Conodont, Miospore and Ostracod Zones Compared

Annales Societatis Geologorum Poloniae (2000), vol. 70: 193-217.

LOWER CARBONIFEROUS (MISSISSIPPIAN) STRATIGRAPHY OF NORTHWESTERN POLAND: CONODONT, MIOSPORE AND OSTRACOD ZONES COMPARED

Hanna MATYJA1, Elżbieta TURNAU2 & Barbara ŻBIKOWSKA1

1 Polish Geological Institute, Rakowiecka 4, 00-975 Warszawa, Poland ~ Institute o f Geological Sciences, Polish Academy o f Sciences, Kraków Research Center, Kraków, Senacka I, 31-002 Kraków, Poland

Matyja, H., Turnau, E. & Żbikowska, В., 2000. Lower Carboniferous (Mississippian) stratigraphy of northwestern Poland: conodont, miospore and ostracod zones compared. Annales Societatis Geologorum Poloniae, 70:193-217.

Abstract: Detailed stratigraphy of the Tournaisian and Visean in western Pomerania has been established on conodonts, miospores and ostracods recovered from 25 boreholes. Miospore associations from the Tournaisian and Visean are assigned to nine biostratigraphic units (zones and subzones) erected earlier. Three successive benthic ostracod assemblages and two sub-assemblages are distinguished for the Tournaisian. The miospore zones/sub­ zones and the ostracod assemblages/subassemblages are correlated with the Tournaisian sandbergi, Lower crenu- lata, isosticha-XJppex cremilata, and typicus conodont zones. Stratigraphic gap has been demonstrated at the Devonian/Carboniferous boundary, using the results of both conodont and miospore studies. The Tournaisian/ Visean boundary has been established approximately on the first appearance of the miospore species Lycospora pusilla Somers.

Abstrakt: Przedstawiono szczegółową stratygrafię turneju i wizenu Pomorza Zachodniego w oparciu o kono- donty, miospory i małżoraczki. Materia! do badań biostratygraficznych pochodził z 25 otworów wiertniczych. Zespoły miospor z badanych utworów zaliczono do dziewięciu wcześniej wyróżnionych jednostek biostratygra­ ficznych (zon i podzon). Dla turneju wyróżniono trzy kolejne zespoły i dwa podzespoły małżoraczków bento- nicznych. Zony/podzony miosporowe i zespoły/podzespoły małżoraczkowe skorelowano z turnejskimi zonami konodontowymi sandbergi, dolna crenulata, isosticha-górna crenulata i typicus. Obecność luki stratygraficznej na granicy dewon/karbon udokumentowano na podstawie konodontów i miospor. Granica turnej/wizen została ustalona jedynie w przybliżeniu, na podstawie pierwszego pojawienia się gatunku miosporowego Lycospora pusilla Somers.

Key words: Tournaisian, Visean, biostratigraphy, conodonts, miospores, ostracods, western Pomerania.

Manuscript received 27 April 2000, accepted 27 October 2000

INTRODUCTION

Lower Carboniferous strata have been recorded in a even on folded lower Palaeozoic rocks (e.g., the Brda 2 number of wells drilled in the coastal part of western Pom­ borehole). This is due to a local tectonic and erosional epi­ erania and in the Koszalin-Chojnice area (Fig. 1). These sode, which took place at the end of the Devonian and dur­ strata were also encountered, but not pierced through, in ing the Tournaisian. The Tournaisian strata are, in most several wells located southwest of the latter area (Żeli­ cases, discordantly overlain by Permian sediments but in chowski, 1983; Żelichowski & Łoszewska, 1987). several sections near Sarbinowo, Karsina and Gozd, it is the In the study area, the lowermost Tournaisian is devel­ lower Visean which underlies the Permian rocks. Younger oped as the Sąpolno Calcareous Shale Formation, the base strata have been penetrated only in the Sarbinowo 1 section of which is Famennian in age (Matyja, 1993). It is likely that where the middle and upper Visean deposits rest uncon­ sedimentation was continuous across the Devonian-Car­ formably on the Ordovician (Bednarczyk, 1974), and are boniferous boundary, although a distinct stratigraphic gap discordantly overlain by the Westphalian. has been noted in some sections (Matyja & Stempień-Sałek, So far, the uppermost Visean and Namurian deposits 1994). In a few sections, however, different units of the have not been recorded in western Pomerania. The top of Tournaisian rest unconformably either on the lower Famen­ the Lower Carboniferous strata is probably of erosional nian (especially in the sections located in the Gozd area), or character and the documented gap spans the topmost 194 H. MATYJA ET AL.

15°00' 16°00' 17°00' 18°00‘

S arbinow o

G rzybow o Gprzy§ł5w9^

54°00'-

Tournaisian and Visean CHOJNICI Upper Ordovician O Devonian and Silurian Middle Teisseyre-Tornquist Devonian tectonic line 25 km

Fig. 1. Location of discussed boreholes against the geological map of pre-Permian deposits in western Pomerania. Geology after Ma­ tyja, 1993, Lipiec & Matyja, 1998, modified. Insert - position of study area

Visean, Namurian and lower part of Westphalian. logical logs as well as some old palynological slides have Toumaisian and Visean deposits in the Kołobrzeg- been reexamined. The here presented interpretation uses the Chojnice area show a great lithological variability. Incom­ upgraded miospore zonal scheme (see Subsection Zonal plete coring coupled with insufficient biostratigraphical schemes) and the results of recent miospore studies in Po­ data have been the main obstacles in reconstructing tire pat­ land and elsewhere. tern of development of the Devonian-Carboniferous suc­ Because our faunal and palynological samples are de­ cession. The first attempt to present the arrangement of the rived from the same boreholes, we were able to calibrate the Carboniferous lithological bodies and their general deposi- conodont, ostracod and miospore zonation schemes used. In tional environments, was that by Dadlez (1978). Żelichow­ this respect, we also discuss some macrofaunal data pub­ ski (1983, 1995; in Żelichowski & Łoszewska, 1987) re­ lished by Korejwo (1993). Our integrated biostratigraphic vised Dadlez’s lithostraphical division and subdivided database permitted to correlate the lithostratigraphic units Lower Carboniferous strata into several informal units and to date their boundaries. called complexes. For prospecting purposes more detailed The studies have been earned out in the Institute of division into units called “series” has been introduced by Geological Sciences of the Polish Academy of Sciences, Lech (1986). Recently, Lipiec (in Lipiec & Matyja, 1998) and in the Department of Regional and Petroleum Geology modified the division of Żelichowski. of the Polish Geological Institute. Early biostratigraphic investigations of the Carbonifer­ ous deposits in the studied area centered on macro- and mi­ crofauna (Błaszyk & Natusiewicz, 1973; Korejwo, 1976, LITHOSTRATIGRAPHY 1979; Matyja, 1976), and spores (Krawczyńska-Grochol- ska, 1975; Tumau, 1975, 1978, 1979; Górecka & Parka, The lithostratigraphic division used in the present paper 1980). A generalized summary of the biostratigraphic divi­ is that by Lipiec (in Lipiec and Matyja, 1998). Inferred spa­ sion based both on published and unpublished data, was tial relationships between the lithostratigraphic units are presented by Żelichowski & Łoszewska (1987). Some opin­ shown in Fig. 2. These relationships reflect a general regres­ ions on age assignements expressed in the earliest papers, sive tendency from an open shelf during the Famennian- were later revised (Matyja & Turnau, 1989; Clayton & Tur- middle Tournaisian (Sqpolno Calcareous Shale Formation), nau, 1990; Avkhimovitch et a!., 1993; Matyja, 1993; Ma­ through very shallow marine in the late Tournaisian (Ku- tyja & Stempień-Sałek, 1994), and the miospore zonal rowo Oolite Formation and Grzybowo Shale Member) to scheme proposed by Tumau (1978, 1979) was partly rede­ terrestrial environment during the latest Toumaisian (Drze- fined by Avkhimovitch & Tumau (1994) and upgraded by wiany Sandstone Formation). The Gozd Arkose Formation Stempień-Sałek (in Matyja & Stempień-Sałek, 1994). reflects the Tournaisian volcanic activity episodes. The details of the conodont and ostracod stratigraphy discussed in this paper are new. On the other hand, the mio­ Sqpolno Calcareous Shale Formation spore part involves only the sample material interpreted ear­ The uppermost Devonian-lowermost Carboniferous lier by Tumau (1975, 1978, 1979), and Avkhimovitch & Scipolno Calcareous Shale Formation overlies the Devonian Tumau (1994). Recently, all previously completed palyno- Krojanty and Klanino formations throughout the investi­ LOWER CARBONIFEROUS STRATIGRAPHY 195

gated area (see fig. 8 in Matyja, 1993). It is a succession of open marine carbonate and clayey deposits. The lower, Fa- Drzewiany Sandstone Formation mennian part of the formation consists of two lithofacies: (1) fossiliferous marly limestones in the shallower part of the basin (northern part of the area), and (2) fossiliferous Grzybowo Shale ------^ marls with thin intercalations of organodetrital limestones Member Kurowo Oolite Formation in the deeper part of the basin (southern part of the area) (see Matyja, 1993; Matyja & Stempieri-Salek, 1994). Gozd Arkose Formation The younger, Toumaisian part of the formation consists Trzebiechowo mainly of black, fine-laminated clayey deposits in which Marl M Э. S^polno Calcareous Shale Formation faunal remains are rare. (upper part) The thickness of the formation (excluding the Trze- biechowo marl Member) varies from more than 300 m in the Wierzchowo-Kurowo area to only about 30 m in the Kar- Fig. 2. Generalized lithostratigraphic chart of Lower Carbonif­ erous deposits of Koiobrzeg-Chojnice area of western Pomerania lino region in the northern part of the area. (after Lipiec in Lipiec & Matyja, 1998, modified) Trzebiechowo MarI Member This unit is an upper part of the S^polno Calcareous BIOSTRATIGRAPHY Shale Formation. It includes marls, limestones (including oolite limestones), dolostones, calcareous claystones, fine­ In the study area, the main biostratigraphic tool for dat­ grained quartz arenites and arkosic arenites. Fauna is repre­ ing and correlating of the shale-rich, open marine lithofacies sented mainly by brachiopods, echinoderms, biyozoans, la- comprising lower and middle parts of the Toumaisian are mellibranchs and gastropods. Ostracods and conodonts conodonts supported by miospores and ostracods. The up­ have also been encountered. In vicinity of Brda, the Trze­ per Toumaisian deposits represent generally very shallow- biechowo Marl Member is up to 600 m in thickness. marine environments, where miospores and ostracods pre­ vail, whereas conodonts are remarkably scarce. The upper­ Gozd Arkose Formation most Toumaisian and Visean are dominated by terrestrial, It contains arkosic sandstones (volcanoclastic, cf. mainly siliciclastic deposits, where miospores are the main Muszyriski et al., 1996), locally calcareous or dolomitic. stratigraphic tool. Tuffites, claystones, marls and oolite limestones occur sub- ordinately. The thickness of the formation may exceed 400 Zonal schemes m. In this section, we have omitted the names of the spe­ Kurowo Oolite Formation cies creators. The list of complete specific names is given in The formation includes oolite, and oolite-skeletal lime­ the Appendix 1. stones and, subordinately, other types of limestones, often dolomitized. Marls and arkosic sandstones may be present Conodonts locally. The oolite-skeletal limestones contain echinoderms, The preliminary “standard” Lower Carboniferous Si- brachiopods, lamellibranchs, ostracods, corals, bryozoans phonodella-based zonation of Sandberg et al. (1978) is and calcareous algae. The formation is up to 200 m thick. based on the first occurrence of Siphonodella species that in most cases are the index species of the zones. The base of Grzybowo Calcareous Shale Member the Carboniferous in offshore marine sequences is defined This member is distinguished within both the Gozd and at the base of the sulcata Zone. The upper limit of the isosti- the Kurowo fonnations. It contains black shales, calcareous cha--Upper crenulata Zone is defined by the last occurrence claystones, marls, limestones, and nodules of anhydrite. of the genus Siphonodella. Fortuitously, this extinction oc­ Fauna is dominated by thin-shelled lamellibranchs, ostra­ curred almost simultaneously with the appearance of the cods, gastropods and, locally, brachiopods. The maximum new gnathodid species Gnathodus typicus, from Gn. delica- thickness is up to 300 m. tus. Lane et al. (1980) proposed a preliminary “standard” conodont zonation for the upper Toumaisian-lower Visean Drzewiany Sandstone Formation interval to follow the “standard” Siphonodella zonation. As In the northeastern part of western Pomerania, this is in the case of the Palmatolepis-based standard Upper Devo­ the uppermost unit of the Lower Carboniferous. It contains nian conodont zonation, both these “standard” Lower Car­ white and red, fine quartz sandstones, variegated mudstones boniferous schemes are applicable mainly to open marine, and claystones, locally calcareous, with anhydrite and pa- offshore settings. On the other hand, extensive shallow- leosol. Rare fauna is limited to few beds, and is represented water environments characterise most of the shelf areas in by thin-shelled lamellibranchs, ostracods, brachiopods and Belgium and in the British Isles where both “standard” zo- crinoids. Goniatites were reported from the upper part of the nations are difficult to apply. Therefore, several local formation in the Sarbinowo 1 section (Korejwo, 1993). The schemes have been proposed in these areas (Groessens, thickness of the Drzewiany Sandstone Formation may ex­ 1974; Conil et al., 1990; Varker&Sevastopulo, 1985; Web­ ceed 400 metres. ster & Groessens, 1990). 196 H. MATYJA ET AL.

Conodont Western Pomerania conodont assemblages Zone panying forms include representatives of Polygnathus spi- anchoralis conodonts not found catus (Fig. 4/6) and Siphonodella obsoleta (smooth mor­ - latus photype - Fig. 4/12). Other conodont faunas consisting al­ upper (2) Ps. minutus typicus lower (1) Gn. cuneiformis most entirely of long-ranging taxa (comp. Fig. 3) such as (Ty) Ps. m ultistriatus Cl. unicornis Bispa- thodus spinulicostatus, Neopolygnathus communis Neopo. carina M2 isosticha - morphotype 1, Polygnathus purus punts, Pandorinellina U. crenulata (Ce2) ? d i . acuieaius acuieaius plumula, Elictognathus bialatus (Fig. 4/13-14) and Elictog- Si. crenulata Bi. aculeatus anteposicornis L. crenulata Po. symmetricus Bi. spinulicostatus nathus laceratus (Fig. 4/15), Bispathodus stabilis morpho­ (Ce-f) Po. distortus Bi. stabilis M1 Po. radinus EI. bialatus type 1, and Polygnathus inornatus. EI. laceratus Neopo, carina M1 The succeeding Lower crenulata Zone has been recog­ Neopo, communis M1 V Pand. plumula nized also in the Rzeczenica 1 section (Appendix 2) by the f Po. flabellus Po. inornatus presence of Siphonodella crenulata and its co-occurrence Po. purus purus Po. triangulus Ps.dentiUneatus with Polygnathus symmetricus (Sandberg et al, 1978; Si. duplicata M1 Ps. nodomarginatus sandbergi Si. quadruplicata Ps. primus Belka, 1985), accompanied (see Fig. 3) by Polygnathus ra- (Sn) Po. spicatus Si. obsoleta Si. obsoleta (smooth morphotype) Si. quadruplicata dinus (Fig. 5/1) and Polygnathus distortus (Fig. 5/6). Unfor­ Si. sulcata tunately, other accompanying fauna consists of long-ran- ging taxa including Polygnathus triangulus (Fig. 5/4) and Polygnathus inornatus (Fig. 5/2), representatives of Sipho­

duplicata upper (2) nodella obsoleta (Fig. 5/12) and Siphonodella quadrupli- (Du) lower (1) cata (Fig. 5/3, 13), Neopoly gnathus communis morphotype sulcata conodonts not found 1, Pseudopoly gnathus nodomarginatus (Fig. 5/7-8), Bis­ pathodus spinulicostatus, Elictognathus bialatus and Elic­ Fig. 3. Characteristic species of Tournaisian conodont zones in Western Pomerania. Important species in bold characters tognathus laceratus (Fig. 5/11) and rare Hindeodus aff. cris- tulus (Fig. 5/10). It should be mentioned that due to the extremely rare occurrence of Siphonodella crenulata and the lack of other Depositional environment within the Pomeranian sedi­ diagnostic species in most of the investigated sections, it is mentary basin underwent evolution from an open shelf dur­ not possible to separate the sandbergi Zone from the Lower ing the early and middle Tournaisian to a very shallow- crenulata Zone (comp. Fig. 3 and Appendix 2). The same water marine, and, subsequently, a terrestrial environment problem arises with separation of the Lower crenulata Zone in the late Tournaisian. Therefore, the Siphonodella-based from the isosticha-Upper crenulata Zone because of the ab­ zonation of Sandberg et al. (1978) and part of the post-Sz- sence of Gnathodus delicatus. The unseparated interval be­ phonodella zonation of Lane et al. (1980) are applicable in tween the sandbergi and the Lower crenulata zones is char­ western Pomerania up to the Tournaisian typicus conodont acterized by the presence of various polygnathids, pseudo- Zone (see Fig. 3). Conodonts younger than the typicus Zone polygnathids and bispathodids, i.e. Pseudopoly gnathus pri­ have not been found so far as the uppermost Tournaisian mus (Fig. 4/1), Polygnathus inornatus (Fig. 4/3), Polygna­ and Visean represent mainly terrestrial deposits with only thus flabellus (Fig. 4/7), Neopoly gnathus carina morpho­ some marine influences. type 1 (Fig. 4/4), Neopoly gnathus communis morphotype 1 The oldest documented Tournaisian conodont fauna in (Fig. 4/5), Bispathodus aculeatus anteposicornis (Fig. 4/8) the Pomerania area is that of the sandbergi Zone. The pres­ and Siphonodella quadruplicata (Fig. 4/11). ence of advanced siphonodellids such as Siphonodella qua­ The presence of Pseudopoly gnathus multistriatus mor­ druplicata, and its co-occurrence with Siphonodella dupli­ photype 2 (Fig. 6/8) and Gnathodus cuneiformis (Fig. 6/11- cata morphotype 1 (Fig. 4/9) suggest that the lowermost 12) well characterize the Lower typicus Zone (Lane et al, part of the Tournaisian succession in the Rzeczenica 1 sec­ 1980) and the equivalent zones (Belka, 1985; Varker & tion is to be correlated with the upper part of the sandbergi Sevastopulo, 1985; Belka & Groessens, 1986; Sevastopulo Zone (Sandberg et al., 1978; Clausen et al., 1989). Accom­ & Nudds, 1987; Carman, 1987; Riley, 1993). Other accom-

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Fig. 4. Conodonts of the sandbergi (Sn) Zone (6, 9, 12-13, 15), unseparated sandbergi - Lower crenulata (Sn-Cei) Zones (1,3-5, 7-8, 10-11,14), and unseparated sandbergi - isosticha-Vpper crenulata (Sn-Ce2) Zones (2). All specimens are from Rzeczenica 1, except when indicated otherwise. All photographs are SEM upper views except 1, 9a (lower views) and 15 (side view). 1 - Pseudopolygnathus primus Branson & Mehl, 2907-2909 m, SEM-823, x80; 2 - Pseudopolygnathus dentilineatus Branson, Bialy Bor 1, 2680-2686 m, SEM-652, x60; 3 - Polygnathus inornatus Branson, 2912-2916 m, SEM-817, x80; 4 - Neopolygnathus carina (Hass), morphotype 1, 2912-2916 m, SEM-814, x80; 5 -Neopolygnathus communis (Branson & Mehl), morphotype 1,2909-2910 m, SEM-816, x80; 6 - Polygnathus spicatus Branson, 2916-2920 m, SEM-668 , x50; 7 - Polygnathus flabellus (Branson & Mehl), 2907-2909 m, SEM-660, x75; 8 - Bispathodus acu­ leatus anteposicornis (Scott, 1961), 2909-2910 m, SEM-666 , x 120; 9-9a - Siphonodella duplicata (Branson & Mehl), morphotype 1, 2916-2920 m, 9: SEM-818, x50, 9a: SEM-822, x4 5 ; 10 - Siphonodella cooperi Hass, morphotype 2, 2909-2910 m, SEM-661, x60; 11 - Siphonodella quadruplicata (Branson & Mehl), 2912-2916 m, SEM-815, x30; 12 - Siphonodella obsoleta Hass, smooth morphotype, 2920-2922 m, SEM-673, x75; 13-14 - Elictognathus bialatus (Branson & Mehl), 13: 2920-2922 m, SEM-670, x 150, 14: 2909-2910 m, SEM-664, x 150; 15 - Elictognathus laceratus (Branson & Mehl), 2920-2922 m, SEM-669, x 100 LOWER CARBONIFEROUS STRATIGRAPHY 197 198 H. MATYJA ETAL.

Fig. 5. Conodonts of the Lower crenulata (Cei) Zone (1-4, 6 -8, 10-12), unseparated Upper duplicata - isosticha-Upper crenulata (Du2-Ce2) Zones (5), and unseparated sandbergi? - Lower crenulata? (Sn?-Cei?) Zones (9). All specimens are from Rzeczenica 1, 2896-2899 m, except when indicated otherwise. All photographs are SEM upper views except 4, 5, 8 (lower views) and 9-11 (side views). 1 - Polygnathus radinus (Cooper), SEM-827, x70; 2 - Polygnathus inornatus Branson, Rzeczenica 1, 2899-2901 m, SEM-657, x70; 3,13 - Siphonodella quadruplicata (Branson & Mehl); 3: SEM-829, *30, 13: SEM-654, *60; 4-5 - Polygnathus triangulus Voges; 4: SEM- 824, x60, 5: Bielica-1, 3516-3517 m, SEM-651, xl20; 6 - Polygnathus distortus Branson & Mehl, SEM-658, x50; 7-8 - Pseudopolyg- nathus nodomarginatus (Branson), 7: SEM-659, xlOO, 8 : SEM-821, x60; 9-10 - Hindeodus aff. cristulus (Youngquist & Miller), 9: Brda-1, 2469-2475 m, SEM-813, x70, 10: SEM-656, x80; 11 - Elictognathus laceratus (Branson & Mehl), SEM-655, x£0; 12 - Si­ phonodella obsoleta Hass, SEM-653, x45 LOWER CARBONIFEROUS STRATIGRAPHY 199

Fig. 6. Conodonts of the Lower typicus (Tyi) Zone. Specimens 1-4, 6 , 7 are from Drzewiany 1, 2733-2736 m, other specimens as indi­ cated below. All photographs are SEM upper views except 1 and 3 (side views). 1-5 - Clydagnathus unicornis Rhodes, Austin & Druce, 1: SEM-819, *60, 2: SEM-644, xlOO, 3: SEM-820, *80, 4: SEM-643, *140, 5: Brda 1, 2192-2198 m, SEM -111, x 9 5 ; 6 -8 - Pseudopolyg- nathus multislriatus Mehl & Thomas, 6-7: morphotype 1, 6 : SEM-641, *100, 7: SEM-642, xl50, 8: morphotype 2, Drzewiany 1, 3003-3004 m, SEM-645, *70; 9 - “Hindeodus” crassidentatus (Branson & Mehl), Chmielno 1, 3588-3599 m, SEM-648, *50; 10 - Neo- polygnathus carina (Hass), morphotype 2, Brda 1, 2325-2326 m, SEM-811, x80; 11-12 - Gnathodus cuneiformis Mehl & Thomas, early phylogenetic forms, Chmielno-1, 3588-3599 m, 11: SEM-834, xl50; 12: SEM-647, xl50 200 H. MATYJA ET AL. 202 H. MATYJA ET AL.

Species defining base M io sp ore o f Z o n e /S u b zo n e (*) Characteristic Fig. 8. Miospore zones and sub­ Zone / Subzone other first appearances assem blage zones for Lower Carboniferous in (** in the upper part of the Zone) western Pomerania and their char­ Lophotriletes tribulosus Dictyotriletes L. pusilla acteristic species D. plumosus (*) pactilis (Pa) Schulzospora spp Cingulizonates bialatus

Schulzospora S. campyloptera (*) Lycospora pusilla campyloptera (Ca) Knoxisporites spp

Lycospora L. pusilla (*) P. claytonii W. planiangulata W. planiangulata (**) A. baccatus pus ilia (Pu) C. multisetus A. trychera

A. solisorta upper A. panda P. claytonii Prolycospora (2) G. multiplicabilis A. baccatus S. claviger (*) C.multisetus

R. clavata R. corynoges p uncatus (Cl) lower C. multisetus V. nitidus D. glumaceus (1) A. baccatus P. claytonii (*)

upper (4) S. pretiosus (*)

middle S. balteatus (*) R. corynoges Convolutispora (3) V. nitidus A. macra major Tumulispora spp C. trychera Retusotriletes spp (Ma) ^ S. delicatus Knoxisporites spp P. uncatus Dictyotriletes spp U. distinctus (*)

R. corynoges lowermost L. excisus

W estern British Isles First appearances Pom erania Series Fig. 9. Correlation of the zonal m iospore of index species m iospore Stages schemes for Lower Carboniferous zonation zonation of British Isles and westen Pom­ Bellispores nitidus- NC erania. Arrows indicate uncertain Reticulatisporites carnosus BRIGANTIAN Tripartites vetustus - position of lower boundary of Ma VF Rotaspora fracta Zone V R. fracta p a Dictyotriletes Raistrickia nigra - NM Triquitrites marginatus pactilis I ASBIAN Perotrilites tessellatus - Qa Schulzospora TC s Schulzospora campyloptera campyloptera E ------S. campyloptera------Knoxisporites triradiatus - TS A HOLKERIAN Knoxisporites stephanephorus Lycospora Pu N ARUNDIAN ------W. planiangulata------pusilla Pu Lycospora pusilla CHADIAN - - L. pusilla - - Schopfites claviger - T CM o Auroraspora macra — S. claviger - 01 Prolycospora___ claytonii ^ u Spelaeotriletes pretiosus - PC R Raistrickia clavata 4 N - S. pretiosus----- Spelaeotriletes balteatus - A BP Convoluti- 3 COURCEYAN Rugospora polyptycha I - S. balteatus----- M a spora ------major 2 Kraeuselisporites hibemicus - S - U. distinctus — HD Umbonatisporites distinctus 1 A -I- K. hibernicus ? - Vallatisporites verrucosus - N VI Retusotriletes incohatus LOWER CARBONIFEROUS STRATIGRAPHY 201

panying forms (Fig. 3, Appendix 2) include many represen­ by Neves el al. (1973) and later gradually refined on the ba­ tatives of Clydagnathus unicornis (Fig. 6/1-5), Pseudo- sis of new studies (see Clayton, 1985; Higgs et al., 1988a: polygnathus multistriatus morphotype 1 (Fig. 6/6-7), rare Higgs et al., 1992). The scheme is keyed to the British Isles Neopolygnathus carina morphotype 2 (Fig. 6/10), and Hin- Carboniferous stages (Higgs e ta i, 1988b; Riley, 1993), and deodus crassidentatus (Fig. 6/9). at some stratigraphic levels to the Irish and Siphonodella based conodont zonations which is discussed in more detail Miospores in the Subsection Results. Tumau (1978, 1979) erected a local miospore zonal The correlation of the Pomeranian and western Euro­ scheme in this region encompassing uppermost Devonian to pean schemes for the Tournaisian was discussed in Clayton lower Westphalian strata. The Carboniferous part of the & Tumau (1990) and Avkhimovitch & Tumau (1994). The scheme comprises six zones and three subzones, two zones present version differs in details from the previous ones due for the Tournaisian, three for the Visean, and one for the to the results of Stempien-Salek (Matyja & Stempieri-Salek, Westphalian. The first two zones have been formally de­ 1994, Stempien-Salek, 1997) who established, that Spelaeo- fined, and the succeeding ones are informal. The miospore triletes balteatus and S. pretiosus appeared earlier than Pro­ species characteristic of the zones are shown in Figs 7, lycospora claytonii. 10-11. In the following text, and in some figures, the names The correlation shown in Fig. 9 is based on the first ap- of the miospore zones are abbreviated to a two-letter nota­ perances of stratigraphically important species. A further tion. However, their full taxonomic titles are given in Figs comment is needed only for correlations at some levels. 8-9. The base of the Ma Zone cannot be confidently corre­ The Tournaisian part of the zonation scheme was subse­ lated with the base of the HD Zone of northwestern Europe. quently modified. Stempien-Salek (in Matyja & Stempien- This is because the presence of Kraeuselisporites hiberni- Salek, 1994) erected four subzones of the Convolutispora cus in the lowermost assemblages of the zone (in the Rze- major (Ma) Zone. They are designated here the lowermost czenica 1 borehole, see Appendix 2) is not certain. Higgs et (Mai), lower (Маг), middle (Маз) and upper (Ma4). The al. (1992) considered Cymbosporites acutus as an important characteristic of the revised and upgraded part of the zonal species for defining the base of the HD Zone in Belgium. scheme is shown in Fig. 8. This species has been recorded from the Mai assemblages; The Prolycospora claytonii (Cl) Zone was initially di­ however, we consider it as an unreliable stratigraphic vided into three subzones. The base of the upper subzone marker because in Ireland, it ranges downwards into the Fa- was based on the first appearance of Rugospora minuta. mennian (Van der Zwan, 1980), and in the East European However, subsequently, it was established that in western Platform, it appears in the Tumulispora malevkensis Zone Pomerania, the range of this species was much wider. Thus, (Byvsheva, 1985; Avkhimovitch, 1993) very near the Devo­ Avchimovitch & Tumau (1994) revised the zonal scheme as nian/Carboniferous boundary. to recognize only two subzones designated Lower Cl (Cli) The correlation of upper part of the (Pomerania) Pu Subzone and Upper Cl (Cb) Subzone. The new Upper Cl Zone with a part of the TS Zone is based on the presence of Subzone contains the original middle and upper Cl subzones Waltzispora planiangulata in higher assemblages of the Pu up to the redefined lower boundary of the Lycospora pusilla zone. In Rtigen, this species first appears in the TS Zone (Pu) Zone. (Carson & Clayton, 1997). It must be emphasized that the statement by Tumau The base of the Pa zone was correlated by Tumau (1978) concerning the first appearance level of Lycospora (1979) with the base of the NM Zone on the first appearance pusilla was erroneous. This species does not occur through­ of Dictyotriletes pactilis. However, specimens assigned at out the P. claytonii Zone, i.e. part of the Tournaisian (see that time to D. pactilis represent an older species D. plumo- discussion in Avkhimovitch & Tumau, 1994). sus (see the Section Systematic comments (miospores). The The local miospore zonation for western Pomerania can Pa zone assemblages contain also Potoniespores delicatus. be correlated at several stratigraphic levels with the zonal This species appears in the upper part of the TC Zone (Clay­ scheme for the type regions of the Lower Carboniferous ton et al., 1977b). Thus, the base of the Pa zone is now con­ stages in the British Isles (Fig. 9). This scheme was erected sidered not older than the upper part of the TC Zone.

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Fig. 7. Miospores of the Convolutispora major (Ma) Zone. Specimens 1,4-9, 15, 16 are from Biely Bor I, 2792-2796 m, specimens 2, 10, 11, 13 are from Rzeczenica 1, 1920-1921 m, other specimens as indicated below. All magnifications x500. 1 - Retusotriletes circu­ laris Tumau, slide V/67; 2 - Verrucosisporites nitidus Playford, slide V/85; 3 - Umbonatisporites distinctus Clayton, Wierzchowo 10, 3545-3551 m, slide VII/19; 4 - Convolutispora mellita Hoffmeister, Staplin & Malloy, slide V/65; 5 - Knoxisporites triradiatus Hoff- meister, Staplin & Malloy, slide V/65; 6 - Knoxisporites hederatus (Ishchenko) Playford, slide V/67; 7 - Convolutispora major (Kedo) Turnau, slide V/64; 8 - Tumulispora variverrucata (Playford) Staplin & Jansonius, slide V/65; 9 - Murospora sublobata (Waltz) Playford, slide V/65; 10 - Lophozonotriletes excisus Naumova, slide V/85; 11 - Tumulispora malevkensis (Kedo) Turnau, slide V/86; 12 - Endocu- leospora gradzinskii Turnau, Rzeczenica 1, depth 2912-2916 m, slide V/83; 13 - Grandispora upensis (Kedo) Byvsheva, slide V/83; 14-15 - Discernisporites micromanifestus (Haquebard) Sabry & Neves, slide V/6 6 ; 16 - Auroraspora macra Sullivan, slide V/65; 17-18 - Cymbosporites acutus (Kedo) Byvsheva, Nieklonice 2, depth 2877-2891 m, slide VII/36; 19 - Kraeuselisporites hibernicus Higgs, Wierzchowo 10, depth 3513-3517 m, slide VII/51; 20 - Indotriradites explanatus (Luber) Playford, Klanino 1, depth 27812787 m, slide 111/83 LOWER CARBONIFEROUS STRATIGRAPHY 203

In the description of the assemblages of the Pa zone, The youngest recognized assemblage, Glyptopleura Turnau (1979) stated that they lacked Rotaspora. However, ruegensis—Carbonita fabulina (R-F) (Fig. 16) contains further study of samples from Sarbinowo 1 borehole re­ species known from the uppermost Toumaisian and Visean vealed the presence of a single specimen of R. fracta in the of Germany and Great Britain (Blumenstengel, 1975a, b; highest assemblage representing the Pa zone. Therefore, it is Robinson, 1978). suggested that the base of the western European Tripartites vetustus-Rotaspora fracta (VF) Zone corresponds to a level R esults within the Pa Zone. Comparison o f conodont, miospore, and benthic ostracod Ostracods stratigraphic schemes In the following text, and in some figures, the names of Conodonts and, to a lesser extent, entomozoids from the the ostracod assemblages are abbreviated to a two-letter no­ Toumaisian succession of the Koszalin-Wierzchowo area tation. However, their full taxonomic titles are given in Fig. provide new biostratigraphic information and control on the 12. age of the miospore zones and benthic ostracod assem­ Only the lowest Carboniferous deposits bear rare ento- blages (Fig. 17). In the following discussion, we will also mozoacean ostracods. Specimens occur as internal or exter­ use information on occurrence of ammonoids, which was nal, typically poorly preserved moulds. Only the latior (La) provided by Korejwo (1979, 1993). There is little faunal entomozoid Zone has been distinguished based on the pres­ control on the age of informal, local miospore zones for the ence of single specimens of the index species Richterina la­ Visean. tior. This zone corresponds to the lowest Toumaisian sul­ Correlation of various biostratigraphic schemes has cata to sandbergi conodont zones (Gross-Uffenorde, 1984; been the concern of Carboniferous biostratigraphers for a Gross-Uffenorde & Schindler, 1990). long time. In western Europe, miospore assemblages from About 80 species of benthic ostracods have been found the Toumaisian conodont dated sequences were studied in in the Toumaisian strata. Only some have been described Ireland (Clayton et al., 1977a, 1978, 1980; Sleeman et al., (Blaszyk & Natusiewicz, 1973). The majority of ostracods 1978; Marchant et al., 1984; Higgs et al., 1988a, b), and belong to unknown and undescribed taxa, but the prelimi­ Belgium (Higgs & Street, 1984; Higgs et al., 1992). The nary investigation of the fauna has shown that about one palynological boundaries within the Irish Dinantian are also third of the species is known from other, sometimes distant dated by other microfauna (Higgs et al., 1988b). Owing to areas. these contributions, the miospore zonation scheme for the A preliminary, informal Toumaisian local zonation that Toumaisian proposed by Higgs et al. (1988a) has been cor­ comprises 4 assemblages, based only on small part of the related with the Irish conodont zonation scheme and the si- ostracod fauna, is proposed here by Żbikowska. This is the phonodellid based scheme, which is shown in Fig 17. This first attempt to show the stratigraphic value of the Tour- chart shows also the correlation of the British Isles and naisian benthic ostracods from Pomerania. Establishing of a western Pomerania miospore zonation schemes for the formal zonation would be possible only after a detailed Toumaisian, based on palynological criteria (see also Fig. analysis of the fauna, which is beyond the scope of this pa­ 9). The validity of this correlation is controlled at a few stra­ per. tigraphic levels by conodonts and entomozoids. Conodonts The characteristics of the assemblages are given in Fig. and miospores provide also control on the age of benthic os­ 12. Lowermost is the Pseudoleperditia vemilosa (Vn) as­ tracod assemblages. These data are discussed below, and semblage which is divisible into the lower (Vni) and the up­ the details of the occurrences are presented in Figs 18, 19, per (Vn2) ones. and in the Appendix 2. The Vni assemblage is characterized by the co­ In the Rzeczenica 1 section (Fig. 18), the Mai assem­ occurrence of Pseudoleperditia venulosa and the short rang­ blages occur just below conodont fauna indicative of the ing species Namaya reticulata. The accompanying known sandbergi Zone, and are bracketed by such fauna (see also species are listed in Fig. 12 and Appendix 2, and illustrated Matyja & Stempieri-Salek, 1994). These assemblages were in Fig. 13. They are characteristic of the lower Toumaisian also found below the latior Zone entomozoids and sand­ deposits of Belgium, North America and Russian Platform bergi - isosticha-Upper crenulata Zone conodonts (Chmiel- (Green, 1963; Becker & Bless, 1974; Becker et al., 1974; no 1 borehole, Fig. 18) and in the same 6 m interval as go- Tchigova, 1977; Bless et al., 1986; Coen et al, 1988). niatites Pseudoarietites dorsoplanus dorsoplanus H. The Vn2 assemblage (Fig. 14) is characterized by the Schmidt (Ga a) (Grzybowo 1, 3297-3303 m, and Wierz- co-occurrence of Pseudoleperditia venulosa and the short chowo 10, 3545-3552 m, Fig. 18). The results indicate that ranging species Chamishaella obscura. It does not contain the base of the Ma Zone is located either within or slightly stratigraphically important species, and its age can be only below the sandbergi Zone. Palynologically, the equation of approximately established on its relation to miospore sam­ the base of the Ma Zone with that of the western European ples, which is discussed below. HD Biozone (which is within the sandbergi Zone) is poorly The succeeding assemblage Cribroconcha postfoveata substantiated because the assignment of specimens from the - Marginia tchigovae (P—T) (Fig. 15) contains species lowermost Mai assemblage from the Rzeczenica 1 section known from the upper Toumaisian deposits of Germany and to Kraeuselisporites hibernicus is uncertain. the Russian platform (Blumenstengel, 1975a; Griindel, The Ma2 miospore assemblages occur with conodonts 1975; Tschigova, 1977). of the unseparated sandbergi - isosticha-Upper crenulata 204 H. MATYJA ET AL.

zones, and entomozoids of the latior Zone (Chmielno 1), data on the equivalents of these zones (see Fig. 9) in the and with the Lower crenulata conodont fauna (Rzeczenica British Isles (Riley, 1993). 1). Thus, the base of the Ma2 subzone is within the sand- In some sections, benthic ostracods were found in asso­ bergi Zone, and a higher part of the subzone corresponds to ciation with conodont, entomozoid and miospore assem­ a part of the Lower crenulata Zone. This agrees well with blages. The ostracod Vni assemblage has been found in as­ the miospore and conodont data from Belgium (Higgs et al., sociation with Mai miospores (Brda 1 borehole), and with 1992) where Umbonatisporites distinctus first appears at a the latior entomozoids, sandbergi - crenulata conodonts, level within the sandbergi Zone. and Маг miospores (Chmielno 1 borehole, see Fig. 18). The In the Gorzyslaw 9 borehole, a miospore assemblage Vn2 assemblage co-occurs with Ma miospores in the Brda 1 representing the Ma3 subzone was found at depth 3141— borehole. The P-T assemblage occurs below the Lower 3142 m by Stempieri-Salek (1997). This level is bracketed typicus conodonts (Brda 1 borehole, see Fig. 19) and in as­ by conodont faunas of the sandbergi or Lower crenulata sociation with the Cl 1 miospores (Chmielno 1 borehole). zones (Fig. 18). Thus, the base of the Ma3 subzone is not The R-F assemblage is associated with the Upper typicus(l) younger than the Lower crenulata Zone. This is the same conodonts (Biesiekierz 1 borehole) and with the CI2 mio­ stratigraphic position as that of the lower boundary of the spores (in the Klanino 1 borehole) (Fig. 19). These data al­ balteatus-polyptycha (BP) Zone in Belgium (Higgs et al., low to establish approximate correlation between the mio­ 1992). spore and benthic ostracod zonations (Fig. 17). The Cl] miospore assemblages were found below, and/or in association with conodonts of the Lower typicus Age of formations Zone (Chmielno 1, Drzewiany 1, and Klanino 1 boreholes, The stratigraphic positions and biozonal assignments of see Figs 18, 19), and the Cb miospore assemblages occur the micropalaeontological samples in the boreholes studied above the Lower typicus faunas (Brda 2 and Drzewiany 1 are shown in Fig. 18 and Fig. 19, and a generalized chronos- boreholes, see Fig. 19). In the Bialy Bor 1 borehole, a cono­ tratigraphic chart of the Tournaisian deposits is in Fig. 18. dont specimen determined as Polygnathus cf. purus purus Species range charts are in the Appendix 2. has been found above the base of the Cl Zone (Matyja, The younger, Carboniferous part of the S^polno Cal­ 1976). Polygnathus purus purus ranges to the upper bound­ careous Shale Formation is well dated by means of cono­ ary of the Lower crenulata Zone (Belka, 1985), but in Bel­ donts, miospores, ostracods, and macrofossils. The oldest gium P. cf. purus purus was found in the cuneiformis Zone conodonts indicate the upper part of the sandbergi Zone, the (Belka & Groessens, 1986, table I) which is equivalent of entomozoid ostracod Richterina (R.) latior indicates the la­ the Lower typicus Zone. tior Zone (Zbikowska, 1992), and miospore assemblages This, and the conodont data on the Ma Zone discussed represent the Ma Zone, the Mai or Маг subzones. Gonia­ above, suggest that the Ma/Cl boundary is within the span tites found in Grzybowo 1 borehole (depth 3297-3303 m), Lower crenulata - Lower typicus zones, and the lower and Wierzchowo 10 (depth 3545-3552 m) give well con­ boundary of the CI2 Subzone is within or above the Lower strained dates for this part of the Sqpolno Calcareous Shale typicus Zone. Formation owing to the occurrence of ammonoids Pseuda- Faunal control on the Visean miospore zones is very rietites dorsoplanus dorsoplanus Schmidt and Gattenpleura scarce. The ammonoid index species of the Goa Zone - sp., indicative of the G aa (Gattendorfia subinvoluta) Zone Goniatites crenistria Phill. - has been found in the Sarbi- of the lowermost Carboniferous (Korejwo, 1979, 1993). nowo 1 borehole at depth 2656-2662 m (Korejwo, 1993), Benthic ostracods belonging to the Vni subassemblage in­ i.e. between the intervals included in the Ca and Pa mio­ cluding species indicative of a lower Tournaisian (Tnlb) spore zones (Fig. 19). This agrees well with the ammonoid age, are also present.

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Fig. 10. Miospores of the Prolycospora claytonii (Cl) Zone and basal part of Lycospora pusilla (Pu) zone. Specimens 1, 12, 13, 17, 22, 23 are from Karsina 1, 2242-2249 m, specimens 3, 8, 20, 24 are from Karsina 1, 2535-2538 m, other specimens as indicated below. All magnifications *500, except when indicated. 1 - Punctatisporites aerarius Butterworth & Williams, slide III/8; 2 - Pustulatisporites unca­ tus (Kedo) Byvsheva, Wierzchowo 10, 3332-3339 m, slide VII/25; 3 - Raistrickia clavata Haquebard emend. Playford, slide 111/22; 4 - Raistrickia corynoges Sullivan, Gozd 2, depth 2807-2812 m, slide IV/87; 5 - Schopjites delicatus Higgs emend. Higgs, Clayton & Kee­ gan, Biesiekierz 1, 2907-2913 m, slide IV/93; 6-7 - Schopfites claviger Sullivan, 6 : Drzewiany 1, 2581-2585 m, slide X/35, 7: Wierzchowo 9, 3424-3430 m, slide VII/80; 8 - Crassispora trychera Neves & Ioannides, slide 111/22; 9 - Umbonatisporites distinctus Clayton, Brda 1, 2260-2266 m, slide 1V/45; 10 - Anaplanisporites baccatus Hoffmeister, Staplin & Malloy, Karsina 1, 2591-2594 m, xlOOO; 11 - Dictyotriletes membranireticulatus Bertelsen, Drzewiany 1, 3053-3056 m, slide X/82; 12-13 - Prolycospora claytonii Tur- nau, slide III/8, 12: *1000; 14: Bascaudaspora submarginata (Playford) Higgs, Clayton & Keegan, Biesiekierz 1, 2907-2913 m, slide IV/87; 15 - Acanthotriletes socraticus Neves & Ioannodes, Drzewiany 1, 30533056 m, slide X/82; 16 - Dictyotriletes glumaceus (Byvsheva) Byvsheva, Wierzchowo 9, 3424-3430 m, slide VI1/77; 17 — Lycospora pusilla (Ibrahim) Somers, slide III/9; 18-19 - Colatis- porites multisetus (Luber) Avchimovitch & Tumau, 18: Gozd 2, depth 2807-2812 m, slide IV/87, 19: Wierzchowo 9, depth 3323-3330 m, slide VII/67, x750; 20 - Aurorasporapanda Tumau, slide 111/22; 21 -Auroraspora macra Sullivan, Wierzchowo 10, 3332-3339 m, slide V II/12; 22 - Rugospora minuta Neves & Ioannides, slide III/7; 23 - Gorgonispora multiplicabilis (Kedo) Tumau, slide III/8; 24 - Aurora­ spora cf. solisorta Hoffmeister, Staplin & Malloy, slide 111/22; 25 - Kraeuselisporites hibernicus Higgs, Brda 2, 2207-2213 m, slide VI/37; 26 - Spelaeotriletes balteatus (Playford) Higgs, Wierzchowo 10, 3301-3307 m, slide VII/8; 27 - Spelaeotriletespretiosus (Play­ ford) Neves & Belt, Gozd 3, 2810-2813 m, slide IV/82 LOWER CARBONIFEROUS STRATIGRAPHY 205 206 H. MATYJA ET AL. LOWER CARBONIFEROUS STRATIGRAPHY 207

The top of the Sąpolno Calcareous Shale Formation is To the west and south from the Gozd-Biesiekierz- dated as the latior entomozoid Zone, and sandbergi or cre- Grzybowo line, the Gozd Arkose Formation is overlain by nulata conodont Zone (Gorzyslaw 9, Karlino 1, and the Kurowo Oolite Formation. The boundary between the Chmielno 1 boreholes). The benthic ostracod P-T assem­ two formations is within or above the Lower typicus Zone blage occurs in the top part of the formation in the Daszewo (Drzewiany 1, Chmielno 1 boreholes). Benthic ostracods R3p borehole. (Daszewo R3p) indicate a position of the boundary not older In the southeasternmost part of the study area, between than the R-F assemblage, i.e. in upper part of the Cl i Sub­ Biały Bór and Brda, the upper boundary of the Sąpolno Cal­ zone (cf. Fig. 17). In the Brda 2 borehole, a higher part of careous Shale Formation (i.e., the upper boundary of the the formation is dated as the Cb subzone. Thus, the Kurowo Trzebiechowo Marl Member) is erosional, except for the Oolite Formation is roughly a time equivalent of the Grzy- Brda 2 borehole. The stratigraphic position of this boundary bowo Calcareous Shale Member. is dated as the Lower crenulata conodont Zone and Маг During the latest Tournaisian, deposition of quartz miospore subzone (in the Rzeczenica 1 borehole), Cli mio- sandstones of the Drzewiany Sandstone Formation replaced spore subzone (in the Biały Bór 1 borehole) and Cb mio­ that of clayey and carbonate sediments of the Grzybowo spore subzone (in the Biały Bór 3 borehole). Calcareous Shale Member and Kurowo Oolite Formation. Over the entire Kołobrzeg-Chojnice area, except for its The lower boundary of the Drzewiany Sandstone Formation southeasternmost part, the limestones and shales of the is within the Cb Subzone (Rosnowo 1, Gozd 2, probably Sąpolno Calcareous Shale Formation are overlain by Wierzchowo 9 and Drzewiany 1 boreholes). coarse-grained sediments included in the Gozd Arkose For­ There are considerable differences between the above, mation. In the northwestern part of the study area, west of miospore based age assignment and that based on macro­ the Kurowo 1 - Wierzchowo 10 line, the boundary between fauna (Korejwo, 1993). Controversies concern mainly the the two formations is within the Convolutispora major mio­ lower parts of the Drzewiany Sandstone Formation (bore­ spore Zone, Маг to Маз subzones (Niekłonice 1, Chmielno holes Drzewiany 1, Gozd 2, Wierzchowo 9) assigned here, 1, Gozd 4 boreholes, probably also Ktanino 1 borehole), but basing on spores, to the Tournaisian. In the opinion of Ko­ to the east (Kurowo 1, Wierzchowo 10, and Drzewiany 1), it rejwo (1993), the presence in these deposits of brachiopod is within a lower part of the Prolycospora claytonii (Cl) species Schizodus orbicularis (Me Coy) and bivalve species Zone. In the terms of the conodont zonation, this lithostra- Sanguinolites abdenensis Ether, indicates the lower Visean tigraphic boundary is within the Lower crenulata Zone in (VI). Although these species are known from the entire Di- the northwest and in the isosticha-Upper crenulata or lower nantian, Korejwo (1993) argued that they had been recorded part of the Lower typicus Zone in the east. mainly from the Visean. In upper Tournaisian, in the area along the Gozd-Bie- The undisputed assignment of the higher parts of the siekierz-Grzybowo line, calcareous claystones replaced the Drzewiany Sandstone Formation in the Karsina 1 section to coarse grained, arkosic sediments. The boundaiy between the Visean has been confirmed by the occurrence of a mio­ the lower part of the Gozd Arkose Formation and the Grzy­ spore assemblage of the lower-middle Visean Lycospora bowo Calcareous Shale Member is dated as Lower typicus pusilla (Pu) Zone. The formation is relatively well dated in Zone (Kłanino 1 borehole), and is within a higher part of the the Sarbinowo 1 section (Fig. 18). Miospores indicate the Cli subzone (Niekłonice 1), or within undivided Cl Zone. presence of the Visean Lycospora pusilla (Pu), Schulzo- Benthic ostracod data (Kłanino 1) are in agreement with this spora campyloptera (Ca) and Dictyotriletes pactilis (Pa) position. Conodonts representing probably the Upper zones. The assemblages of the Pu zone in this section in­ typicus Zone have been found found in the Grzybowo Cal­ clude younger elements not found below the triradiatus- careous Shale Member in the Biesiekierz 1 borehole, and stephanephorus (TS) Zone (see Fig. 11) suggesting a mid­ miospore assemblages representing the Cb subzone have dle Visean age, while miospore species present in the upper­ been recorded from the Rosnowo 1 borehole. most assemblage point to a late Visean (Brigantian) age. In

4 ------

Fig. 11. Miospores of the Dictyotriletes pactilis (Pa) zone. All specimens are from Sarbinowo 1 borehole, specimens 1, 4, 28 are from depth 2559-2562 m, slide IV/16, specimens 2, 3, 6 , 7,9, 10-12, 15 17-19,21-27,31 are from depth 2534-2537 m, slide IV/7, specimens5, 8, 13, 14, 29 are from depth 2534-2537 m, slide IV/9, specimens 16, 20 are from depth 2534-2537 m, slide IV/14, specimen 30 is from depth 2559-2562 m, slide IV/21. All magnifications x500.1 - Chetosphaeritespollenisimilis (Horst) Butterworth & Williams; 2 - Pilosis- porites venustus Sullivan & Marshall; 3 - Orbispoi'is convolutus Butterworth & Spinner; 4 - Punctatisporites aerarius Butterworth & Wil­ liams; 5 - Anapiculatisporites concinnus Playford; 6 - Lophotriletes tribulosus Sullivan; 7 - Converrucosisporites horridus (Ishchenko) Turnau var. trigonalis Jachowicz; 8 - Waltzispora sp.; 9 - Waltzispora planiangulata Sullivan; 10 - Foveosporites insculptus Playford; 11 - Corbulispora cancellata (Waltz) Bharadwaj & Venkatachala; 12-13 - Dictyotriletes plumosus (Butterworth & Spinner) Neville & Wil­ liams; 14 - Diatomozonotriletes cervicornutus (Staplin) Playford; 15 - Diatomozonotriletes saetosus (Haquebard & Barss) Hughes & Playford; 16, 20 - Murospora aurita (Waltz) Playford; 17 - Potoniespores delicatus Playford; 18 - Cingulizonates bialatus (Waltz) Smith & Butterworth; 19 - Lycospora noctuina Butterworth & Williams; 21 - Knoxisporites cf. stephanephorus Love; 22 - Densosporites sp.; 23 - Densosporites variabitis (Waltz) Potonie & Kremp; 24 - Lycospora pusilla (Ibrahim) Somers; 25 - Sclndzospora plicata Butterworth & Williams; 26 - MonUospora culta (Byvscheva) Byvscheva; 27 - Densosporites sp.; 28 - Schulzospora ocellata (Horst) Potonie & Kremp; 29 - Schulzospora campyloptera (Waltz) Hoffmeister, Staplin & Malloy; 30 - Perotrilites tessellatus (Staplin) Neville; 31 - Kraeuselisporites echinatus Owens, Michell & Marshall 208 H. MATYJA ET AL.

Benthic ostracod Species restricted to Other species assemblage/subassemblage assemblage / subassemblage present middle part of this section, the goniatites Goniatites crenis- Glyptopleura ruegensis 8. binodosus tria Phill. and Prolecanites cf. serpentinus (Phill.) have B. fortis - Carbonita fabulina G. annularis been recorded by Korejwo (1993). They indicate the pres­ G. ruegensis S. electa A. auadrata R - F C. fabulina ence of the late Visean Goa ammonoid Zone. The deposits

Cribroconcha postfoveata E. cf. kiselensis of a higher part of the Drzewiany Sandstone Formation in M. tschigovae - Marginia tschigovae G. reticulocostatus S. electa the Gozd 2 section (depth 2508-2504 m) yielded a macro- C. quasicornigera C. postfoveata A. similaris faunal assemblage similar to that found in Sarbinowo 1 P-T S. alekseevae S. longa Pseudoleperditia uPPer C. elata borehole in the middle Visean (V2) deposits. (2) C. obscura A. acutiangulata P. venulosa It is concluded that the Drzewiany Sandstone Forma­ venulosa ------C. triceratina B. lecta lower N. reticulata tion spans the uppermost Toumaisian and much of the Vn (1) S. tersiensis A. rara Visean.

Fig. 12. Benthic ostracod assemblages/subassemblages for Tournaisian in western Pomerania and their characteristic species

iSWf?

Fig. 13. Ostracod assemblage lower Pseudoleperditia vemilosa (Vni). Specimen 1 is from Brda 1, 2676-2682m, specimens 2-11 are from Chmielno 1, 3952-3962 m. 1 -N a m a ya reticulata Green; 2 - Pseudoleperditia venulosa (Kummerow); 3 - Cotyellina triceratina (Posner); 4 - Shishaella alekseevae Tschigova; 5 - Shivaella longa (Tschigova); 6 - Amphissites similaris Morey; 7 - SulcocaveUina tersi- ensis Bushmina; 8 - Acutiangulata acutiangulata (Posner); 9 - A. rara Bushmina; 10 - Bairdia tecta Bushmina; 11 - Richterina (Rich- terina) latior Rabien LOWER CARBONIFEROUS STRATIGRAPHY 209

Fig. 14. Ostracod assemblage upper Pseudoleperditia venulosa (V112). All specimens are from Brda 1 .1 - Pseudoleperditia venulosa (Kummerow), 2524.5-2528 m; 2 - Coryellina triceratina (Posner), 2611-2616 m; 3 - Chamishaella obscura Tschigova, 2560-2563 m; 4 - Shishaella longa (Tschigova), 2676-2682 m; 5 - Sulcocavellina tersiensis Bushmina, ibidem; 6 -Acutiangulata acutiangulata (Posner), 2611-2616 m; 7 - Bairdia lecta Bushmina, ibidem

Chronostratigraphic boundaries the biostratigraphic gap seems to comprise a similar time in­ terval. There is no conodont data suggesting the presence of Devonian/Carboniferous boundary conodont zones older than the sandbergi Zone. The Global Stratotype Section and Point for the Devo­ A similar range of this stratigraphic gap is also indi­ nian-Carboniferous boundary has been defined at La Serre, cated by miospore analysis. Two consecutive, local rnio- southeast Montagne Noir France (see Paproth et. a l, 1991). spore zones - Tumulispora rarituberculata (Ra), and Con- The section fulfills the demands of the Group, especially the volutispora major (Ma) were distinguished in the Devo­ condition that specimens of Siphonodella praesulcata nian/Carboniferous transition beds (Turnau, 1978). This should be followed by S. praesulcata-sulcata transitional author suggested (see Tumau, 1978, fig. 3) that a high rate forms. of species disappearances and the first appearances at the In western Pomerania, the top of the Upper Devonian Ra/Ma zonal boundary indicates the presence of a stra­ sequence yielded abundant and diverse conodont fauna in­ tigraphic gap. Varying opinions on the extent of this gap dicative of the Upper expansa and/or Lower praesulcata were discussed in Tumau (1979), Clayton & Tumau (1990), zones (Matyja, 1993). The base of the Lower Carboniferous Avkhimovitch et al. (1993), Matyja & Stempieri-Salek sequence is characterised by rare though relatively diverse (1994). The up to-date information on stratigraphical ranges conodonts characteristic of the sandbergi Zone. In the Rze- of several critical species in the nortwestem Europe (Higgs czenica 1 section, there are only some metres of a shale de­ et al., 1988a) and Belarus (Avkhimovitch, 1993) suggests void of fauna between the documented Devonian Upper ex­ that in western Pomerania, the counterparts of the north­ pansa - Lower praesulcata zones and the Carboniferous western European spore zones lepidophyta-explanatus sandbergi Zone. In other investigated sections, in which De­ (LE), lepidophyta-nitidus (LN) and most of, or the entire vonian/Carboniferous boundary runs within cored intervals, verrucosus-incohatus (VI) Zone are missing. 210 H. MATYJA ET AL.

Fig. 15. Ostracod assemblage Cribroconcha postfoveata-Marginia tschigovae (P-T). Specimens 1, 2 are from Brda 1, 2319-2326 m, specimens 3, 4, 6 , 8 are from Brda 1, 2260-2266 m, specimens 5, 7 are from Chmielno 1, 3794-3796 m. 1 - Amphissites similaris Morey; 2 - Shivaella longa (Tschigova); 3 - Marginia tschigovae (Palant); 4 - Carboprimitia elata Tschigova; 5 - Graphiadactyllis reliculocosta- tus Grundel; 6 - Cribroconcha quasicornigera Bushmina; 7 - C. postfoveata Griindel; 8 - Editia cf. kiselensis (Posner) s. Robinson

The presence in some sections of goniatites of the Gat- investigation (Sevastopulo & Hence, 1999). tendorfia subinvoluta (Go) Zone of the lowermost Tour- It is difficult to establish the position of the Tournai­ naisian ( see Korejwo, 1979, 1993) suggests, however, that sian-Visean boundary in the investigated sections of the range of the stratigraphic gap could be smaller (in some western Pomerania mainly because of the lack of key fauna. sections?), and limited to the Devonian Middle-Upperprae- The boundary is placed tentatively at the first appearance of sulcata Zones and the Carboniferous sulcata-Lower dupli­ Lycospora pusilla. This first appearance, at least in Europe, cata Zones. has been traditionally equated with the discussed boundary The nature and possible causes of the gap were dis­ (Clayton et a i, 1990; Tumau et al., 1997) but, in precise cussed in details by Matyja (1993). Apart from the question terms, the CM/Pu boundary may be older (Riley, 1993, see of the range of the gap, it is clear, however, that the upper­ also Carson & Clayton, 1997). most Famennian-lowermost Toumaisian deposits show ex­ tremely reduced thickness, not more than several metres (see Figs 18-19). SUMMARY AND CONCLUSIONS

Tournaisian-Visean boundary The detailed conodont, miospore and ostracod analyses The working group of the Subcomission of Carbonifer­ permitted to distinguish: ous Stratigraphy of IUGS is currently trying to identify a (a) the Toumaisian sandbergi, Lower crenulata, isosti- boundary and to select the boundary stratotype and GSSP c/za-Upper crenulata and typicus conodont zones; that would closely correspond to the base of Visean as pro­ (b) nine local Toumaisian and Visean miospore zones posed during the 1967 Carboniferous Congress at Sheffield. and subzones: major (M ai-M a4), claytonii (CI1-CI2), pu­ A lineage within Eoparastaffella has been established in silla, campyloptera and pactilis; sections in southern China, and sections in Ireland are under (c) three Toumaisian, local benthic ostracod assem­ LOWER CARBONIFEROUS STRATIGRAPHY 211

Fig. 16. Ostracod assemblage Glyptopleura ruegensis-Carbonita fabulina (R-F). Specimens 1,3,4 are from Klanino 1 (depth indicated below), specimens 2, 5-7 are from Biesiekierz 1, 2890-2894 m. 1 - Shishaella electa Tschigova, 2392.3-2394 m; 2 - Beyrichiopsis fortis Jones & Kirkby; 3 - Beyrichiopsis binodosus Błaszyk & Natusiewicz, 2394-2397 m; 4 - Glyptopleura ruegensis Blumenstengel, 2463-2467 m; 5 - Glyptolichwinella annularis (Kummerow); 6 - Acutiangulata quadrata Robinson; 7 - Carbonita fabulina (Jones & Kirkby) blages and two subassemblages: Pseudoleperditia venulosa area). The Kurowo Oolite Formation and Grzybowo Cal­ (Vnj-Vn2), Cribroconchapostfoveata—Marginia tchigovae careous Shale Member are late Toumaisian in age, and are (P-T) and Glyptopleura ruegensis-Carbonita fabulina roughly time equivalents. The Drzewiany Sandstone For­ (R-F). mation spans latest Toumaisian and Visean. Integrated biostratigraphic analysis enabled correlation The uppermost Famennian-lowermost Toumaisian un- of local miospore and ostracod schemes with the “standard” fossiliferous, black clayey deposits rich in pyrite and or­ conodont zonation. The base of Mai subzone is within or ganic matter are reduced to several metres in thickness. The below the sandbergi Zone, that of Ma2 subzone is within results of both conodont and miospore studies suggest pres­ sandbergi zone, the Ma2/Ma3 subzonal boundary is not ence of a stratigraphic gap that comprises the uppermost Fa- younger than the Lower crenulata Zone, and base of Cl mennian (part of the Middle and the Upper praesulcata Zone is within or below the typicus Zone. The benthic ostra­ Zones) and the lowermost Toumaisian (the sulcata, dupli­ cod assemblage Vn corresponds to Mai - Mas (part) sub­ cata, and the lower part of the sandbergi Zone). A similar zones; P-T assemblage encompasses Ma3 (part), Ma4 and range of the gap is also indicated by the miospore data as the Cl i (part) subzones; R-F assemblage corresponds to Cl i equivalents of the western European miospore zones lepido- (part) and Cb subzones. phyta- explanatus, lepidophy-tanitidus, and most of, or the The oldest Carboniferous part of the S^polno Calcare­ entire verrucosus-incohatus Zone are missing. The results ous Shale Formation corresponds to the sandbergi or Upper of earlier studies on macrofauna suggest that the gap could duplicata zones. The top of the formation is diachronous, be smaller and limited to the Middle - Upper praesulcata corresponding to the Lower crenulata Zone (in the north­ Zones and to the Carboniferous sulcata and Lower dupli­ west), isosticha-Upper crenulata or typicus (in the east), and cata zones. Upper(?) typicus (Trzebiechowo Marl Member in the Brda The Tournaisian-Visean boundary has been established 212 H. MATYJA ET AL.

British Entomo- Western Pomerania taxa: Anaplanisporites baccatus, Colatisporites multisetus, C onodont Isles Benthic zoid Miospore miospore ostracod Prolycospora claytonii, Schopfites delicatus, Schopfites zonation zonation zonation zonation assembl. claviger and Verrucosisporites nitidus. In the present paper, some other species are listed under anchoralis generic or specific names differing from those used in the - latus aerlier papers (Tumau, 1975, 1978, 1979). These areKraeu- selisporites hibernicus Higgs (formerly Hymenozonotriletes mehli latus explanatus (Luber) Kedo morphological type I; Tumau 1978, pp. 12-13, pi. 5, figs. 16, 19, 20), Lophozonotriletes

typicus excisus Naumova, 1953 (formerly Tumulispora dentata unzoned (Hughes et Playford) n. comb.; Tumau, 1975, p. 516, pi. 5,

PC fig. 1), and Dictyotriletes glumaceus Byvsheva, 1972 (for­ merly Dictyotriletes margodentatus nov. sp.; Tumau, 1978, p. 8, pi.2, fig. 15). Some other taxonomic problems are dis­ isosticha 4 I cussed below. - U. crenulata BP 3 i L. crenulata Ma ------Genus Dictyotriletes Naumova emend. Smith et Butter- 2 worth, 1967 HD sandbergi 4-I--J-H1;------' Dictyotriletes plumosus (Butterworth et Spinner) emend Neville et Williams, 1963 U. duplicata L. duplicata Fig. 9(12-13)

sulcata 1979 Dictyotriletes pactilis Sullivan; Tumau, pi. 2, figs 6-8. Description: Trilete spores c. 60 (im in diameter, trilete mark tec- tate, rays extending almost to spore body margin. Exine 3 (xm thick. Distal surface bears a prominent reticulum. Lumina up to 24 Fig. 17. Correlation of biostratigraphic zonations for Tour- Hm across, muri narrow, up to 10 |xm high, wider at base, tapering naisian; * conodont zone of Irish conodont zonation (shallow wa­ to u membranous ridge with a frilled crest. One rnurus may almost ter facies) dating the PC/CM boundary (Higgs et al., 1988b); completely encircle the equator. relevant range charts are shown in the Appendix 2 Remarks: The assignement to D. pactilis was incorrect, the latter species lacks trilete rays.

approximately on the first appearance of the miospore spe­ Genus Pustulatisporites Potonie et Kremp emend. Im- cies Lycospora pusilla Somers. The boundary runs within grund, 1964 the lower part of the Drzewiany Sandstone Formation. The maximum thickness of the most completely pre­ Pustulatisporites uncatus (Kedo) Byvsheva, 1985 served Toumaisian deposits exceeds 800 metres (e.g., in the Fig. 8 (2) Kurowo 1 and Grzybowo 1 boreholes) and might have been even greater in the Wierzchowo-Brda area where the Tour- 1978 Pustulatisporites gibberosus (Haquebard) Playford; Tumau, naisian deposits, devoid of their upper parts (i.e., rocks of p. 7, pi. 1, figs 26, 27. 1979 Pustulatisporites gibberosus (Haquebard) Playford; Turnau, Upper typicus and anchoralis-latus conodont Zones), are pi. 1 , fig. 20 . over 650 m thick. 1980 Pustulatisporites uncatus (Kedo) nov. comb; Byvsheva, p. The penetrated fragments of the lower Visean are up to 58 (combination not valid). 200 m thick (Gozd 2 borehole) and those assigned to the 1985 Pustulatisporites uncatus (Kedo) Byvsheva; Byvsheva, pp. middle and upper parts of the Visean, are 260 m thick in the 95-96, tab. 18, figs 11-13, cum synonimis. Sarbinowo 1 section. Dimensions (after Tumau, 1978): 34.5(41.5)49.9 |xm (26 speci­ mens). Remarks: Tumau (1978, p. 7) noted that Pomeranian specimens SYSTEMATIC COMMENTS (MIOSPORES) assigned to P. gibberosus were smaller than those from the type material (see Playford, 1964). It appears that our specimens answer Most miospore species dealt with in this paper were de­ more closely the description of P. uncatus (Byvsheva, 1985, p. termined and described more than 20 years ago. Subse­ 95-96). quently, the second author worked on miospore taxonomy with such specialists in Carboniferous palynology as T.V. Genus Indotriradites Tiwari, 1964 Byvsheva, V.I. Avkhimovitch, G. Clayton, and K. Higgs. These studies, and the general progress in taxonomy of Pa­ Indotriradites explanatus (Luber) Playford, 1991 laeozoic spores resulted in changes in some specific and ge­ Fig. 7 (20) neric assignments. This topic was discussed in Clayton & 1941 Zonotriletes explanatus Luber; Luber & Waltz, p. 10, pi. 1, Tumau (1990), Avkhimovitch & Tumau (1994), and Tur- fig. 4. nau et al. (1994). The discussion concerned the following 1978 Hymenozonotriletes explanatus (Luber) Kedo morphologi- CONODONT MIOSPORE NW SE ZONES ZONES Gorzystaw Daszewo Wierzchowo Brda

Lycospora pusilla p u Drzewiany Sandstone Formation anchoralis - latus 2 Grzybowo Kurowo Grzybi Kurowo Prolycospora Shale Mb. - Oolite ^glshale Oolite U claytonii — • Fm. Fm. typicus — CI 1

isosticha -! Gozd Arkose Formation GRZYBOWO 1 U. crenulata 3 anchoralis Convolutispora z P L. crenulata major 2 -latus Sqpoino Calcareous Shale Formation Ma - 3- sandbergi 1 < U U duplicata — T

— typicus — WIERZCHOWO 9 sulcata Stratigraphic gap L P U praesulcata- C/3 CHMIELNO 1 M isosticha P T __ ACIS expansa S^polno Calcareous Shale Formation -U. crenulata WIERZCHOWO 4 P BIAŁY BOR 3 < 4022 m L. crenulata ■4055 P -3485 -3509 ACI2 sandbergi WIERZCHOWO 10 P A Cl BIAŁY BOR 1 BIELICA 1 R R N P P U |T?T°T°r3: x ci,— Ea asio A Cl, 3 duplicata— MSn-Ce2

L O X MaM - RZECZENICA 1 2801 x Ma? A Ma? ) M Du2-Ce2- P sulcata ' AM a, 1- X Ma2- , A Ma,.-.. 'Gaa

U z < z praesulcata M A R a? 0 -3716 > Grzybowo Drzewiany S^polno Calcareous Trzebiechowo Gozd Arkose Kurowo Oolite arkosic quartzitic marly nodular oolite ŁAJ Calcareous Sandstone shales i _ y-f nOm L Shale Formation Marl Member Formation Formation !•*•!•/!•*>! sandstones > !\*X v sandstones limestones limestones limestones O Shale Formation Formation ^MENNIAN ŁL Z> cored expansa u organodetritai 1 ; 1 i 1 1 dolomitic continuation conodont goniatite entomozoid benthic ostracode limestones anhydrite interval . . j ... 1 : limestones limestones of a section zone ^ a zone zone assemblage ■100

Fig. 18. Biostratigraphic correlation of borehole sections between Gorzystaw and Rzeczenica; all microfossil and goniatite bearing intervals dichotoma Entomozoid Zone. Insert shows biostratigraphic correlation of Pomerania Carboniferous lithostratigraphic units. Range of Famen- are marked. Carboniferous biostratigraphic zones/assemblages marked by two letter notations: full zonal names are in Figs 3, 10, 12, other no­ nian-Toumaisian stratigraphic gap within the Sqpolno Calcareous Shale Formation is also shown, arrow indicates an alternative position of the tations: La - latior Entomozoid Zone, Gaa - Gattendorfia subinvoluta Zone, Goa - Goniatites crenistria Zone, Famennian zones: Ex3 - Pri - gap upper range (lithostratigraphic units after Lipiec in Lipiec & Matyja, 1998) Upper expanse* - Lower praesulcata conodont zones, Ra - rarituberculata Miospore Zone, H-Di and H-D 2 - Lower and Upper hemi- sphaerica- Fig. 19. Biostratigraphic correlation o f borehole sections between Biesiekierz and Brda; all microfossil and goniatite bearing intervals are marked. See Fig. 18 for additional explanations additional for 18 Fig. See marked. are intervals bearing goniatite and microfossil all Brda; and Biesiekierz between sections borehole f o correlation Biostratigraphic 19. Fig. U. DEVON!AŃ T O U R N A I S I A N VISEAN FAMENNIAN . crenulata U. isosticha -latus . crenulata L. anchoralis typicus duplicata sulcata

ABNW 1 SARBINOWO Shale Formation Shale Sąpolno CalcareousSąpolno limestones organodetrital Caradoc 2796

Trzebiechowo Marl Member Marl limestones

IKOIE 1 NIEKŁONICE Gozd ArkoseGozd Formation dolomitic limestonBS 54 m 2514 l - m P

2595 CI2- AC Formation KurowoOolite ROSNOWO 1 ROSNOWO anhydrite P -3099 m -3099

| Shale Formation Shale | Grzybowo v L j interval ■j cored ■ Calcareous ; MTy,? — MTy,? CD R-F — T - P d c V, i oVn, X Ma A Cl - A ACI; Ma,?-

2 - ŁNN 1 KŁANINO

P S il- 2356 m 2356 il- S 2732 - 2779 2546 2410 56m contact m 2576 - tectonic- m 2576 - ^Ma - a? M I^ C A

Sandstone Drzewiany Formation I- C A 9 KŁANINO 2 KŁANINO erosional

P -2178 m -2167 r^ P M -APu- I C A " a R A . aena I Fmnin Dvna ? Devonian ? Devonian ? Famennian I. Famennian I.

KARSINA 1 KARSINA 2

sandstones arkosic ----- contact, range uncertaincontact,range tectonic-erosional P ------2682’ 2750 - 2750 - C - Cl A i c a 2

GOZD2 sandstones quartzitic P 2973 continuation of a sectionof a X X X Cl,?- A Cl2? —i Ma Ma„- 2 ? -

GOZD 3 GOZD usoe marls mudstones

P -2842'*' Ma' -2842'*' __ 2842 zone conodont X X Ma;-|| CI,— GOZD 4 GOZD P 2779 2750 miospore , zone aT- M A A Cl — A X Cif UOO 1 KUROWO m

P -2586 MTyn zone limestones marly goniatite X JkClr A Ra A ACI- Cl-

zone entomozoid Caradocian assemblage benthicostracode oolite limestones

0 100 m Appendix 2 Range charts of conodont, miospore and ostracod species

Conodont species range charts

Rzeczenica 1 Gorzysław 9 Karlino 1 Kłanino 1

Grzybowo Sąpolno S^polno Calcareous Shale Fm. S^polno Calcareous F o r m a tio n Formation — E > Shale Fm. Formation / Member Calc. Sh. Trzebiechowo Marl Member Shale Fm. Fm. S S S 5 Depth (m) Depth (m) -D» 1 Depth (m) i S S Upper Lower isost. - 2922 2922 - 2920 2 9 20 -29 16 2 9 16 -29 12 2912-2911 2911 -29 10 2 9 10 -29 09 2909 - 2907 2901 - 2899 2899 - 2896 2925 2925 - 2924 expansa L. cren. Conodont Zone — £> typicus ? Conodont Zone L. dupl. L. dupl. U. cren. Lower (Ex,) (D u,- Sn) (Du, - Ce,) Conodont Zone sandb. ? (Ty,?) Lower crenulata -** sandb. praesul. Lower (Sn -C e i) sandb. (Sn - Ce2) Conodont Zone Upper crenulata (Sn) sandbergi Bispathodus spinulicostatus expansa (Ce,) Pseudopolygnathus multistriatus (morphotype 1 ] + (Sn - Ce,) Polygnathus vogesi (Exj-Pr,) Siphonodella duplicata (morphotype 2) Polygnathus inornatus + Bispathodus costatus (morphotype 1) Siphonodella sulcata + Neopolygnathus communis (morphotype 1 Siphonodella quadruplicata + + + Polygnathus distortus Polygnathus inornatus Neopolygnathus communis (morphotype 1) + Polygnathus radinus Polygnathus streeli Siphonodella crenulata + + Neopolygnathus carina (morphotype 1) + + Polygnathus flabellus + Polygnathus symmetricus + Polygnathus triangulus + + Bielica 1 Biesiekierz 1 Hindeodus aff. cristulus + + Chmielno 1 Pseudopolygnathus primus + Gozd Sąpolno Trzebiechowo Grzybowo Sąpolno Formation Pseudopolygnathus nodomarginatus + + Formation Calc. Sh. Fm. Arkose Fm. Formation / Member Calc. Sh. Marl Shale Fm. Siphonodella cooperi (morphotype 2) + Fm. Member o § + + + Siphonodella obsoleta Depth (m) CO Bispathodus aculeatus anteposicornis + Depth (m) o Depth (m) Bispathodus spinulicostatus + + + + + 4 0 10 -40 09 3599 3599 - 3588 + + + + + + + 3953 - 3952 L. Neopolygnathus communis (morphotype 1) 3587 - 3586 3517 -35 16 u. Lower Polygnathus purus purus + + + Conodont Zone — £> typicus ? typicus ? isosticha - Lower Polygnathus purus subplanus + praesulcata Lower praesulcata (Ty,?)

Drzewiany 1

Trzebiechowo Kurowo Trzebiechowo Sąpolno Gozd Kurowo Formation / Member Member / Formation Marl Oolite Marl Member Formation —£> Calc. Sh. Arkose Oolite M ember Fm. Fm. Fm. Fm. 2 1 l £ CO Depth (m) -----£ > 1 Depth (m) Depth (m) CM 4 CD (D CJ Sj 5 S 2478 2478 - 2473 2311 -2305 L. crenulata ? Lower isosticha - Lower Lower Conodont Zone typicus U. crenulata typicus sandbergi ? Conodont Zone — £> ? typicus (Sn? - C e , ?) (TYi) (Ty,) L. crenulata H V i) (C e i.2)

+ Pseudopolygnathus multistriatus (morphotype 1) + + Neopolygnathus carina (morphotype 2) Pseudopolygnathus multistriatus (early morphotype) Pseudopolygnathus multistriatus (morphotype 1) + Pseudopolygnathus multistriatus (morphotype 2) + Clydagnathus unicornis + Clydagnathus unicornis + Clydagnathus unicornis + + Siphonodella isosticha Bispathodus aculeatus aculeatus + Neopolygnathus communis (morphotype 1) + + Neopolygnathus communis (morphotype 1) + Polygnathus inornatus + Hindeodus aff .cristulus + + Siphonodella sulcata + Appendix 2 Miospore species range charts (selected boreholes)

Rzeczenica 1 Wierzchowo 10 Drzewiany 1 Sarbinowo 1

Sąpolno Drzewi; Formation — £> Drzewiany Sandstone Fm. Formation / Member —£> Calc. Sh. Trzebiechowo Marl Member Formation —£> Gozd Arkose Fm. Formation Kurowo Oolite Fm. Sandston cn ■q- Fm. £ in CM | | § 1 1 Depth (m) °? Depth 1 (m) ----£> CM co Depth (m) — £> £ 3 IO s S 3 8 CO ° CM CM 2911 -29102911 3003 2999 - 3003 - 2933 2937 - 2922 2923 2920 2921 - 2920-2916 2915-2913 2896 2899 - Miospore Subzone Cl Miospore Zone Pu Ca Pa Ostracod species range charts Miospore Subzone — D> Ma Ma C | Miospore Zone/ Subzone — $> Ra Ma1 Ma2 Miospores: Miospores: Anaplanisporites baccatus + + + + Brda 1 Miospores : Miospores: Acanthotriletes socraticus Crassispora trychera + + Sąpolno Trzebiechowo + + + + + + Auroraspora macra Lycospora pusilla + + + + + + Grandispora cornuta + + + + + + + Auroraspora macra Form ation/Member — £> Calc. Sh. Mari Colatisporites multisetus Rugospora minuta + + + + Auroraspora macra + + Auroraspora asperella + Fm. Member Convolutispora mellita Waltzispora planiangulata + + + + + + Converrucosisporites curvatus + + Baculatisporites fusticulus + + + Crassispora trychera Colatisporites multisetus + + + + + Bascaudaspora submarginata + + + + Retispora lepidophyta* + + Corbulispora cancellata Punctatisporites aerarius + + + + s + + + + + + Convolutispora major + 1 s Diducites versabilis* Dictyotriletes glumaceus Corbulispora cancellata + + + + Convolutispora mellita + + + Depth (m) — £> Grandispora conspicua + + + + Discernisporites micromanifestus Lophotriletes tribulosus + + + CO Crassispora trychera + + + + + 1 S 1 Grandispora lupata + + + + + + + Knoxisporites literatus Convolutispora mellita + Discernisporites micromanifestus + + Raistrickia variabilis + + Lophozonotriletes excisus Schulzospora campyloptera + + + Diaphanospora angusta + + Prolycospora claytonii Benthic ostracod Retispora cassicula* + + Knoxisporites stephanephorus + + Vn P-T + Punctatosporites scabratus assemblages v n , Tumulispora rarituberculata + + + + + + + + + Endoculeospora gradzinskii Dictyotriletes castanaeformis + + + Pustulatisporites uncatus Knoxisporites literatus + + + + + + + + Foveospores insculptus + Knoxisporites cf. ruhlandi + Ostracodes: Endoculeospora gradzinskii + + + + + Indotriradites explanatus + Retusotriletes occultus Dictyotriletes plumosus + + + + Schopfites delicatus Umbonatisporites abstrusus + + Knoxisporites hederatus Murospora aurita + Pseudoleperditia venulosa + + + Spelaeotriletes pretiosus + + + Lophozonotriletes excisus + + Microreticulatisporites densus + Shishaella alekseevae + + + + Tumulispora malevkensis Umbonatisporites distinctus Pustulatisporites uncatus + + + + + Lycospora noctuina + + Coryellina triceratina + + + Grandispora uncata + + + + Tumulispora rarituberculata + + + Spelaeotriletes obtusus + Cingulizonates bialatus + + Amphissites similaris + + + Retusotriletes incohatus Verrucosisporites nitidus Tumulispora rarituberculata + + + + Kraeuselisporites cf. echinatus + + cutiangulata acutiangulata + + + + Knoxisporites pristinus + + Leiotriletes sphaerotriangularis Umbonatisporites distinctus + + + + Chaetosphaerites pollenisimilis + + Acutiangulata rara + + + Tumulispora variverrucata + Anaplanisporites baccatus + + + + + Perotriiites tesselatus + + Chamishaella obscura + Kraeuselisporites hibernicus ? + Verrucosisporites nitidus Convolutispora major Densosporites variabilis + Shivaella longa + + Grandispora upensis + Spelaeotriletes balteatus + + Reticulatisporites planus Potoniespores delicatus + Sulcocavellina tersiensis + Reticulatisporites planus + Spelaeotriletes pretiosus + + + + Baculatisporites fusticulus + Schulzospora ocellata + Bairdia lecta + Convolutispora major + + Raistrickia variabilis Grandispora uncata Schulzospora plicata + Cribroconcha quasicornigera + + + + + + + Schopfites delicatus + Murospora sublobata Lophozonotriletes excisus Diatomozonotriletes cervicornutus + Marginia tschigovae + Prolycospora claytonii + + + Dictyotriletes membranireticulatus Asperispora acuta + Densosporites dentatus + Carboprimitia elata + Anaplanisporites baccatus + + + Bascaudaspora submarginata Raistrickia corynoges + + Pilosisporites venustus + Editia cf. kiselensis + Colatisporites multisetus + + + Punctatisporites pseudobesus Tumulispora ordinaria + + Foveospores insculptus + + + Perotrilites ordinarius Umbonatisporites distinctus + Dictyotriletes glumaceus Rotaspora fracta + + + Raistrickia corynoges Cyrtospora cristifera + Acanthotriletes socraticus Kraeuselisporites hibernicus + Raistrickia condylosa Vallatisporites pusillites* + Schopfites claviger Kłaninol Knoxisporites literatus + Rugospora radiata* + Auroraspora panda Grandispora echinata + Raistrickia corynoges + Sąpolno Grzybowo Drzewiany Tripartites incisotrilobus Biesiekierz 1 Formation Calc. Sh. Shale Sandstone Verrucosisporites nitidus + + + Rugospora minuta Fm. Fm. Fm. Indotriradites explanatus + Gorgonispora multiplicabilis Grzybowo Formation — £> Shale Umbonatisporites distinctus + Raistrickia clavata £ Fm. 5 £ Biały Bór 1 Depth (m) ----D> » - 2 Niekłonice 1 Trzebiechowo Mari CM Member Depth (m) — £> CM i Member Sąpolno Gozd 3 Benthic ostracod Formation — £> tS 2917.6-2890.7 Vn P-T R-F Calc. Sh. Fm. Arkose Fm. assemblages Depth (m) — £> £ 4 2 Benthic ostracod | co J5 $ S CD 1 R-F Ostracodes: Depth (m) ----£> assemblages Miospore Subzone — D> Ma2_4 Cl-t Carboprimitia elata + 1 1 1 1 1 Ostracodes: Amphissites similaris + Miospores: Shishaella electa + Marginia tschigovae + Miospore Subzone — 3> Ma Ma Cl Auroraspora macra + + + Karsina 1 Beyrichiopsis fortis + Cribroconcha postfoveata + Convolutispora major + + Glyptolichwinella annularis + Graphiadactyllis reticulocostatus + Miospores: Convolutispora mellita + + + Formation Drzewiany Sandstone Fm. Acutiangulata quadrata + Shishaella electa + + + + + Auroraspora macra + + + Corbulispora cancellata + + + Carbonita fabulina + Beyrichiopsis binodosus + + Knoxisporites triradiatus + + CD Discernisporites micromanifestus + + S § B. fortis + Lophozonotriletes excisus + + + 1 CN CM CM CM Endoculeospora setacea + Depth (m) Glyptolichwinella annularis + Endoculeospora gradzihskii + + Chmielno 1 Foveosporites appositus + ? 05 n s ? Glyptopleura ruegensis + + Raistrickia corynoges + + + + + Knoxisporites literatus + + CM CM CM CM CM CM Gozd Acutiangulata quadrata + + Grandispora cf. lupata + Knoxisporites hederatus + Formation — 5> Arcose Punctatisporites glaber + + + Knoxisporites pristinus + Miospore Subzone / Zone— ? > Cl Pu Fm. Verrucosisporites nitidus + + Knoxisporites triradiatus + Retusotriletes incohatus + + + + + s 3 § Pustulatisporites uncatus + Knoxisporites margarethae Miospores: Leiotriletes sphaerotriangularis + + Depth (m) ^ Convolutispora major + + Anaplanisporites baccatus + + + + + + Daszewo R3P Indotriradites explanatus + Murospora sublobata + i Auroraspora macra + + + + + + 1 1 Sąpolno Gozd + + + + Punctatosporites scabrosus + + Knoxisporites literatus Auroraspora panda + + + Formation — £> Calc. Sh. Arcose + Pustulatisporites uncatus + + Cyrtospora cristifera Colatisporites multisetus + + + + + + Benthic ostracod Fm. Fm. Convolutispora mellita + + + Schopfites delicatus + + Vn r - Convolutispora mellita + + + + + assemblages 1 + Tripartites incisotrilobus + Discernisporites micromanifestus Gorgonispora multiplicabilis + + + + + rr ° 05 + + Knoxisporites pristinus + Tumulispora rarituberculata Leiotriletes sphaerotriangularis + + + + + Ostracodes: Knoxisporites hederatus + Tumulispora variverrucata + Prolycospora claytonii + + + + + + Depth (m) ---- £ > Namaya reticulata + Si1 Corbulispora cancellata + + Verrucosisporites nitidus + + Punctatisporites aerarius + + + + + 1 I Pseudoleperditia venulosa + 1 Foveosporites insculptus + Anaplanisporites delicatus + Raistrickia corynoges + + + Coryellina triceratina + Umbonatisporites distinctus + + Acanthotriletes socraticus + Raistrickia clavata + + + + Shishaella alekseevae + + Benthic ostracod Dictyotriletes papillatus + Baculatisporites fusticulus + Retusotriletes occultus + P-T R-F Shivaella longa + + assemblages Rupospora polyptycha + Bascaudaspora submarginata + + Schopfites claviger + + + + + + + Amphissites similaris + Anaplanosporites baccatus Colatisporites multisetus + + Schopfites delicatus + + + + + + Ostracodes: + + Sulcocavellina tersiensis + Crassispora trychera Crassispora trychera + Auroraspora solisortus + + + Bairdia lecta + Carboprimitia elata + Colatisporites multisetus Dictyotriletes glumaceus + Retusotriletes circularis + Kraeuselisporites hibernicus + + + Coryellina triceratina + + Dictyotriletes membranireticulatus + Crassispora trychera + + + Acutiangulata rara Prolycospora claytonii + + + + Richterina (R.) latior + Graphiadactyllis reticulocostatus + + Prolycospora claytonii + + Knoxisporites hederatus Retusotriletes occultus + + + Acutiangulata acutiangulata + + Cribroconcha quasicornigera + Raistrickia clavata + Retusotriletes incohatus Reticulatisporites planus + Baculatisporites fusticulus + Marginia tschigovae + Autiangulata acutiangulata + + Spelaeotriletes pretiosus + Schopfites delicatus + Discernisporites micromanifestus + Cribroconcha postfoveata + Beyrichiopsis binodosus + Umbonatisporites distinctus + Raistrickia clavata + Lycospora pusilla + + + Acutiangulata quadrata + Dictyotriletes planus + Graphiadactyllis reticulocostatus Tripartites incisotrilobus + Rugospora minuta + +

* probably redeposited LOWER CARBONIFEROUS STRATIGRAPHY 213

cal type II; Turnau, p. 13, pi. 5, fig. 18. MIOSPORES 1985 Hymenozonotriletes explanatus (Luber) Kedo; Byvsheva, pp. 139-140, pi. 27, fig. 13. Acanthotriletes socraticus Neves & Ioannides, 1974 1991 Indotriradites explanatus (Luber) Playford, pp. 103-104, pi. Anapiculatisporites concinnus Playford, 1962 3, figs 17, 18. Anaplanisporites baccatus Hoffmeister, Staplin & Malloy, 1955 Auroraspora asperella (Kedo) Van der Zwan, 1980 Remarks. Turnau (1978, pp. 12-13) noted, that in various papers, Auroraspora macra Sullivan, 1968 the concept of H. explanatus varied, probably because the species Turnau, 1978 was originally too generally described, and not sufficiently illus­ Auroraspora panda trated. This author described two differing morphological types Auroraspora solisorta Hoffmeister, Staplin & Malloy, 1955 (type I and type II) that represented H. explanatus in the broad Baculatisporitesfusticulus Sullivan, 1968 sense. At the present state of recognition of the world Carbonifer­ Bascaudaspora submarginata (Playford) Higgs, Clayton & Kee­ ous miospore floras, the concept of the discussed species is quite gan, 1988 clear (see Byvsheva, 1985; Playford, 1990). Cingulizonates bialatus (Waltz) Smith & Butterworth, 1967 Chaetosphaerites pollenisimilis (Horst) Butterworth & Williams, 1958 Colatisporites multisetus (Luber) Avkhimovitch & Turnau, 1994 Acknowledgements Converrucosisporites curvatus (Naumova) Turnau, 1975 Converrucosisporites horridus (Ishchenko) Turnau, 1979 var. We sincerely thank our collegues who rendered help during trigonalis Jachowicz, 1967 the preparation of this paper, and especially Elżbieta Tarka (PIG, Convolutispora major (Kedo) Turnau, 1978 Warszawa) and Dr. Leszek Chudzikiewicz (ING PAN, Kraków) Convolutispora mellita Hoffmeister, Staplin & Malloy, 1955 for graphic elaboration of the Figures, Maria Sidorowicz (ING Corbulispora cancellata (Waltz) Bharadwaj & Venkatachala, PAN, Kraków) for laboratory preparation of palynological sam­ 1971 ples, and Dr Andrzej Łaptaś for his help in computer problems. Crassispora trychera Neves & Ioannides, 1974 Cymbosporites acutus (Kedo) Byvsheva, 1985 Cyrtospora cristifera (Luber) van der Zwan Densosporites dentatus (Waltz) Potonie & Kremp, 1956 APPENDIX 1 - LIST OF CONODONT, MIOSPORE Densosporites variabilis (Waltz) Potonie & Kremp, 1956 AND OSTRACOD SPECIES Diaphanospora angusta (Haquebard) Playford & McGregor, 1993 Diatomozonotriletes cervicornutus (Staplin) Playford, 1963 CONODONTS Diatomozonotriletes saetosus (Haquebard & Barss) Hughes & Playford, 1961 Bispathodus aculeatus aculeatus (Branson & Mehl, 1934) Dictyotriletes castanaeformis (Horst) Sullivan, 1964 Bispathodus aculeatus anteposicornis (Scott, 1961) Dictyotriletesglumaceus (Byvsheva) Byvsheva, 1980 Bispathodus spinulicostatus (Branson, 1934) Dictyotriletes membranireticulatus Bertelsen, 1972 Bispathodus stabilis (Branson & Mehl, 1934) Dictyotriletes plumosus (Butterworth & Spinner) Neville & Wil­ Clydagnathus unicornis Rhodes, Austin & Druce, 1969 liams, 1963 Elictognathus bialatus (Branson & Mehl, 1934) Dictyotriletes papillatus (Naumova) Byvsheva, 1963 Elictognathus laceratus (Branson & Mehl, 1934) Diducites versabilis (Kedo) Van Veen, 1981 Gnathodus cuneiformis Mehl & Thomas, 1947 Discernisporites micromanifestus (Haquebard) Sabry & Neves, Hindeodus aff. cristulus (Youngquist & Miller, 1949) 1971 “Hindeodus ” crassidentatus (Branson & Mehl, 1934) Endoculeospora gradzinskii Turnau, 1975 Neopolygnathus carina (Hass, 1959) Foveosporites appositus Playford, 1971 Neopolygnathus communis (Branson & Mehl, 1934) Foveosporites insculptus Playford, 1962 Pandorinellina plumula (Rhodes, Austin & Druce, 1969) Gorgonispora multiplicabilis (Kedo) Turnau, 1978 Polygnathus distortus Branson & Mehl, 1934 Grandispora conspicua (Playford) Playford, 1964 Polygnathus flabellus (Branson & Mehl, 1934) Grandispora cornuta Higgs, 1975 Polygnathus inornatus Branson, 1934 Grandispora echinata Haquebard, 1957 Polygnathus purus purus Voges, 1959 Grandispora lupata Turnau, 1975 Polygnathus purus subplanus Voges, 1959 Grandispora upensis (Kedo) Byvsheva, 1980 Polygnathus radinus (Cooper, 1939) Grandispora uncata (Haquebard) Playford, 1971 Polygnathus spicatus Branson, 1934 Indotriradites explanatus (Luber) Playford, 1991 Polygnathus symmetricus Branson, 1934 Knoxisporites hederatus (Ishchenko) Playford, 1963 Polygnathus triangulus Voges, 1959 Knoxisporites literatus (Waltz) Playford, 1976 Polygnathus vogesi Ziegler, 1962 Knoxisporites margarethae Hughes & Playford, 1961 Pseudopoly gnathus dentilineatus Branson, 1934 Knoxisporites pristinus Sullivan, 1968 Pseudopolygnathus multistriatus Mehl & Thomas, 1947 Knoxisporites ruhlandi Doubinger & Raucher, 1966 Pseudopoly gnathus nodomarginatus (Branson, 1934) Knoxisporites stephanephorus Love, 1960 Pseudopolygnathus primus Branson & Mehl, 1934 Knoxisporites triradiatus Hoffmeister, Staplin & Malloy, 1955 Siphonodella cooperi Hass, 1959 Kraeuselisporites echinatus Owens, Mishell & Marshall, 1976 Siphonodella crenulata (Cooper, 1939) Kraeuselisporites hibernicus Higgs, 1975 Siphonodella duplicata (Branson & Mehl, 1934) Leiotriletes sphaerotriangularis (Loose) Potonie & Kremp, 1954 Siphonodella isosticha (Cooper, 1939) Lophotriletes tribulosus Sullivan, 1968 Siphonodella obsoleta Hass, 1959 Lophozonotriletes excisus Naumova, 1953 Siphonodella quadruplicata (Branson & Mehl, 1934) Lycospora noctuina Butterworth & Williams, 1958 Siphonodella sulcata (Huddle, 1934) Lycospora pusilla (Ibrahim) Somers, 1972 214 H. MATYJA ETAL.

Microreticulatisporites densus (Love) Sullivan, 1964 Cribroconcha postfoveata Griindel, 1975 Monilospora culta (Byvsheva) Byvsheva, 1980 Editia cf. kiselensis (Posner in Tschigova, 1960) s. Robinson, 1978 Murospora aurita (Waltz) Play ford, 1962 Glyptopleura ruegensis Blumenstengel, 1977 Murospora sublobata (Waltz) Playford, 1962 Glyptolichwinella annularis (Kummerow, 1939) Orbisporis convolutus Butterworth & Spinner, 1967 Graphiadactyllis reticulocostatus Griindel, 1975 Perotrilites ordinarius Tumau, 1979 Marginia tschigovae (Palant, 1960) Perotrilites tessellatus (Staplin) Neville, 1973 Namaya reticulata Green, 1963 Pilosisporites venustus Sullivan & Marshall, 1966 Pseudoleperditia venulosa (Kummerow 1939) Potoniespores delicatus Playford, 1962 Richterina (Richterina) latior Rabien, 1960 Prolycospora claytonii Tumau, 1978 Shishaella alekseevae Tschigova, 1977 Punctatisporites aerarius Butterworth & Williams, 1958 Shishaella electa Tschigova, 1977 Punctatisporites glaber (Naumova) Playford, 1962 Shivaella longa (Tschigova, 1960) Punctatisporites pseudobesus Playford, 1962 Sulcocavellina tersiensis Bushmina, 1968 Punctatosporites scabrosus (Kedo) Tumau Pustulatisporites uncatus (Kedo) Byvsheva, 1985 Raistrickia clavata (Haquebard) Playford, 1964 Raistrickia condylosa Higgs, 1975 REFERENCES Raistrickia corynoges Sullivan, 1968 Raistrickia variabilis Dolby & Neves, 1970 Avkhimovitch, V. I., 1993. Zonation and spore complexes of the Reticulatisporites planus Hughes & Playford Devonian and Carboniferous boundary deposits of the Pripyat Retispora macroreticulata (Kedo) Byvsheva, 1985 Depression (Byelorussia). Annates Societe Geologique Bel­ Retispora lepidophvta (Kedo) Playford, 1976 gique, 115: 425-451. Retusotriletes circularis Turnau, 1978 Avkhimovitch, V. I. & Tumau, E., 1994. The Lower Carbonifer­ Retusotriletes incohatus Sullivan, 1964 ous Prolycospora claytonii Zone of Western Pomerania and Retusotriletes occultus Turnau, 1978 its equivalents in Belorussia and northwestern Europe. An­ Rotaspora fracta Schemel, 1950 nates Societatis Geologorum Poloniae, 63: 249-263. Rugospora minuta Neves & loannides, 1974 Avkhimovitch, V. I., Turnau, E. & Clayton, G., 1993. Correlation Rugosporapolyptycha Neves & loannides, 1974 of uppermost Devonian and Lower Carboniferous miospore Rugospora radiata (Jushko) Byvsheva, 1985 zonations in Byelorussia, Poland and western Europe. An- Schopfites claviger Sullivan, 1968 nales Societe Geologique Belgique, 115: 453-458. Schopfites delicatus Higgs emend. Higgs, Clayton & Keegan, Becker, G. & Bless, M. J. M., 1974. Ostracode stratigraphy of the 1988 Ardenno-Rhenish Devonian and Dinantian. International Schulzospora campyloptera (Waltz) Hoffmeister, Staplin & Mal­ Symposium on Belgian Micropaleontological Limits from loy, 1955 Emsian to Visean, Namur 1974, 1: 1-52. Schulzospora ocellata (Horst) Potonie & Kremp, 1956 Becker, G., Bless, M. J. M., Streel, M. & Thorez, J., 1974. Palynol- Schulzospora plicata Butterworth & Williams, 1958 ogy and ostracode distribution in the Upper Devonian and ba­ Spelaeotriletes balteatus (Playford) Higgs, 1996 sal Dinantian of Belgium and their dependence on sedi­ Spelaeotriletes obtusus Higgs, 1975 mentary facies. Mededelingen Rijks Geologische Dienst, Spelaeotriletes pretiosus (Playford) Neves & Belt, 1970 Nieuwe Serie, 25 (2): 9-99. Tripartites inciso-trilobus (Naumova) Karczewska & Turnau, Bednarczyk, W., 1974. The Ordovician in the Koszalin - Chojnice 1974 region (Western Pomerania). Acta Geologica Polonica, 24: Tumulispora malevkensis (Kedo) Turnau, 1978 581-600. Tumulispora ordinaria Staplin & Jansoniu, 1964 Belka, Z., 1985. Lower Carboniferous conodont biostratigraphy in Tumulispora rarituberculata (Luber) Potonie, 1966 the northeastern part of the Moravia-Silesia Basin. Acta Geo­ Tumulispora variverrucata (Playford) Staplin & Jansonius, 1964 logica Polonica, 35: 33-60. Umbonatisporites abstrusus (Playford) Clayton, 1970 Belka, Z. & Groessens, E. 1986. Conodont succession across the Umbonatisporites distinctus Clayton, 1970 Tournaisian Visean Boundary Beds at Salet, Belgium. Bulle­ Vallatisporites pusillites (Kedo) Dolby & Neves, 1970 tin de la Societe Beige de Geologie, 95: 257-280. Verrucosisporites nitidus Playford, 1964 Bless, M. J. M., Crasquin, S., Groos-Uffenorde, H. & Lethiers, F., Waltzispora planiangulata Sullivan, 1964 1986. Late Devonian to Dinantian Ostracodes (comments on taxonomy, stratigraphy and paleoecology). Annales Societe Geologique Belgique, 109: 1-8. OSTRACODS Blumenstengel, H., 1975a. Zur biostratigraphischen und faziellen Bedeutung der Ostracoden des Dinant von Riigen und Hid- Acutiangulata acutiangulata (Posner, 1960) densee. Zeitschrift fu r Geologische Wissenschaften, 3 (7): Acutiangulata quadrata Robinson, 1978 951-969. Acutiangulata rara Bushmina, 1978 Blumenstengel, H., 1975b. Zur Gattung Glyptopleura Girty (Os- Amphissites similaris Morey, 1936 tracoda) aus dem Dinant von Riigen. Zeitschrift fur Geolo­ Bairdia lecta Bushmina, 1970 gische Wissenschaften, 5 (10): 1235-1251. Beyrichiopsisfortis Jones & Kirkby, 1886 Blaszyk, J. & Natusiewicz, D., 1973. Carboniferous ostracods Beyrichiopsis binodosus Blaszyk & Natusiewicz, 1973 from the borings in northwestern Poland. Acta Palaeonto- Carbonita fabulina (Jones & Kirkby, 1879) logica Polonica, 18(1): 117-151. Carboprimitia elata Tschigova, 1977 Byvsheva, T. V., 1980. Zonal spore assemblages of upper Tour­ Chamishaella obscura Tschigova, 1977 naisian deposits of eastern regions of the Russian Platform. Coryellina triceratina (Posner, 1955) (In Russian only). In: Byvsheva, T. V. (ed.) Palynological In­ Cribroconcha quasicornigera Bushmina, 1968 vestigations o f Proterozoic and Phanerozoic oil and gas bear­ LOWER CARBONIFEROUS STRATIGRAPHY 215

ing regions o f USSR. Trudy VNIGNI, 217, pp. 53—61. Formation, Alberta. Research Council Alberta, Bulletin, 11: Byvsheva, T. V., 1985. Spores from Toumaisian and Visean de­ 1-237. posits of Russian Platform. (In Russian only). In: Menner, V. Groessens, E., 1974. Distribution de conodontes dans le Dinantien V. & Byvsheva, T. V. (eds), Atlas of spores and pollen o f oil- de la Belgique. International Symposium on Belgian Micro- bearing strata o f the Phanerozoic o f the Russian and Turan paleontological limits from Emsian to Visean, Namur, 1964, Plates. Trudy VNIGNI, 253: 80-157, 203-217. 17: 1-193." Carman, M. K., 1987. Conodonts o f the Lake Valley Formation Groos-Uffenorde, H., 1984. Review of the stratigraphy with ento- (Kinderhookian-Osagean), Sacramento Mountains, New mozoid ostracodes. In: Southerland P. K. & Manger, W.L. Mexico, USA. In: Brencle, P. L., Lane, H. R. & Manger, W. (eds), Compte Rendu Neuvieme Congres International Stra­ L. (eds), Selected studies in Carboniferous paleontology and tigraphie Geologie Carbonifere, 2: 212-222. biostratigraphy. Courier Forschungsinstitut Senckenberg, 98: Groos-Uffenorde, H. & Schindler, E., 1990. The effect of global 47-73. events on entomozoacean Ostracoda. In: Whatley, R & May- Carson, B. & Clayton, G., 1997. The Dinantian (Lower Carbonif­ bury, C. (eds), Ostracoda and global events, British Micropa- erous) palynostratigraphy of Rtigen, northern Germany. In: laeontological Society Publication Series: pp. 101-112. Podemski, M., Dybova-Jachowicz, S., Jaworowski, K., Ju­ Grtindel, J., 1975. Neue Ostacoden der Healdiacea und Quasillita- reczka, J. & Wagner, R. (eds), Proceedings of the XIII Inter­ cea aus dem Dinant der Insel Riigen. Zeitschrift fu r Geolo­ national Congress Carboniferous Permian. Prace Państwo­ gische Wissenschaften, 3: 971-983. wego Instytutu Geologicznego, 157: 219-228. Higgs, K. T., Clayton, G. & Keegan, J. B., 1988a. Stratigraphie Clausen, C. D., Leuteritz K. & Ziegler, W. 1989. Ausgewahlte and systematic palynoiogy of the Toumaisian rocks of Ire­ Profile an der Devon/Karbon-Grentze im Sauerland (Rheini- land. Geological Survey Ireland, Special Paper, 1: 5-93. sches Schiefergebirge). Das Oberdevon des Rheinischen Higgs, K. T., Dreesen, R. & Dusar, M., 1992. Palynostratigraphy Schiefergebirges. Fortschritte in der Geologie von Rheinland of the Tournaisian (Hastarian) rocks in the Namur Synclinor- und Westfalen, 35: 161-226. ium, West Flanders, Belgium. Review of Palaeobotany and Clayton, G., 1985. Dinantian miospores and inter-continental cor­ Palynoiogy, 72: 159-164. relation. Compte Rendu 10 Congress Stratigraphie Geologie Higgs, K. T., McPhilemy, B., Keegan, J. B. & Clayton G., 1988b. Carbonifere (Madrid 1983), 4: 9-23. New data on Palynological boundaries within the Irish Dinan­ Clayton, G., Colthurst, J. R. J., Higgs, K., Jones, G. L. L. & Kee­ tian. Review of Palaeobotany and Palynoiogy, 56: 61-68. gan, J. B., 1977a. 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Trudy CNIGRI, 137: 1-107. 130: 15-30. Marchant, T. R., Sevastopulo, G. D. & Clayton, G., 1984. Prelimi­ Dadlez, R., 1978. Sub-Permian rock complexes in the Koszalin - nary correlation of Irish Toumaisian conodont, foraminiferal Chojnice zone. (In Polish, English summary). Kwartalnik and miospore zonal schemes. In: Southerland P. K. & Man­ Geologiczny, 22: 269-301. ger, W. L. (eds), Compte Rendu Neuvieme Congres Interna­ Górecka, T. & Parka, Z. 1980. Stratigraphy o f Carboniferous de­ tional Stratigraphie Geologie Carbonifere, 2: 282-288. posits from borehole Koszalin 1G-1 on palynological data. (In Matyja, H., 1976. Biostratigraphy of the Devonian-Carboniferous Polish, English summary). Prace Naukowe Instytutu Gór­ passage beds from some selected profiles of NW Poland. Acta nictwa Politechniki Wrocławskiej, 35, Studia Materiałowe, Geologica Polonica, 26: 490-539. 16: 35-44. Matyja, H., 1993. Upper Devonian of Western Pomerania. Acta Green, R., 1963. 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Matyja, H. & Stempien-Salek, M., 1994. Devonian/Carboniferous Turnau, E., 1979. Correlations of Upper Devonian and Carbonifer­ boundary and the associated phenomena in Western Pomera­ ous deposits of Western Pomerania, based on miospore study. nia (NW Poland). Annales Societe Geologique Belgique, 116: (In Polish, English summary). Annales Societatis Geologo- 249-263. rum Poloniae, 49: 231-269. Matyja, H. & Turnau, E., 1989. Conodonts and spores from the Turnau, E., Avkhimovitch, V. I., Byvscheva, T. V., Clayton, G., Devonian/Carboniferous boundary beds in Poland. X f Con- Higgs, K. T. & Owens, B., 1994. Taxonomy and stratigraphi­ gres International Stratigraphie Geologie Carbonifere Bejing cal distribution of Verrucosisporites nitidus Playford, 1964 1987, Compte Rendu 3: 61-72. and related species. Review of Palaeobotany and Palynology, Muszynski, A., Biernacka, J., Lorenc, S., Protas, A., Urbanek, Z. 81: 289-295. & Wojewoda, J., 1996. Petrology and sedimentary environ­ Turnau, E., Avchimovitch, V. I., Byvsheva, T. V., Carson, B., ment of Lower Carboniferous volcanoclastic sediments in the Clayton, G. & Owens, B., 1997. The first appearance in region of Dygowo and Klanino (Koszalin-Chojnice zone). (In Europe o f Lycospora pusilla (Ibrahim) Somers and its rela­ Polish only). Geologos, 1: 93-126. tionship to the Toumaisian/Visean boundary. In: Podemski, Neves, R., Gueinn, K. J., Clayton, G., Ioannides, N. S., Neville, R. M., Dybova-Jachowicz, S., Jaworowski, K., Jureczka, J. & S. W., & Kruszewska, K., 1973. Palynological correlations Wagner, R. (eds), Proceedings of the XIII International Con­ within the Lower Carboniferous of Scotland and Northern gress Carboniferous Permian. Prace Państwowego Instytutu England. Royal Society Edinbourg Transactions, 69 (2): 2 3 - Geologicznego, 157: 289-294. 70. Van derZwan, C., 1980. Aspects of Late Devonian and Early Car­ Paproth, E., Feist, R. & Flajs, G., 1991. Decision on the Devo­ boniferous palynology of southern Ireland. III. Palynology of nian-Carboniferous boundary stratotype. Episodes, 14: 331— Devonian-Carboniferous transition sequences with special 336. reference to the Bantry Bay area, Co. Cork. Review ofPalaeo- Playford, G., 1964. Miospores from the Mississippian Horton botany and Palynology, 30: 165-286. Group, eastern Canada. Geological Survey of Canada Bulle­ Varker, W. J. & Sevastopulo, G. D., 1985. The Carboniferous Sys­ tin, 107: 1-47. tem: Part. 1 - Conodonts of the Dinantian Subsystem from Playford, G., 1991. Australian Lower Carboniferous miospores Great Britain and Ireland. In: Higgins, A. C. & Austin, R. L. relevant to extra-Gondwanic correlation: an evaluation. Cou­ (Eds), A stratigraphical index o f conodonts. British Micropa- rier Forschungsinstitut Senckenberg, 130: 85-125. laeontological Society Series: pp. 167-209. Riley, N.J., 1993. Dinantian (Lower Carboniferous) biostratigra­ Webster, G. D. & Groessens, E., 1990. Conodont subdivision of phy and chronostratigraphy in the British Isles. Journal o f the the Lower Carboniferous. Courier Forschungsinstitut Senck­ Geological Society o f London, 150: 427^146. enberg, 130: 31-40. Robinson, E., 1978. The Carboniferous. In: Bate, R. & Robinson, Żbikowska, B., 1992. Entomozoaceans (Ostracoda) from the Up­ E. (eds), A stratigraphical index o f British Ostracoda, Geo­ per Devonian and Lower Carboniferous of Western Pomera­ logical Journal Special Issue, 8: 121-166. nia. (In Polish only). Przegląd Geologiczny, 40 (10): 612. Sandberg, C. A., Ziegler, W., Leuteritz, K. & Brill, S. M., 1978. Żelichowski, A. M., 1983. The Carboniferous in western Pomera­ Phylogeny, speciation, and zonation of Siphonodella (Cono- nia. Przegląd Geologiczny, 31 (6): 356-364. donta, Upper Devonian and Lower Carboniferous). Newslet­ Żelichowski, A. M., 1995. Western Pomerania. In: Zdanowski, A. ters on Stratigraphy, 1 (2): 102-120. & Żakowa, H. (eds), The Carboniferous System in Poland. Sevastopulo, G. & Hence, L. 1999. Report on the Working Group Prace Państwowego Instytutu Geologicznego, 148: 97- 100. to establish a boundary close to existing Tournaisian-Visean Żelichowski, A. M. & Łoszewska, Z., 1987. Stratigraphy and litho- boundary within the Lower Carboniferous. XlVth Interna­ logical characteristic. (In Polish, English summary). In: Ra­ tional Congress Carboniferous-Permian, Programme with czyńska, A. (ed.), Geological structure of the Pomeranian Abstracts: 130. Swell and its basement. Prace Instytutu Geologicznego, 119: Sevastopulo, G. & Nudds J. R., 1987. Courceyan (Early Dinan­ 27-46. tian) biostratigraphy of Britain and Ireland: coral and cono- dont zones compared. Courier Forschungsinstitut Sencken­ berg, 98: 39-46. Sleeman, A. G., Reilly, T. A. & Higgs, K. T., 1978. Preliminary Streszczenie stratigraphy and palynology of five sections through the Old Head Sandstone and Kinsale Formations (Upper Devonian to Lower Carboniferous), on the west side of Cork Harbour. STRATYGRAFIA DOLNEGO KARBONU Geological Survey Ireland Bulletin, 2: 167-186. (MISSISIPPIANU) POMORZA ZACHODNIEGO: Stempien-Salek, M., 1997. Miospore stratigraphy of Upper Devo­ PORÓWNANIE ZON KONODONTOWYCH, MIO- nian and lowermost Carboniferous of western Pomerania. (In SPOROWYCH I MAŁŻORACZKOWYCH Polish only). Unpublished Ph. D. Thesis, Institute o f Geologi­ cal Sciences, Polish Academy o f Sciences, Warszawa, 109 pp. Hanna Matyja, Elżbieta Turnau & Barbara Żbikowska Tchigova, W. A., 1977. Stratigraphy and correlation of Devonian and Carboniferous hydrocarbon-bearing deposits of the Euro­ Przedstawiona w pracy biostratygrafia utworów dolnego kar- pean part of the USSR and foreign countries. Nedra, Mosfo’a, bonu strefy Koszalin-Wierzchowo Pomorza Zachodniego (Fig. 1) 262 pp. (In Russian only). oparta jest na zintegrowanych badaniach konodontów, miospor i Turnau, E., 1975. Microflora of the Famennian and Tournaisian malżoraczków. Konodonty i małżoraczki pozyskano jedynie z ut­ deposits from boreholes of Northern Poland. Acta Geologica worów turneju. Zbadane materiały pochodziły z 25 otworów Polonica, 25: 505-528. wiertniczych. Posłużono się podziałem litostratygraficznym Lipca Turnau, E., 1978. Spore zonation of uppermost Devonian and (Lipiec & Matyja, 1998) przedstawionym schematycznie na Fig. 2. Lower Carboniferous of Western Pomerania. Mededelingen Dla przeprowadzonych wydzieleń biostratygraficznych wyko­ Rijks Geologische Dienst, 30-1: 1-34. rzystano stratygraficzne schematy zonalne: ( 1 ) “standardowy” schemat konodontowy oparty na linii ewolucyjnej rodzaju Si- LOWER CARBONIFEROUS STRATIGRAPHY 217

phonodella i “po-siphonodellowy” schemat Lane et al. (1980), (2) przedstawiono na Fig. 17. lokalny schemat miosporowy zaproponowany przez Turnau Przeprowadzone badania pozwoliły na określenie wieku for­ (1978, 1979) i zmieniony/uzupełniony przez Avkhimovitch & macji karbońskich i ich granic (Fig. 18, 19) oraz ustalenie poło­ Turnau (1994) i Matyję & Stempień-Sałek (1994), (3) wprowa­ żenia granic chronostratygraficznych - granicy dewon/karbon i dzony w niniejszej pracy podział oparty na małżoraczkach bento- tumej/wizen. W terminologii zon konodontowych, karbońska nicznych. Wyróżniono także jedną zonę standardowego podziału część formacji iłowców wapnistych z Sąpólna zawiera się w prze­ opartego na entomozoidach. dziale sandbergi - dolna crenulata, tylko na południowym wscho­ Nie we wszystkich zespołach konodontów napotkano gatunki dzie (ogniwo margli z Trzebiechowa) utwory te sięgają aż do zony przewodnie, toteż w licznych przypadkach można było określić je­ typicus. Granica formacji iłowców wapnistych z Sąpólna z nad- dynie przedziały obejmujące dwie lub trzy zony (por. Fig. 3). Ty­ ległą formacją piaskowców arkozowych z Gózdu jest diachro- powe zespoły gatunków konodontów zilustrowano na Fig. 4-6. niczna; na zachód od linii Kurowo 1 - Wierzchowo 10 przebiega Zespoły gatunków miospor typowych dla zon lokalnego sche­ ona w zonie dolna crenulata, a na wschód od tej linii w zonie matu turneju i wizenu zilustrowano na Fig. 7, 10-11, a charakte­ isosticha-górna crenulata, lub w dolnej części poziomu typicus. rystykę zmodyfikowanego schematu dla turneju i wizenu poka­ Formacja iłowców wapnistych z Grzybowa i formacja wapieni zano na Fig. 8. Schemat ten można na podstawie pierwszych po­ oolitowych z Kurowa są w przybliżeniu równowiekowe mieszcząc jawień gatunków zonalnych korelować ze schematem miospo- się w zakresie zony typicus. Formacja piaskowców kwarcowych z rowym dla rejonów typowych pięter dolnego karbonu Wysp Bry­ Drzewian obejmuje najwyższy turnej po górny wizen (brygant). tyjskich (Fig. 9). Potwierdzono obecność luki stratygraficznej obejmującej po­ Wprowadzony w niniejszej pracy podział biostratygraficzny granicze systemów dewońskiego i karbońskiego. Brakujące zony dla turneju, oparty na małżoraczkach bentonicznych, obejmuje konodontowe to środkowa praesulcata, sulcata, duplicata, (lub, na trzy zespoły, z których najniższy podzielono na dwa podzespoły. podstawie goniatytów, za Korejwo (1979, 1993), tylko dolna du­ Charakterystykę schematu przedstawiono na Fig. 12, a gatunki ty­ plicata) i ich odpowiedniki w zonacji miosporowej. Luka ta nie powe dla poszczególnych zespołów i podzespołów zilustrowano manifestuje się żadnymi widocznymi oznakami przerwy w sedy­ na Fig. 13-16. mentacji lub niezgodnością. Ustalenie położenia granicy tur- Konodonty, miospory i małżoraczki pozyskano niejednokrot­ nej/wizen jest trudne z powodu braku diagnostycznej fauny. nie z tych samych profili, z wzajemnie przekładających się pozio­ Postawiono ją w przybliżeniu w poziomie pierwszego pojawienia mów opróbowania. Pełną dokumentację dotyczącą głębokości po­ się gatunku miospor Lycospora pusilla Somers. brania prób i występowania gatunków zamieszczono w dodatku (Appendix 2). Dzięki zintegrowaniu badań można było ustalić wzajemne relacje pomiędzy poszczególnymi podziałami, co