Geological Survey of Denmark and Greenland Bulletin 6, 73-88 73Geological Survey of Denmark and Greenland Bulletin 5, 73–88 © GEUS, 2004 Jurassic dinoflagellate cyst stratigraphy of Hold with Hope, North-East Greenland Stefan Piasecki, Michael Larsen, Jens Therkelsen and Henrik Vosgerau Dinoflagellate cysts of the Middle–Upper Jurassic succession on northern Hold with Hope have been studied in order to establish a biostratigraphic framework and to date the succession. The Pelion Formation is characterised by abundant Chytroeisphaeridia hyalina and Sentusidinium spp., with some Ctenidodinium thulium and Paragonyaulacysta retiphragmata in the lower part. Mendicodinium groenlandicum appears higher in the formation followed by Trichodinium scarburghense in the upper part. The succeeding Payer Dal Formation contains Scriniodinium crystallinum, Rigaudella aemula and Leptodinium subtile in the lower part and Dingodinium jurassicum and Prolixosphaeridium granulosum in the uppermost part. The Bernbjerg Forma- tion contains abundant Sirmiodinium grossii and Gonyaulacysta jurassica. Adnatospahaeridium sp., Cribroperidinium granuligerum, Glossodinium cf. dimorphum and Scriniodinium irregulare appear in the lower part of the formation, followed by Avellodinium spp. in the highest part. The dinoflagellate cyst assemblages in the Pelion Formation indicate an Early–Late Callovian age (C. apertum – P. athleta Chronozones). This is supported by ammonites in the lower part of the formation, which refer to the C. apertum and P. koenigi Chronozones. A significant hiatus, from Late Callovian to Middle Oxfordian, is present between the Pelion Formation and the overlying Payer Dal Formation. The age of the Payer Dal Formation is Middle Oxfordian to earliest Late Oxfordian (C. tenuiserratum – A. glosense Chronozones). The Payer Dal Formation is conform- ably overlain by the Bernbjerg Formation of Late Oxfordian to possibly earliest Kimmeridgian age (A. glosense – P. baylei Chronozones). The A. glosense Chronozone is also documented by abundant ammonites in the lowermost part of the formation. Keywords: ammonites, dinoflagellate cysts, Jurassic, North-East Greenland, stratigraphy S.P., M.L., J.T.* & H.V.‡, Geological Survey of Denmark and Greenland, Øster Voldgade 10, DK-1350 Copenhagen K, Denmark. E-mail: sp@geus.dk Present addresses: *Skude & Jacobsen, Næstvedvej 1, DK-4760 Vordingborg, Denmark. ‡Roskilde Amt, Køgevej 80, DK-4000 Roskilde, Denmark. The recognition of Middle–Upper Jurassic sediments on northern Hold with Hope added a missing link to the chain of Jurassic sedimentary exposures along the east coast of Greenland (Figs 1, 2; Stemmerik et al. 1997; Kelly et al. 1998; Larsen et al. 1997; Vosgerau et al. 2004, this volume). Sedimentological and biostrati- graphical analysis of the succession formed the basis for correlation with lithostratigraphical units in Wolla- ston Forland and Jameson Land, and subdivision into the Pelion, Payer Dal and Bernbjerg Formations (Fig. 3). A new member of the Pelion Formation, the Spath Plateau Member, was erected (Vosgerau et al. 2004, this volume). Correlation was based on very few, poorly preserved Middle Jurassic ammonites in situ in the lower sandstone-dominated part of the succession, and more abundant Upper Jurassic ammonites of the Up- per Oxfordian, the A. glosense Zone, in the mudstone- dominated upper part of the succession. The content of dinoflagellate cysts was studied in order to improve the biostratigraphic dating of the succession, and to GEUS Bulletin no 5.pmd 29-10-2004, 11:1473 74 improve the knowledge of Jurassic dinoflagellate cysts in this region in general. The results reported here allow correlation with corresponding assemblages from Store Koldewey and Hochstetter Forland in the north and Jameson Land – Milne Land in the south (Fig. 1). Geological setting The Late Palaeozoic – Mesozoic extensional basin com- plex in East Greenland is approximately 700 km long in a north–south direction. Jurassic sediments are present and exposed from Jameson Land in the south to Store Koldewey in the north (Surlyk 1977). In the northern part of the rift system, e.g. the Wollaston For- land Basin, rifting was initiated in Middle Jurassic time, and marine Bajocian–Bathonian sandstones onlap Cal- edonian basement rocks or Permian carbonates (Vischer 1943; Surlyk 1978). Deposition took place on the hang- ingwall of W–SW-tilted fault blocks. Jurassic rifting culminated in the Volgian with strong rotational block faulting (Surlyk 1978). During this episode the wide original fault blocks, defining the Wollaston Forland Basin, were divided into smaller blocks (Vischer 1943; Surlyk 1978). A similar tectonic development may have occurred in the Geographical Society Ø and Traill Ø area towards the south (Donovan 1957; Price & Whit- ham 1997). The Cretaceous period was generally char- acterised by subsidence controlled by thermal contrac- tion (Surlyk et al. 1981; Price & Whitham 1997). The East Greenland rift basin complex was uplifted during the Cenozoic. Sediments of Jurassic age were first recognised on Hold with Hope by Stemmerik et al. (1997). They are limited to the north coast of Hold with Hope from Stensiö Plateau to Steensby Bjerg (Fig. 2), where they occur on the hangingwall of small fault blocks that dip mainly to the west and south-west. Bedding planes within the Triassic and Jurassic seem to be parallel, whereas the boundary with the overlying Cretaceous succession is an angular unconformity (Vosgerau et al. 2004, this volume). The thickness of the Jurassic suc- cession varies significantly depending on its position on the hangingwall and the depth of Cretaceous ero- sion. The Jurassic succession includes shallow marine sandstones of the Pelion and Payer Dal Formations (Vardekløft Group), and offshore transition – lower shoreface heteroliths and offshore mudstones of the Bernbjerg Formation, Hall Bredning Group (Fig. 3). The Spath Plateau Member of the Pelion Formation was erected to accommodate sandy heteroliths and Fig. 1. Locality map of East Greenland and eastern North Green- land. The white region illustrates the permanent inland ice cap of Greenland, the grey areas are ice-free. Hold with Hope is located between 73ºN and 74ºN. Scoresby Sund St. Koldewey Kuhn Ø Fig. 2 Wollaston Forland Hold with Hope Geographical Society Ø Traill Ø Milne Land Jameson Land Hochstetter Forland 200 km 20°W28°W36°W42°W 12°W 70°N 28°W 20°W 72°N 74°N 76°N 78°N 80°N 12°W 82°N GEUS Bulletin no 5.pmd 29-10-2004, 11:1474 75 offshore mudstones that contrast with the generally coarse-grained sandstone facies of the Pelion Forma- tion (Vosgerau et al. 2004, this volume). The succes- sion on Hold with Hope resembles the well-known Jurassic succession in the Wollaston Forland and Jameson Land Basins towards the north and south. The Middle Jurassic Pelion Formation is c. 190 m thick, the Upper Jurassic Payer Dal Formation is 50–80 m thick and the Bernbjerg Formation is estimated to be c. 130 m thick (Fig. 4; Vosgerau et al. 2004, this volume). Samples and methods The dinoflagellate cysts have been studied in three sections (Fig. 4), in combination with a number of geographically and stratigraphically scattered samples on northern Hold with Hope. The main area of expo- sure is located on the northern and western slopes of Steensby Bjerg towards Gael Hamke Bugt and along the Gulelv river (Fig. 2, Locality 1). Samples from a number of short, vertical sections are combined into a composite section representing the entire succession (Fig. 2, Locality 1, sections A–E). The Payer Dal For- mation was also sampled at the Sortelv river, south of Steensby Bjerg (Fig. 2, Locality 2). Samples from a third section through the Pelion Formation at Stensiö Pla- teau (Fig. 2, Locality 3) provide good supplementary material from the lowermost part of the succession, which is poorly represented in the section at Steensby Bjerg. Most of the analysed samples are from fine- grained thin beds or lamina in the otherwise coarse- grained, sandy Pelion and Payer Dal Formations. The number of samples and their stratigraphical distribu- Fig. 2. Geological map of the northern Hold with Hope which illustrates the distribution of the studied Jurassic succession. Localities 1, 2 and 3 are marked; the succession at Locality 1 has been compiled from a number of short laterally correlated sections (1A–1E). Ice Undifferentiated superficial deposits Dolerite sill Plateau basalt Normal fault Inferred fault Locality Paleocene Lower Cretaceous Middle and Upper Jurassic Lower Triassic Permian 2 km Crystalline basement 1B 1A 1C 1D 1E 2 3 ■■ ■■ 3 ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■■ ■■ ■■ ■ ■ ■ ■ ■■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■■ ■■ ■■ ■ ■ ■■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ Steensby Bjerg Gael Hamke Bugt Diener Bjerg Sortelv Spath Plateau Stensiö Plateau 21°00' 21°15'W 74°00'N 73°55'N Hold with Hope G ul el v ■ ■ ■■ ■■ ■ ■ ■■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ GEUS Bulletin no 5.pmd 29-10-2004, 11:1475 76 tion are controlled by the occurrence and accessibility of these fine-grained beds. In contrast, the shale of the Bernbjerg Formation provides productive samples throughout the formation. Standard palynological preparation has been per- formed on most samples. A minority of the samples were prepared by the tank-preparation method (Poulsen et al. 1990). Both methods involve treatment with hydrofluoric (HF) and hydrochloric acids (HCl) followed by filtering at 20 µm mesh size, short oxida- tion by nitric acid (HNO 3 ) and washing in low concen- tration potassium hydroxide (KOH). Biostratigraphy The ammonites and dinoflagellate cysts have been analysed and correlated to the Boreal ammonite and dinoflagellate stratigraphy, i.e. East Greenland strati- graphy (Callomon 1993; Milner & Piasecki 1996; Pia- secki 1996; Piasecki & Stemmerik 2004, this volume; Piasecki et al. 2004, this volume). Ammonites Ammonites are very restricted in the Jurassic succes- sion on Hold with Hope, and only three horizons have been dated and correlated with the standard Boreal ammonite stratigraphy (Callomon 1993). A specimen referred to Cadoceras cf. breve (J.H. Callomon and P. Alsen, personal communications 1997) was found 10 m A. mutabilis R. cymodoce P. baylei Bernbjerg Formation Payer Dal Formation Sandstone lower sandstone unit Spath Plateau Member A. rosenkrantzi A. regulare A. glosense C. tenuiserratum C. densiplicatum C. cordatum Q. mariae Q. lamberti P. athleta E. coronatum K. jason P. koenigi C. nordenskjoeldi C. apertum C al lo vi an O xf or di an K im m er id gi an U pp er Ju ra ss ic M id dl e Ju ra ss ic L L M Pelion Formation M U U S. calloviense A. serratum Chronozones Lithology Lithostratigraphy Heterolithic sandstone Ammonite Dinoflagellate cyst Mudstone Fig. 3. Schematic correlation of the Jurassic succession on northern Hold with Hope. The lithostratigraphical units are correlated with the Middle to Upper Jurassic chronozonation on the basis of ammonites and dinoflagellate cysts. Points of correlation to chronozones are indicated by ammonite or dinoflagellate cyst signatures. The subdivision of the chronozones corresponds to the ammonite faunas in the biozonation. Facing page: Fig. 4. Simplified sedimentological logs of the Jurassic succes- sion from Localities 1, 2 and 3 on northern Hold with Hope. The formal and informal lithostratigraphic units are indicated together with the ammonite horizons; l.s., lower shale. GEUS Bulletin no 5.pmd 29-10-2004, 11:1476 77 Silt Sand Pebbles F M C Locality 1 Locality 2 Lithology Locality 3 Poor exposure 427851 427850 427859 427810 427809 427808 427796 427793 427790 427780 427840 444854 444832 444855 444857 433158 433157 433859 GGU sample no. 433159 433858 444856 433868 444830 433869 433865 427833 427836 427730 427717 427729 427729 427818 427782 427705 427858 GGU sample no. Siltstone Poor exposure A. glosense A. glosense Poor exposure up pe r sa nd st on e un it l. s. un it Sp at h Pl at ea u M em be r Pe lio n Fo rm at io n Pe lio n Fo rm at io n C . a pe rt um – P . k oe ni gi Be rn bj er g Fo rm at io n Pa ye r D al F or m at io n lo w er sa nd st on e un it C . a pe rt um – P . k oe ni gi K. ja so n P. at hl et a A. g lo se ns e C . t en ui se rr at um P. ba yle i 50 100 150 200 250 300 350 m 0 Silt Sand Pebbles F M C 0 30 m P. koenigi Spath Plateau Member C. apertum Silt Sand Pebbles F M C 0 50 m Silty sandstone Sandstone Pebbly sandstone Pebble lag Structures Horizontal lamination Planar bedding Wave ripple Planar cross-bedding Trough cross-bedding Ammonite/Zone Hummocky cross-stratification Cross-lamination lo w er sa nd st on e un it Pa ye r D al F or m at io n C . t en ui se rr at um – A . g lo se ns e GEUS Bulletin no 5.pmd 29-10-2004, 11:1477 78 above the base of the lower sandstone unit in the Pelion Formation and indicates the Cadoceras apertum Zone (Fig. 4). A poorly preserved ammonite referred tenta- tively to Cadoceras septentrionale (P. Alsen, personal communication 1998) in the lowermost Spath Plateau Member of the Pelion Formation indicates the Pro- planulites koenigi Zone. Much higher in the succes- sion, in the basal Bernbjerg Formation, the presence of Amoeboceras ilovaiskii (J.H. Callomon and P. Alsen, personal communications 1997) indicates the Amoe- boceras glosense Zone. These three ammonite horizons occur at separate localities (Fig. 4). The C. apertum Zone is identified in the succession at Stensiö Plateau (Locality 3), the P. koenigi Zone is identified in the succession at Gulelv (Locality 1) and the A. glosense Zone is identified in the section at Sortelv (Locality 2). A calcareous con- cretion with a specimen of Cranocephalites sp. (C. pompeckji Zone) is reworked into the Cretaceous ba- sal conglomerate. The ammonite data thus indicate that parts of the lower Pelion Formation are equivalent to the C. apertum – P. koenigi Chronozones, Lower Cal- lovian, and parts of the lower Bernbjerg Formation are equivalent to the A. glosense Chronozone, Upper Oxfordian. A more detailed stratigraphical framework is provided by the more consistently occurring dino- flagellate cysts. Dinoflagellate cysts The dinoflagellate cyst data are described below in relation to five lithostratigraphic units, as presented by Vosgerau et al. (2004, this volume). Pelion Formation, lower sandstone unit The dinoflagellate cyst assemblages are of low to mod- erate diversity and density in the samples from this coarse-grained unit. The most diverse assemblages were recovered from the succession at Stensiö Plateau (Figs 2, 4, 5, Locality 3). Many of the species in this assem- blage are known from strata in East Greenland older than the Early Callovian age indicated here by ammo- nites (Milner & Piasecki 1996). Three assemblages have been distinguished in this unit, based on a limited number of samples. A lower assemblage of poor di- versity with frequent Chytroeisphaeridia hyalina and Sentusidinium sp. D (Fensome 1979) is followed by a middle assemblage of higher diversity with abundant Sirmiodinium grossii, Valensiella dictydia and Sentu- sidinium spp. The third and uppermost assemblage, above the ammonite horizon of the C. apertum Zone, is moderately to highly diverse and contains abundant Chytroeisphaeridia hyalina, Rhynchodiniopsis clado- phora, R. cf. cladophora and Pareodinia pachyceras (Fig. 5). The corresponding succession at Steensby Bjerg (Figs 2, 6, Locality 1) contains a very poor dinoflagellate cyst assemblage and Chytroeisphaeridia hyalina is the only frequent species. However, also at this locality slightly more species appear in the uppermost strata of the unit, thus showing an upwards increase in diversity. Correlation. The succession of species appearances up through the lower sandstone unit of the Pelion Formation in the Stensiö Plateau succession (Locality 3) does not yield any significant stratigraphic informa- tion. However, the abundance of Chytroeisphaeridia hyalina combined with the earliest appearance of Fromea tornatilis, Pareodinia prolongata, Aldorfia al- dorfensisandKallosphaeridium sp. in this unit are con- sidered indicative of the C. apertum Chronozone based on comparison to the dinoflagellate records in Jameson Land and Store Koldewey (Milner & Piasecki 1996; Pia- secki et al. 2004, this volume). This is also in accordance with the ammonite record in this succession. The poor dinoflagellate assemblage from the ‘lower sandstone unit’ at Steensby Bjerg (Locality 1) does not provide clear correlation but contains some character- istic species, e.g. Paraevansia brachythelis which has its lowest record in the C. apertum Chronozone on Store Koldewey (Piasecki et al. 2004, this volume). Several species that are restricted to the upper as- semblage of the Stensiö Plateau succession are also limited to the topmost strata of the corresponding unit in the succession at Steensby Bjerg: Aldorfia aldorfensis, Lithodinia planoseptata, Ctenidodinium thulium and Pareodinia prolongata. However, other species from the upper assemblage in the Stensiö Plateau succes- sion (C. apertum Chronozone at Locality 3) appear for the first time at a stratigraphically higher level in the Steensby Bjerg succession (Locality 1). This may re- flect the restricted material and data from this unit in the Steensby Bjerg succession (Locality 1). Age. The age of the ‘lower sandstone unit’ of the Pelion Formation is Early Callovian, equivalent to the C. apertum – P. koenigi Chronozones based on ammo- nites and dinoflagellate cysts. GEUS Bulletin no 5.pmd 29-10-2004, 11:1478 79 Depositional environment. The presence of a low di- verse assemblage with Limbicysta bjaerkei in the basal strata combined with significant, upwards increasing diversity indicate that deposition of this unit began in a marginal marine environment and changed to depo- sition in a fully marine environment. The preferred habitat of L. bjaerkei is non-marine (Bailey & Hogg 1995) but it also has been recorded in restricted ma- rine dinoflagellate cyst assemblages, for example in the basal strata of the Payer Dal Formation in Hoch- stetter Forland (Piasecki & Stemmerik 2004, this vol- ume). Here, L. bjaerkei occurs together with the ma- rine fauna immediately above non-marine–brackish sediments. Pelion Formation, Spath Plateau Member, lower shale unit The diversity and especially abundance of dinoflagel- late cysts reach a maximum in the basal mudstone of the Spath Plateau Member. In the Stensiö Plateau suc- cession (Locality 3), the composition of the assemblage is not significantly different from the highest assem- blage in the unit below. However, in the Steensby Bjerg succession (Locality 1), several species appear strati- graphically delayed compared to the Stensiö Plateau succession and their appearance in this ‘lower shale unit’ produces a local, significant increase in the diver- sity (Fig. 6). Chytroeispharidia hyalina is very abun- dant at both localities together with frequent Sirmiod- inium grossii, Sentusidinium pelionense, Rhynchodini- opsis cladophora, R. cf. cladophora and Sentusidinium sp. D (Fensome 1979). Correlation. The ammonite biostratigraphy shows that the mudstone is within or above the C. apertum and the P. koenigi Chronozones at Localities 1 and 3, re- spectively. The dinoflagellate biostratigraphy suggests that this mudstone is of the same age at Localities 1 and 3, i.e. equivalent to the P. koenigi Chronozone, but the stratigraphic resolution does not exclude the possibility that the basal mudstone at Locality 3 may include strata from the C. apertum Chronozone. This is the stratigraphical lower limit based on ammonites (Fig. 4). It is possible that the mudstone is diachronous. The ammonite found in sandstone at the lithostrati- graphic transition to the basal mudstone of the Spath Plateau Member at Locality 1 (Fig. 4), is referred to the Proplanulites koenigi Zone. Most of the dinoflagellate species that appear just above the ammonite at this locality, are reported to appear for the first time in or near the C. apertum Chronozone. The highest occur- rence of Paragonyaulacysta retiphragmata is found at the same level in both successions (Localities 1, 3) and indicates the P. koenigi Chronozone based on its last occurrence in the Jameson Land Basin (Milner & Piasecki 1996). The highest occurrence of Kallosphaer- idium hypornatum in Jameson Land is also in the P. koenigi Chronozone. Pareodinia stegasta appears in the basal mudstone as it does in a stratigraphically comparable transgressive shale unit on Store Kolde- wey (Piasecki et al. 2004, this volume). The lower boundary of the Spath Plateau Member is a major drowning surface overlain by mudstone both on Hold with Hope and on Store Koldewey (Piacecki et al. 2004, this volume; Vosgerau et al. 2004, this volume). Age. The age of the ‘basal shale unit’ of the Spath Plateau Member is Early Callovian, equivalent to the C. apertum – P. koenigi Chronozones. Depositional environment. The maximum diversity and density of dinoflagellate cysts in the Middle Jurassic succession occur in this unit and indicate deposition of shelf mudstone in a fully marine environment dur- ing flooding. Pelion Formation, Spath Plateau Member, upper sandstone unit Samples are available only from the succession at Steensby Bjerg (Locality 1). The dinoflagellate assem- blage is moderately rich and diverse. The bulk of the species are the same as in the shale below, but are combined with more species higher in the succession that typically appear in the Callovian. Chytroeisphaer- idia hyalina, Gonyaulacysta jurassica, Rhynchodini- opsis cladophora and Sentusidinium spp. are most fre- quent. Mendicodinium groenlandicum appears in the lower part of the unit and Tubotuberella eisenackii and Trichodinium scarburghense appear higher in the unit. Correlation. The overall Callovian dinoflagellate as- semblage provides few stratigraphical markers. The unit is stratigraphically restricted downwards by the pres- ence of Lower Callovian dinoflagellate cysts and am- monites (P. koenigi Chronozone) in the shale unit be- low. Records from the Jameson Land Basin indicate that Mendicodinium groenlandicum appears in the K. GEUS Bulletin no 5.pmd 29-10-2004, 11:1479 80 H old w ith H ope, Locality 3, Stensiö Plateau Metres 5030 Sample height Age Stage Formation 45.00 37.00 31.25 28.00 23.00 21.00 7.50 6.50 2.25 1.00 444853 444857 444856 444855 433869 444832 444830 433868 444854 433865 Cretaceous Steensby Bjerg Middle Jurassic Callovian Pelion 1 Tasmanites spp. 2 Valensiella dictydia 3 Solisphaeridium ankyleton 4 Leiofusa jurassica 5 Rhynchodiniopsis cf. regalis? 6 Sentusidinium spp. 7 Pareodinia halosa 8 Chytroeisphaeridia hyalina 9 Valensiella ovula 10 Sentusidinium cf. pelionense 11 Sentusidinium sp. D (Fensome 1979) 12 Fromea tornatilis 13 Atopodinium spp. 14 Valvaeodinium hanneae 15 Ctenidodinium thulium 16 Nannoceratopsis plegas var. dictyornata 17 Paraevansia spp. 18 Sirmiodinium grossii 19 Lithodinia spongiosa 20 Cyclopsiella spp. 21 Rhynchodiniopsis cladophora 22 Tubotuberella spp. 23 Ambonosphaera calloviana 24 Lithodinia spp. 25 Valvaeodinium leneae 26 Sentusidinium pelionense 27 Paragonyaulacysta retiphragmata 28 Pareodinia spp. 29 Pterospermopsis sp. A (Fensome 1979) 30 Valensiella spp. 0 2010 40 GGU sample no. G E U S B ulletin no 5.pm d 29-10-2004, 11:14 80 81 Fig. 5. D istrib u tio n ch art o f d in o flagellate cysts in th e Ju rassic su ccessio n at Lo cality 3, Sten siö P lateau , n o rth ern H o ld w ith H o p e. T h e first ap p earan ces o f sp ecies are stratigrap h ically arran ged . T h e Ju rassic su ccessio n is o verlain u n co n fo rm ab ly b y C retaceo u s strata o f th e Steen sb y B jerg Fo rm atio n (K elly et a l. 1998) – see sam p le at 45 m . 31 Solisphaeridium spp. 32 Lithodinia planoseptata 33 Aldorfia aldorfensis 34 Atopodinium haromense 35 Kallosphaeridium hypornatum 36 Gonyaulacysta jurassica 37 Pareodinia "granulata" 38 Pareodinia prolongata 39 Endoscrinium galeritum 40 Pareodinia pachyceras 41 Kallosphaeridium praussii. 42 Pilosidinium fensomei 43 Rhynchodiniopsis cf. cladophora 44 Chlamydophorella ectotabulata 45 Gonyaulacysta cf. helicoidea 46 Micrhystridium spp. 47 Sentusidinium sparsibarbatum 48 Mendicodinium spp. 49 Pareodinia stegasta 50 Paraevansia brachythelis 51 Lithodinia cf. callomonii 52 Gonyaulacysta pectinigera 53 Escharisphaeridia rudis 54 Veryhachium sortehatense 55 Micrhystridium cf. deflandrei 56 Tubotuberella eisenackii 57 Solisphaeridium cf. stimuliferum 58 Paragonyaulacysta sp. (Fensome 1979) 59 Batioladinium pelliferum 60 Escharisphaeridia spp. 61 Hystrichodinium spp. 62 Chytroeisphaeridia spp. A LPH A BET IC A L SPEC IES LIST 33 A ldorfia aldorfensis 23 A m bonosphaera calloviana 34 A topodinium harom ense 13 A topodinium spp. 59 B atioladinium pelliferum 44 C hlam ydophorella ectotabulata 8 C hytroeisphaeridia hyalina 62 spp. C hytroeisphaeridia 15 C tenidodinium thulium 20 spp. C yclopsiella 39 E ndoscrinium galeritum 60 spp. E scharisphaeridia 53 E scharisphaeridia rudis 12 F rom ea tornatilis 45 cf. G onyaulacysta helicoidea 36 G onyaulacysta jurassica 52 G onyaulacysta pectinigera 61 H ystrichodinium spp. 35 K allosphaeridium hypornatum 41 m K allosphaeridiu praussii 4 Leiofusa jurassica 51 Lithodinia cf.callom onii 32 Lithodinia planoseptata 19 Lithodinia spongiosa 24 Lithodinia spp. 48 M endicodinium spp. 55 M icrhystridium cf. deflandrei 46 M icrhystridium spp. 16 N annoceratopsis plegas var. dictyornata 29 P terosperm opsis sp. A (F ensom e 1979) 50 P araevansia brachythelis 17 P araevansia spp. 27 P aragonyaulacysta retiphragm ata 5837 P areodinia "granulata" 7 P areodinia halosa 40 P areodinia pachyceras 38 P areodinia prolongata 28 P areodinia spp. 49 P areodinia stegasta 42 P ilosidinium fensom ei 43 R hynchodiniopsis cf.cladophora 5 R hynchodiniopsis cf. regalis ? 21 R hynchodiniopsis cladophora 10 cf. S entusidinium pelionense 26 S entusidinium pelionense 11 S entusidinium sp. D (F ensom e 1979) 47 S entusidinium sparsibarbatum 6 S entusidinium spp. 18 S irm iodinium grossii 3 S olisphaeridium ankyleton 57 S olisphaeridium cf. stim uliferum 31 S olisphaeridium spp. 1 Tasm anites spp. 56 Tubotuberella eisenackii 22 Tubotuberella spp. 2 V alensiella dictydia 9 V alensiella ovula 30 V alensiella spp. 14 V alvaeodinium hanneae 25 V alvaeodinium leneae 54 V eryhachium sortehatense - P aragonyaulacysta sp. (F ensom e 1979) > 50 specim ens 2–50 specim ens 2–4 specim ens 1 specim en 5–19 specim ens G E U S B ulletin no 5.pm d 29-10-2004, 11:14 81 82 Hold with Hope, Locality 1, Steensby Bjerg M et re s 30 0 20 0 10 0 0 Sa m pl e he ig ht A ge St ag e Fo rm at io n 360.00 349.00 262.00 248.00 221.00 219.00 202.00 168.00 134.00 121.00 77.00 70.00 60.00 51.00 39.00 36.00 33.00 30.00 27.00 10.00 9.00 G G U s am pl e no . 427851 427850 427859 427858 427810 427809 427808 427796 427793 427790 427780 427840 427833 427836 427730 427729 427818 427782 427705 427717 427729 La te Ju ra ss ic M id dl e Ju ra ss ic K im m .? M id dl e – U pp er O xf or di an C al lo vi an Be rn bj er g Pa ye r D al Pe lio n Pe lio n – Sp at h Pl at ea u M em be r 1 Li m bi cy st a bj ae rk ei 2 P ar ae va ns ia b ra ch yt he lis 3 C hy tr oe is ph ae rid ia cf . c er as te s 4 R hy nc ho di ni op si s cf . c la do ph or a 5 C hy tr oe is ph ae rid ia h ya lin a 6 E sc ha ris ph ae rid ia cf .p oc oc ki i 7 V al en si el la d ic ty di a 8 E sc ha ris pa ha er ia la ev ig at a 9 A to po di ni um sp p. 10 S en tu si di ni um c f. pe lio ne ns e 11 S irm io di ni um g ro ss ii 12 P ar eo di ni a "g ra nu la ta " 13 N an no ce ra to ps is p el lu ci da 14 V al en si el la o vu la 15 G on ya ul ac ys ta c f. he lic oi de a 16 P ar eo di ni a pr ol on ga ta 17 C te ni do di ni um th ul iu m 18 Li th od in ia sp p. 19 A ld or fia a ld or fe ns is 20 Li th od in ia p la no se pt at a 21 A to po di ni um p ol yg on al e 22 K al lo sp ha er id iu m h yp or na tu m 23 B ar ba ta cy st a cr eb er ba rb at a 24 A lg ae in de t. 25 G on ya ul ac ys ta ju ra ss ic a 26 R hy nc ho di ni op si s cl ad op ho ra 27 Tu bo tu be re lla s pp . 28 P ar ag on ya ul ac ys ta r et ip hr ag m at a 29 V al en si el la s pp . 30 Li th od in ia s po ng io sa 31 P ar eo di ni a ha lo sa 32 K al lo sp ha er id iu m p ra us si i 33 C yc lo ps ie lla sp p. 34 S en tu si di ni um sp . D ( F en so m e 19 79 ) 35 S ur cu lo sp ha er id iu m sp p. 36 S en tu si di ni um sp p. 37 M en di co di ni um g ro en la nd ic um 38 P ar eo di ni a ce ra to ph or a 39 V er yh ac hi um s pp . 40 Tu bo tu be re lla d an ge ar di i 41 Li th od in ia cf . s po ng io sa 42 V al en si el la s p. ( F en so m e 19 79 ) GEUS Bulletin no 5.pmd 29-10-2004, 11:1482 83 43 Fromea tornalis 44 Lithodinia jurassica 45 Escharisphaeridia rudis 46 Kallosphaeridium spp. 47 Durotrigia spp. 48 Nannoceratopsis plegas var. dictyornata 49 Lithodinia valensi 50 Mendicodinium "granulatum" 51 Pareodinia pachyceras 52 Chlamydophorella ectotabulata 53 Atopodinium haromense 54 Ambonosphaera calloviense 55 Sentusidinium pelionense 56 Gonyaulacysta spp. 57 Pareodinia stegasta 58 Tubotuberella eisenackii 59 Trichodinium scarburghense 60 Gonyaulacysta eisenackii 61 Pareodinia spp. 62 Rigaudella filamentosa 63 Rhyncodiniopsis spp. 64 Barbatacysta verrucosa 65 Endoscrinium galeritum 66 Scriniodinium crystallinium 67 Leptodinium subtile 68 Escharisphaeridia pocockii 69 Scriniodinium spp. 70 Pareodinia scopaeus 71 Apteodinium cf. nuciforme 72 Scriniodinium inritibilum 73 Tubotuberella cf. dangeardii 74 Endoscrinium cf. galeritum 75 Meiourogonyaulax spp. 76 Epiplosphaera spp. 77 Dingodinium jurassicum 78 Tubotuberella cf. apatela 79 Escarisphaeridia erythrocoma 80 Sentusidinium sp. E (Fensome 1979) 81 Valensiella cf. dictydia 82 Tenua cf. hystrix 83 Sirmiodiniopsis spp. 84 Escharispahaeria spp. 85 Pareodinia borealis 86 Rhynchodiniopsis sp. (cf. "machaera") 87 Atopodinium cf. haromense 88 Rhynchodiniopsis spp. 89 Avellodinium spp. 90 Systematophora spp. 91 Sentusidinium myriatrichum 92 Prolixosphaeridium granulosum 93 Cribroperidinium granuligerum 94 Endoscrinium luridum 95 Circulodinium distinctum 96 Scriniodinium irregulare 97 Glossodinium dimorphum 98 Adnatosphaeridium spp. > 50 specim ens 20–50 specim ens 5–19 specim ens 2–4 specim ens 1 specim en G E U S B ulletin no 5.pm d 29-10-2004, 11:14 83 84 jason Chronozone and Trichodinium scarburghense appears in the P. athleta Chronozone (Milner & Pia- secki 1996; Piasecki 1996). Age. The age of the upper sandstone unit of the Spath Plateau Member, Pelion Formation, is therefore Early to Late Callovian, equivalent to the P. koenigi – P. athleta Chronozones (Fig. 4). Depositional environment. The organic matter is domi- nated by terrestrial palynomorphs and debris. The pro- portion of brown and black lath-shaped woody mate- rial increases upwards until it completely dominates the organic content in the upper Pelion Formation. The upwards increase and dominance of woody ma- terial suggests deposition in the lower shoreface envi- ronment in front of a prograding shoreline. Payer Dal Formation The Payer Dal Formation was analysed from two lo- calities at Steensby Bjerg, along the Sortelv (Locality 2) and Gulelv (Locality 1) rivers (Figs 2, 4, 6, 7). The for- mation is characterised by frequent Rigaudella aemula, Rhynchodiniopsis cladophora, Sirmiodinium grossii and Gonyaulacysta jurassica. New, stratigraphically characteristic species appear in the lower part of the formation at Sortelv: Wanaea digitata, Rigaudella aemula and Leptodinium subtile. Higher in the forma- tion at both localities further stratigraphically signifi- cant species appear: Scriniodinium crystallinum, En- doscrinium galeritum, Chytroeisphaeridia chytroeides, Rhynchodiniopsis sp., Prolixosphaeridium granulosum and Dingodinium jurassicum. Correlation. The dinoflagellate assemblage represents a characteristic Lower to Middle Oxfordian assemblage with frequent Rigaudella aemula, Scrinidinium crys- tallinum and Endoscrinium galeritum, as known from the Jurassic succession elsewhere in East Greenland such as in Milne Land (Piasecki 1996). This Lower– Middle Oxfordian assemblage in Milne Land reaches close to the top of the Middle Oxfordian before gradual replacement by an Upper Oxfordian assemblage. Wanaea spp. occurs only to the top of the Lower ALPHABETICAL SPECIES LIST 98 Adnatosphaeridium spp. 19 Aldorfia aldorfensis 54 Ambonosphaera calloviense 71 Apteodinium cf. nuciforme 87 Atopodinium cf. haromense 53 Atopodinium haromense 21 Atopodinium polygonale 9 Atopodinium spp. 89 Avellodinium spp. 23 Barbatacysta creberbarbata 64 Barbatacysta verrucosa 52 Chlamydophorella ectotabulata 3 Chytroeisphaeridia cerastes 5 Chytroeisphaeridia hyalina 95 Circulodinium distinctum 93 Cribroperidinium granuligerum 17 Ctenidodinium thulium 33 Cyclopsiella spp. 77 Dingodinium jurassicum 47 Durotrigia spp. 74 Endoscrinium cf. galeritum 65 Endoscrinium galeritum 94 Endoscrinium luridum 76 Epiplosphaera spp. 79 Escarisphaeridia erythrocoma 8 Escharispahaeria laevigata 84 Escharispahaeria spp. 6 Escharisphaeridia cf. pocockii 68 Escharisphaeridia pocockii 45 Escharisphaeridia rudis 43 Fromea tornalis 97 Glossodinium dimorphum 60 Gonyaulacysta eisenackii 15 Gonyaulacysta cf. helicoidea 25 Gonyaulacysta jurassica 56 Gonyaulacysta spp. 22 Kallosphaeridium hypornatum 32 Kallosphaeridium praussii 46 Kallosphaeridium spp. 1 Limbicysta bjaerkei 41 Lithodinia cf. spongiosa 44 Lithodinia jurassica 20 Lithodinia planoseptata 30 Lithodinia spongiosa 18 Lithodinia spp. 49 Lithodinia valensi 75 Meiourogonyaulax spp. 50 Mendicodinium "granulatum" 37 Mendicodinium groenlandicum 48 Nannoceratopsis plegas var. dictyornata 13 Nannoceratopsis pellucida 2 Paraevansia brachythelis 28 Paragonyaulacysta retiphragmata 12 Pareodinia "granulata" 85 Pareodinia borealis 38 Pareodinia ceratophora 31 Pareodinia halosa 51 Pareodinia pachyceras 16 Pareodinia prolongata 70 Pareodinia scopaeus 61 Pareodinia spp. 57 Pareodinia stegasta 92 Prolixosphaeridium granulosum 4 Rhynchodiniopsis cf. cladophora 86 Rhynchodiniopsis sp. (cf. "machaera") 26 Rhynchodiniopsis cladophora 88 Rhynchodiniopsis spp. 63 Rhynchodiniopsis spp. 62 Rigaudella filamentosa 66 Scriniodinium crystallinium 72 Scriniodinium inritibilum 96 Scriniodinium irregulare 69 Scriniodinium spp. 10 Sentusidinium cf. pelionense 91 Sentusidinium myriatrichum 55 Sentusidinium pelionense 34 Sentusidinium sp. D (Fensome 1979) 80 Sentusidinium sp. E (Fensome 1979) 36 Sentusidinium spp. 83 Sirmiodiniopsis spp. 11 Sirmiodinium grossii 35 Surculosphaeridium spp. 90 Systematophora spp. 82 Tenua cf. hystrix 59 Trichodinium scarburghense 78 Tubotuberella cf. apatela 73 Tubotuberella cf. dangeardii 40 Tubotuberella dangeardii 58 Tubotuberella eisenackii 27 Tubotuberella spp. 81 Valensiella cf. dictydia 7 Valensiella dictydia 14 Valensiella ovula 42 Valensiella sp. (Fensome 1979) 29 Valensiella spp. 39 Veryhachium spp. 24 Algae indet. 67 Leptodinium subtile Previous page: Fig. 6. Distribution chart of dinoflagellate cysts in the Jurassic succession at Locality 1, Steensby Bjerg, northern Hold with Hope. The first appearances of species are stratigraphically arranged. Alphabetical species list given above. GEUS Bulletin no 5.pmd 29-10-2004, 11:1484 85 Hold with Hope, Locality 2, Sortelv 20 Sa m pl es h ei gh t 34.00 32.00 28.50 25.00 9.00 G G U s am pl e no . 433859 433159 443158 433157 433858 La te Ju ra ss ic O xf or di an Pa ye r D al F or m at io n 1 S cr in io di ni um cf . i nr iti bi lu m 2 C hy tr oe is ph ae rid ia c er as te s 3 W an ae a sp p. 4 R ig au de lla fi la m en to sa 5 S te ph an el yt ro n sp p. 6 A to po di ni um h ar om en se 7 G on ya ul ac ys ta ju ra ss ic a 8 S irm io di ni um g ro ss ii 9 R hy nc ho di ni op si s cl ad op ho ra 10 Tr ic ho di ni um s ca rb ur gh en se 11 E nd os cr in iu m g al er itu m 12 Le pt od in iu m s ub til e 13 R ig au de lla a em ul a 14 A to po di ni um sp p. 15 P ar eo di ni a "g ra nu la ta " 16 S ur cu lo sp ha er id iu m sp p. 17 C irc ul od in iu m d is tin ct um 18 Tu bo tu be re lla a pa te la 19 W an ae a di gi ta ta 20 P ar eo di ni a bo re al is 21 E sc ha ris ph ae rid ia la ev ig at a 22 V al en si el la d ic ty di a 23 S cr in io di ni um c ry st al lin iu m 24 A m bo no sp ha er a ca llo vi an a 25 P ar eo di ni a ce ra to ph or a 26 C hy tr oe is ph ae rid ia c hy tr oe oi de s 27 P ro lix os ph ae rid iu m g ra nu lo su m 28 E sc ha ris ph ae rid ia sp p. ALPHABETICAL SPECIES LIST 24 Ambonosphaera calloviana 6 Atopodinium haromense 14 Atopodinium spp. 2 Chytroeisphaeridia cerastes 26 Chytroeisphaeridia chytroeoides 17 Circulodinium distinctum 11 Endoscrinium galeritum 21 Escharisphaeridia laevigata 28 Escharisphaeridia spp. 7 Gonyaulacysta jurassica 12 Leptodinium subtile 15 Pareodinia "granulata" 20 Pareodinia borealis 25 Pareodinia ceratophora 27 Prolixosphaeridium granulosum 9 Rhynchodiniopsis cladophora 13 Rigaudella aemula 4 Rigaudella filamentosa 1 Scriniodinium cf. inritibilum 23 Scriniodinium crystallinium 8 Sirmiodinium grossii 5 Stephanelytron spp. 16 Surculosphaeridium spp. 10 Trichodinium scarburghense 18 Tubotuberella apatela 22 Valensiella dictydia 19 Wanaea digitata 3 Wanaea spp. M et re s A ge St ag e Fo rm at io n 30 10 20–50 specimens 5–19 specimens 2–4 specimens 1 specimen Fig. 7. Distribution chart of dinoflagellate cysts in the Jurassic succession at Locality 2, Sortelv, western Steensby Bjerg, Hold with Hope. The first appearance of species is stratigraphically arranged. G E U S B ul le tin n o 5. pm d 29 -1 0- 20 04 , 1 1: 14 85 86 Oxfordian in Milne Land, whereas Leptodinium subtile rarely occurs below the Middle Oxfordian and Prolixo- sphaeridium granulosum does not occur below the Upper Oxfordian. The Payer Dal Formation at Locality 1 is therefore considered Middle to Late Oxfordian in age, and the presence of Wanaea digitata, Wanaea sp. and Trichodinium scharburghense in the assem- blage is due to reworking. In Milne Land, the appear- ance of Leptodinium subtile in the C. tenuiserratum Chronozone coincides with the gradual disappearance of Rigaudella spp., and the following appearances of Dingodinium jurassicum and Prolixosphaeridium granulosum in the A. glosense Chronozone. A corre- sponding sequence of events in the Steensby Bjerg succession indicates a Middle–Upper Oxfordian suc- cession, C. tenuiserratum – A. glosense Chronozones. Consequently, a significant Late Callovian – earliest Middle Oxfordian hiatus occurs between the Pelion and Payer Dal Formations. However, several samples in the boundary interval (c. 30 m thick) were barren of dinoflagellate cysts and parts of the succession were therefore not dated. The dinoflagellate cysts, which are considered reworked, indicate that Lower Oxfordian sediments have been present in the region. Age. The age of the Payer Dal Formation is Middle– Late Oxfordian, equivalent to the C. tenuiserratum – A. glosense Chronozones based on dinoflagellate cysts. Ammonites in the overlying Bernbjerg Formation sup- port this age of the uppermost Payer Dal Formation as they indicate the A. glosense Chronozone. Depositional environment. The organic matter is domi- nated by terrestrial palynomorphs and debris, and the proportion of brown and black lath-shaped woody material is high in the Payer Dal Formation. The or- ganic content suggests deposition in a lower shore- face environment. Bernbjerg Formation The Bernbjerg Formation is represented by a few sam- ples from the lower and upper parts of the formation at Steensby Bjerg (Locality 1). The Bernbjerg Forma- tion contains abundant Sirmiodinium grossii and Gonyaulacysta jurassica. In the lower levels of the formation, the presence of abundant Leptodinium subtile is combined with the appearance of Paragon- yaulacysta borealis, Rhynchodiniopsis sp. and Tenua cf. hystrix. The assemblage is very similar to the as- semblage in the upper Payer Dal Formation partly due to the continued presence of Endoscrinium galeritum and Scriniodinium crystallinum. The stratigraphically important Taeniophora sp. / Adnatosphaeridium sp. (informal name ‘A. hartzii’ in: Piasecki 1980) appears in the uppermost sample from the formation. Correlation. The continued presence of Endoscrin- ium galeritum and Scriniodinium crystallinum from the Payer Dal Formation below, and the absence of Taeniophora sp. / Adnathosphaeridium sp. (‘A. hart- zii’) correlates with the lower Upper Oxfordian, A. glosense Chronozone, by comparison to dinoflagellate floras from Milne Land (Piasecki 1996). This is in ac- cordance with abundant ammonites of the Amoeboce- ras glosense Zone in these strata, and with the absence of the uppermost Oxfordian dinoflagellate cyst spe- cies that appear above. The upper part of the Bernbjerg Formation contains abundant Gonyaulacysta jurassica and Sirmiodinium grossii in combination with Adnatosphaeridium sp. (‘A. hartzii’), Cribroperidinium granuligerum, Sciniodin- ium irregulare, Glossodinium cf. dimorphum, Endos- crinium luridum and Prolixosphaeridium granulosum. The composite dinoflagellate cyst flora indicates an Upper Oxfordian to lowermost Kimmeridgian succes- sion, A. serratum – P. baylei Chronozones. The pres- ence of Avellodinium spp. in the uppermost sample could indicate the lowermost Kimmeridgian A. mutabilis Chronozone, but this is not supported by any other stratigraphical diagnostic species such as Perisseiasphaeridium pannosum (Piasecki 1996; Piasecki & Stemmerik 2004, this volume). Age. The age of the Bernbjerg Formation is Late Oxfordian – earliest Kimmeridgian, equivalent to the A. glosense – P. baylei Chronozones based on dino- flagellate cysts. Ammonites in the lower part of the Bernbjerg Formation indicate the A. glosense Chrono- zone and confirm the Late Oxfordian age for this part of the formation. Depositional environment. The organic content is dominated by terrestrial sporomophs and woody ma- terial but dinoflagellate cysts occur frequently. A dep- ositional environment of lower shoreface to open shelf is interpreted on this basis. GEUS Bulletin no 5.pmd 29-10-2004, 11:1486 87 Correlations The Pelion Formation on northern Hold with Hope comprises two main units, a lower sandstone unit fol- lowed by mudstones and heterolithic sandstones of the Spath Plateau Member. The same overall pattern occurs in the Pelion Formation on Store Koldewey at Ravn Pynt (Piasecki et al. 2004, this volume). How- ever, on Store Koldewey, the lower sandstone unit is older (Bathonian) than the lower sandstone unit on Hold with Hope. The mudstone and overlying sand- stone on Store Koldewey are basically of the same Early Callovian age as the lowermost Spath Plateau Member on Hold with Hope (C. apertum – P. koenigi Chronozones). The marine flooding represented by deposition of this mudstone can be traced from Milne Land and Jameson Land in the south (P7 – third order sequence; Engkilde & Surlyk 2003) to Hold with Hope and Store Koldewey in the north. The Payer Dal Formation is defined on Kuhn Ø where it comprises two units that are of Early–Middle Oxfordian age and early Late Oxfordian age (Alsgaard et al. 2003). On Hold with Hope, the exposure of the oldest part of the Payer Dal Formation at Sortelv (Fig. 2; Locality 2) is limited by a fault, and older strata may be present in the subsurface. However, no strata of Early Oxfordian age have been recorded here, and the age of the Payer Dal Formation on Hold with Hope is Middle–Late Oxfordian, partly corresponding to the upper part of this formation on Kuhn Ø. Sedimentation of fine-grained sand and mudstone of the Bernbjerg Formation began in the A. glosense Chron on Hold with Hope as in Wollaston Forland to the north (Surlyk 1977). Conclusions The combined biostratigraphical dataset from ammo- nites and dinoflagellate cysts dates the stratigraphical range of the lithological units with a high degree of precision (Figs 3, 4). However, the extent of non-dep- ositional or erosional hiati in or between the units can- not be determined with the same certainty due to the limited number of productive samples. The ‘basal sand- stone unit’ of the Pelion Formation ranges from the uppermost C. apertum Chronozone to the lower P. koenigi Chronozone (Figs 3, 4). The age is therefore Early Callovian. The dinoflagellate assemblages show no indication of a break in sedimentation so the suc- cession is considered complete. The Spath Plateau Member of the Pelion Formation comprises the P. koe- nigi, K. jason and P. athleta Chronozones (Fig. 3). The age is therefore Early to Late Callovian, but a part of the succession occurs above the highest productive sample and may therefore be younger. A considerable hiatus is present between the Pelion Formation and the overlying Payer Dal Formation. However, the exact stratigraphical position of the unconformity and the extent of the hiatus cannot be determined precisely, because no productive samples were recovered from the boundary interval. The avail- able data suggest a hiatus that comprises most of the Late Callovian, Early Oxfordian and earliest Middle Oxfordian. The Payer Dal Formation ranges from the C. tenuiserratum to the A. glosense Chronozones, and the age is consequently Middle to Late Oxfordian (Fig. 3). The dinoflagellate assemblages indicate no break in deposition at the boundary to the Bernbjerg Forma- tion, and the A. glosense Chronozone is also identified in the basal Bernbjerg Formation on the basis of am- monites. The Jurassic succession and the Bernbjerg Formation are limited upwards by pre-Barremian, Cre- taceous erosion, and the highest samples are referred to the A. rosenkrantzi – P. baylei Chronozones at the Oxfordian–Kimmeridgian boundary (Fig. 3). The age of the Bernbjerg Formation is thus Late Oxfordian, possibly earliest Kimmeridgian. The Jurassic succession on northern Hold with Hope correlates well with the corresponding Jurassic suc- cessions towards the north and the south, but appears more fragmented compared to these successions. A Boreal Bathonian (Bajocian–Bathonian) succession has been deposited in this region, at least partly, but was removed by later erosion as indicated by the reworked ammonite of the P. pompeckji Zone. The previous pres- ence of a Lower Oxfordian succession is similarly indi- cated by reworked dinoflagellate cysts. The magnitude of the hiatus below the Payer Dal Formation is Late Callovian – Middle Oxfordian. Acknowledgements The present biostratigraphic study was supported by the Carlsberg Foundation (Carlsbergfondet Ans. 980089/ 20-262). John H. Callomon and Peter Alsen are thanked for identification of ammonites from Hold with Hope. 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