Organic-Walled Dinoflagellate Cyst Records from a Prospective Turonian – Coniacian (Upper Cretaceous) GSSP, Słupia Nadbrzeżna, Poland

Accepted Manuscript

Organic-walled dinoflagellate cyst records from a prospective Turonian – Coniacian (Upper Cretaceous) GSSP, Słupia Nadbrzeżna, Poland

Kate Olde, Ian Jarvis, Martin Pearce, Ireneusz Walaszczyk, Bruce Tocher

PII: S0195-6671(16)30068-4 DOI: 10.1016/j.cretres.2016.04.010 Reference: YCRES 3388

To appear in: Cretaceous Research

Received Date: 2 July 2015 Revised Date: 31 March 2016 Accepted Date: 15 April 2016

Please cite this article as: Olde, K., Jarvis, I., Pearce, M., Walaszczyk, I., Tocher, B., Organic-walled dinoflagellate cyst records from a prospective Turonian – Coniacian (Upper Cretaceous) GSSP, Słupia Nadbrzeżna, Poland, Cretaceous Research (2016), doi: 10.1016/j.cretres.2016.04.010.

This is a PDF file of an unedited manuscript that has been accepted for publication. As a service to our customers we are providing this early version of the manuscript. The manuscript will undergo copyediting, typesetting, and review of the resulting proof before it is published in its final form. Please note that during the production process errors may be discovered which could affect the content, and all legal disclaimers that apply to the journal pertain. ACCEPTED MANUSCRIPT spp. spp. . ramosus anyosphaeridium . cooksoniae . buspina . mantellii O. complex Florentinia spp. F H. recurvatum T X. ceratoides O. poculum E. phragmites H. bowerbankii S. turonica . C. reticulata 9. 14. 13. 15. 16. 17. F 18. 2. 3. S. r 4. S. longifurcatum 7. O. operculata 8. 10 12. Pervosphaeridium Stage Zone SamplesHeight (m)Lithology 1. C. d. distinctum 5. F 6. 11.

29 7

6 erectus Event 24 23 HO S. 21 5 turonica

lower Coniacian 20

Cremnoceramus d.erectus LOFO C.d. erectus 18 MANUSCRIPT 17 4 16

Cww waltersdorfensis Event Dinocyst 14 abundance maximum 13 3 12 11 10

uronian Acme C.d. 9 2

T distinctum 8

upper 5 1 herbichi Event 4 Mytiloides scupini

2 opoka (siliceous marl) 1 0 quantified opoka abundance with rare cherts 25 5 Słupia Nadbrzeżna Relative abundance (%) present cherty opoka

Olde et al. Fig. 4 ACCEPTED Olde et al. / Cretaceous Research ** (2016) ** - ** ACCEPTED MANUSCRIPT 1 Organic-walled dinoflagellate cyst records from a prospective Turonian –

2 Coniacian (Upper Cretaceous) GSSP, Słupia Nadbrze żna, Poland

4 Kate Olde a, Ian Jarvis a, * , Martin Pearce b, a , Ireneusz Walaszczyk c, Bruce Tocher d

5 aKingston University London, Department of Geography and Geology, Kingston upon

6 Thames KT1 2EE, UK

7 bEvolution Applied Ltd, 50 Mitchell Way, Upper Rissington, Cheltenham GL54 2PL, UK

8 cFaculty of Geology, University of Warsaw, Al. wirki i Wigury 93, PL-02-089 Warszawa,

9 Poland

10 dStatoil, 2103 CityWest Blvd Ste 800, Houston TX 77042-2834, USA

12 Keywords: Turonian, Coniacian, GSSP, Palynology, Dinoflagellate cyst 13 MANUSCRIPT 14 ABSTRACT

15 A river section at Słupia Nadbrze żna, central Poland, has been proposed as a candidate

16 Turonian – Coniacian (Cretaceous) GSSP, in combination with the Salzgitter-Salder quarry

17 section of Lower Saxony, Germany. Results of a high-resolution (25 cm) palynological study

18 of the boundary interval in the Słupia Nadbrze żna section are presented. Terrestrial

19 palynomorphs are rare; marine organic-walled dinoflagellate cysts dominate the palynological 20 assemblage. TheACCEPTED dinoflagellate cyst assemblage has a low species richness (5 – 11 per 21 sample; total of 18 species recorded) and diversity (Shannon index H = 0.8 – 1.4), dominated

22 by four taxa: Circulodinium distinctum subsp. distinctum; Oligosphaeridium complex;

23 Spiniferites ramosus subsp. ramosus; Surculosphaeridium longifurcatum . Declining

24 proportions of O. complex and S. ramosus subsp. ramosus characterise the uppermost

Olde et al. / Cretaceous Research ** (2016) ** - ** ACCEPTED MANUSCRIPT 25 Turonian, with an increased dominance of S. longifurcatum in the lower Coniacian. The

26 Turonian – Coniacian boundary interval includes an acme of C. distinctum subsp. distinctum

27 in the upper Mytiloides scupini Zone, a dinoflagellate cyst abundance maximum in the

28 Cremnoceramus walterdorfensis walterdorfensis Zone, and the highest occurrence of

29 Senoniasphaera turonica in the basal Coniacian lower Cremnoceramus deformis erectus

30 Zone. Most previously reported Turonian – Coniacian boundary dinoflagellate cyst marker

31 species are absent; a shallow-water oligotrophic epicontinental depositional setting, remote

32 from terrestrial influence, likely limited species diversity and excluded many taxa of

33 biostratigraphic value.

34 * corresponding author. Email address: [email protected] (I. Jarvis).

35 1. Introduction 36 The Słupia Nadbrze żna river cliff section, centralMANUSCRIPT Poland, combined with the Salzgitter- 37 Salder quarry of Lower Saxony, Germany, has been proposed as a composite Global

38 Boundary Stratotype Section and Point (GSSP) for the base of the Coniacian Stage at 89.75

39 Ma (Walaszczyk and Wood, 1998; Walaszczyk et al., 2010; Ogg et al., 2012).

40 During the Late Cretaceous, Słupia Nadbrzeżna was located in a pelagic carbonate

41 setting on the eastern margin of the Central European epicontinental basins system (Voigt et

42 al., 2008; Fig. 1). The section forms part of the expanded Upper Cretaceous succession of the

43 Middle Wisła (Vistula) River, and is exposed in the western Wisła river cliff in the village of 44 Słupia Nadbrze żACCEPTEDna (50.9501°N, 21.8078°E), situated 150 km SSE of Warsaw. The exposure 45 exists in a poor state, requiring excavation before study (Walaszczyk et al., 2010), but yields

46 well-preserved inoceramid bivalve assemblages. The approximately 10 m section consists of

47 opoka (siliceous marl) facies with varying proportions of chert (Fig. 2).

Olde et al. / Cretaceous Research ** (2016) ** - ** ACCEPTED MANUSCRIPT 48 The Słupia Nadbrze żna section spans the upper Turonian uppermost Mytiloides scupini

49 Zone to the lower Coniacian lowest Cremnoceramus deformis erectus Zone, and provides an

50 expanded and more complete Turonian – Coniacian boundary record than the better-exposed

51 Salzgitter-Salder section (Wood et al., 2004; Walaszczyk et al., 2010), which was proposed as

52 the base Coniacian GSSP by the Coniacian Working Group of the Subcommission on

53 Cretaceous Stratigraphy (Kauffman et al., 1996). The proposed base of the Coniacian is taken

54 at the lowest occurrence of the inoceramid bivalve Cremnoceramus deformis erectus (Meek,

55 1877) [= C. rotundatus (sensu Tröger, 1967 non Fiege, 1930)]. This lies above the lowest

56 occurrence of the ammonite Forresteria (Harleites) petrocoriensis (Coquand, 1859),

57 traditionally used as a Coniacian marker in the stratotype area of the Aquitaine Basin

58 (Kennedy and Walaszczyk, 2004; Fig. 3). Inoceramid records indicate condensation and a

59 minor hiatus at the stage boundary in the stratigraphically more extensive section at

60 Salzgitter-Salder (Wood et al., 2004; Walaszczyk et al., 2010); this hiatus provides the 61 rationale for using the two sections as a composite MANUSCRIPT GSSP. 62 The lithostratigraphy, macrofossil, foraminiferal and nannofossil biostratigraphy and

63 carbon stable-isotope chemostratigraphy of Słupia Nadbrze żna and Salzgitter-Salder have

64 been described by Walaszczyk and Peryt (1998), Walaszczyk and Wood (1998), Kennedy and

65 Walaszczyk (2004), Wood et al. (2004), Lees (2008) and Walaszczyk et al. (2010). In terms

66 of carbon stable isotopes, the Turonian – Coniacian boundary lies at an inflection point from

67 long-term falling to rising δ13 C values (Voigt and Hilbrecht, 1997; Wiese, 1999; Jarvis et al., 68 2006). Most of ACCEPTEDthe succession at Słupia Nadbrze żna represents the upper part of the broad 69 δ13 C minimum that occurs globally at the Turonian – Coniacian boundary (Wendler, 2013;

70 Jarvis et al., 2015), the Navigation Carbon Isotope Event (CIE; Fig. 2) of Jarvis et al. (2006).

71 However, carbon and oxygen stable-isotope values from Słupia Nadbrze żna show high-

72 amplitude variation with lithology (Figs. 2, 3), indicating that the section has likely been

Olde et al. / Cretaceous Research ** (2016) ** - ** ACCEPTED MANUSCRIPT 73 affected by diagenesis (cf. Walaszczyk et al., 2010). Carbon stable-isotope values are around

74 1 ‰ lower than those found at an equivalent level in Salzgitter-Salder (Fig. 2), offering

75 further evidence of a diagenetic overprint.

76 2. Materials and Methods

77 Twenty-one samples from the Słupia Nadbrze żna section that had been collected for

78 stable-isotope analysis (Walaszczyk et al., 2010) were selected for palynological preparation.

79 Splits (20 g) of chipped samples were processed for quantitative palynological analysis.

80 Palynomorphs >15 m were concentrated by a commercial processing company (PLS Ltd,

81 Holyhead, UK) using the HCl-HF method of Lignum (2009), modified from Lignum et al.

82 (2008, ‘Company B’ methodology). Oxidation of the samples was unnecessary due to the low

83 concentration of amorphous organic matter present. All samples were spiked with tablets

84 containing the modern spore Lycopodium to allow statistically valid quantitative analysis 85 (dinoflagellate cysts per gram, dpg). MANUSCRIPT 86 Palynomorph identification and counting was undertaken using a Leitz Laborlux S light

87 microscope with a 40x objective. Three hundred organic walled dinoflagellate cysts

88 (dinocysts) were identified per sample. Broken or partial specimens were added to the count

89 only if there was more than half of the specimen present. Unidentifiable specimens were

90 recorded as ‘indeterminate’, and were not included in the count of 300, but were included

91 when calculating total palynomorphs per gram. Following this count, the remainder of the

92 slide was scanned to identify any additional species, which were marked as ‘present’, but in

93 abundances too ACCEPTEDlow to be recorded among the 300. The presence of any other palynomorphs

94 such as pollen grains, spores, acritarchs and foraminiferal test linings was also noted.

95 All materials used in this study are held by the Department of Geography and Geology,

96 Kingston University London (London, UK).

Olde et al. / Cretaceous Research ** (2016) ** - ** ACCEPTED MANUSCRIPT 97 3. Results and discussion

98 Dinoflagellate cysts recovered from Słupia Nadbrze żna are well preserved, but the

99 assemblage exhibits a low species richness (18 species recorded), with between 5 and 11

100 species identified in each sample (Fig. 3; Appendix A, B). Dinoflagellate cysts are numerous

101 (up to ~1500 dinoflagellate cysts per gram of sediment; Fig. 3) and at least 300 specimens

102 were identified in all samples. Species diversity is low with Shannon (Shannon–Wiener)

103 index values of H = 0.8 – 1.4 (Fig. 3). Approximately 90 % of the assemblage throughout the

104 section is made up of four species: Circulodinium distinctum subsp. distinctum ,

105 Oligosphaeridium complex , Spiniferites ramosus subsp. ramosus and Surculosphaeridium

106 longifurcatum (Figs. 4, 5.4 – 5.7). Approaching the stage boundary, O. complex and S.

107 ramosus subsp. ramosus decline in relative abundance, while S. longifurcatum increases,

108 showing a particular peak around the waltersdorfensis inoceramid Event.

109 Dinoflagellate cyst abundance does not display a consistent long-term trend but peaks 110 immediately above the waltersdorfensis Event, inMANUSCRIPT the mid-C. w. waltersdorfensis Zone (Fig. 111 3). Diversity shows a progressive smooth decline through the section, but with a pronounced

112 trough in the uppermost Turonian coincident with the abundance maximum. Other diversity

113 and dominance indices (not plotted; see Appendix B) closely follow the Shannon index trend.

114 Domination of the assemblage by S. longifurcatum accounts for low Shannon index diversity

115 values over this interval (Figs. 3, 4). A sharp recovery of diversity occurs at the stage

116 boundary, followed by continuing falling values above. 117 TerrestrialACCEPTED palynomorphs occur sporadically in low abundance through the section, 118 generally with < 10 bisaccate pollen grains per gram (< 1 % of the palynomorphs counted),

119 with the exception of the lowest sample, in which 27 bisaccate pollen grains per gram were

120 recorded. Pollen grains occur consistently only in the lowest metre of the section (Fig. 3).

Olde et al. / Cretaceous Research ** (2016) ** - ** ACCEPTED MANUSCRIPT 121 3.1. Dinoflagellate cyst biostratigraphy

122 Surculosphaeridium longifurcatum , which was used by Williams (1977) to define an

123 acme zone representing the Turonian, is a frequent component of the Słupia Nadbrze żna

124 Turonian – Coniacian boundary assemblage (Figs. 4, 5.6). However, S. longifurcatum is a

125 long-ranging species, from upper Barremian (Prössl, 1990) to Campanian (Williams and

126 Bujak, 1985; Kirsch, 1991; Williams et al., 1993; Pearce, 2000). At Słupia Nadbrze żna, it is

127 most abundant (40 – 68 % of the assemblage) higher in the section, in the uppermost

128 Turonian – basal Coniacian. A comparable trend has been observed in the Bch-1 core near

129 Prague, Czech Republic (Olde et al., 2015a, b). Here, Surculosphaeridium longifurcatum

130 occurs throughout the uppermost Cenomanian – lower Coniacian, but it is only common in

131 the uppermost Cenomanian – basal middle Turonian and then again in the uppermost upper

132 Turonian M. scupini Zone to lower Coniacian, including a peak around the Navigation CIE. 133 Circulodinium distinctum subsp. distinctum MANUSCRIPTconstitutes ~40% of the dinoflagellate cysts 134 assemblage throughout the Słupia Nadbrze żna section (Figs. 4, 5.8). Turonian acmes of C.

135 distinctum subsp. distinctum have been found to have biostratigraphic significance in other

136 European sections (FitzPatrick, 1995; Pearce, 2000; Pearce et al., 2003; Olde et al., 2015a)

137 but, to our knowledge, an acme at the Turonian – Coniacian boundary has not been recorded

138 elsewhere.

139 Senoniasphaera turonica , a characteristic Turonian species (Pearce et al., 2011), was

140 identified in 4 samples from the Słupia Nadbrze żna section (Figs. 4, 5.2). Its highest 141 occurrence (HO)ACCEPTED is at 5.5 m in the lower Coniacian C. erectus Zone, below the erectus Event. 142 The highest occurrence of this species has been recorded near the Turonian – Coniacian

143 boundary elsewhere, extending into the basal Coniacian in the English Chalk (Pearce, 2000;

144 Pearce et al., 2003, 2011). In the Czech Republic Bch-1 well, the HO of this species occurs in

145 the mid-S. neptuni Zone (upper Turonian), below the Hitch Wood CIE (Olde et al., 2015a).

Olde et al. / Cretaceous Research ** (2016) ** - ** ACCEPTED MANUSCRIPT 146 The HO of Oligosphaeridium poculum occurs in the lower Coniacian at Słupia

147 Nadbrze żna (Fig. 4). The HO of this species was considered to be lower Turonian by

148 Williams et al. (2004). However, in NW Europe, a regional reoccurrence datum level for the

149 species occurs in lower to middle Turonian (Pearce, 2000; Pearce et al., 2009, Olde et al.,

150 2015a), and it is recorded sporadically above this, ranging into the Coniacian in the Trunch

151 borehole of eastern England (Pearce, 2000) and in the Běchary Bch-1 borehole of the Czech

152 Republic (Olde et al., 2015a). Our records from Słupia Nadbrze żna support an extended range

153 for this taxon.

154 The main Turonian – Coniacian boundary dinoflagellate cyst events observed in the

155 Czech Republic and elsewhere (Olde et al., 2015a) have not been recorded at Słupia

156 Nadbrze żna; for example, the lowest occurrences of Surculosphaeridium belowii and

157 Cribroperidium wilsonii , and the lowest common occurrence of Oligosphaeridium

158 pulcherimum, are unrepresented due to an absence of the index species. Additionally, other 159 key boundary datum levels, such as the highest MANUSCRIPT common occurrence of Cauveridinium 160 membraniphorum immediately below the Navigation CIE in the uppermost Turonian, and the

161 HO Kiokansium unituberculatum immediately above the Navigation CIE in the lower

162 Coniacian (Olde et al., 2015a) are unrepresented, perhaps due to the very limited stratigraphic

163 range of the Polish section, which is largely confined to the Navigation CIE interval (Fig. 2).

164 3.2. Palaeoenvironmental interpretation

165 The dinoflagellate cyst assemblages at Słupia Nadbrze żna are characterised by low

166 abundances, lowACCEPTED species richness and diversity, and an absence of peridinioid taxa, which

167 typify environments with elevated nutrient levels (Jacobsen and Anderson, 1986; cf. Olde et

168 al., 2015b). The dinoflagellate cyst taxon C. distinctum subsp. distinctum is placed within the

169 Areoligeraceae, a family that is usually considered to have inner-neritic and reduced salinity

Olde et al. / Cretaceous Research ** (2016) ** - ** ACCEPTED MANUSCRIPT 170 environmental affinities (e.g. Batten, 1982; Harker et al., 1990; Wilpshaar and Leereveld,

171 1994; Leereveld, 1995; Pearce, 2000). Surculosphaeridium longifurcatum has also been

172 previously attributed an inner-neritic affinity (Pearce, 2000; Pearce et al., 2003).

173 Foraminiferal assemblages at Słupia Nadbrze żna show a dominance of benthic species

174 (~80 %) in the upper Turonian (Fig. 3), with a short (one sample) increase in planktonic taxa

175 at the Turonian – Coniacian boundary (~45 %), above which planktonic forms become even

176 rarer, making up less than 10 % of foraminiferal specimens in the Coniacian (Walaszczyk and

177 Peryt, 1998; Walaszczyk et al., 2010). This contrasts strongly with the Salzgitter-Salder

178 succession, where planktonic taxa constitute >50 % of the foraminiferal assemblage in the

179 uppermost Turonian, increasing through the M. scupini Zone to ~90 % across the stage

180 boundary and throughout the lower Coniacian C. erectus Zone (Walaszczyk et al., 2010).

181 Low planktonic/benthic ratios at Słupia Nadbrze żna support an inner-neritic setting for the

182 area at that time. 183 The Słupia Nadbrze żna section is poorly MANUSCRIPT exposed and weathered, offering the 184 possibility that the observed palynological and calcareous microfossil assemblages are not

185 solely a product of the depositional environment, but may have been modified by diagenesis

186 and/or weathering. Different dinoflagellate cyst species respond differently to oxidation, with

187 some being very sensitive and others being very resistant (Zonneveld et al., 1997). Modern

188 dinoflagellate cysts most vulnerable to degradation are often produced by heterotrophic

189 peridinioid species (Zonneveld et al., 1997, 2008). The absence of peridinioid cysts could 190 therefore be an artefactACCEPTED of preservation: most recovered forms identified are large and robust. 191 However, Zonneveld et al.’s (1997, 2008) studies focussed on Cenozoic peridinioid cysts

192 within the Congruentidiaceae family; there is little evidence to suggest that this selective

193 preservation applies equally to Late Cretaceous peridinioids. On balance, the lack of

Olde et al. / Cretaceous Research ** (2016) ** - ** ACCEPTED MANUSCRIPT 194 peridinioid specimens in the Słupia Nadbrze żna section is considered to most likely reflect the

195 depositional environment.

196 The combination of low dinoflagellate cyst species richness and diversity, and an

197 absence of peridinioid forms suggest stressed palaeoenvironmental conditions. The lack of

198 peridinioids, in particular, indicates an oligotrophic depositional environment. The prevalence

199 of C. distinctum subsp. distinctum and benthic foraminifera suggests a relatively shallow-

200 water ‘inner-shelf’ setting for Słupia Nadbrze żna during the late Turonian. However, the lack

201 of terrestrial palynomorphs is not typical of such an environment. The most likely

202 interpretation therefore is of a shoal setting within an extensive shallow epicontinental sea.

203 Rising sea levels accompanying the Turonian eustatic highstand limited siliciclastic

204 sedimentation in Poland to the margins of Fennoscandia (Krassowska, 1997; Walaszczyk in

205 Voigt et al., 2008), in the vicinity of Gda ńsk (Fig. 1). Słupia Nadbrze żna, situated more than

206 300 km to the SE, was sufficiently far from any landmass to account for the lack of terrestrial 207 palynomorphs. MANUSCRIPT 208 The influx of S. longifurcatum over the C. waltersdorfensis Event is coincident with a

209 minor negative δ13 C excursion that may be indicative of a short-term sea-level fall at this

210 level. This suggests that the relative abundance of S. longifurcatum is negatively correlated

211 with local sea level (i.e., it becomes more abundant during times of lowered sea level). The

212 subsequent ~0.5 ‰ positive-δ13 C excursion is coupled with a S. longifurcatum minimum, and

213 peaks in foraminifera planktonic/benthic ratio and dinoflagellate cyst diversity (Fig. 3). These 214 features likely reflectACCEPTED a short-term transgression coincident with the base Coniacian, as noted 215 also in the Czech Republic (Uli čný, et al. 2014; Jarvis et al., 2015; Olde et al., 2015b).

Olde et al. / Cretaceous Research ** (2016) ** - ** ACCEPTED MANUSCRIPT 216 4. Conclusions

217 Palynological investigations of the prospective Turonian – Coniacian GSSP at Słupia

218 Nadbrze żna reveal an assemblage dominated by well-preserved organic walled dinoflagellate

219 cysts, though abundance, species richness and diversity are low. Due to the paucity of

220 palynomorph species, few datum levels are of biostratigraphic utility. These include the

221 highest occurrence of Senoniasphaera turonica in the lowest Coniacian Cremnocermaus

222 deformis erectus Zone and, potentially, a dinoflagellate cyst abundance maximum in the

223 uppermost Turonian Cremnocermaus walterdorfensis walterdorfensis Zone.

224 Palynological results suggest a relatively shallow-water pelagic environment for the

225 Słupia Nadbrze żna Turonian – Coniacian boundary sediments, though diagenetic overprinting

226 or weathering evidenced by stable-isotope results may also have affected the assemblages.

227 Oligotrophic conditions in a distal epicontinental sea, remote from terrestrial influence, are

228 indicated by the low dinoflagellate cyst diversity, an absence of peridinioid species, and a 229 paucity of terrestrial palynomorphs. MANUSCRIPT

230 Acknowledgments

231 Kate Olde acknowledges receipt of a Kingston University London PhD studentship and

232 support by Statoil Petroleum AS contract 4501936147. Przemysław Gedl (Polish Academy of

233 Sciences), two anonymous referees, and editor Eduardo Koutsoukos provided valuable critical

234 reviews. 235 ACCEPTED

Olde et al. / Cretaceous Research ** (2016) ** - ** ACCEPTED MANUSCRIPT 236 Appendix A. Species list

237 List of dinoflagellate cyst species identified from Turonian – Coniacian boundary interval in

238 the Słupia Nadbrze żna section. Numbers refer to order of species plotted in Fig. 4. Selected

239 species are illustrated in Fig. 5. Numerical data are listed in Appendix B. Taxonomic

240 references are given in Fensome et al. (2008) and Pearce et al. (2011).

241 10. Cassiculosphaeridia reticulata Davey, 1969

242 1. Circulodinium distinctum subsp. distinctum (Deflandre and Cookson, 1955) Jansonius,

243 1986

244 15. Exochosphaeridium phragmites Davey et al., 1966

245 8. Florentinia buspina (Davey and Verdier, 1976) Duxbury, 1980

246 17. Florentinia cooksoniae (Singh, 1971) Duxbury, 1980; emend. Duxbury, 1980

247 5. Florentinia mantellii (Davey and Williams, 1966) Davey and Verdier, 1973

248 6. Florentinia spp. 249 16. Hystrichosphaeridium bowerbankii Davey and MANUSCRIPT Williams, 1966 250 11. Hystrichosphaeridium recurvatum (White, 1842) Lejeune-Carpentier, 1940

251 7. Odontochitina operculata (Wetzel, 1933) Deflandre and Cookson, 1955

252 2. Oligosphaeridium complex (White, 1842) Davey and Williams, 1966

253 13. Oligosphaeridium poculum Jain, 1977

254 12. Pervosphaeridium spp.

255 18. Senoniasphaera turonica (Prössl, 1990 ex Prössl, 1992) Pearce et al., 2011 256 3. Spiniferites ramosusACCEPTED subsp. ramosus (Ehrenberg, 1838) Mantell, 1854 257 4. Surculosphaeridium? longifurcatum (Firtion, 1952) Davey et al., 1966

258 9. Tanyosphaeridium spp.

259 14. Xenascus ceratioides (Deflandre, 1937) Lentin and Williams, 1973

Olde et al. / Cretaceous Research ** (2016) ** - ** ACCEPTED MANUSCRIPT 260 Appendix B. Numerical palynological data from the Turonian – Coniacian boundary interval

261 at Słupia Nadbrze żna.

262

263 References

264 Batten, D.J., 1982. Palynofacies and salinity in the Purbeck and Wealden of southern

265 England, in: Banner, F.T., Lord, A.R. (Eds.), Aspects of Micropalaeontology. George

266 Allen & Unwin, London, pp. 278–308.

267 Fensome, R.A., MacRae, R.A., Williams, G.L., 2008. DINOFLAJ2, Version 1. American

268 Association of Stratigraphic Palynologists, Data Series, 937.

269 FitzPatrick, M.E.J., 1995. Dinoflagellate cyst biostratigraphy of the Turonian (Upper

270 Cretaceous) of southern England. Cretaceous Research 16, 757–791.

271 Harker, S.D., Sarjeant, W.A.S., Caldwell, W.G.E., 1990. Late Cretaceous (Campanian) 272 organic-walled microplankton from the interior MANUSCRIPT plains of Canada, Wyoming and Texas: 273 biostratigraphy, palaeontology and palaeoenvironmental interpretation. Palaeontographica

274 Abteilung B 219, 243 pp.

275 Jacobsen, D.M., Anderson, D.M., 1986. Thecate heterotrophic dinoflagellates: feeding

276 behaviour and mechanisms. Journal of Phycology 22, 249–258.

277 Jarvis, I., Gale, A.S., Jenkyns, H.C., Pearce, M.A., 2006. Secular variation in Late Cretaceous

278 carbon isotopes and sea-level change: evidence from a new δ13 C carbonate reference

279 curve for the ACCEPTEDCenomanian - Campanian (99.6 - 70.6 Ma). Geological Magazine 143, 561–

280 608.

281 Jarvis I., Trabucho-Alexandre, J., Gröcke, D.R., Uli čný, D., Laurin, J., 2015. Stable-isotope

282 chemostratigraphy: intercontinental correlation of organic carbon and carbonate records,

Olde et al. / Cretaceous Research ** (2016) ** - ** ACCEPTED MANUSCRIPT 283 and evidence of climate and sea-level change during the Turonian (Cretaceous). The

284 Depositional Record 1, 53–90 doi: 10.1002/dep2.6.

285 Kauffman, E.G., Kennedy, W.J., Wood, C.J., 1996. The Coniacian stage and substage

286 boundaries, in: Rawson, P.F., Dhondt, A.V., Hancock, J.M., Kennedy, W.J. (Eds.),

287 Proceedings "Second International Symposium on Cretaceous Stage Boundaries" Brussels

288 8-16 September 1995. l'Institut Royal des Sciences Naturelles de Belgique, pp. 81–94.

289 Kennedy, W.J., Walaszczyk, I., 2004. Forresteria (Harleites) petrocoriensis (COQUAND,

290 1859) from the Upper Turonian Mytiloides scupini Zone of Slupia Nadbrzezna, Poland.

291 Acta Geologica Polonica 54, 55–59.

292 Kirsch, K.-H., 1991. Dinoflagellatenzysten aus der Oberkreide des Helvetikums und

293 Nordultrahelvetikums von Oberbayern. Munchner geowissenschaftliche Abhandlungen:

294 Reihe A, Geologie und Paläontologie 22, 1–306. 295 Krassowska, A., 1997. The epicontiental Permian MANUSCRIPTand Mesozoic in Poland. Upper Cretaceous. 296 Prace Pa ństwowego Instytutu Geologicznego 153, 367–402 (in Polish).

297 Leereveld, H., 1995. Dinoflagellate cysts from the Lower Cretaceous Rio Argos succession

298 (SE Spain). Laboratory of Palynology and Palaeobotany Contributions Series Utrecht 2, 1–

299 175.

300 Lees, J.A., 2008. The calcareous nannofossil record across the Late Cretaceous

301 Turonian/Coniacian boundary, including new data from Germany, Poland, the Czech 302 republic and England.ACCEPTED Cretaceous Research 29, 40–64. 303 Lignum, J., 2009. Cenomanian (Upper Cretaceous) palynology and chemostratigraphy:

304 dinoflagellate cysts as indicators of palaeoenvironmental and sea-level change.

305 unpublished PhD thesis, School of Geography, Geology and the Environment, Kingston

306 University London, Kingston upon Thames, UK, 582 p.

Olde et al. / Cretaceous Research ** (2016) ** - ** ACCEPTED MANUSCRIPT 307 Lignum, J., Jarvis, I., Pearce, M.A., 2008. A critical assessment of standard processing

308 methods for the preparation of palynological samples. Review of Palaeobotany and

309 Palynology 149, 133–149.

310 Ogg, J.G., Hinnov, L.A., Huang, C., 2012. Cretaceous, in: Gradstein, F.M., Ogg, J.G.,

311 Schmitz, M.D., Ogg, G.M. (Eds.), The Geological Time Scale 2012. Elsevier, Amsterdam,

312 pp. 793–853.

313 Olde, K., Jarvis, I., Pearce, M.A., Uli čný, D., Tocher, B.A., Trabucho-Alexandre, J., Gröcke,

314 D., 2015a. A revised northern European Turonian (Upper Cretaceous) dinoflagellate cyst

315 biostratigraphy: integrating palynology and carbon isotope events. Review of Palaeobotany

316 and Palynology 213, 1–16.

317 Olde, K., Jarvis, I., Uli čný, D., Pearce, M.A., Trabucho-Alexandre, J., Čech, S., Gröcke, D.R.,

318 Laurin, J., Švábenická, L., Tocher, B.A., 2015b. Geochemical and palynological sea-level 319 proxies in hemipelagic sediments: a critical assess MANUSCRIPTment from the Upper Cretaceous of the 320 Czech Republic. Palaeogeography, Palaeoclimatology, Palaeoecology 435, 222-243.

321 Pearce, M.A., 2000. Palynology and Chemostratigraphy of the Cenomanian to Lower

322 Campanian Chalk of Southern and Eastern England. Unpublished PhD thesis, School of

323 Earth Sciences and Geography, Kingston University London, Kingston upon Thames, UK,

324 432 p.

325 Pearce, M.A., Jarvis, I., Swan, A.R.H., Murphy, A.M., Tocher, B.A., Edmunds, W.M., 2003. 326 Integrating palynologicalACCEPTED and geochemical data in a new approach to palaeoecological 327 studies: Upper Cretaceous of the Banterwick Barn Chalk borehole, Berkshire, UK. Marine

328 Micropaleontology 47, 271–306.

329 Pearce, M.A., Jarvis, I., Tocher, B.A., 2009. The Cenomanian-Turonian boundary event,

330 OAE2 and palaeoenvironmental change in epicontinental seas: new insights from the

Olde et al. / Cretaceous Research ** (2016) ** - ** ACCEPTED MANUSCRIPT 331 dinocyst and geochemical records. Palaeogeography, Palaeoclimatology, Palaeoecology

332 280, 207-234.

333 Pearce, M.A., Lignum, J.S., Jarvis, I., 2011. Senoniasphaera turonica (Prössl, 1990 ex Prössl,

334 1992) comb. nov., senior synonym of Senoniasphaera rotundata alveolata Pearce et al.,

335 2003: an important dinocyst marker for the Lower Turonian chalk of NW Europe. Journal

336 of Micropalaeontology 30, 91–93.

337 Prössl, K.F., 1990. Dinoflagellaten der Kreide - Unter-Hauterive bis Ober-Turon - im

338 Niedersächsischen Becken. Stratigraphie und fazies in der Kernbohrung Konrad 101 sowie

339 einiger anderer bohrungen in Nordwestdeutschland. Palaeontographica. Abteilung B 218,

340 93-191.

341 Uli čný, D., Jarvis, I., Gröcke, D.R., Čech, S., Laurin, J., Olde, K., Trabucho-Alexandre, J.,

342 Švábenická, L., Pedentchouk, N., 2014 A high-resolution carbon-isotope record of the 343 Turonian stage correlated to a siliciclastic basin MANUSCRIPT fill: Implications for mid-Cretaceous sea- 344 level change. Palaeogeography, Palaeoclimatology, Palaeoecology 405: 42-58. doi:

345 10.1016/j.palaeo.2014.03.033.

346 Voigt, S., Hilbrecht, H., 1997. Late Cretaceous carbon isotope stratigraphy in Europe:

347 correlation and relations with sea level and sediment stability. Palaeogeography,

348 Palaeoclimatology, Palaeoecology 134, 39–59.

349 Voigt, S., Wagreich, M., Surlyk, F., Walaszczyk, I., Uli čný, D., Čech, S., Voigt, T., Wiese, F., 350 Wilmsen, M.,ACCEPTED Niebuhr, B., Reich, M., Funk, H., Michalík, J., Jagt, J.W.M., Felder, P.J., 351 Schulp, A.S., 2008. Cretaceous, in: McCann, T. (Ed.), The Geology of Central Europe

352 Volume 2: Mesozoic and Cenozoic. The Geological Society of London, London, pp. 921–

353 997.

Olde et al. / Cretaceous Research ** (2016) ** - ** ACCEPTED MANUSCRIPT 354 Walaszczyk, I., Peryt, D., 1998. Inoceramid - foraminiferal biostratigraphy of the Turonian

355 through Santonian deposits of the Middle Vistula Section, Central Poland. Zentralblatt für

356 Geologie und Paläontologie I, 11/12, 1501–1513.

357 Walaszczyk, I., Wood, C.J., 1998. Inoceramids and biostratigraphy at the Turonian/Coniacian

358 boundary; based on the Salzgitter-Salder Quarry, Lower Saxony, Germany, and the Słupia

359 Nadbrze żna section, central Poland. Acta Geologica Polonica 48, 395–434.

360 Walaszczyk, I., Wood, C.J., Lees, J.A., Peryt, D., Voigt, S., Wiese, F., 2010. The Salzgitter-

361 Salder Quarry (Lower Saxony, Germany) and Słupia Nadbrze żna river cliff section

362 (central Poland): a proposed candidate composite Global Boundary Stratotype Section and

363 Point for the Coniacian Stage (Upper Cretaceous). Acta Geologica Polonica 60, 445–477.

364 Wendler, I., 2013. A critical evaluation of carbon isotope stratigraphy and biostratigraphic

365 implications for Late Cretaceous global correlation. Earth-Science Reviews 126, 116–146. 366 Wiese, F., 1999. Stable isotope data ( δ13 C, δ18 O) fromMANUSCRIPT the Middle and Upper Turonian (Upper 367 Cretaceous) of Liencres (Cantabria, northern Spain) with a comparison to northern

368 Germany (Söhlde & Salzgitter-Salder). Newsletters on Stratigraphy 37, 37–62.

369 Williams, G.L., 1977. Dinocysts: their palaeontology, biostratigraphy and palaeoecology, in:

370 Ramsey, A.T.S. (Ed.), Oceanic Micropalaeontology. Academic Press, London, pp. 1231–

371 1325.

372 Williams, G.L., Bujak, J.P., 1985. Mesozoic and Cenozoic dinoflagellates, in: Bolli, H.M., 373 Saunders, J.B.,ACCEPTED Perch-Nielsen, K. (Eds.), Plankton Stratigraphy. Cambridge Earth Science 374 Series, Cambridge, pp. 847–964.

375 Williams, G.L., Stover, L.E., Kidson, E.J., 1993. Morphology and stratigraphic ranges of

376 selected Mesozoic-Cenozoic dinoflagellate taxa in the Northern Hemisphere. Geological

377 Survey of Canada Paper 92-10, 139 p.

Olde et al. / Cretaceous Research ** (2016) ** - ** ACCEPTED MANUSCRIPT 378 Wilpshaar, M., Leereveld, H., 1994. Palaeoenvironmental change in the Early Cretaceous

379 Vocontian Basin (SE France) reflected by dinoflagellate cysts. Reviews on Palaeobotany

380 and Palynology 84, 121–128.

381 Wood, C.J., Walaszczyk, I., Mortimore, R.N., Woods, M.A., 2004. New observations on the

382 inoceramid biostratigraphy of the higher part of the Upper Turonian and the Turonian -

383 Coniacian boundary transition in Poland, Germany and the UK. Acta Geologica Polonica

384 54, 541–549.

385 Zonneveld, K.A.F., Versteegh, G.J.M., deLange, G.J., 1997. Preservation of organic-walled

386 dinoflagellate cysts in different oxygen regimes: A 10,000 year natural experiment. Marine

387 Micropaleontology 29, 393–405.

388 Zonneveld, K.A.F., Versteegh, G., Kodrans-Nsiah, M., 2008. Preservation and organic

389 chemistry of Late Cenozoic organic-walled dinoflagellate cysts: A review. Marine 390 Micropaleontology 68, 179–197. MANUSCRIPT 391

ACCEPTED

Olde et al. / Cretaceous Research ** (2016) ** - ** ACCEPTED MANUSCRIPT 392 Figure Captions

393 Fig. 1. Location of the Słupia Nadbrze żna and Salzgitter-Salder candidate GSSP sections and

394 Turonian palaeogeography of central Europe. Map compiled from Voigt et al. (2008).

395 Fig. 2. Stratigraphy, key inoceramid bivalve ranges, macrofossil events, unsmoothed carbon

396 stable-isotope profiles, and correlation of the Turonian – Coniacian boundary interval

397 between the Salzgitter-Salder (Germany) and Słupia Nadbrze żna (Poland) sections. Cww =

398 Cremoceramus walterdorfensis walterdorfensis . LO = lowest occurrence. Compiled from

399 Walaszczyk et al. (2010).

400 Fig. 3. Carbon and oxygen stable-isotope profiles, foraminifera planktonic / benthic (P/B)

401 ratio, and organic walled dinoflagellate cyst abundance, species richness and diversity

402 through the Turonian – Coniacian boundary interval at Słupia Nadbrze żna. Cream band

403 indicates extent of the Navigation Carbon Isotope Event (CIE) of Jarvis et al. (2006); blue 404 bands are inoceramid bivalve events. The recorded MANUSCRIPT position of the ammonite Forresteria 405 (Harleites) petrocoriensis is indicated (arrow). Numbered circles indicate positions of stable-

406 isotope samples; filled circles are samples that were additionally processed for palynology.

407 Coloured dots and thin joining lines show data values; thicker coloured lines are three-point

408 moving averages (except for lower resolution foraminifera data). LO = lowest occurrence.

409 Lithology and biostratigraphy after Walaszczyk and Wood (1998), Kennedy and Walaszczyk

410 (2004) and Walaszczyk et al. (2010).

411 Fig. 4. Range ACCEPTED chart of dinoflagellate cyst species identified in the Słupia Nadbrze żna 412 Turonian – Coniacian boundary section. Dinoflagellate cyst relative abundances are given as

413 a percentage of specimens of each species in a sample. Note the different abundance scales

414 used for the four dominant taxa (blue shaded profiles; left) and other species (right).

415 Potentially significant dinoflagellate cyst biostratigraphic datum levels are indicated. Cream

Olde et al. / Cretaceous Research ** (2016) ** - ** ACCEPTED MANUSCRIPT 416 band indicates extend of the Navigation CIE; blue bands are inoceramid bivalve events. LO =

417 lowest occurrence; HO = highest occurrence. Lithology and inoceramid biostratigraphy after

418 Walaszczyk et al. (2010). Selected species are illustrated in Fig. 5.

419 Fig. 5. Selected dinoflagellate cyst species identified from the Turonian – Coniacian boundary

420 interval at Słupia Nadbrze żna. 1, Tanyosphaeridium sp., sample 2, 0.25 m. 2, Senoniasphaera

421 turonica , sample 16, 3.75 m. 3, Florentinia mantellii sample 1, 0 m. 4, Oligosphaeridium

422 complex , sample 4, 0.75 m. 5, Surculosphaeridium longifurcatum , sample 14, 3.25 m. 6,

423 Spiniferites ramosus subsp. ramosus , sample 17, 4.0 m. 7, Circulodinium distinctum subsp.

424 distinctum , sample 16, 3.75 m. 8, Cassiculosphaeridia reticulata, sample 4, 0.75 m. 9,

425 Oligosphaeridium poculum, sample 20, 4.75 m. 10, Pervosphaeridium sp., sample 12, 2.75 m.

426 11, Odontochitina operculata , sample 1, 0 m. 20 m scale-bar is used for all photos.

MANUSCRIPT

ACCEPTED

ACCEPTED MANUSCRIPT

Gdańsk Boreal N Sea Mid-Polish Warsaw Salzgitter -Salder Berlin Trough

Sudetic Islands Słupia Nadbrzeżna

Kraków Rhenish Prague Massif MANUSCRIPT Bohemian Massif

Munich Penninic Ocean100 km

emergent highs shallow deep basin epicontinental sea basin subject to Late major fault candidate Cretaceous inversion GSSPs

Olde et al. Fig. 1

ACCEPTED ACCEPTED MANUSCRIPT

Stage Zone Height (m)LithologyBed

Cci 85 oods) Isomicraster oods) 75 ( W 73 Inoceramid bivalve ranges b 71 a and macrofossil events

70 (Heinz) 80 (Heinz) 69 Micraster 67 cortestudinarium

65 a 75 13 63 δ C . hannovrensis (Andert) (Andert) (Andert) Cremnoceramus crassus inconstans 61 Cremnoceramus crassus inconstans ( W C. w 60 59

58 (Meek) (Meek) (Meek) 70 57 (Meek) lower Coniacian 55 Słupia b 53 Nadbrzeżna a erectus III dc b hannovrensis Cremnoceramus walterdorfensis hannovrensis a 52 51 65 c Lithology Height (m)Zone Stage b 50 a 7 b 49 erectus I 6 a erectus II C. d. erectus Andert 48 5 Coniacian 47 MANUSCRIPT C. d. erectus erectus I Cremnoceramus deformis erectus Cremnoceramus deformis erectus Cremnoceramus deformis erectus 60 Cremnoceramus deformis erectus LO C.d. erectus 46 waltersdorfensis II b 4 Cww 45 Didymotis II Cww Cremnoceramus walterdorfensis waltersdorfensis a waltersdorfensis I Navigation waltersdorfensis I Cremnoceramus walterdorfensis waltersdorfensis (Andert) 44 3 spp. 43 herbichi CIE spp. c 2 b 42 a herbichi uronian 1 T Inoceramus lusatiae Andert 55 Inoceramus lusatiae 41 M. scupini Mytiloides Mytiloides 0 Height (m) 40

39 Didymotis I 0.8 1.0 1.2 1.4 1.6 1.8 uronian Andert Andert 13 T b 38 δ Ccarb (‰VPDB) a M. scupini 50 37 upper opoka 36 spp. limestone (siliceous marl)

35 marl opoka Height (m) with rare cherts clay Inoceramus lusatiae Inoceramus lusatiae

34 Mytiloides 45 cherty opoka

1.8 2.0 2.2 2.4 2.6 13 Salzgitter-Salder δ Ccarb (‰VPDB) macrofossil event carbon isotope event Olde et al. ACCEPTEDFig. 2 ACCEPTED MANUSCRIPT

-3.0 -2.5 -2.0 300 900 1500 0.8 1.0 1.2 1.4

Stage Zone SamplesHeight (m)Lithology 1.0 1.2 1.4 1.6 0 25 50 5 6 7 8 9 10

30 29 7 13 18 Dinocyst Dinocyst 28 δ C δ O abundance species 27 richness 26 Dinocyst 25 Foraminifera 6 erectus Event diversity 24 P/B ratio 23 22 21 5

Lower Coniacian 20 19 Cremnoceraums d.erectus LO C.d. erectus 18 LO C.d. erectus 17 4 16

Cww 15 14 waltersdorfensis 13 3 Event 12 11 MANUSCRIPTNavigation 10 9 2 CIE F. (H.) petrocoriensis CIE 8 (Coquand) 7 6

Upper Turonian 5 1 herbichi Event 4 Mytiloides scupini 3 2 1 0 opoka (siliceous marl) <10 10-30 pollen opoka 1.0 1.2 1.4 1.6 0 25 50 5 6 7 8 9 10 with rare cherts δ13C (‰VPDB) P/B ratio (%) Number of species cherty opoka -3.0 -2.5 -2.0 300 900 1500 0.8 1.0 1.2 1.4 δ18O (‰VPDB) Palynomorphs per gram Shannon index (H) Słupia Nadbrzeżna

Olde et al. Fig. 3 ACCEPTED ACCEPTED MANUSCRIPT spp. spp. . ramosus anyosphaeridium . cooksoniae . buspina . mantellii O. complex Florentinia spp. F H. recurvatum T X. ceratoides O. poculum E. phragmites H. bowerbankii S. turonica . C. reticulata 9. 14. 13. 15. 16. 17. F 18. 2. 3. S. r 4. S. longifurcatum 7. O. operculata 8. 10 12. Pervosphaeridium Stage Zone SamplesHeight (m)Lithology 1. C. d. distinctum 5. F 6. 11.

29 7

6 erectus Event 24 23 HO S. 21 5 turonica

lower Coniacian 20

Cremnoceramus d.erectus LOFO C.d. erectus 18 MANUSCRIPT 17 4 16

Cww waltersdorfensis Event Dinocyst 14 abundance maximum 13 3 12 11 10

uronian Acme C.d. 9 2

T distinctum 8

upper 5 1 herbichi Event 4 Mytiloides scupini

2 opoka (siliceous marl) 1 0 quantified opoka abundance with rare cherts 25 5 Słupia Nadbrzeżna Relative abundance (%) present cherty opoka

Olde et al. Fig. 4 ACCEPTED ACCEPTED MANUSCRIPT

2 3 4

MANUSCRIPT 5 6 7

20 μm 8 9 10 11

Olde et al. Fig. 5 ACCEPTED ACCEPTED MANUSCRIPT Organic-walled dinoflagellate cysts have been recovered from the Turonian – Coniacian candidate GSSP

All samples yielded abundant well-preserved specimens enabling quantitative analysis

Assemblages have low species richness and diversity, and are dominated by four taxa; they include few biostratigraphic marker species

Terrestrial palynomorphs are poorly represented

Deposition occurred in a relatively shallow water pelagic environment in the Eastern European epicontinental sea

MANUSCRIPT

ACCEPTED