Printer Friendly

A large Late Devonian arthrodire (Vertebrata, Placodermi) from Poland.


The genus Dunkleosteus (formerly Dinichthys in part) includes about eight species (if including D. belgicus (Leriche), 1931) which are found in Laurussia (USA, Canada, Belgium, Poland) and Gondwana (Morocco). The problem of the phylogenetic position of Dunkleosteus has been discussed by many authors (see comments in Carr & Hlavin 1995, 2010), but there is a general consensus about its affinities within Pachyosteomorphi Stensio, 1944 and the family Dunkleosteidae Stensio, 1944. Most of the Dunkleosteus material comprises more or less articulated skull roofs. This emblematic material is a rich collection from the Cleveland Shales Formation. In Europe, Dunkleosteus is known from the Famennian of Belgium (Leriche 1931) and Poland (Kulczycki 1957; Ivanov & Ginter 1997; Szrek 2009; Szrek & Niedzwiedzki 2015). Kulczycki (1957) described a new species of Dunkleosteus denisoni, based on a median dorsal plate from the middle Famennian of the Holy Cross Mountains. In 2009 Szrek also identified the same species from the so-called Kellwasser horizon (Plucki locality), uppermost Frasnian in age. All these specimens present typical features of this genus except for their small sizes. A similar situation concerns the nuchal plate illustrated by Ivanov & Ginter (1997, fig. 4B) from the Famennian of the Ostrowka quarry, which (although undescribed) represents a typical Dunkleosteus, but below most of Cleveland Dunkleosteus size. In the opinion of Ivanov & Ginter (1997) it resembles D. marsaisi Lehman, 1954 from the early Famennian of Morocco (Lehman 1956).

Although tens of placoderm fossil remains were collected in Plucki during long-term excavation works between 1996 and 2006 (see Szrek 2008, 2009; Szrek & Niedzwiedzki 2015; Dworczak & Szrek 2016), only few specimens have been described formally. The first data about placoderms from Plucki were presented by Ivanov & Ginter (1997) who initially described a partly preserved skull-roof of an eastmanosteid arthrodire. Later, Szrek (2007a, 2007b, 2008) and Szrek & Ginter (2008) mentioned the Plucki placoderm assemblage but the first detailed description was published by Dworczak & Szrek (2016) who described remains of Aspidichthys ingens Koenen, 1883. Most of the material is described in the unpublished PhD thesis of Szrek (2009).

The aim of the present paper is therefore to describe a new material of Dunkleosteus, initially identified by Szrek (2009), but not formally described. The material includes the largest representatives of the Polish placoderms and comprises head- and trunk-shield elements.


The source locality of the reported material is located in the Plucki village near the town of Lagow in the central part of the Holy Cross Mountains (central Poland, Fig. 1). This locality represents important strata of the Frasnian--Famennian boundary. The first report about the Plucki locality was given by Sobolev (1912) and Czarnocki (in the 1920s, general geology field notes--unpublished until 1989), followed by Makowski (1963, 1971) and Dzik (1985) who described a rich goniatite fauna within black bituminous limestone. The first published details about the section exposed in the Plucki site were due to Szulczewski (1989) who used for the first time the term 'Upper Kellwasser Limestone', labelling a black bituminous limestone horizon. Then several papers on the stratigraphy, geochemistry and palaeontology of the site were published by Bond et al. (2004), Dworczak & Szrek (2016), Dzik (2002), Filipiak (2002), Ginter (1995, 2002), House (2002), Ivanov & Ginter (1997), Racki et al. (2002), Szrek (2007a, 2007b, 2008, 2009), Szrek & Ginter (2008), Woroncowa-Marcinowska (2006) and Rakocinski et al. (2016). This locality was also a source of material for few scientific projects and MSc and PhD theses by Janiszewska (2008), Szrek (2009) and Dworczak (2016).

The section studied in the Plucki outcrop is about 5 m thick and resembles the Kellwasser-like horizon. The entirely Frasnian lower part (up to 30 cm) is characterized by marls at the bottom with limestone above. The limestone middle part (up to 10 cm) is rich in cephalopods and arthrodire placoderms. According to the detailed analysis of Janiszewska et al. (2007), the Frasnian--Famennian boundary is putatively situated within this part of the horizon. The uppermost part entirely belongs to the Famennian and is characterized by abundant invertebrate and fish material. Part of the internal structure of the Kellwasser-like horizon is characterized by the occurrence of a breccia-like structure (unpublished data by P. Szrek and S. Salwa). It is composed of few lithological components: big fragments of solid black dolomitic limestone of fossiliferous and non-fossiliferous types occur in the form of clasts and are surrounded by less-solid dark brown limestone. Bones within the horizon reflect signs of pre-fossilization damage of potential mechanic origin. It is expressed by the occurrence of broken bones surrounded by the sediment. This points to a damage before final burial.

Fossils are much less numerous or absent above the Kellwasser-like horizon. They comprise only pelagic invertebrates.


The material analysed consists of seven described specimens representing isolated parts of disarticulated head and trunk shields. The fragmentary condition of the material precludes authors to perform a cladistic analysis beyond the proposed systematic attribution.

Two accumulations of big skeletons have been ascertained within the Frasnian part of the Kellwasser-like horizon. These skeletons are disarticulated, however, it seems that they particularly represent single individuals.

The material collected comprises therefore putative associations of two individuals. Association 1 consists of the posterior part of a skull roof including the nuchal plate and partly preserved paranuchal (mostly left one) and central plates (Muz. PGI-NRI 1809.II.18, Fig. 2A--C), both partially preserved anterior dorsolateral plates (Muz. PGI-NRI 1809.II.20,21; Fig. 3A, B and the right suborbital plate (Muz. PGI-NRI 1809.II.22; Fig. 3C, D). Association 2 comprises the posterior part of a skull roof including the nuchal plate and partly preserved paranuchal and central plates (MWG UW ZI/43/0053, Fig. 4A, B), a fragment of a left central plate associated with part of the pineal plate (Muz. PGI-NRI 1809.II.23; Fig. 4C) and a median dorsal plate preserved in most of its original shape (Muz. PGI-NRI 1809.II.19, Fig. 5).

All specimens are preserved 3-dimensionally. Features of their preservation point to a pre-fossilization damage shown by the broken margins covered by the sediment. According to the recent interpretation of the origin of the Plucki section (unpublished data by P. Szrek and S. Salwa, see also Dworczak & Szrek 2016), it is likely that the bones were redeposited to their place of final burial from the shallower environment, during a slump event.

The material is housed in the Geological Museum of the Polish Geological Institute-National Research Institute, Warsaw (abbreviated Muz. PGI-NRI) and at the Faculty of Geology, University of Warsaw, Warsaw (abbreviated MWG UW).


Class PLACODERMI M'Coy, 1848 Order ARTHRODIRA Woodward, 1891 Family DUNKLEOSTEIDAE Stensio, 1963 Genus Dunkleosteus Lehman, 1956

Dunkleosteus sp. Figures 2-5

Age. Upper Devonian, uppermost Frasnian, Palmatolepis linguiformis conodont Zone.

Description. Specimen Muz. PGI-NRI 1809.II.18 (Figs 2A, B, 6A) represents the posterior part of the head and comprises the nuchal plate, part of the left paranuchal and very partially preserved central plates. The external surface is strongly abraded and natural boundaries are difficult to distinguish. The posterior margin of the nuchal plate is slightly embayed and has a single posteromedian process (Figs 2B, 6A). The anterior margin of this plate that contacts with the central plates bears a prominent wide V-shaped projection between both central plates. The side margins of the nuchal plate are more or less straight. Its posterolateral wings are well visible. Its visceral side is also partially abraded, especially in the anterior portion and there is no visible contact of the nuchal plate with the centrals. The levator pits are ellipsoidal in shape and about 1.4 cm wide, however, their shape may have been modified by erosion. They are separated by the median septum which is about 1 cm wide. They are bounded anteriorly by the huge transverse occipital thickening (3.7 cm at the thickest point) and posteriorly by a poorly developed and narrow transverse ridge of about 0.5 cm wide. Part of the left paranuchal is preserved and provides the morphology of the lateral articular fossa and partially, the para-articular process. The lateral articular fossa is ellipsoidal in shape and is 7.2 cm wide and about 2 cm deep. The paraarticular process is broken at the base. The transverse occipital thickening of the nuchal plate is continuing that of the paranuchal plates which are preserved on the both sides of the specimen. Internal and external openings of the endolymphatic duct are also preserved (Fig. 6B). The internal opening is located about 1 cm ahead towards levator pits at the base of the occipital thickening (Fig. 2B). The external opening is visible about 1.5 cm from the posterior margin of the paranuchal plate (Fig. 4B). On its outer surface the paranuchal plate carries the sensory line grooves for the main lateral line and posterior pitline. Their connection is not preserved but it seems that they meet at about 80[degrees]. Parts of two poorly preserved anterior dorsolateral plates (Muz. PGI-NRI 1809.II.20--right, Muz. PGI-NRI 1809.II.21 left; Fig. 3A, B) and the right suborbital plate (Muz. PGI-NRI 1809.II.22) have been found in association with specimen Muz. PGI-NRI 1809.II.18 (Fig. 2A--C). The suborbital plate comprises the suborbital lamina preserved only in its anteriormost part and the blade which seems to be preserved completely but is strongly eroded. The blade is about 18 cm long and its maximum width reaches 4 cm. The lamina for the posterior supragnathal is well visible, especially on the cross section (Fig. 3D, D1). Anterior dorsolateral plates have no natural margins and the only feature well recognizable is a broken glenoid condyle.

Specimen MWG UW ZI/43/0053 (Fig. 4A, B) represents a mostly preserved nuchal plate with very partially preserved paranuchal and right central plates. Both the visceral and outer surfaces are well visible. This specimen is 27 cm wide and 18 cm long. The nuchal plate outline is trapezoidal with a transverse anterior margin, however, a poorly visible V-shaped incision is observed between centrals. On the right side of the outer surface the boundary of the nuchal plate and paranuchal plates is recognizable. Its course is straight and starts from the posterior margin of the plate (not preserved) and runs towards the front with a gentle curve directed to the symmetry axis. This part is about 15.5 cm long and then turns to the left at about 90-95[degrees]. This part is visible at a distance of only 4 cm and has transverse, gently undulating shape directed towards ahead. Based on proportions, it seems that the anterior margin of the nuchal plate might be about 18 cm long. Features of the paranuchal and very partially preserved central plates are very limited for analysis because neither sensory canals nor openings are visible. Moreover, the boundary between the central and paranuchal plates is uncertain. The entire outer surface is smooth, without tubercles. The internal surface possesses a well-developed transverse occipital thickening (Fig. 4A). It is correlated with the thickening of the paranuchal plates which is preserved on the right side of the specimen. Levator pits have ellipsoidal shape with the longer axis about 1.3 cm parallel to the posterior margin of the plate. They are bounded anteriorly by the transverse occipital thickening and posteriorly by a poorly developed narrow transverse ridge about 0.6 cm wide. The levator pits are separated by a prominent median septum about 1.7 cm wide. The transverse occipital thickening is continuing on the paranuchal plate. Anteriorly to the occipital thickening there occurs the cucullaris depression which is about 0.5 cm thick in its thinnest point in the middle of the depression. It is bounded anteriorly by a not very prominent pre-endolymphatic thickening. The paranuchal margin is visible on the visceral side and shows that the nuchal plate has large overlap areas on the visceral surface for the central and paranuchal plates. Specimen Muz. PGI-NRI 1809.II.23 (Fig. 4C) is a partially preserved fragment of the anterior part of the left central plate associated with part of the pineal plate. The anterior margin shows elongated contact faces for the posterior margin of the preorbital plate. This margin is transverse and gently curved backwards. On the visceral side the deep depression of the pineal pit is bordered posteriorly and laterally by a ridge which is opened anteriorly (Fig. 4C1). No natural margins could be recognized due to the high degree of abrasion of both surfaces of the specimen.

A median dorsal plate has been found in association with the nuchal described above. Specimen Muz. PGI-NRI 1809.II.19 (Fig. 5) is partially preserved but shows the almost complete morphology of the plate. The plate is broken into several pieces. The posterior part and the uncomplete anterior part show a natural margin. The plate is relatively big: its preserved part is about 50 cm long measured from the natural anterior margin to the broken carinal process and a maximum of about 45 cm wide. The external surface lacks tubercles. The hind margin is rounded. The anterior margin forms a deep and rounded embayment of the posterior part of the nuchal gap. This plate is strongly arched transversely: the anterior part is gently curved, but the posterior lateral sides meet together at an angle of about 80[degrees] and form a crest. The keel on the visceral side is well visible along the entire plate, starting from the most anterior part where it forms a delicate and thin septum (about 0.2 mm). The posterior part becomes thicker and finally forms a carinal process which is broken almost at the base. There are elongated contact faces on the posterolateral margins of the plate for the posterior dorsolateral plates.

Discussion. The described specimens, especially the nuchal plates, clearly represent the genus Dunkleosteus and differ from other big arthrodires (after Lehman 1956, Denison 1978 and Dennis-Bryan 1987) in the emarginated posterior border of the skull roof, paranuchal plates extending back beyond the nuchal plate and showing a para-articular process, lack of dermal ornament, short, broad and triangular nuchal plate. The ventral surface of the head shield has a massive nuchal thickening and lateral consolidated parts. Levator pits are situated posteroventrally and separated by a well-developed median septum. Moreover, the median dorsal plate has a massive keel and carinal process. The anterolateral plates have large lateral laminae. Those features, including also the big size, distinguish the described specimens from other arthrodires, especially from Eastmanosteus (see discussion in Dennis-Bryan 1987 and Carr & Hlavin 2010).

Specimens MWG UW ZI/43/0053 (Fig. 4A, B), Muz. PGI-NRI 1809.II.19 (Fig. 2A, B) and Muz. PGI-NRI 1809.II.23 (Fig. 4C) putatively represent one individual and similarly another association of specimens Muz. PGI-NRI 1809.II.18 (Fig. 2A, B), Muz. PGI-NRI 1809.II. 20, 21 (Fig. 3A, B) and 22 (Fig. 3C, D). There is of course a possibility that all fragments represent different fishes and species as well. It was one of the reasons why we have decided to leave the identification rather tentative.

The nuchal plate in both cases described above has a rectangular anterior margin with a V-shaped incision between centrals (see Muz. PGI-NRI 1809.II.18; Fig. 2C1, 6B) and moreover a deep overlap area for the central and paranuchal plates. These are characteristic features of Dunkleosteus (compare Heintz 1931, 1932, text-fig. 12; pl. 1) which brings the Polish specimens closer to Dunkleosteus marsaisi (Lehman 1956, pl. 6; or Moroccan D. terreli if is synonymized with D. marsaisi (Lehman, 1954) from Morocco (Rucklin 2002)) and Dunkleosteus sp. illustrated by Ivanov & Ginter (1997, fig. 4B). The nuchal plate outline fits well with Dunkleosteus marsaisi (Lehman 1956, fig. 8) and D. intermedius (terreli) (Heintz 1932, text-fig. 12) but is narrower. It resembles the nuchal plate of D. amblyodoratus Carr & Hlavin, 2010 (fig. 6A--C) also in size, however, Polish specimens have a more prominent anterior part. Also, the occipital thickening is roughly typically developed and resembles many specimens referred to Dunkleosteus. Both the described nuchal plates are characterized by a similar development of the levator pits areas which show the same thin transverse ridge that is bounding pits posteriorly. In specimen MWG UW ZI/43/0053 (Fig. 4A) this ridge is almost incorporated into the posterior margin of the plate, whereas it is more prominent in specimen Muz. PGI-NRI 1809.II.18 (Fig. 2A, B). This difference may be ontogenetic because specimen MWG UW ZI/43/0053 (Fig. 4A) is larger and therefore may represent an older stage than PGI-NRI 1809.II.18 (Fig. 2A, B). Anyway, this feature (pits bounded by the ridge are small posteriorly or almost absent) is unusual for Dunkleosteus (e.g. Carr & Hlavin 2010, fig. 6A, B) and occurs not very often. A similar case was illustrated by Lehman (1956, pl. 16F), who identified his fragmentary specimen as Dinichthyidae sensu lato. The shape and morphology of levator pits on specimen Muz. PGI-NRI 1809.II.18 (Fig. 2A1), which are more rounded than ellipsoidal and are bounded posteriorly by a very thin transverse ridge, are similar to features present also in the specimen illustrated by Lehman (1956, pl. 16F). A comparable feature occurs in some undescribed specimens stored in the Famennian part of the collection, in the Cleveland Natural History Museum. This may be a diagnostic character for a new species that must be carefully studied in the future based on additional material.

The morphology of the suborbital plate cannot be recognized in details, especially due to the suborbital lamina. The postorbital region is partially preserved but the cross section illustrates well the prominent linguiform process that is common within the genus (e.g. Dean 1908, fig. 60; Heintz 1932, text-figs 21, 22).

The median dorsal plate resembles the Dunkleosteus pattern in its outline (e.g. Dean 1908, fig. 61) but is different from most of the dunkleosteid median dorsal plates (see Heintz 1932, text-fig. 44; Lehman 1956, pl. 14). However, anterolateral margins are not recognized; they must have had deep embayment in the anterior part comparable to that of D. marsaisi (Lehman 1956, pl. 14B). The development of the keel on the specimen analysed is quite typical for the genus. It is present along almost the entire plate and gradually becomes crude at the posterior margin with the carinal process, resembling the specimens of Dunkleosteus illustrated by Heintz (1932, text-fig. 44). The comparison with other material from the Holy Cross Mountains indicates different affinities. The specimens of Dunkleosteus denisoni described by Kulczycki (1957: 313, text-fig. 10, pl. VI, fig. 4, fig. VII) represent a much smaller taxon which possesses a huge keel and carinal process. Though, even if the keel and process are broken, it is clear that these were not very prominent in the specimen described herein (comp. Kulczycki 1957, pl. VII and Fig. 5). Moreover, specimens described by Kulczycki (1957) are middle Famennian in age.

Other features like the morphology of the transverse occipital thickening, cucullaris depression, the morphology of the internal side of the pineal opening and the position of the external and internal opening for the endolymphatic duct fit to the general morphology of the genus Dunkleosteus illustrated by Leriche (1931), Heintz (1932, text-figs 12, 13, pls 1, 2) and Stensio (1963, fig. 112A, B).

The reconstructed width of the skull is about 50 cm. Based on proportions of the best-preserved specimens from the Cleveland collection it is likely that the form described from the Holy Cross Mountains reached more than 60 cm in skull length and is a bit larger than D. marsaisi (skull length about 50 cm).


The described specimens represent the oldest occurrence of the genus Dunkleosteus in Europe, being uppermost Frasnian in age. Moreover, it is the first Dunkleosteus from Poland described with certainty based on skull remains. The material is preserved in associations with two individuals which probably represent the same taxon at different ontogenetic stages.

According to essential features, these specimens are closest to Dunkleosteus marsaisi (Lehman 1956) by the external shape and internal morphology of the nuchal plate, internal morphology of the pineal plate and similar sizes. The Polish specimen differs from the Moroccan one in the development of the levator pits area, which may be a specific character for the possible distinction of a separate species of Dunkleosteus.

Acknowledgements. We thank Daniel Goujet and Alexander Ivanov for their very useful reviews and helpful comments. We are also grateful for Lukasz Gagala and Stanislaw Krupa for providing a part of the studied collection. P. Szrek was funded by the Polish Geological Institute-National Research Institute (grant No. 61.2401.1301.00.0). P. Szrek and O. Wilk were funded by the National Science Foundation (grant No. 2016/23/B/ST10/03262). The publication costs of this article were covered by the Estonian Academy of Sciences.


Bond, D., Paul, B. & Racki, G. 2004. Extent and duration of marine anoxia during the Frasnian--Famennian (Late Devonian) mass extinction in Poland, Germany, Austria and France. Geological Magazine, 141, 173-193.

Carr, R. & Hlavin, W. J. 1995. Dinichthyidae (Placodermi): a paleontological fiction? Geobios, 19, 85-87.

Carr, R. & Hlavin, W. J. 2010. Two new species of Dunkleosteus Lehman, 1956, from the Ohio Shale Formation (USA, Famennian) and the Kettle Point Formation (Canada, Upper Devonian), and a cladistics analysis of the Eubrachthoraci (Placodermi Arthrodira). Zoological Journal of the Linnean Society, 159, 195-222.

Czarnocki, J. 1989. Clymenids of the Holy Cross Mountains. Prace Panstwowego Instytutu Geologicznego, 77, 1-91 [in Polish, with English summary].

Dean, B. 1908. Studies on fossil fishes. Memoir American Museum of Natural History, 5, 211-287.

Denison, R. H. 1978. Handbook of Paleoichthyology, Vol. 2--Placodermi (Schultze, H.-P., ed.). Gustav Fischer, Stuttgart--New York, 128 pp.

Dennis-Bryan, K. 1987. A new species of eastmanosteid arthrodire (Pisces: Placodermi) from Gogo, Western Australia. Zoological Journal of the Linnean Society, 90, 1-64.

Dworczak, P. G. 2016. Rodzaj Aspidichthys (Placodermi) z gornego dewonu Gor Swietokrzyskich [Genus Aspidichthys from the Upper Devonian of the Holy Cross Mountains]. MSc thesis. Instytut Geologii Uniwersytetu im. Adama Mickiewicza w Poznaniu, 32 pp. [in Polish, with English summary].

Dworczak, P. & Szrek, P. 2016. The Late Devonian placoderm Aspidichthys Newberry, 1873 from the Holy Cross Mountains, Poland. Fossil Record, 20, 9-19.

Dzik, J. 1985. Phylogeny of the Nautiloidea. Palaeontologia Polonica, 45, 1-219.

Dzik, J. 2002. Emergence and collapse of the Frasnian conodont and ammonoid communities in the Holy Cross Mountains, Poland. Acta Palaeontologica Polonica, 47, 565-650.

Filipiak, P. 2002. Palynofacies around the Frasnian/Famennian boundary in the Holy Cross Mountains, southern Poland. Palaeogeography, Palaeoclimatology, Palaeoecology, 181, 313-324.

Ginter, M. 1995. Ichthyoliths and Late Devonian events in Poland and Germany. Ichthyolith Issues, Special Publication, 1, 23-30.

Ginter, M. 2002. Chondrichthyan fauna of the Frasnian--Famennian boundary beds in Poland. Acta Palaeontologica Polonica, 47, 329-338.

Heintz, A. 1931. A new reconstruction of Dinichthys. American Museum Novitates, 457, 1-5.

Heintz, A. 1932. The structure of Dinichthys. A contribution to our knowledge of the Arthrodira. The Bashford Dean Memorial Volume Archaic Fishes, 4, 115-224.

House, M. R. 2002. Strength, timing, setting and cause of mid-Palaeozoic extinctions. Palaeogeography, Palaeoclimatology, Palaeoecology, 181, 5-25.

Ivanov, A. & Ginter, M. 1997. Comments on the Late Devonian placoderms from the Holy Cross Mountains (Poland). Acta Palaeontologica Polonica, 42, 413-426.

Janiszewska, K. 2008. Mikrofacje, stratygrafia i mikroskamienialosci kregowcow pogranicza franu i famenu rejonu Lagowa w Gorach Swietokrzyskich [Microfacies, Stratigraphy and Vertebrates Microfossils at the Frasnian--Famennian Boundary of the Lagow Area in the Holy Cross Mountains]. Unpublished MSc thesis, Instytut Geologii Podstawowej, Wydzial Geologii UW [in Polish, with English summary].

Janiszewska, K., Szrek, P. & Woroncowa-Marcinowska, T. 2007. Zapis zdarzen biotycznych na pograniczu fransko-famenskim w Pluckach kolo Lagowa [Record of biotic events at the Frasnian-Famennian boundary in Plucki near Lagow]. In Granice Paleontologii (Frontiers of Palaeontology), XX Konferencja Paleobiologow i Biostratygrafow PTG Sw. Katarzyna pod Lysica, 10-13 wrzesnia 2007 [20th Conference of Paleobiologists and Biostratigraphers of the Polish Geological Society, September 10-13, 2007] (Zylinska, A., ed.), pp. 63-66. Geological Faculty, University of Warsaw.

Koenen, A. V. 1883. Beitrag zur Kenntniss der Placodermen des norddeutschen Oberdevon's. Abhandlungen Konigliche Gesellschaft der Wissenschaften, Gottingen, 30, 1-10.

Kowalczewski, Z. 1971. Main geological problems of the Lower Devonian in the Swietokrzyskie Mts. Geological Quarterly, 15, 263-283 [in Polish, with English summary].

Kulczycki, J. 1957. Upper Devonian fishes from the Holy Cross Mountains. Acta Palaeontologica Polonica, 2, 285-380.

Lehman, J. P. 1956. Les Arthrodires du devonien superieur du Tafialet (Sud Marocain). Service Geologique Maroc, Notes et Memoires, 129, 1-70.

Leriche, M. 1931. Les poissons famenniens de la Belgique. Memoire Acad Royale de Belgique, 10, 1-72. Makowski, H. 1963. Problem of sexual dimorphism in ammonites. Palaeontologia Polonica, 12, 1-92.

Makowski, H. 1971. A contribution to the knowledge of Upper Devonian ammonoids from the Holy Cross Mts. Acta Geologica Polonica, 21, 131-136.

M'Coy, F. 1848. On some new fossil fishes of the Carboniferous period. Annals and Magazine of Natural History, 2, 1-10.

Racki, G., Racka, M., Matyja, H. & Devleeschouwer, X. 2002. The Frasnian/Famennian boundary interval in the South Polish--Moravian shelf basins: integrated event-strati-graphical approach. Palaeogeography, Palaeoclimatology, Palaeoecology, 181, 251-297.

Rakocinski, M., Pisarzowska, A., Janiszewska, K. & Szrek, P. 2016. Depositional conditions during the Lower Kellwasser Event (Late Frasnian) in the deep-shelf Lysogory basin of the Holy Cross Mountains (Poland). Lethaia, 49, 571-590.

Rucklin, M. 2002. New finds of placoderms from the Late Devonian of Morocco. In 7th European Workshop on Vertebrate Palaeontology, Sibiu, Romania, Abstracts. p. 31.

Sobolev, D. 1912. O verkhnem neodevone Lagowa [On the Upper Devonian of Lagow]. Izvestiya Varshavskogo Politekhnicheskogo Instituta, 3, 1-32 [in Russian].

Stensio, E. 1944. Contributions to the knowledge of the vertebrate fauna of the Silurian and Devonian of Podolia II--Note on two Arthrodires from the Downtonian of Podolia. Arkiv for Zoologi, 35, 1-83.

Stensio, E. 1963. Anatomical studies on the arthrodiran head. Part I. Kunglia Svenska Vetenskapsakademiens Handlingar, 9, 1-419.

Szrek, P. 2007a. The facies-related distribution of placoderms in the Late Devonian of the Holy Cross Mountains. Ichthyolith Issues, 10, 85-86.

Szrek, P. 2007b. Ryby pancerne a zapis gornego zdarzenia Kellwasser w Pluckach kolo Lagowa. In Granice Paleontologii, XX Konferencja Paleobiologow i Biostratygrafow PTG Sw. Katarzyna pod Lysica, 10-13 wrzesnia 2007 [20th Conference of Paleobiologists and Biostratigraphers of the Polish Geological Society, September 10-13, 2007] (Zylinska, A., ed.), pp. 133-134. Geological Faculty, University of Warsaw.

Szrek, P. 2008. Vertebrates from the upper Kellwasser limestone, Frasnian--Famennian boundary beds (Upper Devonian) of the Holy Cross Mountains (Poland). Journal of Vertebrate Paleontology, 28, 150.

Szrek, P. 2009. Placoderm Fishes from the Devonian of the Holy Cross Mountains. Unpublished PhD dissertation. University of Warsaw, Warsaw, 144 pp. [in Polish, with English summary].

Szrek, P. & Ginter, M. 2008. Kellwasserkalk layers at Plucki near Lagow. Ichthyolith Issues, 11, 46-50.

Szrek, P. & Niedzwiedzki, G. 2015. Placoderm faunas from the Lower to Upper Devonian of the Holy Cross Mountains. In 13th International Symposium on Early and Lower Vertebrates Melbourne, Australia, August 3rd-7th 2015 (Trinajstic, K., Johanson, Z., Richter, M. & Boisvert, C., eds), appendix 1. Royal Society of Victoria, Melbourne.

Szulczewski, M. 1989. Swiatowe i regionalne zdarzenia w zapisie stratygraficznym pogranicza franu i famenu Gor Swietokrzyskich [Global and regional events in the stratigraphic record on the Frasnian--Famennian boundary of the Holy Cross Mountains]. Przeglad Geologiczny, 37, 551-557.

Szulczewski, M. 1995. Depositional evolution of the Holy Cross Mts. (Poland) in the Devonian and Carboniferous--a review. Geological Quarterly, 39, 471-188.

Woodward, A. S. 1891. Catalogue of the Fossil Fishes in the British Museum (Natural History), Vol. 2. London, 567 pp.

Woroncowa-Marcinowska, T. 2006. Upper Devonian goniatites and co-occuring conodonts from the Holy Cross Mountains: studies of the Polish Geological Institute collections. Annales Societatis Poloniae, 76, 113-160.

Piotr Szrek (a) and Olga Wilk (b)

(a) Polish Geological Institute--National Research Institute, 4 Rakowiecka Street, 00-975 Warszawa, Poland;

(b) Faculty of Geology, University of Warsaw, 93 Zwirki i Wigury Street, 02-089 Warszawa, Poland;

Received 1 August 2017, accepted 31 October 2017, available online 19 January 2018

Suur Hilis-Devoni artrodiir (Vertebrata, Placodermi) Poolast

Piotr Szrek ja Olga Wilk

On kirjeldatud Placodermi klassi kuuluvat artrodiiri Dunkleosteus sp., kelle jaanukid leiti Ulem-Devoni (Frasnesi) nn Kellwasseri taseme kivimitest Plucki paljandist Swietokrzyskie magedest Poolast. Kahe isendi osaliselt sailinud jaanukid on ilmselt umber setitatud madalaveelisemast faatsiesest suvaselfi alale. Leitud fragmendid on siin nimetatud Dunkleosteus sp., kuid nad on sarnased Dunkleosteus marsaisi'le Maroko Famenne'ist. See viitab, et Poola vorm voib olla uus liik, kuid selle toestamine vajab lisamaterjali leidmist ja uurimist. Kirjeldatud eksemplarid on Dunkleosteus'e perekonna vanimad esindajad Euroopas, koige taielikumad Poolas, kuuludes suurimate plakodermide hulka, kelle pea on 60 cm pikk.
COPYRIGHT 2018 Estonian Academy Publishers
No portion of this article can be reproduced without the express written permission from the copyright holder.
Copyright 2018 Gale, Cengage Learning. All rights reserved.

Article Details
Printer friendly Cite/link Email Feedback
Author:Szrek, Piotr; Wilk, Olga
Publication:Estonian Journal of Earth Sciences
Article Type:Report
Date:Mar 1, 2018
Previous Article:The Borschovo section of the Gauja and Amata regional stages (Leningrad Region, Russia): sedimentology and biostratigraphy.
Next Article:Chondrichthyans from the Devonian--Early Carboniferous of Belarus.

Terms of use | Privacy policy | Copyright © 2022 Farlex, Inc. | Feedback | For webmasters |