Late Cretaceous mega-, meso-, and microfloras from Lower Silesia

ADAM T. HALAMSKI, JIŘÍ KVAČEK, MARCELA SVOBODOVÁ, EWA DURSKA, and ZUZANA HEŘMANOVÁ

Halamski, A.T., Kvaček, J., Svobodová, M., Durska, E., and Heřmanová, Z. 2020. Late Cretaceous mega-, meso-, and microfloras from Lower Silesia. Acta Palaeontologica Polonica 65 (4): 811–878.

Late Cretaceous plants from the North Sudetic Basin (Lower Silesia, south-western Poland) are reviewed on the basis of megaflora from 17 localities (270 identifiable specimens), mesoflora from two localities, and microflora from four localities. Major sites are Rakowice Małe and Bolesławiec. Eight megafloral assemblages are distinguished (Assemblage 1, Turonian; Assemblages 2, 3, lower–middle Coniacian; Assemblages 4, 5, upper Coniacian?–lower Santonian?; Assemblages 6–8, lower–middle Santonian); the bulk of the palaeoflora is from Assemblages 4–6 and 8. Megaflora consists of 29 taxa (6 ferns, 4 conifers, and 19 angiosperms). Geinitzia reichenbachii is the most common species. Dryophyllum westerhausianum (Richter, 1904) Halamski and Kvaček comb. nov. is a trifoliolate leaf re-interpreted as a representative of Fagales. Three species of Dewalquea are distinguished: Dewalquea haldemiana, Dewalquea insignis, and Dewalquea aff. gelindenensis. Platanites willigeri Halamski and Kvaček sp. nov. is characterised by trifoliolate leaves, the median leaflet of which is ovate, unlobed, with a serrate margin, and cuneate base. Palaeocommunities inferred from the megafossil record include: a back swamp forest dominated by Geinitzia, with abundant ferns; a Dryophyllum-dominated riparian forest; a forest with Dewalquea and Platanites willigeri possibly located in the marginal part of the alluvial plain; dunes with D. haldemiana and Konijnenburgia; a fern savanna with patches of Pinus woodlands. Palynoassemblage A from the Nowogrodziec Member, studied mostly at Rakowice Małe and Żeliszów, consists of 126 taxa, including 105 terrestrial palynomorphs (54 bryophyte, lycophyte, and pteridophyte spores, 16 gymnosperms, 35 angiosperms). The mega- and mesofossil records are dominated by angiosperms; the palynoassemblages are dominated by ferns. Palaeocommunities represented solely by the microfossil record are halophytic (with Frenelopsis and unconfirmed presence of Nypa) and pioneer vegetation. Palaeocommunities are intermediate in general character between those pre-dating the Cretaceous Terrestrial Revolution and modern, angiosperm-dominated vegetation. In comparison to older plant assemblages from contiguous areas laurophylls are much rarer; this might correspond to a real phenomenon of exclusion of lauroids from Santonian riparian forests. The studied assemblage is more similar to younger palaeofloras than to older ones; this might be interpreted as stabilisation of communities after a period of pronounced change related to the rise to dominance of the angiosperms. In contrast to widespread endemism among vertebrates of the European Archipelago, the plant cover consists mostly of species that are widely distributed.

Key words: Angiospermae, Leptosporangiatae, palaeobotany, palynology, taxonomy, Coniacian, Santonian, Poland.

Adam T. Halamski [ath@twarda.pan.pl], Institute of Paleobiology, Polish Academy of Sciences, ul. Twarda 51/55, ­00-818 Warszawa, Poland.

Jiří Kvaček [jiri.kvacek@nm.cz] and Zuzana Heřmanová [zuzka.hermanova@gmail.com], National Museum, Václavské náměstí 68, 115 79 Praha 1, Czech Republic.

Marcela Svobodová [msvobodova@gli.cas.cz], Institute of Geology of the Czech Academy of Sciences, Department of Paleobiology and Paleoecology, Rozvojová 269, 165 00 Praha 6, Czech Republic.

Ewa Durska [edurska@uw.edu.pl], Faculty of Geology, University of Warsaw, ul. Żwirki i Wigury 93, 02-089 Warszawa, Poland.

Received 4 March 2020, accepted 6 August 2020, available online 13 November 2020.

Copyright © 2020 A.T. Halamski et al. This is an open-access article distributed under the terms of the Creative Commons Attribution License (for details please see http://creativecommons.org/licenses/by/4.0/), which permits unrestricted use, distribution, and reproduction in any medium, provided the original author and source are credited.

Introduction

The region of Lower Silesia (Dolny Śląsk, Niederschlesien in former German literature, south-western Poland) was important in the early days of palaeobotany (Goeppert 1844: 161–163). The first fossil vegetal remains ever figured as such may have been Carboniferous plants from Silesia (Volkmann 1720) and plant fossils from Lower Silesia were discussed by Schlotheim (1820), Sternberg (1821), and Rhode (1821–1823). Late Cretaceous plant assemblages from Silesia range from the Cenomanian (Goeppert 1841; Niebuhr 2019) through the Turonian (Macko 1963; Płachno et al. 2018), Coniacian (Velenovský 1883; Langenhan and Grundey 1891; Frič 1897; Halamski and Kvaček 2015) to the Santonian (Roemer 1889; Halamski et al. 2018b).

The aim of the present paper is the systematic description of plant fossils and palaeoecological reconstruction of communities found in outcrops situated in the North Sudetic Basin (study area ca. 300 km2) and ranging from Turonian to Santonian in age. The assemblages consist of mega-, meso- and microfossils; a complete treatment of the megaflora and a synopsis of the microflora are provided, whereas mesofossils have been treated separately (Heřmanová et al. 2019; ZH, JK, ATH, and Jiřina Dašková, unpublished material), so only a general account of the mesoassemblage is given here.

Institutional abbreviations.—BGR, Bundesanstalt für Geo­wissenschaften und Rohstoffe, Berlin-Spandau, Germany; MB, Museum für Naturkunde, Berlin, Germany; MGUWr, Muzeum Geologiczne Uniwersytetu Wrocławskiego, Wrocław, Poland; MMG, Museum of Mineralogy and Geology, Senckenberg Natural History Collections Dres­den, Germany; NMP, National Museum, Prague, Czech Republic; ZPAL, Institute of Paleobiology, Polish Academy of Sciences, Warsaw, Poland.

Other abbreviations.— ≡, homotypic synonym (ICN, Art. 14.4); auct., auctorum (Latin: of authors), for a taxon of uncertain authorship; coll., collection (referring to an owner, not necessarily the collector); ICN, International Code of Nomenclature for algae, fungi, and plants; leg. legit (Latin: collected), indicating the collector; s.n., sine numero (Latin: without number, for a specimen belonging to an established collection but lacking an inventory number; ubi syn., ubi synonymia (Latin: where the synonimy [can be found]), for a reference containing an extensive synonymy list.

Historical background

If one disregards data on the geology of the area along the Kwisa river forming the easternmost extremity of Lusatia then belonging to the state of Saxony, provided by Charpentier (1778), the earliest geological description of the North Sudetic Basin was given by von Raumer (1819: 128–130), but the first author to deal systematically with Cretaceous plants therefrom was Heinrich Robert Goeppert (Göppert). He described a tree fern from Żeliszów (Goeppert 1836b: 449) and signalled conifer wood and fruits from the vicinity of Lwówek Śląski (Goeppert 1844: 170). Heinrich Robert Goeppert assembled an important collection of Creta­ceous plants (kept in MGUWr) and studied and annotated other specimens (like those from the secondary school at Lwówek Śląski, now in MB, see below). A short overview of “nearly finished works” on that subject was published as a summary of a lecture given on 1st November 1865 (Goeppert 1866a). A paper on Cretaceous index plants (Goeppert 1886b) included data from a few localities in Lower Silesia (“Geinitzia cretacea” Ulina, Nowogrodziec, Bolesławiec, Rakowice Małe; “Cunninghamites oxycedrus” Rakowice Małe; “Credneria sp.” Wartowice Nowe (erroneously as Cenomanian); “Debeya serrata” Ołdrzychów, probably erroneously for Ulina; “Gleichenia dresleriana” environs of Lwówek). However, no systematic treatment has ever appeared, so Goeppert’s identifications cited by Geinitz (1849–1850), Williger (1882: 84, 86–89, 94, 102, 104–108), and after him by Scupin (1913: 65) and Milewicz (1997: 31), are in some cases nomina nuda. They are discussed in the systematic part of the present paper.

Cretaceous angiosperms from the North Sudetic Basin were first recorded in print by Drescher (1863) from the “Schichten von Neu-Warthau” (Assemblage 2 herein). Among several dozens of animal taxa he mentioned also “Credneria denticulata Z.” and the conifer “Geinitzia cretacea Endl.” (Drescher 1863: 311). Geinitzia was also reported from Ołdrzychów by Klocke (1864: 262).

The paper by Williger (1882), although devoted pri­marily to stratigraphy and the fossil fauna of the North Sudetic Basin, is nonetheless of special importance, insofar as in several cases it has been the only source providing detailed lists of plant taxa coming from single outcrops, allowing thus to supplement, or even to correct, laconic or partly false labels. The debt of the present authors to Gustav Williger is expressed in naming Platanites willigeri Halamski and Kvaček sp. nov. in his honour.

Roemer (1886, 1889) studied fossil plants from the ceramic clays mined in the suburbs of Bolesławiec. He described seven taxa in total, including one new species (Menispermites bunzlavensis Roemer, 1889). Unfortunately, only a small part of his collection could be found in MGUWr, whereas the rest (including types and most of figured speci­mens) seems to be lost.

An important collection of plant fossils from the North Sudetic Basin was assembled in the Löwenberger Gymnasium (secondary school at Lwówek Śląski), at least in part by the teacher and cantor Ernst Friedrich Dresler, the author of a local flora (Dresler 1883). These specimens are the basis of lists given by Goeppert (1866a), Williger (1882) and Scupin (1913), but, as mentioned previously, no systematic treatment of them has ever been published. The collection was acquired by MB (probably partly in 1909 and partly in 1926) and was studied by the present authors.

It is of interest to note that the area was intensely mined for coal from the second half of the eighteenth century to the second half of the nineteenth century (Maciejak and Maciejak 2013) and some historical specimens do indeed come from coal mines. Active and former sandstone quarries (Żeliszów, Rakowice Małe) are at present the best localities for the fossil flora. Details on history of existing collections and on collectors are given by Mohr (2009). Cretaceous fauna, palaeogeography, and stratigraphy were dealt with, among others, by Scupin (1913) and Andert (1934).

Detailed maps (1:25 000) of the studied area and/or corresponding explanations were published by Kühn and Zimmermann (1918), Baraniecki et al. (1955), Milewicz (1955, 1956a, 1964), and Berezowska and Berezowski (1982). An important cartographic work made by Georg Berg (sheets Bunzlau and Kaiserswaldau) was never published, but its manuscript is kept in the BGR. A synthesis of the Cretaceous stratigraphy of the North Sudetic Basin was given by Milewicz (1997), and a short overview in English was published by Walaszczyk (2008). Sedimentological studies of interest for the present study were published by Milewicz (1956b), Górniak (1986), Leszczyński (2010, 2018), and Chrząstek and Wypych (2018).

Palynomorphs from Rakowice Małe were studied by Thiergart (1942) who described a new species, Spori­tes appendicifer (now Appendicisporites appendicifer; Schi­zaea­ceae) from that locality (see also Thiergart 1949). In 1957 Wilfried Krutzsch collected at Rakowice Małe and included these strata in his palynological zoning of the Central European Cretaceous: the “Löwenberger Bild” encompasses uppermost Coniacian to lower Santonian strata (Krutzsch 1958: 512, table 1), but details were not provided. This is also the case for two further publications in which the “Löwenberger Bild” is used as an equivalent of the lower Santonian (Krutzsch 1959a: pl. 4: 12–13, 1966a: 96–97). A few spores and pollen grains from Rakowice Małe were illustrated by Pacltová and Krutzsch (1970: pls. 100: 11, 101: 9–13, 28–32).

A palynoflora from the North Sudetic Basin was studied by the Polish palaeobotanist Jadwiga Raniecka-Bobrowska (1904–1990; see biographic note by Grabowska 1992), culminating in an internal report (Raniecka-Bobrowska 1968) with cursory descriptions of over seven hundred palynotaxa (see below, Material and methods, Microflora) based on material from nine boreholes. It was intended to form the basis of a future monograph (Raniecka-Bobrowska 1968: 8), which, however, was never prepared. Results were published only in abridged form (Raniecka-Bobrowska 1984, 1989), with generalised data and description of a single new species, Catinipollis lwowekensis Raniecka-Bobrowska, 1984 from a borehole near Bolesławiec. A few illustrations from the above-mentioned report were also published in a short account of Late Cretaceous palynofloras from Poland by Grabowska (2003), but without detailed provenance data. The palynological part of the present paper is partly based on Raniecka-Bobrowska (1968).

In the monograph of Cretaceous fruits and seeds from Central Europe Knobloch and Mai (1986) described two mesofossil species from Rakowice Małe, namely Calathiocarpus octocostatus (Knobloch, 1971) Knobloch and Mai, 1986 and Walbeckia guttaeformis (Knobloch, 1971) Knobloch and Mai, 1986.

Studies of the Cretaceous megaflora of this region, which were abandoned for more than a century, except for a short literature-based overview by Lilpop and Kostyniuk (1957), were resumed starting with Mohr (2009) who provided an account of the palaeobotanical collections in MB from a historical point of view. In the revision of the Cretaceous tree fern stems from Bohemia and Silesia Greguš et al. (2013) described Protopteris punctata (Sternberg, 1820) Presl in Sternberg, 1838, from the environs of Lwówek Śląski and Protopteris singeri (Goeppert, 1836b) Presl in Sternberg, 1838, from Żeliszów. Preliminary results of the present work were presented by Halamski and Kvaček (2018, 2019), Heřmanová et al. (2018), and Halamski et al. (2018b, 2019).

Geological setting

The Cretaceous plant fossils described in the present paper come from 17 localities (described in the Appendix 1) situated in an area between Nowogrodziec and Bolesławiec in the north and Lwówek Śląski in the south (Fig. 1). From a geographic point of view (Kondracki 1998; Bína and Demek 2012), this region belongs to the West Sudetic Foothills (Pogórze Zachodniosudeckie). More precisely, five localities are situated in the Pogórze Izerskie (German: Isergebirgs-Vorland, Czech: Frýdlantská pahorkatina) and twelve in the Pogórze Kaczawskie (German: Bober-Katz­bach-­Vorgebirge), the two subregions being separated by the valley of the Bóbr river.

The North Sudetic Basin or North Sudetic Synclinorium (Niecka Północnosudecka) is a geological structure situated on the northern foreland of the Sudetes, the latter forming the north-eastern edge of the Bohemian Massif. The strata belonging to the North Sudetic Basin lie unconformably upon the Variscan basement and consist of Upper Carboniferous, Permian, Lower to Middle Triassic, and Upper Cretaceous sedimentary and volcanic rocks (Śliwiński et al. 2003; Żelaź­niewicz 2005). The present tectonic structure of the basin is due to a wide-scale inversion related to multiphase convergence between Africa–Iberia and Western-Central Europe (e.g., Kley and Voigt 2008) that began in the Cretaceous and continued in the Paleogene (Solecki 2011), the detailed timing of which being, however, poorly constrained (Sobczyk et al. 2019 and references therein).

The Cretaceous part of the North Sudetic Basin, which may be considered as the south-eastern prolongation of the East Brandenburg Basin, consists of limestone, marl and marly sandstone, sandstone, mudstone, and claystone, locally with coal intercalations (Milewicz 1997: fig. 6). The age of the Cretaceous succession in the North Sudetic Basin ranges from the Cenomanian to the Santonian (Milewicz 1997; Walaszczyk 2008). The Cenomanian to middle Conia­cian rocks are of marine origin, whereas younger deposits are of marine origin in the western part of the Basin and of brackish to alluvial origin in its central and eastern parts, including the study area.

The outcrops dealt with in the present paper are situated in the central part of the North Sudetic Basin. No Cretaceous plant megafossils are known from either the western part of the North Sudetic Basin as it is mostly covered by Tertiary deposits, or from Cenomanian to Santonian rocks cropping out in the eastern and south-eastern extremities of the basin (Wleń Trough, Świerzawa Trough; Milewicz 1997: fig. 1).

During the first half of the Late Cretaceous, more precisely starting with the Cenomanian transgression during which the major part of Central Europe was flooded (Voigt et al. 2008: 924) and ending with the middle Santonian regression due to tectonic uplift (Walaszczyk 2008: 960), the present territory of Lower Silesia belonged to a seaway between the Tethys and the Northern Ocean with scattered islands, the so-called European Archipelago (Csiki-Sava et al. 2015 and references therein).

Scupin (1911, map re-published in Scupin 1913, 1937) may have been the first to reconstruct two major islands, the “Riesen-Gebirgs-Insel” (now usually referred to as the West Sudetic Island) and the “Ost-Sudetische Landmasse” (East Sudetic Island), with the “Löwenberger Becken” (North Sudetic Basin) situated between them. It is generally agreed that the size and the extent of the two islands changed during their existence, but the precise position of coastlines remains a subject of controversy (Kędzierski 2005 and re­ferences therein; Biernacka and Józefiak 2009; Biernacka 2012). The landscape of the more southerly situated parts of the European Archipelago (namely the present-day Nysa Kłodzka Graben) is reconstructed as having been smoothly hilly (Migoń and Lidmar-Bergström 2001; Uličný 2001; August and Wojewoda 2004; Sobczyk et al. 2019). By way of contrast, the landscape of the area considered herein may have been flat to weakly undulating (Raniecka-Bobrowska 1968: 1 and references therein).

According to Leszczyński (2018: 810–811), the two above-mentioned islands existed as separate landmasses up to the early Coniacian. The regression that took place in the middle Coniacian resulted in a retreat of the sea to the west and in the merging of the two islands with emergence of the study area and sedimentary hiatus (Milewicz 1956b). A consequence of the late Coniacian transgression was the formation of an embayment aligned in an approximately NW-SE direction, ca. 35 km long and 15 km wide (Leszczyński 2018: fig. 40D; middle and late Coniacian coastlines are shown in Fig. 1C). This palaeogeographical disposition is supposed to have persisted until the final retreat of the sea from the study area in the middle Santonian.

A short survey of the Cretaceous strata of the North Sudetic Basin follows in stratigraphic order. Details on single outcrops are given in the Appendices 1 and 2.

Cenomanian.—A major marine transgression took place in the middle (perhaps even early) Cenomanian (Skelton 2003; Torsvik and Cocks 2017: 235; Voigt et al. 2008). These transgressive deposits lie mostly on Triassic rocks, less commonly on Permian or Paleozoic rocks (Mile­wicz 1997: 9); their thickness is quite varied, but usually about 100 m (Walaszczyk 2008). Cenomanian palaeofloras are rich and diversified in Bohemia (e.g., Heer 1869; Velenovský 1889; Eklund and Kvaček 1998; Kvaček and Friis 2010; Kvaček et al. 2012; Greguš and Kvaček 2015) and known also in southernmost Lower Silesia (Niebuhr 2019), but no plant fossils have ever been found in Cenomanian strata of the study area.

Turonian.—The Turonian deposits are ca. 150 m thick (Walaszczyk 2008). A single specimen of Geinitzia reichenbachii is described as coming from Turonian marl (lower part of the Rakowice Wielkie Formation) cropping out in an unidentified quarry near Lwówek. This is separated herein as Assemblage 1.

Lower–middle Coniacian.—Lower to middle Coniacian sand­stone belongs to the upper part of the Rakowice Wielkie For­mation.

According to Williger (1882: 84), the lowest part of Conia­cian sandstone can be separated as the Wartowice beds (Neuwarthauer Schichten), including outcrops of which having yielded fossil plants at Wartowice and Zbylutów. Independently of the question of the detailed stratigraphic position of the discussed beds within the Coniacian sandstone, the plant assemblage may be distinguished on account of preservation of leaves coated by a brown ferrugineous substance and by its floristic composition (Ettingshausenia sp. 1, Pinus). This is termed herein Assemblage 2.

The Żerkowice Member (obere Quadersandstein sensu Williger 1882; uppermost part of the Rakowice Wielkie Formation) consists of sandstone beds and is ca. 100 m thick (Leszczyński 2018: 789). Plants are preserved as poor leaf imprints in sandstone, unidentifiable wood fragments, and tree fern stems (their stratigraphic position within this level is presumed) coming from Czaple and Żerkowice are termed herein Assemblage 3.

Coniacian–Santonian.—Unlike the previously described Cenomanian to Coniacian succession, which is entirely of marine origin (Walaszczyk 2008), the rocks forming the Nowogrodziec Member of the Czerna Formation were deposited in a mixed (coastal, lacustrine, paludal and lagoonal) environment (Leszczyński 2010). The period of non-deposition corresponds to the hiatus between the Żerkowice Member of the Rakowice Wielkie Formation and the Nowogrodziec Member of the Czerna Formation and was sufficiently long to allow the erosion of the lower to middle Coniacian sandstone (Berezowska and Berezowski 1982: 43 and references therein).

This part of the succession, which has yielded most of the plant fossils described in the present paper, is best exposed in the quarry at Rakowice Małe (see Appendix 1) and could also be observed at Żeliszów. Former outcrops include Żerkowice, Huzarski Skok, and Ołdrzychów (see also Leszczyński 2018). At Rakowice Małe it is up to 10 m thick (usually less); the basal part (ca. 70 cm) is made up of light multi-coloured clayey mudstone (Leszczyński 2018: fig. 16B; Fig. 2B) with subordinate flat pebbles of iron claystone, on surfaces of which plant imprints occur (Assemblage 4 herein), whereas the remaining part consists of dark claystone with irregular coal intercalations (Assemblage 5 herein; Leszczyński 2018: fig. 16C–G; Fig. 2F). The presence of amber in the coal (Fig. 2C) was noted by Goeppert (1836a) and Halamski et al. (2018b).

Santonian.—The part of the Czerna Formation overlying the Nowogrodziec Member is composed mostly of sandstone with subordinate intercalations of white clay used for the ceramic industry at the famous factory in Bolesławiec. It was interpreted as a deltaic deposit (Milewicz 1997, 2006). In more detail, the sedimentary environment may have consisted of a mosaic of deltaic plains, alluvial plains, wetlands, and shallow lakes (Górniak 1986: 128).

The sandstone is fine- to medium-grained, seldom coarse-­­grained with beds about 0.5–3 m thick (Berezowska and Berezowski 1982: 45). A brackish fauna consisting of bivalves and gastropods may be locally abundant (Scupin 1913; Milewicz 1964: 30). Fossil plants from the sandstone beds are preserved as mostly colourless imprints of isolated leaves without cuticles or fine venation details (Assemblage 6 herein). The most abundant fossils come from Ulina; other localities include Ocice, Otok, Rakowice Małe, and Żerkowice.

Plants from a single collection at Nowe Jaroszowice differ from Assemblage 6 both by systematic composition (Platanites sp. 1, otherwise unknown) and preservation (fer­rugineous crusts) and so are separated herein as the Assemblage 7.

Megafloral remains from white “ceramic clays” are ter­med herein the Assemblage 8. Claystone and mudstone­ beds form intercalations, lenses and beds up to 6 m thick within sandstone (Berezowska and Berezowski 1982: 46). Plant remains (angiosperm leaves and Geinitzia twigs) form mass accumulations, in which majoritarily fragmented leaves recover one another (see Roemer 1889). Compound leaves of Dewalquea insignis and Dewalquea aff. gelindenensis are preserved with leaflets in organic connection, although no cuticles or fine venation details can be observed. Plants from the outcrop at Bolesławiec were described by Roemer (1889). Another locality was noted on labels as Luisenhain (name of a pre-1945 restaurant, no Polish equivalent; see Appendix 1 for a more detailed description and for the explanation of confusion of specimens coming from these two localities).

Stratigraphic distribution of plant fossils.—The stratigra­phic distribution of the plant assemblages studied in the present paper is as follows: (i) Turonian: Rako­wice Wielkie Formation—Assemblage 1; (ii) lower–middle Coniacian: Rakowice Wielkie Formation—Assemblages 2 and 3; (iii) upper Coniacian? or lower Santonian?: Czerna Formation, Nowogrodziec Mem­ber—Assemblages 4 and 5; (iv) lower to middle Santonian: Czerna Formation, unnamed member—Assemblages 6–8.

It is worth to underline that the units (i) to (iv) are considered to form a stratigraphic succession, whereas the ordering of assemblages within units, except for the directly observed succession of 4 and 5, is either tentative (2, 3) or represents facies variants (6–8). The exact position of the Coniacian–Santonian boundary is unknown, it might run as low as between the Rakowice Wielkie and Czerna formations or as high as in the basal part of the unnamed member of the Czerna Formation.

Finally, it might be of interest to note that due to lithological similarity Tertiary (Oligocene) plant-bearing sandstone beds from northern Silesia were several times mistaken for Cretaceous. This error was corrected already by Williger (1882: 124; see also Milewicz 1976: 24; Raniecka-Bobrowska 1977: 173), but Lilpop and Kostyniuk (1957: 144) mistakenly listed the Oligocene palm Flabellaria chamaeropifolia Goeppert, 1836b from Parowa (Tiefenfurth) near Bolesławiec as Cretaceous. This is also the origin of the erroneous information on the presence of palm macroremains in the Cretaceous of Silesia in Cieśliński (1989: 326).

Detailed stratigraphy of the Nowogrodziec Member.—The main purpose of excavations led by the present authors at Rakowice Małe (2017–2018) and at Żeliszów (2018–2019) was to investigate mesofossils and palynomorphs from Assem­­blage 5/Palynoassemblage A, i.e., the part of the Nowo­gro­dziec Member with coaly intercalations.

The Nowogrodziec Member of the Czerna Formation consists of clay and claystone, either with (upper part) or without (basal part; Fig. 2D) coaly intercalations, and is thus sharply separated from underlying and overlying sandstone (Fig. 2). At Rakowice Małe it is up to 10 m thick (less than 6 m in the section RK-4; Fig. 2A, B), whereas at Żeliszów it is about 4 m thick (Fig. 2E, F). At Rakowice Małe the easily observable top of the sandstone of the Rakowice Wielkie Formation was taken as a reference level (“0”). In both quarries strong lateral variations of thickness and lithology of the Nowogrodziec Member were evident. For example, no distinct root horizon could be found in the measured section RK-4, whereas about 10 m eastwards such a horizon was easily observable. At Żeliszów, some 30 m westwards from the trench (Fig. 2H), the Nowogrodziec Member is altogether absent and the sandstone of the Rakowice Wielkie Formation is in direct contact with the sandstone of the Czerna Formation.

The stratigraphy of the Nowogrodziec Member at Rakowice Małe was discussed by Leszczyński (2010). At Żeliszów, we were able to examine a single trench (Fig. 2F) and its stratigraphic interpretation is provided in Fig. 2E. It may be noted that, as far as it could be observed, coaly intercalations at Rakowice Małe are decametre-long layers (Fig. 2B), whereas at Żeliszów they instead consist of decimetre-scale lenses.

The age of the Nowogrodziec Member was given as early Santonian on the basis of inoceramid bivalves from the Węgliniec IG-1 borehole (Mitura et al. 1969). This dating was accepted by Milewicz (1997). Walaszczyk (2008) briefly commented on these data as requiring reinterpretation, resulting in the age of the strata being viewed as late Coniacian. Such an assignment was repeated by Leszczyński (2010).

The micropalaeobotanical data assembled during the present investigations seem to indicate a Santonian age, yet it would be imprudent to consider this dating as decisive. Dinocysts are rare in the investigated samples. Concerning the pollen grains, the genus Neotriangulipollis, present in the material studied, is usually reported to occur from the middle Santonian to the lower Campanian (Góczán et al. 1967). It is uncertain to what extent the vertical distribution this seldom reported genus may be considered as fully known (see discussion in the Systematic palaeontology). Interporopollenites turgidus Tschudy, 1975, was found in the section RK-4 (depth 110–130 cm). Given its oldest reported occurrences are from the Santonian of Vendée (France; Azéma et al. 1981), and from the Santonian–Campanian deposits of Portugal (Kedves and Hegedus 1975), it is also suggestive of the Santonian rather than Coniacian.

Material and methods

Megaflora.—Lower Silesia is by no means an exception to the general situation in much of Europe, where the significant deterioration of quality of outcrops has occurred over the last decades. Small quarries are most often no more used and disappear, which is not compensated by the growth of a smaller number of large quarries. This is why the description of the megaflora is based mostly on historical specimens. The richest collections are those in MB which originate partly from the secondary school at Lwówek Śląski (see above), and partly from the Prussia Geological Survey (transferred from the Survey to MB by Walther Gothan). Another important collection is that in MGUWr, which dates back in part to Heinrich Robert Goeppert and partly to subsequent workers. Unfortunately, the specimens from Bolesławiec studied by Roemer (1889) could be traced only in part; the remaining ones are most likely lost.

Most of the material consists of leaves. Those belonging to Assemblages 2–4 and 6–8 are imprints, whereas those from Assemblages 1 and 5 contain some original carbonaceous matter, but no interpretable results were obtained from micromorphological studies so far. The entire palaeo­flora is thus studied according to the methods developed for the study of poorly preserved (i.e., without either cuticles or fine venation details) Cretaceous assemblages, the most important element of which are morphographic systematics and widely, but precisely defined, fossil-genera (Halamski and Kvaček 2015: 102–103; Halamski et al. 2018a: 128). In accordance with editorial practice, plant taxon names are given with fully spelt authors’ names and year, following the zoological convention.

Subordinately, the presence of conifer cones and isolated cone scales, as well as of a single macroscopically recognisable platanoid infructescence, was noted in the Assemblage 5. Together with tree fern stems described in a previous paper (Greguš et al. 2013), plant fossil-taxa totalled 29 species.

Land plants from Assemblages 2 and 3 co-occur with an abundant marine fauna, similar to the situation in the Coniacian of the Idzików beds (Halamski and Kvaček 2015: pl. 1: 1, 2) or in the Campanian of eastern Poland and western Ukraine (Halamski 2013: fig. 2A).

Microflora.—For palynological study, mainly fine-grained, grey mudstone samples were selected at 20 or 40 cm intervals (more densely if changes of lithology occurred) and treated using a standard palynological extraction technique involving HCl-HF-HCl and acetolysis or heavy liquid ZnCl2 used for gravity separation. Some samples were sieved through 10 µm sieves. The residues were mounted in glycerine jelly; 5–10 slides were studied of each sample. Most samples contained enough spores and pollen admixed with marine microfossils for quantitative analysis. Counts are based on 5–10 slides, with totals of 170–220 grains per count. The slides were examined with a Leica DM2500 light microscope and for the microflora photos, the programme IM50 was used. Residues and slides are stored in the paleobotani­cal collection of the Institute of Geology, Department of Paleobiology and Paleoecology, Prague, Czech Republic.

Numerous palynomorphs were recovered by the present authors from the coaly (upper) part of the Nowogrodziec Member, i.e., from claystone corresponding to Assemblage 5 in terms of the megaflora. More precisely, 26 samples from Rakowice Małe (mainly from the section RK-4, see Fig. 2) and 14 from Żeliszów (see Fig. 2) were analysed for palynological content. This is termed herein Palynoassemblage A. Moreover, we studied historical samples from, and nearby, Rakowice Małe, including the former coal mines (MB.Pb.s.n., Wenig-Rackwitz, Andreashof, Zimmer 6/50: sample 1334; MB.Pb.s.n., Wenig-Rackwitz, Koniferen-Zweige: sample 1338; both prepared by Barbara Mohr) from Ołdrzychów (MGUWr 5638p), and from an uncertain location (MB.Pb.2008/0362, “Lwówek”, see that entry in the Appendix 1). They are tentatively referred to the Palynoassemblage A.

The MB.Pb.2008/0372 of Konijnenburgia cf. galleyi from Assemblage 4 at Żerkowice yielded poorly preserved spores (see Systematic palaeontology).

Concerning the strata overlying the Nowogrodziec Member, Raniecka-Bobrowska (1968, 1984, 1989, see also Grabowska 2003) was able to extract numerous palynomorphs from boreholes drilled through the upper part of the Santonian succession south of Bolesławiec. Given the importance of these unpublished data, they are summarised here and in some cases quoted in extenso. Raniecka-Bobrowska (1968) provides information on depths but not on lithologies, so it is impossible to translate these indications into the scheme of eight assemblages presented here and we refer to them collectively under Palynoassemblage B corresponding thus to Assemblages 6–8 in terms of megaflora.

Three samples from Assemblage 8 (MGUWr 2880p from Bolesławiec, MB.Pb.s.n. from Luisenhain, and MB.Pb. 2008/0331 from an unknown locality) were analysed for palynological content during the present study, but invariably only plant detritus without any identifiable palynomorphs was recovered.

As far as possible, in the systematic part palynomorphs are arranged according to a natural system, after Cavalier-Smith (1981), Wingate (1981), Friis et al. (2011), and Williams et al. (2017).

Systematic palaeontology

Megaflora

Kingdom Plantae Linnaeus, 1753 sensu Cavalier-Smith (1981)

Division Filicophyta Boureau, 1970

Class Leptosporangiatae von Goebel, 1881

Order Matoniales Pichi Sermolli ex Reveal, 1993

Family Matoniaceae Presl, 1848

Genus Konijnenburgia Kvaček and Dašková, 2010

Type: Konijnenburgia latifolia (Nathorst, 1908) Kvaček and Dašková, 2010 ≡ Nathorstia latifolia Nathorst, 1908; Cenomanian, Upper Cretaceous; Atanekerdluk, Greenland.

Konijnenburgia cf. galleyi (Miner, 1935) Kvaček and Dašková, 2010

Figs. 3, 4D–G.

Material.—Rakowice Małe, Assemblage 4, upper Conia­cian?–lower Santonian?: MB.Pb.2008/0365a, 2018/0062, MGUWr 6154p; Żerkowice, Assemblage 4, upper Conia­cian?–lower Santonian?: MB.Pb.2008/0372, 0373, 0374.

Description.—The available material consists of accumulations of fragments, the largest of which (Fig. 4F) shows the rachis 6 cm long and two pinnules in organic connection to the rachis.

Pinnules linear, 7–14.5 mm wide, integrimarginate, with neuropteridic base; median nerve 0.6–0.9 mm wide, subtransversely striated. Sori circular or elliptic, 1.2–1.7 mm wide, 1.5–2.0 mm long, the distance between adjacent ones 2–3 mm; sorus consisting of a median depression and 14–17 radially arranged sporangia.

Sporangia wedge-shaped (Fig. 3A1), 30–40 µm wide and 100 µm long, in some cases showing fragments of an annulus with thickly cutinised cells (Fig. 3A3) in marginal part. Fractured sporangia show a sporangial wall that is 20–40 µm thick (Fig. 3A2), it cannot be ruled out that the sporangium wall is covered by additional tissues, the unusually great apparent wall thickness resulting from the presence of a greater number of laminar structures, either a poorly preserved indusium or a leaf lamina. Spores smooth.

Remarks.—The studied material is included into Konijnen­burgia on account of the general organisation of the frond and the form of the sporangia. In quantitative characters (pinnule width and number of sporangia per sorus) it agrees best with K. galleyi (Miner, 1935) Kvaček and Dašková, 2010, known from a single fragmentary, but well-preserved specimen coming from the Cenomanian Dakota Sandstone of Kansas (Miner 1935: 288–289; pl. 1: 1–4). It differs from K. bohemica from the Bohemian Cenomanian in possessing a higher number of sporangia per sorus (12–14 in K. bohemica), in the apparent absence of any indusium, and in having pinnules distinctly separated and attached to the rachis through petiolules. Thickly cutinised cells of the annulus (Fig. 3A3) are similar to those of Konijnenburgia bohemica (Kvaček and Dašková 2010). The seemingly lacking indusium is considered here as a weak distinguishing character due to its tendency to fall off during the ripening of spores in modern species of Matoniaceae (van Konijnenburg-van Cittert 1993). Separated pinnules with petiolules occur in the type species K. latifolia from the Cenomanian of Greenland (Kvaček and Dašková 2010); however, this character can be variable within a single frond. Due to poor preservation, especially of spores, an open nomenclature is used.

The discussed fern is sometimes labelled as “Gleichenia dresleriana Goeppert” in the collections; the name appears also in floristic lists in Williger (1882) and Milewicz (1997). However, the name Gleichenia dresleriana Goeppert is a nomen nudum because no diagnosis has ever been published.

Order Cyatheales Frank, 1877

Family unknown

Genus Protopteris Sternberg, 1838

Type: Protopteris punctata (Sternberg, 1820) Presl in Sternberg, 1838 ≡ Lepidodendron punctatum Sternberg, 1820; Peruc-Korycany Formation, Cenomanian, Upper Cretaceous; Kounice, Bohemia.

Protopteris punctata (Sternberg, 1820) Presl in Sternberg, 1838

1820 Lepidodendron punctatum; Sternberg 1820: 20, 23, pl. 4: 1.

2013 Protopteris punctata (Sternberg) C. Presl in Sternberg; Greguš et al. 2013: 72–73, pl. 1: 1–8; pl. 2: 1 [ubi syn.].

Material.—Unknown locality in the Lwówek Śląski area, Assemblage 3, Coniacian: MGUWr 7398p.

Description.—Sandstone cast of a stem showing helically arranged leaf scars with typical traces of vascular bundles and adventitious roots among them. For a detailed description see Greguš et al. (2013).

Remarks.—The exact provenance of the stem fragment MGUWr 7398p, which is the only specimen of P. punctata from Silesia, is uncertain. It is labelled “Löwenberg” (now Lwówek Śląski), but possibly this should be understood rather as an indication of a region, and not of a precise locality. It is interesting to note, however, that it is quite unlikely that the age of MGUWr 2885p be Cenomanian, but rather either Turonian or Coniacian (Greguš et al. 2013); it is thus younger than all Bohemian material of this species.

Stratigraphic and geographic range.—Cenomanian, Bohe­mia; Coniacian, Silesia (Greguš et al. 2013: 72).

Protopteris singeri (Goeppert, 1836b) Presl in Sternberg, 1838

1836 Caulopteris singeri; Goeppert 1836b: 449, pl. 41: 1, 2.

2013 Protopteris singeri (Göppert) C. Presl in Sternberg; Greguš et al. 2013: 73–74; pl. 2: 2–5 [ubi syn.].

Material.—Żeliszów, Assemblage 3, Coniacian: MGUWr 2885p.b (holotype), MGUWr 2885p.a.

Description.—Sandstone casts of stems covered by helically arranged leaf scars. For a detailed description see Greguš et al. (2013).

Remarks.—This species is known solely from two specimens. According to the results of a more detailed field investigation, their age, given as Turonian–Coniacian by Greguš et al. (2013), is more probably Coniacian.

Stratigraphic and geographic range.—Type locality only.

Order and family unknown

Genus Cladophlebis Brongniart, 1849

Type: Cladophlebis albertsii (Dunker, 1846) Brongniart, 1849 ≡ Neuropteris albertsii Dunker, 1846; Lower Cretaceous, northern Germany.

Remarks.—It should be noted that C. albertsii, the type of the genus, has petiolulate (“neuropteridic”) pinnules. The original specific diagnosis is somewhat confused on that matter, referring to “pinnulis… sessilibus” (Dunker 1846: 8). It is clear, however, that this should not be understood as meaning sessile pinnules, as the description of the shape of the base follows: “basi rotundatis vel subcordatis”. The figure showing single points of attachment of pinnules to the rachis (Dunker 1846, pl. 7: 6a) is also clear, despite the very short petiolule.

It follows that the genus name Cladophlebis should not be applied to fernlike foliage with broad-based pinnules, as was done, among others, by Harris (1961) and Miller and Hickey (2008). A complete revision of Cladophlebis is, however, beyond the scope of the paper.

Cladophlebis sp. 1

Fig. 4B.

Material.—Rakowice Małe, Assemblage 5, late Coniacian–early Santonian?: MB.Pb.2018/0067.

Description.—The available material consists of two specimens, one (Fig. 4B) relatively small-sized but sufficient to partly decipher the architecture of the frond, the other showing solely two pinnules.

Frond bipinnate (preserved length ca. 20 mm, preserved width ca. 17 mm), rachis of the (n – 1)-th order ca. 1.5 mm thick, pinnulae inserted on rachises of both n-th and (n – 1)-th order; the two inserted on the rachis of the (n – 1)-th order lanceolate, the single one entirely preserved among those on the rachis of n-th order with rounded apex. Angle between the midvein of the pinnule and the rachis 50–90° (the difference between two pinnules on either side of the rachis). Pinnules shortly petiolulate, with a broad base, straight midvein and forking secondaries, 2.5–3.5 times as long as wide.

Remarks.—The fragmentary character of the studied material precludes any detailed comparison. Cladopteris alber­tsii is generally similar to the material from Rakowice Małe, with the exception of apparently possessing more curved midveins. Cladophlebis frigida (Heer, 1882) Seward, 1926, from the Lower Cretaceous of Greenland has longer pinnules (Heer 1922: pl. 10: 1–4). Cladophlebis sp. from the lower Maastrichtian? of the southern border of the Holy Cross Mountains (Central Poland) has elliptic pinnules (Halamski 2013). In Cladopteris gosauensis Kvaček and Herman in Herman and Kvaček, 2010, from the Campanian of Grünbach pinnules are sessile and their length-to-width ratio does not exceed 2 (Herman and Kvaček 2010).

Cladophlebis? sp. 2

Fig. 4A.

Material.—Żeliszów, Assemblage 5, upper Coniacian?–lower Santonian?: MGUWr 7556p.

Description.—The available pinna fragment consists of two nearly oppositely arranged pinnules. Each pinnule is lanceolate in shape, ca. 8 mm long and 2–3 mm wide, with broad slightly decurrent base and acute apex. Venation obscured by carbonaceous matter.

Remarks.—Cladophlebis? sp. 2 differs from Cladophlebis sp. 1 in having acute apices of pinnulae, decurrent bases, and suboppositely arranged pinnulae. The fragmentary character of the studied material precludes any detailed comparison like in the case of Cladophlebis sp. 1. Similarities with fronds of “Sphenopteris” dubia (Velenovský, 1888) Kva­ček and Halamski in Halamski and Kvaček, 2016, and Anemia fremontii Knowlton, 1917, can be noted, but in Cla­do­phlebis? sp. 2 pinnulae arrangement on the rachis is subopposite.

Genus Coniopteris Brongniart, 1849

Type: Coniopteris murrayana (Brongniart, 1835) Brongniart, 1849 ≡ Pecopteris murrayana Brongniart, 1835; Jurassic, Yorkshire, United Kingdom.

Remarks.—Coniopteris was interpreted as a representa­tive of the Dicksoniaceae by Harris (1961). Kvaček and Manum (1993) applied the fossil-genus name Coniopteris to their specimen because of difficulties in distinguishing between species belonging to the Dennstaedtiaceae and the Dicksoniaceae. Li et al. (2020) interpreted Coniopteris as a stem group of Polypodiales.

Coniopteris? sp.

Fig. 4C.

Material.—Rakowice Małe, Assemblage 5, upper Conia­cian?–lower Santonian?: MB.Pb.2018/0006.

Description.—The only available specimen consists of three pinnae of last order arranged parallel to each other in a way suggesting they were attached to a common axis; the organic connection with a tiny fragment of rachis of the (n – 1)-th order is preserved, but is so small, that the direction of branching cannot be verified.

Frond at least bipinnate, branching catadromous?, preserved length of pinnae of the n-th order up to 25 mm. Pinnules small, trilobately dissected, 3–5 mm long and 2–3 mm wide; the terminal lobe of each pinnule always larger than the lateral ones. The first (catadromous) pinnule at the base of a pinna of the n-th order subcircular in shape. Venation difficult to observe.

Remarks.—The pinnules of the described fern are intermediate in shape between those of Coniopteris hymenophylloides (Brongniart, 1828) Seward, 1900, and C. murrayana from the Middle Jurassic of Yorkshire (Harris 1961). However, both have first pinnules of a pinna developed into aphlebioid filiform processes (van Konijnenburg-van Cittert and Morgans 1999), which is not the case in the studied material.

Division Gymnospermae (Lindley, 1830) Prantl, 1874

Class Coniferae (Jussieu, 1789) Engler, 1892

Order Pinales Gorožankin, 1904

Family Pinaceae Lindley, 1836

Genus Pinus Linnaeus, 1753

Type: Pinus sylvestris Linnaeus, 1753; Recent, Eurasia.

Pinus longissima Velenovský, 1885

Fig. 5G.

1882 Pinus Quenstedti Heer; Williger 1882: 84.

1885 Pinus longissima m.; Velenovský 1885: 29–30, pl. 1: 14–17.

Material.—Wartowice, Assemblage 2, Coniacian: MB.Pb. 2008/0337.

Description.—Ovuliferous cone 180 mm long and up to 25 mm broad, consisting of numerous helically arranged cone-scales, each scale bearing a distally diamond-shaped apophysis (escutcheon) with umbo. Some cone-scales apparently with two seeds on the adaxial side.

Remarks.—The described specimen bears a manuscript label by Heinrich R. Goeppert saying “Pinus longissima Goepp.”; this name, however, has never been validly published. Velenovský (1885) used the epithet longissimus (“the longest” in Latin) for the description of a Cenomanian ovuliferous cone from Kralupy nad Vltavou in Bohemia (Velenovský 1885: pl. 1: 14–17). The Coniacian cone from Wartowice belongs to the species described from the Bohemian Cenomanian. The oldest representatives of the modern genus Pinus are known from the Cretaceous (Miller 1988; Ryberg et al. 2012, Kvaček 2013b; Falcon-Lang et al. 2016).

Stratigraphic and geographic range.—Cenomanian, Bohe­mia (Dijkstra 1973: 665 and references therein); Conia­cian, Silesia (this paper). A poorly preserved specimen from the Lower Greensand (Aptian) of Maidstone, England was compared to this species by Stopes (1915: 141); this was misindexed as an indication of the presence of this species in England by Seward (1919: 385).

Family Cupressaceae Gray, 1821

Genus Protodammara (Hollick and Jeffrey, 1906) Mays and Cantrill, 2018

Type: Protodammara speciosa Hollick and Jeffrey, 1906; Rari­tan Formation, Turonian?, Upper Cretaceous; Kreischerville, Staten Island, New York, USA.

Protodammara sp.

Figs. 2C, 5D, F.

Material.—Rakowice Małe, Assemblage 5, upper Conia­cian?–lower Santonian?: MB.Pb.2008/0249, 2018/0078.

Description.—Several ovuliferous cone scales on a bedding plane. Each cone scale 10–12 mm broad and 10–15 mm long, peltate, with resin ducts, 7–9 per cone scale. Head of each scale roundish, adaxially bearing 7–9 scar-like structures.

Remarks.—In the studied material no seed is attached to the cone scale, so it is not clear whether the scar-like structures are genuine seed attachment scars or only ridges of the cone scale surface. Similar isolated cone scales from the Bohemian Cenomanian were reported by Velenovský (1885) as Dammara borealis Heer, 1882 (JK, unpublished data). Morphology of the cone scales, particularly the arrangement of resin ducts, resembles that in the genus Doliostrobus Marion, 1884 (Bůžek et al. 1968; Kvaček 1971), a member of the family Doliostrobaceae Kvaček, 2002. The present material differs from Doliostrobus in lacking an apical spiny process.

Family unknown

Genus Geinitzia (Endlicher, 1847) Harris, 1979

Type: Geinitzia reichenbachii (Geinitz, 1842) Hollick and Jeffrey, 1909 ≡ Araucarites reichenbachii Geinitz, 1842; Cretaceous, Saxony, Germany.

Geinitzia reichenbachii (Geinitz, 1842) Hollick and Jeffrey, 1909

Fig. 5A–C.

1842 Araucarites reichenbachii; Geinitz 1842: 98. pl. 24: 4.

1909 Geinitzia reichenbachii; Hollick and Jeffrey 1909: 38; pl. 5: 7–10, pl. 8: 3, 4, pl. 16: 2–4; pl. 17: 1–4, pl. 18: 1–4.

2009 Geinitzia reichenbachii (Geinitz 1842) Hollick et Jeffrey 1909; Bosma et al. 2009: 489–490, figs. 3D, 4G, H [ubi syn.]

2018 Geinitzia reichenbachii (Geinitz, 1842) Hollick et Jeffrey 1909; Halamski et al. 2018a: 128; pl. 2: 6, 9.

Material.—Lwówek Śląski, Assemblage 1, Turonian: MB.Pb. 2018/0028 (Lettengrube bei Löwenberg, Slg. Dres­ler 1909, Turonmergel 29. Juli 1898). Huzarski Skok, Assem­blage 4, upper Conia­cian?–lower Santonian?: MB.Pb.2018/0064. Rako­wice Małe, Assemblage 4, upper Conia­cian?–lower San­tonian?: MB.Pb.2008/0240, 0252, 0254. Ołdrzychów, Assemblage 5, upper Conia­cian?–lower Santonian?: MB.Pb. 2008/0265–0267, 2018/0024.1–3, 0025.1–2; MGUWr 5638p, 5615p; MMG PnK 36, 37. Rakowice Małe, Assemblage 5, upper Conia­cian?–lower Santonian?: MB.Pb.2008/0239, 0241 (coll. Dres­ler?), 0242 (coll. Schäfer), 0246 (coll. Dresler 1909), 0248, 0253, 0363, 2018/0069.1–10, 2018/0070.3–4, 0071.1–12, 0073.1–31, 0074.1–6, 0075.1–20. Żeliszów, Assemblage 5, upper Conia­cian?–lower San­to­nian?: MB.Pb.2008/0251a; Assemblage 5, upper Conia­cian?–lower Santonian?: MB.Pb. 2008/0316, 317 (coll. Klotzsch). Rakowice Małe, Assemblage 6, lower–middle Santonian: MB.Pb.2008/0244. Wło­dzice, Assemblage 6, lower–middle Santonian: MGUWr 5594p, 5649p. Bolesła­wiec, Assemblage 8, lower–middle Santonian: MB.Pb.2018/0049. Luisenhain, Assemblage 8, lower–middle Santonian: MB.Pb.2018/0043, 0044. Dobra, Assemblage 8, lower–middle Santonian: MGUWr 5614p. Uncertain locality, Assemblage 8, lower–middle Santonian: MB.Pb.2018/0042.

Description.—The available material consists of numerous twig fragments ca. 1 mm thick and up to ca. 5 cm in length (Fig. 5C), but usually shorter. Leaves helically arranged, spreading from axes at an angle of 20–40°, basally not contracted, falcate, up to 13 mm long (Fig. 5B), with acute apices.

Remarks.—Geinitzia reichenbachii is one of the most common conifers in the Upper Cretaceous of Europe, possibly representing more than one biological species. In the studied material it is the most abundant taxon in terms of the number of specimens and is present in the Turonian, Coniacian, and Santonian. In adjacent areas it is known from the Turonian of Silesia (Roemer 1886; Płachno et al. 2018), Coniacian of the Kłodzko region and Bohemia (Halamski and Kvaček 2015, 2016; Halamski et al. 2018a), Campanian of Grünbach in Austria (Herman and Kvaček 2010), and Campanian and Maastrichtian of eastern Poland and western Ukraine (Halamski 2013; see also Kunzmann 2010).

Stratigraphic and geographic range.—Late Cretaceous; Europe, North America.

Geinitzia cf. formosa Heer, 1871

Fig. 5E.

Material.—Rakowice Małe, Assemblage 5, upper Conia­cian?–lower Santonian?: MB.Pb.2008/0245 (coll. W. Zimmer 1912), MB.Pb.2008/0247 (coll. W. Zimmer 1919), MB.Pb.2008/0250 (coll. W. Zimmer 1911), MB.Pb.2018/0070.1–2.

Description.—The available material consists of longitudinal sections of female cones appearing on broken rock slabs.

Ovuliferous cones incompletely preserved, subcylindrical in shape, in the best preserved specimen (Fig. 5D) width ca. 13 mm, preserved length ca. 25 mm. Cone scales arranged helically, of conical shape. Seeds not observed.

Remarks.—The described ovuliferous cones are similar in architecture and shape to Geinitzia formosa described from the Santonian of Quedlinburg (Kunzmann 1999). The diagnosis of G. formosa includes seed shape, a character that cannot be checked in the studied material, hence open nomenclature is applied. Geinitzia schlotheimii Heer, 1871, from the Santonian of Aachen has ovoid (less elongate) cones (Kunzmann et al. 2003) and peltate to truncate scales (Halamski and Kvaček 2015). Fricia nobilis Velenovský, 1885, from the Turonian of Bohemia has larger ovoid cones (Kvaček 2013a).

Division Angiospermae Braun and Doell ex Doell, 1857

Class Dicotyledoneae de Candolle, 1817

Supersubclass Eudicotyledoneae Doyle and Hotton ex Halamski, 2013

Subclass Ranunculidae Takhtajan ex Reveal, 1992 emend. nov.

Remarks.—The paraphyletic group of eudicots consisting of the Ranunculales, Proteales (incl. Platanales), and Buxales is usually referred to by various informal names, for example “non-core eudicots”. An available name under the ICN is the subclass Ranunculidae Takhtajan ex Reveal, 1992.

Order Proteales Jussieu ex Berchtold and Presl, 1820

Family Platanaceae Lestiboudois, 1826

Genus Platananthus Manchester, 1986

Type: Platananthus synandrus Manchester, 1986, middle–upper Eocene, Oregon, USA.

Platananthus sp.

Fig. 6.

Material.—Żerkowice, Assemblage 5, upper Coniacian?–lower Santonian?: MB.Pb.2008/0251a.

Description.—Globular reproductive structure 10×12 mm consisting of radially arranged units interpreted here as staminate flowers ca. 5 mm long, with well-developed tepals, each up to 1.5 mm in width. Stamens are poorly preserved.

Remarks.—In shape and size the described specimen resembles isolated reproductive units from the Bohemian Cenomanian described as Platanathus sp. (Kvaček 2003). Knobloch and Mai (1986, 1991) described male and female reproductive structures of Platanus richteri Knobloch and Mai, 1986, from the Santonian of Quedlinburg, Saxony-Anhalt, Germany, both of which are, however, significantly smaller than the studied material.

Subclass Rosidae Takhtajan, 1967 sensu Soltis et al. (2018)

Order Fagales Engler, 1892 sensu Soltis et al. (2018)

Family unknown

Genus Dryophyllum (Debey in de Saporta, 1865) Jones, Manchester, and Dilcher, 1988

Type: Dryophyllum subcretaceum Debey ex de Saporta, 1865; Eocene, Sézanne, France.

Remarks.—This genus is used here as a fossil genus of the Fagales sensu lato, as argued in detail in Halamski and Kvaček (2015: 109–110).

Dryophyllum westerhausianum (Richter, 1904) Halamski and Kvaček comb. nov.

Figs. 7–9, 15C.

1904 Bignonia Westerhausiana n. sp.; Richter 1904: 20, pl. 2: 1–6.

non 1977 Dewalquea westerhausiana; Rüffle and Knappe 1977: 279, pl. 4: 1.

Basionym.—Bignonia westerhausiana Richter, 1904 (Rich­ter 1904: 20; pl. 2: 1–5; see Appendix 4).

Material.—Otok, Assemblage 6, lower–middle Santonian: MB.Pb.2008/0262, 2018/0039. Rakowice Małe, Assem­blage 6, lower–middle Santonian: MB.Pb.2008/0256. Ulina, Assemblage 6, lower–middle Santonian: MGUWr 1699p.b, 1715p, 2707p, 2709p, 5593p, 5616p.a, 5617–5619p, 5637p, 5651p (mostly coll. Goeppert), MB.Pb.2008/0346, 0360, 0368, 2018/0029, 0045.

Description.—Leaf compound, trifoliolate (Fig. 8E). Leaf­lets notophyll to mesophyll (maximal recorded length ca. 10 cm, Fig. 9C; estimated total length over 15 cm), petiolulate, blade attachment marginal; base shape decurrent; apex poorly preserved, straight (Fig. 8A, C). Blade shape oblong, seldom ovate, length-to-width ratio ca. (3.5–)4–5(–6). Margin unlobed, serrate. Teeth regularly spaced, ca. 1–2 per cm, sinus shape rounded, proximal flank flexuous, distal flank concave (Fig. 9A, B).

Primary venation pinnate, midvein strong. Major secondaries craspedodromous, spacing irregular, 1–4 per 2 cm, attachment excurrent, angle to midvein variable, 50–70(–80°). Intersecondaries none. Tertiaries percurrent, straight to sinuous (Fig. 9B). Quaternaries poorly preserved, reticulate?

Remarks.—The discussed species is included in Dryo­phyllum on account of several architectural features, among which marked asymmetry of lateral leaflets (Halamski and Kvaček 2015: pl. 4: 1, 3, 4) and lack of intersecondaries allow the distinction with Debeya Miquel, 1853. The type species of the latter, Debeya serrata Miquel, 1853, from the Maastrichtian of Kunrade (Limburg, Netherlands), possesses numerous intersecondaries (Miquel 1853: pl. 1: 1) and lateral leaflets differing only weakly from the median one.

Rüffle and Knappe (1977) interpreted Bignonia westerhausiana Richter, 1904, as a platanoid. However, such an interpretation is based on a specimen from another locality (not given, but not Westerhausen; Rüffle and Knappe 1977: 279) and of manifestly different architecture (pentafoliolate and not trifoliolate; Rüffle and Knappe 1977: pl. 4: 1), so is likely to be erroneous.

Coniacian Dryophyllum geinitzianum (Goeppert, 1844) Halamski and Kvaček, 2015, is very similar to the discussed species in leaf architecture, venation pattern, and serration of the margin; the main difference is in the leaflets of the former being less elongate (length-to-width ratio 2.5–4; Halamski and Kvaček 2015). The similarity of D. westerhausianum to D. geinitzianum was stressed already by Richter (1904: 20).

Ternstroemites longifolius (Friedrich, 1883) Rüffle and Krutzsch, 2005, from the Maastrichtian of Eisleben has simi­lar serration of the margin, but secondaries are much denser and brochidodromous. It is possible that Aralia veatchii Knowl­ton, 1917, from the Frontier Formation of Wyoming should be interpreted as a trifoliolate leaf (see especially Knowlton 1917: pl. 39) analogous to Dryophyllum westerhausianum.

“Dryandroides” quercinea Velenovský, 1883, descri­bed from the Coniacian of Česká Lípa is distinguished from Dryophyllum by narrower leaves with stronger teeth (Halamski and Kvaček 2016) and the presence of intersecondaries. For a discussion on the ecological segregation of the two species, see below (group Fagofolia, Dryandroides).

Stratigraphic and geographic range.—Saxony, Westers­hausen (Santonian); Lower Silesia, Assemblage 4 (a single specimen; upper Coniacian?–lower Santonian?) and Assem­blage 6 (lower–middle Santonian).

Subclass, order, and family unknown

Remarks.—As shown by Halamski (2013), compound leaves are typical of many eudicots. However, this feature alone does not allow any closer systematic distinction, even between basal and core eudicots, and says nothing about subclass- or order-level placement.

Debeya group sensu Krassilov et al. (2005)

Remarks.—Similarities among Late Cretaceous and Paleo­gene pedate, palmate, and trifoliolate compound leaves were observed by several authors (see historical account in Krassilov et al. 2005: 124–125), but taxonomic treatments and palaeobiological interpretations diverged widely. Rather than using a widely understood and manifestly artificial grouping, we follow Krassilov et al. (2005) in recognising an informal Debeya group encompassing a few fossil-genera with several species, but excluding species of globally similar morphology, yet distinguished by minute morphological details believed to be of taxonomic significance.

A palaeobiological interpretation of Cretaceous leaves without attached reproductive structures is largely hypothetical, but two suppositions on the systematic placement of the Debeya group that have been argued for in most detail (Platanales: Crane 1989; Ranunculales: Krassilov et al. 2005: 126) are as a matter of fact easily reconcilable, insofar as the two above-mentioned orders are phylogenetically very close to each other. It might thus be supposed that the Debeya group belongs to extinct representatives of basal eudicots (herein subclass Ranunculidae). It would, however, be premature, to formally propose such a systematic treatment. The species to be excluded from the Debeya group as understood herein are those interpreted as members of the Chloranthaceae (Cenomanian of Bohemia; JK, unpublished data; see also Halamski 2013: 419) or of the Fagales (see above).

The oldest undisputed representatives of the Debeya group are from the Turonian of Negev (Israel; Krassilov et al. 2005) and the youngest uncontested ones are from the Paleocene. However, similar plants in need of revision were reported from strata as old as Cenomanian and as young as Oligocene (Crane 1989 and references therein).

Genus Dewalquea de Saporta and Marion, 1873

Type: Dewalquea haldemiana Debey ex de Saporta and Marion, 1873; Campanian, Upper Cretaceous, Haldem, Westphalia.

Remarks.—Dewalquea was treated either as a separate genus (de Saporta and Marion 1873) or subgroup of Debeya (Knobloch 1964; Halamski 2013). Krassilov et al. (2005) stressed the necessity of fine distinctions within the Debeya group, for which reason the genus rank is adopted here.

The tertiaries of D. haldemiana, the type species, are ramified (Halamski and Kvaček 2013). Species with simi­lar leaf architecture but with percurrent tertiaries, like Dewalquea paulinae (Halamski, 2013) Halamski comb. nov. [basionym: Debeya (Dewalquea) paulinae Halamski, 2013; Halamski 2013: 419, fig. 2B; see Appendix 4] from the upper Campanian of eastern Poland should possibly be segregated into another genus. The tertiary venation of Dewalquea insignis Hosius and von der Marck, 1880, is unknown.

The representatives of Dewalquea in the studied material are segregated into three species on account on the characters summarised in Table 1 (with the reservation that the architecture of the leaf of D. haldemiana is described on the basis of the better preserved type material, not of that from Lower Silesia)

Stratigraphic and geographic range.—Turonian, Near East (Krassilov et al. 2005); Coniacian to Paleocene, Europe; Late Cretaceous, North America (Berry 1910, 1916b; see also Crane 1989: 177). The genus (see also van der Burgh 2008: 11–12) lacks a comprehensive revision.

Dewalquea haldemiana Debey ex de Saporta and Marion, 1873

Fig. 10A–D.

1873 Dewalquea haldemiana (Araliophyllum haldemianum Deb. Ms.); de Saporta and Marion 1873: 60–61, pl. 7: 1–2.

1889 Dewalquea haldemiana; Roemer 1889: 143, in part: non fig. 12: 3.

non 2009 Debeya haldemiana; Mohr 2009: text-fig. 11.

2013 Debeya haldemiana (Debey ex de Saporta and Marion, 1873) Knobloch, 1964; Halamski 2013: 422, figs. 7B, G, 8, 9C, D, E, 10C.

2013 Debeya (Dewalquea) haldemiana (Debey ex de Saporta et Marion 1873) Halamski, 2013; Halamski and Kvaček 2013: 83–84; text-fig. 1 [ubi syn.].

2016 Debeya (Dewalquea) haldemiana (Debey ex de Saporta & Marion, 1873) Halamski, 2013; Halamski et al. 2016: 217–221; figs. 2a, e, f, 5 [ubi syn.].

Material.—Rakowice Małe, Assemblage 4, upper Conia­cian?–lower Santonian?: MB.Pb.2008/0256, 0320, 0365, 2018/0059 (coll. Schaefer), MB.Pb.2018/0060, 0063a, 0065, 0066, 0080.1–3, 0084, 0088. Żerkowice, Assemblage 4, upper Conia­cian?–lower Santonian?: MB.Pb.2018/0079; Assem­blage 5, upper Conia­cian?–lower Santonian?: MB.Pb. 2018/0058; Assemblage 7, lower–middle Santonian: MB.Pb. 2008/0344. Bolesławiec, Assem­blage 8, lower–middle San­to­nian: MGUWr 1699p.a.

Description.—Leaf compound, pedate, consisting of seven subsessile leaflets, petiole most probably present but not preserved in the studied material. Leaflet width never exceeding 10 mm, maximum preserved length 9 cm, estimated length ca. 15 cm. Base cuneate, apex not preserved. Margin unlobed, untoothed. Venation pattern pinnate, probably brochidodromous (Fig. 10D), secondaries departing at ca. 45°.

Remarks.—The material from Assemblage 4 described herein as D. haldemiana is fragmentary. Nonetheless, the coriaceous, oblong leaflets with length-to-width ratios exceeding 10 and thickened entire margins are sufficiently characteristic to be identified, like in the case of mass accumulations of leaflets of the same species in the Campanian of Scania (Halamski et al. 2016: fig. 5). The material from Bolesławiec figured by Roemer as D. haldemiana (1889) has wider leaflets and is described below as D. aff. gelindenensis; that figured by Mohr (2009) from the same outcrop has serrate margins (Fig. 10F4, F5) and is decribed below as D. insignis; however, a single genuine specimen of D. haldemiana (Fig. 10C) was found in the same outcrop as well.

Stratigraphic and geographic range.—Late Coniacian to Santonian: Lower Silesia (this work); Campanian: Westphalia (Hosius and von der Marck 1880), Scania (Halamski et al. 2016), Roztocze (Halamski 2013); Maastrichtian: Volhynia-Podolia Upland (Halamski 2013).

Dewalquea insignis Hosius and von der Marck, 1880

Figs. 10E–F, 11, 15E.

1880 Dewalquea insignis Hos. & v. d. Marck; Hosius and von der Marck 1880: 172–173, pls. 32: 111–113, 33: 109, 34: 110.

2009 Debeya haldemiana; Mohr 2009: text-fig. 11.

2013 Debeya insignis (Hosius and von der Marck, 1880) Knobloch, 1964; Halamski 2013: in part: 421–422, figs. 7A, C, 8?, 9A?, F?

Material.—Bolesławiec, Assemblage 8, lower–middle San­to­nian: MB.Pb.2008/0323, 0325; MGUWr 1699p.b, 5639p.

Description.—Leaf compound, pedate, consisting of up to presumably nine subsessile to shortly petiolulate leaflets; leaf most probably petiolate but petiole not preserved in the studied material. Leaflets lanceolate, 11–18 mm wide, in the only subcomplete specimen median leaflet 18 mm wide, then width gradually diminishing towards the external leaflets 11 mm wide; preserved length up ca. 8 cm, estimated length up to ca. 12 cm, estimated length-to-width ratio ca. 5–8. Margin serrate, teeth ca. 2 per cm (Figs. 10F4, F5, 11A2), but often not observable, proximal side straight, distal side concave. Venation pattern pinnate (Fig. 11B), camptodromous or craspedodromous (interpretation uncertain); midvein thick, secondaries departing at an angle of ca. 45–60°, then curving towards the apex, possibly sometimes entering the teeth.

Remarks.—Dewalquea insignis was described from the Campanian of Haldem (Westphalia) by Hosius and von der Marck (1880) who interpreted the original material as having leaves with serrate margins and this condition should be retained, despite the reservations expressed by Halamski (2013) when selecting the lectotype. The venation pattern of the type material is pinnate craspedodromous according to Hosius and von der Marck (1880); this character was not observable during its examination by ATH in 2012 (Halamski 2013: fig. 7A, C). The venation pattern of leaves from Lower Silesia is similar to that described by Hosius and von der Marck (1880). Dewalquea aquisgranensis de Saporta and Marion, 1873, originally described from the Aachen Formation (sables d’Aix-la-Chapelle, Robaszynski et al. 2002), the age of which is middle Santonian to probable earliest Campanian (Batten and Li 1987; Batten et al. 1988; Streel et al. 1994; the confusion resulting from dealing with a Cretaceous plant in a monograph devoted to Paleocene flora was stressed already by Stockmans 1946: 28–29), has the same leaf organisation and similarly shaped leaflets, but the venation pattern is very different, with secondaries forming numerous anastomoses (de Saporta and Marion 1873: pl. 8: 5–7). Dewalquea pulchella Knowlton, 1917, from the Frontier Formation of Wyoming (USA) is similar in shape, with the exception of leaflets being subsessile and 5(–6) in number.

The plant material from the Campanian to Maastrichtian of eastern Poland reported under D. insignis by Halamski (2013: fig. 9A, F) is entire-margined and probably represents a different species. D. haldemiana, the most common representative of Dewalquea in the studied material, has narrower and entire-margined leaflets.

Stratigraphic and geographic range.—Santonian of the Liège-Limburg Basin, Belgium and Lower Silesia, Poland.

Dewalquea aff. gelindenensis de Saporta and Marion, 1873

Figs. 12, 15A.

Material.—Bolesławiec, Assemblage 8, lower–middle San­to­nian: MGUWr 2880p (coll. Jonas 1885; figured by Roemer 1889: pl. 12: 3 as Debeya haldemiana), MGUWr 2881p (coll. F. Roemer 1886), MGUWr 6150p.

Description.—Leaves compound, pedate, petiolate, of (five to?) seven petiolulate leaflets. Petiole distally widened (Fig. 10A3). Petiolules short (never exceeding 5 mm). Leaflets symmetric, with marginal blade attachment, notophyll, up to ca. 25 mm in width, preserved length ca. 7 cm, estimated length >10 cm, estimated length-to-width ratio 4–5. The median leaflet always the widest, the lateral ones narrower; sometimes, but apparently not always, leaflet width gradually decreasing from the median leaflet towards the external ones. Base cuneate, apex possibly straight. Margin unlobed, untoothed (Fig. 10A2, XB3). Venation pattern pinnate camptodromous (Fig. 10A2); midvein stout; secondaries excurrent, departing at (45–)60–90°, gently curving, quite irregularly spaced, 1–3 per cm; finer venation not preserved.

Remarks.—The described material is distinguished from both co-occurring representatives of Dewalquea in having wider leaflets, and from D. aquisgranensis in lacking marginal serration (see Table 1).

To date, three entire-margined species of Dewalquea with more than three leaflets per leaf have been described: D. gelindenensis de Saporta and Marion, 1873, from the Paleocene of Belgium, as well as D. reniformis Krassilov in Krassilov et al., 2005, and D. gerofitica (Dobruskina, 1997) Krassilov in Krassilov et al., 2005 from the Turonian of Negev (Krassilov et al. 2005). The former is relatively close to the material described herein in leaflet shape and venation; however, the Paleocene species has always slightly emarginate apices (de Saporta and Marion 1873: pl. 9: 1, 4, 5). This character is difficult to check in plants from Lower Silesia, but a single leaflet seems to show a straight apex; one cannot be certain, however, that this is not a preservational artefact. In all other leaflets apices are not preserved. The two Turonian species differ from the material described herein in terms of leaf organisation (high divergence angle of leaflets for the former, leaf composed of four, more seldom five leaflets for the latter). To sum up, the material described here might represent a new species, but is described under open nomenclature due to insufficient preservation.

Leaves from eastern Poland described as Debeya insignis by Halamski (2013: figs. 8, 9A, F), but differing in having entire margins (see above), may represent the same species, although their preservation is rather fragmentary.

Genus Dalbergites (Velenovský, 1885) Halamski and Kvaček, 2015

Type: Dalbergites atavius (Velenovský, 1885) Halamski and Kvaček, 2015 ≡ Cassia atavia Velenovský, 1885; Coniacian, Upper Cretaceous; Idzików, Kłodzko region, Poland.

Dalbergites sp.

Fig. 17F.

Material.—Rakowice Małe, Assemblage 5, upper Conia­cian?–lower Santonian?: MB.Pb.2018/0068. Żerko­wice, As­sem­blage 5, upper Coniacian?–lower Santonian?: MB.Pb. 2018/0023.

Description.—Lamina incompletely preserved, ca. 20 mm long and 13 mm wide, medially asymmetrical. Base rounded? Apex not preserved. Venation pinnate, secondaries poorly preserved, proximally decurrent, distally excurrent(?), departing at an angle of 50–80°. Margin unlobed, untoothed.

Remarks.—Small asymmetric phyllomes are interpreted as leaflets of pinnately compound leaves (Halamski and Kvaček 2015).

Supersubclass, class, order, and family unknown

Remarks.—As argued in detail in Halamski and Kvaček (2015: 102–103) and Halamski et al. (2018a: 128), Creta­ceous angiosperm leaves are mostly described under a morphographic system, an inherently temporary, yet necessary solution (Bengtson 1985).

Form group Cinnamomophylls (Crabtree, 1987) Halamski, 2013

Fossil-genus Cinnamomoides Seward, 1925

Type: Cinnamomoides newberryi Berry, 1911 sensu Seward (1925); Upper Cretaceous, Atanekerdluk, Greenland. See Halamski (2013: 428) for a detailed discussion on the type and Halamski and Kvaček (2015: 113) for an emended diagnosis.

Cinnamomoides sp.

Fig. 17B.

Material.—Huzarski Skok, Assemblage 4, upper Conia­cian?–lower Santonian?: MB.Pb.2018/0079. Rako­wice Małe, Assem­blage 4, upper Coniacian?–lower Santonian?: MB.Pb. 2008/0364.

Description.—Leaf simple, blade shape elliptic. Base shape decurrent, apex not preserved. Venation pattern acrodromous with three main veins. Margin unlobed, untoothed.

Remarks.—The material described herein under Cinnamo­moides sp. is poorly preserved, yet easily separable from other similar taxa in the studied flora on account of trifurcate venation.

Form group Platanofolia Krassilov, 1979

Remarks.—Platanoids are relatively frequent and diversified in the studied material. They are present in Assemblages 2, 6, 7, and 8 and Platananthus sp. in Assemblage 5 (four or five out of a total of eight assemblages). Platanoid foliage is represented by four species (out of a total of 18 angiosperm foliage taxa). It is worth noting, however, that all reports of representatives of Credneria Zenker, 1833 from the Upper Cretaceous of Lower Silesia (Drescher 1863; Williger 1882; Lilpop and Kostyniuk 1957) are shown herein to be based on misidentified specimens of Ettingshausenia.

Genus Ettingshausenia Stiehler, 1857

Type: Ettingshausenia cuneifolia (Bronn, 1837) Stiehler, 1857 ≡ Credneria cuneifolia Bronn, 1837. Cenomanian, Upper Cretaceous; Niederschöna, Saxony.

Remarks.—Ettingshausenia may be understood either broadly (Maslova et al. 2005; Herman and Kvaček 2010) or narrowly (Golovneva 2011). Following arguments given by Halamski and Kvaček (2015: 119) the former intepretation is used herein.

Ettingshausenia cf. superstes (Velenovský, 1882) Kvaček and Halamski in Halamski and Kvaček, 2015

Fig. 13A–C, E.

Material.—Czaple, Assemblage 2, Coniacian: MB.Pb.2008/ 0369. Wartowice, Assemblage 2, Coniacian: MB.Pb.2008/ 0332, 0333, 0334. Zbylutów, Assemblage 2, Coniacian: MB.Pb.2008/0336.2.

Description.—The available material consists of fragments of medium-sized leaves with weakly developed lobes.

Lamina probably notophyll, in the most complete specimen (Fig. 13B2) observed length about 6.7 cm and estimated laminar length-to-width ratio about 1.5. Base sharply cuneate (Fig. 13B); lateral lobes weakly developed, incised to about one tenth of the blade (Fig. 13C, E); a single observed large lobe (Fig. 13E) interpreted as the terminal one. Venation palmately pinnate brochidodromous to camptodromous with strong basal veins emerging from leaf base. Tertiary veins percurrent (Fig. 13B1).

Remarks.—This leaf type is similar to Ettingshausenia superstes, from the Coniacian of the Bohemian Cretaceous Basin (Velenovský 1882: 15–16 [8–9], pl. 4 [2]: 7–9; Halamski and Kvaček 2015: 311–312, fig. 6I–K), but differs in having small lobes which are not preserved in the holotype. Ettingshausenia onomasta (Bayer, 1896) Kvaček and Halamski in Halamski and Kvaček, 2015, from the Coniacian of Idzików (Halamski and Kvaček 2015) differs from the studied material in having well-developed lobes, which are acute-attenuate. Ettingshausenia gruenbachiana Herman and Kvaček, 2010, from the Campanian of Austria and Ettingshausenia senonensis (Knobloch, 1964) Kvaček and Váchová, 2006, are entire-margined, yet both differ from the studied material in having well-pronounced lobes.

Ettingshausenia sp. 1

Figs. 13D, F, G, 15F, G.

Material.—Ulina, Assemblage 6, lower–middle Santonian: MGUWr 5616p.b (coll. Goeppert), MB.Pb.2008/0264, 0338.

Description.—The available material consists of subcomplete to incomplete relatively large, trilobed leaves.

Lamina notophyll to mesophyll, maximal observed length about 9 cm, laminar length-to-width ratio about 1.1 (Fig. 13G) to 1.6 (Fig. 13D). Base cuneate. Lobes incised to one seventh to one sixth of the length. Venation palmately pinnate with robust basal veins emerging from the leaf base. Secondaries excurrent, departing at 30° (Fig. 13D) to 60° (Fig. 13G). Percurrent tertiary veins poorly preserved.

Remarks.—Ettingshausenia sp. 1 differs from Ettingshau­senia cf. superstes in displaying stronger lobes. Similar­ities with Ettingshausenia onomasta from the Coniacian of Idzików (Halamski and Kvaček 2015) should be noted; however, the fragmentary character of the specimen, including in particular a poorly preserved leaf margin, precludes further comparison, so open nomenclature is used here. Variability of leaves classified here as Ettingshausenia sp. 1 is significant; it may correspond to polymorphism within a single tree, to a single variable species that cannot be further subdivided, to a single species with geographical races or ecotypes (Sell and Murrell 2018: xi), or finally to several biological species.

The specimen MGUWr 5616p (Fig. 13F) shows the co-occurrence of Ettingshausenia sp. 1 (5616p.b, lower leaf) and Dryophyllum westerhausianum (upper leaf, 5616p.a).

Genus Platanites Forbes, 1851

Type: Platanites hebridicus Forbes, 1851; Paleocene, Isle of Mull, Inner Hebrides, Scotland, UK.

Remarks.—Platanites hebridicus is a trifoliolate platanoid leaf (see Boulter and Kvaček 1989 for a detailed description). Other species, described in much detail, are the similarly trifoliolate P. marginatus (Lesquereux, 1873) Johnson, 1996, from the Upper Cretaceous and lower Ter­tiary of South and North Dakotas, Montana, Wyoming, Colorado, Utah, and Arizona (Johnson 1996) and P. raynoldsii (Newberry, 1868) Manchester, 2014, from the Paleo­cene of North America (Manchester 2014). Platanites resembles Ettingshausenia and extant Platanus, but has compound leaves. However, discriminating between compound and simple leaves can be difficult in incomplete fossils. Fragmentary specimens of Platanites can be distinguished by basal secondaries connecting between the diverging primary veins displaying a chevron pattern. Such a pattern is usually absent in Ettingshausenia and even if it does occur, the chevrons are blunt, never sharp. The poorly preserved available material does not offer any traces of the trifoliolate condition of the original leaves, which anyway is seldom preserved in the fossil record and not necessarily constant in the living plant (Manchester 2014: 166). Erlingdorfia Johnson, 1996, is another trifoliolate platanoid distinguished by strongly trilobate median leaflets and bilobate lateral leaflets.

As far as it could be checked, this is the oldest record of the genus Platanites.

Platanites willigeri Halamski and Kvaček sp. nov.

Figs. 14, 15B, 16A, B.

Etymology: In honour of Gustav Williger (1856–1937; for biographic notes see Springer 1914: 114–117, Anonymous 1937), in recognition of his contribution to the study of the Cretaceous of Lower Silesia (Williger 1882).

Type material: Holotype: MB.Pb.2008/0335, basal part of a median leaflet; designated herein (Fig. 14B). Paratype 1: MB.Pb.2008/0328, incomplete median leaflet (about two thirds of the blade, with margin, lacking base and apex) (Figs. 14A, 16A). Paratype 2: MB.Pb.2018/0054.1, a complete lateral leaflet (Fig. 14C). Both paratypes from the same horizon and probably the same locality.

Type locality: Probably Luisenhain, temporary excavations in the first half of the 20th century. In the collection the type material is labelled “Bunzlau”, but due to recent mislabelling of some specimens (see Appendix 1, entry on Luisenhain) it is unfortunately impossible to be certain about the original locality.

Type horizon: Czerna Formation, most probably lower or middle Santonian.

Material.—Luisenhain, Assemblage 8, lower–middle San­to­nian: MB.Pb.2008/0356 (coll. W. Zimmer 1913), MB.Pb. 2018/0056 (coll. W. Zimmer 1912); Assemblage 8, lower–middle San­to­nian: MB.Pb.2008/0321, 0329 (counterpart of the paratype 1); MB.Pb.2018/0046, 0048, 0050, 0051.

Diagnosis.—Leaf interpreted as trifoliolate (Fig. 15D); terminal leaflet ovate, base cuneate; margin serrate, teeth rarely spaced; venation palmately pinnate, palinactinodromous; midvein stout, two basal veins emerging from leaf base, secondary veins forming chevron pattern by interconnected secondary veins between adjacent primaries in the lower part of the lamina. Presumed lateral leaflets unlobed with pinnate venation.

Description.—The available material consists of isolated, most often incomplete laminae, interpreted as terminal (median) leaflets and in a single case a lateral leaflet belonging to a compound trifoliolate leaf, petiolate and with petiolulate leaflets.

Terminal leaflet: blade attachment marginal, laminar size probably microphyll to notophyll; laminar length-to-width ratio probably ca. 1.5–1.6; laminar shape ovate, unlobed, medially asymmetric. Base symmetrical, cuneate (Fig. 14B; concave sensu Ellis et al. 2009). Apex not preserved.

Venation of the median leaflet approximately pinnate with mostly a single primary vein (Fig. 14A), but sometimes the first secondary vein being nearly as thick as the midvein (Fig. 16A) resulting in a quasi-palmate pattern. Compound agrophic veins present. Major secondaries craspedodromous, seldom semicraspedodromous, attachment decurrent, angle approximately uniform, 40–50°, spacing apparently decreasing distally. Marginal veins probably absent. Intersecondaries mostly absent (see Remarks). Tertiaries percurrent, mostly convex, relatively sparsely spaced, angles between them and the midvein mostly acute.

Margin of the median leaflet toothed, tooth spacing irregular. Teeth 1–2 per cm, varying in size, but forming not two distinct size classes; most often supplied by a single principal vein. Sinus shape rounded. Proximal flank weakly convex, distal flank straight to concave.

Presumed lateral leaflet (Fig. 14C): lamina lanceolate in shape, laminar length-to-width ratio ca. 1.7; apex shape rounded, probably retuse; teeth regular, blunt; venation pinnate.

Remarks.—Platanoid affinities of the described leaves are undeniable on account of the venation pattern and tooth characters. Its architecture and shape show notable similarities to those of Platanites raynoldsii and Platanites marginatus of North America. From those leaves P. willigeri differs in having a less decurrent base. From Platanites hebridicus it differs in having more pronounced lobes and in the pre­sence of lateral leaflets. However, the preservation of our material is fragmentary and no specimen shows the physical connection of leaflets.

Similarities of the presumed median leaflet to Plati­meliphyllum palanense (Budantsev, 1983) Maslova, 2002, from the upper Paleocene–lower Eocene of Kamchatka (Maslova 2002: text-fig. 1; see also Maslova 2008: 1399–1400) should be noted. However, the generic diagnosis of Platimeliphyllum Maslova, 2002, includes cuticular features (see also Kodrul and Maslova 2007), so this name cannot be used for the material from the North Sudetic Basin. Another similar leaf is Protophyllum zaissanicum Romanova, 1963, from the uppermost Cretaceous (to lower Paleogene?) of Kyin-Kerish Hill in Kazakhstan (Romanova 1963; see also Kutuzkina 1974: 149, pl. 72: 1); it differs in more closely spaced leaf margin teeth.

Further leaves showing some characters in common with the laminae interpreted herein as median leaflets of a trifoliolate leaf include Late Cretaceous–Paleogene representatives of Platimelis Golovneva, 1994 that have relatively densely spaced small, symmetric teeth and cordate bases (Golovneva 1994; Moiseeva 2012). Leaves of Evaphyllum Maslova, 2003 (type and only known species E. kamchaticum Maslova, 2003, from the upper Paleocene–lower Eocene of Kamchatka (Russia); see also Maslova 2010: 1448–1449) are elliptic in shape. Leaves reported from the Coniacian to Campanian Valižgenian taphoflora of Kamchatka by Budancev (1983) as Platanus crednerioides Budancev, 1983 (Budancev 1983: pl. 22: 4), and Pseudoprotophyllum bore­ale (Dawson, 1883) Hollick, 1930 (Budancev 1983: pl. 23: 2), differ from our species, the former in having larger teeth, the latter in having agrophic veins forming a more complex system. Both Pseudoprotophyllum Hollick, 1930 and Pseudoaspidiophyllum Hollick, 1930, from the Creatceous of Alaska have peltate bases. In Viburniphyllum de Saporta, 1868, and Grewiopsis de Saporta, 1868, secondaries are more branched.

Platanophyllum Fontaine, 1889 was used by Arens and Allen (2014: 188) to accommodate simple, unlobed platanoid leaves found in the basal part of the Hell Creek Formation (Maastrichtian) in Montana (USA). Such a treatment seems inappropriate given the fragmentary character of the type material of Platanophyllum (P. crassinerve Fontaine, 1889; Potomac Group, Lower Cretaceous, Virginia, USA).

Stratigraphic and geographic range.—Assemblage 8 (lower–middle San­to­nian) at Luisenhain, Poland. Several specimens in MB are labelled “Bunzlau”, but this locality does not appear on the original labels (see Appendix 1, Luisenhain); all material of this species possessing original labels is from Luisenhain. It is uncertain whether P. willigeri is present at Bolesławiec, Poland.

Platanites sp. 1

Figs. 15D, 16C, E.

Material.—Nowe Jaroszowice, Assemblage 7, lower–middle San­to­nian: MB.Pb.2008/0268, 0344.

Description.—Leaf interpreted as trifoliolate, but in the available material only simple blades (presumably corresponding to median leaflets) are preserved. Blade attachment marginal, petiol(ul)e very long. Venation palmately pinnate. Secondaries connecting primaries in a way similar to a chevron pattern, with the angle of the secondaries being very wide (over 120°).

Remarks.—Interpretation of this fragmentary material is tentative. The similarity of the shape and architecture of the described phyllomes to those of the central leaflets of Platanites marginatus and P. hebridicus is striking. The long petiol(ul)e is also consistent with such an interpretation. However, it cannot be excluded that all specimens are distorted taphonomically in a similar way, or, in other words, they are lacking analogous parts, and that the original shape of the blade was different.

Viburnum vitifolium de Saporta and Marion, 1878, was described on the basis of a single specimen from Gelinden (de Saporta and Marion 1878: 73–75, pl. 12: 1) which is early Paleocene (Danian) in age (Kvaček 2010), and is also similar to Platanites sp. 1 described herein; differences include the margin, which is entire in our material and dentate in the Paleocene species.

Comparable leaves were described by Wolfe and Wehr (1987) from the Eocene of Republic (Washington state, USA) as Macginitiea gracilis (Lesquereux, 1872) Wolfe and Wehr, 1987. They have a similar arrangement of the basal veins, but are distinguished from the studied material by a sharp characteristic chevron pattern formed by interconnected secondaries (Wolfe and Wehr 1987; Manchester 2014) which is absent in the described material (compare Fig. 16C3 and Manchester 1986: fig. 5A–C). Members of Recent Diploclisia Miers, 1851 (Menispermaceae) are simi­lar in shape and in venation; the main veins, however, are craspedodromous (Yu and Chen 1991: pl. 22: 5, 13).

Poorly preserved MB.Pb.2008/0340, 0341, and s.n. from the same outcrop might belong here.

Form group Magnoliaephylls Crabtree, 1987

Genus Laurophyllum Goeppert, 1854

Type: Laurophyllum beilschmiedioides Goeppert, 1854; Eocene, Java.

Remarks.—We use this genus as emended by Halamski and Kvaček (2015: 114–116). The emendation of this genus by Hill (1986) is rejected as manifestly different from the intention of the first author (cuticles instead of impressions).

Laurophyllum? sp.

Fig. 16D.

Material.—Czaple, Assemblage 2, lower–middle Conia­cian: MB.Pb.2018/0022. Otok, Assemblage 6, lower–middle Santonian: MB.Pb.2018/0021. Ulina, Assemblage 6, lower–middle Santonian: MB.Pb.2008/0263, 2018/0034, 0036. Bolesławiec, Assemblage 8, lower–middle Santonian: MGUWr 5607p (coll. O. Tornier). Luisenhain, Assemblage 8, lower–middle Santonian: MB.Pb.2018/0057.1–4. Assem­blage 8, lower–middle Santonian: MB.Pb.2008/0322, 0326, 0358, 2018/0047.

Description.—Leaves simple, microphyll to notophyll (possibly up to 10 cm long), petiolate. Blade shape ovate. Base shape convex, rounded, possibly concavo-convex? Apex not preserved, possibly convex to straight with acute angle. Venation pattern pinnate, midvein stout, secondaries excurrent, angle to midvein 50–70°, their course nearly straight (weakly curving towards the apex). Margin unlobed, untoothed.

Remarks.—Rather variable, but mostly poorly preserved, long entire-margined ovate leaves are described here under the fossil-genus Laurophyllum, similarly to previous taxo­nomic treatments of Late Cretaceous Central European floras (Halamski and Kvaček 2015, 2016). If secondaries are preserved in the material studied, they differ from those in L. acuminatum (Goeppert, 1844) Kvaček and Halamski in Halamski and Kvaček, 2015, in their less curved course.

Genus Araliaephyllum Fontaine, 1889

Type: Araliaephyllum obtusilobum Fontaine, 1889; Lower Cretaceous, Virginia, USA.

Araliaephyllum? sp.

Fig. 17D.

Material.—Assemblage 6?, lower–middle Santonian: MGUWr 2704p (locality uncertain; labelled “Bunzlau”, but the specimen is in sandstone; coll. Goeppert).

Description.—The single available leaf is incomplete, preserved width ca. 41 mm, estimated width <50 mm, preserved length ca. 71 mm, estimated length ca. 78 mm. Blade attachment marginal, size notophyll; base convex, apex unknown; blade symmetrical, ovate, probably palmately lobed (trilobate), lobes probably small. Midvein stout, two main secondaries departing near the base at an angle of ca. 40°, excurrent, slightly curved admedially, interpreted as entering the lobes; in the distal part of the median lobe poorly preserved traces of weaker excurrent secondaries departing at an angle of ca. 60°. Margin entire.

Remarks.—The interpretation of this single incomplete spe­cimen is based on the assumption that the missing parts formed lateral lobes; given the size of the parts of the leaf with ­incompletely preserved margin, the lobes must have been narrow and arguably relatively short. Trilobate leaves from the Turonian–Santonian of Klikov in Bohemia were described by Němejc (1961) under Araliophyllum Ettings­hau­sen, 1868, and from the Cenomanian of Maletín in Moravia by Greguš and Kvaček (2015) under Araliaephyllum Fontaine, 1889 (for discussion of relationships between both genera see Greguš and Kvaček 2015: 330); however, in these forms the secondaries are straight and the lateral lobes are larger. Similar forms were also described by Lesquereux (1892) and by Newberry (1895) from the Upper Cretaceous of North Ame­rica. Smilacites panartius (Bayer, 1896) Halamski and Kvaček, 2015, from the Coniacian of Idzików is superficially similar in having the proximal part of the blade much wider than the distal one, but the base is hastate and there are no lobes; the venation pattern consists of seven primaries.

Form group Fagofolia Krassilov, 1979

Genus Dryandroides Unger, 1850

Type: Not selected.

Remarks.—The generic placement of the discussed species is purely conventional (Halamski and Kvaček 2016).

“Dryandroides” quercinea Velenovský, 1883

Fig. 17E.

1883 Dryandroides quercinea sp. n.; Velenovský 1883: 8 [33], pl. 2 [10]: 8a–15.

2016 “Dryandroides” quercinea Velenovský, 1883; Halamski and Kvaček 2016: 312–313; fig. 4A, B, D, E [ubi syn.].

Material.—Bolesławiec, Assemblage 8, lower–middle San­to­nian: MB.Pb.2008/0360.

Description.—The available specimen is a fragment of a leaf ca. 2 cm wide and 4.5 cm long, representing the distal part without the tip of the apex, the general form of which can, however, be reconstructed. Blade shape possibly ovate, apex acuminate. Venation pattern pinnate craspedodromous, secondaries departing at ca. 45–70°. Margin serrate.

Remarks.—This single incomplete specimen is similar to Dryophyllum westerhausianum, from which it differs, however, in the apex being acuminate and not straight. It is accommodated in the poorly known species “Dryandroides” quercinea described from the Coniacian of Bohemia (see Halamski and Kvaček 2016 for revision of the type material).

Halamski and Kvaček (2016) noted that “Dryandroides” quercinea and Dryophyllum geinitizianum do not co-occur in Bohemian Upper Cretaceous localities. In Lower Silesia the situation is similar: the only specimen of “Dryandroides” quercinea is known from the Assemblage 8, whereas Dryophyllum westerhausianum is common in Assemblage 6.

From group Rosifolia Krassilov, 1979

Genus Ternstroemites Berry, 1916a

Type: Ternstroemites eoligniticus Berry, 1916a; lower Eocene; Tennessee, USA (by subsequent designation of Andrews 1955: 249).

Remarks.—Ternstroemites was originally interpreted (Berry 1916a) as a form genus of the family Ternstroemiaceae Mirbel, 1816 (now included in the Pentaphylacaceae Engler in Engler and Prantl, 1897; at a time included in the Theaceae Mirbel, 1813, as e.g., by Wolfe and Wehr 1987: 16; see also Prince 2007). Krassilov (1979: 62) synonymised Ternstroemites with Celastrinites de Saporta, 1865. We follow the usage of Herman and Lebedev (1991: 87–88) who consider it as a valid form genus of dicots.

Ternstroemites? sp.

Fig. 17C.

Material.—Bolesławiec, Assemblage 8, lower–middle San­to­nian: MB.Pb.2018/0045.

Description.—The single available specimen consists of two laminae (Fig. 17C1), one incomplete (preserved length ca. 45 mm, preserved width ca. 20 mm) and one fragmentary, interpreted herein as leaflets of a compound leaf. Blade shape possibly elliptic, neither base nor apex preserved. Margin serrate; teeth ca. 2 per cm, acute, anteriorly directed, proximal side concave to straight, distal side concave.

Venation pattern (Fig. 17C2) pinnate brochidodromous (rarely semicraspedodromous?). Midvein stout. Secondaries rather densely and somewhat irregularly spaced, excurrent, departing at 70–90°; intersecondaries ca. one per intercostal area, departure similar to that of secondaries, disappearing about halfway to margin; tertiaries not preserved.

Remarks.—This leaf fragment is included into Tern­stroe­mites Berry, 1916a, on account of a serrate margin and a brochidodromous venation pattern with numerous intersecondaries. Four Cretaceous representatives of this genus, namely T. harwoodensis (Dawson, 1883) Bell, 1957, from the Campanian of Vancouver Island (Bell 1957) and the Coniacian of Kamchatka (Herman and Lebedev 1991), T. ripleyensis Berry, 1925, T. cretaceus Berry, 1925, and T. tennesseensis Berry, 1925, the latter three from the Ripley Formation of eastern United States (Berry 1925) are more finely serrate. Ternstroemites longifolius (Friedrich, 1883) Rüffle and Krutzsch, 2005, from the Maastrichtian of Eisle­ben (Saxony-Anhalt, Germany) has similar serration of the margin, but secondaries are much denser. It should, however, be kept in mind that such a fragment might have belonged to a leaf of very different architecture, like for example that of Araliopsoides kiensis (Baikovskaya, 1957) Golovneva in Golovneva and Nosova, 2012, from the Cenomanian of Siberia illustrated by Golovneva and Nosova (2012: fig. 8.7).

Ficonium silesiacum (Velenovský, 1885) Halamski and Kvaček, 2015, known from a single specimen from the Coniacian of Idzików, has a venation pattern with similarly numerous intersecondaries, but secondaries are camptodromous rather than brochidodromous and the margin is entire (Halamski and Kvaček 2015: text-fig. 10).

Form group unknown

Genus Salicites (Hisinger, 1837) Halamski and Kvaček, 2015

Type: Salicites? wahlbergii (Nilsson, 1832) Hisinger, 1837 ≡ Phyllites (Salix?) wahlbergii Nilsson, 1832; Campanian, Upper Cretaceous; Köpinge, Scania, Sweden.

Remarks.—The emended diagnosis of Salicites was given by Halamski and Kvaček (2015: 122); the type species was revised by Halamski et al. (2016: 222).

Salicites petzeldianus Goeppert, 1844

Fig. 17G, I.

1844 Salicites Petzeldianus; Goeppert 1844: 220.

2015 Salicites petzeldianus Goepp. 1844; Halamski and Kvaček 2015: 122–123; text-fig. 14; pl. 10: 1, 4, 6–8.

Material.—Uncertain, Bolesławiec or Luisenhain, Assem­blage 8, lower–middle Santonian: MB.Pb.2018/0052.1–2, 0054.2–3.

Description.—Leaf simple, microphyll (ca. 3–6 cm long), petiolate. Blade attachment marginal, blade symmetrical, shape elliptic; base decurrent, asymmetric; apex rounded. Venation pattern pinnate, midvein stout; secondaries probably camptodromous, their attachment excurrent, spacing decreasing distally. Margin unlobed, untoothed.

Remarks.—The described material agrees with S. petzeldianus Goeppert, 1844, in the observable characters of shape (blade and base) and venation pattern. This generalised form may, in fact, correspond to more than one biological species.

Stratigraphic and geographic range.—Coniacian, Kłodzko region; Santonian, Lower Silesia.

Genus Dicotylophyllum auct.

Type: See discussion in Halamski (2013: 429–430).

Dicotylophyllum sp. 1

Fig. 17H.

Material.—Rakowice Małe, Assemblage 5, upper Conia­cian?–lower Santonian?: MB.Pb.2018/0076.1. Żerkowice, Assem­blage 5, upper Coniacian?–lower Santonian?: MB.Pb. 2018/0058.

Description.—The better preserved specimen, MB.Pb.2018/ 0076.1 (Fig. 17H), is an incomplete microphyll leaf 26 mm long and 9 mm wide. Laminar shape approximately elliptic, blade medially symmetrical, base most probably rounded, apex straight. Primary venation pinnate; midvein stout, keeping approximately the same width from the base to the apex; secondaries excurrent, angle to midvein from 40–50° in the basal region to ca. 30° in apical region, densely spaced (ca. 9 per cm in the basal region, spacing weakly increasing distally), their course probably brochidodromous. Margin serrate, teeth ca. 9 per cm, regularly spaced, their proximal flank convex to straight, distal flank convex to concave. The other specimen is a leaf fragment with a similar margin.

Remarks.—This leaf differs from all other described herein in the tooth form. Dicotylophyllum sp. 3 sensu Halamski and Kvaček (2015) from the Coniacian of Krosnowice (Idzików beds) is similar in having closely spaced teeth, but ovate in shape.

Dicotylophyllum sp. 2

Fig. 17J.

Material.—Uncertain, Bolesławiec or Luisenhain, Assem­blage 8, lower–middle Santonian: MB.Pb.2018/0053.

Description.—The single available leaf is incomplete, preserved length 44 mm, estimated length 80 mm?, preserved width 22 mm. Blade elliptic in shape, base straight, apex not preserved. Margin entire. Venation pinnate camptodromous: proximal secondaries decurrent, distal secondaries excurrent; poorly preserved tertiaries departing from midvein between the leaf base and the first secondaries, otherwise tertiaries not observable.

Remarks.—Dicotylophyllum sp. 2 differs from Cinnamo­moides sp. in the basal venation pattern (the departure of the proximal secondaries is closer to the base in the latter) and from Salicites sp. in the variable attachment of secondaries (excurrent and decurrent within the same leaf) and greater length-to-width ratio.

Class Monocotyledoneae de Candolle, 1817

Order and family unknown

Genus Monocotylophyllum Reid and Chandler in Reid et al., 1926

Type: Not designated (see Andrews 1955: 190).

Monocotylophyllum sp.

Fig. 17A.

Material.—Uncertain, Bolesławiec or Luisenhain, Assem­blage 8?, lower–middle Santo­nian: MGUWr 5639p.b.

Description.—The available material is a leaf fragment ca. 2.5 cm wide and ca. 3.5 cm long, suggestive of a linear leaf blade. It is uncertain whether the margin is preserved. Venation consisting of continuous parallel veins, ca. 10–17 per cm.

Remarks.—Monocotylophyllum is a form genus for monocot leaves not unlike in general form as those of Recent Acorus Linnaeus, 1753 (see Bogner and Mayo 1998: fig. 1C), Typha Linnaeus, 1753 (see Mikulska 1977: pl. 595: 2), or Iris Linnaeus, 1753 (see Skwirzyńska 1990: pls. 235, 238).

Palynology

Kingdom Alveolata Cavalier-Smith, 1981

Division Dinophyta Dillon, 1963 (= Dinoflagellata Bütschli, 1885)

Genus Chatangiella Vozzhennikova, 1967 emend. Lentin and Williams, 1976

Type: Chatangiella niiga Vozzhennikova, 1967; Santonian, Upper Cretaceous; river Romanicha, Khatanga Depression, West Siberia, Russia.

Chatangiella verrucosa (Manum, 1963) Lentin and Williams, 1976

Fig. 18M.

Remarks.—A single specimen found in sample 1338 from Rakowice Małe. Known from the Cenomanian–Turonian boundary to the late Campanian (Williams et al. 2004), from the middle Cretaceous according to Williams et al. (2017: 167).

Genus Dinogymnium Evitt, Clarke, and Verdier, 1967 emend. Lentin and Vozzhennikova, 1990

Type: Dinogymnium acuminatum Evitt, Clarke and Verdier, 1967; Uhalde Formation, Maastrichtian, Upper Cretaceous; Stanislaus County, California, USA.

Dinogymnium cretaceum (Deflandre, 1936) Evitt, Clarke, and Verdier, 1967

Fig. 18L.

Remarks.—Known from the Cenomanian (Boltenhagen 1980) to the Maastrichtian (M’Hamdi et al. 2015), “?Senonian” according to Williams et al. (2017: 273). Dinogymnium sp. (Fig. 18A) has been found in samples RK-4–110, 230.

Kingdom Plantae Linnaeus, 1753 sensu Cavalier-Smith (1981)

Division Marchantiophyta Stotler and Crandall-Stotler in Crandall-Stotler and Stotler, 2000

Genus Zlivisporis Pacltová, 1961

Type: Zlivisporis blanensis Pacltová, 1961; Turonian–Santonian, ­Upper Cretaceous; Zliv-Blana, South Bohemia, Czech Republic.

Zlivisporis simplex (Cookson and Dettmann, 1958) Braman, 2001

Fig. 18X.

Remarks.—Known from the Lower Cretaceous to the ?lowest Campanian (Braman 2001).

Division Bryophyta Schimper, 1876 sensu stricto

Genus Cingutriletes Pierce, 1961 emend. Dettmann, 1963

Type: Cingutriletes clavus (Balme, 1957) Dettmann, 1963 ≡ Sphagnites clavus Balme, 1957; Donnybrook Sandstone, ?Lower Cretaceous; Murphy’s Shaft near Donnybrook, Perth Basin, Western Australia.

Cingutriletes clavus (Balme, 1957) Dettmann, 1963

Fig. 19A.

Remarks.—We use this genus as emended by Dettmann (1963) (see Jameossanaie 1987: 12).

Division Lycophyta Scott, 1909

Genus Camarozonosporites Pant ex Potonié, 1956 emend. Klaus, 1960

Type: Camarozonosporites cretaceus (Weyland and Krieger, 1953) Potonié, 1956 ≡ Rotaspora cretacea Weyland and Krieger, 1953; Carnian, Triassic; Eastern Alps, Austria.

Camarozonosporites insignis Norris, 1967

Fig. 18AB.

Remarks.—Known from the Lower Triassic (Song et al. 2000) to the Miocene (Barss et al. 1979). Representatives of Camarozonosporites Pant in Potonié, 1956, are spores of isosporous lycophytes (order Lycopodiales de Candolle ex Berchtold and Presl, 1820).

Genus Echinatisporis Krutzsch, 1959b

Type: Echinatisporis longechinus Krutzsch, 1959b; middle Eocene; Geiseltal, Saxony-Anhalt, Germany.

Echinatisporis varispinosus (Pocock, 1962) Srivastava, 1975

Fig. 18Q.

Remarks.—Known from the Berriasian (Ricketts and Sweet 1986) to the late Maastrichtian (Nichols et al. 1990). Another species from Palynoassemblage B is reported under open nomenclature as Echinatisporis sp. (Fig. 19B). Representatives of Echinatisporis Krutzsch, 1959b are microspores of heterosporous lycophytes belonging to the order Selaginellales Prantl, 1874.

Division Filicophyta Boureau, 1970

Class Leptosporangiatae von Goebel, 1881

Order Osmundales Link, 1833b

Family Osmundaceae Berchtold and Presl, 1820

Genus Biretisporites Delcourt and Sprumont, 1955 emend. Delcourt, Dettmann, and Hughes, 1963

Type: Biretisporites potoniaei Delcourt and Sprumont 1955; Wealdian, Lower Cretaceous; Hainaut, Belgium.

Biretisporites cf. deltoideus (Rouse, 1959) Dettmann, 1963

Fig. 18AH.

Remarks.—Known from the Albian (Brideaux 1968) to the Oligocene (Singh 1982).

Genus Baculatisporites Pflug and Thomson in Thomson and Pflug, 1953

Type: Baculatisporites primarius (Wolff, 1934) Thomson and Pflug, 1953 ≡ Sporites primarius Wolff, 1934; Pliocene, Freigericht mine near Dettingen a.M., Bavaria, Germany.

Baculatisporites parvopunctatus Weyland and Greifeld, 1953

Fig. 19C.

Remarks.—Reported from the Albian (Burger 1980) to the Eocene (Krutzsch 1959b). Spores belonging to Bacu­lati­sporites Thomson and Pflug, 1953 were probably produced by osmundaceous ferns.

Order Gleicheniales Link, 1833a

Family Gleicheniaceae Presl, 1825

Genus Glecheniidites Cookson, 1953 emend. Brenner, 1963

Type: Glecheniidites senonicus Ross, 1949; upper Santonian or lower Campanian, Upper Cretaceous; Åsen, Kristianstad Basin, Scania, Sweden (see Skarby 1964).

Glecheniidites circiniidites (Cookson, 1953) Brenner, 1963

Fig. 18W.

Remarks.—Found in sample RK-4, almost all depths. Reported from the Toarcian (Tchoumatchenco et al. 1992) to the Quaternary (Truswell 1987).

Genus Clavifera Bolkhovitina, 1953 emend. Bolkhovitina, 1966

Type: Clavifera triplex (Bolkhovitina, 1953) Bolkhovitina, 1966 ≡ Gleichenia triplex Bolkhovitina, 1953; Aptian, Lower Cretaceous; Moscow region, Russia.

Clavifera triplex (Bolkhovitina, 1953) Bolkhovitina, 1966

Fig. 19K.

Remarks.—Known from Cretaceous to Paleogene (Bolkho­vitina 1966).

Genus Foveogleicheniidites Burger, 1976

Type: Foveogleicheniidites confossus (Hedlund, 1966) Burger in Norvick and Burger, 1976 ≡ Gleicheniidites confossus Hedlund, 1966; Woodbine Fm., Cenomanian, Upper Cretaceous; Bryan County, Oklahoma, USA.

Foveogleicheniidites sp.

Fig. 19O.

Remarks.—Representatives of Foveogleicheniidites Burger in Norvick and Burger, 1976 are known from the Barremian (Burger 1988) to the early Miocene (Macphail and Truswell 2004).

Order Schizaeales Schimper, 1869

Family Schizaeaceae Kaulfuss, 1827

Genus Appendicisporites Weyland and Krieger, 1953

Type: Appendicisporites tricuspidatus Weyland and Greifeld, 1953; Santonian, Upper Cretaceous; Aachen area, Nordrhein-Westfalen, Germany.

Appendicisporites appendicifer (Thiergart, 1942) Krutzsch, 1959b

Fig. 18AA.

Remarks.—Described from Rakowice Małe (Thiergart 1942), most probably from levels corresponding to our Assemblage 5 in which we have found, however, only fragmentary material of this characteristic species. The best specimen, illustrated herein, is from sample 1334. Slightly younger specimens (our Assemblages 6–8) were illustrated by Raniecka-Bobrowska (1984, 1989: pl. 205: 3) and by Grabowska (2003: pl. 28: 27). This species is rarely, but consistently, found in various Cenomanian deposits of the Bohemian Cretaceous Basin (Svobodová 1997) and by Góczán and Siegl-Farkas (1990) in Santonian or Campanian Oculopollis zaklinskaiae–Tetracolporopollenites (Brecolpi­tes) globosus Zone of Hungary.

Appendicisporites foveolatus (Deák, 1962) Wingate, 1980

Fig. 18Z.

Remarks.—The oldest occurrences are from the upper Albian (Wingate 1980).

Appendicisporites cristatus (Markova in Ivanova and Markova, 1961) Pocock, 1964

Fig. 18AG.

Remarks.—Found in almost all samples from section RK-4. Known from the Lower Triassic (Song et al. 2000) to the Danian (Shugaevskaya 1978).

Genus Cicatricosisporites Potonié and Gelletich, 1933

Type: Cicatricosisporites dorogensis Potonié and Gelletich, 1933; Eocene, Dorog, Hungary.

Cicatricosisporites potomacensis Brenner, 1963

Fig. 19D.

Remarks.—Originally described from the Lower Creta­ceous of Maryland (USA), but reported since from the Valanginian–Barremian of Israel (Brenner and Bickoff 1992), the Campanian (Srivastava 1975; Miki 1977) and even the Danian (Hargrove and Engelhardt 1997).

Cicatricosisporites dorogensis Potonié and Gelletich, 1933

Fig. 19N.

Remarks.—Originally described from the Eocene, but subsequently reported from the Valanginian–Barremian of Israel (Brenner and Bickoff 1992).

Genus Klukisporites Couper, 1958

Type: Klukisporites variegatus Couper, 1958; Lower Deltaic subseries, Bathonian, Middle Jurassic; Yorkshire, England.

Klukisporites pseudoreticulatus Couper, 1958

Fig. 19E.

Remarks.—Reported by Kemp (1970) from the Albian of Southern England (UK). The oldest occurrence might be in the Aalenian (Boulter and Windle 1993) or even the Toarcian (Goryacheva et al. 2018) and the youngest in the Campanian (Gies 1972).

Genus Distaltriangulisporites Singh, 1964 emend. Singh, 1971

Type: Distaltriangulisporites perplexus (Singh, 1964) Singh, 1971; Lower Cretaceous; Mannville, Alberta, Canada.

Distaltriangulisporites perplexus (Singh, 1964)
Singh, 1971

Fig. 19G.

Remarks.—Originally described from the Lower Cretaceous of Alberta (Singh 1964); present in the same area in the Santonian–Campanian (Payenberg et al. 2002).

Genus Trilobosporites Pant ex Potonié, 1956

Type: Trilobosporites hannonicus (Delcourt and Sprumont, 1955) Potonié, 1956 ≡ Concavisporites hannonicus Delcourt and Sprumont, 1955; Wealdian, Lower Cretaceous; Hainaut, Belgium.

Trilobosporites sp.

Fig. 19F.

Remarks.—Representatives of this genus are reported from the Berriasian (Batten 1973) to the Santonian (Knauer and Siegl-Farkas 1992).

Genus Corniculatisporites Bolkhovitina, 1953 emend. Kuvaeva, 1972

Type: Corniculatisporites alekhinii (Bolkhovitina, 1953) Kuvaeva, 1972; Campanian, Upper Cretaceous; Ural Mts.

Corniculatisporites alekhinii (Bolkhovitina, 1953) Kuvaeva, 1972

Fig. 18AI.

Remarks.—A monolete schizaeaceous spore, originally described from Campanian strata of northern Urals, then by Kuvaeva (1972) from the upper Albian of Caucasus and Crimea and by Juhász (1977) from upper “Vraconian” (upper Albian to lower Cenomanian; Gignoux 1950; Czaplicka et al. 1968) of Bákony Mountains, Hungary.

Order Cyatheales Frank, 1877

Genus Cyathidites Couper, 1953

Type: Cyathidites australis Couper, 1953; Ohika beds, Jurassic; Buller Gorge, West Coast, New Zealand.

Cyathidites minor Couper, 1953

Fig. 18AF.

Remarks.—Originally described from Jurassic Ohika beds of New Zealand (Couper 1953: 28), known from the Upper Triassic to the Upper Cretaceous (Ziaja 2006: 13).

Order Polypodiales Link, 1833b

Genus Verrucatosporites Pflug and Thomson in Thomson and Pflug, 1953

Type: Verrucatosporites alienus (Potonié, 1931) Thomson and Pflug, 1953 ≡ Sporonites alienus Potonié, 1931; Oligocene to lower Miocene; Beisselsgrube, Ville, Nordrhein-Westfalen, Germany (Potonié 1931b).

Verrucatosporites sp.

Fig. 18AE.

Remarks.—Spores belonging to Verrucatosporites Pflug and Thomson in Thomson and Pflug, 1953, were mostly produced by representatives of Polypodiales (van Uffelen 1991).

Division unknown

Genus Corrugatisporites Weyland and Greifeld, 1953

Type: Corrugatisporites toratus Weyland and Greifeld, 1953; Santonian, Upper Cretaceous; Quedlinburg, Sachsen-Anhalt, Germany.

Corrugatisporites sp.

Fig. 18AD.

Remarks.—The botanical affinity of plants producing spores belonging to Corrugatisporites Weyland and Greifeld, 1953 is unknown.

Division Gymnospermae (Lindley, 1830) Prantl, 1874

Class Coniferae (Jussieu, 1789) Engler, 1892

Genus Classopollis Pflug, 1953

Type: Classopollis classoides Pflug, 1953; Lias, Siegelsum, Holstein, Germany.

Classopollis cf. martinotii Reyre, 1970

Fig. 18AC.

Remarks.—Pollen of representatives of Cheirolepidiaceae Takhtajan, 1963. Classopollis classoides Pflug, 1953, produced by species of Frenelopsis (Schenk, 1869) Reymanówna and Watson, 1976, was found in samples RK-4-90–130, 170, 350, 410, 430, 450, 490, 530, 570.

Genus Cerebropollenites Nilsson, 1958

Type: Cerebropollenites mesozoicus (Couper, 1958) Nilsson, 1958 ≡ Tsugaepollenites mesozoicus Couper, 1958; Upper Deltaic subseries, Bathonian, Middle Jurassic; Gristhorpe, Yorkshire, England.

Cerebropollenites mesozoicus (Couper, 1958) Nilsson, 1958

Fig. 19I.

Remarks.—Produced by representatives of Pinaceae Lindley, 1836 close to modern Tsuga Carrière, 1855 (Shang and Zavada 2003).

Genus Taxodiaceaepollenites (Potonié, 1931) Kremp ex Potonié, 1958

Type: Taxodiaceaepollenites hiatus (Potonié, 1931) Kremp ex Potonié, 1958 ≡ Pollenites hiatus Potonié, 1931; Oligocene to lower Miocene; Beisselsgrube, Ville, Nordrhein-Westfalen, Germany (Potonié 1931a).

Taxodiaceaepollenites hiatus (Potonié, 1931) Kremp ex Potonié, 1958

Fig. 18P.

Remarks.—Found in almost all samples, known from the Jurassic (Wang et al. 1984) to the Miocene (Weems and McCartan 1990).

Genus Podocarpidites Cookson, 1947b emend. Potonié, 1958

Type: Podocarpidites ellipticus Cookson, 1947b; Tertiary, Waterfall Gorge, Kerguelen Islands.

Remarks.—Podocarpidites was proposed by Cookson (1947b: 131) who did not selected a type species, which was first done by Couper (1953: 35). However, before 1958 proposing a genus name without indicating the type species did not invalidate the publication (ICN, Art. 40.1), so the spelling “Podocarpidites Cookson ex Couper” (e.g., Couper 1953: 35) is incorrect. Couper (1953) and Potonié (1958) emended the diagnosis.

Podocarpidites sp.

Fig. 19P.

Remarks.—Podocarpidites Cookson, 1947b, is a genus accommodating pollen of the Podocarpaceae Endlicher, 1847. Bisaccate pollen is very rare in Palynoassemblage A and infrequent in Palynoassemblage B.

Class Gnetopsida Thomé, 1886

Genus Ephedripites Bolkhovitina, 1953

Type: Ephedripites mediolobatus Bolkhovitina, 1953; Hauterivian, Lower Cretaceous; Kazakhstan.

Ephedripites virginiaensis Brenner, 1963

Fig. 19M.

Remarks.—Representatives of Ephedripites Bolkhovitina, 1953 are present in Palynoassemblages A and B; they were produced by species of Ephedraceae Dumortier, 1829 (Ruiz and Quattrochio 1997).

Class unknown

Genus Cycadopites Wodehouse, 1933

Type: Cycadopites follicularis Wilson and Webster 1946; Maastrichtian to Paleogene, Montana, USA.

Remarks.—Cycadopites was proposed by Wodehouse (1933) without selecting the type species, the material from the Eocene Green River Fm. at Parachute Creek, Colorado, being described as Cycadopites sp. The type species from the Fort Union Fm. of Montana was selected by Wilson and Webster (1946). However, similarly as in the case of Podocarpidites described above, the authorship of the genus should be described to Wodehouse (1933), following Andrews (1955: 141) not to “Wodehouse ex Wilson and Webster”, as done, among others, by Potonié (1958: 92) or Leffingwell (1970: 28).

Cycadopites sp.

Fig. 18K.

Remarks.—Cycadopites Wodehouse, 1933, is a pollen type that can be derived from Bennettitales, Ginkgoales, Cyca­dales, Pentoxylales, and some Peltaspermales (Zavialova and van Konijnenburg-van Cittert 2012: 15 and references therein). Found in almost all samples from the section RK-4.

Division Angiospermae Braun and Doell ex Doell, 1857

Class Dicotyledoneae de Candolle, 1817

Order Fagales Engler, 1892 sensu Soltis et al. (2018)

Normapolles group sensu Polette and Batten (2017)

Genus Complexiopollis Krutzsch, 1959a emend. Tschudy, 1973b

Type: Complexiopollis praeatumescens Krutzsch, 1959a; marls with Inoceramus labiatus, lower Turonian, Upper Cretaceous; Pirna, Saxony, Germany.

Remarks.—The original spelling of the epithet is praeatumescens (by reference to the “atumescens group”; Krutzsch 1959a: 135); the spelling praetumescens (e.g., Néraudeau et al. 2017) is incorrect.

Complexiopollis complicatus Góczán, 1964

Fig. 18B.

Remarks.—Reported from the upper Cenomanian (Kedves 1980; uncertain); otherwise known in the Oculopollis–Trilobosporites Dominance Zone (Góczán and Siegl-Farkas 1990) to the lower Campanian (Siegl-Farkas 1988). Another representative of this genus is reported under open nomenclature as Complexiopollis sp. (Fig. 18C). Four other species were found by Raniecka-Bobrowska (1984, 1989: pl. 216: 6–11, pl. 217: 1–2) in Palynoassemblage B.

Genus Emscheripollis Krutzsch, 1959a

Type: Emscheripollis inflatius Krutzsch, 1959a; Coniacian?, Upper Cretaceous; Weißwasser-Rietschen 19 borehole, Lusatia, Saxony, Germany (Krutzsch 1959a: 137, 139).

Emscheripollis sp.

Remarks.—Three taxa from Rakowice Małe belonging to Emscheripollis Krutzsch, 1959a were illustrated by Pacltová and Krutzsch (1970: pl. 101: 9–13, 28–32). Raniecka-Bob­rowska (1984, 1989: pl. 217: 3–7) found these three taxa and two other species in Palynoassemblage B. Representatives of this genus are known from the Turonian (Krutzsch 1958) to the Maastrichtian (Olaru 1974).

Genus Interporopollenites Weyland and Krieger, 1953

Type: Interporopollenites proporus Weyland and Krieger, 1953; lower Campanian, Upper Cretaceous; Aachen area, Nordrhein-Westfalen, Germany.

Interporopollenites turgidus Tschudy, 1975

Fig. 18G.

Remarks.—Originally described from the Paleocene of Kentucky (USA), known in the Turonian and Santonian of Vendée, France (Azéma et al. 1981).

Genus Minorpollis Krutzsch, 1959a

Type: Minorpollis minimus Krutzsch, 1959a; Coniacian, Upper Cretaceous; Weisswasser-Rietschen, Lusatia, Saxony, Germany.

Minorpollis minimus Krutzsch, 1959a

Fig. 18D.

Remarks.—Found in almost all samples in the section RK-4 and in Palynoassemblage B (Raniecka-Bobrowska 1984, 1989: pl. 217: 8, 9). Known from the Coniacian (Góczán et al. 1967) to the Eocene (Krutzsch 1959a).

Genus Plicapollis Pflug, 1953

Type: Plicapollis serta Pflug, 1953; middle Senonian, Upper Cretaceous; Aachen area, Nordrhein-Westfalen, Germany.

Plicapollis serta Pflug, 1953

Fig. 18E.

Remarks.—Present in Palynoassemblages A and B (Ranie­cka-­Bobrowska 1984, 1989: pl. 218: 4, 5). Known from the Coniacian (Krutzsch 1966a) to the Eocene (Góczán et al. 1967).

Genus Pseudoplicapollis Krutzsch in Góczán et al., 1967

Type: Pseudoplicapollis palaeocaenicus Krutzsch in Góczán et al., 1967; middle Paleocene, Wehmingen near Sarstedt, Lower Saxony, Germany.

Pseudoplicapollis peneserta (Pflug, 1953) Krutzsch, 1967

Fig. 18H.

Remarks.—Found in almost all samples in the section RK-4 and in Palynoassemblage B (Raniecka-Bobrowska 1984, 1989: pl. 218: 7). Known from the Coniacian (Hradecká et al. 1999) through the Santonian (Góczán and Siegl-Farkas 1990) to the Maastrichtian (Góczán et al. 1967).

Genus Neotriangulipollis Góczán, Groot and Krutzsch in Góczán et al., 1967

Type: Neotriangulipollis piolencensis Groot and Krutzsch in Góczán et al., 1967; Santonian, Upper Cretaceous; Piolenc, Vaucluse, southern France.

Neotriangulipollis sp.

Fig. 18I.

Remarks.—Representatives of Neotriangulipollis were known from the middle Santonian to the lower Campanian (Góczán et al. 1967). However, Néraudeau et al. (2017) recently reported a Neotriangulipollis co-occurring with Cenomanian–Turonian forms like Atlantopollis microreticulatus Krutzsch in Goczán et al., 1967 or Complexiopollis praeatumescens Krutzsch, 1959a.

Genus Pecakipollis Krutzsch and Pacltová in Góczán et al., 1967

Type: Pecakipollis bohemiensis Krutzsch and Pacltová in Góczán et al., 1967; Turonian–Santonian, Upper Cretaceous; borehole Pecák, Southern Bohemia, Czech Republic.

Pecakipollis sernoensis Pacltová and Krutzsch, 1970

Fig. 18N.

Remarks.—Two another species are reported under open nomenclature as Pecakipollis sp. (Fig. 18R) and aff. Pecaki­pollis sp. (Fig. 19J). Representatives of Pecakipollis possibly occur from the upper Coniacian (Góczán et al. 1967) to the middle Santonian (Pecák borehole, South Bohemian Basins; Pacltová 1981).

Genus Triangulipollis Krutzsch in Góczán et al., 1967

Type: Triangulipollis turonicus Krutzsch in Góczán et al., 1967; middle Turonian, Upper Cretaceous; Zeichen near Pirna, Saxony, Germany.

Triangulipollis sp.

Fig. 18O.

Remarks.—Representatives of Triangulipollis are known possibly from the Cenomanian (Durand and Louail 1976: 1721, under open nomenclature) and certainly from the Turonian (Batten 1989: 13) to the Paleocene (Mikhelis 1981).

Genus Trudopollis Pflug, 1953 emend. Krutzsch in Góczán et al., 1967

Type: Trudopollis pertrudens Pflug, 1953; Danian; Wehmingen near Sarstedt, Hannover, Germany.

Trudopollis fossulotrudens (Pflug in Thomson and Pflug, 1953) Pflug, 1953

Fig. 18S.

Remarks.—Known from the Coniacian to the Santonian.

Trudopollis sp.

Fig. 18F, V.

Remarks.—Species belonging to this genus are found in almost all samples in the section RK-4. We have found also atypical four-pored forms (Fig. 18F) similar to those reported by Pacltová (1981) from the Santonian of the borehole Pecák in the South Bohemian Basin. Representatives of Trudopollis Pflug, 1953, are known from the Turonian (Krutzsch 1958) to the Eocene–Oligocene boundary beds (Aleksandrova et al. 1985).

Genus Oculopollis Pflug, 1953

Type: Oculopollis concentus Pflug, 1953; middle Senonian, Upper Cretaceous; Aachen area, Nordrhein-Westfalen, Germany.

Oculopollis sp.

Fig. 18T, U.

Remarks.—Representatives of Oculopollis Pflug, 1953 are known from the Coniacian to the Paleocene.

Genus Piolencipollis Groot and Krutzsch in Góczán et al., 1967

Type: Piolencipollis piolencensis Groot and Krutzsch in Góczán et al., 1967; Santonian, Upper Cretaceous; Piolenc, Vaucluse, southern France.

Piolencipollis sp.

Fig. 19L.

Remarks.—Due to the mediocre quality of printing in Ranie­cka-Bobrowska (1984, 1989) we illustrate again a specimen from Palynoassemblage B. Representatives of the genus Piolencipollis are diagnostic for the Santonian.

Order unknown

Genus Tricolporites Cookson, 1947a

Type: Tricolporites sphaerica Cookson, 1947a; late Eocene–Miocene, Maryvale, Victoria, Australia.

Remarks.—We follow Stover and Partridge (1973: 258) and de Villiers and Cadman (1997: 90) in considering Tri­colporites as a valid genus introduced by Cookson (1947a: 195; publication date September 1947). Alternatively it has been considered either as a valid genus introduced by Cookson (1947b: 134) with Tricolporites prolata Cookson, 1947b (Tertiary, Waterfall Gorge near Port Jeanne d’Arc, Kerguelen Islands) as the type (Cookson 1947b, publication date December 1947; Tschudy 1973a: 30), a genus invalidly proposed by Cookson (1947a, b) but validated by Srivastava (1972: 10) with T. prolata as the type species (Potonié 1960: 154, 1975: 116), or a nomenclaturally valid genus with T. sphaerica as the type species but synonymous with Rhoipites Wodehouse, 1933 (Kemp and Harris 1977: 36; Pocknall and Crosbie 1982: 7). Revision of this genus is out of scope of the present paper.

Tricolporites sp.

Fig. 18Y.

Remarks.—Tricolporites is a form genus of dicotyledonous pollen. Detailed investigation is often conducted using LM and SEM studies on the same specimen (Zetter 1989; Zetter et al. 2002).

Class Monocotyledoneae de Candolle, 1817

Order Arecales Bromhead, 1840

Family Palmae Jussieu, 1789
(= Arecaceae Berchtold and Presl, 1820)

Genus Spinizonocolpites Muller, 1968

Type: Spinizonocolpites echinatus Muller, 1968; Engkilili Formation, Cretaceous–Paleocene (after Muller 1968; upper Paleocene to middle Eocene according to Hutchinson 2005: 48–49 and references therein); Lupar river area, Sarawak, Borneo, Malaysia.

Remarks.—Spinizonocolpites is the original spelling (Mul­ler 1968: 11) and must be retained; frequently used Spino­zonocolpites (e.g., Graham 2011: 337) is incorrect.

Spinizonocolpites sp.

Fig. 18J.

Remarks.—The genus Spinizonocolpites is used for dispersed pollen of the palm genus Nypa Steck, 1757. Up to now, the oldest confirmed reports of Nypa were from the Maastrichtian (possibly upper Campanian; see review in McLoughlin et al. 2018).

Spermatophytes, division, class, order, or family unknown

Genus Catinipollis Krutzsch, 1966b

Type: Catinipollis geiseltalensis Krutzsch, 1966b; middle Eocene; Geiseltal, Sachsen-Anhalt, Germany.

Catinipollis lwowekensis Raniecka-Bobrowska, 1984

Fig. 19H.

Remarks.—This species was described from borehole KB-13, at a depth of 94.5 m. Due to the mediocre quality of print in the protologue we are reproducing two of the original photographs herein. The holotype is poorly preserved. We have not found any similar pollen in Palynoassemblage A. The only other species of this genus is the type species. The botanical affinities of these pollen grains are unknown (Krutzsch 1966b: 43–44).

Palaeoecology

Composition of the megaflora

Quantitative data on the fossil megaflora studied are given in Table 2. It should be noted that the assemblages as defined herein represent a wide spectrum of time-averaging (Behrensmeyer et al. 1992), were not sampled equally, and come from layers displaying different preservational potential, so only a general interpretation can be given.

The flora is dominated by angiosperms in terms of both taxa (19/29 ≈ 66%) and specimens (157/270 ≈ 58%). However, the most abundant single species is the conifer Geinitzia reichenbachii which accounts for 38.5% of the specimens of the studied material (Halamski and Kvaček 2019), whereas the second most abundant species, the dicot Dewalquea haldemiana, is represented by 17 specimens (6.3% of the material). G. reichenbachii must clearly have been common, even if the numerical value of its dominance may be positively biased by the fact that even small fragments of conifer twigs are identifiable, whereas similar-sized scraps of angiosperm leaves mostly are not. As has been commented several times already, fossil species G. reichenbachii may have corresponded to more than one biological species.

Out of 29 identified megafossil taxa, 13 are represented by single specimens and additional five by two specimens each. An elementary rarefaction analysis indicates that the original diversity is far from being sampled. As far as assemblages are concerned, four of them (Assemblages 1, 2, 3, 7) are represented by less than ten specimens, which means that their analysis can be made only in very general terms. Assemblages 4–6 and 8 are represented by numbers of specimens varying between 25 and 108.

General characteristics of the mesofossil assemblage

Mesofossils were recovered solely from Assemblage 5 at Rakowice Małe and from one layer (150–200 cm) at Żeliszów. Mesoassemblages at both localities are different, the former being dominated by Normapolles fruits and corresponding to alluvial plain and “upland” vegetation, the latter being rich in conifers and representing a swamp forest (ZH, JK, ATH, and J. Dašková, unpublished material).

The fruits belonging to the Normapolles complex are small-sized reproductive structures, interpreted as corresponding mostly to extinct fagalean dicots (Friis et al. 2006, 2011, and references therein), are an important part of Late Cretaceous floras of the Northern hemisphere. From Rakowice Małe locality nine species of Normapolles affinity are currently known (enumeration based both on specimens collected during the present study and by previous authors): Calathiocarpus octocostatus (Knobloch, 1970) Knobloch and Mai, 1986, Walbeckia guttaeformis (Knobloch, 1970) Knobloch and Mai, 1986, Caryanthus communis Knobloch and Mai, 1986, Caryanthus trebecensis Knobloch and Mai, 1983, Caryanthus triasseris (Knobloch, 1964) Knobloch and Mai, 1986, Caryanthus sp., Zlivifructus microtriasse­ris (Knobloch and Mai, 1986) Heřmanová, Kvaček and Halamski in Heřmanová et al., 2019, Zlivifructus vachae Heřmanová, Dašková, and Kvaček in Heřmanová et al., 2017, and one unknown taxon. All of them represent small flowers and fruits. The flowers are bisexual, bisymmetrical, and have an inferior ovary with a hypanthium. The tepals are attached on top of the hypanthium. A detailed reinterpretation of Zlivifructus microtriasseris was given by Heřmanová et al. (2019). Unfortunately the present authors did not succeed in finding the most productive layer sampled by Ervín Knobloch with more diverse Normapolles inflorescences and lycophyte megaspores Ricinospora sp. (ZH, JK, ATH, and J. Daš­ková, unpublished material).

The Żeliszów locality provided mesofossils mostly in form of coniferous shoots (Cunninghamites cf. squamosus Heer, 1871, Geinitzia formosa and seeds (Alapaya sp., Seletya sp.). Angiosperm mesofossils were represented by reproductive units of plants belonging to the Normapolles group, either with a single bract bearing three male flowers or with female unisexual flowers. A cluster of Minorpollis pollen, probably a fragment of an anther, was found in a staminate flower. Among other mesofossils may be noted: rare clitellate cocoons assigned to Dictyothylakos sp. and and the problematic mesofossil Costatheca striata (Dijkstra, 1949) Hall, 1967.

Microflora

General characteristics of the palynoassemblages.—In a very general way the palynoassemblages investigated both by the present authors and by Raniecka-Bobrowska (1968) may be described as rich. The Normapolles group is represented by numerous taxa, which is quite typical for Central Europe, particularly in the Santonian–Campanian which is a period of great diversity for this grouping (Friis et al. 2011: 339). Fern spores are another abundantly represented group, the Gleicheniaceae especially in Palynoassemblage A and the Schizeaceae especially in Palynoassemblage B (Raniecka-Bobrowska 1984: 463). In Palynoassemblage A dinocysts and prasinophytes are relatively rare compared to non-marine palynomorphs; Raniecka-Bobrowska (1968) does not provide data on marine palynoflora. Both palynoassemblages contain reworked spores: in the Palynoassemblage B Raniecka-Bobrowska (1968) identified Carboniferous megaspores Cingulizonates radiatus Dybová and Jachowicz, 1957, and a representative of “Hymenozonosporites” (nomen nudum; see Potonié 1956: 66), as well as Triassic to Liassic Zebrasporites cf. interscriptus (Thiergart, 1949) Klaus, 1960. The presence of reworked sporomorphs was noted also in Palynoassemblage A, but they have not been documented in detail.

Palynoassemblage A.—From the Assemblage 5 we reco­vered 126 taxa of palynomorphs (see Appendix 3) and moreover two species of foraminiferal linings. They can be divided as follows: fungal spores, 2 taxa; land plants, 105 palynotaxa (spores, 54 palynotaxa; gymnosperm pollen, 16 palynotaxa; angiosperm pollen, 35 palynotaxa); non-marine algae, 4 palynotaxa; marine organisms, 15 palynotaxa (dinocysts, 11 palynotaxa; prasinophytes, 4 palynotaxa).

No significant vertical variation among successive samples was noted (Fig. 20). In particular, in RK-4 there was no overall trend of either increasing or decreasing salinity, as samples with no marine palynomorphs occur in all parts of the analysed section. In terms of terrestrial palynomorphs, the samples from Rakowice Małe contain more taxa than those from Żeliszów.

Quantitative data for two samples illustrate the typical composition of the palynoassemblage: Rakowice Małe (MB.Pb.2018/0005): fern spores 30%, gymnosperm pollen 30%, angiosperm pollen 32%, dinoflagellate cysts and foraminifers 8%; Ołdrzychów (MGUWr 5638p): fern and bryophyte spores 36%, Taxodiaceaepollenites hiatus (the only gymnosperm present) 27%, Normapolles 27%, dinoflagellate cysts and foraminifers 10%.

The Palynoassemblage A belongs to the Oculopollis–Complexiopollis Dominance Zone, encompassing the Conia­cian and early Santonian (Siegl-Farkas and Wagreich 1996: 131).

Marine microflora from the Palynoassemblage A.—Marine palynomorphs are rather rare, both in terms of taxa (15 species) and of specimens, the latter accounting for up to 10% of assemblages (see above), but it may be that dinocysts are altogether absent (MB.Pb.2008/0362; RK-4-150, 370, 470, 590). If present, dinoflagellate cysts are mostly broken. At Żeliszów, only a single dinocyst was found (Subtilisphaera sp., depth 180 cm); foraminifer linings and prasinophytes occur only at a depth of 180–200 cm and are otherwise absent.

Peridinioid dinocysts Alterbia, Chatangiella, Isabeli­di­nium, Spinidinium, and Subtilisphaera as well as the gony­aulacoid Spiniferites tend to occur in water that is eutrophic because of significant nutrient supply due to either upwelling or terrigenous input (Wall et al. 1977; Arai and Viviers 2013). Dinogymnium is an estuarine genus (May 1977). The species Spiniferites ramosus is known in recent environments from regions where upper water salinity can be reduced permanently, or seasonally, by river discharge or snow melt. Open sea species, like Surculosphaeridium longifurcatum, are rare.

Among prasinophycean algae, Crassosphaera and Tas­manites are characteristic for marine environments. On the contrary, representatives of Leiosphaeridia and Ptero­spermella belong to so-called “disaster species” (Tappan 1980) able to thrive under conditions hazardous to other species (Guy-Ohlson 1996), such as reduced salinity.

To sum up, marine influence during the time of deposition of the upper part of the Nowogrodziec Member was relatively limited, more so at Żeliszów due to its greater distance from the open sea (see palaeogeography in Fig. 1C).

Land microflora of Palynoassemblages A and B.—The global compositions of the land microflora from Palynoassemblages A and B are similar. The relative ratios of spores vs. pollen taxa are identical (in both cases spores 54%, pollen 44%; see Raniecka-Bobrowska 1984). The ratios of gymnosperm to angiosperm pollen are also close: gymnosperms 31%, angiosperms 69% in Palynoassemblage A, one third to two thirds in Palynoassemblage B (Raniecka-Bobrowska 1984). This may be interpreted as testifying to a relative overall stability of regional vegetation pattern during the later half of the period studied herein, even if the megafloral record contains plant fossils corresponding to various single palaeocommunities.

In Palynoassemblage A, among the 105 palynotaxa corresponding to land plants (Appendix 3), the following ones are the most frequent: spores (Costatoperforosporites cf. foveolatus, Cyathidites minor, Deltoidospora sp., Dic­tyo­phyllidites harrisii, Gleicheniidites apilobatus, G. cir­ciniidites, G. seno­nicus, Laevigatosporites ovatus, Sterei­spo­rites antiqua­sporites, Stereisporites sp.), gymnosperm pollen (Cycadopites sp., Taxodiaceaepollenites hiatus, Taxo­diaceaepollenites sp.), angiosperm pollen (Com­plexio­pollis sp., Minorpollis minimus, Pecakipollis sp., Plica­pollis serta, Plicapollis sp., Pseudo­plicapollis peneserta, Retitricolporites sp., Tricolpites sp., Trudopollis sp., Vacuo­pollis sp.).

From the Palynoassemblage B, Raniecka-Bobrowska (1968) assembled data on occurrences of over 700 morphotypes but they are not always identified, some are reworked (see above), and some are probably duplicated. In total 153 taxa of palynomorphs are sufficiently common to be included in a synoptic table. Taxa in common between Palynoassemblages A and B include: Appendicisporites appen­dicifer, Gleicheiniidites senonicus, Minorpollis mini­mus, and Pseudoplicapollis peneserta. Notable taxa absent in Palyno­assemblage A are, among others: Trilobo­zonosporites exoticus Pacltová, 1961, Foveasporites budejo­vi­censis (Pacl­tová, 1961) Pacltová and Krutzsch, 1970, Taurocusporites europaeus Krutzsch, 1973, Densoisporites velatus Weyland and Krieger, 1953, Podocarpidites sp., Semioculopollis praedicatus (Weyland and Krieger, 1953) Krutzsch in Góczán et al., 1967 and Piolencipollis sp. (Raniecka-Bobrowska 1984, 1989). Palynoassemblage B is richer in gymnosperm pollen in the lower part and in angiosperm pollen in the upper part (Raniecka-Bobrowska 1968: 27–28).

According to Krutzsch (1966a: 97), the “Löwenberger Bild” is characterised by the presence of Normapolles genera Pecakipollis, Papillopollis, Pseudotrudopollis, Extra­tri­poropollenites, Capipollis, Santonipollis, and ?Mag­no­poro­pollis. Out of these seven genera, only representatives of Pecakipollis were found during the present investigation. However, in the investigated material from Palynoassemblage A we found numerous representatives of Trudopollis, Com­plexiopollis, Interporopollenites, and Neotriangulipollis cf. piolencipollis. We have no satisfactory explanation for such a marked difference in the composition of the Normapolles group from the same strata.

Comparisons.—According to Raniecka-Bobrowska (1968), Santonian Palynoassemblage B is very similar but richer than that described by Weyland and Greifeld (1953) from coeval strata from Quedlinburg. There are also similarities with Turonian–Santonian palynofloras from Bohemia (Pacltová 1961), but in this case differences are also notable: several representatives of Cicatricosisporites, Appendicisporites, and Gleicheniidites common in Lower Silesia are absent in Bohemia; in contrast, Papillopollis and Santonipollis occur in Bohemia, but are not known from Lower Silesia.

A Turonian–Santonian palynoflora from the Klikov For­mation at Gmünd (Austria) was analysed by Zetter et al. (2002). This palynoassemblage is dominated by angiosperms (65 taxa, 60%), mainly by the Normapolles group (37%); bryophyte and pteridophyte spores are also numerous (25 taxa, 30%), whereas gymnosperms are rare (10%). The general aspect of the palynoassemblage in which Nor­ma­polles and ferns are the major groups is similar; there are, however, many differences in details: Araucariacidites is the most common gymnosperm at Gmünd, whereas it is absent in Lower Silesia; sulcate angiosperm pollen grains are more diverse at Gmünd.

Differences with a Santonian palynoassemblage from Romania, consisting of 45 pteridophyte, 8 gymnosperm, and 13 angiosperm taxa (Ţabără and Slimani 2019), are notable, even if a detailed comparison is hampered by the fact that many palynomorphs are identified only at genus level. The only species in common is Cicatricosisporites dorogensis. There are numerous representatives of Vadaszisporites Deák and Combaz, 1967 which is entirely absent in Lower Silesia.

Compared to slightly older (Coniacian) assemblages of Idzików (lower Idzików beds; Kvaček et al. 2015) and Březno (Halamski et al. 2018), Palynoassemblage A studied herein is characterised by fewer, less well preserved, and less diverse marine elements, but land plant palynomorph assemblages are globally similar. The presence of Pecakipollis and Neotriangulipollis, absent at Idzików and Březno, should, however, be noted. All in all, the microfossil record analysed herein should be understood as corresponding to broadly similar plant palaeocommunities preserved in marginal marine environment, as opposed to a fully marine setting represented by the Idzików and Březno beds.

An important difference from the slightly younger (Oculopollis zaklinskaiae–Tetracolporopollenites globosus Zone, late Santonian) palynoassemblage from Iharkút (Hungary) is that in the latter ferns are only a minor component (Bodor and Baranyi 2012). Overall, however, the palaeocommunity reconstructed as a Normapolles-related forest with herbaceous angiosperm and fern-dominated undergrowth (Siegl-Farkas and Wagreich 1996; Bodor and Baranyi 2012; Botfalvai et al. 2016) is of the same type as in Lower Silesia. Complexiopollis complicatus is a species in common. Late Santonian palynoassemblages from Bulgaria (Pavlishina et al. 2019) differ in the presence of numerous Krutzschipollis and Vadaszisporites grains.

Reconstruction of palaeocommunities

Palaeoecological studies are based on studies of museum specimens, freshly collected mega-, meso-, and microfloristic material, as well as on geological observations in the field. The available information allows a general scheme of plant palaeocommunities to be reconstructed.

Turonian and early to middle Coniacian.—The available plant material belonging to the Assemblages 1–3 is scarce and, as said above, can be interpreted only in very general terms.

The single Turonian plant in the studied material is Geinitzia reichenbachii. It may be noted that this species is also present in a small assemblage of Turonian plants known from the Opole Basin (Goeppert 1866b: 644; Płachno et al. 2018: 164). It is impossible to say whether it grew in the same type of community as in the Assemblage 5 (see below).

As far as the Assemblages 2 and 3 (treated jointly for the purpose of palaeoecological interpretation) are concerned, the notable feature is the presence of Pinus longissima and of two species of Protopteris, otherwise absent in the studied material. The tree ferns are an element of relatively well understood hygrophilous vegetation (Kvaček 2017: 45) On the other hand, the pine probably dwelt in an upland area (Kvaček 2017: 52), the vegetation of which is usually only imprefectly represented in the fossil record. This means that the Assemblages, as presently constituted, are heterogenous, i.e. consisting of a taphonomically mixed land plants having lived in different environments. For palynological record of upland vegetation, see below.

Late Coniacian?–early Santonian?—According to Lesz­czyński (2010), the depositional environment of the basal part of the Nowogrodziec Member (Assemblage 4 herein) was a lake, whereas that of the remaining part (Assemblage 5 herein) showed some marine influence, either as a marsh, a lagoon, or a (brackish) sea embayment. Fossil plant assemblages preserved in these two different sedimentary environments are different as well.

The most common plants of the Assemblage 4 are the fern Konijnenburgia and the angiosperm Dewalquea haldemiana. Geinitzia reichenbachii is relatively rare here (only four specimens out of 26, compared to 91 out of 108 in Assemblage 5). Dewalquea haldemiana is most often found in marine sediments (Hosius and von der Marck 1880; Halamski 2013; and especially Halamski et al. 2016) and may have been a species growing on coastal dunes (see Krassilov 2003: 94 for an analogous interpretation of single-species accumulations of Debeya pachyderma). Konijnenburgia, possessing a strongly cutinised epidermis and large indusia, is interpreted to have been a xerophytic fern living in an open habitat known as a fern savanna (Crane 1987: 124; fern steppe sensu Kvaček 2017: 46, see also Batten 1974; fern prairie sensu Friis et al. 2011: 468; see Krassilov 2003: 94 for an opposite view), that is, an open palaeocommunity dominated by ferns (see also below). Konijnenburgia may have grown both in a fern savanna and on dunes.

Assemblage 5 represents back and coast swamps, in some cases coal-forming. It is dominated by cupressoid conifers Geinitzia, Protodammara, Alapaya, and abundant ferns (Cladophlebis, Coniopteris) and lycophytes. Such communities are relatively well known in the fossil record; they have been reported from the Cenomanian of western France (Peyrot et al. 2019), from the Coniacian Idzików beds (Kvaček et al. 2015) and Březno Formation (Halamski et al. 2018a), and from the Campanian of Grünbach (Herman and Kvaček 2010) and Utah (Parker 1976). It is worth noting that Konijnenburgia, known in Assemblage 4, is absent. This conifer–fern–lycophyte palaeocommunity is also well represented in the palynoassemblage, with Taxodiaceaepollenites (the nearest living relatives thereof being the swamp trees Taxodium and Glyptostrobus), Cycadopites (pollen of cycads from lowland freshwater swamps, possibly drought tolerant; Abbink 1998; Barrón et al. 2006: 195), Biretisporites and Dictyophyllidites (two fern spore genera characteristic for swamps; Hampson et al. 2017), as well as Stereisporites (spores of the peat moss Sphagnum). Among non-marine algae, Ovoidites parvus dwelt in open waters of peat marshes.

However, several palynomorphs from Palynoassemblage A are suggestive of a different environment, not recorded in the megafossil record, namely salt-tolerant mangrove vegetation (Uličný et al. 1997; Kvaček 2000; Kvaček et al. 2006). This is especially evident for Classopollis classoides (pollen of cheirolepidiaceous Frenelopsis; Abbink 1998; Batten and MacLennan 1984; Riding et al. 2013), but several fern spore genera may have been produced by plants dwelling in this environment (Deltoidospora and several spores of schizeaceaous ferns; see also the situation described by Polette et al. 2018: 219). Megafossil remains from such communities were recorded from the Coniacian of the Idzików beds (Kvaček et al. 2015) and Březno Formation (Halamski et al. 2018a: 137).

It is well known that the mangrove-palm Nypa has been forming this kind of vegetal communities since the latest Cretaceous. The oldest known true mangroves were those formed by Nypa (Maastrichtian or possibly latest Campanian; El-Soughier et al. 2011; McLoughlin et al. 2018 and references therein) and by Palaeowetherellia (Euphorbiaceae; Maastrichtian, Egypt; Mazer and Tiffney 1982). The presumed Santonian mangroves from Scania were revealed to be based on a misinterpretation (McLoughlin et al. 2018), but palms are known already from Turonian swamps (Coiffard and Gomez 2010: 166). The presence of Spinizonocolpites sp. in the studied material is suggestive of the existence of Nypa (possibly in association with the mangrove-forming conifer Frenelopsis) in the Coniacian–Santonian of Lower Silesia, but at present only a single pollen grain has been found, so such an inference must be treated as unconfirmed.

The mesofossil record of Normapolles plants (Cary­anthus, Zlivifructus) might correspond to forests occurring in well drained parts of aluvial plains and on the lower parts of slopes, with schizaeaceous ferns (Cicatricosisporites, Appendicisporites) forming the understory. It might have been tempting to associate the fagalean foliage Dryophyllum with Normapolles-producing trees, but the association of Normapolles with riparian settings has never been noted before.

The upland flora growing on slopes and further inland is preserved only fragmentarily. This palaeocommunity is tentatively reconstructed as a fern savanna with the matoniaceous fern Konijnenburgia (macrorests in Assemblage 4), co-occurring with producers of Ephedripites pollen and of matoniaceous and schizaeaceous thick-walled spores. Fern savannas with matoniaceous ferns are known from the English Wealden (Phlebopteris, Harris 1981) and from the Barremian of Europe (Coiffard et al. 2007, de la Fuente and Zetter 2016, Martín-Closas et al. 2016); matoniaceous and other drought-tolerant ferns inhabited xeric habitats in the Cenomanian of western France (Peyrot et al. 2019). It is uncertain whether fern savannas were replaced by other communities already in the Cretaceous (Crane et al. 1987: 124) or persisted into the Paleocene (Coe et al. 1987: 136). In the Lower Silesian Cretaceous there may have been patches of Pinus woodlands (macrorests in Assemblage 2). It must be noted that given the relatively small size of the island and the presumably subdued topography, “uplands” should be understand more in relative than in absolute way.

Early–middle Santonian.—The sandstone, mudstone, and claystone beds and rare coal seams of the Czerna Formation are interpreted as having been deposited in a mosaic of deltaic plains, alluvial plains, wetlands, and shallow lakes (Górniak 1986). The preservation of compound leaves with articulated leaflets is a strong argument for pre-burial transport having been relatively short in Assemblage 8 (Figs. 10F, 12) and Assemblage 6 (Figs. 8C–E, 9B, C).

Assemblage 6 is preserved in sandstone. They may contain a brackish macrofauna, although the investigated material was collected in a period when sedimentological details were not recorded, so the precise relationships of the fauna- and flora-bearing beds is not known. Sandstone may represent either deltaic or river channel deposits, so Assemblage 6 should be interpreted as representing trees forming riparian forests (Fig. 21), possibly on relatively coarse clastic substrates. It may be that the tree ferns Protopteris (known from Assemblage 3) may have formed a part of this assemblage as well. Betulaceae-like trees-dominated forests with diversified ferns in the understory were present in the Maastrichtian of Isona (Spain; Villalba-Breva et al. 2015; Marmi et al. 2016).

Assemblage 7 is very small in terms of the number of specimens it contains, but a meaningful interpretation is possible in the context of Assemblage 6 and, to a lesser extent, Assemblage 8. The absence of Platanites sp. 1 from Assemblages 6 (preserved in a similar lithology) and 8 is a hint of local variation among the palaeocommunities of the deltaic-alluvial plain of the investigated area. Possibly this species belonged to a different variant of riparian forests (Fig. 21) than that recorded in Assemblage 6. Given the position of the locality Nowe Jaroszowice in the central part of the marine embayment (Fig. 1C), as compared with that of Bolesławiec, it may be that the Platanites willigeri forest occupied a more humid setting, but a levee cannot be excluded either.

Assemblage 8 is preserved in claystone. Mass accumulation of leaves and subcomplete compound leaves are suggestive of parautochthonous character of this assemblage (Figs. 11A, 12A–C). In this case the original community may be hypothetically reconstructed to have dwelt in marginal parts of the alluvial plain (Górniak 1986: 128), for example in lakes having only limited contact with the marine embayment (Alexandrowicz 1976: 193). However, it is difficult to say whether the actual habitat of Assemblage 8 was drier or wetter than that of Assemblage 6.

General character of the communities.—The abundance and diversity of ferns, a group represented mostly in the palynological record, is a feature of the studied plant assemblages not found in today’s world. A similar situation was noted by Wing et al. (2012) in an upper Campanian site in Wyoming (USA) and interpreted as a palaeocommunity intermediate in general character between pre-angiosperm and modern vegetation. In other words, the so-called Cretaceous Terrestrial Revolution (Lloyd et al. 2008) had still not been completed.

However, the abundance and diversity of angiosperms in mega-, meso-, and microfossil records are unlike the situation in Wyoming where flowering plants were presumably growing only in patches and occupying mostly disturbed habitats (Wing et al. 2012). At least some Cretaceous Lower Silesian forests must have been angiosperm-dominated.

It is also worth noting that both in Lower Silesia and in Wyoming the most abundant ferns belong to the early-diverging orders Gleicheniales and Schizaeales, whereas the Polypodiales are much less frequent. This situation corresponds to a period before, or at the very beginning of, the major radiation of modern ferns (Schneider et al. 2004; Schuettpelz and Pryer 2009). It may be asked whether these ferns were already adapted to low-level light intensity in closed-canopy forests through the acquisition of the neochrome (Li et al. 2014; see also Watkins and Cardelús 2012), but the dating of this event is poorly constrained and the data at hand are insufficient to estimate the ecological form of the Cretaceous forests of Lower Silesia.

The aquatic communities, described for example in the Cretaceous of southern France (e.g., de Saporta 1890; Samuel and Gaillard 1984) or Spain (Marmi et al. 2016), are represented in Lower Silesia by lycophyte megaspores Ricinospora sp. (ZH, JK, ATH, and J. Daš­ková, unpublished material).

Comparison of mega-, meso-, and microfossil records

The megafossil assemblage from the North Sudetic Basin consists of 29 taxa and the mesofossil flora of 14 taxa (ZH, JK, ATH, and J. Daš­ková, unpublished material). Palyno­assemblage A is composed of 105 taxa of land plants, over three times more than the number of megafossil taxa, and if pollen and spores known from the Palynoassemblage B are added, even more.

A meaningful comparison of the three kinds of plant fossil record can be done in a twofold way. First, comparison may bear on a single assemblage (palaeocommunity), which is the most obvious approach from a taphonomical point of view. Such a comparison of mega- and microfossil records from a Jurassic bed in Yorkshire was conducted by Slater and Wellman (2015). Secondly, given the well-known fact that most palynological records reflect regional vegetation and the megafossil record is biased towards particular, more local palaeocommunities, one may compare the total assemblages to draw inferences on regional scale.

As far as major plant groups across all assemblages are concerned, bryophytes (sensu lato) and lycophytes are known solely from the microfossil record and ferns are underrepresented as megafossils. This is analogous to the situation described for the Jurassic of Yorkshire by Slater and Wellman (2015). In contrast to the situation in Yorkshire, conifers are very well represented in the megafossil record and no single plant group seems underrepresented in the microfossil record.

In the mega- and mesofossil record the vegetation appears dominated by angiosperms and this is probably true as far as the forest-forming species are concerned. The microfossil record is dominated by ferns and corresponds to understory vegetation, vines, and possibly other non-forest palaeocommunities.

As outlined above, Assemblage 5 in the megafossil record corresponds to a backswamp forest (a single palaeocommunity), the mesofossil record to the backswamp forest, as well as the alluvial plain and “upland” vegetation (ZH, unpublished material), whereas the microfossil record documents the three above-mentioned palaeocommunities, but also the halophilous vegetation and fern savannas. A similar situation occurs in Assemblages 6–8, that correspond to variants of climax forest associations, whereas some heliophilous ferns and lycophytes known solely from the microflora might have belonged to pioneer communities (Raniecka-Bobrowska 1968; see also Spicer 2003: 138), like Lygodium, Pityrogramma, or Lycopodium cernuum in the modern flora (Verdoorn 1938; Spicer et al. 1985). Such palaeocommunities are also not reflected in the megafossil record here studied.

Comparison to previously described palaeofloras

It is interesting to compare the mainly Coniacian–Santonian palaeoflora of Lower Silesia described herein with other assemblages of plant fossils from the same palaeogeographic region, i.e., from the European Archipelago. The most striking feature in common with Coniacian palaeofloras (Idzików beds: Halamski and Kvaček 2015; Chlomek beds: Halamski and Kvaček 2016; Březno beds: Halamski et al. 2018a) is perhaps the abundance of trifoliolate fagaleans belonging to Dryophyllum, D. geinitzianum at Idzików and D. westerhausianum described here, arguably dominating one of the palaeocommunities. Other taxa in common are not numerous, including Dryandroides quercinea, Salicites petzeldianus, Geinitzia reichenbachii, Laurophyllum spp., and Konijnenburgia (the same as or closely related to the fern described under Nathorstia by Halamski and Kvaček 2015 and Halamski et al. 2018a). One should also note the general similarity of the palynoassemblages (see above).

Another approximately coeval palaeoflora is that from the Harz Mountains (Quedlinburg and environs; Richter 1904, 1905; Mägdefrau 1968: 350–358). There is one characteristic species in common, Dryophyllum westerhausianum, but the emblematic Credneria is altogether absent in Silesia. There are some similarities in the palynofloras (Weyland and Greifeld 1953), but an overall estimation of similarity cannot be made, as the German flora is in need of revision.

The comparison with the slightly younger flora of the Aachen Formation (sables d’Aix-la-Chapelle, Robaszynski et al. 2002; middle Santonian to probably earliest Campanian according to Batten and Li 1987; Batten et al. 1988; and Streel et al. 1994) is hampered by its poor preservation, which motivated Stockmans (1946) to describe most of the taxa under open nomenclature, and with schematic illustrations. One may wonder whether Dicotylophyllum sp. (Stockmans 1946: pl. 4: 10) be not an isolated leaflet of Dewalquea haldemiana or whether Dicotylophyllum sp. (Stockmans 1946: pl. 4: 14) or might be related to our Dicotylophyllum sp. 2. In very general terms, Lower Silesian and Belgian assemblages seem quite different, as coarsely serrate leaves (“Quercus” sensu Hosius and von der Marck 1880) are numerous there (Stockmans 1946: pl. 3: 1, 8, 20–27) and altogether absent in the material studied herein.

Finally, as noted above, the palaeoflora described herein shows some similarities with the plant fossil assemblage from the Frontier Formation (eastern North America). For historical reasons, palaeobotanists were only seldom attempted a direct comparison of coeval Cretaceous assemblages from Europe and North America, although similarities between European and American conifer floras were listed by Bosma et al. (2009). Such a collation for angiosperms is likely to be a fruitful subject of future research.

Temporal trends observed in the Late Cretaceous vegetation of Central Europe

Generally speaking, the angiosperm-dominated mega- and mesoassemblages and fern-dominated microassemblages do broadly correspond to general trends recorded in the northern temperate zone, both in Europe and in North America. Generally speaking, in North America palynofloras start being dominated by angiosperms between the Turonian and the Campanian, which is the case of megafossil assemblages since the Santonian (Upchurch and Wolfe 1987: 88), although major differences may be due to latitude, climate, and facies (Spicer 1990; Wing and Sues 1992; Wolfe 1997; Spicer et al. 2002). For example, conifers were favoured in cooler climates (Doyle et al. 1982) and in swamp forests (Saward 1992).

More in detail, it should be observed first that Assemblages 4–8 (late Coniacian? to early–middle Santonian) are chronologically relatively close to each other, all belonging to a time interval spanning about four million years (base of the Coniacian 89.8 Ma, Coniacian/Santonian boundary 86.3 Ma, top of the Santonian 83.6 Ma; Gradstein et al. 2012). Assemblages 4–5 are nearly coeval with the flora from the upper Idzików beds (see Halamski and Kvaček 2015: 100, 140 for details of the ammonite-based dating). For the purpose of establishing a general panorama of the vegetation we have treated Assemblages 4–8 as approximately coeval.

A striking difference between Coniacian and Santonian riparian forest palaeocommunities of the Central European Archipelago (Coniacian, Idzików beds: Halamski and Kvaček 2015; Kvaček et al. 2015; Chlomek beds: Halamski and Kvaček 2016; Santonian, present study) is the role of laurophylls. This morphotype, probably representing at least in part the magnolioid angiosperms belonging to the Lauraceae (and perhaps a few related families), is a major element of Coniacian palaeofloras, accounting for ca. 25–40% of the material according to localities of the Idzików beds; (Halamski and Kvaček 2015: 128) and for over 15% in the Chlomek beds (Halamski and Kvaček 2016: 299, 310). In the studied material the laurophylls are represented by 14 poorly preserved specimens (6% of the material). This is all the more striking given the similarity of the other dominant elements in the three above-mentioned cases (Dryophyllum, see above).

The platanoid-laurophyll riparian forests were a common element of latest Early and early Late Cretaceous vegetation in Europe (Kvaček et al. 2006; Coiffard et al. 2009) and analogous communities may still be found, for example in Mexico (Brand 1936). However, in the later part of the Late Cretaceous laurophylls are relatively rare in European palaeofloras (Herman and Kvaček 2010; Halamski 2013). In the Aachen sands palaeofloras the situation seems analogous to that in the approximately coeval material described here: only a few of the morphotypes illustrated by Stockmans (1946) belong to laurophylls. It seems that the exclusion of laurophylls from communities of riparian forests in Central Europe might be quite precisely dated to the Santonian, but evidently such a conclusion is based on a scarce factual material and should be confirmed by studies based on a greater number of palaeofloras.

It may also be noted that, if the Santonian vegetation described herein is broadly similar to Campanian palaeofloras from Central and Northern Europe (Halamski 2013; Halamski et al. 2016), among the three possibilities invoked by Halamski and Kvaček (2018: 192) to explain the peculiar character of the early Campanian Grünbach palaeoflora (Herman and Kvaček 2010), namely facies, climate, and age, at least age may be definitively discarded.

Another notable feature of the studied palaeoflora is the presence of long-ranging plant taxa. Dewalquea haldemiana is known from the late Coniacian to the Maastrichtian. Perhaps more interestingly, some of the described plant fossils represent species that are identical or closely related, to Paleocene taxa. This may concern Platanites willigeri similar to upper Paleocene–lower Eocene Platimeliphyllum palanense, Platanites similar to congeneric species known from the Maastrichtian of Montana and the Paleocene of the Isle of Mull, and Dewalquea aff. gelindenensis closely related to Dewalquea gelindenensis from the Paleocene of Belgium. Longevity of plant species may be interpreted as correlated with stability of communities (Paczoski 1933, DiMichele et al. 2004; but see Levin 2000: 171–173 and references therein). Consequently, it may be hypothesised that after a period of pronounced changes in the vegetation of Europe related to the establishment of angiosperm-dominated assemblages (e.g., Coiffard and Gomez 2010), plant communities in the later part of the Late Cretaceous become stabilised and thus more resilient to structural modifications. The major change of plant communities would thus have occurred during a period of stable greenhouse climate (Kaufmann 1995 and references therein), whereas the stabilisation of communities would have taken place simultaneously with a major cooling trend having started in the Campanian and continuing until the end of the Mesozoic (Linnert et al. 2014 and references therein).

It is at present unclear how this might relate to the conclusion made by Bosma et al. (2009: 494) about a distinct turnover in conifer floras between the Santonian and Campanian in the Netherlands. This turnover might, however, be more local phenomenon rather than a global one, insofar as, for example, Geinitzia reichenbachii is altogether absent in the Maastrichtian in the Netherlands (Bosma et al. 2009), but present in both the Campanian and Maastrichtian in Poland (Halamski 2013). Dutch Cretaceous angiosperms lack a comprehensive modern treatment.

Ecosystems of the European Archipelago: comparison of palaeobotanical and palaeozoological data

A recent synthesis of Cretaceous vertebrate faunas from the European Archipelago (Csiki-Sava et al. 2015) showed a peculiar zoogeographic pattern demonstrating both a uniqueness of the whole zooprovince on the one hand and high degree of endemicity between islands on the other. In other words, there are high-level taxa endemic for Europe, but not a single vertebrate species confirmed from more than one region (Csiki-Sava et al. 2015).

It should, however, be stressed that calling the above-mentioned distribution a ‘biogeographic’ repartition, as done by Csiki-Sava et al. (2015), might be misleading, insofar as a vertebrate-based zoogeographic pattern is not necessarily representative for the biosphere as a whole. Such is the present-day situation in South Africa, which in terms of zoogeographic regionalisation belongs to the Ethiopian region along with the major part of the continent (Darlington 1957), but forms a separate phytogeographic unit of the highest rank (South African Kingdom or Capensis; Engler 1910: 479–510; Takhtajan 1986).

Indeed, the above-mentioned Cretaceous palaeozoogeographic pattern is in stark contrast to the palaeophytogeographic one. There is no high-rank taxon peculiar to Europe, and most species for which a detailed identification was possible have been documented from several localities, like Dryophyllum westerhausianum, Dewalquea haldemiana, D. insignis, and others. The closest relatives of Konijnenburgia cf. galleyi and of Platanites willigeri are from North America. The Cretaceous “Quercus” described from Haldem (Hosius and von der Marck 1880) and Aachen region (Stockmans 1946) are known also from Morocco (Carpentier 1950). This conclusion is consistant with on the observation that only minor differences existed between European and Potomac provinces (Vakhrameev 1991: 223) and is still more evident in palynological analyses: the studied area belongs to the Normapolles Province with globally similar palynoassemblages spread between eastern North America, Central Europe, and a part of Asia (Vajda and Bercovici 2014: 32–33 and references therein). Some taxa, like Distaltriangulisporites perplexus, are common to both the studied area and Canada.

Conclusions

The megaflora of the North Sudetic Basin, studied on the basis of 270 specimens from 17 localities (study area ca. 300 km2), is represented by 29 species (6 ferns, 4 coni­fers, 19 angio­sperms), grouped in eight assemblages (Assemblage 1, Turo­nian; Assemblages 2, 3, lower–middle Coniacian; Assem­bla­ges 4, 5, upper Coniacian?–lower Santo­nian?; Assemblages 6–8, lower–middle Santonian).

Dryophyllum westerhausianum (Richter, 1904) Halam­ski and Kvaček comb. nov. is reinterpreted as a member of the Fagales.

The following new combination is introduced: Dewal­quea paulinae (Halamski, 2013) Halamski comb. nov. [basionym: Debeya paulinae Halamski, 2013].

Platanites willigeri Halamski and Kvaček sp. nov. is described. It is represented by trifoliolate leaves with ovate, unlobed median leaflets. Along with Platanites sp. 1, these are the oldest (Santonian) records of the genus.

The studied plants are interpreted to have dwelt in the following palaeocommunities: (i) back swamp forest dominated by Geinitzia, with ferns; (ii) Dryophyllum-dominated riparian forest with Ettingshau­senia (Santonian); possibly Normapolles-dominated (as recorded by mesofossils) on the lower parts of slopes (hinterland); (iii) another variant of riparian forest with Platanites sp. 1 (Santonian); (iv) forest with Dewalquea spp. and Platanites willigeri in the marginal part of the alluvial plain; (v) fern savanna with patches of Pinus woodlands (documented in the Coniacian); (vi) dunes with Dewalquea haldemiana and Konijneburgia aff. galleyi; (vii) halophytic vegetation (mangroves) with Frenelopsis; a single grain of Spinizonocolpites sp. is suggestive of Nypa as a part of this community, but this requires confirmation; (viii) pioneer vegetation with lycophytes and ferns.

Out of these, i–vi, are known from the megafossil record, i, ii, also from the mesofossil record, and vii, viii, solely from the microfossil record.

The mega- and mesofossil records are dominated by angiosperms (canopy-forming species), whereas the microfossil record is dominated by fern spores (understory, vines, pioneer vegetation). Palaeocommunities are intermediate in general character between those pre-dating the Cretaceous Terrestrial Revolution and modern, angiosperm-dominated vegetation.

Microfossils from the Nowogrodziec Member were examined in detail. Palynoassemblage A (corresponding to Assemblage 5) consists of 105 taxa, largely fern spores (especially Gleicheniaceae) and representatives of the Normapolles group. Palynoassemblage B (corresponding to Assemblages 6–8; data after an unpublished report by Raniecka-Bobrowska 1968) is overall similar, but the dominant fern group is the Schizaeaceae.

A striking similarity among Coniacian floras from European Archipelago is the abundance of trifoliolate fagaleans (Dryophyllum westerhausianum in the North Sudetic Basin, D. geinitzianum at Idzików and Březno). On the other hand, a striking difference is the rarity of laurophylls. It is possible that exclusion of lauroids from riparian forests began about the Santonian.

Several species present in the palaeoflora described here are are the same as, or are related to, those that occur in younger (including Paleocene) assemblages. This might be interpreted as stabilisation of communities after a period of pronounced change related to the rise of dominance of angiosperms.

In contrast to the vertebrate-based palaeozoological pattern showing the Cretaceous European Archipelago as a zone of high endemism with strong differentiations between single islands, the plant cover of the same area and period is mostly comprised of widely distributed species, some of which are similar to, or possibly identical with, those found in North America.

Acknowledgements

This study could not be completed without the friendly help of Paweł Raczyński (MGUWr), both in the field and in the museum collections. Access to the quarries at Rakowice Małe and at Żeliszów was kindly authorised by Alfred Sroka (Chairman of the Board, Kwarcyty Bolesławieckie S.A.). The following curators and staff are thanked for granting the access to the collections and various help: Angela Ehling (BGR), Barbara Mohr, Catrin Puffert, and Eva-Maria Sadowski (all MB), Lutz Kunzmann (MMG), Dario De Franceschi (Muséum national d’Histoire naturelle, Paris, France), Emmanuel Robert (Université Claude Bernard-Lyon 1, Lyon, France), Yves Dutour, Nicolas Vialle, and Séverine Berton (all Muséum d’Histoire naturelle d’Aix-en-Provence, Aix-en-Provence, France). Markus Wilmsen (Senckenberg Naturhistorische Sammlungen Dresden, Germany) and Markus Fengler (Moritzburg, Germany) helped in finding biographic data on Gustav Williger. Aurelio J. Patierno (British Library, London) provided publication months needed for checking priority between two names published in the same year. Ireneusz Walaszczyk and Mariusz Niechwedowicz (both Faculty of Geology, University of Warsaw, Poland) commented on inoceramid and dinocyst data, respectively. Irena Grabowska (formerly Polish Geological Institute, Warsaw, Poland) kindly supplied unpublished data of the late Jadwiga Raniecka-Bobrowska. Drawings were made by Bogusław Waksmundzki (Faculty of Geology, University of Warsaw, Poland) and Andrzej Baliński (ZPAL) helped with the plates. Maceration of palynological samples was made by Alena Tichá in the Laboratory of the Czech Geological Survey (Prague, Czech Republic). The text benefited from detailed reviews by Robert Spicer (The Open University, Milton Keynes, UK) and Steven Manchester (Florida Museum of Natural History, Gainesville, USA). Research was financed through the grant “The Late Cretaceous flowering plant expansion in the context of the transgression of the Central European Sea” (2016/21/B/NZ8/02443) of the National Science Centre, Poland to ATH. Additional palynological analyses at Żeliszów by MS were financed by institutional support DKRVO 2019-2023 2.I.b of the Czech Ministry of Culture and RVO6785831 of the Institute of Geology of the Czech Academy of Sciences. All the above-mentioned persons and institutions are gratefully acknowledged.

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Appendix 1

Description of localities.

All the localities listed below are situated in the territory of Poland and belong to the present administrative unit called województwo dolnośląskie; before 1945 they were all parts of the German Provinz Schlesien (or Provinz Niederschlesien). Up to 1815, however, the border between Lusatia (Łužyca, Łužica, Łużyce, Lausitz) and Silesia was situated on the Kwisa (Queis) river, so the localities Ołdrzychów and Osiecznica are not in the historical territory of Silesia (Pysiewicz-Jędrusik et al. 1998); this is why they are included in the geological description of Saxony (Charpentier 1788).

Polish toponyms not found on official 1:25 000 maps (451.23 Bole­sławiec, published 1984; 451.32 Nowogrodziec, published 1976; 451.41 Gościszów, published 1984; 451.42 Raciborowice Górne, published 1992; 451.43 Lwówek Śląski, published 1976; 451.44 Pielgrzymka, published 1984) are after Staffa et al. (2002, 2003) and Jończy (2016). Corresponding German maps are the 1:25 000 Meßtischblätter: 4758 Siegersdorf (published 1943); 4759 Bunzlau (published 1943); 4858 Naumburg a.Q. (published 1937); 4859 Löwen­berg (published 1937); 4860 Gröditzberg (published 1939).

Bolesławiec (Bunzlau).—The locality yielding Cretaceous (Santonian) plant fossils was described by Roemer (1887, 1889) as located a quarter of a mile south-east from the town centre along the road to Łosice (then Looswitz or Losswitz), so at about 51°15’8”N 15°34’57”E (southwards from the present streets Starzyńskiego and Kosiby, now partly covered by a forest, partly constructed). All specimens are imprints in white ceramic clays, but in a few cases some organic matter is preserved as well. This is the type locality of Menispermites bunzlavensis Roemer, 1889. Assemblage 8.For confusion in respect of specimens coming from Bolesła­wiec and from Luisenhain, see the entry on the latter locality.

Czaple (Hockenau).—The village is situated ca. 8 km E from Lwówek. Two specimens come from a hill called Kopka (formerly Hockenberg; Williger 1882: 86). Assemblage 2.

Dobra (Doberau, Dobrau).—The village is situated ca. 3 km NW from Bolesławiec. A single specimen (MGUWr 5638p) of Geinitzia reichenbachii is labelled “Doberau, coll. Goeppert”.

Gaszów (Gähnsdorf, Gehnsdorf).—Williger (1882: 89) lists “Caulopteris sp. ind.” from that locality (5.5 km NE from Lwówek). Material not extant.

Hochkirch.—Williger (1882: 94) listed “Credneria sp. ind.” from “Hochkirch”. This toponym may correspond to Kościelec 6.5 km south of Legnica or to Przesieczany 10 km NE from Zgorzelec (Rymut 1999). However, this may also be a misprint for Holzkirch (Kościelnik 4 km south of Lubań). Material not traced.

Huzarski Skok (Husarensprung).—This toponym, referring to an episode reported variously as having taken place during either the Silesian wars in 1761 or the Napoleonic wars in 1813 (Staffa et al. 2002: 215), denotes a rock overhanging an abandoned channel of the Bóbr river west of Żerkowice. A single collect made in 1925 by E. Zimmermann is labelled “ca. 300 m W von Km 7,7 des Chaussee Löwenbg–Bunzlau (NW vom Husarensprung)” and consists of plant imprints in iron claystone. Assemblage 4.

Luisenhain.—Several plant fossils in white ceramic clays are labelled “Luisenhain” (MB). According to an undated short letter from [E.] Zimmermann to W. Gothan kept in MB, this name refers to a restaurant situated along the road from Lwówek Śl. to Bolesławiec. Its detailed situation is shown on a handwritten map by Berg made in 1936 and kept in BGR. The fossil locality is a (former) clay pit situated ca. 300 m south from the restaurant, thus very close to Ulina (see that entry). Assemblage 8. Unfortunately new MB labels had been prepared incautiously and some of them saying “Luisenhain bei Bunzlau” were transcribed solely as “Bunzlau”. The present author (ATH) was able to see that for some specimens that have both old and new labels. However, specimens having only new labels saying “Bunzlau” may come either indeed from Bolesławiec or from Luisenhain. Such specimens are described as coming from an uncertain locality in the Assemblage 8, among them are the types of Platanites willigeri.

Lwówek Śląski (Löwenberg in Schlesien).— Six previously unpublished fossil plant specimens, all collected before 1900, are labelled as coming from near Lwówek. Apparently, such an indication should be understood quite broadly.The specimen of Geinitzia reichenbachii (MB 1.1.1.) collected on 29th July, 1898 (presumably by E. Dresler) from light Turonian claystone is especially important because it is the only Turonian plant fossil from the studied area. Unfortunately, the label (“Lettengrube b. Löwenbg. Turonmergel.”) is insufficiently precise. According to Williger (1882), clay pits were situated east from the town. Assemblage 1. Five further specimens (MB.Pb.2008/0316–0319, 0362) label­led “im hangend. Thon d. Kohlen in der Quadersandsteinform; coll. Klotzsch” are in dark clays; today the nearest outcrop of the corresponding strata is at Rakowice Małe. Assemblage 5.

Nowe (Neuen).—Williger (1882: 107) listed Muensteria schneideriana and Cylindrites spongioides. Both are trace fossils and not plants.

Nowe Jaroszowice (Neu-Jäschwitz).—The village (formerly also Jasiowice) is located ca. 4 km south from Bolesławiec. A clay mine situated east from Gröbel-Vorwerk (itself located NW from the village; Staffa et al. 2002: 361) yielded a few plant fossils found between 1912 and 1916 and kept in MB. Assemblage 7.

Ocice (Ottendorf).—The village is situated approximately halfway between Bolesławiec and Nowogrodziec. Two specimens of Dryophyllum westerhausianum come from the quarry (details unknown). Williger (1882: 108) lists a Geinitzia specimen from iron claystone (specimen not found).

Ołdrzychów (Ullersdorf am Queis).—Five Geinitzia twigs (collected in 1863, 1874, and 1877) come from this locality (now part of the town Nowogrodziec; coordinates of the church in Ołdrzychów: 51°11’46”N 15°23’7”E). The precise origin of the plant fossils is unknown. According to the lithology, they belong to the Assemblage 5.Confusion between Ullersdorf am Queis (Ołdrzychów) and Ullersdorf am Bober (Ulina) was taking place already among German-speaking palaeontologists, as testified by MB labels on which the name of either locality was corrected into the other (in both directions). According to Williger (1882), the only plant fossils found at Ołdrzychów are Geinitzia in clays. On the contrary, a more diversified angiosperm assemblage is known from Ulina; some of these specimens are mislabelled at MB [for example “Salicites dubius m. foliis latioribus Göppert” reported from Ulina by Williger (1882) but labelled as coming from Ołdrzychów]. Milewicz (1997: 31) misread Williger’s data and erroneously listed five species of angiosperms from Ulina as coming from Ołdrzychów.

Osiecznica (Wehrau).—This locality (the birthplace of the famous geologist A.G. Werner) is situated in the valley of Kwisa north from Nowogrodziec. The geological setting is relatively complicated, because similar lithologies occur in the Cretaceous and in the Oligocene (see Badura et al. 2011: 28–32). According to Williger (1882: 113–114), the palm Flabellaria chamaeropifolia Goeppert, 1836b, is Oligocene in age, but the seeds described from the environs of Osiecznica and nearby Kliczków (Klitschdorf) as Palmacites legitimus Goeppert, 1878 are Cretaceous. The material of the latter could not be traced.

Otok (Uttig).—The village is situated ca. 4 km SW from Bolesławiec. Three plant specimens come from here, one of which is located “am Bober, südl. v. Uttig”. It is possible that all the specimens labelled as “Otok” come from the quarries in the Bóbr valley. Assemblage 6.

Rakowice Małe (Wenig-Rackwitz).—The main locality is a large quarry (Rakowiczki mine; entrance: 51°9’58”N 15°32’48”E, western end: 51°9’58”N 15°32’25”E) situated on the southern flank of the Ostrzyca (Steinberg) hill. It was abandoned about 2009. Rocks that can be observed in the quarry include Coniacian sandstone belonging to the Żerkowice Member of the Rakowice Wielkie Formation, upper Coniacian or lower Santonian coaly clays belonging to the Nowogrodziec Member of the Czerna Formation, and Santonian sandstone belonging to the Czerna Formation; a detailed sedimentological account was given by Leszczyński (2010). Most of the plant fossils come from the Nowogrodziec Member that can be further subdivided into a multicoloured basal part with plant-bearing iron clays (Assemblage 4; the richest level according to Williger 1882: 104) and dark clays with coal intercalations (Assemblage 5; Williger 1882: 104–105). Santonian sandstone yielded rare imprints grouped as Assemblage 6. Besides the quarry, plant fossils were collected in other outcrops and in coal mines. Neither the outcrops nor the mines exist anymore. The outcrops are described on MB labels as located between the Ostrzyca hill and the Bóbr river. The mines were active from about 1789 to the second half of the nineteenth century (Haacke 1924, Maciejak and Maciejak 2013). The mines Gottes Segen and Georg Wilhelm were located west from the present quarry (Maciejak and Maciejak 2013: fig. 4), Entremonia was on the riverbank of the Bóbr, whereas Tremonia was located a few kilometres further northwest, near Andrzejówka (formerly Andreasthal, now a part of Kotlice, see Staffa et al. 2003: 87; erroneously given as a part of Włodzice Małe by Maciejak and Maciejak 2013). “Rakowice Małe” (without further details) is the type locality of the fern spore Sporites appendicifer Thiergart, 1942 (now Appendicisporites). One may presume that both the palynological material of Thiergart (1942) and Krutzsch (1958) as well as mesofossils of Knobloch and Mai (1986) came from the quarry, as the mining activity in the area is supposed to have stopped earlier.

Ulina (Ullersdorf am Bober).—Formerly a village (the name does not appear on the official Polish 1 : 25 000 map), now a part of Kraszowice. A tile factory was functioning there till the 1990-ies. Ceramic clays were exploited on a hill north-east from the village (ca. 51°11’57”N 15°33’36”E) in pits up to 5 m deep (information gathered from habitants in April 2018); as of 2018, these former excavations are completely overwhelmed. One may presume that rich collections of fossil angiosperms labelled as Ulina (Williger 1882: 103) come from sandstone found in such clay pits. Assemblage 6.

See also the entry on Luisenhain.

For the explanation of confusion between Ołdrzychów (Ullersdorf am Queis) and Ulina (Ullersdorf am Bober), see the entry on the former locality.

Wartowice (Neu-Warthau).—The village is situated ca. 5 km SE from Bolesławiec; a few quarries, exploited since the Middle Ages, are located south from the village (Staffa et al. 2002: 613). Several plant species are known from the Wartowice beds at the type locality (Williger 1882: 84). Assemblage 2.

Włodzice (Walditz).—Two specimens of Geinitzia (MGUWr, coll. Goeppert) are labelled “Walditz”; it is uncertain whether this refers to Włodzice Małe (Wenig-Walditz) ca. 2 km N from Rakowice Małe on the left bank of the Bóbr, or to Włodzice Wielkie (Gross-Walditz) directly opposite on the right bank of the Bóbr. Based on lithology, these specimens are tentatively included into the Assemblage 6.

Zbylutów (Deutmannsdorf).—An outcrop of the Wartowice beds situated on Karczmisko (Kretschamberg) hill NE from Zbylutów yielded a few plant fossils. Assemblage 2.

Żeliszów (Giersdorf).—An old quarry situated ca. 1 km SE from the village was re-activated about 2017. The environs of the quarry were erroneously interpreted as entirely belonging to the Rakowice Wielkie Formation by Baraniecki et al. (1955), but in 2017 a previously unnoticed occurrence of coaly layers (Nowogrodziec Member) with mesoflora was discovered (first signalled by Halamski et al. 2018b). Assemblage 5. The trunk of the tree fern Protopteris singeri described by Goeppert (1836) from Żeliszów was interpreted as coming from either Turonian or Coniacian sandstone (Greguš et al. 2013). According to the data in Williger (1882: 87), the Coniacian age (Assem­blage 3) should be preferred. According to Milewicz (1997: 31), Debeya serrata was listed from this locality by Roemer (1886); however, such an information is not given in the referred paper; no other reference on the presence of Debeya or Dryophyllum at Żeliszów could be traced.

Żerkowice (Sirgwitz).—A quarry exploiting Coniacian sandstone is located north from the village at 51°9’42”N 15°34’17”E. Milewicz (1997) was still able to observe coaly sediments (analogous to those cropping out in Rakowice Małe) in this quarry, but as of 2017 this part of the succession was completely covered (ATH and P. Raczyński, personal observations). Rich collections of fossil plants belonging to to Assemblages 4, 5, and 6 are kept in MB.

Appendix 2

German-Polish dictionary of toponyms.

The following is provided to facilitate interpreting pre-1945 literature. Hydronyms are listed for reference purposes only. For the names of coal mines, see the entry on Rakowice Małe in the Appendix 1.

Bober – Bóbr (river)

Bunzlau – Bolesławiec

Deutmannsdorf – Zbylutów

Doberau – Dobra

Gähnsdorf (Gehnsdorf) – Gaszów

Giersdorf – Żeliszów

Hockenau – Czaple

Klitschdorf – Kliczków (see Osiecznica)

Kretschamberg – Karczmisko hill (see under Zbylutów); not to be confused with Karczmarka (Kretschamberg) near Trzebień (Kittlitztreben).

Löwenberg (in Schlesien) – Lwówek Śląski

Naumburg am Queis – Nowogrodziec

Neu-Jäschwitz – Nowe Jaroszowice

Neuen – Nowe

Neu-Warthau – Wartowice

Ottersdorf – Ocice

Queis – Kwisa (river)

Ullersdorf am Bober – Ulina

Ullersdorf am Queis – Ołdrzychów

Sirgwitz – Żerkowice

Uttig – Otok

Walditz – Włodzice

Wehrau – Osiecznica

Wenig-Rackwitz – Rakowice Małe

Appendix 3

Palynoassemblage A—list of taxa.

Dinocysts and acritarchs

Alterbia sp.

Chatangiella verrucosa (Manum, 1963) Lentin and Williams, 1976

Dinogymnium cretaceum (Deflandre, 1936) Evitt, Clarke, and Verdier, 1967

Dinogymnium sp.

Fromea amphora Cookson and Eisenack, 1958

Isabelidinium sp.

Micrhystridium sp.

Spinidinium sp.

Spiniferites ramosus var. ramosus (Ehrenberg, 1838) Davey and Williams, 1966

Subtilisphaera sp.

Surculosphaeridium longifurcatum (Firtion, 1952) Davey, Downie, Sarjeant, and Williams, 1966

Fungal spores

Dicellaesporites sp.

Pluricellaesporites psilatus Clarke, 1965

Prasinophytes

Crassosphaera sp.

Leiosphaeridia sp.

Pterospermella helios (Cookson and Eisenack, 1958) Eisenack, 1972

Tasmanites sp.

Non-marine algae

Ovoidites parvus Nakoman, 1966

Paralecaniella sp.

Tetraporina sp.

Schizocystia sp.

Bryophytes s.l.

Cingutriletes clavus Dettmann, 1963

Stereisporites antiquasporites Dettmann, 1963

Stereisporites psilatus Detmann, 1963

Stereisporites sp.Zlivisporis blanensis Pacltová, 1961

Zlivisporis simplex (Cookson and Dettmann, 1958) Braman, 2001

Zlivisporis sp.

Lycophytes

Camarozonosporites ambigens (Fradkina, 1967) Playford, 1971

Camarozonosporites insignis Norris, 1967

Echinatisporis varispinosus Srivastava, 1975

Retitriletes austroclavatidites (Cookson, 1953) Döring, Krutzsch, Mai, and Schulz in Krutzsch, 1963

Pteridophytes

Aequtriradites spinulosus (Delcourt and Sprumont, 1955) Cookson and Dettmann 1961

Apiculatisporites asymmetricus Cookson and Dettmann, 1958

Appendicisporites foveolatus (Deák, 1962) Wingate, 1980

Appendicisporites cristatus (Markova in Ivanova and Markova, 1961) Pocock, 1964

Appendicisporites sp.

Biretisporites cf. deltoideus (Rouse, 1949) Dettmann, 1963

Cicatricosisporites potomacensis Brenner, 1963

Cicatricosisporites venustus Deák, 1963

Cicatricosisporites sp.

Cicatricososporites cf. phaseolus (Delcourt and Sprumont, 1955) Krutzsch, 1959

Clavifera triplex (Bolkhovitina, 1966) Bolkhovitina, 1968

Concavissimisporites punctatus Brenner, 1962

Concavissimisporites sp.

Converrucosisporites proxigranulatus Brenner, 1962

Converrucosisporites sp.

Corniculatisporites alekhinii (Bolchovitina, 1953) Kuvaeva, 1972

Coronatispora sp.

Corrugatisporites sp.

Costatoperforosporites cf. foveolatus Deák, 1962

Cyathidites minor Couper, 1953

Deltoidospora juncta (Kara-Murza, 1954) Singh, 1964

Deltoidospora sp.

Dictyophyllidites harrisii Couper, 1958

Foveogleicheniidites confossus (Hedlund, 1966) Burger in Norvick and Burger, 1976

Gleicheniidites apilobatus Brenner, 1963

Gleicheniidites circiniidites (Cookson, 1953) Brenner, 1963

Gleicheniidites senonicus Ross, 1949

Ischyosporites pseudoreticulatus (Couper, 1958) Srivastava, 1975

Ischyosporites sp.

Klukisporites pseudoreticulatus Couper, 1958

Laevigatosporites ovatus (Wilson and Webster, 1946) Thomson and Pflug, 1953

Leptolepidites sp.

Osmundacidites cf. wellmanii Couper, 1953

Osmundacidites sp.

Ornamentifera baculata Singh, 1971

Pilosisporites sp.

Polypodiaceoisporites sp.

Matonisporites sp.

Plicifera delicata Bolchovitina, 1968

Polypodiidites sp.

Reticulosporis gallicus Deák, 1967

Toroiosporis sp.

Undulatosporites sp.

Varirugosisporites verrucosus (Deák, 1964) Juhász, 1979

Verrucatosporites sp.

Gymnosperms

Cerebropollenites mesozoicus (Couper, 1958) Nilsson, 1958

Classopollis classoides (Pflug, 1953) Pocock and Jansonius, 1961

Classopollis martinotii Reyre, 1970

Classopollis major Groot and Groot, 1962

Classopollis sp.

Cycadopites nitidus (Balme, 1957) Pocock, 1970

Cycadopites sp.

Ephedripites sp.

Monosulcites minimus Cookson, 1947

Monosulcites sp.

Parvisaccites radiatus Couper, 1958

Pinuspollenites sp.

Podocarpidites sp.

Sequoiapollenites sp.

Taxodiaceaepollenites hiatus (Potonié, 1931) Kremp, 1949

Taxodiaceaepollenites sp.

Taxodiaceaepollenites vacuipites (Wodehouse, 1933) Wingate, 1980

Angiosperms

Bohemiapollis sp.

Bohemiperiporis zaklinskai Pacltová, 1968

Clavatipollenites minutus Couper, 1958

Clavatipollenites sp.

Complexiopollis complicatus Góczán, 1964

Complexiopollis sp.

Emscheripollis sp.

Interporopollenites cf. turgidus (Weyland and Krieger, 1953) Tschudy, 1975

Interporopollenites sp.

Liliacidites sp.

Minorpollis minimus Krutzsch, 1959

Neotriangulipollis sp.

Neotriangulipollis cf. piolencipollis Groot and Krutzsch, 1967

Nyssapollenites sp.

Oculopollis minimus Siegl-Farkas, 1982

Oculopollis spp.

Pecakipollis sernoensis Pacltová, 1970

Pecakipollis sp.

Pflugipollis sp.

Piolencipollis sp.

Plicapollis serta Pflug, 1953

Plicapollis sp.

Pseudoplicapollis peneserta Krutzsch in Góczán et al., 1967

Pseudoplicapollis spp.

Psilatricolpites subtilis (Groot, Penny, and Groot, 1963) Singh, 1983

Retitricolporites sp.

Semioculopollis minimus (Góczán, 1964) Goczán, Groot, Krutzsch, and Pacltová, 1967

Striatopollis paraneus (Norris, 1967) Singh, 1971

Tricolporoidites subtilis Pacltová, 1971

Tricolpites vulgaris Brideaux, 1968

Tricolpites minutus (Brenner, 1963) Dettmann, 1973

Tricolpites sp.

Tricolporites sp.

Trudopollis fossulotrudens (Pflug in Thomson and Pflug, 1953) Pflug, 1953

Trudopollis spp.

Vacuopollis sp.

Appendix 4

New combinations.

Dryophyllum westerhausianum (Richter, 1904) Halamski and Kvaček comb. nov.—Basionym: Bignonia westerhausiana Richter, 1904 [Richter, Über Kreidepfl. Umgeb. Quedlinburgs: 20; pl. 2: 1–5; 1904].

Dewalquea paulinae (Halamski, 2013) Halamski comb. nov.—Basionym: Debeya (Dewalquea) paulinae Halamski, 2013 [Acta Palaeontologica Polonica 58: 419, fig. 2B].

Acta Palaeontol. Pol. 65 (4): 811–878,

2020 https://doi.org/10.4202/app.00744.2020