Biostratigraphical correlation of spore and conodont zonations within Givetian and ?Frasnian of the Lublin area (SE Poland)

Review of Palaeobotany and Palynology 164 (2011) 30–38

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Review of Palaeobotany and Palynology j o u r n a l h o m e p a g e : w w w. e l s ev i e r. c o m / l o c a t e / r ev p a l b o

Biostratigraphical correlation of spore and conodont zonations within Givetian and ?Frasnian of the Lublin area (SE Poland) Elżbieta Turnau a,⁎, Katarzyna Narkiewicz b a b

Institute of Geological Sciences, Polish Academy of Sciences, Kraków Research Centre, Senacka 1, 31-002 Kraków, Poland Polish Geological Institute, National Research Institute, Rakowiecka 4, 00-975 Warszawa, Poland

a r t i c l e

i n f o

Article history: Received 11 December 2009 Received in revised form 5 July 2010 Accepted 15 July 2010 Available online 22 July 2010 Keywords: spores conodonts Givetian Frasnian biostratigraphy intercalibration

a b s t r a c t Givetian and ?Frasnian spores associated with conodont elements occur in two boreholes in the Lublin area allowing definition of the stratigraphical relationship of the first appearance or last occurrence of selected spore species and form features to the conodont division. Spore data from a section lacking conodonts but correlatable on lithostratigraphy with the conodont bearing one are also considered. The spore zonal scheme for Western Pomerania is correlated with the conodont zonation. The first occurrence of Chelinospora concinna (base of the Ex 2 Subbiozone) and Kraeuselisporites spinutissimus are probably within the range of rhenanus/varcus to ansatus Biozones, not above the ansatus Biozone. The first occurrence of Samarisporites triangulatus (base of the Ex 3 Subbiozone) is in the ansatus Biozone. The disappearance of Aneurospora extensa (base of the Aur Biozone) is within the range of ansatus to hermanni Biozones. The species Corystisporites pomeranius and multifurcate-spined spores appear in the falsiovalis Biozone, probably in the Upper falsiovalis Biozone. The first occurrence of Tholisporites densus (base of the Den Biozone) is somewhat higher but still in the same biozone. © 2010 Elsevier B.V. All rights reserved.

1. Introduction The first comprehensive spore zonation scheme for the Devonian of the Old Red Sandstone Continent and adjacent areas was described by Richardson and McGregor (1986). Other, widely used schemes for the Devonian are that for the Ardenne–Rhine regions (Streel et al., 1987), and that for Eastern Europe (Avkhimovitch et al., 1993). The zonal boundaries of all those schemes are correlated with the conodont scheme and other schemes based on marine faunas, but these correlations are, in most cases, only approximate. Data on conodonts and spores recovered from the same section are rare. Spores were recovered from Siegenian to Famennian conodontbearing strata in Melville Island (Canadian Arctic), but conodonts are only sparsely present there (McGergor and Uyeno, 1972). Most biostratigraphical contributions on spores from sediments dated by conodonts concern Western Europe (summarized in Streel, 2009). Givetian and Frasnian conodonts and spores have been recovered from sections in Boulonnais, France (Brice et al., 1979, 1981; Loboziak and Streel, 1980, 1981), and in the Eifel Mountains (Loboziak et al., 1991). Famennian spore assemblages were found in conodont dated sections in Belgium, in the Dinant Synclinorium, Ardennes (Loboziak et al., 1995; Maziane et al., 1999). Important spore and conodont data

⁎ Corresponding author. E-mail address: [email protected] (E. Turnau). 0034-6667/$ – see front matter © 2010 Elsevier B.V. All rights reserved. doi:10.1016/j.revpalbo.2010.07.003

on the uppermost Famennian (Strunian), and the Devonian/Carboniferous boundary beds, have been presented by Higgs and Streel (1984). Both microfossil groups also occur in Givetian strata exposed in the Holy Cross Mountains (Malec and Turnau, 1997; Turnau and Racki, 1999). The subsurface Givetian deposits of the Lublin area (Fig. 1) comprise alternating clastic, evaporite and carbonate rocks, and the Frasnian deposits are developed in carbonate–sulfate facies. Comprehensive information on geology of these deposits may be found in Miłaczewski (1981), Miłaczewski et al. (1983), and Narkiewicz et al. (1998). Conodonts and spores discussed in this paper are derived from two borehole sections situated in the central (Giełczew PIG 5) and southeastern part (Terebin IG 5) of the Lublin area. Spores were also found in the Giełczew PIG 6 borehole. The lithostratigraphic division of these strata, after Narkiewicz (personal communication, 2010) is shown in Figs. 2 and 3. The spore assemblages are assignable to the local scheme for Western Pomerania (NW Poland) as proposed by Turnau (1996, 2007). The assemblages contain some species of distinctive morphology and wide geographical distribution. Their importance for stratigraphy has been recognized by numerous authors, four are zonal index species, other may, in the future, be useful for subdividing the existing zones. The objective of this paper is to establish the stratigraphical position of the first or last appearances of these spore taxa, and some form features, in relation to the conodont zones, and to correlate the spore zonal scheme for Western Pomerania with conodont zonations. Our conclusions are based primarily on the results from the Lublin area, but revised conodont

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datings of spore biohorizons from the Holy Cross Mountains are also taken into consideration. 2. Conodont zonation

Fig. 1. Simplified location map of study area (after Pożaryski and Dembowski, 1983, altered); tectonic units: RKE — Radom–Kraśnik Elevation, LT — Lublin Trough, EPEEP — Elevated Part of East European Platform. Insert shows areas in Poland discussed in the text: WP — Western Pomerania, HCM — Holy Cross mountains, LA — Lublin area.

The shallow marine facies of the Givetian of the study area are not favourable for development of conodont faunas. Diversified and relatively abundant assemblages only occur in isolated carbonate layers representing open marine transgressive episodes (Figs. 2 and 3, see also Narkiewicz and Bultynck, 2007, fig. 7, 8). The interlayered carbonate, clastic, and evaporite successions contain poorer and less diversified microfauna or are entirely barren. The conodont assemblages represent polygnathid, through polygnathid–icriodid, icriodid–polygnathid to icriodid biofacies. Conodont stratigraphic division of the Middle Devonian is usually based on occurrence of index species characteristic of the deeper facies (see Ziegler and Klapper, 1982; Bultynck, 1987; Klapper and Johnson, 1990; Ziegler and Sandberg, 1990; Bultynck and Gouwy, 2008). Applicability of this zonation to shallower facies, where these species are rare or absent, is not satisfactory. Therefore, for the Givetian of the Lublin area, Narkiewicz and Bultynck (2007) applied an alternative conodont zonation. The division by Bultynck (1987) has been used for the Lower and Middle Givetian. New data on the subterminus fauna obtained in North America, Europe and North Africa allowed the introduction for the Upper Givetian of the expansus and subterminus Biozones (Narkiewicz and Bultynck, 2010). The index species of the former – Icriodus expansus Branson and Mehl, 1938 – is a deeperwater form, but is also encountered, though in lesser numbers, in shallow water facies. The expansus Biozone includes most of the hermanni Biozone, and the disparilis to norrisi Biozones (Fig. 4). The

Fig. 2. Stratigraphy of pertinent part of Giełczew PIG 5 and Giełczew PIG 6 borehole sections, and location of conodont and spore samples. Numbers 1, 3–7 mark levels of species or morphological features first (FOB) or last (LOB) occurrence: 1. C. concinna, FOB, 3. S. triangulatus, FOB, 4. A. extensa, LOB, 5. C. pomeranius, FOB, 6. multifurcate-spined spores, FOB, 7. T. densus, FOB. Lithostratigraphic division after Narkiewicz (personal communication, 2010).

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Fig. 3. Stratigraphy of pertinent part of Terebin IG 5 borehole section, and location of conodont and spore samples. Numbers 1–5 mark levels of first (FOB) or last (LOB) occurrence: 1. C. concinna, FOB, 2. K. spinutissimus, FOB, 3. S. triangulatus, FOB, 4. A. extensa, LOB, 5. C. pomeranius, FOB. Lithostratigraphic division after Narkiewicz (personal communication, 2010).

subterminus Biozone with the Icriodus subterminus Youngquist, 1947 index species is divisible into three subbiozones. The Lower subterminus Subbiozone based on the first appearance of I. subterminus corresponds to the uppermost part of the hermanni Biozone

and Lower disparilis Biozone. The Middle subterminus Subbiozone based on the first appearance of Polygnathus angustidiscus Youngquist, 1945 and Mehlina gradata Youngquist, 1945 corresponds approximately to the Upper disparilis Biozone, and the Upper

Fig. 4. Correlation of Middle Devonian and basal Frasnian alternative and “standard” conodont zonations, and spore zonation for Western Pomerania. Abbreviation: S&D — Sandberg and Dreesen.Pl. I. Givetian and ?Frasnian spores from Lublin area. Givetian and ?Frasnian spores from Lublin area.

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Plate I. 1. 2. 3,4. 5. 6. 7. 8. 9. 10. 11. 12,13.

Chelinospora concinna, Terebin IG 5 borehole, depth 1604.10 m, slide TI/94. Tholisporites densus, Giełczew PIG 6 borehole, depth 2007.5 m, slide GIV/57. Aneurospora extensa, Terebin IG 5 borehole, depth 1557.35 m. 3. Slide TII/59, 4. Slide TII/54. Geminospora aurita, Terebin IG 5 borehole, depth 1557.35 m, slide TII/54. Geminospora compta, Terebin IG 5 borehole, depth 1598.95 m, slide TII/1. Geminospora lemurata, Terebin IG 5 borehole, depth 1598.95 m, slide TI/99. Lanatisporis bislimbatus, Terebin IG 5 borehole, depth 1604.10 m, slide TI/94. Samarisporites triangulatus, Terebin IG 5 borehole, depth 1577.2 m, slide TIII/54. Kraeuselisporites spinutissimus, Terebin IG 5 borehole, depth 1604.10 m, slide TI/94. Corystisporites pomeranius, Giełczew PIG 6 borehole, depth 2009.30 m, slide GIV/61. Ancyrospora. cf. pulchra, Giełczew PIG 5 borehole, depth 1965.45 m, slide GIII/78, 13. fragment of specimen in 12. showing multifurcate spine (arrow).

subterminus Subbiozone based on the first appearance of Skeletoganthus norrisi (Uyeno, 1967) and Pandorinellina insita (Stauffer, 1940) is approximately the equivalent of the norrisi Biozone. The biostratigraphic interpretation takes into account the verified total ranges of all taxa (that are mostly not index taxa) correlated with the standard division. It should be added that the conodonts derived from the sporebearing strata in the Giełczew PIG 5 and Terebin IG 5 boreholes (Figs. 2 and 3) did not allow identification of all the biozones and subbiozones of the alternative zonation. 3. Conodont control on selected palynological events: correlation of zonations Givetian and ?lower Frasnian spore assemblages from the Lublin area have been assigned to the zonation scheme introduced by Turnau (1996) for part of Eifelian and Givetian of Western Pomerania. Subsequently, it was expanded (Turnau, 2007) to embrace the Late Givetian and Frasnian. This scheme is partly the modified zonation for Eastern Europe by Avkhimovitch et al. (1993). The part pertinent to the present paper comprises three interval biozones and three subbiozones (Fig. 4). The Geminospora extensa (Ex) Biozone comprises three subbiozones (Ex 1–3). Its lower boundary is marked by the first appearance of Geminospora lemurata Balme emend. Playford, 1983. The lower boundary of the Ex 1 Subbiozone is equivalent of the

lower boundary of the Ex Biozone. The base of the Ex 2 Subbiozone is defined by the first appearance of Chelinospora concinna Allen, 1965, and Samarisporites triangulatus Allen, 1965 marks the base of the Ex 3 Subbiozone. The base of the Geminospora aurita (Aur) Biozone is marked by the last occurrence of Aneurospora extensa (Naumova) Turnau, 1996. The assemblages of this biozone are poorly diversified and dominated by Geminospora spp. Impoverished assemblages dominated by Geminospora and Aneurospora commonly contain Ancyrospora, and lack several species typical of the Ex Biozone. The Aur Biozone is equivalent to most of the Ancyrospora incisa–Geminospora micromanifesta (IM) Subbiozone of Eastern Europe that was distinguished in the Holy Cross Mountains (Turnau and Racki, 1999). The lower boundary of the Tholisporites densus (Den) Biozone was placed at the level of the appearance of T. densus McGregor, 1960. The succession of spore assemblages just below this boundary is poorly known both in Western Pomerania and in the study area. So far, in Western Pomerania, conodont data related to this scheme are very rare; and reasonable recovery of conodont elements only starts from the biozones in the range of transitans/ punctata. The data from the study area allow correlation of this zonation with conodont stratigraphical schemes (Fig. 4). The stratigraphical relationship between the first appearance of selected, non-zonal species and form features and the conodont faunas are also discussed below. All the spore taxa discussed are illustrated in Plate I.

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3.1. Chelinospora concinna Allen, 1965 This is a stratigraphically important and geographically widely distributed species that has been recorded from the Givetian and Frasnian of Euramerica and Australia (McGregor and Playford, 1992), and Brazil (Burjack et al., 1987; Loboziak et al., 1988). Its first appearance defines the base of the Ex 2 Subbiozone (Turnau, 1996), and the bases of some other western and eastern European biozones (Streel et al., 1987; Obukhovskaya, 2000). In the Lublin area, in the Terebin IG 5 borehole, the lowest occurrence of Chelinospora concinna is in the Żniatyń Member of the Telatyn Formation (Fig. 3) at the depth 1604.1 m, above a long, palynologically barren and/or un-sampled interval. Conodont elements found 1 m below, in the Machnów Member, are indicative of biozones in the range of rhenanus/varcus to ansatus based on the presence of I. latecarinatus Bultynck, 1974, and those occurring above represent the ansatus Biozone based on the presence of P. cf. ansatus Ziegler and Klapper, 1976 (Narkiewicz and Bultynck, 2007, fig. 4F) and I. platyobliquimarginatus Bultynck, 1987 (op. cit., fig. 4T). In the Giełczew PIG 5 borehole, C. concinna first occurs in the Giełczew Member of the Telatyn Formation at a depth of 2018.87 m (Fig. 2), also above a long interval that lacks spores. Conodont elements found c. 45 and 75 m below are indicative of biozones in a wide range between hemiansatus and ansatus based on the presence of I. lindensis Weddige, 1977 (Narkiewicz and Bultynck, 2007, fig. 9U), and those from a sequence just above the spore level indicate the presence of the ansatus Biozone based on occurrence of P. ansatus (op. cit. fig. 4C) and I. arkonensis arkonensis Stauffer 1938 (op. cit., fig. 4M). The data from these boreholes indicate that, in the study area, the first appearance of C. concinna is probably within the range of rhenanus/varcus to ansatus Biozones, and likely not above the ansatus Biozone. In the Holy Cross Mts. in central Poland, Chelinospora concinna first appears in sample P10, in the lithostratigraphical unit XXV, subunit B (Malec and Turnau, 1997, fig. 6). In the same unit, four samples from a 3.3 m interval below sample P10 did not contain this species. Conodont elements were found in the same lithostratigraphic subunit, in sample K3, c. 2.5 m below palynological sample that contained C. concinna. This conodont sample (op. cit., pl. I, fig. 9, 13) contained representatives of Icriodus aff. I. eslaensis Van Adrichem Boogaaert, 1967, and I. arkonensis walliserianus Weddige, 1988 (see Section 4.2). The stratigraphical range of I. arkonensis walliserianus is from the ensensis to ansatus Biozones (see Narkiewicz and Bultynck, 2007, p. 428), but the age of sample K3 may be determined more precisely using data provided by conodont elements from the underlying and overlying strata. The samples K12 and K8 are from the top part of the unit XX, and samples K28 and K31 from the unit XXVA, all four from below the discussed sample K3. The unit XX may be assigned to conodont biozones in the range of timorensis to rhenanus/varcus based on the presence of P. timorensis Klapper et al., 1970 (Malec and Turnau, 1997, pl. II, fig. 7) and I. obliquimarginatus Bischoff and Ziegler, 1957 (op. cit., pl. I, fig. 2). Moreover, the fauna from sample K28 from the unit XXVA, below sample K3, is indicative of position not higher than the ansatus Biozone. This fauna included representatives of Polygnathus pseudofoliatus Wittekind, 1966 (see Section 4.2). The last occurrence of this species is noted in the ansatus Zone (Narkiewicz and Bultynck, 2007). A conodont element representing I. brevis Stauffer, 1938 was found in sample K31 (see Malec and Turnau, 1997, pl. I, fig. 10), taken from the same unit from above sample K28. This species first appears in upper part of the timorensis Biozone (Bultynck and Gouwy, 2008). It follows that the strata between samples K28 and K31 are within the range of timorensis (upper part) to ansatus Biozones. The fauna from sample K1 taken from the unit XXVIIIB, above both conodont sample K3 and palynological sample P10, represents

the ansatus Biozone based on joined occurrence of P. ansatus Ziegler ad Klapper, 1976 (Malec and Turnau, 1997, pl. II, fig. 10, 11), P. beckmani Bischoff, Ziegler and Klapper, 1957 (op. cit. pl. III, fig. 9), and I. arkonensis walliserianus (op. cit., pl. I, fig. 11, determined by Malec as Icriodus sp.). Those two species last mentioned occur for the last time in the ansatus Biozone (Klapper and Johnson, 1980; Narkiewicz and Bultynck, 2007). The data from the Holy Cross Mts. discussed above indicate that the level in unit XXVB corresponding to sample K3, and the level of palynological sample P10 are within the range of upper part of timorensis to ansatus Biozones. In Boulonnais (France), Chelinospora concinna first appears in the Couderousse Member of the Blacourt Formation exposed near Ferques (Brice et al., 1979). The conodont fauna from this member was termed fauna V. It was considered to correspond to the Middle or Upper varcus Biozone (Loboziak and Streel, 1980, Streel and Loboziak, 1996, Streel, 2009). The lowest level with C. concinna was that of palynological sample 1 taken from a sequence between the conodont samples 7 and 8. The revision of the fauna V from the Couderousse Member reveals that the sequence corresponding to the samples 7 to 9 belongs to the ansatus Biozone (Narkiewicz and Bultynck, 2010). This fauna does not contain the index species of the ansatus Biozone, its position is established based on compilation of total stratigraphic ranges of the species encountered. For the sequence bracketed by the samples 7 and 9, the important species are Polygnathus alatus Huddle, 1934 (Narkiewicz and Bultynck, 2010, tab. 7), and Polygnathus pseudofoliatus (Brice et al., 1979, pl. XXVII, fig. 6). The former species was encountered in sample 7. Its stratigraphical first occurrence is in the ansatus Zone (Huddle and Repetski, 1981) while P. pseudofoliatus, found in samples 7, 8 and 9, disappears in that Biozone. The data from the Lublin area and the Holy Cross Mountains concerning the first appearance of C. concinna are consistent with the revised data from France, though the Polish data are less tightly constrained. 3.2. Kraeuselisporites spinutissimus (Kedo) McGregor and Camfield, 1982 This is a widely distributed species of distinct morphology that may be stratigraphically useful. It has been recorded from the Givetian of Canada (McGregor and Camfield, 1982), Poland (Turnau, 1996) and Eastern Europe (Avkhimovitch et al., 1993), but, until now, it has not been found in a conodont-bearing section. In the Lublin area, in the Terebin IG 5 borehole, the lowest occurrence of Kraeuselisporites spinutissimus is in the Żniatyń Member of the Telatyn Formation (Fig. 3) at the depth 1604.1 m, above a long, palynologically barren and/or not sampled interval. Conodonts found in three samples below that level are indicative of biozones in the range of rhenanus/varcus to ansatus, and those occurring above represent the ansatus Biozone (see Section 3.1). 3.3. Samarisporites triangulatus Allen, 1965 Morphology of this species is distinct and it is widely distributed in the northern hemisphere occurring from western Canada to southeastern Asia (Allen, 1982). It has also been recorded from Australia (McGregor and Playford, 1992), North Africa (Loboziak and Streel, 1995) and South America (Burjack et al., 1987; Loboziak et al., 1988). Samarisporites triangulatus is considered to be of stratigraphical importance, its first appearance defines bases of biozones of a few zonal schemes for the Devonian (Richardson and McGregor, 1986; Streel et al., 1987; Turnau, 1996, Obukhovskaya, 2000). The position of the first occurrence biohorizon of S. triangulatus has been established on direct conodont data in the Eifel Mountains, but the identity of the specimens is questioned and is discussed in Section 4. In the study area, the first appearance of Samarisporites triangulatus is in the Pełcza Member of the Telatyn Formation from the

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Terebin IG 5 borehole at the depth 1577.20 m (Fig. 3). Three samples below this level (depth 1604.1 m), in the underlying member, did not contain S. triangulatus. The assemblage including this species is associated with conodont taxa indicative of the ansatus Biozone based on the presence of P. cf. P. ansatus and I. platyobliquimarginatus. In The Giełczew PIG 5 borehole, S. triangulatus first occurs in the Giełczew Member of the Telatyn Formation at a depth of 2018.87 m, above a long interval that did not contain spores. Below, at a depth of 2099.2 m, there occur conodonts indicative of biozones in the range of hemiansatus to ansatus (for details see Section 3.1). The data from the Terebin IG 5 borehole imply that, in the study area, the first appearance of Samarisporites triangulatus is within the ansatus Biozone. This is consistent with the information obtained in the Holy Cross Mts. In that area, the first appearance of the species under discussion is not dated by conodonts, but it is worth noting that it was first recorded from the basal part of the Nieczulice beds in a few meters sequence which also yielded ammonoids of the Maenioceras terebratum Biozone (Turnau and Racki, 1999) corresponding (Becker and House, 1994) to a middle part of the Middle varcus Biozone (here the ansatus Biozone). In Boulonnais, Samarisporites triangulatus occurs in the Couderousse Member of the Blacourt Formation exposed near Ferques (Brice et al., 1979). The lowest sample containing this species is above a long palynologically barren interval. The position of this sample is below the conodont faunas IV and V discussed above. This record indicates that the first appearance of S. triangulatus is not higher than the ansatus Biozone. In the Eifel region, the first appearance of spores assigned to Samarisporites triangulatus was noted in the lower part of the Kerpen Formation at Kerpen (Loboziak et al., 1991). Weddige (1996) assigned the formation to the lower Givetian, hemiansatus Biozone, but it cannot be ruled out that this unit may also represent a lower part of the timorensis Biozone. The stratigraphical position of the Kerpen Formation was established based on a bipennatus–lilliputensis fauna that occurs in upper part of obliquimarginatus Biozone (Weddige, 1988; Loboziak et al., 1991). The obliquimarginatus Biozone includes the entire hemiansatus Biozone and the lower part of the timorensis Biozone (Bultynck, 1987; Bultynck and Gouwy, 2008). The species Bipennatus bipennatus (Bischoff and Ziegler, 1957) and Icriodus lilliputensis Burjack et al., 1987 cooccurring in the Kerpen fauna first appear in upper part of the hemiansatus Biozone determining the position of the lower part of the formation. The first appearance of S. triangulatus in the Lower Givetian is quite exceptional as all other records show that this event occurs in Middle Givetian (Richardson and McGregor, 1986; McGregor and Playford, 1992; Avkhimovitch et al., 1993; Turnau and Racki, 1999; Obukhovskaya, 2000; Marshall et al., 2007). Therefore, the assignment of the Kerpen specimens to S. triangulatus is, in our opinion, debatable (see Section 4).

3.4. Aneurospora extensa (Naumova) Turnau, 1996 The apparently sudden disappearance in the Givetian of Aneurospora extensa and of several spore taxa, such as Geminospora compta (Naumova) Arkhangelskaya, 1987, Lanatisporis bislimbatus (Tschibrikova) McGregor and Camfield, 1982, and Kraeuselisporites spinutissimus, at the boundary between two palynological zones is known from a wide territory of Eastern Europe (Obukhovskaya, 2000). The event corresponds to the boundary between the Geminospora extensa (EX) and the Contagisporites optivus–Spelaeotriletes krestovnikovii (OK) Biozones of Avkhimovitch et al. (1993), and between the Geminospora extensa (Ex) and Geminospora aurita (Aur) spore Biozones of Turnau (1996, 2007). But in Russia, the position of this boundary is not known, because there is a disconformity separating the Mullino and Pashia Horizons corresponding respectively to the EX and IM Biozones (Rzhonsnitskaya, 2000). The event has also been described from Poland (Turnau and Racki, 1999; Turnau, 2008).

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In the Terebin IG 5 borehole, the impoverished spore assemblage lacking Aneurospora extensa first occurs in the Rachanie Member of the Telatyn Formation at a depth of 1540.62 m, above c. 12 m thick interval barren of spores (Fig. 3). Conodont elements found c. 11 m below possibly represent the subterminus Biozone (based on occurrence of Icriodus subterminus). In the Giełczew PIG 5 borehole, the discussed assemblage first occurs in the Giełczew Member of the Telatyn Formation at a depth of 1999.08 m, above c. 5 m spore barren interval (Fig. 2). This level is sandwiched between conodont samples indicating the ansatus Biozone (c. 3 m below) and ansatus–subterminus Biozones (c. 20 m above). These data are not very precise suggesting that the position of the extinction event under discussion is within the range ansatus–subterminus Biozones. According to Turnau and Racki (1999, fig. 4, tab. 2), in the Holy Cross Mts., Aneurospora extensa disappears in unit XXVIIIB at Włochystudnia locality, where the spore assemblages are associated with limited conodont fauna that includes I. difficilis Ziegler and Klapper, 1976 and P. linguiformis Hinde, 1879 morphotype gamma. This fauna was interpreted as representing the hermanni Biozone because its taxonomic composition was similar to that from the same unit (in a different locality) that supposedly contained Schmidtognathus sp. (Malec and Turnau, 1997). However, it appears that a representative of that genus occurs only in the succeeding unit (see discussion in WoroncowaMarcinowska, 2005). The composition of the conodont assemblage from the Włochy-studnia locality alone is indicative of biozones in the range of rhenanus/varcus to hermanni. The combined data discussed above suggest that the Givetian spore extinction event is within the range of ansatus to hermanni Biozones. It is obvious that more work is needed to establish its exact position. 3.5. Corystisporites pomeranius Stempień-Sałek, 2002 This is a distinct species known from Belarus (Obukhovskaya, 2000), and Poland — from the study area, and Western Pomerania (Stempień-Sałek, 2002; Turnau, 2007, 2008). It is considered characteristic of the Acanthotriletes bucerus–Archaeozonotriletes variabilis insignis (BI) Biozone that spans the Givetian/Frasnian boundary (Obukhovskaya, 2000). The position of its first occurrence has not, so far, been precisely established in terms of conodont zonation. In the study area, the species first appears in the Giełczew PIG 5 borehole, in the Giełczew Member of the Telatyn Formation (Fig. 2) at a depth of 1965.45 m. Below, in the same unit, in the 30 m thick sequence, seven samples did not contain its representatives. Conodont elements indicative of the Lower, and, possibly, the Upper falsiovalis Biozone were found in samples from below this level. The fauna from depth 1969.7 m contained I. subterminus, Pan. cf. Pandorinellina insita, and P. webbi (Narkiewicz and Bultynck, 2007, tab. 2) which indicates the presence of the Lower falsiovalis Biozone (Upper subterminus Subbiozone). The fauna from the higher sample (depth 1967.1 m) contained elements assigned to I. subterminus and, notably, to I. cf. I. symmetricus Branson and Mehl, 1938 (Narkiewicz and Bultynck, 2007, fig. 5N). The analysis of the stratigraphical range of I. symmetricus, based on data from various regions (Narkiewicz and Bultynck, 2010) reveals that the first appearance of this taxon, the index species of the symmetricus Biozone, is in the interval comprising the upper part of the MN 1 Biozone and the lower part of the MN 2 Biozone (Lower–Upper falsiovalis Biozone, see Fig. 4). Unfortunately, the assignment of elements from Giełczew PIG 5 borehole, sample at 1967.1 m, to the species under discussion is uncertain, hence the placement of the Frasnian lower boundary in this section (Fig. 2) is only tentative. Conodonts were also found in this borehole in the succeeding Lipowiec Member of the Modryń Formation. The assemblage included two representatives of P. cf. P. denisbriceae Bultynck, 1970. The last occurrence of this species is in the interval MN 1–MN 2 corresponding to the Upper falsiovalis Biozone (Klapper, 1997; Ovnatanova and Kononova, 2008; Narkiewicz and Bultynck, 2010).

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It follows that Corystisporites pomeranius first appears in the falsiovalis Biozone, and likely in the upper part of Lower falsiovalis or in Upper falsiovalis Biozones. In the Terebin IG 5 borehole, Corystisporites pomeranius occurs in the Rachanie Member of the Telatyn Formation (Fig. 3) at a depth of 1525.92 m. In the 79 m thick sequence below, in the same member and in the underlying two members, twelve samples did not contain its representatives. The conodont elements from sample at 1551.2 m (first appearance in the section of I. subterminus and, moreover the occurrence of P. alatus and Polygnatghus xylus — Narkiewicz and Bultynck, 2007, tab. 4, fig. 10N–10O) probably represent the subterminus Zone. The species Corystisporites pomeranius has also been recorded from conodont-bearing sections in Western Pomerania (Turnau, 2007, 2008), but good recovery of conodonts starts only from the transitans– punctata Biozones (Matyja, 2007, 2008).

3.6. Multifurcate spinose spores Ancyrate (bifurcate or multifurcate) exoexinal processes (born by spores that are otherwise structurally distinct) are features typical of Middle and Upper Devonian spore assemblages. Bifurcate spinose spores are typical of the Middle Devonian while multifurcate processes are encountered in the Upper Devonian (McGregor et al., 1985), their first appearance is considered to be near the Middle/ Upper Devonian boundary (Richardson and McGregor, 1986). In the study area, the presence of multifurcate processes (born by Ancyrospora spp., see Plate I) was first noted in the Giełczew PIG 5 borehole, in the Giełczew Member of the Telatyn Formation (Fig. 2), at a depth of 1965.45 m. Below, in the same unit, in the 30 m thick sequence, seven samples did not contain spores of that morphology. Conodont elements indicative of the upper part of Lower falsiovalis or in Upper falsiovalis Biozones were found in samples from below this level, and those implying a position not above the Upper falsiovalis Biozone were found in the overlying unit (for details see Section 3.5). It follows that multifurcate spiny spores first appear in the falsiovalis Biozone, and more likely in the Upper falsiovalis Biozone. In Boullonais, the first entry of multifurcate-spined species Hystricosporites multifurcatus (Winslow) Mortimer and Chaloner, 1967 is in the Noces Member of the Beaulieu Formation, in bed 5 of unit O (Brice et al., 1981; Loboziak and Streel, 1981). The zonal species Verrucosisporites bulliferus Richardson and McGregor, 1986 (marking the base of the bulliferus–media Biozone of Streel et al., 1987) first appears in the same sample. Conodonts were recovered from samples 34 and 35 derived from the same member, from the overlying unit P (Brice et al., 1979, tab. III). It was suggested by Brice et al. (1981) that the assemblages represented the Middle asymmetricus Biozone (punctata Biozone in the “standard” conodont zonation). The recent revision of conodont associations from these samples revealed the presence of Ancyrodella gigas form 1 Klapper, 1985 (P. Bultynck, personal communication, 06. 2010). The same taxon occurs in the higher unit R (Brice et al., 1979, pl. XXVII, fig. 14). Based on the presence of this species and of Polygnathus asymmetricus ovalis Ziegler and Klapper, 1964 (Brice et al., 1979, pl. XXVII, fig. 14) – now Mesotaxis ovalis – the conodont assemblage from the samples nearest to the spore level may be assigned to the interval of middle part of MN 4 to MN 5, i.e. transitans to punctata Biozones (Klapper, 1997; Ziegler and Sandberg, 1990). Conodonts occur also in the strata underlying the Noces Member, in the Cambresèque member, sample 32 (Brice et al., 1979). This fauna that was recently revised by Narkiewicz and Bultynck (2010, tab 7) represents the interval MN 3 to MN 4 (Upper falsiovalis to transitans Biozones). It follows that the base of the bulliferus–media Biozone, and the first appearance of multifurcatespined spores in Boulonnais are within the range Upper falsiovalis to punctata Biozones, probably, as suggested by Streel (2009, fig. 1), in the transitans Biozone.

3.7. Tholisporites densus McGregor, 1960 Distinct morphology and wide lateral distribution make Tholisporites densus important for stratigraphy, its first appearance marks the base of the Den Biozone (Turnau, 2007). This species has been recorded from the Frasnian of Arctic Canada (McGregor, 1960; McGergor and Uyeno, 1972), Australia (McGregor and Playford, 1992), Russian Platform (Raskatova, 1969; Arkhangelskaya, 1987, Avkhimovitch et al., 1993). According to McGregor and Playford (1992), in Canada the species is thought to appear in the latest Givetian. The position of its first occurrence has not, so far, been precisely established in terms of conodont zonation. In the study area, Tholisporites densus was encountered in one sample from the Giełczew PIG 6 borehole. The sample is derived from the top part of the Giełczew Member of the Telatyn Formation (Fig. 2) taken at a depth of 2007.5 m — less than 1 m below the boundary with the Modryń Formation. The sample below (depth 2009.3 m) did not contain this species. Conodont elements (of the transitans–linguiformis Biozones) occur only much higher in the section and are not helpful for the present discussion but the conodont data from the Giełczew PIG 5 borehole may be useful, the two wells are only 400 m apart. The fauna found in the Giełczew PIG 5 borehole in the top part of the Giełczew Member, at a depth of 1967.1 m, may suggest the presence of the upper part of Lower falsiovalis or Upper falsiovalis Biozone, and the fauna from c. 3 m above the base of this formation is not younger than this biozone (for details see Section 3.5). It follows that Tholisporites densus first appears in the falsiovalis Biozone, and probably within the range of MN 1–MN 2, i.e. in the upper part of Lower falsiovalis or in Upper falsiovalis Biozone. The discussed species has also been recorded from conodont-bearing sections in Western Pomerania (Turnau, 2007, 2008), but good recovery of conodonts starts only from the transitans–punctata Biozones (Matyja, 2007, 2008). 4. Taxonomic comments on selected taxa 4.1. Spores Corystisporites pomeranius Stempień-Sałek, 2002 (Plate I, 11) 2000 Perotrilites (?) vermiculatus Medyanik in litt., Obukhovskaya, fig. 5 (9), (nomen nudum). 2002 Corystisporites pomeranius Stempień-Sałek, p. 173, fig. 7 (A–C). Description of specimens: Zonate spores, rounded triangular in outline. Spore body 82–98 μm in diameter, triradiate rays extending almost to equator, with lips 10 μm high at the apex, diminishing in height towards equator. In the region of the proximal pole the exine is thicker forming a darker area similar in outline to the outline of the spore body. Zona is about 1/6 spore body radius interradially, and 1/4 to 1/5 of the radius at the apices. Distal spore surface is ornamented with closely spaced spines usually 3 μm in length. Bases of neighboring spines may fuse to form rugulae. Remarks: According to Stempień-Sałek (2002), the overlapping basal parts of ornamentation elements appear as deeply incised zona. However, examination of numerous specimens from Western Pomerania and the study area, reveals that the zona is entire, and thus the taxon should be better accommodated in Kraeuselisporites. Samarisporites triangulatus Allen, 1965 (Plate I, 9) non? 1991 Samarisporites triangulatus (Allen, 1965; Loboziak et al., pl. 2, figs. 4–12) Remarks: As noted by McGregor et al. (1985) “The species, as it has been circumscribed by some authors, may be divisible into two or more species with distinct stratigraphic ranges”. The most notable feature of this species is the presence of equatorial zona that is narrow or absent at interradial margins and wide at radial apices where it forms conspicuous extensions. This feature is not exclusive to Samarisporites triangulatus, there are species similar in structure, but differing in other

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characteristics, especially in sculpture. In S. triangulatus sensu Allen, the proximal surface is laevigate, distally the central area supports a variable ornament of conical elements, occasionally fused forming cristae or an imperfect reticulum; the zona is laevigate or with a sparse ornament of small cones. The specimens from the study area conform to that description. Specimens from the Kerpen Formation posses small radial extensions and they appear on illustrations given in Loboziak et al. (1991) as being distally ornamented by a faint perfect reticulum. In the opinion of Streel (2009) these atypical spores represent an “early form” of the discussed species. In our opinion, the Kerpen specimens may not represent S. triangulatus not only because their radial extensions are small, but also they are distally ornamented by a fine, perfect reticulum. However, only direct observations of the Loboziak et al. slides or new Kerpen material could clarify this problem.

the Ex 2 Subbiozone, are not above the ansatus Zone, probably within the range of rhenanus/varcus to ansatus Biozones. The first occurrence of the zonal species Samarisporites triangulatus, and the base of the Ex 3 Subbiozone are in the ansatus Biozone. The disappearance of Aneurospora extensa accompanied by disappearance of numerous taxa, and the base of the Aur Biozone are within the range of ansatus to hermanni Biozones. The first occurrence of Corystisporites pomeranius and multifurcate-spined spores is within the falsiovalis Biozone, and more likely in Upper falsiovalis Biozone. The first occurrence of Tholisporites densus, and the base of the Den Biozone are in the falsiovalis Biozone, and more likely in Upper falsiovalis Biozone (based on lithostratigraphic correlation between neighboring boreholes).

4.2. Conodonts

Acknowledgements

Icriodus aff. I. eslaensis Van Adrichem Boogaaert, 1967 1997 Icriodus eslaensis Van Adrichem Boogaaert, 1967; Malec and Turnau, pl. I, fig. 9 (only). Remarks: The specimen assigned by Malec and Turnau (1997, pl. I, fig. 9) to I. eslaensis has been included by the present authors in Icriodus aff I. eslaensis because in this specimen the posterior extension is too short and it bears only two denticles, while in typical representatives of I. eslaensis there are three to five denticles. Icriodus arkonensis walliserianus Weddige, 1988

We would like to thank Pierre Bultynck and Marek Narkiewicz for discussion and help in solving problems related to stratigraphy. Thanks are also due to Lech Miłaczewski and Gordon D. Wood for providing the palynological samples, and to Leszek Chudzikiewicz and Janek Turczynowicz for the technical assistance with figures and plate. Thanks are also due to Professor Maurice Streel and to the anonymous reviewer for constructive reviews.

1997 Icriodus eslaensis Van Andrichem Boogaaert, 1988; Malec and Turnau, pl. I, fig. 13. 1997 Icriodus sp.; Malec and Turnau, pl. I, fig. 11. Remarks: This subspecies has been identified based on illustrations in Malec and Turnau (1997, pl. 1, figs. 11, 13). In that paper, the respective specimens were assigned to I. eslaensis and Icriodus sp. In both cases, the anterior ending of the spindle is contracted and extended as compared to the posterior one, which is typical of specimens of I. arkonensis walliserianus, similarly as the facts that the denticles of the middle row are positioned almost opposite those of the lateral rows, and the denticles of the lateral rows are larger than those of the middle row, and are elliptically extended. In representatives of I. eslaensis, the denticles of the middle row alternate with those of the side rows, and they are distinctly shifted forward. Also, the denticles of the side rows are rounded and are almost of the same size as those of the middle row. Polygnathus pseudofoliatus Wittekind, 1966 1997 Polygnathus pseudofoliatus Wittekind, 1966; Malec and Turnau, pl. II, fig. 6. 1997 Polygnatghus xylus xylus Stauffer, 1940; Malec and Turnau, pl. II, figs. 4, 5. Remarks: We have included in this species the specimens assigned by Malec and Turnau (1997, pl. III, figs. 4. 5) to Polygnatghus xylus xylus Stauffer, 1940. The figured specimens are ornamented while typical representatives of P. xylus xylus have a smooth platform devoid of ornamentation (see diagnosis in Klapper et al., 1970). The figured specimens probably represent intermediate stages of Polygnathus pseudofoliatus, as they are derived from the same sample in which the adult specimen of this species has been correctly recognized (see Malec and Turnau, 1997, pl. III, fig. 6). 5. Conclusions Givetian and ?Frasnian conodont faunas have been reported from spore-bearing sections in the Lublin area. This allows definition of spore species first appearance biohorizons in terms of conodont zonations, and enables to intercalibrate spore zonation scheme for Western Pomerania with the “standard” and alternative conodont zonations. The first occurrence of the zonal species Chelinospora concinna and the distinctive species Kraeuselisporites spinutissimus, and the base of

References Allen, K.C., 1965. Lower and Middle Devonian spores of North and Central Westspitsbergen. Palaeontology 8, 687–748. Allen, K.C., 1982. Samarisporites triangulatus Allen 1965, an important Devonian miospore and its synonymous species. Pollen et Spores 24, 157–166. Arkhangelskaya, A.D.A., 1987. Novyi rod i nekotorye vidy spor franckogo yarusa Volgogradskoi oblasti. Geologicheski Zhurnal 3, 84–91 (in Russian). Avkhimovitch, V.I., Tchibrikova, E.V., Obukhovskaya, T.G., Nazarenko, A.M., Umnova, V.T., Raskatova, L.G., Mantsurova, V.N., Loboziak, S., Streel, M., 1993. Middle and Upper Devonian miospore zonation of Eastern Europe. Bul. Centr. Recher. Explor.-Product. Elf-Aquitaine 17, 79–147. Becker, R.T., House, M.R., 1994. International Devonian goniatite zonation, Emsian to Givetian, with new records from Morocco. Cour. Forsch.-Inst. Senckenberg 169, 79–135. Brice, D., Bultynck, P., Deunff, J., Loboziak, S., Streel, M., 1979. Données biostratigraphiques nouvelles sur le Givétien et le Frasnien de Ferques (Boulonnais, France). Ann. Soc. Geol. Nord. XCVIII, 325–344. Brice, D., Coen, M., Loboziak, S., Streel, M., 1981. Précisions biostratigraphiques relatives ou Dévonien supérieur de Ferques (Boulonnais). Ann. Soc. Geol. Nord., C 159–166. Bultynck, P., 1987. Pelagic and neritic conodont successions from the Givetian of preSahara Morocco and the Ardennes. Bull. Inst. Roy. Sc. Nat. Belgique, Sc. terre 57, 149–181. Bultynck, P., Gouwy, S., 2008. Reference sections for the Middle Givetian substage. Subcommission on Devonian Stratigraphy Newsletter, 23, pp. 21–26. Burjack, M.I.A., Loboziak, S., Streel, M., 1987. Quelques données nouvelles sur les miospores dévoniennes du Bassin du Paran (Brésil). Sci. Géol., Bull. 40, 381–391. Higgs, K., Streel, M., 1984. Spore stratigraphy at the Devonian–Carboniferous boundary on the northern “Rhenisches Schefergebirge“, Germany. Cour. Forsch.-Inst. Senckenberg 67, 157–179. Huddle, J.W., Repetski, J.E., 1981. Conodonts from the Genesse Formation in western New York. Geol. Surv. Prof. Pap. 1032 (B), 1–66. Klapper, G., 1997. Graphic correlation of Frasnian (Upper Devonian) sequences in Montagne Noire, France, and western Cnada. Geol. Soc. Amer. Spec. Pap. 321, 113–129. Klapper, J., Johnson, J.G., 1980. Endemism and dispersal of Devonian conodonts. J. Paleont. 54, 400–455. Klapper J., Johnson J.G. 1990. Revisions of Middle Devonian conodont Zones. In: Johnson, J.G. (Ed.), Lower and Middle Devonian brachiopod dominated communities of Nevada, and their position in a biofacies-provinces-realm model. J. Paleont., 64, 934–941. Klapper, G., Philip, G.M., Jackson, J.H., 1970. Revision of the Polygnathus varcus group (Conodonta, Middle Devonian). N. Jahrb. f. Geol. Paläont., Monatsh. 11, 650–657. Loboziak, S., Streel, M., 1980. Miospores in Givetian to Lower Frasnian sediments dated by conodonts from the Boulonnais, France. Rev. Palaeobot. Palynol. 29, 285–299. Loboziak, S., Streel, M., 1981. Miospores in middle–upper Frasnian to Famennian sediments partly dated by conodonts (Boulonnais, France). Rev. Palaeobot. Palynol. 34, 49–66. Loboziak, S., Streel, M., 1995. Late Lower and Middle Devonian miospores from Saudi Arabia. Rev. Palaeobot. Palynol. 89, 105–113. Loboziak, S., Streel, M., Burjack, M.I.A., 1988. Miospores du Dévonien Moyen et Supérieur du Basin du Parana, Brésil: systématique et stratigraphie. Sci. Géol. Bull. 41, 351–377.

38

E. Turnau, K. Narkiewicz / Review of Palaeobotany and Palynology 164 (2011) 30–38

Loboziak, S., Streel, M., Weddige, K., 1991. Miospores, the lemurata and triangulatus levels and their faunal indices near the Eifelian/Givetian boundary in the Eifel (F.R.G.). Ann. Soc. Geol. Belg. 113, 299–313. Loboziak, S., Avkhimovitch, V.I., Streel, M., 1995. Miospores from the type locality of the Esneux Formation, Middle Famennian of the Ourthe valley, eastern Belgium. Ann. Soc. Geol. Belg. 117, 95–102. Malec, J., Turnau, E., 1997. Middle Devonian conodont, ostracod and miospore stratigraphy of the Grzegorzowice–Skały sections, Holy Cross mountains, Poland. Bull. Pol. Acad. Sci. Earth Sci. 45, 67–86. Marshall, J.A.E., Astin, T.R., Brown, J.F., Mark-Kurik, E., Lazauskiene, J., 2007. Recognizing the Kačák Event in the Devonian terrestrial environment and its implications for understanding land–sea interactions. In: Becker, R., Kirchgasser, W.T. (Eds.), Devonain Events and Correlations, 278. Geol. Soc. London, Spec. Publ., pp. 133–155. Matyja, H., 2007. Lito- i biostratygrafia. In: Matyja, H. (Ed.), Polskie Łąki PIG 1, Profile Głebokich otworów wiertniczych Państwowego Instytutu Geologicznego, 122. Państwowy Instytut Geologiczny Warszawa, pp. 54–62. Matyja, H., 2008. Lito- i biostratygrafia osadów dewonu obszaru pomorskiego. In: Matyja, H. (Ed.), Jamno IG 1, IG 2, IG 3, Profile Głebokich otworów wiertniczych Państwowego Instytutu Geologicznego, 124. Państwowy Instytut Geologiczny Warszawa, pp. 117–125. Maziane, N., Higgs, K., Streel, M., 1999. Revision of the late Famennian miospore zonation scheme in eastern Belgium. J. Micropalaeont. 18, 17–25. McGergor, D.C., Uyeno, T.T., 1972. Devonian spores and conodonts of Melville and Bathurst islands, District of Franklin. Geol. Surv. Can. Paper 71-13, 1–36. McGregor, D.C., 1960. Devonian spores from Melville Island, Canadian Arctic Archipelago. Palaeontology 3, 26–44. McGregor, D.C., Camfield, M., 1982. Middle Devonian miospores from the Cape de Bray, Weatherall and Hecla Bay formations of northeastern Melville Island, Canadian Arctic. Geol. Surv. Can. Bull. 348, 1–104. McGregor, C.D., Playford, G., 1992. Canadian and Australian Devonian spores: zonation and correlation. Geol. Surv. Can. Bull. 438, 1–125. McGregor, D.C., Norris, A.W., Uyeno, T.T., 1985. Intra Devonian Series Boundaries in Canada. Cour. Forsch.-Inst. Senckenberg 75, 157–176. Miłaczewski, L., 1981. Dewon południowo-wschodniej Lubelszczyzny. Prace Państwowego Instytutu Geologicznego, 101, 5–90. Miłaczewski, L., Radlicz, K., Nehring, M., Hajłasz, B., 1983. Osady dewonu w podłożu zachodniej części lubelskiego odcinka niecki brzeżnej. Biuletyn Instytutu Geologicznego, 344, 23–56. Narkiewicz, K., Bultynck, P., 2007. Conodont biostratigraphy of shallow marine Givetian deposits from the Radom–Lublin area, SE Poland. Geol. Quart. 51, 419–442. Narkiewicz, K., Bultynck, P., 2010. The Upper Givetian (Middle Devonian) subterminus conodont Zone in North America, Europe and North Africa. J. Paleont. 84 (4), 588–625. Narkiewicz, M., Miłaczewski, L., Krzywiec, P., Szewczyk, J., 1998. Zarys architektury depozycyjnej basenu dewońskiego na obszarze radomsko-lubelskim. Prace Państwowego Instytutu Geologicznego, 165, 57–72. Obukhovskaya, T.G., 2000. Miospores of the Givetian–Frasnian boundary deposits in Belarus. Acta Palaeobot. 40, 17–23. Ovnatanova, N.S., Kononova, L.T., 2008. Frasnian conodonts from the Eastern Russian Platform. Paleont. J. 42, 997–1166.

Pożaryski, W., Dembowski, Z. (Eds.), 1983. Mapa geologiczna Polski i krajów ościennych bez utworów kenozoicznych, mezozoicznych i permskich 1:1 000 000. Inst. Geol. Warszawa. Raskatova, L.G., 1969. Sporovo-pyltsevye kompleksy srednego i verkhnego Devona jugo-vostochno chasti centralnogo devonskogo polya. Izdatelstvo. Voronezhkogo Universiteta. Voronezh. (in Russian). Richardson, J.B., McGregor, D.C., 1986. Silurian and Devonian spore Zones of the Old Red Sandstone Continent and adjacent regions. Geol. Surv. Can. Bull. 364, 1–79. Rzhonsnitskaya, M.A., 2000. Devonian stage boundaries on the East European (Russian) Platform. In: Bultynck, P. (Ed.), Subcommission on Devonian Stratigraphy Recognition of Devonian Series and Stage Boundaries in Geological Areas, 225. Cour. Forsch.-Inst, Senckenberg, pp. 227–237. Stempień-Sałek, M., 2002. Miospore taxonomy and stratigraphy of Upper Devonian and lowermost Carboniferous in Western Pomerania (NW Poland). Ann. Soc. Geol. Pol. 72, 163–190. Streel, M., 2009. Upper Devonian miospore and conodont zone correlation in western Europe. In: Königshof, P. (Ed.), Devonian Change: Case Studies in Palaeogeography and Palaeoecology, 314. Geol. Soc. London, Spec. Publ., pp. 163–176. Streel, M., Loboziak, S., 1996. Middle and Upper Devonian miospores. In: Jansonius, J., McGregor, D.C. (Eds.), Palynology: Principles and Applications, 2. Amer. Assoc. Stratigr. Palynol. Foundation, pp. 575–587. Streel, M., Higgs, K., Loboziak, S., Riegel, W., Steemans, P., 1987. Spore stratigraphy and correlation with faunas and floras in the type marine Devonian of the Ardenne– Rhenish regions. Rev. Palaeobot. Palynol. 50, 211–229. Turnau, E., 1996. Miospore stratigraphy of Middle Devonian deposits from Western Pomerania. Rev. Palaeobot. Palynol. 93, 107–125. Turnau, E., 2007. Palinostratygrafia. In: Matyja, H. (Ed.), Polskie Łąki PIG 1, Profile Głebokich otworów wiertniczych Państwowego Instytutu Geologicznego, 122. Państwowy Instytut Geologiczny Warszawa, pp. 62–69. Turnau, E., 2008. Wyniki badań palinostratygraficznych. In: Matyja, H. (Ed.), Jamno IG 1, IG 2, IG 3, Profile Głebokich otworów wiertniczych Państwowego, Instytutu Geologicznego, vol. 124, pp. 125–135. Państwowy Instytut Geologiczny Warszawa. Turnau, E., Racki, G., 1999. Givetian palynostratigraphy and palynofacies: new data from the Bodzentyn Syncline (Holy Cross Mountains, central Poland). Rev. Palaeobot. Palynol. 106, 237–271. Weddige, K., 1988. Systematic Paleontology. In: Ziegler, W. (Ed.), Guide to Field Trips, Part 1, 102. Cour. Forsch.-Inst. Senckenberg, pp. 154–155. Weddige, K., 1996. Devonian Korrelationstabelle. Senckenbergiana Lethaea 76 (1/2), 267–286. Woroncowa-Marcinowska, T., 2005. Middle Devonian conodonts from black shales of the Ścignia section, Góry Świętokrzyskie Mountains, central Poland. In: Tyszka, J., Oliwkiewicz-Miklasińska, M., Gedl, P., Kaminski, M.A. (Eds.), Methods and Applications in Micropalaeontology, 124. Studia Geol. Pol, pp. 159–170. Ziegler, W., Klapper, G., 1982. The disparilis Conodont Zone, the proposed level for the Middle–Upper Devonian boundary. Cour. Forsch.-Inst. Senckenberg 55, 463–491. Ziegler, W., Sandberg, C.A., 1990. The Late Devonian standard conodont zonation. Cour. Forsch.-Inst. Senckenberg 121, 10115.