Annales Societatis Geologorum Poloniae (2002), vol. 72: 163-190.

MIOSPORE TAXONOMY AND STRATIGRAPHY OF UPPER DEVONIAN AND LOWERMOST CARBONIFEROUS IN WESTERN POMERANIA (NW POLAND)

Marzena STEMPIEN-SALEK

Polish Academy o f Sciences, Institute o f Geological Sciences, ul. Twarda 51/55, 00-818 Warszawa, Poland, e-mail: [email protected]

Stempien-Salek, M., 2002. Miospore taxonomy and stratigraphy of Upper Devonian and lowermost Carboniferous in western Pomerania (NW Poland). Annales Societatis Geologorum Poloniae, 72: 163-190.

Abstract: Five local miospore zones, six subzones and two assemblages are distinguished for the Frasnian to lower Toumaisian deposits in the Kolobrzeg region (western Pomerania): assemblage I, Membrabaculisporis radiatus-Tholisporites densus (RD), Membrabaculisporis radiatus-Cymbosporites boafeticus (RB), Lagenoispo- rites immensus-Diducites poljessicus (IP) Zone, assemblage II, Tumulispora rarituberculata (Ra) and Convolu- tispora major (Ma) Zone. The first three biozones and the two assemblages are new in this region. The local miospores zones distinguished in western Pomerania are correlated with the European standard miospore and conodont zonations. Two new miospore species and one new variety are described, two species is emended.

Key words: Frasnian, Famennian, lowermost Carboniferous, NW Poland, miospores, stratigraphy.

Manuscript recdeived 6 November 2001, accepted 13 June 2002

INTRODUCTION PREVIOUS PALYNOLOGICAL STUDIES OF UPPER DEVONIAN AND LOWER The main purpose of this study was to determine, using CARBONIFEROUS OF WESTERN palynological methods, the stratigraphical position of the POMERANIA Człuchów, Kłanino, Sąpolno Calcareous Shale, and Gozd Arkose formations of western Pomerania. The zones of the The earliest results of palynological studies concerning miospore zonal scheme for Famennian and Lower Carbon­ the Devonian-Carboniferous succession of western Pome­ iferous of that area established by Tumau (1978, 1979) are rania were published in the seventies of the twenty century. rather wide. The present studies have allowed to establish a The evolution of palynostratigraphical divisions of the Up­ provisional zonation for the Frasnian and lower part of the per Devonian-lowermost Carboniferous is shown in figure Famennian, and to subdivide some of the previously erected 2. The first account of the Carboniferous miospore assem­ zones. The studied borehole sections are dated on cono- blages from the study area was that by Krawczyńska-Gro- donts, which permits to define the boundaries of the mio­ cholska (1975), who included the deposits from the Sarbi­ spore zones in terms of the “standard” conodont zonation. nowo 1 borehole in the Namurian and Westphalian. Subse­ The preliminary results of my studies, concerning the upper quently, the strata included by this author in the Namurian Famennian and lowermost Carboniferous have been pub­ were assigned by Tumau (1979) to the Visean. Tumau lished in the paper by Matyja & Stempień-Sałek (1994), and (1975, 1978, 1979) studied miospore assemblages from those on the Frasnian and lowermost Famennian are sum­ more than thirty borehole sections and proposed a miospore marised in Stempień-Sałek (2000). zonal scheme including eleven zones, five for the Famen­ The palynological material on which this work is based nian, two for the Toumaisian, three for the VisJan and one is derived from the Strzeżewo 1, Gorzysław 8, Gorzysław 9, for the Westphalian. The youngest Toumaisian zone of this Gorzysław 11, Gorzysław 14 and Karcino 2 boreholes scheme, i.e. the Prolycospora claytonii (Cl) Zone was di­ drilled in the area near Kołobrzeg, and from Chmielno 1 and vided into three subzones. Avkhimovitch & Tumau (1994) Rzeczenica 1 boreholes from the area to south-east from revised that division, distinguishing only two subzones, and Kołobrzeg (Fig. 1). presented a new proposal of palynological correlation of the 164 M. STEMPIEŃ-SAŁEK

MATERIAL AND METHODS

The palynological samples were black, dark grey and grey shales, claystones and mudstones some of which were intercalations within carbonates. Standard laboratory meth­ ods were employed. Samples were crushed and immersed in hydrochloric acid to remove carbonates. Subsequently, the mineral matter was dissolved in hydrofluoric acid, and the organic residues were oxidated using fuming nitric acid. This was followed by heavy liquid flotation using solution of cadmium-jodate + potassium-jodate of specific weight 2.2 g/cm3. Slides were prepared using elvacite or glycerine gelly. The number of the samples processed was 125, and Fig. 1 Position of western Pomerania (A) and location of stud­ 83 of these contained determinable spores. Two hundred ied boreholes (B): S.l - Strzeżewo 1, G.8 - Gorzyslaw 8, G.9 - Gorzyslaw 9, G.l 1 -Gorzyslaw 11, G. 14-Gorzyslaw 14, Ka. 2 - sixty five slides were prepared. Karcino 2, Ch.l - Chojnice 1, Ko.l - Koczała 1, Rz.l - Rzecze­ nica 1 GEOLOGICAL BACKGROUND lower zonal boundary (Fig. 2). The present author (in Ma­ tyja & Stempień-Sałek, 1994) upgraded the scheme pro­ GEOLOGICAL SITUATION posed by Tumau (1978, 1979) introducing two subzones of the Tumulispora rarituberculata (Ra) Zone, and four of the Western Pomerania is dissected by the Teisseyre tec­ Convolutispora major (Ma) Zone (Fig. 2). This subdivision tonic zone called within its Polish part the Teisseyre-Tom- allows a more precise correlation of the local scheme with quist zone (Dadlez, 1990, 1993; see also Fig. 1). The zone that for northwestern Europe (Higgs et al., 1988). forms also the south-eastern limit of the East European Plat­ Other contributions to the miospore stratigraphy of the form. The Teisseyre-Tomquist zone is characterized by upper Famennian and Carboniferous of the study area are high mobility expressed by high rate of sedimentation, erro- those by Górecka & Parka (1980), and Kmiecik (1991, sion and tectonics. In the younger Palaeozoic, these pro­ 1995). The former authors included in the Westphalian the cesses increased gradually and rhythmically from the Late deposits from the Koszalin IG 1 borehole assigned by Tur- Devonian up to the Late Carboniferous (Dadlez, 1978). nau (1979) to the Visean. The latter author studied some up­ In western Pomerania, the Devonian-Carboniferous per Famennian to Stephanian deposits, and distinguished 8 succession rests unconformably on the Ordovician and Silu­ miospore zones of the northwestern European scheme. This rian graptolite shales strongly folded due to the Caledonian results are not shown in figure 2 as they were published in a orogeny. In the region of Kołobrzeg the Devonian rests on brief conference abstract, without photographic documenta­ steeply deeping Caradocian shales (Dadlez, 1993). The tion and species range charts. Caledonian deformation in that area may be due to the In sum the miospore stratigraphic scheme in western oblique collision of small crustal blocks, related to the Bal- Pomerania for the Devonian and Carboniferous, includes tica or Gondwana, with the East European craton (Dadlez, more than ten zones distinguished for the Famennian to 1993). None of the boreholes studied reaches this older Pa­ Stephanian (Tumau, 1978, 1979; Kmiecik, 1986). Some of laeozoic substratum. the zones, however, are very wide, especially those for the Sedimentation of the Devonian-Carboniferous cycle Famennian. The Frasnian in Pomerania has not been, till started probably in Early Devonian (Dadlez, 1978, 1990, now, studied by palynologists. 1993), and not later than the Eifelian (Lobanowski, 1968; The problem of the presence and extent of the stra­ Pajchlowa, 1968; Tumau, 1995), covering different units of tigraphic gap at the Devonian-Carboniferous boundary has the Silurian (Teller, 1974), and Ordovician (Bednarczyk, been the concern of biostratigraphers for a long time. Vary­ 1974). The Devonian deposits are developed in various fa­ ing opinions on this matter are illustrated in figure 2. The des. Generally, those older than the Upper Devonian are presence of a gap was first suggested by Tumau (1978), and mostly siliciclastic rocks (Dadlez, 1978). In Late Devonian, it was discussed, in the terms of miospore zonations, in or at the close of the Givetian, the discussed area was in­ Clayton & Tumau (1990) and Avkhimovitch et al. (1993a). vaded by marine transgression leaving clastic and carbonate The extent of the gap was first defined in terms of the cono- sediments. The next widening of the marine basin took dont zonation in Matyja & Tumau (1989), it was also dis­ place in the early Famennian, and regressive tendencies cussed in Matyja & Stempień-Sałek (1994) and Matyja et reigned during the late Famennian (Dadlez, 1993). The Car­ al. (2000). In Matyja & Stempień-Sałek paper, the present boniferous deposits, resting concordantly on the Devonian author suggested that the upper extent of the gap coincides vary both vertically and laterally in facies development. with the lower boundary of the Krauselisporites hibernicus- They are represented by three main types of sediments. Umbonatisporites distinctus (HD) Zone of the division of Starting from the oldest, they are clayey shales, arkosic Higgs et al. (1988). Previously, it was considered that the sandstones and various limestones (marly, oolitic, dolomitic gap ends slightly below (Clayton & Tumau, 1990), or and other). Vertical displacements (the diastrophic move­ slightly above (Avkhimovitch et al., 1993a) this level. ments toward the close of the Early Carboniferous) caused MIOSPORE TAXONOMY AND STRATIGRAPHY 165

Streel Avkhi- Avkhi- Stempień- et al. Clayton movitch, movitch Sałek Tumau 1987 & Tumau & 1979 Higgs Tumau & Tumau Present et al. 1990 Clayton 1992 paper 1988 1993a

Cl CM Cl Cl PC C li Ma BP Ma HI) Ma Ma Ma VI

LN LE LL Ra Ra LV Lu, Ve VCo GF GH “V” stratigraphic gap 'TV’ no data BM BJ

Fig. 2. Evolution of palynostratigraphical divisions of the Upper Devonian-lowermost Carboniferous in western Pomerania

the regional absence of the Namurian and Westphalian and clastic-carbonate-evaporitic rocks, and the Mesozoic suc­ the variable truncation of the Lower Carboniferous sedi­ cessions. ments. The Upper Carboniferous grey limnic sediments of coal-bearing association pass upwards into clastic sedi­ LITHOSTRATIGRAPHY ments of red-bed association. The thickness of the Lower Carboniferous is at least 1500 m (Dadlez, 1993) or about The first, informal lithostratigraphic division of the De­ 1300 m (Żelichowski, 1983, 1987). vonian-Carboniferous succession of western Pomerania Starting from the Late Devonian, there was a gradual was proposed by Dadlez (1978) who distinguished several and rhythmical intensification of erosional processes and lithostratigraphic units called complexes and sub-comple- tectonic movements. The main phases of these processes xes. The division by Dadlez was subsequently modified and took place (1) at the beginning of the Carboniferous, and (2) complemented by Milaczewski (1979, 1980, 1986, 1987), at the end of the Early and the beginning of the Late Carbon­ Żelichowski (1983, 1987), and Matyja (1993) who distin­ iferous. The main structural reorganisation and strongest guished in the Upper Devonian sequence five (informal) erosion of the Devonian-Carboniferous succession took formations and four members. Most of these formations place at the Carboniferous-Permian transition, after the correspond to the “complexes” of Dadlez (1978), and have block movements in the area. Due to these movements, the the same names, but the members are new units. Recently, discussed region is divided into tectonic blocks of various Lipiec (Lipiec & Matyja, 1998) introduced a lithostrati­ sizes, one of which is the Kołobrzeg block (Dadlez, 1990, graphic scheme for the Lower Carboniferous. It includes 1993). The erosion removed, first of all, the Upper Carbon­ seven formations and two members. iferous deposits, subsequently, to a lesser extent, the Lower The lithostratigraphic division adopted in this paper Carboniferous ones. The Devonian deposits are still less af­ (Figs 3 and 4) is that by Matyja (1993, 1998) and Lipiec & fected, but erosion has reached in places the Middle Devo­ Matyja (1998). nian (Dadlez, 1978). The Devonian-Carboniferous succes­ In Człuchów Formation (boreholes: Strzeżewo 1, Go- sion of complicated structure is overlain discordantly by rzysław 8, Gorzyslaw 11 and Gorzyslaw 14) Matyja (1993) red, clastic deposits of the Lower Permian, Zechstein distinguished five members, namely the Unisław, Strze- 166 M. STEMPIEŃ-SAŁEK

żewo, Gorzysław, Bielica, and Gościno members. The Uni­ boundary runs within a bed of black claystone and is not sław and Gościno members are not represented in the bore­ marked by any characteristic sedimentary features (Matyja holes studied (Fig. 3). The thicknes of the Człuchów Forma­ 1993, 1998; Matyja & Stempień-Sałek, 1994). tion in this region varies from 400 m trough 700 m. The Lower Carboniferous Gozd Arkose Formation, the The Strzeżewo Member, lowest of the investigated deposits of which have been pierced in the Chmielno 1 units, has been pierced in the Strzeżewo 1, and Gorzysław 8, borehole, includes mainly clastic rocks. As a rule, the base 11,14 boreholes. The unit includes monotonous, thin bed­ of the formation is placed at the base of the first bed of arko- ded, almost black bituminous shales and marly shales and sic sandstone. Various sandstones of grey colour, arkosic subordinate micritic, more or less marly, limestones. The sandstones including pyroclastic material, dark grey mud­ shales include pyrite aggregates and rare fossils characteris­ stones and black claystones are common. Thin beds of tic mainly of pelagic environment, such as entomozoacean shale, claystone and oolitic limestone occur subordinately. ostracods and tentaculitids. Plant detritus and land plant They contain rare foraminifers, crinoids, brachiopods, spores are present. conodonts, miospores and acritarchs. The present paper The Gorzysław Member (boreholes Gorzysław 8 and concerns only the basal part of the formation. 14, Karcino 2) includes mainly grey marls and nodular lime­ stones. Contribution of shales in this unit is distinctly FAUNAL STRATIGRAPHY smaller than in the underlying member. The nodular lime­ stones often contain crinoid debris, articulate brachiopods, In western Pomerania, the rocks of the Devonian-Car­ agglutinated foraminifers, benthic and entomozoacean os­ boniferous succession contain diverse fossils that make dat­ tracods as well as cephalopods, tentaculitids and conodonts. ing of these sediments possible. Ammonoids are rare and In some sections, crinoid-bryozoan wackestone with rare accordingly the ammonoid stages have not been distin­ coral debris and chaetetid fragments are present. Thin shale guished. Biostratigraphy is based on conodonts, brachio­ partings are rich in miospores and acritarchs. pods, entomozoids, and miospores. In the following text, The Bielica Member (borehole Gorzysław 8) includes the author gives the borehole names only if they are con­ light micritic limestones with accumulations of bryozoan cerned in the present paper (Fig. 1). Unless otherwise stated, debris, brachiopods, ostracods, and crinoids, as well as mas­ all conodont data given below are after Matyja (1993) and sive micritic limestones with dispersed crinoid detritus, Matyja et al. (2000). bryozoans, coral colonies, less commonly with stromato- The Człuchów Formation is dated on conodonts (Figs poroids, algae, conodonts and miospores. 3,4), entomozoacean ostracods and brachiopods. The oldest In the region of Kołobrzeg, the Kłanino Formation part of the Strzeżewo Member is dated as the conodont (boreholes Gorzysław 8 and 9) is typified by predominance punctata Zone, and the top part as the Middle triangularis of carbonates, mainly laminated, sandy grainstones with al­ Subzone. In the region of Kołobrzeg, conodonts indicative gae, foraminifers, gastropods, ostracods, crinoidal detritus, of the Upper hassi, jameiae, or Lower rhenana zones/sub­ conodonts and miospores, and dasycladacean grainstones zones have been found within this member (Figs 3, 4; bore­ with intraclasts and almost devoid of organic remains. The holes Strzeżewo 1 and Gorzysław 8,11). The overlying Go­ thickness of the Kłanino Formation in the region of Koło­ rzysław Member is dated in the Kołobrzeg region as the Up­ brzeg is 150 m. per triangularis and crepida zones (Figs 3, 4; boreholes The Sąpolno Calcareous Shale Formation (boreholes: Gorzysław 8, 14 and Karcino 2). In other regions of Pom­ Gorzysław 8 and 9, Karcino 2, Rzeczenica 1 and Chmielno erania, the lower part of the Gorzysław Member is dated as 1) includes the uppermost Devonian and lowermost Car­ Middle triangularis Subzone, and its top part as the Upper boniferous deposits. Grey, marly limestones and marls pre­ rhom boidea Subzone. In the higher part of the Bielica vail within the lower, Devonian part of the formation. They Member, in the region of Kołobrzeg, there occur conodonts contain abundant fossils of which the most important are fo­ of the marginifera Zone (Figs 3, 4; borehole Gorzysław 8). raminifers, ostracods, stromatoporoids, crinoids, brachio­ In other parts of Pomerania, the Lower and the Upper m ar­ pods, conodonts and miospores (Matyja & Stempień-Sałek, ginifera subzones have been distinguished within this mem­ 1994), also acritarchs (Stempień-Sałek, 1996). Such depos­ ber. Entomozoacean ostracods have been recorded from the its are characteristic for shallow environment of marly- Człuchów Formation by Żbikowska (1992). In the Strze­ carbonate ramp developed below the wave base level but żewo Member, this author distinguished the cicatricosa within the photic zone (Matyja, 1998). The younger, Car­ Zone (the boreholes Gorzysław 8 and 11), the sarteńaeri boniferous part of the formation includes mainly dark grey Zone (the borehole Gorzysław 8) and the serratostriata- and black, finely laminated claystones, calcareous clay- nehdensis Zone (the boreholes Gorzysław 8, 11 and Ko­ stones, marls and limestones (Lipiec & Matyja, 1998; Ma­ czała 1). In the Gorzysław Member, the zones sartenaeri tyja et a i, 2000) containing abundant spores and infrequent and sigm oidale have been distinguished. Brachiopods from acritarchs. Fauna is rare. The thickness of the Carboniferous the Człuchów Formation have also been determined. Matyja part of the Sąpolno Calcareous Shale Formation may exceed (1972) recorded several Devonian and Famennian species 300 m. from the Bielica Member. The Devonian-Carboniferous system boundary lies The Kłanino Formation is, in the region of Kołobrzeg, within this formation. This is a hidden stratigraphic gap. Its dated by means of conodonts as upper Famennian expansa extent defined in the terms of the conodont zonation is from Zone (Figs 3, 4). No other fauna has been recorded here. In middle praesulcata to part of sandbergi zones (Fig. 4). The other regions of Pomerania, the dating is more precise. The MIOSPORE TAXONOMY AND STRATIGRAPHY 167

8 8 - anhy­ Ma - 15- 23 23 - zone, conglomerate, 14- - 2 - fine-grained quartz sandstone, Membrabaculisporis radiatus - Cymbo- marly shale, 13- Tumulispora Tumulispora rarituberculata - RB - 19 arcosic sandstone, marl, 1 - 1 Ra - 12- Zone, 22 22 - Assemblage II, 21 21 - Zone, nodular algal-foraminiferal-crinoid, packstone/grainstone, - 7 massive micritic limestone, 6 - 6 marly brachiopod-crinoid wackestone, 11 - 11 Membrabaculisporis radiatus - Tholisporites densits -RD - 18 marly algal wackestone to packstone, Lagenoisporites Lagenoisporites immensus - Diducites poljessicus 10- IP - 20 20 - Zone, marly limestone, dolomitic sandstone, - 9 5 - algal-foraminiferal-peloidal grainstone, -palynological sample, - / 7 Assemblage 1 , 4 - 4 16 mudstone, Fig. Fig. 3. Lithology, lithostratigraphy and stratigraphic biozonation (conodont and palynological zones) of studied boreholes. 3 3 - marly dolomite, drite drite nodules, sporites sporites boafeticus 168 M. STEMPIEŃ-SAŁEK

SPORE DIVISION CONODONT DIVISION FORMATIONS Members OTHER BOREHOLES BOREHOLESin this paper Pomerania £ GOZD Cl 1 typicus < ARKOSE 4 isosticha - up. crenulata Fm 3 X < Ma 1. crenulata 2 X 1 1 o sandbergi XX H SĄPOLNO CALCAREOUS duplicata SHALE sulcata Fm praesulcata Ra X X z expansa < KŁANINO postera z Fm m w • trachytera § BIELICA M marginifera X < Ass. II w -—S' - Rhomboidea X GORZYSŁAW M. IP Crepida XX Triangularis XX o RB Linguiformis CZŁUCHÓW ■§ rhenana X Z Fm s X < o jamiae !Z)z % hassi b puncatata X u. t-a Ass. I 00 transitans . iii r falsiovalis

stratigraphic gap no data

Fig. 4. Generalized lithostratigraphy and biostratygraphy of Upper Devonian-lowermost Carboniferous in Western Pomerania

lower part of the formation corresponds to the Lower ex­ Devonian part of the formation as the hemispherica-dicho- panse* Zone, though the basal part may belong to the mar- toma Zone (Żbikowska, 1992). Among trilobites, single ginifera Zone (Matyja, 1993). The top part of the formation specimens of Moschoglossis sp. indicate the lower and mid­ is not younger than the Middle expansa Zone. dle Toumaisian (Korejwo, 1976). The stratigraphic position of the Sąpolno Calcareous The present paper concerns only the basal part of the Shale Formation that belongs to the Famennian and Hasta- Gozd Arkose Formation. In this part no conodont faunas rian has been established on goniatites, brachiopods, cono- have been found. Brachiopods fauna is described by Ko­ donts, ostracods and trilobites. Goniatites are rare. Only rejwo (1993). Entomozoids indicate latior Entomozoid Toumaisian Pseudoarietites dorsoplanus dor sop] anus Zone (Żbikowska, 1992). Schmidt, P. ex gr. dorsoplanus dorsoplanus Schmidt, and Gattenpleura sp. have been recorded in Wierzchowo 10 borehole, near the Chmielno 1 borehole (Korejwo, 1979, P AL YNOSTRATIGRAPH Y 1993). Brachiopods from the Famennian and Carboniferous part of the Sąpolno Calcareous Shale Formation are de­ The miospore assemblages studied contain numerous scribed by Matyja (1976) and Korejwo (1993). In the region stratigraphically important species known from the Devo­ of Kołobrzeg, the basal part of the Sąpolno Formation is nian and the Lower Carboniferous of western and eastern dated on conodonts as expansa-praesulcata zones, and the Europe. However, it would have been difficult to adopt one top part as sandbergi or Lower crenulata Zone (Matyja et of the zonal schemes for western (Streel el al., 1987; Higgs al., 2000). In other regions of Pomerania, the dating is more et al., 1988) or eastern Europe (Avkchimovitch, 1993; precise - the lower part of the formation corresponds to the Avkhimovitch et al., 1993a) because of quantitative and Upper expansa or Lower praesulcata subzones, and the up­ qualitatite differences between the assemblages studied and per to the Lower crenulata Subzone. Entomozoids date the those from the regions mentioned. MIOSPORE TAXONOMY AND STRATIGRAPHY 169

SELECTED MIOSPORE SPECIES 1

' ' , SUBZONES sp. / /

sp. 3 •Li 2 Sn3 a- •2 LOCAL LOCAL MIOSPORE <3- o ZONES ZONES -c> Ci, Umbonatisporites Umbonatisporites abstrusus T. rarituberculataT. Verrucosisporites nitidus Crassispora trychera Umbonatisporites distinctus Convolutispora Convolutispora subtilis Corbulispora Corbulispora vimineus Grandispora villosa Grandispora lupata Geminospora condensa Knoxisporites literatus Tumulispora malevkensis Convolutispora major Cymbosporites acutus Cymbosporites acutus \ Prolycospora claytonii Cristatisporites Cristatisporites deliquescens Corystisporites pomeranius Tolisporites densus Cymbosporites vetlasjanicus Samarisporites Samarisporites triangulatus Lagenoisporites immensus Diducites poljessicus Diducites versabilis Diducites commutatus Spelaeotriletes resolutus Retispora macroreticulata Retispora lepidophyta Lophozonotriletes excisus Murospora dubitata Pustulatisporites gibberosus Raistrickia corynoges Spelaeotriletes obtusus Schopfites delicatus Spelaeotriletes balteatus Raistrickia condylosa Hystricosporites Membrabaculisporis radiatus Auroraspora Auroraspora macra Archaeoperisaccus Archaeoperisaccus oncinnus \ Ancyrospora Auroraspora aspella \ Aneurospora Aneurospora greggsii u k; 1 1 i i ■ i i i C l, XX X X X X XX X X X X XX X XX X X XX M a4 XX X x XX X XX XXX X X X XX X X X M a3 XXX X XX X XX XX X X X X X XX X M a2 X XXXX X X X X X XX XX X X X X X XX M a, X X XXXXX XXX X X X XX XX X XX X Ra2 XX X X X XXXX XXX X X Ra] XX X XXXXXX XXX Ass II XX X XX XXXX IP XX XX X X X RB X X XX X X XX RD X X X XXXXX X Ass I XXX XX

Fig. 5. Range chart of selected most stratigraphically useful miospore specics referred to in the present paper

In the deposits studied, the author distinguished three barren intervals of significant thickness between some of miospore zones, two assemblages and six subzones (Fig. 2) the biostratigraphic units. In the following text, the units are of the previously established zones in order to extend the described in ascending order. previous division and to make it more precise. The five old­ In this section, names of miospore species are given est zones/assemblages for the Frasnian and lower Famen- without the creator’s names. The list of complete names is nian, i.e. the assemblage I, Membrabaculisporis radiatus- given at the appendix 1. Quantitative and qualitative data Tholisporites densus (RD), Membrabaculisporis radiatus- from the studied boreholes are given at the appendix 2. Cymbosporites boafeticus (RB), and Lagenoisporites im- mensus-Diducites poljessicus (IP) zones, and assemblage II, Assemblage I have been defined for the first time. The two younger zones The miospore associations basal part of the deposits - Tumulispora rarituberculata (Ra) and Convolutispora studied are poor in taxa and they lack index species. For this major (Ma) belong to the zonation scheme proposed by Tur- reason they are included in an assemblage, not a zone. The nau (1978). The present author introduced six subzones of assemblage I was distinguished in the Gorzyslaw 11 bore­ these zones (Stempień-Sałek, 1994). hole (Figs 1, 3). The lower boundary of the assemblage is The core recovery in the boreholes studied was incom­ not known. The following species are characteristic for this plete, and the lithology of the rocks was often unfavourable unit: Ancyrospora fidus, A.jurcul, A. langi, Apiculiretusis- for preservation of palynological material. For these rea­ pora nitida, Cristatisporites deliquescens, Geminospora sons, the palynological data obtained are in many cases nalevkinii, G. notata, G. rugosa, Hymenozonotriletes argu- fragmentary. Nevertheless, the distinguished zones are dis­ tus, Hystricosporites furcatus, H. multifurcatus, H. porrec- tinct, and their age inferred from palynological data is, in tus, Perotrilites magnus, P. minor, Samarisporites acanthy- most cases, confirmed by direct conodont data (after Ma­ rugosus, S. triangulatus and Verrucosisporites cf. evlanenis tyja, 1993), also by some ostracod data (after Żbikowska, (Fig. 5). These are mostly species of a long stratigraphic 1992). range, and there are no stratigraphically important taxa known from the Ardenne-Rhine regions, such as Verruco­ sisporites bulliferus, Cirratriradites jekhovskii or Lophozo- DESCRIPTION OF ZONES notriletes media. On the other hand, the author recorded the The zones and assemblages for the Frasnian and lower presence of Cristatisporites deliquescens, which appears at Famennian of western Pomerania introduced here are of the base of the eastern European Geminospora semilucensa- assemblage-zone character. They are not formally defined Perotrilites donensis (SD) Zone (Avkhimovitch et al., as the author feels that the number of samples and the diver­ 1993b). This indicates that the assemblage I is not older, and sity of some assemblages are not sufficient, and there are probably corresponds, to this zone, or to a part of it. The di­ 170 M. STEMPIEŃ-SAŁEK

rect conodont data inddicate that the SD Zone corresponds sisporites grumosus (OG) Zone (Obukhovskaya, 1986) to the punctata-hassi zones. Thus, the base of the assem­ which corresponds to the conodont rhenana Zone. The stra- blage I is not older than the punctata Zone (Fig. 4). In the re­ tigraphic distribution of Cristatisporites deliquescens is gion of Kołobrzeg, the basal part of the Człuchów Forma­ wide. On the Russian Platform, the species disappears at the tion is not dated on conodonts. In other regions of Pomera­ top of the Cristatisporites deliquescens-Verrucosisporites nia, this part (included in the Unisław Member) corresponds evlanensis (DE) Zone that ranges to the uppermost gigas to the falsiovalis-punctata zones and the basal part of the Zone (Avkhimovitch et al. 1993b). In Canada, the range of overlying Strzeżewo Member is thought to belong to the C. deliquescens extends into the lowermost part of the punctata Zone (Matyja, 1998). torquata-gracilis Zone, i.e. also to the conodont Lower tri­ angularis Zone (Richardson & McGregor, 1986). It may be Membrabaculisporis radiatus-Tholisporites dens us (RD) thus conjectured that the lower boundary of the RB zone is assemblage Zone not older than the conodont rhenana Zone and the upper one The zone has been distinguished in the Strzeżewo 1 and is not younger than the triangularis Zone. Gorzysław 11 boreholes (Figs 1,3). The lower zonal bound­ This is consistent with the direct conodont data (see Fig. ary is marked by the first appearance of Membrabaculispo­ 3) which indicate that the RB zone corresponds to the Upper ris radiatus. Other species appearing close to and above this rhenana and triangularis zones, and to Entomozoacean boundary are Archaeoperisaccus concinnus, Convolutis- cicatricosa-sartenaeri zones (Matyja, 1993). pora subtilis, Tholisporites densus, Laevigatosporites The RB miospore assemblages do not contain species ovalis and Aneurospora greggsii. Species A. concinnus, C. which would allow palynological correlation with the Ar- subtilis, T. densus, S. triangulatus and S. acanthyrugosus denne-Rhine regions, but on conodont data one may sup­ disappear at the upper zonal boundary. The characteristic pose that the zone is the equivalent of a higher part of the assemblage includes the species mentioned above, and Sa- zone “IV” and with zone “V” of the division by Streel et al. marisporites triangulatus, Cristatisporites deliquescens and (1987). Cymbosporites acanthaceus, also some forms of Ancyro- spora, Geminospora and Hystricosporites (Fig. 5). Lagenoisporites immensus-Diducites poljessicus (IP) In eastern Europe, M. radiatus first appears in the A r- Zone chaeoperisaccus ovalis-Verrucosisporites grumosus (OG) The zone has been distinguished in the Gorzyslaw 8, Zone, and, more precisely, in its middle subzone Cymbo­ and Karcino 2 boreholes (Figs 1, 3). The lower boundary of sporites vetlasjanicus (CVe). It may be concluded that the the IP zone is marked by the first appearance of Lagenois­ RD zone for Pomerania corresponds to a higher part of the porites immensus and Diducites poljessicus. Other species eastern European OG Zone. The miospore assemblages of appearing above and close to the boundary are Corbulis- the CVe Subzone occur in association with conodonts of the pora vimineus and Lophozonotriletes curvatus. The last oc­ Lower rhenana Zone. It may be thus inferred that the base currence of Laevigatosporites ovalis, Cymbosporites boafe­ of the Pomeranian RD zone is not older than the rhenana ticus and Corbulispora vimineus has been recorded from the Zone. This conclusion is in agreement with the results pub­ upper part of the zone. The characteristic assemblage in­ lished by Matyja (1993) as in the boreholes studied the RD cludes, beside the species listed above, Aneurospora greg- zonal assemblages are associated with conodont faunas in­ gsi and Hystricosporites spp (Fig. 5). dicative of Upper hassi or Lower rhenana zones (Fig. 3). On the Russian Platform Lagenoisporites immensus Considering the conodont data, one can suppose than the first appears in the Convolutispora zadonica (Za) Subzone RD zone may be the equivalent of a part of the “IV” zone of of the Cyrtospora cristifer-Diaphanospora zadonica (CZ) Streel et al. (1987) that corresponds to upper /?av.v/-lowcr Zone, and the acme of its occurrence is in the Lagenoispor­ triangularis conodont zones. ites immensus (Im) Zone. Diducites poljessicus appears also in the Im Zone. It seems plausible that the IP zone is the Membrabaculisporis radiatus-Cymbosporites boafeticus equivalent of the eastern European Za Subzone and the Im (RB) Zone Zone. These are approximately correlated with the conodont The zone has been distinguished in the Gorzysław 8, G. crepida and rhomboidea zones (Avkhimovitch et al., 11 and G. 14 boreholes (Figs. 1, 3). The lower boundary of 1993b). In western Pomerania, the miospore assemblages of the zone is marked by the first appearance of Cymbosporites the IP Zone occur below and in association with conodonts boafeticus and C. vetlasjanicus. Membrabaculisporites ra­ of the Middle and Middle-Upper crepida Subzones (Fig. 3). diatus and do not range above the upper boundary of the In the Ardenne Rhine regions, L. immensus is absent, zone and Cristatisporites deliquescens disappears in the and D. poljessicus appears in the “IV” zone, which is obvi­ lower part of the zone. The characteristic assemblage in­ ously earlier than in eastern Europe as the zone “IV” corre­ cludes the index species and Cristatisporites deliquescens, sponds to the jamiae Zone (Streel et al., 1987). The pre­ Laevigatosporites ovalis, Aneurospora greggsii, Apiculire- sented conodont data suggests that the IP zone is a part tusispora nitida, Diducites radiatus, Perotrilites magnus, equivalent of the Grandispora gracilis-Acanthotriletes hir- Retusotriletes planus, R. incohatus, R. pychovi and also tus (GH) Zone that is considered to correspond to Upper forms belonging to Ancyrospora, Geminospora and Hystri­ crepida - lowermost marginifera Subzones (Streel et al, cosporites (Fig. 5). 1987). In Belorussia, Cymbosporites boafeticus first appears in an upper part of the Archaeoperisaccus ovalis-Verruco- MIOSPORE TAXONOMY AND STRATIGRAPHY 171

Fig. 6. Correlation of the zonal schemes for Upper Devonian and lowermost Carboniferous of western Europe, eastern Europe and western Pomerania

Assemblage II denne-Rhine regions, Diducites versabilis appears earlier The miospore associations of the assemblage II were re­ than in eastern Europe i.e. it appears in the zone “V”. covered only from the Gorzyslaw 8 borehole (Figs 1, 3). The assemblages were reasonably rich in specimens and Diducites versabilis (Ve) and Grandispora lupata (Lu) taxa, but they have been recovered from few samples only Zones and thus establishing a zone would not be justified. The Tumau (1978) established Diducites versabilis (Ve) lower boundary of the assemblage is marked by the first ap­ Zone. The base of this zone was defined on the first appear­ pearance of Diducites versabilis, Grandispora villosa and ance of D. versabilis (synonym Rugospora versabilis) and Spelaeotriletes resolutus. They are accompanied by Aneu- Retispora lepidophyta. In the region of Kołobrzeg, D. rospora greggsii, Auroraspora macra, D. commutatus, D. versabilis has been found in associations lacking R. lepido­ poljessicus, Lagenoisporites immensus, Lophozonotriletes phyta. Thus, the assemblage II is considered older than the curvatus and Hystricosporites spp (Fig. 5). zone Ve of Tumau. The latter zone is succeeded by the In eastern Europe, Diducites versabilis first appears at lupata (Lu) Zone characterized by the presence of Grandis­ the base of the Discernisporites golubinicus (DG) Subzone pora lupata and R. lepidophyta, and by the absence of Tu- of the Diducites versabilis-Grandispora famenensis (VF) mulispora rarituberculata. Such associations have not been Zone. This subzone is correlated on indirect data with the encountered by the author. The reasons why, in the region of Uppermost marginifera to Middle expansa conodont zones Kołobrzeg, the zones Ve and Lu have not been distin­ (Avkhimovitch et al., 1993b). The miospore associations of guished may be the incomplete coring of the boreholes and the assemblage II were found 35 m below conodont fauna unfavourable lithology of the Kłanino Formation. indicative of the marginifera Zone, and thus it is not younger than this conodont zone and is equivalent of the Tumulispora rarituberculata Zone miospore VF Zone. Tumau (1978) has established the Tumulispora raritu­ Avkhimovitch et al. (1993b) supposed that VF Zone is berculata Zone. The present author distinguished this zone the equivalent of the Ardenne Rhine Rugospora versabilis- in the Gorzysław 9, Chmielno 1 and Rzeczenica 1 bore­ Grandispora cornuta (Co) Zone that is dated as trachytera- holes. The assemblages include: Knoxisporites literatus, expansa conodont zones (Streel et al., 1987). In the Ar- Raistrickia minor, Tumulispora rarituberculata, T. malevk- 172 M. STEMPIEN-SALEK

ensis, T. obscura, Umbonatisporites abstrusus and Verruco­ Rzeczenica 1 boreholes. The lower boundaiy of the zone is sisporites nitidus. The two last mentioned species first ap­ marked by the first appearance of Umbonatisporites distinc­ pear in the higher part of the zone. The assemblages include tus. Crassispora trychera and Schopfites delicatus appear also species which appear earlier, such as: Diducites com- close to this boundary. In the Rzeczenica 1 borehole, the mutatus, D. versabilis, Auroraspora macra, Grandispora miospore assemblages of the Маг subzone are accompanied lupata and Retispora lepidophyta (Fig. 5). by conodont faunas of the Lower crenulata Zone and in the The author subdivided the Ra Zone into two subzones Chmielno 1 boreholes - by unseparated sandbergi-isosticha named Rai and Ra2. The base of the Rai subzone is marked Upper crenulata zones (Matyja et al., 2000). by the first appearance of U. abstrusus and V nitidus. In the Ardenne-Rhine regions, the lower boundary of The Ra Zone was first correlated by Tumau (1978) with the Kraeuselisporites hibernicus-Umbonatisporites distinc­ part of the Vallcitisporites pussillites-Spelaeotriletes lepido- tus (HD) Zone is marked by the first appearance of Krause- phytus (PL) Zone established for the British Isles and subse­ lisporites hibernicus and Cymbosporites acutus. Umbospo- quently (Tumau, 1979) with the upper part of Vallatispor- rites distinctus appears some distance above the first ap­ ites pussillites-Spelaeotriletes lepidophytus (PL) and lower pearance level of Krauselisporites hibernicus (Higgs et al, part of Verrucosisporites nitidus-Vallatisporites vallatus 1992). In Pomerania, U. distinctus also appears above the (NV) zones. At present, the Ra zone is considered to be base of the Ma Zone, such as Cymbosporites acutus, Convo­ older than the R. lepidophyta-I. explanatus (LE) Zone, be­ lutispora major, Auroraspora asparella, Lophozonotriletes cause the Ra associations lack several species present in the excisus, Murospora dubitata, Pustulatisporites gibberosus, LE Zone (Clayton & Tumau, 1990; Avkhimovitch et al., Raistrickia corynoges and Spelaeotriletes obtusus. In the 1993a). The species not found in the Ra Zone are Indotrira- Ardenne-Rhine regions, the lower boundary of the HD zone dites explanatus, Vallatisporites vallatus, V. verrucosus, V. has no faunal control, but the first appearance of U. distinc­ pussilites and Rugospora flexuosa. tus is dated as the sandbergi conodont Zone (Higgs et al., It has been noted, that in Pomerania, Verrucosisporites 1992). Thus, it appears, that the Mai and Маг subzones are nitidus appears earlier than in other regions of Europe, in the equivalents of the western European HD Zone, and they level Lower or Middlepraesulcata Zone (Matyja & Tumau, may be correlated with the sandbergi-crenulata Zones. 1989). In Ireland, the first appearance of the species is be- The Middle Convolutispora major (Маз) Subzone has lived to be Upper praesulcata Zone (Higgs et al., 1988), and been distinguished in the Gorzyslaw 9 and Chmielno 1 in Sauerland - Middle praesulcata or Upper praesulcata boreholes. Its lower boundary is marked by the first appear­ (Streel et al., 1987). ance of Spelaeotriletes balteatus. The characteristic assem­ To sum up - the Ra Zone is of late Famennian age, it blage is the same as for the entire Ma Zone enriched with correspons to the conodont Upper expansa and Lower to Spelaeotriletes balteatus. In western Europe, S. balteatus Middle praesulcata zones. appears in the Spealeotriletes balteatus-Rugospora polyp­ tycha (BP) Zone (Higgs et al., 1988, 1992). It is suggested Convolutispora major (Ma) Zone that the lower boundaries of the Маз Subzone and the BP The Ma Zone established by Tumau (1978) has been Zone are time equivalents. The base of the BP Zone is distinguished by the author in deposits from the Gorzyslaw within the Lower crenulata conodont Zone (Higgs et al., 8 and 9, Chmielno 1 and Rzeczenica 1 boreholes. The mio- 1992). In the Gorzyslaw 9 borehole, the assemblages of the spore associations of the zone include several species which Маз subzone are accompanied by conodont faunas of sul­ have not been recorded from the preceding Ra Zone. These cata or Lower crenulata zones. are: Convolutispora major, Auroraspora asperella, Cymbo- The Upper Convolutispora major (Ma4) Subzone has sporites acutus, Lophozonotriletes excisus, Murospora du- been distinguished in the Chmielno 1 borehole. Its lower bitata, Pustulatisporites gibberosus, Rastrickia corynoges boundary is marked by the first appearance of Spelaeo­ and Spelaeotriletes obtusus. The characteristic assemblage triletes pretiosus. The characteristic assemblage includes 5. includes also some older species: Tumulispora malevkensis, pretiosus and the species characteristic of the entire Ma T. rarituberculata, T. obscura, Verrucosisporites nitidus Zone, except for S. obtusus. and Umbonatisporites abstrusus (Fig. 5). In western Europe, S. pretiosus marks the base of the The succession of some first appearances within the Ma Spelaeotriletes pretiosus-Raistrickia clavata (PC) Zone Zone has permitted to distinguish four interval subzones (Neves et al., 1973, Higgs et al., 1988). The lower boundary (Matyja & Stempien-Salek, 1994). They have been desig­ of the zone is dated as Lower crenulata conodont Zone. nated Mai, Ma2, Ma3, and Ma4 . This level is close below the base of the isostichci Lower The lowermost Convolutispora major (Mai) Subzone crenulata conodont Zone, at the base of Tn2b (Higgs et al, has been distinguished in deposits from Gorzyslaw 9, 1992). On the Russian Platform S. pretiosus first appears at Chmielno 1 and Rzeczenica 1 (Figs 1,3, 5). The characteris­ the base of the Colatisporites multisetus-Spelaeotriletes tic of the subzone is as that given for the entire zone. Nota­ pretiosus (MP) Zone which is also dated as the isosti- bly, Umbonatisporites distinctus is absent. In the boreholes cha-Upper crenulata Zone (Avkhimovitch & Tumau, Rzeczenica 1 the assemblages of the Mai subzone are ac­ 1994). Thus it may be supposed that the base of the Ma4 companied and in the borehole Gorzyslaw 9 - by conodonts Subzone may also correspond to a level within the conodont of the duplicatai - sandbergi Conodont Zone zone mentioned above. So far, no conodont faunas have The Lower Convolutispora major (Ma2) Subzone has been found in association with the Ma4 miospore assem­ been distinguished in Gorzyslaw 8 and 9, Chmielno 1 and blages. MIOSPORE TAXONOMY AND STRATIGRAPHY 173

SYSTEMATIC DESCRIPTIONS Genus Hystricosporites McGregor 1960

The suprageneric classification adopted in this section Hystricosporites furcatus Owens 1971 is that introduced by Potonie & Kremp (1954), with the sub­ Fig. 7J sequent modifications by Dybova & Jachowicz (1957), But- terworth & Williams (1958), Dettman (1963), Neves & 1971. Hystricosporites furcatus Owens: p. 28, tab. 6, figs. 7-9. Owens (1966), Smith & Butterworth (1967) and Potonie Material: 15 specimens. (1970). Description: Miospores 71-87 pm in diameter, of circular amb. Described are species defining the zonal boundaries, Trilete rays not always visible due to prominent ornamentation, 1/2-3/4 of spore radius in length, accompanied by elevated, and some other, reasonably represented forms (at least 4 slightly sinuous labra about 15 pm high at the proximal pole, ter­ specimens found) which have not been described from the minating at curvatural ridges. Contact faces covered with radial, study area before. The type and figured specimens are flat ridges 6-8 pm in width. Exine outside contact faces orna­ housed in the Institute of Geological Sciences, Polish Acad­ mented with regularly distributed cylindrical, bifurcate processes emy of Sciences, Warszawa. 18-25 pm in length, 5-8 pm wide at base. Tips of the bifurcation “extended” (sensu Owens, 1971). About 20 processes cross the equator. Remarks: The specimens from Pomerania are smaller than those Antetunna SPORITES Potonie, 1893 described by Owens (1971), which are 82.5 -174.9 pm in diame­ ter. Turma TRILETES Reinsch, 1881, emend. Potonie et Distribution: Poland - western Pomerania, Gorzyslaw 8 and 11, Kremp 1954 Karcino 2 boreholes, zones RB, IP, assemblage II, Uppermost Suprasubturma ACAVATITRILETES Dettman 1963 Frasnian, lower Famennian (this paper); Arctic Canada - Queen Subturma AZONOTRILETES (Luber) Dettman 1963 Elizabeth Islands, lower Frasnian (Owens, 1971). Infraturma APICULATI (Bennie et Kidston) Potonie 1956 Subinfraturma NOD ATI Dybova et Jachowicz 1957, Hystricosporites multifurcatus (Winslow) Mortimer et sensu Potonie 1960 Chaloner 1967 Fig. 7 (E, F) Genus Corystisporites Richardson 1965 Type species Coiystisporites pomeranius Stempieri-Salek, 1967. Hystricosporites multifurcatus (Winslow) Mortimer et Cha­ new species loner: p. 195-196, tab. 26, figs 5-9. Fig. 7 (A-C) Material: 5 specimens. Description: Miospores 68-86 pm in diameter. Amb circular or Holotype: ING PAN, slide G.8.5.1, Fig. 7A. triangular with convex sides. Triradiate rays 2/3 of spore radius in Etymology: (Latin) pomeranius - derived from Pomerania. length, accompanied by elevated, sinuous labra up to 15 pm high Material: 22 specimens. at the proximal pole, not always visible due to dense ornamenta­ Dimension: 80 |im. tion. Contact faces smooth, exine outside contact faces orna­ Diagnosis: Azonate miospores with sculpture consisting of spi- mented with regularly distributed appendages 20-22 pm in length, nose processes with pointed apices. Triradiate mark with elevated up to 8 pm wide at base, with reflexed, multifurcate terminations. lips. Width of appendages at the base of multifurcation about 6 pm. Description: Miospores 75-90 pm in diameter, of circular, oval or About 15 appendages cross the equator. subtriangular amb. Trilete rays 3/4 of spore radius in length, ac­ Distribution: Poland - western Pomerania, Gorzyslaw 8 and 11 companied by elevated, sinuous labra 7 pm high at the proximal boreholes, assemblage I, zones DT, RD, assemblage II, Frasnian, pole, diminishing in height toward equator, often poorly visible lower Famennian (this paper); France, middle and Upper Frasnian due to density of ornamentation. Exine of the distal hemisphere or­ (Taugourdeau-Lantz, 1971), Frasnian and lower Famennian (Lo- namented with densely set, translucent conical elements termi­ boziak & Streel, 1988), Frasnian (Streel et ah, 1987); U S A -O h io , nated with darker, massive spinose tips. Elements of ornamenta­ Middle Devonian, basal part of Mississippian (Winslow, 1962). tion are 6 pm in length, 4-6 pm wide at base, and their massive ter­ minal spines are up to 2 pm in length. The bases of these elements are often interconnected with irregular, triangular wrinkles to form Hystricosporites porrectus (Balme et Hassel) Allen 1965 a reticulate pattern. At equator, the overlapping basal parts of orna­ Fig. 7 (D, L) mentation elements appear as a deeply incised zona. 1962. Archaeotriletesporrectus Balme et Hassel: p. 10, tab. 5, figs Remarks: The described species differs from Corystisporites 1-4. multispinosus Richardson (1965) in having shorter ornamentation 1965. Hystricosporites porrectus (Balme et Hassel), Allen: p. 698, elements terminated with solid spines. tab. 95, figs 1-3. Type-locality: Gorzyslaw 8 borehole, western Pomerania. Type-level: Czhichow Formation; IP Zone, sample G.8.5, depth Material: 31 specimens. Description: Miospores 80-105 pm in diameter. Amb circular or 3667-3669 m. triangular with convex sides. Triradiate rays 2/3 of spore radius in Stratigraphic distribution: Gorzyslaw 8 and 11 boreholes, as­ length, accompanied with elevated, sinuous labra up to 20 pm high semblage I, zones RD-IP, Frasnian, lower Famennian (this paper). at the proximal pole, not always visible due to dense ornamenta­ Deposition of types: slide G.8.5.1. tion. Contact faces smooth. Exine outside contact faces ornamen­ ted with regularly distributed cylindrical, densely set appendages 20-35 um in length, 5-6 pm wide at base, with bifurcate termina­ tion. Tips of the bifurcation “reflexed” are curved toward the spore body. About 28 appendages cross the equator. 174 M. STEMPIEN-SALEK

Distribution: Poland - western Pomerania, Gorzysiaw 8 and 11, tains, Zone LN, Uppermost Famennian (Tumau, 1990), Pomerania Strzezewo 1 and Karcino 2 boreholes, zones RD, RB and IP, Up­ and Holy Cross Mountains, zones LN-C1, Uppermost Famennian, per Frasnian, lower Famennian (this paper); Spitsbergen, Givetian Toumaisian (Clayton & Tumau, 1990); Brazil, zones LN-BP, Up­ (Allen, 1965); France - Boulonnais, middle Frasnian (Taugour- permost Famennian, lower Toumaisian (Loboziak et al.y 1988). deau-Lantz, 1971); western Australia, Upper Devonian (Playford, The species is common in western and eastern Europe in Upper­ 1982). most Famennian and lower Toumaisian.

Hystricosporites suborlovicus (Kedo) comb. nov. Umbonatisporites distinctus Clayton 1971 Fig. 7K Fig. 8A

Basionym: 1974. Archeozonotriletes suborlovicus Kedo: p. 58, 1971. Umbonatisporites distinctus Clayton: tab. 5, figs 16-17. tab. 13, fig. 19. Material: 18 specimens. Material: 8 specimens. Description: Miospores 55-75 ц т in diameter. Amb circular. Description: Miospores 70-78 ц т in diameter. Amb circular or Trilete rays straight, 1/3 to 1/2 of spore radius in length. Contact subtriangular with convex sides. Triradiate rays not always visible faces smooth, the remaining exine surface ornamented with dis­ due to dense ornamentation, about 1/2 of spore radius in length, ac­ crete, cylindrical appendages 8-15 ц т in length, 2-3 ц т in width, companied by labra up to 4 ц т wide. Contact faces smooth, exine terminated by a wide, dome-shaped tip up to 4 ц т in width sur­ outside contact faces ornamented with regularly distributed, cylin­ mounted by a spine up to 4 ц т in length. drical, densely set, bifurcate processes 10-12 ц т in length, 2-3 Distribution: Poland - western Pomerania, Gorzysiaw 9, ц т wide at base, narrowing to 1.5 ц т below the bifurcation at Chmielno 1, and Rzeczenica 1 boreholes, Subzones Маг, Маз and which point they are often broken off. Tips “reflexed or extended”. Ma4, lower Toumaisian (this paper), zones Ma-Cl, Toumaisian Up to 30 appendages project at the equator. (Tumau, 1978, 1979); Belarus - Pripyat Depression, zone U, Remarks: According to the original description of Archcieozono- Toumaisian (Avkhimovitch, 1993), common in western Europe, triletes suborlovicus these spores posses a central body. This fea­ from Zone HD. ture has not been observed in our material, probably because our specimens are much darker (more mature). Otherwise, the de­ scribed specimens are closely comparable with those from the Type species Umbonatisporites distinctus var. crinitus var. Pripyat Depression. nov. Distribution: Poland - western Pomerania. Gorzysiaw 8 and Kar­ Fig. 7 (G-I) cino 2 boreholes, zone IP, assemblage II, lower Famennian (this paper); Belarus - Pripyat Depression, lower and middle Famen­ Holotype: ING PAN, slide G.9.5.L, Fig. 7H. nian (Kedo, 1974). Etymology: (Latin) crinitus - with long hair. Material: 10 specimens. Dimension: 65 ц т in diameter. Genus Umbonatisporites (Hibbert et Lacey) Clayton 1971 Diagnosis: Azonate miospores with fine hair-like processes. Description: Miospores 55-85 ц т in diameter.Amb circular. Umbonatisporites abstrusus (Playford) Clayton 1971 Trilete rays straight, 3/4 of spore radius in length. Contact faces Fig. 8 (В, C) smooth, the remaining exine surface covered by densely set, cylin­ drical appendages 6-13 ц т in length, 0.5-1 ц т wide at base, 2-3 1971. Umbonatisporites abstrusus (Playford) Clayton: p. 591. ц т apart. Appendages have a 2.5 ц т wide thickening situated at Material: 8 specimens. half of their length and a dome shaped tip up to 4 ц т in width, sur­ Description: Miospores 60-68 ц т in diameter. Amb circular. mounted by a spine about 4 ц т in length. Trilete rays straight, 1/3 to 1/2 of spore radius in length. Contact Remarks: Umbonatisporites distinctus var. crinitus differs from faces smooth, exine outside contact faces ornamented with small U. distinctus Clayton (1971) in having more closely spaced, thin­ appendages up to 2 ц т in diameter, about 1.5 ц т wide at base, and ner and longer in relation to spore radius appendages. about 2 ц т apart. Terminations of the appendages are dome­ Type-locality: Gorzysiaw 9 borehole, western Pomerania. shaped or flattened, their width equals the appendage length. Some Type-level: S^polno Formation, Subzone Маг, sample G.9.5, terminations bear a small spine. depth 3149-3150 m. Distribution: Poland - western Pomerania, Gorzysiaw 8 and 9, Stratigraphic distribution: Gorzysiaw 8 and 9, Chmielno 1 bore­ Rzeczenica 1 boreholes, Subzones Ra2 and Маг, Uppermost Fa­ holes, Subzone Маг, Toumaisian (this paper). mennian, lowermost Toumaisian (this paper), Holy Cross Moun­ Deposition of types: slide G.9.5.1.

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Fig. 7. Miospores from Upper Frasnian, Famennian and lower Carboniferous in western Pomerania. Specimens С, E, F are from Gorzysiaw 11.14, 3284-3285 m DT Zone, other specimens as indicated below. All magnifications x 500 except when indicated. A - Co- lystisporitespomeranius n. sp., holotype, Gorzysiaw 8.5, 3667-3669 m, IP Zone; В - Corystisporitespomeranius n. sp., Gorzysiaw 11.10, 3246-3247 m, RD Zone; С - Coiystisporites pomeranius n. sp.; D - Hystricosporites porrectus (Balme et Hassel) Allen, Gorzysiaw 11.10, 3246-3247 m, RD Zone, magnification x 300. E, F - Hystricosporites multifurcatus (Winslow) Mortimer et Chalomer, magnifica­ tion x 300 and x 1400; G - Umbonatisoporites distinctas var. crinitus var. nov., holotype, Gorzysiaw 9.5, 3149-3150 m, Маг Zone; H - Umbonatisoporites distinctus var. crinitus var. nov., ibidem\ I - Umbonatisoporites distinctus var. crinitus var. nov., Gorzysiaw 9.4, 3148-3149 m, Маг Zone, magnification x 400; J - Hystricosporites furcatus Owens, Gorzysiaw 8.3, 3514-3516 m, magnification x 400, assemblage И; К - Hystricosporites suborlovicus (Kedo) comb, nov., ibidem; L - Hystricosporites porrectus (Balme et Hassel) Allen, Gorzysiaw 8.5, 3667-3669 m, IP Zone MIOSPORE TAXONOMY AND STRATIGRAPHY 175 176 M. STEMPIEN-SALEK

Subinfratumia BACULATI Dybova et Jachowicz 1957 Distribution: Poland - western Pomerania, Gorzyslaw 11, Genus Raistrickia (Schopf, Wilson et Bentall) Potonie et Strzezewo 1 boreholes, zone RD, Upper part of Frasnian (this pa­ Kremp 1954 per), Zone Ex, Givetian (Tumau, 1995); Belarus - Pripyat Depres­ sion, Frasnian (Obukhovskaya, 1986), Zone OG, Frasnian (Avkhimovitch et a l, 1993 b); Canada - Queen Elizabeth Islands, Raistrickia ramiformis (Kedo) Avkhimovitch et Higgs Frasnian (Owens, 1971). 1988 Fig. 8D Genus Corbulispora Bharadwaj et Venkatachala 1961 1978. Raistrickia variabilis Dolby et Neves: Somers et Streel, p. 149, tab.l, fig. 2. Corbulispora cf. cancellata (Waltz) Bharadwaj et 1988. Raistrickia ramiformis (Kedo) Avkhimovitch et Higgs: Venkatachala 1961 Avkhimovitch, Byvsheva, Higgs, Streel & Umnova, tab. 1, Fig. 8N fig. 16. 1988. Raistrickia minor (Kedo) Neves et Dolby: Higgs, Clayton & Material: 9 specimens. Keegan, p. 59, tab. 4: 14, 17. Description: Miospores 70-94 ц т in diameter. Amb oval, trilete Material: 7 specimens. rays straight, 3/4 of spore radius long, accompanied by lips. Exine Description: Miospores 33-58 nm in diameter. Amb circular. ornamented with ridges and rare warts; ridges slightly sinuous Trilete rays not visible due to dense ornament covering the entire forming an irregular, imperfect reticulum. Width of ridges and exine surface. The ornamentation elements are cylindrical, 1/2 to warts 5-7 ц т, width of lumina 8-10 ц т. Exine about 2 ц т wide at 3/4 of spore radius in length, 2-6 (tm wide at base, 10-15 (xm equator. apart, with flattened and laterally extended, ramified terminations Remarks: The described form differs from Corbulispora cancel­ which in some specimens are as wide as the appendages are long. lata (Waltz) Bharadwaj et Venkatachala (1961) in having less dis­ The terminations of neighbouring appendages are often in contact. tinct lips, more complete reticulum, more straight ridges and lower Exine about 2 jxm thick at equator. number of warts. Remarks: Raistrickia variabilis Dolby et Neves sensu Somers et Distribution: Poland-western Pomerania, Gorzyslaw 8 borehole, Streel (1978, tab. 1, fig. 2) and R minor sensu Higgs et al. (1988, Zone Ra and Ma (Ma2 i Маз), Upper part of Famennian, Tour- tab. 4, figs 14, 17) have been considered here as synonymous with naisian (this paper). the described species as they have identical appendages with later­ ally extended terminations. Subturma ZONOTRILETES Waltz 1935 Distribution: Poland - western Pomerania, Gorzyslaw 8 and 9 Infraturma PATINATI Butterworth et Williams 1958 boreholes, Subzones Rai, Raj, Ma2, Upper Famennian, Tour- Genus Cymbosporites Allen 1965 naisian (this paper); Belarus - Pripyat Depression, Zone PLE, Fa­ mennian (Kedo & Golubtsov, 1971); Germany, Famennian (Somers & Streel, 1978). Cymbosporites acutns (Kedo) Byvsheva 1985 Fig. 8 (E-H) Infraturma MURONATI Potonie et Kremp 1954 1985. Cymbosporites acutus (Kedo) Byvsheva: p. 127, tab. 24, Genus Convolutispora Hoffmeister, Staplin et Malloy 1955 fig. 13 non 1980. Asperispora acuta Van der Zwan: p. 227 tab. 13, figs Convolutispora subtilis Owens 1971 1-5. Fig. 8L non 2000. Grandispora acuta Higgs, Avkhimovitch, Loboziak, Maziane-Serraj, Stempien-Salek & Streel: pi. 1, figs 1 -6. 1971. Convolutispora subtilis Owens: p. 35, tab. 9, figs 3-6. Material: 48 specimens. Material: 5 specimens. Description: Miospores 48-67 ц т in diameter. Amb subtriangu­ Description: Miospores 48-58 |j.m in diameter. Amb circular or lar, sides convex, apices broadly rounded. Trilete rays straight or subtriangular. Trilete rays straight, 3/4 of spore radius in length. slightly sinuous, about 3/4 of spore radius in length. Proximal sur­ Exine ornamented with fine, sinuous, densely set ridges 2-3 |mi in face smooth, distal surface thicker than the proximal one, covered length and width. The profiles of ridges rounded. On contact faces by discrete, closely set spines 5-13 ц т in length, which have bul­ ridges are lower and more spaced. Exine about 2 fim thick at equa­ bous bases 5-8 ц т in diameter, and acute terminations. Exine tor. about 3 ц т thick at equator.

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Fig. 8. Miospores from Upper Frasnian, Famennian and Lower Carboniferous in Western Pomerania. All magnifications x 500 except when indicated. A - Umbonatisporites distinctus Clayton, Chmielno 1.6, 3907-3925 m, Маз_4 Zone; В - Umbonatisporites abstrusus (Playford) Clayton, Gorzyslaw 9.3, 3146-3147 m, Маг Zone; С - Umbonatisporites abstrusus (Playford) Clayton, Gorzyslaw 8.1, 3216-3218 m. Маг Zone; D - Raistrickia ramiformis (Kedo) Avkhimovitch et Higgs, Gorzyslaw 9.13, 3207-3208 m, Rai Zone; E - Cym­ bosporites acutus (Kedo) Byvsheva, Gorzyslaw 9.6, 3154-3155 m, Маг Zone; F, G, H - Cymbosporites acutus (Kedo) Byvsheva, Gorzyslaw 9.4, 3148-3149 m, Маг Zone; I -Cymbosporites vetlasjanicus (Medianik et Obukhovskaya): Avkhimovitch et al., Gorzyslaw 14.2, 2943-2950 m, RB Zone, magnification x 700; J, К - Cymbosporites boafeticus (Tchibrikova) Obukhovskaya, ibidem; L - Convolut­ ispora subtilis Owens, Gorzyslaw 11.6, 3193-3194 m, RD Zone; M - Aneurospora greggsii (McGregor) Streel: Becker et al., Gorzyslaw 8.5, 3667-3669 m, IP Zone; N - Corbulispora cf. cancellata Bharadwaj et Vencatachala, Gorzyslaw 9.3, 3146-3147 m, Маг Zone; О, P - Tholisporites densus McGregor, Gorzyslaw 11.10, 3246-3267 m, RD Zone; R, S - Tholisporites densus McGregor, 11.12, 3270-3271 m, RD Zone, magnification x 800 and x 2500 MIOSPORE TAXONOMY AND STRATIGRAPHY 177 178 M. STEMPIEN-SALEK

Remarks: Specimens included by Van der Zwan (1980, p. 227, Genus Tholisporites Butterworth et Williams 1958 tab. 13, figs 1 -5) in Asperispora acuta and by Higgs et al. (2000, p. 213, pi. 1, figs 1-6) in Grandispora acuta are only superficially Tholisporites densas McGregor 1960 similar to Cymbosporites acutus as they are camerate while Cym- Fig. 8 (O-S) bosporites acutus from Pomerania and C. acutus described from eastern Europe by Kedo (1963) and Byvsheva (1985) are acamer- 1960. Tholisporites densus McGregor: p. 37, tab. 13, figs 6, 7. ate. In comparison with specimens described in Kedo (1963) and 1987. Archaeozonotriletes densus Arkhangelskaya: p. 87, 88, tab. Byvsheva (1985) those from Pomerania have larger spines, which 6, fig. 5. have a wider size range (5-13 |.im to 2.5-8 (xm given by the above Material: 6 specimens. authors). Description: Miospores 45-52 (im in diameter. Amb circular Distribution: Poland - western Pomerania, Gorzyslaw 8 and 9, or oval. Trilete rays slightly sinuous, accompanied by lips about 1 Chmielno 1, Rzeczenica 1 boreholes, Zone Ma, Toumaisian (this (im in height, extending 3/4 of spore radius. Exine much thicker paper); Belarus - Pripyat Depression, Upper Famennian-Tour- distally than proximally. A thin, translucent, irregularly folded naisian (Kedo, 1963); Russia-Toumaisian (Byvsheva, 1985). membrane extends over the proximal surface; the folds are about 1 |im in width, some of them touch or are fused; they peter out in Cymbosporites boafeticus (Tchibrikova) Obukhovskaya equatorial region. Spores without ornamentation. 1986 Distribution: Poland - western Pomerania, Gorzyslaw 11 Fig. 8 (J, K) borehole, zone RD, Upper Frasnian (this paper), Jamno IG 1 bore­ hole, punctata conodont Zone (personal information, Tumau, 1972. Archaeozonotriletes boafeticus Tchibrikova: p. 128, tab. V, 1995); northern Canada, probably Frasnian (McGregor, 1960), figs 1-2 Upper Givetian-middle Frasnian, Zone OB and OT (McGregor & 1993. Cymbosporites boafeticus (Tchibrikova) Obukhovskaya: Playford, 1992); Russian Platform, Frasnian (Arkhangelskaya, Avkhimovitch, Tchibrikova, Obukhovskaya, Nazarenko, 1987). Umnova, Raskatova, Loboziak & Streel, pi. 17, fig. 12, pi. 18, fig. 13, pi. 19, fig. 12. Suprasubturma LAMINATITRILETES Smith et Material: 9 specimens. Butterworth 1967 Description: Miospores 50-65 |.im in diameter. Amb circular Subturma ZONOLAMINATITRILETES Smith et or subtriangular with convex sides and broadly rounded apices. Butterworth 1967 Trilete rays slightly sinuosus, accompanied with labra about l|j.m in height, extending almost to equator. Ray terminations forked Infraturma CRASSITI (Bharadwaj et Venkatachala) which is often invisible due to dense ornamentation. Proximal sur­ emend. Utting 1987 face smooth. Exine of the distal hemisphere distinctly thicker in re­ Genus Aneurospora Streel 1964 lation to that of the proximal one, ornamented with discrete, conical elements up to 2 (j.m in length, up to 4 |im wide at base. Ex­ Aneurospora greggsii (McGregor) Streel 1974 ine about 3 nm thick at equator. Fig. 8M Distribution: Poland - western Pomerania, Gorzyslaw 11 and 14, Karcino 2 boreholes, zones RB-IP, Upper Frasnian and 1972. Archaezonotriletes vasjamicus Tchibrikova: p.125, Tab. 4, lower Famennian (this paper); Russia - south Ural and Russian fig. 11-13 Platform, Frasnian (Tchibrikova, 1972); Belarus - Pripyat Depres­ 1974. Aneurospora greggsii (McGregor) Streel: Becker, Bless, sion, Frasnian (Obukhvskaya, 1986), Pripyat Depression, Frasn­ Streel & Thorez, p. 24, tab. 16, figs 6-15 cum synonimis. ian, Famennian, zones DE-CZ (Avkhimovitch et al., 1993b). 1993. Geminospora vasjamica (Tchibrikova) Obukhovskaya et Nekryata: Avkhimovitch, Tchibrikova, Obukhovskaya, Cymbosporites vetlctsjanicus Medianik et Obukhovskaya: Nazarenko, Umnova, Raskatova, Loboziak & Streel, tab. 18, figs 4-5, tab. 19, fig. 5. Avkhimovitch et al. 1993 Fig. 81 Material: 22 specimens. Description: Miospores 50-65 jxm in diameter. Amb subtriangu­ 1993. Cymbosporites vetlasjanicas Medianik et Obukhovskaya: lar, sides convex, apices broadly rounded. Trilete rays straight, ex­ Avkhimovitch, Tchibrikova, Obukhovskaya, Nazarenko, tending almost to equator, terminating at curvaturae imperfectae. Umnova, Raskatova, Loboziak & Streel: tab. 14, figs 6, 9. Exine ornamented with densely set cones up to 1 |im in height. On Material: 2 specimens. contact faces, cones are more spaced or absent. Exine about 2 (am Description: Miospores 45-55 |im in diameter. Amb circular or thick at equator. subtriangular, with convex sides and rounded apices. Trilete rays Distribution: Poland - western Pomerania, Gorzyslaw 8 and 14, straight, accompanied by labra up to 1 |im in height, extending al­ Karcino 2 boreholes, zones RB, IP, assemblage II, Uppermost most to equator. Proximal surface smooth, exine of distal hemi­ Frasnian-lower Famennian (this paper), southeastern Poland, Pi- sphere distinctly thicker in relation to the proximal one ornamen­ onki 4 borehole, Givetian/Frasnian (Tumau, 1985, 1986), Holy ted with discrete conical elements up to 2 |im wide and high. Exine Cross Mountains, Zone LN, Upper Famennian (Tumau, 1990); about 3 (im thick at equator. southern Ural, lower Famennian (Tchibrikova, 1972); Belarus - Distribution: Poland - western Pomerania, Gorzyslaw 11 bore­ Pripyat Depression, Frasnian-Famennian (Obukhovskaya and hole zone RB, Frasnian/Famennian transition beds (this paper); Nekryata in Avkhimovitch et a l, 1993b); Canada - Alberta, Ghost Belarus - Pripyat Depression, Frasnian, zones OG and DE (Media­ River Formation, Givetian-Frasnian (McGregor, 1964). Common nik &Obukhovskaya: Avkhimovitch et al., 1993b). in Europe from Frasnian to Famennian. MIOSPORE TAXONOMY AND STRATIGRAPHY 179

Subturma CINGULICAVATI Smith et Butterworth 1967 Samarisporites cf. triangulatus Allen 1965 Genus Cristatisporites (Potonie et Kremp) Butterworth Fig. 9E 1967 Material: 5 specimens. Description: Miospores 55-68 (un in diameter. Amb subtriangu­ lar, sides straight or slightly convex, apices triangular. Trilete rays Cristatisporites deliquescens (Naumova) Arkhangielskaya accompanied with slightly sinuous labra up to 3 fim in height, ex­ 1987 tending to equator. Contact faces smooth, exine outside contact Fig. 9 0 faces finely granulate and covered by spaced cones and spines up to 5 |.im wide at base, 2-5 (a.m in length. Some cones are sur­ 1953. HymenozonotriletesdeliquescensNaumova: p. 67, tab. 9, fig. mounted by spines (the total length of biform elements up to 6 8 . fun). In equatorial view, at intexine margin, the bases of spines and 1987. Cristatisporites deliquescens (Naumova) Arkhangelskaya: cones are joined to form a reticulum. p. 89, tab. 6, fig. 4. R em arks: Samarisporites cf. triangulatus from Pomerania differs Material: 4 specimens. from Samarisporites triangulatus Allen (1965) in being slightly Description: Miospores 86-96 uni in diameter. Amb subtriangu- larger, having less convex sides and less elongated, more acute lar, sides convex, apices broadly rounded. Trilete rays slightly apices. sinuosus, accompanied by lips 2-3 |un in width, extending 2/3 of Distribution: Poland - western Pomerania, Strzezewo 1, Gorzy­ spore radius. Amb of the intexine oval or slightly subtriangular. slaw 11 boreholes, assemblage I, zone RD, Frasnian (this paper). Exoexine extended laterally at equator to form a differentially thickened zona; inner thicker portion 3-4 p.m in width, thinner, Suprasubturma CAMERATITRILETES Neves et Owens outer portion 10-15 |im in width. Exine surface finely granulate, distal surface ornamented with spaced mamillate spines 4—6 nm 1966 long, 3—4 p.m wide at base. Spines often corroded. Subturma SOLUTITRILETES Neves et Owens 1966 Remarks: In our specimens, the trilete rays extend to the inner Infratunna DECORATI Neves et Owens 1966 part of the cingulizona while in those from the Russian Platform, Genus Grandispora Hoffmeister, Staplin et Malloy emend. they are longer, extending beyond this part of zona. The zona in Neves et Owens 1966 specimens from Pomerania is narrower than in those from the Rus­ sian Platform. The spines of the specimens from Pomerania are Grandispora villosa (Avkhimovitch) comb. nov. corroded. Fig. 9 (G, K, L) Distribution: Poland - western Pomerania, Gorzyslaw 11 and 14 boreholes, assemblage I, zones RD and RB, Frasnian and lower­ Basionym : 1974. Hvmenozonotriletes villosus Avkhimovitch: p. most Famennian (this paper); Russian Platform - Voronezh area, 98, tab. 28. fig. 4. Frasnian (Naumova, 1953), eastern part of Russian Platform, Up­ Material: 5 specimens. per Frasnian (Tchibrikova, 1977), Frasnian, equivalents of Zones Dimension: 30-40 |xm in diameter. OG-DE (Arkhangelskaya, 1987); Belarus - Pripyat Depression, Diagnosis: Trilete camerate miospores, exoexine detached from Zones OG-DE (Avkhimovitch et al., 1993b). intexine, sculpture consisting of discrete, spinose processes. Description: Amb subtriangular, sides convex, apices broadly rounded. Trilete rays straight, extending almost to equator. Spores Samarisporites triangulatus Allen 1965 cavate, intexine well delimited, radius 1/2 to 3/4 of spore radius. Fig. 9 (A-D) Exoexine detached from intexine, forming a pseudosaccus appear­ ing as an equatorial zona. Contact faces smooth, the remaining part 1965. Samarisporites triangulatus Allen: p. 716, tab. 99, figs 1-6. of exine ornamented with discrete, regularly distributed cones 1-2 Material: 23 specimens. p.m high and wide at base, 1-2 |im apart. Description: Miospores 40-58 |j.m in diameter. Amb subtriangu­ Remarks: Specimens are listed by Avchimovitch (1974), non de­ lar, sides convex, apices slightly rounded, elongated, reminding of scribed. ears. Trilete rays straight, accompanied by slightly sinuous labra Distribution: Poland-western Pomerania, Gorzyslaw 8 borehole, about 2 (im in height, extending onto the zona. Intexine circular or assemblage II, Famennian (this paper); Belarus - Pripyat Depres­ subtriangular in outline, closely appressed to exoexine. Contact sion, Famennian (Avkhimovitch, 1974). faces smooth, exine outside contact faces finely granulate, and or­ namented with spaced cones and spines up to 5 fim wide at base, Genus Rugospora Neves et Owens 1966 2-5 p.m in length. Some cones are surmounted by a spine (the bi­ form elements are up to 6 |xm in length). In equatorial view, at in­ texine margin, bases of spines and cones are fused to form a Ritgospora granulatipimctata (Hoffmeister, Staplin et reticulum. Malloy) Higgs et al. 1988 Distribution: Poland - western Pomerania, Strzezewo 1, Gorzy­ Fig. 9F slaw 11 boreholes, assemblage I, zone RD, Frasnian, (this paper), Givetian Subzonc Ex3, (Tumau, 1985, 1986), central Poland, Holy 1988. Ritgospora granulatipimctata (Hoffmeister, Staplin et Mal­ Cross Mountains, Givetian, Subzone Ex3 (Malec & Tumau, 1997; loy) Higgs, Clayton & Keegan: p. 72, tab. 12, figs 4-5, cum Tumau et Racki, 1999); France, middle Frasnian (Taugourdeau- synonimis. Lantz, 1971), Givetian/Frasnian (Loboziak & Streel, 1981, 1988); Material: 10 specimens. Belgium, Frasnian (Streel & Loboziak, 1987); Ireland, Givetian/ Description: Miospores 33-44 |im in diameter. Amb circular or Frasnian (Clayton & Graham, 1974); Spitsbergen, Upper Givetian subtriangular, sides convex, apices broadly rounded. Trilete rays (Allen, 1965); Tunisia, Libya, Givetian/Frasnian (Loboziak & straight, extending almost to equator, accompanied by slightly Streel, 1989); North America, Givetian/Frasnian (McGregor, sinuous, wide lips up 3 |im in height. Exine detached from intex­ 1979); Brazil - Parana Basin, Givetian-Frasniani (Loboziak et al., ine. Intexine distinct, outline conformable with amb, usually form­ 1988). ing 5/6 of the total spore diameter, laevigate or finely granulate. 180 M. STEMPIEN-SALEK

Exoexine densely ornamented by small wrinkles and rugulae. Toumaisian (this paper); Ireland, Zones VI-BP, Toumaisian Wrinkles 1-2 ц т in width, closely spaced, radially, sinuous ar­ (Higgs et al., 1988). ranged radialy. Distribution: Poland - western Pomerania, Gorzyslaw 8 and 9 Spelaeotriletes resolntus Higgs boreholes, Zone Ma (Mai, Маг, Маз), (this paper), Zone Ma, (Tur- Fig. 9 (I, J) nau, 1975); Belarus - Pripyat Depression, Toumaisian (Kedo, 1963); Russian Platform, Lower Carboniferous (Byvsheva, 1976); 1975. Spelaeotriletes resolutiis Higgs: p. 400, tab. 6. figs 4-6, non Ireland, Upper Famennian-Toumaisian (Van der Zwan, 1980), figs 7-9. Zones LL-PC, Upper Famennian, Toumaisian (Higgs etal., 1988); 1993. Spelaeotriletespapulosus (Sennova) Avkhimovitch: Avkhi- USA - Illinois, Kentucky, Mississipian (Hoffmeister et al., 1955). movitch, Tchibrikova, Obukhovskaya, Nazarenko, Umnova, Raskatova, Loboziak & Streel, tab. 21, fig. 4, tabl. 22, figs 7, Genus Retispora Staplin 1960 8, tabl. 24, fig. 4. Material: 33 specimens. Retispora macroreticulata (Kedo) Byvsheva 1985 Description: Miospores 40-57 ц т in diameter. Amb subtriangu­ Fig. 9N lar, sides convex, apices broadly rounded. Trilete rays accompa­ nied by slightly sinuous lips up to 3 ц т in height, extending almost 1985. Retispora macroreticulata (Kedo) Byvsheva; p. 141, tab. 28, to equator where they merge with short arcuate ridges. Exine ca­ fig. 11, cum synonimis. vate. Radius of intexine 3/4 of spore radius. Contact faces smooth, Material: 6 specimens. the remaining part of exine surface covered with elements varying Description: Spores 95-160 ц т in diameter. Amb circular, oval in form in the same specimen. These are grana, cones and bacula or subtriangular. Trilete rays straight, extending to equator, often with bulbous bases. Some cones are surmounted by a spine. The obscured by ornamentation. Exine cavate. Intexine oval in outline, ornamentation elements are up to 4 ц т in height, 1.5-2.5 ц т wide radius 1/2-3/4 of spore radius. Exoexine reticulate, muri 2 ц т high at base; some bases of elements are in contact. Exoexine about 2 and wide, lumina polygonal, up to 15 ц т in diameter. ц т thick. Distribution: Poland - western Pomerania, Gorzyslaw 9 and Distribution: Poland - western Pomerania, Gorzyslaw 8 and 9, Rzeczenica 1 boreholes, Zone Ra, Upper Famennian (Tumau, Rzeczenica 1 boreholes, assemblage II, subzones Rai, Ra г, Mai, 1978; this paper) Holy Cross Mountains, Zone LL, upper part of Маг, Upper part of Famennian, Toumaisian (this paper); Ireland, Famennian (Tumau, 1990); Belarus - Pripyat Depression, Upper Upper Famennian (Higgs, 1975), Zones VI-PC, Toumaisian Famennian (Kedo & Golubtsov, 1971; Kedo, 1974); Russian Plat­ (Higgs et al., 1988); Russian Platform, Upper Famennian-Tour- form, Upper Famennian (Byvsheva, 1985); Ireland, Upper Famen­ naisian, Zones Im-VF, Famennian (Avkhimovitch et al., 1993b). nian (Higgs, 1975), Zones LL-LE, Upper Famennian (Higgs & Russel, 1981; Higgs et al., 1988); Germany - Rheinisches Infraturma PLANATI Neves et Owens 1966 Schiefergebirge, zone LL, Upper Famennian (Higgs & Streel, Genus Auroraspora (Hacquebard, Staplin et Malloy) 1984). Richardson 1960

Genus Spelaeotriletes Neves et Owens, 1966 Auroraspora hvalina (Naumova) Streel 1974 Fig. 9R Spelaeotriletes obtusus Higgs 1975 Fig. 9H 1974. Auroraspora hyalina (Naumova) Streel: Becker et al., p. 26, cum synonimis. 1975. Spelaeotriletes obtusus Higgs: p. 400, tab. 6, figs 1-3. Material: 16 specimens. Material: 26 specimens. Description: Miospores 30-50 ц т in diameter. Amb circular or Description: Miospores 56-72 ц т in diameter. Amb circular, subtriangular. Triletes rays straight, 1/2 of spore radius in length, oval or subtriangular. Trilete rays straight, accompanied by sinu­ accompanied by labra about 3 ц т in height. Exine cavate. Intexine ous lips ending at curvaturae imperfectae. Exine cavate. Intexine small, radius 1/2 of spore radius, exoexine smooth or finely granu­ not always visible due to dense ornamentation, radius 1/2 to 3/4 of late, about 2 ц т thick. spore radius. Outside contact faces exine ornamented with densely Distribution: Poland - western Pomerania, Gorzyslaw 8 and 9 set, discrete pila and bacula 2^1 ц т long, 1-3 ц т wide at base. boreholes, Subzones Rai, Raz, Mai, Маг, Upper Famennian- Distribution: Poland - western Pomerania, Gorzyslaw 8 and 9, Toumaisian (this paper); Russian Platform, Famennian (Naumova, Rzeczenica 1, Chmielno 1 boreholes, Zone Ma (Mai, Маг, Маз), 1953), Famennian-Toumaisian (Byvsheva, 1985); France - Bou-

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Fig. 9. Miospores from Upper Frasnian, Famennian and Lower Carboniferous in western Pomerania. Specimens A, C, D, О are from Gorzyslaw 11. 17, 3319-3337 m, DT Zone, other specimens as indicated below. All magnifications x 500. A, C, D - Samarisporites trian- gulatus Allen; В - Samarisporites triangulatus Allen, Gorzyslaw 11.12, 3270-3271 m, RD Zone; E - Samarisporites cf. triangulatus Al­ len, Gorzyslaw 11.8, 3226-3227 m, RD Zone; F - Rugospora granulatipunctata (Hacquebard, Staplin et Malloy) Higgs et al., Gorzyslaw 9.9, 3187-3188 m, Mai Zone; G, K, L - Grandispora villosa (Avkhimovitch) comb, nov., Gorzyslaw 8.3, 3514-3516 m, assemblage II; H - Spelaeotriletes obtusus Higgs, Chmielno 1.5, 3952-3962 m, Маг Subzone; I, J - Spelaeotriletes resolutus Higgs, Gorzyslaw 9.11, 3198-3199 m, Rai Subzone; M - Diducites versabilis (Kedo) Van Veen, Gorzyslaw 9.13, 3207-3208 m, Rai Subzone; N - Retispora macroreticulata (Kedo) Byvsheva, Gorzyslaw 9.11, 3198-3199 m, Rai Subzone; О - Cristatisporites deliquescens (Naumova) Ark- hangielskaya; P - Diducites poljessicus (Kedo) Van Veen, Karcino 2.1, 2939-2940 m, IP Zone; R - Auroraspora hyalina (Naumova) Streel: Becker et al., Gorzyslaw 9.4, 3148-3149 m, Маг Subzone; S - Cristatisporites cf. deliquescens (Naumova) Arkhangielskaya, Gorzyslaw 11.14, 3284-3285 m, DT Zone MIOSPORE TAXONOMY AND STRATIGRAPHY 181 182 M. STEMPIEN-SALEK

lonnais, Frasnian/Famennian transition (Loboziak & Streel, 1988); paper), Zones Ve, Lu, Ra, Upper Famennian (Tumau, 1979), Holy Belgium, Upper Frasnian-Famennian (Becker et al., 1974); Brazil, Cross Mountains, Famennian (Tumau, 1990); Belarus - Pripyat palynozone IV, Frasnian (Loboziak et al., 1988); Libya, palyno- Depression, Devonian/Carboniferous transition (Kedo, 1974; zone 11, Upper Famennian (Massa & Moreau-Benoit, 1976; Avkhimovitch et al., 1988b); Ireland, Zones LL-VI, Upper Famen­ Moreau-Benoit, 1980, 1989). nian, Toumaisian (Van Veen, 1981), Zones LL-LN, Upper Famen­ nian (Van der Zwan, 1980); France -Boulonais, Upper Famennian (Streel et al., 1987; Loboziak & Streel, 1988); Belgium - Arden­ Diducites poljessicus (Kedo) Van Veen 1981 nes, Famennian (Streel in Becker et al., 1974); Germany - Fig. 9P Rheinisches Schiefergebirge, Zones LL-LN, Upper Famennian 1957. Hymenozonotriletes poljessicus (Kedo); p. 25, tab. 3, figs (Higgs & Streel, 1984). 6- 8. 1974. Aurorasporapoljessica (Kedo) Streel: Becker et al., p. 26, Subturma MEMBRANATITRILETES Neves et Owens tab. 20, figs 8-14. 1966 1981. Diducites poljessicus (Kedo) Van Veen: p. 271, tab. 4, figs Infraturma CONTINUATI Neves et Owens 1966 1-4, 6. Genus Geminospora Balme 1962 Material: 4 specimens. Description: Miospores 67-75 pm in diameter. Amb circular or Type species Geminospora condensa Stempien-Salek, new oval. Trilete rays straight, extending to the intexine margin. Exine species cavate. Intexine attached to exoexine proximally, often situated Fig. 10 (A, D, E) out of centre, outline subtriangular, sides convex, apices rounded, surface bearings few irregular folds. Radius of intexine 2/3-3/4 of Holotype: ING PAN, slide G.9.11.2, 26/37, Fig. 10A. spore radius. Exoexine bilayered, smooth or finely granulate. Etymology: (Latin) condensa - dense (from densely set elements Outer exoexine thinner than the inner one, visible at equatorial of ornamentation). margin. Material: 28 specimens. Distribution: Poland - western Pomerania, Gorzyslaw 8, Karcino Dimension: 52 pm in diameter. 2, zone IP, assemblage II, Famennian (this paper); Ireland, zones Diagnosis: Miospores cavates, sculpture consisting of dense spi- LL, LE, LN, Famennian (Van Veen, 1981; Van Veen et Van der nose processes. Zwan, 1978), Zone PL (Higgs, 1975); Ardennes, Famennian Description: Miospores 50-65 pm in diameter. Amb subtriangu­ (Streel in Becker et al., 1974); Germany, LL, LE, LN zones (Higgs lar, sides convex, apices broadly rounded. Trilete rays straight or & Streel, 1984); France - Boulonnais, Frasnian and Famennian, slightly sinuous, extending almost to equator, often obscured by from zone “IV” (Streel et al., 1987; Loboziak & Streel, 1988); Be­ dense ornament. Exine cavate, cava visible only in thinner and less larus - Pripyat Depression, Famennian (Kedo, 1957); Famennian densely ornamented specimens. Intexine thick, radius 4/5 of spore from Zone Im (Avkhimovitch et al., 1993b). radius. Exoexine ornamented distally and proximo-equatorially with densely set, mamillate spines 2 do 3 |im wide at base, up to 3 pm in length. Some spines are fused at base with the neighbouring Diducites versabilis (Kedo) Van Veen 1981 elements, or are about 1 pm apart. Fig. 9M Remarks: Geminospora condensa has similar amb, and size as 1981. Diducites versabilis (Kedo) Van Veen: p. 268, tab. 2, figs 5-6, Grandispora lupata Tumau (1975), but has thicker exine, more tab. 3, figs 1-6, 9, cum synonimis. closely spaced and wider spines, and narrower camera. Type-locality: Gorzyslaw 9 borehole, western Pomerania. Material: 17 specimens. Type-level: Sapolno Calcareous Shale Formation, Subzones Rai, Description: Miospores 45-60 pm in diameter. Amb oval or sub- Famennian, sample G.9.11., depth 3198 m. triangular, sides convex, apices broadly rounded. Trilete rays ex­ Deposition of types: slide G .9.11.2, 26/37. tend almost to intexine margin, accompanied by labra up to 5 pm in height. Exine cavate. Intexine outline conformable with amb, ra­ dius 1/2-2/3 of spore radius. Exoexine smooth, bilayered, outer layer visible at equatorial margin, thinner than the inner one, trans­ lucent, radially folded, folds 2-6 pm in height. Distribution: Poland - western Pomerania, Gorzyslaw 8 and 9, Chmielno 1 boreholes, assemblage II, Zone Ra, Famennian (this

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Fig. 10. Miospores from Upper Frasnian, Famennian and Lower Carboniferous in estem Pomerania. Specimens 9,12, 13, are from Gorzyslaw 11.10, 3246-3247 m, RD Zone, other specimens as indicated below. All magnifications x 500, except when indicated. A - Geminospora condensa n. sp., holotype, Gorzyslaw 9.11, 3198-3199 m, Rai Zone; B - Membrabaculisporis radiatus (Naumova) Arkhangelskaya, Gorzyslaw 11.12, 3270-3271 m, RD Zone; C, F - Membrabaculisporis radiatus (Naumova) Arkhangelskaya, Gorzyslaw 14. 2, 2943-2950 m, RB Zone; D - Geminospora condensa n. sp., ibidem; E - Geminospora condensa n. sp., Gorzyslaw 9.13, 3207-3208 m, Rai Zone; G - Archaeoperisaccus concinnus Naumova, Gorzyslaw 11.12, 3270-3271 m, RD Zone; H - Ancyrospora langii (Taugourdeau-Lantz) Allen, Gorzyslaw 11.17, 3319-3337 m, DT Zone, magnification x 400; I, M - Ancyrosporafldus (Naumova) Obukhovskaya: Avkhimovitch et al., magnification * 400; J, K - Lagenoisporites immensus (Nazarenko et Nekryata) Avkhimovitch et Tumau: Avkhimovitch et al., Karcino 2.1, 2939-2940 m, IP Zone; L - Ancyrospora furcula Owens, magnification x 400 MIOSPORE TAXONOMY AND STRATIGRAPHY 183 184 M. STEMPIEN-SALEK

Genus Membrabaculisporis Arkhangelskaya 1985 pendages with bulbous bases and tapering stems which have flat­ tened, bifurcate or multifurcate termination. Appendages 10-20 Membrabaculisporis radiatus (Naumova) Arkhangelskaya |rm in length, 6-10 |xm in basal width, about 5 |xm wide at half of their length. About 20 appendages with bases in contact are visible 1985 around the equator. Fig. 10 (B, C, F) Distribution: Poland - western Pomerania, Gorzyslaw 11 bore­ 1953. Hymenozonotriletes radiatus Naumova: p. 62, tab. 8, fig. 13. hole, assemblage I, zone RD, Frasnian (this paper); north Canada, 1985. Membrabaculisporis radiatus (Naumova) Arkhangelskaya: Frasnian (Owens, 1971). p. 74. Material: 10 specimens. Ancyrospora langii (Taugourdeau-Lantz) Allen 1965 Description: Miospores 78-98 |xm in diameter. Amb circular to Fig. 10H oval. Trilete rays straight, extending to intexine margin, often ob­ scured by ornamentation. Exine camerate, three layered. Intexine 1960. Archaeotriletes langii Taugourdeau-Lantz: p. 145, pi. 3, figs thin, occasionally folded, radius 1/3 of spore radius, attached to 33, 34, 39. exoexine in proximal region. Exoexine of contact faces smooth. 1965. Ancyrospora langii (Taugourdeau-Lantz) Allen: p. 743, tab. The remaining surface ornamented with densely set, narrow bacula 106, figs 5-7. with thickened, rounded terminations, up to 5 nm in length, about Material: 14 specimens. 2 p.m wide at tip, 1—4 |j.m apart. In compressed spores the bacula Description: Miospores 60-110 ^m in diameter. Amb subtriangu- have mostly radial orientation. Tips of bacula are covered by a lar, sides slightly convex. Trilete rays accompanied by slightly membrane. sinuous labra up to 10 (xm in height at the proximal pole, extending Remarks: In Remarks with specimens from the type area, those almost to equator, visible only in specimens with thin exine. Con­ from Pomerania do not have punctation on the outer exoexine, tact faces smooth, the remaining part of exine ornamented with which is reduced (or damaged). densely set appendages 12^10 nm in length, 10-12 fxm wide at Distribution: Poland - western Pomerania, Gorzyslaw 11 and 14, base, with tapering stems which are about 1 (im in width at 3/4 of Strzezewo 1 boreholes, zones RD, RB, Upper Frasnian-lower Fa- their length and have bifurcate terminations. The appendages are mennian (this paper); Russian Platform, Upper Frasnian (Nau­ often broken within the thinnest part. Bases of appendages are oc­ mova, 1953), Zones OG, DE, Frasnian (Avkhimovitch et al., casionally fused with the neighbouring ones. 1993b). Distribution: Poland - western Pomerania, Gorzyslaw 11, Strze­ zewo 1 boreholes, assemblage I, zones RD-RB, Frasnian-lower INCERTAE SEDIS Famennian (this paper); France - Boulonnais, Frasnian (Taugour- Genus Ancyrospora (Richardson) Richardson 1962 deau- Lantz, 1971), Givetian, Frasnian (Loboziak & Streel, 1981, 1988); Germany, Eifel, Upper Eifelian-Givetian (Loboziak et al., 1990); Spitsbergen, Givetian (Allen, 1965); Tunisia, Libya, Frasn­ Ancyrospora fidus (Naumova) Obukhovskaya: ian (Loboziak & Streel, 1989); Algeria - Givetian-Frasnian (Bou- Avkhmovitch et al. 1993 mendjel et al., 1988). Fig. 10(1, M) 1953. Archaeotriletes fidus Naumova: p. 52, pi. VI, figs 5-6. Genus Lagenoisporites Potonie et Kremp emend. Dybova- 1993. Ancyrospora fidus (Naumova) Obukhovskaya: Avkhi­ Jachowicz et al. 1979 movitch, Tchibrikova, Obukhovskaya, Nazarenko, Umnova, Raskatova, Loboziak & Streel, tab. 9, fig. 16, tab. 12, fig. 10. Lagenoisporites immensus (Nazarenko et Nekryata) Material: 27 specimens. Avkhimovitch et Tumau 1993 Description: Miospores 66-90 |im in diameter. Amb subtriangu- Fig. 10 (J, K) lar, sides straight or slightly convex. Trilete rays straight, extend­ ing to equator, accompanied by slightly sinuous labra up to 20 ^m 1971. Hymenozonotriletes immensus Nazarenko et Nekryata: high at the pole. Exine extended laterally at equator to form a nar­ Kedo, Nazarenko, Nekryata, Raskatova, Sennova &Tchi- row zona. Contact faces smooth, the remaining surface covered by brikova, p. 188, tab. 16: 1-4. densely set appendages 10-30 |xm in length, 8-10 |im wide at base. 1993. Lagenoisporites immensus (Nazarenko et Nekryata) Avkhi­ The appendages have slightly laterally extended or truncated ter­ movitch et Tumau: Avkhimovitch V. I., Tumau, E. & Clay­ minations. Some 20-25 appendages cross the equator. ton, pi. 21, fig. 1, pi. 22, fig. 12. Distribution: Poland - western Pomerania, Gorzyslaw 8, 11 and Material: 7 specimens. 14, Strzezewo 1 boreholes, assemblage I, zone RB, Frasnian, Description: Miospores 75-100 nm in diameter, usually pre­ lower Famennian (this paper); Russian Platfonn, Upper Devonian served in lateral compression. Outline irregular. Trilete mark in the (Naumova, 1953), zones EX-SD, Belarus - Pripyat Depression, form of a gula. Exine cavate, exoexine forms a distal pseudosaccus Upper Givetian-Frasnian (Avkhimovitch et al., 1993b). which in an oblique compression forms an asymmetric zona 1/2 to 1/1 of spore radius in width. Exine finely punctate. Ancyrospora furcula Owens 1971 Remarks: Lagenoisporites is a megaspore genus (Dybova-Jacho- Fig. 10L wiczowa et al., 1979). L. immensus is of miospore size and it should be transferred to some other genus. However, the material 1971. Ancyrospora furcula Owens: p.71, pi. 23, figs 1-4. from Pomerania is poor in specimens giving insufficient base for a Material: 7 specimens. taxonomic evaluation. Description: Miospores 75-98 |im in diameter. Amb subtriangu- Distribution: Poland - western Pomerania, Gorzyslaw 8, Karcino lar, sides convex. Trilete rays extending almost to equator, accom­ 2 boreholes, zone IP, assemblage II, Famennian (this paper); Bela­ panied by slightly sinuous labra up to 20 (im high at the proximal rus - Prypiat Depression, zone CZ (subzone Za-VF, Famennian pole (visible only in specimens with thin exine). Contact faces (Avkhimovitch et al., 1993b); USA, Zone torquata-gracilis-fructi- smooth, the remaining surface ornamented with densely set ap­ cosa, Famennian (Richardson & Ahmed, 1989). MIOSPORE TAXONOMY AND STRATIGRAPHY 185

SUMMARY APPENDIX 1 List of all miospore species determined The presented miospore data and their Remarks with Ancyrospora fidus (Naumova) Obukhovskaya: Avkhimovitch et those on conodont faunas from western Pomerania indicate al. 1993b that the first appearances of several stratigraphically impor­ Ancyrospora langii (Taugourdeau-Lantz) Allen 1965 tant miospore species are isochronous over large areas, and Ancyrospora furcula Owens 1971 thus, palynology is a good tool for local correlation of Up­ Aneurospora greggsii (McGregor) Streel in Becker et al. 1974 per Devonian and Toumaisian strata. Apiculiretusispora nitida Owens 1971 The Pomeranian miospore zonal scheme can be corre­ Archaeoperisaccus concinnus Naumova 1953 lated, at several stratigraphical levels, with the schemes for Archaeozonotriletes variabilis Naumova 1953 the Devonian and Lower Carboniferous of eastern Europe. Auroraspora asperella (Kedo) Van der Zwan 1980 These levels are marked by the following events: first ap­ Auroraspora hyalina (Naumova) Streel: Becker et al. 1974 Auroraspora macra Sullivan 1968 pearance of Membrabaculisporis radiatus (lower boundary Colatisporites multisetus (Luber) Avkhimovitch et Tumau 1994 of the RD zone), first appearance of Lagenoisporites im­ Convolutispora crassitunicata (Obukhovskaya) Obukhovskaya: mensus (lower boundary of the IP zone), first appearance Avkhimovitch et al. 1993b level of Diducites versabilis (lower boundary of the Assem­ Convolutispora major (Kedo) Tumau 1978 blage II) and first appearance of Knoxisporites literatus Convolutispora mellita Hoffmeister, Staplin et Malloy 1955 (lower boundary of the Ra Zone). Convolutispora subtilis Owens 1971 The proposed miospore zonal scheme is also correlat- Corbulispora cf. cancellata (Waltz) Bharadway et Venkatachala able, at several stratigraphical levels, with the miospore zo­ 1961 nal schemes for the type regions for Devonian and Lower Corbulispora vimineus (Nekryata) Obukhovskaya et Nekryata carboniferous in western Europe. These levels are marked 1983 by the following events: first appearance of Knoxisporites Cotystisporites pomeranius n.sp. Crassispora trychera Neves et Ioannides, 1974 literatus (lower boundary of the zone Ra), first appearance Cristatisporites deliquescens (Naumova) Arkhangelskaya 1987 of Umbonatisporites distinctus (lower boundary of the Маг Cymbosporites acanthaceus (Kedo) Obukhovskaya: Avkhi­ Subzone), first appearance of Spelaeotriletes balteatus movitch el al. 1993b (lower boundary of the Маз Subzone), first appearance of Cymbosporites acutus (Kedo) Byvsheva 1985 Spelaeotriletes pretiosus (lower boundary of the Ma4 Sub­ Cymbosporites boafeticus{Tchibrikova) Obukhovskaya: Avkhi­ zone). movitch et al. 1993b The results of the miospore study indicate that (a) the Cymbosporites eximius(Obukhovskaya) Obukhovskaya: Avkhi­ Człuchów Formation represents the frasnian and most of the movitch et al. 1993b Famennian (except its Uppermost part), (b) the Sąpolno Cymbosporites vetlasjanicus Medianik et Obukhovskaya: Avkhi­ Calcareous Shale Formation spans the Uppermost Famen­ movitch et al 1993b Cyrtospora cristifera (Luber) Van der Zwan 1979 nian and lowermost Toumaisian, and (c) the Gozd Arkose Cyrtospora cf. cristifera (Luber) Van der Zwan 1979 Formation is of Toumaisian age. Diaphanospora platyrugosa (Naumova) Obukhovskaya: Avkhi­ The miospore zones distinguished may be considered movitch et al. 1993b equivalents of the conodont zones: Assemblage I = (proba­ Diducites commutatus (Naumova) Avkhimovitch 1988b bly) the punctata Zone, RD zone = hassi-rhenana zones, Diducites compactus (Nekriata) Nekriata 1979 RB zone = rhenana-triangularis zones, IP zone = crepida Diducites mucronatus (Kedo) Van Veen 1981 zone, Assemblage II = (probably) marginifera Zone, Ra Diducites poljessicus (Kedo) Van Veen 1981 zone = Upper expansa-Lower praesulcata zones, Mai and Diducites radiatus (Kedo) Obukhovskaya: Avkhimovitch et al. Маг Subzones = middle and Upper part of sandbergi Zone, 1993b Маз = Lower crenulata zone, Ma4 = propably isosticha-U- Diducites versabilis (Kedo) Van Veen 1981 Diducites vishenensis Obukhovskaya et Avkhimovitch: Avkhi­ pper crenulata zone. movitch et al. 1993b The composition of the Pomeranian miospore assem­ Discernisporites micromanifestus (Hacquebard) Sabry et Neves blages from the Frasnian and Lower Famennian is similar to 1971 that of the contemporaneous assemblages described from Endoculeospora gradzihskii Tumau 1975 eastern Europe. On the other hand, the Upper Famennian Geminospora condensa n. sp. and Toumaisian assemblages are closely comparable with Geminospora micromanifesta (Naumova) Arkhangelskaya 1985 those described from western Europe. Geminospora nalevkinii (Naumova) Obukhovskaya 1986 The stratigraphic gap within the Sąpolno Calcareous Geminospora notata (Naumova) Obukhovskaya: Avkhimovitch et Shale Formation includes an Upper part of the Famennian al. 1993b and the lowermost Toumaisian. Geminospora notata var. microspinosa Tchibrikova 1972 Geminospora rugosa (Naumova) Obukhovskaya: Avkhimovitch et al. 1993b Gorgonispora crassa (Winslow) Higgs et al. 1988 Acknowledgements Grandispora aspersa (Avkhimovitch) Avkhimovitch 1976 Grandispora cornuta Higgs 1975 The author wishes to express their sincere gratitude to Profes­ Grandispora echinata Hacquebard 1957 sor Elżbieta Tumau who translated and critically discussed the text Grandispora famenensis (Naumova) Streel var. minutus Nekryata and to Elżbieta Kowalczyk for rendering the drawings. 1974 186 M. STEMPIEN-SALEK

Grandispora lupata Tumau 1975 REFERENCES Grandispora uncata (Hacquebard) Playford 1971 Grandispora villosa (Avkhimovitch) comb. nov. Allen, K. C., 1965. Lower and Middle Devonian spores of North Hymenozonotriletes cirgutus Naumova 1953 and Central Vestspitsbergen. Palaeontology, 8: 687-748. Hystricosporites corystus Richardson 1962 Arkhangelskaya, A. D., 1985. Spory iz otlozhenij tumejskogo i Hystricosporites furcatus Owens 1971 vizenskogo jarasov Russkoj plity. (In Russian). In: Menner, Hystricosporites multifurcatus (Winslow) Mortimer et Chaloner V. V. & Byvsheva, T. V. (eds). Atlas spor i pylcy neftegazo- 1967 nosnykh tolshtch fanerozoia Russkoj i Turanskoi plit. Trudy Hystricosporites porrectus (Balme et Hassel) Allen 1965 VNlGRlNedra: 1-79. Hystricosporites reflexus Owens 1971 Arkhangelskaya, A. D., 1987. Novyj rod i nekatoryje widy spor Hystricosporites suborlovicus (Kedo) comb. nov. franskovojarusa wolgogradskoj oblasti. (In Russian). Paleon- Indotriradites explanatus (Luber) Playford 1991 tologiczeskij Zurnal, (3), Akademia Nauk USSR: 84—92. Knoxisporites literatus (Waltz) Playford 1963 Avkhimovitch, V. I., 1974. Palynological characteristics of the Laevigatosporites ovalis Kosanke 1950 Upper Famennian saliferous formation in the Pripyat Depres­ Lagenoisporites immensus (Nazarenko et Nekryata) Avkhi­ sion. (In Russian). Paleozoic spores o f Belorussia, Minsk, movitch et Tumau: Avkhimovitch et al. 1993b BelNIGRl: 95-107. Lophozonotriletes excisus Naumova 1953 Avkhimovitch, V. I., 1976. Famennian spore assemblages in the Lophozonotriletes fursenkoi Nekryata 1979 salt-bearing and suprasalt measures of the Pripyat Depression Lophozonotriletes multiformis Tchibrikova 1972 and their stratigraphic significance. (In Russian). Thesis syn­ Membrabaculisporis radiatus (Naumova) Arkhangelskaya 1985 opsis, Vilnius State University: pp. 30. Murospora dubitata Higgs 1975 Avkhimovitch, V. I., 1986. Zonal differentiation and correlation of Plicatispora scolecophora (Neves et Ioannides) Higgs et al. 1988 the Devonian/Carboniferous boundary deposits in Belorussia Pustulatisporires gibberosus (Hacquebard) Playford 1964 (Pripyat Depression) with the standard sections of the Raistrickia corynoges Sullivan 1968 Franco-Belgian Basin by the spores. Palaeontology and its Raistrickia minor (Kedo) Neves et Dolby f967 role in the knowledge study of the Geological Structure of Be­ Raistrickia ramiformis (Kedo) Avkhimovitch et Higgs: Avkhi­ lorussia. (In Russian). Nauka i Technika: 145-165. movitch et al. 1988b Avkhimovitch, V. I., 1993. Zonation and spore complexes o f the Raistrickia spathulata (Winslow) Higgs 1975 Devonian and Carboniferous boundary deposits of the Pripyat Raistrickia variabilis Dolby et Neves 1970 Depression (Belorussia). Annales de la Societe Geologique de Retispora lepidophyta (Kedo) Playford 1976 Belgique, 115: 425-452. Retispora macroreticulata (Kedo) Byvsheva 1985 Avkhimovitch, V. I. & Tumau, E., 1994. The Lower Carbonifer­ Retusotriletes cohatus Sullivan 1964 ous Prolycospora claytoni Zone o f Western Pomerania and its Retusotriletes planus Dolby et Neves 1970 equivalents in Belorussia and North-westem Europe. Annales Retusotriletes pychovi Naumova 1953 Societatis Geologorum Poloniae, 63: 249-263. Rugospora radiata, Avkhimovitch et al. 1988a Avkhimovitch, V. I., Nekryata, N. S. & Obukhovskaya, T. G., Rugospora granulatipunctata (Hoffmeister, Staplin et Malloy) 1988a. Devonian palynostratigraphy of the Pripyat Depres­ Higgs et al. 1988 sion, Byelorussia. In: Devonian o f the World. Proceedings o f Samarisporites triangulatus Allen 1965 the II International Symposium. Devonian System, Calgary, Schopfltes cf. delicatus (Higgs) Higgs et al. 1988 Canada, 3: 559-567. Spelaeotriletes balteatus (Playford) Higgs 1975 Avkhimovitch V. I., Tumau, E. & Clayton, G., 1993a. Correlation Spelaeotriletes obtusus Higgs 1975 of uppermost Devonian and Lower Carboniferous miospore Spelaeotriletes pretiosus (Playford) Neves et Belt 1971 zonations in Belorussia, Poland and Western Europe. Annales Spelaeotriletes resolutus Higgs 1975 de la Societe Geologique de Belgique, 115: 453—458. Tholisporites densus McGregor 1960 Avkhimovitch, V. I., Byvsheva, T. V., Higgs, K., Streel, M. & Tumulispora malevkensis (Kedo) Tumau 1978 Umnova, V. T., 1988b. Miospore systematics and stra­ Tumulispora obscura Staplin et Jansonius 1964 tigraphic correlation of Devonian-Carboniferous boundary Tumulispora rarituberculata (Luber) Playford 1991 deposits in the eastern part of the USSR and Western Europe. Umbonatisporites abstrusus (Playford) Clayton 1971 Courier Forschimgsinstitut Senckenberg, 100: 169-191. Umbonatisporites distinctus Clayton 1971 Avkhimovitch, V. I., Tchibrikova, E. V., Obukhovskaya, T. G, Umbonatisporites distinctus var. crinitus, n. var. Nazarenko, A. M., Umnova, V. T., Raskatova, L. G., Mant- Vallatisporites cf. pussilites (Kedo) Dolby et Neves 1970 surova, V. N., Loboziak, S. & Streel, M., 1993b. Middle and Velamisporites cf. caperatus (Higgs) Higgs et al. 1988 Upper Devonian mispore zonation of Eastern Europe. Bulle­ Velamisporites magnus (Huphes et Hay ford) Playford 1971 tin des Centres de Recherche Exploration-Production Elf Verrucosisporites evlanensis (Naumova) Obukhovskaya: Avkhi­ Aquitaine, 17: 79-147. movitch et al. 1993b Balme, B. E., 1962. Upper Devonian (Frasnian) spores from the Verrucosisporites cf. evlanensis (Naumova) Obukhovskaya: Carnarvon basin, Western Australia. The Palaeobotanist, 9: Avkhimovitch et al. 1993b 1- 10 . Verrucosisporites grumosus (Naumova) Sullivan 1964 Becker, G., Bless, M. J. M., Streel, M. & Thorez, J., 1974. Palynol- Verrucosisporites nitidus Playford 1964 ogy and ostracod distribution in the Upper Devonian and ba­ Verrucosisporites oppressus (Higgs) Higgs et al. 1988 sal Dinantian of Belgium and their dependence on sedimen­ Verrucosisporites scurrus (Naumova) McGregor et Camfield 1982 tary facies. Mededelingen Rijks Geologische Dients, Nieuwe Serie, 25: 9-99. Bednarczyk, W., 1974. The Ordovician in the Koszalin-Chojnice region (Western Pomerania). Acta Geologica Polonica, 24: 581-600. Appendix 2 I I I I 1 I I I I I I I ] I I

| I 1

O pussilites x crinitus cancellata LU is delicatus delicatus

DC cf. sp. | var. var. cf. zonation CO

cf. cf. O | 1 3

CO zonation CD (D I cf.

X] £ number of Pomeranian m iospore of of palynological sample scurrus obscura 2 1 randispora randispora lupata FORMATION BOREHOLE Depth Depth in metres and num ber 7. 7. 1/. 1/. Convolutispora Convolutispora major mellita C. Corbulispora Corbulispora Crassispora trychera Cymbosporites acutus Discernisporites micromanifestus \ condensa Geminospora Gorgonispora crassa G \ cf. Velamisporites caperatus V. magnus nitidus Verrucosisporites Raistrickia corynoges Raistrickia \ SAMPLE resolutus Tumulispora malevkensis Plicatispora scolecophora Plicatispora gibberosus Pustulatisporites granulatipunctata Rugospora Auroraspora Auroraspora asperella A. hyalina Diducites commutatus D. versabilis Endoculeospora gradzinski Knoksisporites literatus Lophozonotriletes excisus ramiformis R. variabilis R. \ Umbonatisporites abstrusus Umbonatisporites distinctus U. distinctus U. R. R. radiata Schopfites Spalaeotriletes balteatus SAMPLE obtusus R. R. minor Retispora Retispora lepidophyta R. macroreticulata A. A. macra Depth Depth in metres and Pomeranian Pomeranian miospore 1 1 I I I I I I | I I I I I palynological samples Convolutispora Convolutispora major Geminospora condensa Grandispora cornuta Grandispora echinata Tumulispora Tumulispora malevkensis Coatisporites Coatisporites multisetus Crassispora trychera Cymbosporites acutus Cyrtospora cristifer Grandispora lupata Tumulispora Tumulispora obscura Tumulispora rarituberculata Vallatisporites Verrucosisporites nitidus Verrucosisporites scurrus Diducites Diducites versabilis Endoculeaspora gradzinski Grandispora uncata Umbonatisporites Umbonatisporites abstrusus Umbonatisporites distinctus Auroraspora Auroraspora macra Indotriradites explanatus Knoxisporites literatus Lophozonotriletes excisus Pustulatisporites gibberosus Raisrickia condylosa Raisrickia corynoges Raisrickia variabilis Spelaeotriletes Spelaeotriletes balteatus Spelaeotriletes obtusus Spelaeotriletes pretiosus Spelaeotriletes resolutus 3141,0-3142,0 Retispora lepidophyta Retispora macroreticulata Rugospora radiata Schopfites M03 sample 1 1 1 1 2 3 1 1 1 1 3 3145,0-3146,0 3863,0-3870,0 2 1 2 C l 10 2 1 15 3 1 2 sample 2 2 3 pr.7 10 1 1 ° ^ 3146,0-3147,0 CD 2 3 1 1 1 2 1 2 2 1 1 3 1 1 2 2 3907,0-3925,0 sample 3 < Ma34 8 2 6 1 1 2 1 3 6 3 2 5 6 5 2 3148,0-3149,0 pr. 6 1 2 4 2 1 2 2 1 sample 4 2 3 2 1 E 3952,03962,0 o LL 2 8 3 1 1 3 1 4 3149,0-3150,0 Ma2 pr. 5 2 2 2 sample 5 3 4 5 2 2 2 1 1 4 1 3 _ l _C 3999,0-4013,0 3154,0-3155,0 LU o Ma1 1 6 1 2 1 2 2 3 4 1 1 2 2 2 2 Ma2 sample 6 1 1 3 4 3 1 2 1 1 3 1 1 CO pr. 4 3175,0-3176,0 S o 4 2 4 1 1 4013,0-4021,0 sample 7 X TO Ra2 4 3 2 1 3 1 3183,0-3184,0 o o pr. 3 sample 8 2 2 1 1 2 1 3 o 4091,0-4108,0 c 1 1 2 1 4 1 3 5 3185,0-3186,0 Pr- 2 sample 8a 1 1 1 1 2 2 o Ra1 4192,0-4210,0 3186,0-3187,0 & 1 5 2 4 2 4 8 1 sample 8b 1 1 1 1 C/3 pr-1 3187,0-3188,0 2896,0-2899,0 sample 9 4 1 1 1 2 2 1 1 2 3 4 2 3 1 2 1 1 5 2 5 2 3 1 2 1 3 3 1 1 1 Mai pr. 12 3188,0-3189,0 Ma2 sample 9a 1 1 2 2 1 2 1 2 1 1 2 1 2899,0-2901,3 © 7 3 2 3 4 3 4 4 1 3 5 5 05 M a?/ 3189,0-3190,0 pr. 11 1 -£Z 1 1 1 2 2 CO Ra? sample 9b E 2910,0-2913,0 3190,0-3191,0 (fi 1 T- u_ Ma1 2 1 2 2 1 1 1 4 1 1 2 1 1 I sample 9c 2 2 1 1 pr. 10 O < JZ V) 0 3191,0-3192,0 o 2920,7-2921,0 03 sample 9d 1 2 1 1 1 1 1 o CO 1 2 3 1 3 2 3 1 3 2 1 3 3 3 2 1 > _o pr. 9 N 3192,0-3193,0 DC CD 1 2 3 2 o 2921,5-2922,0 o o sample 9e LII cc 10 10 6 2 3 5 6 9 8 1 6 1 8 2 3 o 3193,0-3194,0 N O pr. 8 o 1 1 1 2 2 1 _c sample 9f O o 2922,0-2922,5 o Ra2 LU c 8 4 1 4 1 1 2 6 1 1 3194,0-3195,0 pr.7 3 1 1 3 5 1 6 sample 9g 1 1 2 N o Ma/Ra CO 3195,0-3196,0 IT 2922,5-2923,0 & 4 1 2 1 1 3 3 3 4 4 1 4 6 sample 9h 2 1 1 1 CO pr. 6 2 1 1 1 3196,0-3194,0 2 2 3 1 1 1 1 1 1 3 1 2923,0-2923,5 sample 9i 8 1 2 1 1 2 3 1 1 4 1 4 1 3197,0-3198,0 pr. 5 sample 10 1 1 1 2 3 1 3 2923,5-2924,0 5 3 3 1 1 3 5 1 3 3198,0-3199,0 pr. 4 1 1 1 2 1 sample 11 1 3 1 2 2 2 9 4 2 3 4 4 1 2 3 2 2 3199,0-3200,0 sample 11a 2 2 1 1 1 2 1 2 1 1 3200,0-3201,0 sample 11b 1 1 1 2 2 1 2 3201,0-3203,0 sample 11c 1 1 1 2 1 1 3 1 Rai 3205,0-3206,0 sample 12 1 1 2 2 2 4 5 2 3 1 3207,0-3208,0 sample 13 2 1 2 2 1 3 2 2 2 2 1 1 1 2 3208,0-3209,0 sample 14 1 1 1 2 1 5 1 2 1 1 3213,0-3214,0 sample 15 1 1 1 1 1 5 2 1 2 1 7 1 2 2 Appendix 2 j J J j j j j j

| | j |

| j | |

| J

| |

[ | | | | j j minutus caperatus | crinitus | cristifer | | j | | cf. var. | zonation J Formation | zonation

sp. | sp. | |

cf. var. 3 ] BOREHOLE BOREHOLE w

Depth and number and Depth w | | j g £ 8? of of sample palynological 3 Pomeranian miospore a 1 o of palynological sample villosa Pomeranian Pomeranian miospore famenensis w pychovi c 1 to Velamisporites magnus Velamisporites evlanensis Verrucosisporites Depth Depth in metres and number Corbulispora Corbulispora vimineus boafeticus Cymbosporites poljessicus Diducites notata Geminospora rugosa G. aspersa Grandispora Laevigatosporites ovalis Laevigatosporites immensus Lagenoisporites Fm D. vishenensis D. Hystricosporites furcatus Hystricosporites porrectus H. suborlovicus H. furssenkoi Lophozonotriletes multiformis L. planus Retusotriletes Aneurospora greggsii Aneurospora Knoxisporites literatus Knoxisporites magnus Velamisporites Verrucosisporites evlanensis Verrucosisporites Velamisporites Tumulispora malevkensis Tumulispora obscura T. rarituberculata T. distinctus U. Grandispora aspersa Grandispora G. G. immensus Lagenoisporites excisus Lophozonotriletes corynoges Raistrickia minor R. Geminospora notata Geminospora condensa G. multifurcatus H. porrectus H. Convolutispora major Convolutispora Corbulispora trychera Crassispora acutus Cymbosporites Retusotriletes planus Retusotriletes resolutus SAMPLE abstrusus Umbonatisporites distinctus U. H. suborlovicus H. dubitata Murospora scolecophora Plicatispora ramiformis R. Hystricosporites furcatus Hystricosporites Diducites commutatus Diducites compactus D. poljessicus D. versabilis D. micromanifestus Discernisporites Cyrthospora ft ft granulatipunctata Rugospora obtusus Spalaeotriletes Auroraspora asperelia Auroraspora A. hyalina Ancyrospora fidus Ancyrospora Ancyrospora greggsii Aneurospora A. A. macra a: i i ! Sąpolno 2939,0-2940,0

Calc. Shale Calc. Shale Formation 3216,0-3218,0 1 6 1 2 16 2 4 2 2 2 4 1 2 1 2 2 1 2 6 2 2 sample 1 1 1 1 1 2 1 2 3 4 Ma2 sample 1 3 3 3 3 8 4 7 9 3 3 ca 3514,0-3516,0 LL 2976,0-2977,0 Ass. II 2 3 1 3 3 1 3 3 2 5 4 2 4 3 2 1 1 4 2 O sample 2 1 1 1 2 1 2 1 2 sample 3 ć . 'O 2977,0-2978,0 3667,0-3669,0 ip 1 2 2 1 1 1 1 1 2 IP sample 5 6 2 2 8 2 1 5 4 4 O -C sample 3 Fm CC 3705,0-3708,0 3 3016,0-3018,0 < "n 1 2 1 1 3 2 1 4 2 3 5 V sample 4 sample 6 O 3735,0-3737,0 3018,0-3020,0 2 3 1 2 1 2 sample 5 1 1 1 1 1 1 1 RB sample 7 j j j 3764,0-3767,0 J j GORZYSŁAW GORZYSŁAW 8 Człuchów Człuchów sample 8 2 3 1 2 2 1 |

|

3939,0-3943,0 | 1 2 1 1 1 1

sample 9 |

LU j j _l 1

o X LU microspinosa j

j c c number

zonation

| 1 Formation

o var. |

| CD ■2 | io

j evlenensis rugosa notata notata boafeticus Depth Depth in metres and §) Pomeranin miospore 1 triangularis of of palynological sample Geminospora nalevkinii Geminospora Cristatisporites deliquescens Cristatisporites Cymbosporites acanthaceus Cymbosporites C. G. radiatus Membrabaculisporis G. G. G. D. radiatus D. Retusotriletes pychovi Retusotriletes ID fidus Ancyrospora greggsii Aneurospora Q E cf. w cf.

zonation 2829,0-2847,5 1 : 0 sample 1 3 2 1 2 1 1 c l

Fm RB BOREHOLE Formation

G. G. 14 2943,0-2950,0

Pomeranian miospore Pomeranian E Człuchów of palynological sample palynological of vetlasjanicus subtilis 5 1 5 1

nalevkinii 3 1 2 1 2 2

rugosa 3 2 grumosus sample 2 Tholisporites densus Tholisporites V. V. Depth in metres and number and metres in Depth micromanifesta Geminospora G Verrucosisporites Convolutispora crassitunicata Convolutispora C. boafeticus Cymbosporites eximius C. H. reflexus H. ovalis Laevigatosporites radiatus Membrabaculisporis incohatus Retusotriletes triangulatus Samarisporites Diducites radiatus Diducites nofate G. argutus Hymenozonotriletes furcatus Hystricosporites Ancyrospora Ancyrospora fidus langii A. pomeranius Corystisporites deliquescens Cristatisporites C. H. H. multifurcatus porrectus H. Aneurospora Aneurospora greggsii Apiculiretusispora nitida Archaeoperisaccus concinnus platyrugosa Diaphanospora A A furcula 1 Archaeozonotriletes Archaeozonotriletes variabilis Samarisporites j J j j ! | | I G. 3050,0-3051,0

2 1 1 1 1 j pr.2 | RB 3060,0-3061,0 pr. 3 1 1 3 2 1 1 2 1 3

3118,0-3122,0 triangulatus - pr. 5 1 1 1 1 1 2 2 2 1 E cf. u_ 3193,0-3194,0 I pr. 6 1 2 1 1 2 2 3 1 1 3 2 1 zonation Formation and and number £ RD 3226,0-3227,0 |

CO BOREHOLE

‘O 1 1 1 1 1 2 2 1 1 1 2 3 1 3 1 1 Depth in metres >- JZ pr. 8 nalevkinii notata rugosa o 3246,0-3247,0 Pomeranian miospore 2 1 3 5 1 2 2 3 2 2 1 4 2 1 1 1 1 2 2 1 of palynological sample Cymbosporites acanthaceus Cymbosporites Geminospora micromanifesta Geminospora G. G. Convolutispora subtilis Convolutispora G. G. G. corystus Hystricosporites porrectus H. radiatus Membrabaculisporis triangulatus Samarisporites Samarisporites O - 2 pr. 10 fidus Ancyrospora A. langii 3270,0-3271,0 0 o 3 2 2 1 3 2 2 2 1 2 2 3 2 1 2 1 1 2 5 1 2 3922.0-3924,0 pr. 12 1 1 2 2 1 1 3284,0-3285,0 sample 0 Ass. 1 pr. 14 2 1 1 2 5 1 1 2 2 1 1 1 2 6 2 1 E 4165,0-4166,0 sample 1 2 1 2 1 2 3 1 1 1 1 1 3319,0-3337,0 O LL 2 3 2 3 1 2 3 3 2 3 5 £ 4290,0-4291,0 pr. 17 5 1 1 1 HI 'O sample 9 SZ RD UJ o 4296,0-4300,0 =3 sample 10 1 1 2 1 N 4355,0-4356,0 h O 1 1 1 W sample 11 4454,0-4458,0 sample 13 1 2 1 1 1 2 3 1 2 2 1 MIOSPORE TAXONOMY AND STRATIGRAPHY 187

Bharadway, D. C. & Venkatachala, B. S., 1961. Spore assemblage nian-Carboniferous boundary in the northem"Rheinisches- out of a Lower Carboniferous shale from Spitsbergen. The Schiefergebirge", Germany. Courier Forschungsinstitut Palaeobotanist, 10: 18—47. Senckenberg, 67: 157-179. Boumendjel, K., Loboziak, S., Paris, F., Steemans, P. & Streel, M. Higgs, K., Clayton, G. & Keegan, J. B., 1988. Stratigraphic and 1988. Biostratigraphie des miospores et des chitinozoair es du Systematic Palynology of the Toumaisian Rocks of Ireland. Silurien superieur et du Devonien dans le bassin d’ Illizi (S.E. The Geologocal Survey o f Ireland. Spetial Paper No 1: pp. 93. du Sahara Algerien). Geobios, 21: 381-391. Higgs, K., Dreesen, R., Dusar, M. & Streel, M., 1992. Palynostra- Butterworth, M. A. & Williams, R. W., 1958. The small spore flo­ tigraphy of the Toumaisian (Hastarian) rocks in the Namur ras of coals in the Limestone Coal Group and Upper Lime­ Synclinorium, West Flanders, Belgium. Review ofPalaeobot- stone Group of the Lower Carboniferous of Scotland. Royal any and Palynology, 72: 149-158. Society Edinbourg Transactions, 63: 353-92. Higgs, K , Avkhimovitch, V. I., Loboziak, S., Maziane-Serraj, N., Byvsheva, T. V., 1976. Zonation of spore complexes from Devo­ Stempień-Sałek, M. & Streel, M., 2000. Systematic study and nian -Carboniferous boundary deposits from the eastern part stratigraphic correlation of the Grandispora complex in the of the Russian platform. (In Russian). In: Byvsheva, T. V. Famennian of northwest and eastern Europe. Review of Pa- (ed.). Results of palynological researches of the Precam- laeobotany and Palynology, 112: 207-228. brium. Paleozoic and Mesozoic o f the USSR. Trudy VNIGRI, Hoffmeister, W. S., Staplin, F. L. & Malloy, R. E., 1955. Missis- 192: 67-93. sipian plant spores from the Hardinsburg Formation of Illinois Byvsheva, T. V., 1985. Spory iz otlozhenij tumejskogo i vizen- and Kentucky. Journal o f Paleontology’, 29: 372-399. skogo jarusov Russkoj plity. (In Russian). In: Menner, V. V. Kedo, G. I., 1957. Stratigraphy and spore-pollen complexes of the & Byvsheva, T. V. (eds). Atlas spor ipylcy neftegazonosnykh lower horizons of the Carboniferous of the Byelorussian SSR. tolshtch fanerozoja Russkoj i Turanskoi plit. Trudy VNIGNI (In Russian). Doklady Akademi Nauk USSR, 115: 1165-1168. Nedra: 80-158. Kedo, G. I., 1963. Spory tumejskogo jarusapripiatskogo progiba i Clayton, G., 1971. A Lower Carboniferous miospore assemblage ikh stratigrafitcheskije znatchenije. (In Russian). Paleontolo­ from the Calciferous Sandstone Measures of the Cock- gia i stratigrafija BBSSR, 4: 3-121. bumspath region of eastern Scotland. Pollen et Spores, 12: Kedo, G. I., 1974. Novyje vidy spor iz verkhnego devona pripyat- 577-600. skoj vpadiny. (In Russian). In: Golubtsov, V. K. & Manykin, Clayton, G. & Graham, J. R., 1974. Miospore assemblages from S. S. (eds), Spory paleozoja Belorussii. Izd. BelNIGRI, Mińsk: the Devonian Sherkin Formation of south-west County Cork, 3-72. Republic of Ireland. Pollen et Spores, 16: 565-588. Kedo, G. I. & Golubcov, V. K , 1971. Palinologitcheskij kriterij Clayton, G. & Tumau, E., 1990. Correlation of the Toumaisian dla opredelenia granicy dewona i karbona w Pripiatskoj miospore zonations of Poland and the British Isles. Annales vpadinie. (In Russian). Palinologia i Stratigrafia paleozoja. Societatis Geologorum Poloniae, 60: 45-58. BelNIGRI Mińsk: 5-34. Dadlez, R., 1978. Sub-Permian rock complexes in the Koszalin- Kedo, G. I., Nazarenko, A. M., Nekryata, N. C., Raskatova, L. G., Chojnice zone. (In Polish, English summary). Kwartalnik Sennova, W. F. & Tchibrikova, E. V., 1971. New spore spe­ Geologiczny, 22: 269-294. cies from Famennian deposits of the Pripyat Depression, cen­ Dadlez, R., 1990. Tektonika południowego Bałtyku. (In Polish, tral regions of Russian Platform, Volga-Urals oil and gas English summary). Kwartalnik Geologiczny, 34: 1-20. bearing region and Timan. (In Russian). In: Golubtsov, V. K. Dadlez, R., 1993. Pre-Cainozoic tectonic of the southern Baltic (ed.), Palinologicheskie Issledovania v Belorussii i drugikh Sea. Kwartalnik Geologiczny, 37: 431-450. raionakh SSSR, Nauka i Tekhnika, Minsk: 172-205. Dettman, M. E., 1963.Upper Mesozoic microfloras from South­ Kmiecik, H., 1986. Palynostratigraphy of the Carboniferous at the eastern Australia. Proceedings o f the Royal Society o f Victo­ margin of the Polish part of the east-European platform. Re­ ria, 77: pp. 148. view o f Palaeobotany and Palynology, 48: 327-345. Dolby, G.& Neves, R., 1970. Palynological evidence concerning Kmiecik, H., 1991. Wyniki badań sporowo-stratygraficznych kar­ the Devonian-Carboniferous boundary in the Mendips, Eng­ bonu pobrzeża i strefy brzeżnej Bałtyku pomiędzy Świnou­ land. C. R. 6 ćme Congrćs International Slratigraphie Geolo­ jściem a Kołobrzegiem. 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Frasnian to Famennian sediments partly dated by conodonts McGregor, D. C. & Camfield, M., 1982. Middle Devonian mio­ (Boulonnais), France. Review of Palaeobotany and Palynol- spores from the Cape de Bray, Weatherall, and Hecla Bay ogy, 34: 49-66. Formations of Northeastern Melville Island, Canadian Arctic. Loboziak, S. & Streel, M., 1988. Synthese palynostratigraphique Geological Survey o f Canada. Bulletin, 348: pp. 105. de l’intervalle Givetien-Famennien du Boulonnais (France). McGregor, D. C & Playford G., 1992. Canadian and Auustralian Le Devonien de Ferques/ Bas-Boulonnais (N. France), in Devonian spores: zonation and correlation. Geological Survey Brice D., (ed), Biostratigraphie du Paleozoique - Universite o f Canada. Bulletin, 438: 1-125. de Bretagne Occidentale, 7: 71-77. Milaczewski, L., 1979. Litologia i stratygrafia dewonu na Po­ Loboziak, S. & Streel, M., 1989. Middle-Upper Devonian Mio- morzu. (In Polish). 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Essai de synthese stra- Mortimer, M. G. & Chaloner, W. G., 1967. Devonian megaspores tigraphique et palynologique du systeme Devonian en Libya from the Wyboston borehole, Bedfordshire, England. Palae­ occidentale. Revue de L 'Institut Francois du Petrole, 31: ontology, 10: 189-213. 287-333. Naumova, S. N., 1953. Spore-pollen assemblages of the Russian Matyja, H., 1976. Biostratigraphy o f the Devonian-Carboniferous platform and their stratigraphie significance. (In Russian). passage beds from some selected profiles of NW Poland. Acta Trudy Instituta Geologicheskikh Nauk, Akademia Nauk USSR Geologica Polonica, 26: 489-539. 143, (Geologicheskaya seriya 60): 1-204. Matyja, H., 1993. Upper Devonian of Western Pomerania. Acta Nekryata, N. S., 1979. Zonal spore assemblages in the Pripyat De­ Geologica Polonica, 43: 27-94. pression intersalt deposits. (In Russian). Doklady Akakademi Matyja, H., 1998. 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Annales de la Societe Geologique de Bel­ boniferous (Dinantian) of the Spilmersford borehole, East Lo­ gique, 116: 249-263. thian, Scotland. Bulletin o f the Geological Survey o f Great Matyja, H., Tumau, E. & Żbikowska B., 2000. Lower Carbonifer­ Britain, 45: 73-79. ous (Mississippian) stratigraphy of northwestern Poland: Neves, R. & Owens, B., 1966. Some Namurian camerate mio­ conodont, miospore and ostracode zones compared. Annales spores from the English Pennines. Pollen et Spores, 8: 337— Societatis Geologorum Poloniae, 70: 193-217. 360. McGregor, D. C., 1960. Devonian spores from Melville Island, Neves, R., Gueinn, K. J., Clayton, G., Ioanides, N., Neville, R. S. Canadian Arctic Archipelago. Palaeontology, 3: 26-44. W. & Kruszewska K , 1973. Palynological correlation within McGregor, D. C., 1964. Devonian miospores from the Ghost River the Lower Carboniferous of Scotland and northern England. Formation, Alberta. 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Similitudes des assemblages de spores d’Europe, walled microphytoplancton of Devonian-Carboniferous d’Afrique du Nord et d’Amerique du Norde au Devonien ter­ boundary beds (Bakken Formation), Southern Saskatchewan: minal. Sciences Geologique Bulletin, 27: 25-38. a systematic and stratigraphic appraisal. Geological Surrey o f Streel, M. & Loboziak S., 1987. Nouvelle datation par miospore du Canada Bulletin, 445: pp. 107. Givetien-Frasnien des sediments non marins du sondage de Potonić, R., 1970. Synopsis der Gattungen der Sporae dispersae. Booischot (Basin de Campine, Belgique). Bulletin Societe V. Teil: Die Nachttrage zur alien Gruppen (Turmae). Beihefte beige Geologie, 96: 99-106. Geologischen Jahrbuch, 87: pp. 222. Streel, M., Higgs, K., Loboziak, S., Riegel, W. & Steemans, P., Potonie, R. & Kremp, G., 1954. Die Gattungen der palaozoischen 1987. Spore stratigraphy and correlation with faunas and flo­ Sporae dispersae und ihre Stratigraphie. 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and Palynology. 46: 311-254. Streszczenie Tumau. E., 1990. Poziomy sporowe famenu i tumeju z otworu wiertniczego Kowala 1. Kwartalnik Geologiczny, 34: 291— 304. TAKSONOMIA I STRATYGRAFIA MIOSPOROWA Tumau, E., 1995. Stratygrafia i korelacja utworów środkowego GÓRNEGO DEWONU I NAJNIŻSZEGO KARBONU dewonu Pomorza środkowego na podstawie analizy palinolo- POMORZA ZACHODNIEGO gicznej. (In Polish, English summary). Przegląd Geologiczny, 43: 211-214. Marzena Stempień-Sałek Tumau. E. & Racki G., 1999. Givetian palynostratigraphy and palynofacies: new data from the Bodzentyn Syncline (Holy W pracy określono metodą palinologiczną wiek formacji Cross Mountains, central Poland). Review of Palaeobotany człuchowskiej, klanińskiej, ilowców wapnistych z Sąpólna i dolnej and Paly nology, 106: 237-271. części piaskowców arkozowych z Gózdu wydzielanych dla gór­ Umnova, V. Т., 1971. On the Devonian/Carboniferous boundary nego dewonu i najniższego karbonu Pomorza Zachodniego (Fig. in the Central regions of the Russian Platform by palynologi- 1), oraz zaprezentowano lokalny, stratygraficzny schemat mio- cal data. (In Russian). Izviesta Akademi Nauk USSR, 4: 109— sporowy dla najwyższego dewonu i najniższego karbonu Pomorza 122. Zachodniego (Fig. 2). Posłużono się podziałem litostratygraficz- Utting, J., 1987. Palynology of the Lower Carboniferous Windsor nym Matyji (1993, 1998) i Lipca (Lipiec & Matyja, 1998) przed­ Group and Windsor-Canso boundary beds of Nova Scotia, stawionym na figurach 3 i 4. Biostratygrafia powyższych utwo­ and their equivalents in Quebec, New Bmnswick and New rów, oparta jest przede wszystkim na badaniach konodontów, a Founland. Geological Survey o f Canada, Bulletin, 374: 1-93. także małżoraczków, brachiopodów oraz miospor. Van der Zwan, C. J., 1979. Aspects of Late and Early Carbonifer­ Stosowany dotychczas schemat miosporowy dla Pomorza ous palynology of southern Ireland; I. The Cyrtospora cris- Zachodniego (Tumau, 1978,1979) jest, przynajmniej dla pewnych tifer morphon. Review o f Palaeobotany and Palynology, 28: interwałów, mało szczegółowy, dlatego też wprowadzono podpo- 1- 20 . działy dla istniejących już zon, a także wydzielono nowe zespoły i Van der Zwan, C. J„ 1980. Aspects of Late Devonian and Early zony miosporowe w osadach franu i dolnego famenu (por. Fig. 2). Carboniferous palynology of southern Ireland; III, Palynol­ Zbadane materiały pochodziły z 9 otworów wiertniczych (por. Fig. ogy of Devonian-Carboniferous transition sequences with 1). Z wyjątkiem otworów wiertniczych Rzeczenica 1 i Chmielno 1 special reference to the Bantry Bay area, Co. Cork. Review o f (Tumau, 1978, 1979, Matyja et al., 2000) utwory z badanych wier­ Palaeobotany and Palynology, 30: 165-286. ceń nie były do tej pory opracowywane pod kątem palinologicz- Van Veen, P. М., 1981. Aspects of late Devonian and early Car­ nym. Utwory starsze, które należą do dewońskiej formacji człu­ boniferous palynology of southern Ireland; IV, Morphologi­ chowskiej, stały się obiektem zainteresowań palinologicznych po raz pierwszy. cal variation within Diducites a new form genus to accomo­ date camerate spores. Review ofPalaebotany and Palynology’, Zespoły gatunków miospor wskaźnikowych dla zon lokal­ 31:261-287. nego schematu miosporowego dla najwyższego dewonu i najniż­ Van Veen, P. M. & Van der Zwan, C. J., 1978. The Devonian-Car­ szego karbonu Pomorza Zachodniego zilustrowano na figurze 5. Na podstawie pierwszych pojawień gatunków wskaźnikowych, boniferous Transition sequence in southern Ireland: Integra­ schemat ten można w części korelować ze schematem miosporo- tion of Paleogeography and Palynology. Palinologia, 1: 469- wym przyjętym dla Europy Zachodniej (Streel et al., 1987; Higgs 479. et al., 1988) i Wschodniej (Avkhimovitch, 1993; Avkhimovitch et Winslow, M. R., 1962. Plant spores and other microfossils from al., 1993b) co przedstawiono na figurze 6. Upper Devonian and Lower Mississippian rocks of Ohio. U. Zbadane utwory są dość szczegółowo datowane na podstawie S. Geology Survey, 364: 93. konodontów (poziomypunctata - dolna crenulata). Miospory i ko- Żbikowska, В., 1992. Entomozoaceans (Ostracoda) from the Up­ nodonty pochodzą z tych samych profili i tych samych lub podob­ per Devonian and Lower Carboniferous of Western Pomera­ nych przedziałów głębokości (por. Figura 3). Fakt ten umożliwia nia (In Polish). Przegląd Geologiczny, 40: 612. datowanie granic wyróżnionych zon miosporowych. Próba kore­ Żelichowski, А. М., 1983. Carboniferous of Western Pomerania lacji stratygraficznego lokalnego schematu miosporowego i zo- (In Polish, English summary). Przegląd Geologiczny, 31 (6): nacji konodontowej zilustrowana została na figurze 4. 356-354. Potwierdzono obecność luki stratygraficznej na granicy de- Żelichowski, А. М., 1987. Sedimentation and framework of the won/karbon (Fig. 6), obejmującej brakujące zony miosporowe: LN basin (In Polish, English summary). In: A. Raczyńska (ed.), i VI. Geological stmcture of the Pomeranian Swell and its base­ W części systematycznej opisano 31 gatunków miospor ment. Prace Instytutu Geologicznego, 119, 48-51. wyznaczających granice zon miosporowych oraz dotychczas nie opisanych z Pomorza Zachodniego. Gatunki te zilustrowane są na figurach 7-10. Listę wszystkich oznaczonych miospor zamiesz­ czono w dodatku (Appendix 1). Dokumentacja ilościowa i jakościowa, oraz dotycząca głębokości pobrania pozytywnych prób na miospory przedstawiona jest w dodatku (Appendix 2).