 1. INTRODUCTION Pennsylvanian (late Carboniferous) coal-bearing deposits have been known in north-western Turkey in the vicinity of Zonguldak since the early 19th century (SCHLEHAN, 1852; SPRATT, 1877), and there were a number of early studies on the stratigraphy, including the plant biostratigraphy, no- tably by ZEILLER (1896, 1899) and RALLI (1896). For many years, coal mining was on a relatively small scale and mainly by foreign companies, and it was not until the mines started to be nationalised in the mid-1930s (GÜNEY, 1967) that there was a marked expansion in geological studies (RALLI, 1933; HARTUNG, 1937; JONGMANS, 1939; GRANCY, 1939; ARNI, 1939); some background comments to these investigations can be found in WAGNER & VAN AMEROM (1995) and WAGNER (1997). Plant biostratig- raphy played a pivotal role in these studies, with numerous published species lists and in some cases specimens illus- trated. After the 1939–1945 war, interest in the palaeobotany of these coal-bearing beds was continued mainly by JONG- MANS (1955), and two of his students, EGEMEN (1958, 1959) and WAGNER (in STOCKMANS, 1962, p. 664, fig. 6). WAGNER (1984) made some brief comments on the Turkish data in his seminal biostratigraphical analysis of Carboniferous Euramerican floras, and subsequently (in KEREY et al., 1986) he made a more in depth analysis and figured several plant fossils. The stratigraphical sequence in the Zonguldak – Amasra Coal Basin has potentially much significance. If, as sug- gested by WAGNER (in STOCKMANS, 1962), there is an essentially complete succession of Namurian and Westphal- ian strata here, it would potentially provide a key link be- tween the successions of the Caucasus and Donets, and the rest of Variscan Euramerica (sensu CLEAL et al., 2010). Moreover, CLEAL et al., (2010, 2011) have suggested that the progressive breakdown in the coal swamp biome in Eura- merica during Westphalian times may have been initiated in the easternmost part of the area and a better understanding of how the Zonguldak – Amasra coal-bearing succession re- lates biostratigraphically to neighbouring areas will clearly be critical to understanding this major change in biotas and habitat. This paper will review the available published data on the distribution of plant macrofossils in the Zonguldak – Amasra Coal Basin and discuss the implications for the stratigraphic age of these deposits. Ab sTRA CT The Zonguldak – Amasra Coal Basin in north-western Turkey has Carboniferous terrestrial deposits ranging in age from Arnsbergian to late Asturian or possibly early Cantabrian. They yield macrofloras that allow detailed biostrati- graphical correlations with sequences in Europe. These correlations suggest there are substantial gaps in the Zongul- dak – Amasra succession, with middle to upper Namurian, upper Langsettian, Duckmantian and lower Asturian stra- ta apparently being missing. This in turn suggests the area was subjected to significant tectonic instability during Pennsylvanian (late Carboniferous) times and that this might have been instrumental in initiating the progressive change in composition and eventual collapse of the coal swamp biome across Variscan Euramerica during Westphal- ian times. Keywords: Palaebotany, Biostratigraphy, Pennsylvanian, Zonguldak-Amasra Coalfield A reappraisal of the Carboniferous macrofloras of the Zonguldak – Amasra Coal Basin, north-western Turkey  Christopher J. Cleal1 and Isabel M. van Waveren2 1 Department of Biodiversity & Systematic Biology, National Museum Wales, Cathays Park, Cardiff CF10 3NP, UK; (chris.cleal@museumwales.ac.uk) 2 Naturalis, P.O. Box 9517, 2300 RA Leiden, The Netherlands; (Isabel.vanWaveren@ncbnaturalis.nl) doi: 104154/gc.2012.19 Geologia CroaticaGeologia Croatica Geologia Croatica 65/3 283–297 7 Figs. 4 Tabs. Zagreb 2012 Geologia Croatica 65/3Geologia Croatica 284 2. GEOLOGICAL bACKGROUND The Zonguldak – Amasra Coal Basin is the primary source of hard coal in Turkey, with proven reserves of 1.1 x 109 tonnes (İNANER & NAKOMAN, 2004). During the 19th century, this area was usually referred to as the Heraclée or Heraclea Coal Basin, after the port with the current written name of Ereğli. Nowadays, however, it is usually referred to as the Zonguldak – Amasra Coal Basin, after its two main coal mining towns (Fig. 1), and this is the name that will be used in this paper. The basin was formed on part of the Pontide Block, a Gondwana-derived microcontinent that had docked with Baltica probably by Ordovician times (KALVODA & BÁBEK, 2010). The Pontides formed a passive margin along this part of Laurussia on which an essentially regressive se- quence was deposited, with Ordovician – Silurian marine clastics, Middle Devonian – Mississippian shallow marine limestones, and uppermost Mississippian and Pennsylvanian terrestrial deposits (YANEV et al., 2006). The Carbonifer- ous terrestrial deposits, which lie conformably on the Viséan marine limestones of the Yılanlı Formation, are about 2100 m thick and were derived from the Laurussian landmass to the north (KEREY, 1985). Based on divisions introduced by RALLI (1896, 1933) this terrestrial interval is usually di- vided into four formations, as summarised in Table 1. 3. CHRONOsTRATIGRAPHY AND bIOsTRATIGRAPHY Late Carboniferous biotas were characterised by strong global provincialism, which was largely the result of latitudinal cli- matic zones (WAGNER, 1994). This has caused major prob- lems with establishing global biostratigraphic correlations and consequently with developing a global chronostratigraphic scheme. Recent improvements in the resolution of radiomet- ric dating (DAVYDOV et al., 2010; SCHMITZ & DAVY- DOV, 2012; WATERS & CONDON, 2012) are now offering the potential of circumventing these biostratigraphical prob- lems and a practical global chronostratigraphy for the Car- boniferous System may appear in the foreseeable future. For now, however, the currently accepted IUGS global chro- nostratigraphy for the Carboniferous (e.g. HECKEL & CLAY TON, 2006) remains a theoretical aim rather than a practical tool for the upper part of the system, at least out- side of the low-latitude marine realm where the boundary stratotypes (GSSPs) of the stage boundaries are located; there remain, for instance, discrepancies between the bio- stratigraphical (e.g. KULLMANN et al., 2007) and radio- metric (DAVYDOV et al., 2010; WATERS & CONDON, 2012) evidence for locating accurately the base of the IUGS Moscovian Stage within the palaeotropical terrestrial se- quences. Figure 1: Location of the Zongul- dak – Amasra Coal Basin. The up- per map shows the main localities in the basin, with a small inset showing their position relative to the Black Sea (redrawn from JONGMANS, 1955). Bottom left is a simplified geological map of the Zonguldak Coalfield (redrawn from GÜNEY, 1967). Bottom right is a simplified geological map of the Amasra Coalfield (redrawn from TOKAY, 1962). Cleal and van Waveren: A reappraisal of the Carboniferous macrofloras of the Zonguldak – Amasra Coal Basin, north-western Turkey Geologia Croatica 285 DIX (1934, 1937) developed the first biostratigraphical scheme for Carboniferous plant macrofossils using biozones, (in this case assemblage zones), that were defined independ- ently of lithostratigraphy (BUREK & CLEAL, 2005). How- ever, DIX (1934, 1937) was rather ahead of her time and her scheme was not widely adopted outside of Britain. It was not until WAGNER (1984) developed a comparable scheme to DIX’s that Carboniferous plant biostratigraphy took on a modern aspect. Like DIX’s scheme, WAGNER’s was based on biozones determined from range charts that showed the stratigraphical distribution of the species. This time, how- ever, the data on which the zones were established were taken from across Europe and North America, and so poten- tially the scheme should have wider application than DIX’s. The zones were concurrent range zones although in a number of cases the boundary between zones was effectively made to coincide with chronostratigraphical stage / substage boun- daries. According to WAGNER (1984) this made sense as many of the substage boundaries had been defined using macrofloral indices. The Asturian and stratigraphically higher substages were indeed defined mainly using macro- floral indices as the faunal data from these strata tend to be limited and often equivocal (e.g. BOUROZ et al., 1972; LAVEINE, 1977; WAGNER, 1998). However, the strati- graphically lower stages and substages were mainly defined on eustatic marine bands and/or changes in the faunas (WA- TERS, 2011), which tended to operate independently of the vegetation changes. Consequently, by forcing the zonal boundaries to coincide with the substage boundaries, parts of the WAGNER (1984) biostratigraphical scheme did not reflect the actual pattern of change in the macrofloras as well as DIX’s (1934, 1937) scheme. Nevertheless, WAGNER’s (1984) scheme has become widely adopted in the literature. CLEAL (1991) modified several aspects of WAGNER’s (1984) scheme. Greater emphasis was given to what defined the boundaries, rather than the content of the zones, there- fore changing them into interval zones. Also, a set of sub- zones was introduced based on some of the temporal changes in the coal swamp vegetation not reflected in the WAGNER (1984) scheme, notably those in the middle Langsettian, mid- dle Bolsovian and upper Asturian substages. This more de- tailed approach helped maintain the integrity of the widely used WAGNER (1984) biozones, whilst also incorporating some of the more “natural” features of the DIX (1934) scheme. 4. PALAEObOTANY The following analysis will mainly focus on the biostratig- raphy and (for the Kozlu Formation) the species diversities of the plant fossils. As is normal in palaeobotanical studies, the fossils are named as fossil-taxa (sensu CLEAL & THOM AS, 2010a,b, McNEILL & TURLAND, 2011), which refer to re- mains of particular parts of the plant rather than whole or- ganisms. Using a similar approach to that advocated by CLEAL (2005, 2007) only the fossil-taxa for one plant part are listed for each plant group, mainly those of the foliage, except for the lycopsids in which the stem / bark fossil-taxa are given. 4.1. Alacaağzı Formation Macrofloras are generally poor in this interval, and many of those that have been reported are difficult to place accurately in a stratigraphical context. However, ZEILLER (1899, p. 83), JONGMANS (1955, p. 58) and KEREY et al. (1986, p. 205) have reported plant fossils from several localities in the Zonguldak Coalfield and small outcrops to the west (Ala- caağzı, Kireçlik, Teflenli). These plant beds all immediately overlie marine limestones presumably of the Kokaksu “Member” and so were probably in the Gökgöl “Member” (see Table 1). These macrofloras are all similar and are sum- marised in Table 2. Fig. 2 shows the ranges of the stratigraphically most in- structive species in the Alacaağzı Formation macrofloras plotted against the WAGNER (1984) / CLEAL (1991) bio- zones. This clearly indicates that the Alacaağzı Formation macrofloras belong to the Lyginopteris stangeri Zone, and probably the lower part of that zone. Although not included in the taxonomic lists in Table 2, JONGMANS (1955) re- peatedly mentioned Mesocalamites stems from these beds, Table 1: Lithostratigraphic divisions of the Zonguldak – Amasra Coal Basin, based on KEREY (1982) and KEREY et al. (1986). Formation Member Facies Palaeoenvironment Thickness Stratigraphical age Kızıllı Alternating coarse and fine clastic deposits; some thin coals, and red beds develop towards top of formation Braided stream system in an intra-montane setting, becoming better drained towards top of section 280 m Late Westphalian Karadon Alternating coarse and fine clastic deposits; some coals, mainly in the lower part of the formation Braided stream and alluvial fan 500 m Middle Westphalian Kozlu Dılaver Alternating coarse and fine clastic deposits, with abundant coals Fluvio-deltaic, floodplain 300–750 m Early Westphalian Kılıç Mainly lacustrine Alacaağzı Asma Mainly sandstones Terrestrial 600 m Namurian Tarlaağzi Mixed coarse and fine clastics Shallow marine Gökgöl Mixed coarse and fine clastics, with thin coals Mainly terrestrial Kokaksu Limestones and clastic deposits Mainly shallow-marine Geologia Croatica 65/3Geologia Croatica 286 which WAGNER (1984) again suggested is a characteristic taxon of the L. stangeri Zone. Similar L. stangeri Zone mac- rofloras have been reported from the upper Rakovski Forma- tion in the Dobrudzha Coal Basin, Bulgaria (KULAKSAZOV & TENCHOV, 1973; TENCHOV, 2004) and the lower Os- trava Formation in Upper Silesia, Czech Republic (PUR- KYŇOVÁ, 1970). In western Europe, such floras are poorly documented, although there are records from the Upper Limestone Formation in Scotland (WALTON et al., 1938). According to WAGNER (1984), this zone indicates a strati- graphical position in the lower Namurian Stage (Arnsbergian Substage) and thus a latest Mississippian age. In the Amasra area to the east, the Alacaağzı Formation is more marine in character (KEREY, 1982; KEREY et al., 1986) and plant remains are consequently rarer. However, low diversity macrofloras comparable to those of the Gökgöl “Member” have been reported from near Güllük and Dökök (CHARLES, 1931; JONGMANS, 1955). WAGNER (1984) suggested there are even older mac- rofloras from the Zonguldak area, belonging to the Neurop- teris antecedens Zone, which would indicate a late Viséan or earliest Namurian age. WAGNER referenced JONG- MANS (1955) for this opinion, but there is nothing recorded in this latter paper to support such a view. Since the Gökgöl “Member” represents the stratigraphically oldest extensive terrestrial deposits in the coalfield, older macrofloras from here would seem to be unlikely. WAGNER (in STOCKMANS, 1962; 1984) also sug- gested that younger, “Namurian B” macrofloras (i.e. belong- ing to the Lyginopteris larischii Zone) occurred in the Zon- guldak area based on evidence in JONGMANS (1955). From the species mentioned by WAGNER (in STOCKMANS, 1962) as suggesting a “Namurian B” age, it is likely that he was referring to the macroflora from north of the Kokaksu Valley listed by JONGMANS (1955, p. 58). This macroflora is very similar to those found in the overlying Koslu Forma- tion except for the presence of rare sphenophytes compara- ble with Asterophyllites unguis JONGMANS & GOTHAN and Asterophyllites heimansii JONGMANS & GOTHAN, which are only known from Namurian strata (JOSTEN, 1983 and references cited therein). However, the robustness of Table 2: Macrofloras from the Alacaağzı Formation (Gökgöl “Member”) in the vicinity of Zonguldak and the small outcrops to the west. 1 2 3 4 5 6 7 8 Sublepidodendron robertii (NATHORST) CHALONER X X X X X X X Eleutherophyllum mirabile (STERNBERG) STUR X X X Sphenophyllum tenerrimum ETTINGSHAUSEN X X X X X Pecopteris aspera BRONGNIART ? X ? X Alloiopteris quercifolia (GÖPPERT) POTONIÉ X X Sphenopteris elegans BRONGNIART X X X X X X Sphenopteris dissecta BRONGNIART ? ? ? ? ? X Lyginopteris distans (STERNBERG) CLEAL, comb. nov. X X X X X Lyginopteris fragilis (BRONGNIART) PATTEISKY X X Lyginopteris dicksonioides (GÖPPERT) NOVIK X Cardiopteridium nanum (EICHWALD) WALTON X X X X X Adiantites oblongifolius GÖPPERT ? ? X X Figure 2: Stratigraphic ranges of the key macrofloral taxa found in the Alacaağzı Formation, plotted against the WAGNER (1984) / CLEAL (1991) biozonal scheme. Ranges mainly as given by WAGNER (1984). Localities: 1 - Near Kirat and Tchatal-Déré, Zonguldak (ZEILLER, 1899) 2 – Kokaksu Valley, Zonguldak (JONGMANS, 1955) 3 – Ali-Mollah Seam, Kiliç Valley, Zonguldak (ZEILLER, 1899; JONGMANS, 1955) 4 – Kilimli tunnel, Zonguldak (JONGMANS, 1955) 5 – Gökgöl section, Üzülmez Deresi, Zonguldak (KEREY et al., 1986) 6 – Kireçlik mines (various coals) (ZEILLER, 1899; JONGMANS, 1955) 7 – Alacaağzı (JONGMANS, 1955) 8 – Teflenli (ZEILLER, 1899) Cleal and van Waveren: A reappraisal of the Carboniferous macrofloras of the Zonguldak – Amasra Coal Basin, north-western Turkey Geologia Croatica 287 Figure 3: Stratigraphic distribution of the macrofloral species of the Kozlu Formation plotted against the lithostratigraphic sequence given by NAKOMAN (1977) (see also KEREY, 1985 and KEREY et al., 1986). Black dots on the range bars designate recorded occurrences of species. Geologia Croatica 65/3Geologia Croatica 288 these species as stratigraphical indices for the middle Namu- rian Stage remains unproven and the identifications were anyway only given with a “cf.” At the moment it seems more likely that these Kokaksu Valley macrofloras originated from the Koslu Formation. KEREY et al. (1986) mentioned lycopsid remains from the Asma “Member” at the top of the formation (e.g. Lepi- dodendron rimosum STERNBERG) but these are biostrati- graphically uninformative. 4.2. Kozlu Formation This is the main productive interval of the basin for coal and there have been many workings especially in the vicinity of Zonguldak. ZEILLER (1899), JONGMANS (1955), EGE- MEN (1959) and KEREY et al. (1986) have provided strati- graphical records of the Kozlu Formation macrofloras from the Zonguldak mines, from which it has been possible to es- tablish a detailed biostratigraphical model (Fig. 3). A total of 76 species have been reported from the forma- tion. Excluding the stratigraphically highest and lowest two macrofloras (to help remove the edge effect inherent when using through-range data – see FOOTE, 2000 and CLEAL, 2007 for further discussion on edge effect in such analyses) estimated landscape-scale species diversities (i.e. species di- versities within the area of the coalfield) vary from 33 to 56 species (mean 43.2, s. d. 5.0) and local-scale diversities (i.e. species diversities observable at a particular locality) from 3 to 37 species (mean 11.2, s. d. 7.9). This is essentially sim- ilar to the diversities recorded by CLEAL (2007) in the Lang- settian Substage in South Wales (landscape diversities mean 38.5, s. d. 5.6; local-scale diversities 13.8, s. d. 5.6). Very similar local-scale diversities were also reported by WING & DIMICHELE (1995) from various Pennsylvanian macro- floras from North America. Although there seems to be some variation in the bios- tratigraphical distribution of the species through the succes- sion, this is mainly due to 24 singleton species. Of the 52 species that occur at more than one stratigraphical level, 39 (75 % of the non-singleton species) range through virtually the entire formation, from the Kürtşerif, Hacıpetro or Çay coal seams near the base to the Büyük or stratigraphically higher seams at the top. Nearly all of the species that have not been recorded to range through the entire formation are lycopsids and herbaceous, sphenopteroid ferns, which are all rare and therefore subject to potential taphonomy-induced sampling problems. There appears, therefore, to be little sig- nificant change in the macrofloras through the formation. When plotted against the biozonal scheme of WAGNER (1984), the Kozlu Formation macrofloras correspond to the Lyginopteris hoeninghausii Zone (Fig. 4). CLEAL (1991) and CLEAL & THOMAS (1994) argued that the zone could be divided into a lower, Neuralethopteris jongmansii Sub- zone and an upper, Laveineopteris loshii Subzone, based on the appearance of several taxa, notably Laveineopteris loshii (BRONGNIART) CLEAL et al., (date) Laveineopteris tenu- ifolia (STERNBERG) CLEAL et al. (1990) Neuropteris het- erophylla BRONGNIART and Lobatopteris miltonii (ARTIS) WAGNER. This change can be recognised in Britain (CLEAL, 2005, 2007), northern France (LAVEINE, 1987) and north- ern Germany (JOSTEN, 1991), where it occurs about one- third of the way up the Langsettian Stage. Since none of these species have been convincingly documented from the Kozlu Formation, it seems reasonable to conclude that this interval belongs to the N. jongmansii Subzone and is thus early Lang- settian in age. EGEMEN (1959) reported L. miltonii from Kozlu Formation macrofloras from Çatalldere and Viran- cıkdere, but he stated that the specimens were poorly pre- served and none were illustrated. JONGMANS (1955) also mentioned L. miltonii from the Leonodas and Sulu seams, but with no comment or justification for the identifications. Significantly, ZEILLER (1899) stated that this species was absent from the Kozlu Formation. A Langsettian age for the Kozlu Formation is in general accord with the views of JONGMANS (1955) and KEREY et al. (1986). These latter authors suggested that the lower part of the formation might range down into the Yeadonian (“Namurian C”) Substage but without giving evidence in support of this idea. The fact that Lyginopteris hoeninghausii and Mariopteris dernoncourtii range down into the lowest part of the Koslu Formation (Fig. 4) strongly suggests that the formation does not in fact extend below the base of the Figure 4: Stratigraphic ranges of the key macrofloral taxa found in the Ko- zlu Formation (based mainly on records in JONGMANS, 1955) plotted against the WAGNER (1984) / CLEAL (1991) biozone scheme. Ranges main- ly as given by WAGNER (1984), CLEAL & THOMAS (1994) and CLEAL (2005, 2007). Cleal and van Waveren: A reappraisal of the Carboniferous macrofloras of the Zonguldak – Amasra Coal Basin, north-western Turkey Geologia Croatica 289 Table 3: Macrofloras from the Karadon Formation. 1 2 3 4 5 6 7 8 9 10 Lepidodendron aculeatum STERNBERG X Lepidodendron obovatum STERNBERG auct. X X X Bothrodendron minutifolium BOULAY X Sigillaria ovata SAUVEUR X Annularia radiata (BRONGNIART) STERNBERG X X X X X X X Annularia rallii (ZEILLER) X X X Annularia spinulosa STERNBERG X X X X Annularia sphenophylloides (ZENKER) GUTBIER X X X X Asterophyllites charaeformis (STERNBERG) UNGER ? X X Asterophyllites equisetiformis BRONGNIART X X X X Sphenophyllum emarginatum (BRONGNIART) X X X X X Sphenophyllum cuneifolium (STERNBERG) ZEILLER X X X X X X X X Sphenophyllum majus (BRONN) BRONN X ? ? Alloiopteris sternbergii (ETTINGSHAUSEN) POTONIÉ X X Alloiopteris coralloides GUTBIER ? X X Oligocarpia brongniartii GÖPPERT X Renaultia chaerophylloides (BRONGNIART) ZEILLER X X Renaultia crepinii (STUR) GOTHAN X X Renaultia footneri (MARRATT) BROUSMICHE X X Sphenopteris limai ZEILLER X X X X Pecopteris plumosa (ARTIS) BRONGNIART X Lobatopteris miltonii (ARTIS) WAGNER X X Eusphenopteris neuropteroides (BOULAY) NOVIK X ? Eusphenopteris nummularia (GUTBIER) NOVIK X X X ? Eusphenopteris striata (GOTHAN) NOVIK ? ? Mariopteris dernoncourtii ZEILLER X X Mariopteris nervosa (BRONGNIART) ZEILLER X X X X X X Mariopteris sauveurii (BRONGNIART) ZEILLER X Mariopteris soubeiranii ZEILLER X Palmatopteris furcata (BRONGNIART) POTONIÉ X ? ? ? ? Alethopteris lonchitica STERNBERG X X X X X X Alethopteris davreuxii (BRONGNIART) ZEILLER X Lonchopteridium karvinense (PURKYŇOVA) KEREY et al. X Reticulopteris muensteri (EICHWALD) GOTHAN X X X X X X Macroneuropteris scheuchzeri (HOFFMANN) CLEAL et al. X X X X X X X Laveineopteris rarinervis (BUNBURY) CLEAL et al. X X X X X Laveineopteris tenuifolia (STERNBERG) CLEAL et al. ? ? ? ? X Paripteris spp. X X X X Linopteris neuropteroides (GUTBIER) ZEILLER X X X X X X X X Linopteris obliqua (BUNBURY) ZEILLER X X X X X X X Cordaites principalis (GERMAR) GEINITZ X X ? Localities: 1 – Taşkesen (JONGMANS, 1955) 2 – Çatalağzı, Gelik Valley (ZEILLER, 1899; JONGMANS, 1955) 3 – Along road to Çaycuma (JONGMANS (1955) 4 – Behind primary school garden, Temmuz Mevkii, Zonguldak (KEREY et al., 1986) 5 – East of Söğütözü (JONGMANS, 1955) 6 – East of Dereustudere, near Söğütözü (JONGMANS, 1955) 7 – Kilçharman, near Söğütözü (JONGMANS, 1955) 8 – North of Karatepe, , near Söğütözü (JONGMANS, 1955) 9 – Between Başköy and Ömerköy, near Söğütözü (JONGMANS, 1955) 10 – Özkem köy, near Söğütözü (JONGMANS, 1955) Geologia Croatica 65/3Geologia Croatica 290 Langsettian L. hoeninghausii Zone (in particular, compare with the range of L. hoeninghausii given in PATTEISKY, 1957). Plant fossils in what was probably the Kozlu Formation were also reported by JONGMANS (1955) from several lo- calities in the Azdavay and Amasra Coalfields. These mac- rofloras are all essentially the same as those found in the Zonguldak Coalfield, including Lyginopteris baeumleri, L. hoeninghausii, Karinopteris acuta and Paripteris gigantea, and lacking Laveineopteris spp., Neuropteris heterophylla and Lobatopteris miltonii. Despite the reported absence of neuralethopterids, these macrofloras clearly belong to the Langsettian L. hoeninghausii Zone and probably the lower subzone. 4.3. Karadon Formation Although the Karadon Formation occurs across the Zongul- dak – Amasra Coal Basin, there has not been the same level of systematic collecting of plant fossils compared with the Kozlu Formation (as discussed above). They are best known from the Gelik Valley near Zonguldak; ZEILLER (1899) and JONGMANS (1955) mention a plant bed that outcrops at several localities including Taşkesen and Çatalağzı that has yielded a diverse macroflora. Diverse Karadon macrofloras have also been found in the vicinity of the villages of Azda- vay and Söğütözü. Table 3 summarises the most diverse ma- crofloras that have been reported to date from this formation. We do not know the relative stratigraphical positions of the various plant-bearing localities within the Karadon For- mation and so it is impossible to develop the same type of biostratigraphical model as we have for the Kozlu Forma- tion (as shown in Fig. 3). However, there is no obvious dif- ference between any of the assemblages in the Karadon For- mation except for how many species each contains; they may, therefore, all be treated together. If the ranges of the most widespread and abundant of the Karadon Formation species are plotted against the zones of the WAGNER (1984) / CLEAL (1991) scheme (Fig. 5) it indicates that they belong to the L. rarinervis Subzone. Similar macrofloras are wide- spread in Variscan Euramerica, having been reported from the Makedonka Formation in the Dobrudzha Coal Basin, Bulgaria (CLEAL et al., 2004), the Lembeck Formation in northern Germany (JOSTEN, 1991), the lower Pennant For- mation in South Wales (CLEAL, 2007) and the South Bar Formation in the Canadian Maritimes (BELL, 1938); for a further discussion on the distribution of this subzone see CLEAL et al., 2010). In western Europe, the zone tends to range from about the level of the Cambriense Marine Band up to the base of the Asturian Substage, and so is regarded as an index for the upper Bolsovian Substage. There is no evidence of Lonchopteris rugosa or lower Paripteris linguaefolia zone floras in the Karadon Forma- tion. To the south of Zonguldak, at exposures along the road to Çaycuma and at Temmuz, JONGMANS (1955) and KE- REY et al. (1986) reported similar macrofloras, but which lack L. rarinervis and include Eusphenopteris obtusiloba (BRONGNIART) NOVIK, and which they interpreted as Duckmantian in age. In part justification for this opinion, KEREY et al. (1986, pl. 10, fig. 1) figured a specimen from here as E. obtusiloba. This interpretation depends on the ac- cepted stratigraphical range of the latter species, which else- where does not normally range above the early Duckmantian Lonchopteris rugosa Zone (VAN AMEROM, 1975). The specimen figured by KEREY et al. (1986) does not show their surface features very clearly, but the pinnules are more deeply incised than is normal for E. obtusiloba and resemble more closely Eusphenopteris striata (GOTHAN) NOVIK. This would be more compatible with its co-occurrence with Macroneuropteris scheuchzeri, which does not normally range below the late Duckmantian Neuropteris semireticu- lata Subzone. It is likely, therefore, that these macrofloras are at the oldest, late Duckmantian and may in fact be as young as late Bolsovian. JONGMANS (1955) reported another small macroflora from the Karadon Formation at Taarlağzi, east of Amasra, which includes Sphenophyllum cuneifolium, Eusphenopteris cf. neuropteroides (BOULAY) NOVIK, Linopteris neurop- teroides and Cordaites palmaeformis GÖPPERT. JONG- MANS suggested a Duckmantian age, but none of these spe- cies is diagnostic of the Lonchopteris rugosa Zone and the quoted assemblage is equally compatible with the Paripteris linguaefolia Zone. Figure 5: Stratigraphical ranges of the key macrofloral taxa found in the Karadon Formation, plotted against the WAGNER (1984) / CLEAL (1991) biozone scheme. Ranges mainly as given by WAGNER (1984), CLEAL & THO- MAS (1994) and CLEAL (2005, 2007). Cleal and van Waveren: A reappraisal of the Carboniferous macrofloras of the Zonguldak – Amasra Coal Basin, north-western Turkey Geologia Croatica 291 Table 4: Macrofloras from the Kızıllı Formation. 1 2 3 4 5 6 7 8 9 10 Bothrodendron minutifolium BOULAY X Lepidodendron aculeatum STERNBERG X Lepidodendron obovatum STERNBERG auct. X X X Lepidodendron ophiurus BRONGNIART X Sigillaria rugosa BRONGNIART X Sigillaria tessellata BRONGNIART X X Asolanus camptotaenia WOOD X Annularia radiata BRONGNIART X ? X X Annularia sphenophylloides (ZENKER) GUTBIER X X X X X X X X X Annularia spinulosa STERNBERG ? X ? X X X X X Asterophyllites equisetiformis BRONGNIART X X X X X Sphenophyllum emarginatum BRONGNIART X X X X X X X X X X Sphenophyllum majus (BRONN) BRONN X X X ? X Sphenophyllum oblongifolium (GERMAR & KAULFUSS) X X X X Urnatopteris tenella (BRONGNIART) KIDSTON X Sphenopteris limai ZEILLER ? Sphenopteris vuellersii STUR X Hymenophyllites quadridactylites (GUTBIER) KIDSTON X Renaultia rotundifolia (ANDRÄ) ZEILLER X X X Renaultia footneri (MARRATT) BROUSMICHE X ? Zeilleria delicatula (STERNBERG) KIDSTON X Pecopteris plumosa (ARTIS) BRONGNIART X X X X X X Lobatopteris vestita auct. X X X X X X X X Acitheca polymorpha (BRONGNIART) SCHIMPER X X Ptychocarpus unitus (BRONGNIART) ZEILLER X X X X X X X Cyathocarpus sp. X X X X X X X Eusphenopteris neuropteroides (BOULAY) NOVIK ? X ? ? X Mariopteris nervosa (BRONGNIART) ZEILLER X X X X Karinopteris daviesii (KIDSTON) BOERSMA ? Palmatopteris alata (BRONGNIART) POTONIÉ ? ? Sphenopteris coemansii STUR X Dicksonites plukenetii (STERNBERG) STERZEL X X X X X X Alethopteris lonchitica STERNBERG X X ? X X X Alethopteris ambigua LESQUEREUX X X X X Alethopteris pseudograndinioides ZODROW & CLEAL X X ? Alethopteris pontica ZEILLER X Lonchopteris rugosa BRONGNIART X ? Callipteridium jongmansii (BERTRAND) WAGNER X ? X X ? ? ? Callipteridium armasii (ZEILLER) WAGNER X ? X X X X ? ? Neuropteris ovata HOFFMANN X X X X X X X X X X Odontopteris reichiana GUTBIER X ? ? ? ? Odontopteris cantabrica WAGNER ? Reticulopteris muensteri (EICHWALD) GOTHAN X X X X X X Macroneuropteris scheuchzeri (HOFFMANN) CLEAL et al. X X X X X X X X X X Laveinopteris rarinervis (BUNBURY) CLEAL et al. X X X X X Linopteris obliqua (BUNBURY) ZEILLER X X X X X X X X X Linopteris neuropteroides (GUTBIER) ZEILLER X X X X X Cordaites spp. X X X X X Localities: 1 - Tarlaağzi, Amasra (ZEILLER 1899; Charles, 1931; JONGMANS, 1955) 2 – Grancy, Pelitova Basin (JONGMANS, 1955) 3 – Azdavavy (JONGMANS, 1955) 4 – Azdavavy, “Rayon C” (JONGMANS, 1955) 5 – Kirmaci (JONGMANS, 1955) 6 – Söğütözü (JONGMANS, 1955) 7 – South of Rive de Fleuve, north of Kızıllı (JONGMANS, 1955) 8 – Red beds near Kızıllı (JONGMANS, 1955) 9 – Between Cebeci köy and Başköy (JONGMANS (1955) 10 – South of Kayabasi, near Söğütözü (JONGMANS, 1955) Geologia Croatica 65/3Geologia Croatica 292 JONGMANS (1955) also reported “Karadon” macro- floras from localities near Koslu, which were reported to in- clude Neuropteris ovata, Callipteridium armasii and Cyat- hocarpus sp. JONGMANS (1955) suggested an Asturian age for the macroflora and, if the latter two taxa can be con- firmed, it would be to late Asturian in age. This is stratigraph- ically much younger than the other Karadon Formation mac- rofloras, and is more comparable in age to the overlying Kızıllı Formation (see below). 4.4. Kızıllı Formation The macrofloras of the Kızıllı Formation are best docu- mented for the Pelitova, Azdavavy and Söğütözü areas in the east of the coal basin, and from where numerous diverse as- semblages have been documented (Table 4). There has been a general consensus that these strata are Asturian (“West- phalian D”) in age (JONGMANS, 1939, 1955; WAGNER in STOCKMANS, 1962; KEREY et al., 1986) partly through the regular appearance of Neuropteris ovata. However, other species that also regularly appear include Dicksonites pluke- netii, Callipteridium spp., Alethopteris ambigua, Alethop- teris pseudograndinioides, Lobatopteris vestita, Acitheca polymorpha, Ptychocarpus unitus and Cyathocarpus spp. These strongly point to the D. plukenetii Subzone in the WAGNER (1984) / CLEAL (1991) scheme (Fig. 6). Similar macrofloras are known from the Gurkovo Formation in the Dobrudzha Coalfield, Bulgaria (CLEAL et al., 2004), the Libiąż Member in Upper Silesia, Poland (MIGIER & KO- TASOWA in ZDANOWSKI & ŻAKOWA, 1995), the upper Heiligenwald Formation in Saarland (CLEAL, 1984), in many coalfields in southern Britain (CLEAL, 1997), the southern Cantabrian Mountains, Spain (WAGNER et al., 1983; WAG- NER & ALVAREZ-VÁZQUEZ, 1991) and the upper Syd- ney Mines Formation in the Canadian Maritimes (ZO- DROW, 1986). Since the overlying Odontopteris cantabrica Zone is taken as an index for the Cantabrian Substage, the D. plukenetii Subzone is an index for the upper Asturian Substage. At several localities there are also records of Odontop- teris spp. and Sphenophyllum oblongifolium, which suggest possibly the early Stephanian Odontopteris cantabrica Zone; examples of these species were figured by ZEILLER (1899, pl. 4, figs 3–6; pl. 6, figs 4–5) which would seem to confirm these identifications. However, without some understanding of the species distributions through the formation, it is im- possible to be sure if it is partly late Asturian and partly early Cantabrian in age, or if the entire interval is Cantabrian; both views would be compatible with the available biostratigraph- ical evidence. 5. DIsCUssION Plant biostratigraphy indicates that the Zonguldak – Amasra Coal Basin has terrestrial deposits ranging in age from Arn- sbergian (latest Mississippian) to late Asturian or possibly Cantabrian (late Middle Pennsylvanian). There has been a widespread assumption that the succession is continuous; for instance, KEREY et al. (1986, p. 211) stated that “there is little discernable evidence for physical breaks in the overall succession…” However, this is not borne out by the plant biostratigraphy, as there is no evidence of any macroflora in the Zonguldak – Amasra Coal Basin of middle or late Nam- urian, late Langsettian, Duckmantian or early Asturian age. The only stratigraphically informative macrofloras from the Alacaağzı Formation (from the Gökgöl Member) indicate an Arnsbergian age. A marine fauna from the overlying Tar- laağzı Member also indicates an early Namurian age (Patti- son in KEREY et al., 1986). This apparent absence of middle and late Namurian macrofloras or faunas is difficult to rec- oncile with the suggestion by KEREY et al. (1986) that there is a gradational contact between the Alacaağzı and Kozlu formations. RALLI (1895) and ZEILLER (1996) recognised the sharp discontinuity between the macrofloras of the Kozlu and Karadon formations, suggesting that it was part of a re- gional unconformity. Significantly, KEREY (1982) also re- garded the boundary to be an abrupt lithological break which he later (KEREY et al., 1986, p. 206) stated was at “…the base of a succession of thick conglomeratic layers just above the Agop Coal Seam.” Kerey (1982) interpreted this as a Figure 6: Stratigraphic ranges of the key macrofloral taxa found in the Kızıllı Formation, plotted against the WAGNER (1984) / CLEAL (1991) biozone scheme. Ranges mainly as given by CLEAL (1978, 1984, 1997, 2007), WAG- NER et al. (1983), WAGNER (1984), ZODROW & CLEAL (1985), WAGNER & ALVAREZ-VÁZQUEZ (1991) and CLEAL & THOMAS (1994). Cleal and van Waveren: A reappraisal of the Carboniferous macrofloras of the Zonguldak – Amasra Coal Basin, north-western Turkey Geologia Croatica 293 change from a predominantly meandering fluvio-lacustrine facies to a braided-stream and alluvial fan facies, but may also indicate a break in the sequence. ARNI (1939) and EGE- MEN (1959), in contrast, argued that there was a floristic transition between the Kozlu and Karadon formations, but this is not borne out by the available evidence: all of the di- verse Kozlu Formation macrofloras unequivocally indicate the Langsettian Lyginopteris hoeninghausii Zone, and prob- ably the lower part of that zone (notably with Lyginopteris and Neuralethopteris) and all of those from the Karadon For- mation belong to the upper Bolsovian Paripteris linguaefolia Zone, (notably with Sphenophyllum emarginatum, Mariopt- eris nervosa, Macroneuropteris scheuchzeri, Laveineopteris rarinervis). Similarly, the suggestion by KEREY et al. (1986) that the boundary between the Karadon and Kızıllı formations is transitional is at variance with the macrofloral evidence, which indicates an absence of middle and late Asturian strata. Here again, KEREY (1982) and KEREY et al. (1986) stated that in the Pelitova and Azdavavy areas the base of the Kızıllı Formation is marked by beds of pebbly sandstone, this time overlying a coal (the Tavan Seam), which tends to suggest a break in the sequence. These age estimates were based on the macrofloral bi- ostratigraphy developed by WAGNER (1984), CLEAL (1991) and CLEAL & THOMAS (1994), mainly in western Europe and North America. It is of course always possible that these biozones cannot be applied as far east as the Zon- guldak – Amasra Coal Basin; it is notable that FISSUNENKO & LAVEINE (1984) reported discrepancies in the strati- graphical ranges of certain plant fossil-species between west- ern Europe and the Ukraine. In contrast, however, a study of the macrofloral biostratigraphy of the Dobrudzha Coalfield in northeastern Bulgaria showed that this biostratigraphy could be broadly applied when local factors (e.g. marine in- fluence) were taken into account (CLEAL et al., 2004). OKAY et al. (1994, 2006) and PHAROAH (1999) sug- gested that prior to the Late Cretaceous opening of the Black Sea, the Istanbul Block and Moesian Platform were located adjacent to each other. This would provide the palaeogeo- graphical context to support the view of TENCHOV (1989) that the Zonguldak – Amasra Coal Basin is part of a belt of coal swamp deposits that extended westwards from the Zon- guldak – Amasra Coal Basin to the Dobrudzha Coalfield in Bulgaria and Upper Silesia on the Czech – Polish border. Macrofloral biostratigraphy allows the succession in the Zon- guldak – Amasra Coal Basin to be compared with these other areas (Fig. 7). This suggests individual units can be broadly correlated: the Alacaağzı Formation with the Rakovski For- mation, the Kozlu Formation with the lower parts of the Załięż Beds and the Mogilishte Formation, the Karadon For- mation with the upper part of the Makedonka Formation, and the Kızıllı Formation with the Libiąz Beds and the Gurkovo Formation. These units are not only similar in age – there are also broad similarities in the facies present (TENCHOV, 2005, 2007; KĘDZIOR et al., 2007). However, it is also clear that there is a progressive eastwards widening of the strati- graphical gaps in the successions. Such disruption to patterns of sedimentation was probably the result of tectonic instabil- ity resulting from the suturing of the terrane to the south and Figure 7: Correlation of the Carboniferous successions of the Zonguldak – Amasra Coal Basin, the Dobrudzha Coal Basin and the Upper Silesia Coal basin, based on macrofloral biostratigra- phy. Based on data given in TENCHOV et al. (in NIKOLOV, 1988), KOTASOWA & MIGIER (in ZDAN OWSKI & ŻAKOWA, 1995), CLEAL et al. (2004, 2010, 2011), TENCHOV (2004, 2005, 2007) and the present paper. Geologia Croatica 65/3Geologia Croatica 294 west of the Pontides (the Sakary – Standja Terrane – OKAY et al., 2006) with the Moesian – Pontides Terrane. It has been suggested that the Sakary – Standja Terrane equates to Amor- ica in western Europe, and the Moesian – Pontides Terrane to Avalonia (STAMPFLI et al., 2002), and so this tectonism observable in northern Turkey is in effect an eastwards ex- tension of the Variscan Orogeny. Variscan tectonic activity would, therefore, appear to have started earlier and be more continuous in the area of the Moesian – Pontides Terrane than in more western parts of Variscan Euramerica. How much this was affecting sedi- ment supply from the hinterland area and how much drain- age patterns within the basin is still unclear. It would be in- formative to have the type of palynology-based vegetation analysis of the Zonguldak – Amasra Coal Basin as has been done in Dobrudzha (DIMITROVA & CLEAL, 2007) to de- termine the details of the tempo and pattern of vegetation change that took place here during Westphalian times. How- ever, the evidence from the Zonguldak – Amasra Coal Basin would seem to support the view of CLEAL et al. (2010, 2011) that the disruption to the coal swamp biome during Westphalian times first started in these easternmost parts of Variscan Euramerica. Although only a preliminary analysis of the published data, this paper provides new insights into the wider geo- logical and palaeontological context of the Zonguldak – Amasra Coal Basin macrofloras. A detailed taxonomic re- view is now clearly needed, especially to improve our under standing of the palaeoecological and floristic setting of this area. The W.J. Jongmans Collection now at Naturalis (Leiden, the Netherlands) probably offers the best starting point for such an analysis. ACKNOWLEDGEMENT This paper is a contribution to IGCP 575: Pennsylvanian ter- restrial habitats and biotas of southeastern Euramerica. It arose out of the first project meeting held at Zonguldak in 2010, which was organised by Prof. Vedat DIDARI (Karael- mas University, Zonguldak) and his colleagues. The authors are grateful to Prof. Vedat DIDARI, and to Dr. Hülya İNANER (Dokuz Eylül University, İzmir), for helpful discussions on the background to the Zonguldak – Amasra Coal Basin; and to Prof. Barry THOMAS (Aberystwyth University) for advice on lycopsid taxonomy. A preliminary version of this paper was presented at the 2011 meeting of IGCP 575 held at the Uni- versity of Zagreb (Croatia), and the authors thank the orga- nisers of that meeting, notably Dr. Jasenka SREMAC. Appendix TAxONOMIC REMARKs ON sELECTED sPECIEs These remarks are not intended to be exhaustive, but are merely to clarify the usage of some of the species names in this paper, and why they differ from those used in the origi- nal publications. Lepidodendron obovatum STERNBERG auct. This spe- cies has been the subject of much confusion. THOMAS (1970) re-examined the type specimen and came to the con- clusion that it was a synonym of L. aculeatum STERN- BERG. However, many authors have referred specimens to L. obovatum that are really L. mannabachense PRESL. The distinction between L. aculeatum and L. mannabachense is based on surface features of their cushion and on their epi- dermal details (THOMAS, 1970), so we are uncertain to which of these two species the L. obovatum determinations should be referred. Sublepidodendron robertii (NATHORST) CHALONER in BOUREAU et al., 1967 (= Lepidodendron robertii NA- THORST, 1914). CHALONER (in BOUREAU et al., 1967) transferred L. robertii to Sublepidodendron presumably as it was thought to be eligulate, although this negative feature has yet to be clearly confirmed. Cardiopteridium nanum (EICHWALD) WALTON, 1941 (= Cyclopteris nana EICHWALD, 1860; ≡ Cardiopteridium spetsbergense NATHORST, 1914; ≡ Cardiopteridium wal- denburgense ZIMMERMANN, 1932). ZEILLER (1899) re- ferred to this species as Cardiopteris polymorpha (GÖP- PERT) SCHIMPER, but JONGMANS (1955) correctly attributed it to Cardiopteridium. JONGMANS used the spe- cies name C. waldenburgense but WALTON (1941) had ear- lier shown that this species merely represents slightly larger forms of C. nanum, the latter name taking priority. Lyginopteris distans (STERNBERG) CLEAL & VAN WAVEREN, comb. nov. (= Sphenopteris distans STERN- BERG, 1825; = Sphenopteris bermudensiformis SCHLO- THEIM ex ZEILLER, 1899; = Lyginopteris bermudensefor- mis (SCHLOTHEIM ex ZEILLER) PATTEISKY, 1929). This species was referred to as S. bermudensiformis by ZEILLER (1899) and JONGMANS (1955), who attributed the name to SCHLOTHEIM (1820). However, as SCHLO- THEIM’s (1820) pre-dates the starting-point for the publica- tion of plant fossil species names (ICBN, Art. 13.1 – Mc- NEILL et al., 2006), the earliest valid publication of the name must be taken to be ZEILLER (1899). As pointed out by KVAČEK & STRAKOVÁ (1977), this is, therefore, pre- dated by the nomenclatural synonym S. distans. Following PATTEISKY (1957), there can be little doubt that this spe- cies belongs to the fossil-genus Lyginopteris and so a new combination is proposed here. Lyginopteris fragilis (SCHLOTHEIM ex BRONGNI- ART) PATTEISKY, 1955 (= Sphenopteris fragilis SCHLO- THEIM ex BRONGNIART, 1828; ≡ Cheilanthites divarica- tus GÖPPERT, 1836; ≡ Sphenopteris divaricata (GÖPPERT) GUTBIER in COTTA et al., 1843). JONGMANS (1955) re- corded this species as Sphenopteris divaricata but according to PATTEISKY (1955) this is a later taxonomic synonym of Lyginopteris fragilis. The latter name is usually attributed to SCHLOTHEIM (1820) but is regarded as published before the starting-point for the publication (ICBN, Art. 13.1). Sphenopteris elegans BRONGNIART, 1822 (≡ Sphe- nopteris adiantoides SCHLOTHEIM ex LINDLEY & HUT- TON, 1834). JONGMANS (1955) referred to this species as Cleal and van Waveren: A reappraisal of the Carboniferous macrofloras of the Zonguldak – Amasra Coal Basin, north-western Turkey Geologia Croatica 295 S. adiantoides, attributing the name to SCHLOTHEIM (1820). However, SCHLOTHEIM’s (1820) book pre-dates the starting-point for the publication of names for plant fos- sil-species (ICBN, Art. 13.1 – McNEILL et al., 2006). The earliest validly published use of this species name was by LINDLEY & HUTTON (1834), but this was predated by its taxonomic synonym S. elegans, and so the latter must take priority. REFERENCEs ARNI, P. (1939): Neue geologische Geschichtspunkte für den Bergbau im westlichen Steinkohlenbecken Nordanatoliens.– Maden Tetkik ve Arama Enstitüsü Yayinlarindan, Seri B: Irdeller, 4/17, 55–63. BELL, W.A. (1938): Fossil flora of Sydney Coalfield, Nova Scotia.– Canada Department of Mines and Resources, Geological Survey Memoir, 215, 1–334. 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