Geological Survey of Denmark and Greenland Bulletin 6, 89-97 89Geological Survey of Denmark and Greenland Bulletin 5, 89–97 © GEUS, 2004 Jurassic dinoflagellate cysts from Hochstetter Forland, North-East Greenland Stefan Piasecki and Lars Stemmerik Three sections in Hochstetter Forland, North-East Greenland, referred to the Jurassic Payer Dal and Bernbjerg Formations, have been analysed for dinoflagellate cysts. The dinoflagellate cysts, new finds of ammonites and previously recorded marine faunas form the basis for improved dating of the succession. The basal strata of the Payer Dal Formation at Kulhus is here dated as Late Callovian, Peltoceras athleta Chronozone, based on the presence of relatively abundant Limbicysta bjaerkei, Mendicodinium groenlandicum, Rhychoniopsis cladophora and Tubotu- berella dangeardii in an otherwise poor Upper Callovian dinoflagellate assemblage. Ammonites have not been recorded from these strata. The upper Payer Dal Formation at Agnetesøelven is dated as Late Oxfordian, Amoeboceras glosense – Amoeboceras serratum Chronozones, based on the presence of Sciniodinium crystallinum, together with Cribroperidinium granuligera and Stephanelytron sp. The age is in accordance with ammonites present in the uppermost part of the formation at Søndre Muslingebjerg. New ammonites in the Bernbjerg Formation at Agnetesøelven together with dinoflagellate cysts indicate an earliest Kimmeridgian age, Rasenia cymodoce and Aulacostephanoides mutabilis Chronozones. The Upper Callovian dinoflagellate cysts from Hochstetter Forland belong to a local brackish to marginal marine assemblage, which only allows a fairly broad correlation to coeval assem- blages in central East Greenland. In contrast, the Oxfordian and Kimmeridgian assemblages are fully marine and can be correlated from Milne Land in central East Greenland via Hochstetter Forland to Peary Land in eastern North Greenland. Keywords: ammonites, Boreal, dinoflagellate cysts, Hochstetter Forland, Jurassic, North-East Greenland Geological Survey of Denmark and Greenland, Øster Voldgade 10, DK-1350 Copenhagen K, Denmark. E-mail: sp@geus.dk The northernmost onshore Jurassic outcrops in East Greenland occur in Hochstetter Forland and, some 60– 80 km farther north, on Store Koldeway (Fig. 1); the stratigraphy of the latter area is described in an ac- companying paper (Piasecki et al. 2004a, this volume). The Hochstetter Forland peninsula is dominated by flat lowlands dissected by small streams; outcrops of pre-Quaternary sediments are restricted to stream cuts and low coastal cliffs scattered throughout the region (Fig. 1). However, at Søndre Muslingebjerg to the south, Caledonian basement and Middle–Upper Jurassic sand- stones and coals are faulted and reach up to approxi- mately 400 m above sea level. Caledonian basement and Jurassic sediments also crop out in northern Hoch- stetter Forland, east of Agnetesø, and the meanders of Agnetesøelven (the river from Agnetesø to the coast) erode into marine Jurassic sediments deposited on basement rocks (Fig. 1). The Jurassic stratigraphy of the Hochstetter Forland area is based on records of marine faunas including ammonites from several isolated exposures (Ravn 1911; Surlyk 1978). The lowermost deposits consist of the non-marine to marginal marine Muslingebjerg Forma- tion, which is undated owing to the absence of marine fossils. The overlying sands of the Payer Dal Forma- tion contain Upper Oxfordian ammonites in the upper GEUS Bulletin no 5.pmd 29-10-2004, 11:1489 90 part, and are followed by mudstones of the Bernbjerg Formation that yield Upper Oxfordian – Lower Kim- meridgian ammonites (Surlyk 1978). The outcrops at Kulhus and Agnetesøelven expose the main part of the Jurassic succession in Hochstetter Forland. These localities were visited during fieldwork in 1987 in or- der to collect material for palynological analysis with the aim of refining the stratigraphy. The present paper describes for the first time the dinoflagellate cyst floras from these northern outcrops close to the transition to the Boreal dinoflagellate cyst province, for example in Peary Land (Håkansson et al. 1981) and on Svalbard (Århus 1988). Material At Kulhus (Fig. 1; Locality 1), on the south coast of Hochstetter Forland west of Søndre Muslingebjerg, sand and coal seams were sampled during a ground stop on helicopter reconnaissance in 1987. Only one sam- ple (GGU 351570) contains dinoflagellate cysts. Two closely situated localities at Agnetesøelven were spot- ted from the air and visited during a short ground stop. The westernmost sandstone outcrop (Locality 2) was measured and two fine-grained samples with at least some potential for palynology were collected from two horizons (Fig. 2). Eastwards and down-river, the sand- stone-dominated succession was seen to be faulted against a succession of laminated mudstones (Locality 3), and this was closely sampled for palynology (Fig. 3). Only a few, well-preserved dinoflagellate cysts were recovered from the sand succession at Locality 2. By 20ºW 20 km 76º30'N Undifferentiated, mostly glacial deposits Cretaceous Locality Fault Caledonian crystalline basement Søndre Muslingebjerg Kulhus Nanok N HOCHSTETTER FORLAND 1: Milne Land 2: Jameson Land 3: Wollaston Forland 4: Hochstetter Forland 5: Store Koldewey 6: Germania Land Jurassic 7: Peary Land Greenland 500 km Agnetesø 2 3 7 1 2 3 4 56 1 1 Agnetesøelven Fig. 1. Simplified sketch map of Hoch- stetter Forland illustrating the Jurassic outcrops and the sampled localities. The map is modified from Surlyk (1978, fig. 1). GEUS Bulletin no 5.pmd 29-10-2004, 11:1490 91 contrast dinoflagellate cysts are abundant but poorly preserved in the mudstones at Locality 3. Ammonites are abundant in the lower, pyritic, part of the mudstone succession and in loose concretionary beds at the base of the cliff. These ammonites provide independent strati- graphical control of the dinoflagellate cyst assemblages. All of the samples from the three localities on Hoch- stetter Forland were prepared by traditional palyno- logical methods and analysed for their content of dinoflagellate cysts. Geology The Jurassic succession on Hochstetter Forland is di- vided into the Muslingebjerg, Payer Dal and Bernbjerg Formations of the Vardekløft Group. The marine sand- stones of the Payer Dal Formation were previously included in the Pelion Member of the Vardekløft For- mation (sensu Surlyk 1978); the Pelion Member is now raised to formation status (Surlyk 2003, fig. 5). Kulhus (Locality 1) The low coastal cliff at Kulhus, south-west Hochstetter Forland (Fig. 1, Locality 1), comprises 3–4 main coal Belemnite Bivalve Oyster Pecten spp. Planolites ispp. Wood Bioturbation Fine-grained sand Planar lamination/bedding GGU sample Fossils, etc. Planar cross-lamination Lenticular lamination Trough cross-bedding Scour and fill Shell bed Structures Lithology Hard bed Mud Sand 0 5 15 25 30 35 10 20 m 351538 351537 351537 Mud Pyrite Ammonite Fig. 2. Sedimentological log of the upper Payer Dal Formation at Agnetesøelven (Locality 2) showing the positions of analysed samples. GEUS Bulletin no 5.pmd 29-10-2004, 11:1491 92 seams interbedded with black carbonaceous shales and light-coloured sandstones of the Muslingebjerg Forma- tion (Clemmensen & Surlyk 1976). No marine fossils have been recorded from the formation but the high sulphur content of the coals and shales suggests a marine depositional environment (Petersen et al. 1998). The Jurassic succession at Kulhus extends up the west- ern flank of Søndre Muslingebjerg where the strati- graphically highest strata contain Upper Oxfordian ammonites referable to the Amoeboceras glosense and/ or A. serratum Zones (Ravn 1911; Sykes & Surlyk 1976). Coals and shales of the Muslingebjerg Formation have been prepared palynologically without finding any microscopic marine fossils. At Kulhus, the first dinofla- gellate cysts appear in the basal mudstone bed of the overlying Payer Dal Formation, immediately above the highest coal seam, at the same level as the earliest ma- rine faunas. Restricted assemblages of sporomorphs from the underlying coals indicate an overall Jurassic age. Agnetesøelven (Localities 2 and 3) Fine-grained sandstone, with abundant marine fossils, is exposed at Locality 2 and referred to the Payer Dal Formation (Figs 1, 2). Shell beds of Pecten spp., oys- ters, other bivalves and serpulids occur throughout the succession and are commonly concentrated in scour fills. Belemnites are present, but no ammonites were recovered during the short visit. Woody material and small logs are also common. The sandstone is intensely bioturbated and many sedimentary structures are ob- literated although cross-bedding or lamination is rec- ognisable in most beds. Planolites ispp. is common at certain horizons. The shale succession exposed at Locality 3 is re- ferred to the Bernbjerg Formation. It consists of lami- nated, dark mudstones alternating with lenticular-bed- ded, fine-grained, grey sandstones (Fig. 3). Ammonites and bivalves are abundant in a concretionary bed low in the section and belemnites and bivalves occur scat- tered higher in the succession. The concretionary beds are washed out from the lowermost succession and lie at the foot of the cliff. They contain accretions of am- monites in several stacked laminae together with abun- dant Buchia sp. Abundant male and female individu- als occur together in the ammonite assemblages (J.H. 351546 351547 351548 351545 351544 351543 351542 351541 351540 351539 Mud Sand 0 5 10 15 20 25 m Fig. 3. Sedimentological log of the Bernbjerg Formation at Agnetesøelven (Locality 3) showing the positions of analysed samples. For legend, see Fig. 2. GEUS Bulletin no 5.pmd 29-10-2004, 11:1492 93 Callomon, personal communication 1999). The assem- blage is equivalent to ammonite Fauna 15 from Milne Land in the lower Rasenia cymodoce Zone, Lower Kim- meridgian (Fig. 4; Birkelund & Callomon 1985; J.H. Callomon, personal communication 1999). Lower Kim- meridgian ammonites have been reported previously from sandstones at the locality of Nanok in southern Hochstetter Forland (Frebold 1932). Ammonites of the lowermost Kimmeridgian Rasenia cymodoce and Aula- costephanoides mutabilis Zones, have been collected from mudstones of the Bernbjerg Formation in Hochstetter Forland (Frebold 1932; Surlyk 1978). Stratigraphy Basal Payer Dal Formation (Locality 1) Dinoflagellate cysts. An unusual and relatively poor assemblage of dinoflagellate cysts was recorded im- mediately above the lithological transition from the barren Muslingeelv Formation to the fossiliferous Payer Dal Formation (Fig. 5). Limbicysta bjaerkei, Pilosidin- ium fensomei and Pareodinia halosa dominate the assemblage, in association with Gonyaulacysta juras- sica, Nannoceratopsis sp., Occisucysta sp., Pareodinia sp., Solisphaeridium sp., Tubotuberella cf. dangeardii and Tubotuberella cf. egemenii. Single specimens of Atopodinium haromense, Mendicodinium groenlandi- cum and Rhynchodiniopsis cladophora were recorded. Age. Stratigraphically diagnostic species are few in this assemblage. In East Greenland, Limbicysta bjaerkei has not been recorded stratigraphically higher than the basal Boreal Middle Jurassic in the Cranocephalites borealis Chronozone in Jameson Land (Milner & Pia- secki 1996). However, a stratigraphical range of Mid- dle Callovian and possibly into lowermost Upper Callovian has been reported from both the Subboreal and Arctic regions (Smelror 1987, 1993). In Jameson Land, M. groenlandicum appears no lower than the Kosmoceras jason Chronozone (mid-Callovian) and distinct Rhynchodiniopsis cladophora and Tubotuberel- la dangeardii appear in the basal Upper Callovian in the Peltoceras athleta Chronozone (Milner & Piasecki 1996). In conclusion, the sparse data indicate an age equivalent to the earliest Late Callovian, P. athleta Chro- nozone (Fig. 4). An Early Callovian age previously in- dicated for this unit (Petersen et al. 1998) was based on a sample that was subsequently found to be from another section and locality. Depositional environment. The dinoflagellate cyst as- semblage is dominated by three species (Fig. 5). Limbicysta bjaerkei is possibly an acritarch because no clear archaeopyle has been documented. The as- semblage differs markedly from normal marine assem- blages described from time equivalent strata in Milne Land (Piasecki 1996). Bailey & Hogg (1995) reported abundant L. bjaerkei in otherwise non-marine assem- blages. This may indicate that the associated, frequent species, Pilosidinium fensomei and Pareodinia halosa, may have had similar environmental preferences. The abundance of L. bjaerkei – together with the restricted LITHOSTRATIGRAPHY BIOSTRATIGRAPHY FORMATION AMMONITE ZONE AGE BASED ON DINOFLAGELLATE CYSTS CHRONOZONES Bernbjerg A. mutabilis R. cymodoce A. mutabilis R. cymodoce Early Kimmeridgian Payer Dal A. glosense – A. serratum A. glosense – A. serratumLate Oxfordian Late Callovian P. athleta Muslingebjerg No marine fossils (Callovian?) pre-P. athleta CHRONOSTRATIGRAPHY Fig. 4. Summary of the Jurassic stratigraphy of Hochstetter Forland. GEUS Bulletin no 5.pmd 29-10-2004, 11:1493 94 assemblage – is taken as evidence for estuarine, brack- ish depositional environments during the initial trans- gression of Hochstetter Forland. Upper Payer Dal Formation (Locality 2) Dinoflagellate cysts. Dinoflagellate cysts are relatively sparse in these sediments. However, the diversity is mo- derately good and the preservation is fine. Ambono- sphaera calloviense is the only dinoflagellate species represented by more than one or two specimens in the assemblage (Fig. 5). Ambonosphaera calloviense, Sirmi- odinium grossii and Sentusidinium sp. are the only species common to both samples. Age. Despite the paucity of dinoflagellate cysts, the co-occurrence of Sciniodinium crystallinum, Cribro- peridinium granuligera and Stephanelytron sp. indi- cates a Late Oxfordian age i.e. Amoeboceras glosense to Amoeboceras serratum Chronozones, by compari- son to Hold with Hope and Milne Land further to the south (Piasecki 1996; Piasecki et al. 2004a, b, this vol- ume; Figs 1, 4). None of the other dinoflagellate cysts are inconsistent with this age, which is also in accord- ance with the age indicated by ammonites from the uppermost Payer Dal Formation at Søndre Muslinge- bjerg (Ravn 1911; Sykes & Surlyk 1976). However, the dinoflagellate cyst assemblage is too restricted to al- low a more precise correlation. Depositional environment. The low abundance com- bined with the moderate diversity of dinoflagellate cysts indicates near-shore marine deposition in a high-en- ergy environment. The sandy sediments with a rich benthic fauna, partly in situ and partly reworked into shell beds, support this interpretation. Bernbjerg Formation (Locality 3) Dinoflagellate cysts. Dinoflagellate cysts are abundant and relatively diverse, but their preservation is poor. The composition of the assemblages varies significantly through the relatively short section (Fig. 5). Extremely abundant Sirmiodinium grossii characterises the lower part of the section and is gradually replaced by abun- dant Gonyaulacysta jurassica sensu lato in the upper part. Five other species appear in succession with dis- tinct and characteristic maxima through the succes- sion (Fig. 5). Abundant Nummus sp. occurs together with the maximum numbers of Escharisphaeridium pocockii in the lower part of the succession. This is followed closely by a maximum abundance of Cribro- peridinium granuligera, then by a maximum of Peris- seiasphaeridium pannosum (together with Gonyaula- cysta jurassica sensu lato) and finally by maximum abundance of Occisucysta cf. monoheuriskos in the uppermost sample. A comparable succession of dinoflagellate cyst as- semblages has been recorded across the boundary of the Payer Dal and Bernbjerg Formations at Kløft II on Store Koldewey (Piasecki et al. 2004a, this volume). At this locality, a maximum of G. jurassica sensu lato is followed by abundant P. pannosum and Occisucysta cf. monoheuriskos, similar to that recorded from the upper part of the section at Agnetesøelven (Locality 3). Assemblages dominated by Nummus sp., E. pocockii and C. granuligera were not recorded at Store Kolde- wey, but these species are present. In contrast, the stratigraphically significant Paragonyaulacysta capillosa is abundant at Store Koldewey, whereas it is rare in the succession at Agnetesøelven. Age. The succession cannot be older than Early Kim- meridgian based on the ammonite fauna in the basal strata, which is indicative of the lower Rasenia cymodoce Zone. This is in accordance with the dinoflagellate cyst assemblage of abundant Sirmiodinium grossii and fre- quent Gonyaulacysta jurassica, Adnatosphaeridium sp. and Paragonyaulacysta capillosa. To the south, on Milne Land, P. capillosa first appears in the R. cymodoce Chronozone and is followed by Perisseiasphaeridium pannosum in the succeeding Aulacostephanoides mutabilis Chronozone (Piasecki 1996). At Agnetesøel- ven, the appearance of P. pannosum higher in the suc- cession accordingly indicates an age equivalent to the A. mutabilis Chronozone for this part of the succes- sion (Fig. 4). Dinoflagellate cysts indicative of younger Jurassic strata were not recorded. Lower Kimmeridgian ammonites have previously been recorded from the Bernbjerg Formation on Hoch- stetter Forland. An ammonite fauna referable to the A. mutabilis Zone has been recovered from the Nanok and Agnetesøelven regions (Frebold 1932; Surlyk 1978). Depositional environment. The dinoflagellate cysts are strongly degraded. They are physically broken, and angular imprints of crystals and deep circular imprints of spherical pyrite framboids obscure the sculpture and structure of their walls. Together with the undisturbed lamination of the sediments, this indicates deposition GEUS Bulletin no 5.pmd 29-10-2004, 11:1494 95 50250 66.00 61.00 56.00 53.00 50.00 47.00 45.00 40.00 25.00 20.00 1.00 351548 351547 351545 351544 351543 351542 351541 351539 351538 351537 351570 Jurassic Oxfordian–KimmeridgianCallovian BernbjergPayer Dal 1 Veryhachium spp. 2 Tubotuberella dangeardii 3 Atopodinium haromense 4 Sentusidinium rioultii 5 Mendicodinium groenlandicum 6 Dissiliodinium spp. 7 Botryococcus spp. 8 Limbicysta bjaerkei 9 Pilosidinium fensomei 10 Solisphaeridium spp. 11 Tubotuberella cf. egemenii 12 Occisucysta spp. 13 Nannoceratopsis spp. 14 Pareodinia cf. stegasta 15 Valensiella spp. 16 Rhynchodiniopsis cladophora 17 Pareodinia spp. 18 Gonyaulacysta jurassica 19 Pareodinia halosa 20 Stephanelytron spp. 21 Tenua spp. 22 Ambonosphaera calloviense 23 Sentusidinium spp. 24 Sirmiodinium grossii 25 Scriniodinium crystallinium 26 Cribroperidinium granuligera 27 Pareodinia cf. pachyceras 28 Scriniodinium spp. 29 Tubotuberella apatela 30 Avellodinium cf. falsificum 31 Rhynchodiniopsis cf. cladophora 32 Scriniodinium cf. crystallinium 33 Leptodinium spp. 34 Leptodinium subtile 35 Cribroperidinium sp. 36 Paragonyaulacysta cf. capillosa 37 Escharisphaeridia pocockii 38 Nummus spp. 39 Atopodinium spp. 40 Occisucysta cf. monoheuriskos 41 Adnatosphaeridium spp. 42 Pareodinia stegasta 43 Epiplosphaera spp. 44 Sentusidinium pelionense 45 Barbatacysta spp. 46 Perisseiasphaeridium pannosum 47 Paragonyaulacysta capillosa 48 Paragonyaulacysta spp. 49 Prolixosphaeridium granulosum 50 Tubotuberella rhombiformis A LPH A B ET IC A L SPEC IES LIST 41 A dnatosphaeridium spp. 22 A m bonosphaera calloviense 3 A topodinium harom ense 39 A topodinium spp. 30 Avellodinium cf. falsificum 45 Barbatacysta spp. 7 Botryococcus spp. 19 Pareodinia halosa 26 C ribroperidinium granuligera 35 C ribroperidinium sp. 6 D issiliodinium spp. 43 Epiplosphaera spp. 37 Escharisphaeridia pocockii 18 G onyaulacysta jurassica 33 Leptodinium spp. 34 Leptodinium subtile 5 M endicodinium groenlandicum 13 N annoceratopsis spp. 38 N um m us spp. 12 O ccisucysta spp. 40 O ccisucysta cf. m onoheuriskos 48 Paragonyaulacysta spp. 47 Paragonyaulacysta capillosa 36 Paragonyaulacysta cf. capillosa 27 Pareodinia cf. pachyceras 14 Pareodinia cf. stegasta 17 Pareodinia spp. 42 Pareodinia stegasta 8 Lim bicysta bjaerkei 46 Perisseiasphaeridium pannosum 9 Pilosidinium fensom ei 49 Prolixosphaeridium granulosum 31 R hynchodiniopsis cf. cladophora 16 R hynchodiniopsis cladophora 32 Scriniodinium cf. crystallinium 25 Scriniodinium crystallinium 28 Scriniodinium spp. 44 Sentusidinium pelionense 4 Sentusidinium rioultii 23 Sentusidinium spp. 24 Sirm iodinium grossii 10 Solisphaeridium spp. 20 Stephanelytron spp. 21 Tenua spp. 29 Tubotuberella apatela 11 Tubotuberella cf. egem enii 2 Tubotuberella dangeardii 50 Tubotuberella rhom biform is 15 Valensiella spp. 1 Veryhachium spp. Sample height Metre GGU sample no. System Stage Formation H o chstetter Fo rland K ulhus and A gnetesø elven > 50 specim ens 20 – 50 specim ens 5–19 specim ens 1– 4 specim ens Fig. 5. Stratigraphical distribution chart of dinoflagellate cysts in samples from all three localities. The sample heights indicated are largely arbitrary, although the three localities are arranged in stratigraphic order. Sample at 1 m is from Locality 1, samples at 20 m and 25 m are from Locality 2 (arbitrary spacing, see Fig. 2 for correct locations) and samples at 40–66 m are from Locality 3 (spacings approximately to scale, see Fig. 3 for precise locations). The recorded species are arranged by their first stratigraphical appearance. GEUS Bulletin no 5.pmd 29-10-2004, 11:1495 96 below wave base in a low-oxygenated environment. Lenticular laminae with small-scale ripples, however, show that the bottom water was not completely stag- nant and that the sea floor was periodically swept by weak bottom currents. Correlation Studies of the Jurassic ammonite and dinoflagellate cyst stratigraphy in East Greenland, combined with sedi- mentological studies and sequence stratigraphical in- terpretations, contribute towards an integrated model in which units can be identified by their content of dinoflagellate cysts. The present study of the dinoflag- ellate cyst assemblages on Hochstetter Forland con- tributes basic data to this complex study. The assemblage dominated by Limbicysta bjaerkei in the basal Payer Dal Formation at Kulhus has not been recorded anywhere else in East Greenland. This assemblage comprises the first marine fossils to have been deposited above the coal-bearing floodplain en- vironment of the Muslingebjerg Formation. The dino- flagellate cyst assemblage records deposition in a mar- ginal marine to brackish environment. The overlying sandstones are interpreted as tidal facies followed by shoreface facies (Petersen et al. 1998), reflecting a rise in relative sea level. This assemblage thus character- ises marginal marine environments at the feather-edge of the Jurassic depositional basin during a major drown- ing event (Alsgaard et al. 2003). The poor dinoflagellate cyst assemblage in the up- per Payer Dal Formation is not representative of this stratigraphic interval, compared to the assemblages recorded from other localities in East Greenland. How- ever, it is associated with a stratigraphic unit equiva- lent to the A. glosense and A. serratum Chronozones that previously has been identified throughout East Greenland, i.e. in Milne Land, Jameson Land and Hold with Hope (Engkilde 1994; Piasecki 1996; Vosgerau et al. 2004, this volume). The dinoflagellate cyst assemblage from the Bernbjerg Formation at Agnetesøelven is known from Milne Land in the south to Store Koldewey in the north, and a similar assemblage occurs in the Ladegårdsåen Formation in Peary Land, North Greenland (Fig. 1; Piasecki 1966; Piasecki et al. 2004a, this volume). The dinoflagellate cyst assemblage correlates with the R. cymodoce and A. mutabilis Chronozones. It is associ- ated with a major Kimmeridgian flooding event which allowed more permanent shelf anoxia to spread to shallow shelf areas of East Greenland (Milne Land, Wollaston Forland, Hold with Hope, Store Koldewey) and North Greenland (Peary Land). Maximum flood- ing occurred in the A. mutabilis to A. eudoxus Chrons. Conclusions New ammonite data confirm and refine earlier age determinations of the Jurassic succession on Hochstet- ter Forland. The age of the upper Payer Dal Formation in Hochstetter Forland is confirmed as Late Oxfordian, and the age of the Bernbjerg Formation is confirmed as earliest Kimmeridgian. The dinoflagellate cyst stratigraphy from the three localities is fragmentary. The assemblage from the lower Payer Dal Formation at Kulhus has not been reported from any other section in East Greenland; it is impor- tant because it represents marginal marine conditions associated with a major flooding event of earliest Late Callovian age, P. athleta Chronozone (Fig. 4). This limits the age of the Muslingeelv Formation upwards. The assemblage in the upper Payer Dal Formation is re- stricted, but supports the previously recorded Late Oxfordian age, corresponding to the A. glosense and/ or A. serratum Chronozones. The third assemblage is well known from East Greenland and dates the Bern- bjerg Formation at Agnetesøelven to the earliest Kim- meridgian, R. cymodoce and A. mutabilis Chronozones (Fig. 4). This assemblage is associated with a major transgressive event characterised by extensive shelf anoxia in East Greenland. Acknowledgements The work was initiated as part of the project ‘Resources of the sedimentary basins of North and East Green- land’ supported by the Danish Research Councils and completed by support from the Carlsberg Foundation Ans. 980089/0-262. John H. Callomon is thanked for the identification of the ammonites. The referees, D.J. Batten and J.B. Riding, provided constructive and very helpful suggestions. GEUS Bulletin no 5.pmd 29-10-2004, 11:1496 97 References Alsgaard, P.C., Felt, V.L., Vosgerau, H. & Surlyk, F. 2003: The Jurassic of Kuhn Ø, North-East Greenland. In: Ineson, J.R. & Surlyk, F. (eds): The Jurassic of Denmark and Greenland. Geological Survey of Denmark and Greenland Bulletin 1, 865–892. Århus, N. 1988: Palynostratigraphy of some Bathonian–Haute- rivian sections in the Arctic, with emphasis on the Janusfjellet Formation type section, Spitsbergen. 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