; Pl. 17, fig.

3.

2004 Cremnoceramus waltersdorfensis waltersdorfensis Andert, 1911; Walaszczyk et al.; fig. 4.4, fig. 5.1–2, 4–5, 7.

2004 Cremnoceramus waltersdorfensis waltersdorfensis Andert, 1911; Wood et al., Pl. 3, figs. 1–5, 7–9, 11–14.

Ma te rial: Sin gle spec i men, sin gle shell.

De scrip tion: Shell slightly con vex, mod er ate in size, elon - gated. Ax ial length is 3.5 cm, the sec ond ary axis is 2.7 cm.

Beak an gle is 105°. Flat umbo, in dis tinct beak. Or na men ta - tion de vel oped as del i cate growth lines.

Oc cur rence: In the Lower Coniacian Rakowice Wielkie For ma tion in Jerzmanice Zdrój (North Sudetic Ba sin).

Tarkowski (1991) de scribed spec i mens of this spe cies from the Up per Turonian and Lower Coniacian in the Opole re - gion where they oc cur in de pos its of the same age as in Ger - many and Rus sia. Ac cord ing to Walaszczyk (1992) and Walaszczyk & Wood (1998), in the up per most Turonian–

Lower Coniacian (Cremnoceramus waltersdorfensis Zone–

Cremnoceramus hannovrensis Zone), known from Eu rope, west ern Asia and North Amer ica. Cremnoceramus walters-

dorfensis is most abun dant in the Lower Coniacian of Europe (Walaszczyk, 1992; Walaszczyk & Wood, 1998). It is also known from the up per most Turonian and Conia- cian of Rus sia and Eng land (Walaszczyk et al., 2004; Wood et al., 2004).

Ge nus Inoceramus Sowerby, 1814 Inoceramus latus Mantell, 1822

Fig. 5A MGU.Wr – 5444s

1912-13 Inoceramus latus Sowerby, 1812-26; Scupin, Tab.

XI, figs 5–6.

1991 Inoceramus latus Mantell, 1822; Tarkowski, p.112–113, Tab. 10.3.

Ma te rial: One spec i men, in di vid ual shell.

De scrip tion: Av er age size. Ax ial length is 1.8 cm; sec ond - ary axis is 1.6 cm. Length of an te rior mar gin about 1 cm.

The shell is slightly con vex with a sharp beak. Beak an gle is 110°. Poorly pre served del i cate growth lines are more con - spic u ous on its ven tral part. This spec i men is very sim i lar to one de scribed by Scupin (1912–13).

Oc cur rence: In the Lower Coniacian Rakowice Wielkie For ma tion in Jerzmanice Zdrój, North Sudetic Ba sin (Scupin, 1912–13). Tarkowski (1991) re ported I. latus from the Mid dle Turonian of the Opole Trough and quoted the oc cur rence of sim i lar spec i mens from the Up per Turonian of Great Brit ain, Ger many and Rus sia, as well as from the Coniacian of the Intra-Sudetic Ba sin.

Inoceramus lusatiae Andert, 1911 Fig. 5B–D

MGU.Wr – 5445s and MGU.Wr – 5446s

1934 Inoceramus lusatiae Andert, 1911; Andert; p.

126–128; fig. 14a, b.

1988 Inoceramus lusatiae Andert, 1911; Walaszczyk; Pl.

5.8.

1991 Inoceramus lusatiae Andert, 1911; Tarkowski, p.113; Tab 7.4.

1992 Inoceramus lusatiae Andert, 1911; Walaszczyk; Pl.

27.1–6.

1998 Inoceramus lusatiae Andert, 1911; Walaszczyk &

Wood; p. 421–424; Pl. I, figs 9–13; Pl. II, figs 1–4; Pl.

3, figs 1, 3–6.

1998 Inoceramus (Inoceramus) lusatiae Andert, 1911;

Noda & Matsumoto; Pl. 4, figs 1–4.

2004 Inoceramus lusatiae Andert, 1911; Wood et al.; Pl. 1, figs 7–8.

2004 Inoceramus lusatiae Andert, 1911; Walaszczyk et al.;

fig. 1.1, 3, 5; fig. 2.1, 3, 8.

Ma te rial: Two in di vid ual shells.

De scrip tion: Me dium-sized, slightly con vex. Beak an gle of 87°. Ax ial length is 3.6 cm; the sec ond ary axis can not be mea sured be cause the shell is bro ken. An te rior mar gin straight, about 1.5 cm in length, pass ing into well rounded ventroanterior mar gin, which is slightly dam aged. Or na - men ta tion oc curs in the pat tern of del i cate, dense growth lines.

Oc cur rence: Re ported from the Lower Coniacian Rako- wice Wielkie For ma tion in the Jerzmanice Zdrój area

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Fig. 5. Inoceramids and other bi valves from Jerzmanice Zdrój. (A) Inoceramid Inoceramus latus Mantell, 1822 (MGU.Wr – 5444s); (B, C) Inoceramid Inoceramus lusatiae Andert,1911 (MGU.Wr – 5445s); (D) Inoceramid Inoceramus lusatiae Andert,1911 (MGU.Wr – 5446s; (E, F) Inoceramid Inoceramus sp. (MGU.Wr – 5447s); (G, H) Bi valve Anatina (Cercomya) lanceolata Geinitz, 1871–1875 (MGU.Wr – 5448s; MGU.Wr – 5449s).

(North Sudetic Ba sin). Ac cord ing to Tarkowski (1991) I.

lusatiae oc curs in the Up per Turonian of the Opole Re - gion. It has also been found in the fol low ing coun tries: in the Mid dle and Up per Turonian of France and NW Ger - many; in the Up per Turonian of the Czech Re pub lic, Ger - many (Sax ony), Rus sia, and the United States; and in the Up per Turonian and Coniacian of Rus sia (Tarkowski 1991). Walaszczyk & Wood (1998) de scribed spec i mens of I. lusatiae from the up per most Turonian (Mytiloides scu- pini–Cremnoceramus waltersdorfensis Zones) to the low er - most Coniacian (Cremnoceramus erec tus Zone) of Cen tral Eu rope. Wood et al. (2004) re ported I. lusatiae from the higher part of the Up per Turonian of Eng land, whereas Walaszczyk et al. (2004) re ported it from the up per most Turonian and the Lower Coniacian of Rus sia. Noda &

Matsomoto (1998) de scribed I. lusatiae from the up per most Turonian to Lower Coniacian of Ja pan.

Inoceramus sp.

Fig. 5E, F MGU.Wr – 5447s

Ma te rial: One dou ble-valved spec i men.

De scrip tion: The whole shell is pre served. The umbo can - not be seen. The shell is smooth with lit tle or na men ta tion.

Only del i cate growth lines are vis i ble. Ax ial length is 3.4 cm; the sec ond axis 2.6 cm. Shell thick ness nearly 2 cm.

Shape and ap pear ance sug gests that it be longs to Inocera- mus; how ever, the poorly pre served top does not al low for pre cise clas si fi ca tion.

Oc cur rence: In the Lower Coniacian, the Rakowice Wielkie For ma tion in the Jerzmanice Zdrój area (North Sudetic Ba sin).

Class: Chondrichthyes Huxley, 1880 Sub class: Elasmobranchii Bonaparte, 1838

Co hort: Euselachii Hay, 1902 Subcohort: Neoselacheii Compagno, 1977

Superorder: Squalomorphi Buen, 1926 Or der: Lamniformes Berg, 1958 Fam ily: Cretoxyrhinidae Glückman, 1958

?Cretoxyrhina mantelli Agassiz, 1843 Fig. 7H

MGU.Wr – 5466s

Ma te rial: One root less tooth.

De scrip tion: The tooth is rel a tively tall and nar row, blade flat and smooth. It does not dif fer sig nif i cantly from the teeth de scribed by Wil liam son et al., (1993) and Cicimurri (2001a, b). The shape sug gests an af fin ity to the Creto- xyrhinidae fam ily, most prob a bly ?Cretoxyrhina mantelli Agassiz, 1843. The spec i men is 1.5 cm long and 0.5 cm wide.

Oc cur rence: Lower Coniacian of the Jerzmanice Zdrój area (North Sudetic Ba sin). If this tooth is of Cretoxyrhina mantelli, then it is of a spe cies that has been pre vi ously de -

scribed by Scupin (1912–13) and Kühn & Zimmerman (1919) from older (Cenomanian–Turonian) de pos its of the North Sudetic Ba sin. NiedŸwiedzki & Kalina (2003) and NiedŸwiedzki (2004) re ported Cretoxyrhinidae teeth from the Turonian of the Opole re gion. Ac cord ing to Cappetta (1987) and Mustafa (2000), Cretoxyrhina mantelli Agassiz, 1843 is the most wide spread spe cies of this shark fam ily, ap pear ing in Cenomanian–Santonian sed i ments of Eu - rope, North and South Amer ica, Mad a gas car and Rus sia.

C. mantelli is pres ent in the Up per Santonian of Jor dan (Mustafa, 2000). Sim i lar teeth were ob served by Cicimurri (2001a, b; 2004) in the Lower Cenomanian and Mid dle Turonian of the United States (Black Hills Re gion of South Da kota and Wy o ming). Willamson et al. (1993) de scribed C. mantelli from the Up per Cenomanian to Lower Turonian of Ar i zona, Ne braska, Texas, Great Brit ain, Bel - gium, and Lith u a nia. Ac cord ing to Wil liam son et al.

(1993), this taxon was also re ported from the Coniacian of Can ada. Radwañski and Marcinowski (1996) found C.

mantelli in the Up per Turonian and Coniacian of the Mangyshlak Moun tains, West ern Kazakhstan.

Al though Cappetta (1987) sug gested that C. mantelli did not sur vive into the Campanian, Thies & Müller (1993) re - ported the pres ence of this spe cies from the Lower Cam- panian of the Aachen area at the Ger man–Bel gian bor der, and Mustafa (2000) states that this spe cies was founf and de - scribed from the Campanian of Swe den.

In ad di tion to the newly de scribed inoceramid and ver te brate re mains, the Lower Coniacian marly sand - stones of the Jerzmanice Zdrój sec tion also con tain foraminifera and bi valves (see also Gawor-Biedowa, 1980;

Teisseyre, 1992; Scupin, 1912–1913). Thin sec tion ob ser va - tions from this study re vealed the fol low ing foraminifera:

Ammodiscus cre ta ceous, Reuss, 1845 (Fig. 3B–D), Gaudry- ina laevigata, Franke, 1914 (Fig. 3E), Gavelinella ammono- ides, Reuss, 1845 (Fig. 3F, G), Gavelinella moniliformis, Reuss, 1845 (Fig. 4A–C), Globotruncana bulloides, Vögler, 1941 (Fig. 4D, E), Heterohelix striata, Ehrenberg, 1840 (Fig. 4F).

The bi valves re cog nised in the Jerzmanice Zdrój sec - tion (Tab. 1) are as fol lows: Anatina (Cercomya) lanceolata Geinitz, 1871–75 (Figs 5G, H, 6A); Crasatella arcaea Roemer, 1841 (Fig. 6B, C); Cucullaea sp. (Fig. 6D, E);

Cytherea sp. (Fig. 6F); Granocardium cf. drescheri Böhm, 1911 (Fig. 6G–I); ?Lima haidingeri Zittel, 1878 (Fig. 7A);

Ostrea (Alectryonia) sudetica Scupin, 1912–13 (Fig. 7B);

Panopea depressa Scupin, 1912–13 (Fig. 7C); Panopea muel- leri Scupin, 1912–13 (Fig. 7D); Tellina strigata Goldfuss, 1834–40 (Fig. 7E, F). The ma jor ity of these taxa were de - scribed by Scupin (1912–13) from other out crops of the Lower Coniacian in the North Sudetic Ba sin. Also from the Jerzmanice Zdrój sec tion are sin gle gas tro pod re mains (Fig. 4G; Tab. 2) and a sin gle prob a ble frag ment of ammonite (Fig. 7G).

LOWER CONIACIAN FAUNA, JERZMANICE ZDRÓJ

43

Fig. 6. Bi valves from Jerzmanice Zdrój. (A) Anatina (Cercomya) lanceolata Geinitz, 1871–1875 (MGU.Wr – 5450s); (B, C) Crasatella arcacea Roemer, 1841 (MGU.Wr – 5451s; 5452s); (D, E) Cucullaea sp. (MGU.Wr – 5453s; MGU.Wr – 5454s); (F) Cytherea sp.

(MGU.Wr – 5455s); (G–I) Granocardium cf. dresecheri Böhm, 1911 (MGU.Wr – 5456s; MGU.Wr – 5457s; MGU.Wr – 5458s).

Fig. 7. Bi valves and other fos sils from Jerzmanice Zdrój. (A) ?Lima haidingeri Zittel, 1865 (MGU.Wr – 5459s); (B) Ostrea (Alectryonia) sudetica Scupin, 1912–1913 (MGU.Wr – 5460s); (C) Panopea depressa Scupin, 1912–1913 (MGU.Wr – 5461s); (D) Panopea muelleri Scupin,1912–1913 (MGU.Wr – 5462s); (E, F) Tellina strigata Goldfuss,1834–1840 (MGU.Wr – 5463s; MGU.Wr – 5464s); (G) A frag - ment of ammonite (MGU.Wr – 5465s); (H) Shark tooth ?Cretoxyrhina mantelli Agassiz, 1843 (MGU.Wr – 5466s).

AGE AS SIGN MENT OF THE JERZMANICE ZDRÓJ SEC TION

The fol low ing inoceramids have been re cog nised by Scupin (1912–13), Walaszczyk (1992) and Walaszczyk &

Wood (1998) as typ i cal for the low est part of the Lower Coniacian: Inoceramus lusatiae Andert, 1911; Cremno- ceramus waltersdorfensis waltersdorfensis Andert, 1911;

Cremnoceramus deformis erec tus Meek, 1877; Inoceramus (Cr.) rotundatus Fiege, 1930; C. websteri Mantell, 1822; I.

hoepeni Heinz, 1933 and I. latus Mantell, 1822.

Among the inoceramids de scribed in the pres ent study (Tab. 1), Cremnoceramus deformis erec tus Meek is known only from the Lower Coniacian, and Cremnocera- mus waltersdorfensis waltersdorfensis Andert only from the Lower and Mid dle Coniacian. Inoceramus lusatiae Andert and I. latus Mantell have a slightly broader strati graphic range, from the Mid dle Turonian to the low est Coniacian.

The inoceramid as sem blage of the Jerzmanice Zdrój sec - tion con firms an Early Coniacian age for the marly sand - stone (Tab. 1) and in di cates de po si tion dur ing the Crem- noceramus deformis erec tus Zone (Walaszczyk, 1992;

Walaszczyk & Wood, 1998). The foraminiferal as sem blage is also typ i cal for the Lower Coniacian (Tab. 2). The marly sand stone may be long to the Gavinella monilifor- mis Zone of the up per most Lower Turonian–Lower Coniacian, re cog nised from the North Sudetic Ba sin by Teisseyre (1992). The strata prob a bly cor re late with the Stensioina exsculpta exsculpta Zone (up per part of the Early Turonian un til Early Coniacian ) of the Intra-Sudetic Ba - sin. Their equiv a lent in the Nysa K³odzka Graben is the Epistomina spinulifera polypioides Zone from the up per - most part of the Up per Turonian and Lower Coniacian (Gawor-Biedowa, 1980). Ac cord ing to Witwicka (1958), the bound ary be tween Turonian and Coniacian is marked by the ap pear ance of Stensioina exsculpta in the Nysa Trough. How ever, Stensioina was not found in the North Sudetic Ba sin, ei ther by Teisseyre (1992) or the present author.

Iden ti fy ing the bound ary be tween Turonian and Co- niacian sed i ments in the North Sudetic Ba sin is a com plex

prob lem and will re quire fur ther in ves ti ga tions. The pre - vi ous inoceramid zonation schemes (Mitura et al., 1969;

Milewicz, 1979) placed the Inoceramus schloenbachi Zone as the up per most Up per Turonian. Mod ern biostra- tigraphy, how ever, con sid ers Inoceramus schloenbachi Böhm, 1911 as a syn onym of Cremnoceramus crassus crassus Petrascheck, 1903: this sug gests the up per part of the Lower Coniacian.

The lit er a ture to date on the Late Cre ta ceous stra tig ra - phy of the North Sudetic Synclinorium leaves many ques - tions still open. Al though Inoceramus schloenbachi Böhm has been most of ten as cribed to the Up per Turonian (Milewicz 1970; 1971; 1979; 1988; 1997; Mitura et al., 1969), it is re garded as Coniacian by Milewicz (1967). And de spite I. schloenbachi be ing found in the Coniacian of the Nysa K³odzka Graben (Radwañska 1962), Mitura et al.

(1969) claim that it was re de pos ited from the Turonian.

The inoceramids found by Scupin (1912–13) and Milewicz (1958, 1966, 1970, 1997) in the Coniacian sed i - ments of the North Sudetic Ba sin – Inoceramus kleini Müller, 1887, I. koeneni Müller, 1887, I. rotundatus Fiege, 1930, I. involutus Sowerby 1812-26, I. percostatus Müller, 1887, I. lusatiae Andert, 1911; I. crassus Petrascheck, 1903, I. latus Sowerby, 1812–26 – sug gest an Early to Mid dle Coniacian age. Milewicz (1997) placed the Lower Conia- cian inoceramids into the Inoceramus rotundatus Zone of Keller (1982).

Based on the fos sil anal y ses in this pa per, the Jerzma- nice Zdrój marly sand stones can be placed into the Crem- noceramus deformis erec tus Zone, which is Lower Conia- cian. As the base of Emscherian is not syn chro nous with the base of Coniacian, and Inoceramus schloenbachi Böhm, 1911 (ac tu ally Cremnoceramus crassus crassus Petrascheck, 1903) sig ni fies the up per part of the Lower Coniacian, and the Turonian–Coniacian bound ary in the North Sudetic Ba sin should now be placed be tween the Inoceramus costellatus Zone and the Inoceramus schloenbachi Zone, as de fined by Milewicz (1979) (Tab. 3).

SED I MEN TARY EN VI RON MENT

The East and West Sudetic is lands in the Late Cre ta - ceous sea of the North Sudetic Ba sin con sti tuted a source area for the Coniacian sand stones of the Jerzmanice Zdrój area. These is lands were of gran ite, gneiss es and other meta mor phic rocks (Radwañski, 1968; Milewicz, 1998).

The East-Sudetic Is land had al ready ap peared in the Early Turonian (Biernacka & Józefiak, 2008) and by the Early Coniacian this is land sep a rated the Nysa K³odzka Graben from the Opole Ba sin (Kêdzierski, 2005).

Thin sec tion ob ser va tions of the Jerzmanice Zdrój Coniacian marly sand stones and sandy lime stone in ter ca - la tions re veal a pau city of feld spars and the pres ence of an - gu lar and subangular to subrounded quartz grains: a short trans por ta tion dis tance is implied.

The inoceramid-dom i nated fos sil as sem blage, and prob a ble ammonite prescence, sug gests some deep en ing of the North Sudetic Sea dur ing the Early Coniacian. The fos sil tooth of a shark from the fam ily Cretoxyrhinidae (?Cretoxyrhina mantelli) sug gests that C. mantelli was large: this is be cause carcharhinid sharks are con sid ered as the mod ern guild coun ter parts for C. mantelli (Shimada, 1997), and this guild in cludes the mod ern Carcharodon carcharias (great white shark), which can be up to 6 m in length. Pe lagic lamniformes like Cretoxyrhina mantelli were ac tive pred a tors feed ing on fast-swim ming fish and rep tiles (Shimada, 1997; NiedŸwiedzki & Kalina, 2003).

The pres ence of C. mantelli in the Coniacian sand stones in Jerzmanice Zdrój is sig nif i cant be cause teeth of this spe cies

LOWER CONIACIAN FAUNA, JERZMANICE ZDRÓJ

45

are found mainly in a deep-wa ter palaeoenvironment and are ab sent, or only rarely oc cur, in near-shore de pos its (NiedŸwiedzki & Kalina, 2003). Nev er the less, Cicimurri (2001a, b; 2004) has de scribed C. mantelli teeth from a shal low ma rine en vi ron ment in the United States (South

Da kota, Wy o ming), but even he claimed that this shark pre ferred off-shore hab i tats. Thus, it seems quite prob a ble that the epicontinental Early Coniacian sea was deep enough for sharks to reach the North Sudetic Basin.

PALAEO GE OGRA PHY

Dur ing the Late Cre ta ceous, the North Sudetic Ba sin be longed to the set of Circum-Sudetic Trap Bas ins to - gether with the Opole Ba sin, Saxonian Ba sin and North Bo he mian Ba sin (Walaszczyk, 1992). Lithostratigraphic and palaeogeographic stud ies sug gest that these bas ins, in - clud ing the Intra-Sudetic Ba sin, must all have been in ter - con nected (e.g. Radwañski, 1966, 1968; Jerzykiewicz, 1971, 1975; Gawor-Biedowa, 1980; Teisseyre, 1992; Mile- wicz, 1997; Wojewoda, 1997; Kêdzierski 2005; Biernacka

& Józefiak, 2008).

The Cre ta ceous ma rine sed i ments in the North Sude- tic Ba sin and the ad ja cent bas ins re cord an Early Turonian and a Late Turonian–Early Coniacian trans gres sion max - ima (Gawor-Biedowa, 1980; Jaskowiak-Schoeneichowa &

Krassowska, 1988; Teisseyre, 1992; Jubitz (1995); Mile- wicz, 1997; Wojewoda, 1997; Rotnicka, 2007).

Pre vi ous stud ies on the Opole Ba sin sug gested that there was only one trans gres sion, ei ther in the Mid dle Turonian (Alexandrowicz, 1974) or in the Late Turonian (Tarkowski, 1991). How ever, trace-fos sil ev i dence proved that there had been two ep i sodes of sea-deep en ing, one in

the Mid dle Turonian and one from the Late Turonian to the Early Coniacian (Kêdzierski & Uchman, 2001). The Mid dle Turonian trans gres sion is fur ther sup ported by ev - i dence of deep-wa ter sharks’ teeth (NiedŸwiedzki &

Kalina, 2003).

As had hap pened dur ing the Turonian, the ma rine trans gres sion reached an other max i mum in the Sudetes dur ing the Early Coniacian. Ac cord ing to Wojewoda (1997), Jerzykiewicz (1971, 1975) and Don & Gotowa³a (2008), from the up per most Late Turonian on wards, the palaeodepth in creased sig nif i cantly in the Nysa K³odzka Graben. NiedŸwiedzki & Salamon (2005) also be lieve that the max i mum trans gres sion in the Nysa K³odzka Graben oc curred in the Early Coniacian (Cremnoceramus deformis erec tus Zone–Cremnoceramus crassus crassus Zone). Teisse- yre (1992) and Milewicz (1997) came to the con clu sion that the North Sudetic sea deep ened in the Early Conia- cian and be came con nected with the Intra-Sudetic Ba sin (Don & Gotowa³a, 2008). Sim i larly, Jubitz (1995) sug - gested that in Brandenburg (Ger many), the transgressive peak took place dur ing the Early Coniacian, whereas in Ta ble 3 Strati graphic di vi sion of the Turonian and Coniacian in the North Sudetic Ba sin

the Bo he mian Mas sif the peak oc curred dur ing the mid dle Late Turonian (Skoèek & Valeèka, 1983).

Kêdzierski & Uchman (2001) cor re lated the Late Cre - ta ceous trans gres sion cy cles in the Opole Ba sin with the more gen eral Eu ro pean bathymetric curve of Haq et al.

(1987). The transgressive–re gres sive cy cles of the Cre ta - ceous North Sudetic Sea also agree with the bathymetric

curves of Haq et al. (1987) and Han cock (1990). Han cock (1990), how ever, pro posed that the two trans gres sion max - ima were al most equally im por tant. But in the North Sudetic and ad ja cent bas ins, the Late Turonian–Early Coniacian peak was more pro nounced, which is in line with the curve of Haq et al. (1987).

SUM MARY AND CON CLU SIONS

The marly sand stones and their sandy lime stone in ter - ca la tions, ex posed in the Jerzmanice Zdrój area, pos sess petrographic fea tures that in di cate a prox i mal source area, prob a bly from the West-Sudetic and East-Sudetic Is lands of the Late Cre ta ceous North Sudetic Sea. Sed i men ta tion took place in an epicontinental ba sin, the North Sudetic Ba sin, which must have been deep enough to en cour age the shark Cretoxyrhina mantelli to live there dur ing the Early Coniacian. In the Early Coniacian, as had hap pened pre vi ously dur ing the Early Turonian, the sea reached its max i mum transgressive ex tent in the Sudetes. In the North Sudetic Ba sin and ad ja cent ar eas, the Late Turo- nian–Early Coniacian trans gres sion was more pro noun- ced, a fea ture which cor re sponds with the global bathy- met ric curve for the Late Cre ta ceous pro posed by Haq et al. (1987).

Nei ther the sharks nor most of the bi valves and inoceramid taxa de scribed in this pa per were pre vi ously known from the Lower Coniacian rocks (Emscherian, af - ter Scupin (1912–13)) in the North Sudetic Synclinorium.

The inoceramids and foraminifers con firm an Early Co- niacian age for the Jerzmanice Zdrój sand stones (Cremno- ceramus deformis erec tus Zone; Gavelinella moniliformnis Zone). The new find ings, when al lied to the strati graphic scheme of Milewicz (1979), im ply that the Turonian–

Coniacian bound ary in the North Sudetic Ba sin should now be placed be tween the Inoceramus costellatus Zone and the Inoceramus schloenbachi Zone.

Ac knowl edge ments

The au thor would like to thank Pawe³ Raczyñski for pho to - graph ing the spec i mens, Rob ert NiedŸwiedzki for pro vid ing the lit er a ture on ver te brates, and Joanna Kostylew and Marek Awdankiewicz for petrographic con sul ta tions. Un der the su per - vi sion of the au thor, MSc stu dent Wojciech Krupa col lected a num ber of the fos sils used in this pa per. The au thor ex tends par - tic u lar thanks to Mariusz Kêdzierski for his care ful and in sight ful re view. Pat rick Roycroft and Andrzej ¯elaŸniewicz are thank - fully ac knowl edged for me tic u lous ed i to rial work.

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