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Print This Article Trace fossils from the Lower Jurassic Ciechocinek Formation, SW Poland 89 Trace fossils from the Lower Jurassic Ciechocinek F ormation, SW Poland Paulina LEONOWICZ Institute of Geology, University of Warsaw, ul. ˚wirki i Wigury 93, PL-02089 Warszawa, Poland; e-mail: [email protected] Key -words: trace fossils, fine-grained clastics, brackish environment, Lower Jurassic, Cz´stochowa-Wieluƒ region. ABSTRACT: Mud-silt deposits of the Lower Jurassic Ciechocinek Formation from the Cz´stochowa-Wieluƒ region are characterized by a low diversity ichnofossil association, which includes the ichnogenera Planolites , Palaeophycus , Helminthopsis , Gyrochorte , Protovirgularia and Spongeliomorpha as well as some unidentified pascichnia. This association points to deposition in a low-energy brackish environment with poorly oxygenated sediments. Changes of seafloor oxygenation, influenced by periodical bottom currents, resulted in various bioturbation intensities, which range from none to high. INTRODUCTION and Leonowicz 2002) and geochemical study of siderites (Leonowicz 2007). In the absence of body During the Early Jurassic the territory of Poland fossils, trace fossils are the most useful tool in was situated in a marginal part of the extensive, environmental interpretations. They are quite epicontinental Central European Basin (Fig. 1: A), common in the Ciechocinek Formation and include which was particularly sensitive to sea-level Diplocraterion parallelum Torell as well as fluctuations, causing frequent displacements of the some other non-identified fodinichnia, repichnia, shoreline and changes of sedimentary environment. domichnia and cubichnia (Pieƒkowski 1988, 2004). The Ciechocinek Formation marks the maximum However, more detailed analysis of the ichnofossil extent of marine sedimentation in Poland, related association was not carried out till now. by Dadlez (1969) and Pieƒkowski (2004) to the The purpose of this paper is to analyse the trace Early Toarcian transgression, which is recorded in fossil association from the Ciechocinek Formation the whole Central European Sea. Fauna in these deposits in the Cz´stochowa – Wielu ƒ region deposits is uncommon and of low diversity. It (Fig. 1: B) in order to determine bottom conditions includes phyllopods, ostracods, scarce foraminifers in the sedimentary basin. Observations of the type and occasional fragments of bivalves, gastropods and distribution of trace fossils were made in and fish teeth (Kopik and Marcinkiewicz 1997; successions cropping out in two clay-pits, which Kopik 1998). The lack of typical marine fauna belong to the “Cerpol-Koz∏owice” Enterprise and indicates that the transgression did not cause the “Boroszów” Brickyard, as well as during development of normal-marine conditions in the examination of cores from 16 boreholes drilled by Polish Basin. Such a conclusion is also confirmed by the Polish Geological Institute. Fresh, unpolished analysis of the dinoflagellate assemblage (Barski surfaces of rocks were observed. In order to reco- 90 Volumina Jurassica, Volumen VI B A WIERUSZÓW WIELU¡ 0 500 km 36 1 12 inferred maximum range PRASZKA of the Lower Jurassic deposits Cretaceous location of the studied area 41 Upper Jurassic 40 16 Kozłowice 49 15 KRZEPICE Middle Jurassic KLUCZBORK Boroszów 50 KŁOBUCK Lower Jurassic 2 Przystajƒ OLESNO 21 Triassic 20 46 45 3 outcrops 25 boreholes CZ¢STOCHOWA profiles presented 0 10 20 km on Fig. 4 Fig. 1. Location of the studied area : A – Polish Basin as a part of the Central European Basin in the Early Jurassic time (after Pieƒkowski 2004); B – location of studied profiles on a geological sketch-map of the Cz´stochowa-Wieluƒ region. gnize the fabric of massive deposits, thin sections, gellate cysts, the deposits of the Ciechocinek made from well consolidated mudstones and Formation were dated to the Margaritatus – siltstones, were examined under the microscope. Tenuicostatum zones (Barski and Leonowicz 2002). Pieƒkowski (2004) placed it within the Lower Toarcian, on the basis of sequence stratigraphy GEOLOGICAL SETTING correlation and the results of macrospore analysis by Marcinkiewicz (1957, 1960, 1964, 1971). He noted The Ciechocinek Formation represents a mud- there one find of Diplocraterion (Nowa WieÊ 12 silt succession (Fig. 2) consisting of poorly borehole) and some, locally common, non-identified consolidated, grey, olive and willow-green mud- trace fossils of fodinichnia and repichnia. stones and siltstones with lenses and subordinate intercalations of sands and sandstones (Teofilak- Maliszewska 1967, 1968; Leonowicz 2005). Up to several centimeter thick lenses and intercalations of siderite as well as small siderite and pyrite concretions are common. In all types of deposits fine plant detritus as well as larger, several centimeter long wood fragments occur. In the area studied the Ciechocinek Formation overlies sand-mud deposits of the Blanowice Formation and is overlain by the similarly developed Borucice Formation (Fig. 3), both of alluvial and lacustrine origin (Pieƒkowski 2004). Depending on the section, boundaries between 5 cm formations are distinct, confined by erosional Fig. 2. Deposits of the Ciechocinek Formation from the Koz∏owice surfaces or gradual, marking continuous changes clay-pit: intercalations of massive muds, lenticular-bedded muds and of sedimentary environment. Based on dinofla- interlaid mud-sand heteroliths. Trace fossils from the Lower Jurassic Ciechocinek Formation, SW Poland 91 ICHNOLOGY OF THE CIECHOCINEK FORMATION Palaeophycus is less common than Planolites in deposits of the Ciechocinek Formation; however, Trace fossil association is not diverse and in the Koz∏owice outcrop numerous specimens includes Planolites , Palaeophycus , Helmintho- occur. It is interpreted as the result of passive filling psis , Gyrochorte , Protovirgularia and Spon- of polychaete burrows (Pemberton and Frey 1982). geliomorpha as well as many small, undetermined It is a facies-crossing, eurybathic form, known from trace fossils, most probably of the pascichnia deep-marine flysch and brackish-marine deposits category. Trace fossils are preserved in mud-silt as well as from the fresh-water environments deposits as endichnia and in sandstone lenses as hypichnia. Thicker, poorly consolidated sandy Chrono- layers are devoid of bioturbational structures. Lithostratigraphy stratigraphy Wr´czyca 3 c i e l Lower s d Planolites isp. (Fig. 5: A-F) s [m] a d Bajocian KoÊcielisko Beds i r u M Aalenian J DESCRIPTION : Unlined and unbranched, r e Połomia Borucice straight, curved or tortuous trace fossils, p p Beds Formation cylindrical or elliptical in cross-section, usually U n a from fraction to 2 mm in diameter, variably oriented i c r to the bedding. Less common are thicker forms, a o r T reaching up to 7 mm in diameter, usually horizontal e Ciechocinek w o Formation or subhorizontal and gently curved. Filling of L burrows is structureless, differing in grain size and/or colour from the host rock, locally pyritized. r Planolites is preserved as full relief in mud-silt e p n p a i deposits or on sole surfaces of sandstones. U c h i c s REMARKS: The size and curvature suggest that a Blanowice s b 100 a Formation s r most of the specimens observed should be assigned n r u e e i J l to Planolites montanus Richter (Fig. 5: C, D, F). w P r o L Larger forms may belong to Planolites e w beverleyensis Billings (Fig. 5: E). Planolites is o L r e common in all types of the Ciechocinek Formation n p a p ? i r deposit. It is referred to vermiform deposit-feeders, U Zagaje Fm. u mainly polychaetes, producing active backfilling m e r e n i (Pemberton and Frey 1982). Planolites is a facies- w S o crossing, eurybathic form, known from shallow L hiatus marine and deep-marine flysch deposits as well as r e p n e.g. p from fresh-water environments ( Ksià˝kiewicz a i U g 1977; Pieƒkowski 1985; Bjerstedt 1987; Beynon and n ? a t r Zagaje Fm. t Pemberton 1992; Pemberton and Wightman 1992; e e w H Buatois and Mángano 1998; Fürsich 1998). o L c i Palaeophycus isp. (Fig. 5: G) s 150 s Rhaetian Wielichowo Beds a i m sf r st sm DESCRIPTION : Straight or gently curved, T thin intercalations predominantly horizontally oriented, unbranched, gravel smooth or rarely faintly ornamented cylindrical of silt (-stone) and mud (-stone) trace fossils up to 10 mm in diameter, slightly sand (-stone) flattened in cross-section. Filling structureless, silt (-stone) grain size: m - mud, m sf st - silt, s - sand st sm of the same lithology as the host rock. Preserved mud (-stone) (f - fine, m - medium) on sole surfaces of sandstones. REMARKS: The lack of thick lining and distinct Fig. 3. Lithostratigraphy of the Lower Jurassic in the Cracow-Silesian region (after Kopik 1998; Pieƒkowski 2004; Deczkowski and Daniec ornamentation suggests that most of the specimens 1981) and the representative lithological profile of the borehole observed represent Palaeophycus tubularis Hall. Wr´czyca 3 (after Leonowicz 2007). 92 Volumina Jurassica, Volumen VI priapulids. Helminthopsis is a facies- Planolites Nowa WieÊ 12 crossing, eurybathic form, known from Palaeophycus [m] 0 Helminthopsis deep-marine flysch to brackish-marine n o i t Gyrochorte deposits as well as from the fresh-water a m Protovirgularia environments ( e.g. Ksià˝kiewicz 1977; r o F Spongeliomorpha Bjerstedt 1987; Beynon and Pemberton e c i Diplocraterion c 1992; Buatois and Mángano 1998). u r data after Pieƒkowski o B (2004) Gyrochorte isp. (Fig. 6: E, F) Kozłowice DESCRIPTION : Winding, horizontal, [m] 0 double ridge separated by a median groove. The surface of ridges is smooth n or has an indistinct, plaited structure, o i t 50 a composed of biserially arranged, m r obliquely aligned pads of sediment. o 20 F k The ridges are curved or gently e n i ? c meandering; they do not branch and o h c often cross themselves. The width e i C of trace fossils changes along their axis m s and generally does not exceed 4 mm. Gyrochorte is preserved as epirelief in gravel and sandstones and mudstones.
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