Geological Survey of Denmark and Greenland Bulletin 1, 723-775 723 The aim of this study was to obtain a better under- standing of the palynomorph flora, the age and the depositional environment of the Neill Klinter Group in Jameson Land, East Greenland (Fig. 1). Although the sedimentology, fossil faunas, ichnofaunas, lithostrati- graphy and sequence stratigraphy of this succession have been studied in detail (Rosenkrantz 1934; Sykes 1974; Dam 1990a, b, 1991; Dam & Surlyk 1995, 1998), there are few published papers on the palynology of the Neill Klinter Group. The group has recently been divided into four formations and nine members (Fig. 2) and a detailed sequence stratigraphic correlation between East Greenland and Norway has been established (Dam & Surlyk 1995, 1998). Lithostratigraphic units of the group that are precisely dated by macrofossils are re- stricted to the Rævekløft Formation and the Lepidopteriselv, Palynostratigraphy and palaeoenvironments of the Rævekløft, Gule Horn and Ostreaelv Formations (Lower–Middle Jurassic), Neill Klinter Group, Jameson Land, East Greenland Eva B. Koppelhus and Gregers Dam The Neill Klinter Group of Jameson Land, East Greenland contains rich and diverse palynomorph assemblages. Spores, pollen and freshwater algae dominate most of the samples, but dinofla- gellate cysts and acritarchs also form important components. The ages suggested by the paly- nomorphs from the Rævekløft, Gule Horn and Ostreaelv Formations span the period from the Early Pliensbachian to the early Aalenian. The number of palynomorphs identified totals 136, including 83 miospore and 53 microplankton species; they are grouped into seven palynologi- cal assemblage zones. In general, there is good agreement between the palynological and sedimentological data, and the palynological data has refined the understanding of the depositional palaeoenvironments of the Neill Klinter Group. In some cases, the boundaries of the palynological assemblage zones are congruent with major sequence stratigraphic surfaces and the palynological data thus sup- port the sequence stratigraphic interpretation. In other cases, however, regional correlation indi- cates that the zone boundaries cross important sequence stratigraphic surfaces, such as sequence boundaries; such behaviour is thought to reflect the facies-dependent nature of certain of the palynological assemblage zones. The pattern of palynological events in East Greenland has also been recognised on the mid-Norwegian shelf. Keywords: East Greenland, Jameson Land Basin, Lower–Middle Jurassic, Early Pliensbachian – early Aalenian, palynostratigraphy, sedimentology, sequence stratigraphic implications, regional correlation E.B.K.* & G.D.‡, Geological Survey of Denmark and Greenland, Geocenter Copenhagen, Øster Voldgade 10, DK- 1350 Copenhagen K, Denmark. Present addresses: *Royal Tyrrell Museum of Palaeontology, Box 7500, Drumheller T0J 0Y0, Alberta, Canada. E- mail: evakoppelhus@hotmail.com ‡DONG A/S, Agern Allé 24–26, DK-2970 Hørsholm, Denmark. Geological Survey of Denmark and Greenland Bulletin 1, 723–775 (2003) © GEUS, 2003 724 Nathorst Fjeld and Skævdal Members of the Ostreaelv Formation. The Neill Klinter Group was sampled inten- sively for palynological analysis at a number of different localities in Jameson Land (Fig. 1). This paper only includes data from the lowermost three formations of the Neill Klinter Group (Rævekløft, Gule Horn and Ostrea- elv Formations). The uppermost formation, the Sortehat Formation, is treated in an accompanying paper (Koppel- hus & Hansen 2003, this volume). Seven palynomorph assemblage zones have been established from the most complete section, at Albuen (Figs 3, 4). Data from other localities have been correlated with this section. Geological setting The Upper Palaeozoic – Mesozoic Jameson Land Basin is located in the present-day land areas of Jameson Land and Scoresby Land, at the southern end of the East Greenland rift system (Fig. 1; Surlyk 1978). This system is part of a larger rift complex separating Greenland from Norway before the opening of the North Atlantic Ocean (Ziegler 1988). The Jameson Land Basin is bounded to the east and west by major N–S-trending faults, and to the north by a NW–SE cross-fault in Kong Oscar Fjord (Surlyk 1977a, 1978, 1990a). The southern boundary is 25 km Illoqqortoormiut 24°W 72°N 71°N N Neill Klinter Group Studied localities Normal fault ? ? Scoresby Sund ? Jameson Land Scoresby Land Kong O scar Fjord Liaselv Rhætelv Lepidopteriselv Ranunkeldal Enhjørningen Dal Horsedal Moskusoksekløft Astartekløft Goniomyakløft Albuen Rævekløft Harris Fjeld Nathorst Fjeld Elis Bjerg Dusén Bjerg Sortehat Primulaelv Qupaulakajik Skævdal Vardekløft Tancrediakløft ? 22°W Liverpool Land Greenland Fig. 1. Map of the Jameson Land region showing the outcrop of the Neill Klinter Group, the location of sections forming the basis of this study and additional localities mentioned in the text. 725 unknown, but the basin probably extended south of Scoresby Sund, an area that is now covered by Palaeogene plateau basalts. The basin was initiated in the Devonian due to extensional collapse of the over-thickened crust of the Caledonian mountain belt. The Devonian phase was probably associated with strike-slip or oblique-slip deformation resulting in the development of NW–SE-trending transverse faults in the north-eastern part of the basin. During Late Carboniferous – Early Permian times, the oblique-slip regime changed to a more orthogonal extensional regime, resulting in the development of basin margin half-grabens (Surlyk et al. 1984, 1986; Surlyk 1990a; Larsen & Marcussen 1992). The period of extensional tectonics was followed by a long period of subsidence lasting from the Late Permian to the Cretaceous, inter- rupted by minor episodes of rifting and faulting (Surlyk 1977a, b, 1990a; Clemmensen 1980a; Surlyk et al. 1981, 1986; Larsen & Marcussen 1992). Triassic – Early Jurassic sedimentation in the Jameson Land Basin was, in addition to tectonic subsidence, also influenced by climate, drainage patterns and eustasy. During the Triassic – earliest Jurassic, a major lacustrine complex was situated in the Jameson Land Basin. The lacustrine deposits record a long-term change from a warm arid to a more temperate humid climate (Clem- mensen 1978a, b, 1979, 1980a, b; Bromley & Asgaard 1979; Dam & Surlyk 1992, 1993). This long-term climatic change was mainly governed by a gradual northwards drift of the Laurasian continent and was accompanied by a long-term eustatic sea-level rise during the Early Jurassic. In the Pliensbachian, the lacustrine complex was transformed into a shallow marine embayment marking the first fully-marine inundation of the basin since Late Permian – Early Triassic times (Surlyk 1990b). The sandstones and mudstones of the Neill Klinter Group were deposited in a wide, shallow tide- and storm-influenced marine embayment, during a period of relative tectonic quiescence. The facies pattern was controlled mainly by relative sea-level fluctuations, sed- iment influx and basinal currents (Sykes 1974; Dam & Surlyk 1995, 1998). Sortehat Ostreaelv Gule Horn Elis Bjerg Skævdal Harris Fjeld Nathorst Fjeld Lepidopteriselv Trefjord Bjerg MemberFormation Albuen Astartekløft Horsedal Rævekløft Rhaetian Hettangian Sinemurian Pliensbachian Toarcian Lo w er M id dl e Ju ra ss ic Tr ia s. U pp er Aalenian Bajocian Bathonian Callovian Oxfordian Kimmeridgian Volgian GroupChronostratigraphy Formation Sortehat Ostreaelv Gule Horn Rævekløft Kap Stewart Ja m es on L an d Super- group Scoresby Sund Hall Bredning Vardekløft Neill Klinter Raukelv Hareelv Olympen Fossil- bjerget Pelion R hæ te lvPrimulaelv Innakajik Fig. 2. Jurassic lithostratigraphy of Jameson Land showing the detailed subdivision of the Neill Klinter Group formalised by Dam & Surlyk (1998). Modified from Surlyk (2003, this volume, fig. 5). Stratigraphy The Pliensbachian – lower Aalenian succession now referred to the Neill Klinter Group was initially described by Rosenkrantz (1929), but was first formally estab- lished as a formation by Surlyk et al. (1973). The Neill Klinter Formation (sensu Surlyk et al. 1973) has subse- quently been raised to group status (Dam & Surlyk 1998) and the Rævekløft, Gule Horn and Ostreaelv Members of Surlyk et al. (1973) have been elevated to formation status. Moreover, the former Sortehat Member of the Vardekløft Formation (Surlyk et al. 1973) has been promoted to formation and transferred to the Neill Klinter Group (Dam & Surlyk 1998). These authors divided the Gule Horn Formation into two new mem- bers and the Ostreaelv Formation into seven new mem- bers (Fig. 2). The Neill Klinter Group is exposed in Jameson Land and Scoresby Land, and in a small fault-bounded out- lier in the southern part of Liverpool Land (Fig. 1); it is 300–450 m thick. The boundary between the Kap Stewart Group and the succeeding Neill Klinter Group is an ero- sional unconformity along the south-eastern basin mar- gin, representing a major hiatus corresponding to the Sinemurian Stage (Harris 1931; Surlyk 1991; Dam & Surlyk 1995, 1998). The unconformity passes basin- wards into a conformity and the contact between the lacustrine mudstones of the Kap Stewart Group and the shallow marine sandstones of the Neill Klinter Group is gradational (Fig. 5; Surlyk 1991; Dam & Surlyk 1995, 1998). The upper boundary of the Neill Klinter Group is placed at a sharp unconformity between the mud- stones of the Sortehat Formation and the sandstones of the Vardekløft Group (Surlyk et al. 1973; Surlyk 1990a; Engkilde 1994; Koppelhus & Hansen 2003, this vol- ume). The Neill Klinter Group and most of its con- stituent formations and members show an overall sheet geometry, although the thicknesses of the units are greatest in the basin centre and thin towards the mar- gins (Dam & Surlyk 1995, 1998). A rich marine fauna is present in the lower part of the Neill Klinter Group (Rosenkrantz 1934). It occurs in the Rævekløft Formation and is restricted to certain levels separated by largely unfossiliferous intervals. Rosenkrantz (1934) identified a lower division, with a diverse fauna (150 species) dominated by bivalves, gas- tropods, cephalopods, echinoids and crinoids, and an upper division yielding a relatively sparse fauna (c. 20 molluscan species). Ammonites of the genus Uptonia occur in the lower division, suggesting that these beds belong to the Early Pliensbachian Jamesoni Zone (Rosenkrantz 1934). In the upper division, Rosenkrantz (1934) found two ammonites, Beaniceras sp. and Lytoceras fimbriatum. Rosenkrantz (1934) referred this division to the Ibex Zone, although the bed also yielded an ammonite that appears to be Aegoceras aff. capri- cornus of the maculatum group, indicative of the Davoei Zone (Callomon 1961; Surlyk et al. 1973). All the belemnites recovered from the Rævekløft Formation by Rosenkrantz were apparently collected from the Jamesoni Zone interval. They indicate that the Jamesoni Zone as adopted by Rosenkrantz (1934) includes the Early Pliensbachian Jamesoni Zone to at least the Ibex Zone and possibly the early Davoie Zone (Doyle 1991). The marine macrofossils of the Lepidopteriselv, Nathorst Fjeld, Skævdal and Trefjord Bjerg Members of the Ostreaelv Formation and the Sortehat Formation are bivalves, brachiopods, crinoids, belemnites, am- monites, and vertebrates (Rosenkrantz 1934). Ammonites collected on the top of Elis Bjerg from strata belonging to the Lepidopteriselv Member include Dactylioceras semicelatum (Simpson) sensu Howarth 1992 (probably including D. groenlandicum Rosenkrantz 1934) and Hildaites sp. aff. murleyi (Moxon). Dactylioceras semi- celatum belongs to the Early Toarcian Tenuicostatum Zone, Semicelatum Subzone (J.H. Callomon, personal communication 1993). Hildaites sp. is an early form, rem- iniscent of Protogrammoceras. Dactylioceras sp. has also been collected at Nathorst Fjeld in the Nathorst Fjeld Member and in the lower part of the Skævdal Member, also suggesting an Early Toarcian Tenuicostatum Zone age (C. Bjerrum and J.H. Callomon, personal commu- nications 1996). Dactylioceras sp. and Hildaites sp., suggestive of the Early Toarcian, have also been col- lected from the Lepidopteriselv Member in Horsedal, although they were both loose specimens. Phydoleoceras sp. has been collected on Nathorst Fjeld in the Trefjord Bjerg Member, just beneath the boundary of the Sortehat Formation (C. Bjerrum, personal communication 1996). The Lepidopteriselv Member has been correlated on sequence stratigraphic grounds with the Nathorst Fjeld Member (Dam & Surlyk 1995, 1998). On Nathorst Fjeld, Rosenkrantz (1934) collected a specimen of the belem- nite Parapassolotheuthis polita at an altitude of 494 m, and ‘Parabrachybelus’ subaduncatus at 509 m. The lower level probably belongs to the Nathorst Fjeld Member, and the upper level to the overlying Skævdal Member. The two species have restricted ranges and are not known to be widespread in Europe. Para- passolotheuthis polita has only been recorded from the Early Toarcian latest Falciferum Zone or earliest Bifrons Zone (Commune Subzone) in Britain, while ‘Para- 726 brachybelus’ subaduncatus, which so far has only been recorded from mainland Europe, has a range probably restricted to the latest Toarcian Levesquei Zone (Doyle 1991). The ammonite Dactylioceras semicelatum (Simp- son) has been collected at the base of the Skævdal Member at Nathorst Fjeld (C. Bjerrum, personal com- munication 1996) and in the Lepidopteriselv Member on top of Elis Bjerg indicating an Early Toarcian Tenuicostatum Zone, Semicelatum Subzone age (J.H. Callomon, personal communication 1993). Based on these data, the Nathorst Fjeld and Lepidopteriselv Members and the lower part of the Skævdal Member include strata with an Early Toarcian Tenuicostatum Zone to latest Falciferum Zone or earliest Bifrons Zone age. Belemnites suggest that the Skævdal Member may also include strata with a latest Toarcian Levesquei Zone age (Doyle 1991; Dam & Surlyk 1998), suggesting either that the Skævdal Member has a very long age range, that the belemnites cannot be used stratigraphically or that the D. semicelatum at the base of the Skævdal Member is reworked. Dam & Surlyk (1995, 1998) interpreted the Neill Klinter Group within a sequence stratigraphic framework and attempted a sequence stratigraphic correlation with the coeval Tilje, Ror, Ile and Not Formations on the mid- Norwegian shelf. This comparison demonstrated that the Lower Jurassic in both regions consists of six sequences and it appears feasible to directly correlate systems tracts on a scale of a few tens of metres between East Greenland and the mid-Norwegian shelf (see Fig. 17). Previous palynological work Previous reports on the palynology of the Neill Klinter Group have been published by Lund & Pedersen (1985) and Underhill & Partington (1994). The former authors studied the Neill Klinter Group together with the over- lying Vardekløft Group (sensu Surlyk 2003, this vol- ume, fig. 5) and the lower part of the Hareelv Formation. Based on material collected from Vardekløft, in the south-eastern part of the basin (Fig. 1), Lund & Pedersen (1985) proposed four assemblage zones for the entire succession based on the miospore assemblages. Dino- flagellate cysts were used to improve the age correla- tion of the spore-pollen assemblages. The three lowermost assemblage zones A, B and C of Lund & Pedersen (1985) cover the Rævekløft, Gule Horn and Ostreaelv Formations of the Neill Klinter Group. Assemblage Zone A is divided into subassemblages A1 and A2; the age of the zone was suggested to be Late Pliensbachian because of the presence of the spore Kraeuselisporites reissingeri and the dinoflagellate cyst Nannoceratopsis triceras. Assemblage Zone B is char- acterised by abundant Spheripollenites subgranulatus and Luehndea spinosa, and an Early Toarcian age was proposed. Assemblage Zone C is characterised by the incoming of the pollen Callialasporites dampieri, the spores Sestrosporites pseudoalveolatus and Staplini- sporites caminus and the dinoflagellate cyst Parvocysta contracta (now Susadinium scrofoides); these species were considered to indicate a Late Toarcian age for the lowermost Assemblage Zone C (subassemblage (C)). Underhill & Partington (1994) discussed the devel- opment of the Lower Jurassic in East Greenland in con- nection with a sequence stratigraphic study of the North Sea. They included 3 sections from Jameson Land, Section 1 from Liaselv, Section 2 from Vardekløft and Section 3 from the Harris Fjeld/Primulaelv area (Fig. 1). Sections 1 and 2 cover the uppermost few metres of the Ostreaelv Formation and all of the Sortehat Formation and Vardekløft Group. Section 3 covers 170 m of the Neill Klinter Group. Underhill & Partington (1994) analysed 48 samples and recognised 11 events. They suggested a Late Pliensbachian – earliest Toarcian age for the Gule Horn Formation and a Toarcian age for the Ostreaelv Formation. Materials and methods Most of the samples used in this study are from the sec- tion at Albuen, in the fifth ravine north of Skævdal (Figs 1, 3). Intervals that proved inaccessible in this ravine were sampled at Astartekløft (see Figs 1, 9). Samples were also obtained from Rævekløft, Tancrediakløft, Qupa- ulakajik, Albuen, Goniomyakløft, Astartekløft, Moskus- oksekløft, Harris Fjeld, Primulaelv, Lepidopteriselv, Liaselv, Horsedal and Ranunkeldal (Fig. 1). A number of samples collected by Claus Heinberg and Tove Birke- lund in 1974 from Lepidopteriselv were also included in the study. The samples were processed for their palynological content using the techniques adopted at the former Geological Survey of Greenland, as described by Nøhr-Hansen (1993). Over 210 samples were analysed for their palynological content by means of a trans- mission light microscope. Two hundred specimens were counted in each sample and all species were registered in the range chart programme SIS and on the video database at the Geological Survey of Denmark and Greenland, where the slides are stored. 727 728 285 280 275 405427 405426 265 270 405425 405424 341235 260 255 405423 341234 405422 M Si Pb Sand 290 m 405430 Bisaccate pollen dominate405429 341236 405428 St ac ke d tid al c ha nn el s St ac ke d tid al c ha nn el s El is B je rg M em be r A lb ue n M em be r A Z 4 A ss em bl ag e Z on e 3 L at e Pl ie ns ba ch ia n SB4 W av e- a nd st or m -d om . sh or ef ac e Cerebropollenites thiergartii becomes rare M Si Pb Sand 210 215 220 405403 405402 405401 225 230 405410 405405 405404 405406 341232 405408 235 240 405417 405416 405414 405413 405411 250 m 245 405421 405420 405419 405418 341233 R es tr ic te d s he lf Su bt id al s an d sh ee t Su bt id al s an d sh ee t St ac ke d tid al c ha nn el s W av e- a nd st or m -d om . sh or ef ac e El is B je rg M em be r A ss em bl ag e Z on e 1 ?E ar ly P lie ns ba ch ia n A ss em bl ag e Z on e 2 A ss em bl ag e Z on e 3 La te P lie ns ba ch ia n SB3 Dinoflagellate cysts disappear Kekryphalospora distincta Nannoceratopsis senex and Limbicysta bjaerkei Abundant Botryococcus and bisaccate pollen Common Lycopodiacidites rugulatus Mancodinium semitabulatum Parvocysta barbata Albuen (A) 729 Mudstone Sandstone Pebbly sandstone Coal Volcanic intrusive Concretion Siderised rip-up mudstone clasts/conglomerate Sharp/erosive or irregular Sharp/planar Gradational Parallel lamination Lenticular bedding Wavy bedding Sedimentary features Bed contacts Flaser bedding Planar cross-bedding Trough cross-bedding Cross-lamination Incipient wave ripple lamination Wave ripple cross-lamination Hummocky and swaley cross-stratification Coarse-grained ripples Biota Structureless Structureless (with quartzite pebbles) Rootlets Plant fragments Drifted plant stems/logs Bivalves Echinoderms Belemnites Weak Moderate bioturbation Intense Arenicolites isp. Diplocraterion parallelum Gyrochorte comosa Ophiomorpha nodosa Phoebichnus trochoides Monocraterion isp. Helminthopsis isp. Planolites beverleyensis Taenidium serpentinum Trace fossils Cone-in-cone structures Thalassinoides isp. Unidentified sinuous horizontal burrow Teichichnus isp. Legend to sedimentary logs Lithology Conglomerate (qz, quartzite clasts) Slumping Cross-bedding with pebbles along foresets Gastropods Ammonites Brachiopods Crinoids Curvolithos multiplex Fig. 3A–C. Sedimentological logs through the Gule Horn (A, B) and Ostreaelv (B, C) Formations, Neill Klinter Group, at Albuen (for location, see Fig. 1); the Gule Horn Formation comprises the Elis Bjerg and Albuen Members, the Ostreaelv Formation is composed of the Astartekløft, Nathorst Fjeld, Skævdal and Trefjord Bjerg Members. Sequence boundaries (SB3–7), palynomorph assemblage zones (AZ) and sample numbers are indicated. The legend accompanying this figure is also applicable to Figs 5, 7, 9 and 15. 730 M Si Pb Sand 315 320 SB5 325 330 335 340 345 350 355 360 m A st ar te kl øf t M em be r Ea rl y T oa rc ia n N at ho rs t Fj el d M em be r T id al c ha nn el T id al c ha nn el Su bt id al s an d sh ee t St or m -d om in at ed sa nd y sh oa l M Si Pb Sand 287 290 295 305 310 315 m 405434 Few palynomorphs 405433 341239 Poor assemblage – only bisaccate pollen 405432 405431 405430 405429 341236 405428 A lb ue n M em be r A ss em bl ag e Z on e 4 La te P lie ns ba ch ia n St or m -d om in at ed o ffs ho re t ra ns iti on SB5 Bisaccate pollen abundant Botryococcus disappears Intrusion A Z 5 405466 Albuen (B) 731 Sk æ vd al M em be r A ss em bl ag e Z on e 6 A Z 7 La te T oa rc ia n Ea rl y A al en ia n T re fjo rd B je rg M em be r So rt eh at Fm Drowning surface 440 m 430 435 420 425 410 415 400 405 390 395 M Si Pb Sand Su bt id al s an d sh ee t Bi ot ur ba te d sh el f SB6 SB7 341248 397452 405449 341247 405450 405451 405452 405453 405454 405455 405456 Nannoceratopsis gracilis abundant P. halosa common Botryococcus reappear Callialasporites dampieri Pareodinia halosa ? M Si Pb Sand 390 m 380 375 385 370 365 360 R es tr ic te d sh el f Sh or ef ac e N at ho rs t Fj el d M em be r Ea rl y T oa rc ia n A ss em bl ag e Z on e 5 A ss em bl ag e Z on e 6 A st ar te kl øf t M em be r 405457 341243 405458 405459 341245 405460 405462 405464 405466 341241 Perinopollenites elatoides acme Drowning surface K. reissingerii S. subgranulatus rare S. subgranulatus abundant Cerebropollenites macroverrucosus becomes abundant Dinoflagellates reappear N. senex Luehndea spinosa Spheripollenites subgranulatus abundant qz Albuen (C) Palynological zones: definition Nine assemblage zones have been recognised in the Neill Klinter Group. The zones are based on the com- position of the entire assemblage of spores, pollen, dinoflagellate cysts, acritarchs and freshwater algae. The assemblage zones are numbered 1–9 and named after the species which dominate the assemblages. Assemblage Zones 1–6 are defined and described in detail in this paper, together with a brief description of Assemblage Zone 7. Assemblage Zones 7–9 are formally defined in the accompanying paper on the Sortehat Formation (Koppelhus & Hansen 2003, this volume). The recorded taxa are listed in full in Appendix 1 and the important species are illustrated in Plates 1–7. The most complete section was sampled at Albuen (Figs 1, 3); approximately 70 samples were analysed for palynomorphs from this section (Fig. 4, facing page 744). These samples yielded rich though not very well- preserved palynomorph assemblages (Plates 1–7), with the exception of samples taken close to the Palaeogene sills and dykes that penetrate the sedimentary succes- sion. These samples were either barren or the paly- nomorphs present were so dark as to be indeterminate. From the productive samples, approximately 150 species of spores, pollen, dinoflagellate cysts, acritarchs and freshwater algae were identified (Appendix 1). The intensively sampled Albuen section forms the reference section for Assemblage Zones 1–6 defined in this paper; Assemblage Zones 7–9 are defined from the borehole at Sortehat (Fig. 1; Koppelhus & Hansen 2003, this vol- ume). In addition to the Albuen reference section, important data for the definition of the assemblage zones were obtained from Ranunkeldal, Goniomyakløft and Astartekløft (Fig. 1). In addition to the formal assemblage zones defined here, a distinctive palynological assemblage was iden- tified in samples from the Horsedal Member of the Ostreaelv Formation at Horsedal. This assemblage is defined as the Deltoidospora Assemblage (see below under the Horsedal locality). Assemblage Zone 1: Cerebropollenites thiergartii – Pinuspollenites minimus – Botryococcus new assemblage zone Occurrence. Albuen 211–222.5 m Goniomyakløft 226.5 m (single sample) Primulaelv 310 m (single sample) Rævekløft 118–122 m Ranunkeldal 306–352.5 m This assemblage zone was recorded from the Rævekløft Formation at Rævekløft and Goniomyakløft and from the Elis Bjerg Member (Gule Horn Formation) at Albuen, Primulaelv and Ranunkeldal. Relative to the sequence stratigraphic scheme of Dam & Surlyk (1995, 1998), the assemblage occurs within sequences SQ1 and SQ2 (see Fig. 17). Reference section. Albuen, 211 m (sample 405401) – 222.5 m (sample 405404; Figs 1–4). Additional section. Ranunkeldal, 306 m (sample 341171) – 352.5 m (sample 341173; Figs 5, 6). Base. The base is not seen in the reference section at Albuen (Figs 3A, 4). At Ranunkeldal, the base of the zone is placed at sample 341171, immediately above the base of the Neill Klinter Group (Figs 5, 6); samples from the underlying Kap Stewart Group are considered to represent a different assemblage but further work is required to precisely define the base of Assemblage Zone 1. Top. The top of the zone is defined by the last sample showing this assemblage (sample 405404 at 222.5 m at Albuen) beneath the first appearance of Nannoceratopsis senex and N. sp. (Figs 3A, 4). Characteristics. Terrestrial palynomorphs (spores and pollen) dominate together with Botryococcus sp. The most common spores are Deltoidospora sp. and Baculatisporites sp., and the pollen is dominated by Cerebropollenites thiergartii and Pinuspollenites min- imus and other bisaccates. Other characteristic species are Cerebropollenites macroverrucosus, Chasmatosporites hians and C. major. No dinoflagellate cysts have been determined with certainty, but a few acritarchs were iden- tified. The freshwater alga Botryococcus sp. occurs in abundance. Suggested age. An Early Pliensbachian age is proposed based on the presence of abundant Cerebropollenites thiergartii. Palaeoenvironment. The assemblage records a strong terrestrial signal, most components being indicative of freshwater to brackish conditions. Botryococcus, for 732 733 M PbSi Sand M PbSi Sand 285 290 295 341168 341167 341169 300 305 310 315 320 325 m 341171 341170 341172 330 335 340 345 350 355 360 m 341173 O pe n la cu st ri ne St or m -d om in at ed o ffs ho re t ra ns iti on K ap S te w ar t G ro up W av e- a nd s to rm -d om in at ed s ho re fa ce El is B je rg M em be r (G ul e H or n Fm ) El is B je rg M em be r A ss em bl ag e Z on e 1 A ss em bl ag e no t de fin ed A ss em bl ag e Z on e 1 T id al c ha nn el Ranunkeldal SB1 qz Fig. 5. Sedimentological log through the uppermost part of the Kap Stewart Group and the Elis Bjerg Member (Gule Horn Formation) of the Neill Klinter Group in Ranunkeldal (for location, see Fig. 1). Sequence boundary (SB1), palynomorph Assemblage Zone 1 and sample numbers are indicated. For legend, see Fig. 3; arrows denote grain- size trends. 734 R an un ke ld al System Lower Jurassic Stage Lithostratigraphy Kap Stewart Group Not defined Lower Pliensbachian Gule Horn Formation Elis Bjerg Member Sinemurian Palynological Assembl. Zones (m) 35 0 34 0 30 0 29 0 31 0 32 0 Sample height 35 2. 50 31 1. 00 30 6. 00 29 9. 00 29 3. 00 28 9. 00 28 5. 00 Sample number 34 11 73 34 11 72 34 11 71 34 11 70 34 11 69 34 11 68 34 11 67 1Trilete sp. 2Ischyosporites variegatus 3Striatella parva 4Retitriletes clavatoides 5Retitriletes sp. 6Deltoidospora spp. 7Baculatisporites sp. 8Tripartina variabilis 9Ischyosporites sp. 10Conbaculatisporites mesozoicus 11Retitriletes semimuris 12Lycopodiacidites rugulatus 13Rogalskaisporites cicatricosus 14Manumia delcourtii 15Calamospora tener 16Retitriletes austroclavatoides 17Cibotiumsporites jurienensis 18Megaspore spp. 19Densoisporites scanicus 20Striatella jurassica 21Densosporites variabilis 22Kekryphalospora distincta 23Sestrosporites pseudoalveolatus 24Chasmatosporites major 25Bisaccate spp. 26Cerebropollenites thiergartii 27Pinuspollenites minimus 28Chasmatosporites apertus 29Corollina torosus 30Chasmatosporites hians 31Perinopollenites elatoides 32Quadraeculina anellaeformis 33Cerebropollenites macroverrucosus 34Ricciisporites tuberculatus 35Vesicaspora fuscus 36Vittatina sp. 37Araucariacites australis 38Ovalipollis ovalis 39Dinocyst sp. 40Nannoceratopsis gracilis 41Veryhachium spp. 42Veryhachium reductum 43Acritarch spp. 44Leiofusa jurassica 45Micrhystridium exilium 46Leiosphaeridia spp. 47Micrhystridium lymensis 48Botryococcus spp. 49Tasmanites sp. 50Foraminifera spp. R ? ? R ? R ? A lp ha be tic al s pe ci es li st 43 A cr ita rc h sp p. 37 A ra u ca ri a ci te s a u st ra lis 7 B a cu la ti sp or it es s p. 25 Bi sa cc at e sp p. 48 B ot ry oc oc cu s sp p. 15 C a la m os p or a t en er 33 C er eb ro p ol le n it es m a cr ov er ru co su s 26 C er eb ro p ol le n it es t h ie rg a rt ii 28 C h a sm a to sp or it es a p er tu s 30 C h a sm a to sp or it es h ia n s 24 C h a sm a to sp or it es m a jo r 17 C ib ot iu m sp or it es j u ri en en si s 10 C on b a cu la ti sp or it es m es oz oi cu s 29 C or ol lin a t or os u s 6 D el to id os p or a s pp . 19 D en so is p or it es s ca n ic u s 21 D en so sp or it es v a ri a b ili s 39 D in oc ys t sp . 50 Fo ra m in ife ra s pp . 9 Is ch yo sp or it es s p. 2 Is ch yo sp or it es v a ri eg a tu s 22 K ek ry p h a lo sp or a d is ti n ct a 44 Le io fu sa j u ra ss ic a 46 Le io sp h a er id ia s pp . 12 Ly co p od ia ci d it es r u gu la tu s 14 M a n u m ia d el co u rt ii 18 M eg as po re s pp . 45 M ic rh ys tr id iu m e xi liu m 47 M ic rh ys tr id iu m l ym en si s 40 N a n n oc er a to p si s gr a ci lis 38 O va lip ol lis o va lis 31 Pe ri n op ol le n it es e la to id es 27 Pi n u sp ol le n it es m in im u s 32 Q u a d ra ec u lin a a n el la ef or m is 16 R et it ri le te s a u st ro cl a va to id es 4 R et it ri le te s cl a va to id es 11 R et it ri le te s se m im u ri s 5 R et it ri le te s sp . 34 R ic ci is p or it es t u b er cu la tu s 13 R og a ls k a is p or it es c ic a tr ic os u s 23 S es tr os p or it es p se u d oa lv eo la tu s 20 S tr ia te lla j u ra ss ic a 3 S tr ia te lla p a rv a 49 Ta sm a n it es s p. 1 Tr ile te s p. 8 Tr ip a rt in a v a ri a b ili s 42 Ve ry h a ch iu m r ed u ct u m 41 Ve ry h a ch iu m s pp . 35 Ve si ca sp or a f u sc u s 36 V it ta ti n a s p. In te rv al n ot s am pl ed 1 Fi g. 6 . P al yn o m o rp h d is tr ib u tio n c h ar t fo r th e u p p er m o st p ar t o f th e K ap S te w ar t G ro u p a n d t h e E lis B je rg M em b er ( G u le H o rn F o rm at io n ) o f th e N ei ll K lin te r G ro u p i n R an u n ke ld al (f o r lo ca tio n , se e Fi g. 1 ). F o r le ge n d , se e Fi g. 4 . example, is a planktonic green alga that occurs in colonies. It is known to adapt to different aquatic envi- ronments (fresh to brackish water), has been recorded from tropical to subarctic regions and has a stratigraphic range from the Precambrian to the present day (Guy-Ohlson 1992). When large numbers of Botry- ococcus are recorded, it indicates that the depositional environment was strongly influenced by fresh or brack- ish waters (Guy-Ohlson 1992). Remarks. Assemblage Zone 1 is equivalent to As- semblage Zone A of Lund & Pedersen (1985), and prob- ably to the lower part of section 3 of Underhill & Partington (1994). The assemblage is similar but not identical to that described from the Chasmatosporites Zone (miospore) and the Mendicodinium reticulatum Zone (dinoflagellate) from the successions of Bornholm and the Øresund area (Koppelhus & Nielsen 1994; Koppelhus & Batten 1996). Assemblage Zone 2: Nannoceratopsis–Botryococcus new assemblage zone Occurrence. Albuen 229–241 m Goniomyakløft 229.8–235 m Lepidopteriselv 638–654 m Liaselv 293–325 m Rævekløft 208–210 m This assemblage zone is characteristic of the Elis Bjerg Member of the Gule Horn Formation where it typically occurs within sequence SQ3 of Dam & Surlyk (1995, 1998), for example at Albuen (Figs 3A, 4), Lepidopteris- elv, Liaselv and Rævekløft. At Goniomyakløft, however, Assemblage Zone 2 was identified in the uppermost Rævekløft Formation and the lowermost Elis Bjerg Member (Figs 7, 8), within sequence SQ2 of Dam & Surlyk (1995, 1998). Reference section. Albuen, 229 m (sample 405405) – 241 m (sample 405417; Figs 3A, 4). Additional section. Goniomyakløft, 229.8 m (sample 405469) – 235 m (sample 405471; Figs 7, 8). Base. The base of the zone is defined by the sample showing the first appearance of Nannoceratopsis senex and N. sp. Top. The top of the zone is defined by the last sample showing this palynomorph assemblage, above which Nannoceratopsis disappears together with most other dinoflagellate cysts. 735 240 245 m M Si Pb Sand 225 230 235 405471 405470 405469 405468 405467 Drowning surface Goniomyakløft St or m -d om in at ed sa nd y sh oa l Su bt id al s an d sh ee t R es tr ic te d sh el f U pp er s ho re fa ce R æ ve kl øf t Fo rm at io n El is B je rg M em be r A ss em bl ag e Z on e 2 G ul e H or n Fo rm at io n SB3 AZ1 Fig. 7. Sedimentological log through the uppermost part of the Rævekløft Formation and the Elis Bjerg Member (Gule Horn Formation) at Goniomyakløft (for location, see Fig. 1). Sequence boundary (SB3), palynomorph assemblage zones (AZ) and sam- ple numbers are indicated. For legend, see Fig. 3. Note that the exact location of sample 405467 is uncertain due to imprecise field records; although here placed immediately beneath the non- exposed interval (226.5–227.8 m), it is possible that it derives from immediately above this interval. For legend, see Fig. 3. 736 G on io m ya kl øf t Lower Pliensbachian Rævekløft Formation Lower Jurassic 23 5. 00 23 4. 50 23 2. 40 22 9. 80 22 6. 50 40 54 71 40 54 70 40 54 69 40 54 68 40 54 67 1Kekryphalospora distincta 2Retitriletes semimuris 3Retitriletes austroclavatoides 4Stereisporites stereoides 5Lycopodiacidites rugulatus 6Baculatisporites sp. 7Deltoidospora spp. 8Densoisporites velatus 9Staplinisporites caminus 10Retitriletes clavatoides 11Striatella seebergensis 12Leptolepidites sp. 13Densoisporites scanicus 14Retitriletes sp. 15Foraminisporis jurassicus 16Tigrisporites microrugulatus 17Striatella scanica 18Rogalskaisporites cicatricosus 19Neoraistrickia gristhorpensis 20Megaspore spp. 21Striatella jurassica 22Todisporites major 23Cibotiumsporites jurienensis 24Neoraistrickia sp. 25Corollina torosus 26Quadraeculina anellaeformis 27Chasmatosporites apertus 28Perinopollenites elatoides 29Bisaccate spp. 30Cerebropollenites thiergartii 31Chasmatosporites hians 32Cerebropollenites macroverrucosus 33Chasmatosporites minor 34Pinuspollenites minimus 35Chasmatosporites major 36Corollina sp. 37Callialasporites sp. 38Dapcodinium sp. 39Mancodinium semitabulatum 40Dinocyst spp. 41Nannoceratopsis sp. 42Crassosphaera spp. 43Acritarch spp. 44Tasmanites sp. 45Botryococcus spp. 46Foraminiferal linings 47Foraminifera spp. ? ? ? ? ? ? ? ? A lp ha be tic al s pe ci es li st 43 A cr ita rc h sp p. 6 B a cu la ti sp or it es s p. 29 Bi sa cc at e sp p. 45 B ot ry oc oc cu s sp p. 37 C a lli a la sp or it es s p. 32 C er eb ro p ol le n it es m a cr ov er ru co su s 30 C er eb ro p ol le n it es t h ie rg a rt ii 27 C h a sm a to sp or it es a p er tu s 31 C h a sm a to sp or it es h ia n s 35 C h a sm a to sp or it es m a jo r 33 C h a sm a to sp or it es m in or 23 C ib ot iu m sp or it es j u ri en en si s 36 C or ol lin a s p. 25 C or ol lin a t or os u s 42 C ra ss os p h a er a s p. 38 D a p co d in iu m s p. 7 D el to id os p or a s pp . 8 D en so is p or it es v el a tu s 13 D en so is p or it es s ca n ic u s 40 D in oc ys t sp p. 46 Fo ra m in ife ra l l in in gs 47 Fo ra m in ife ra s pp . 15 Fo ra m in is p or is j u ra ss ic u s 1 K ek ry p h a lo sp or a d is ti n ct a 12 Le p to le p id it es s p. 5 Ly co p od ia ci d it es r u gu la tu s 39 M a n co d in iu m s em it a b u la tu m 20 M eg as po re s pp . 41 N a n n oc er a to p si s sp . 19 N eo ra is tr ic k ia gr is t h or p en si s 24 N eo ra is tr ic k ia s p. 28 Pe ri n op ol le n it es e la to id es 34 Pi n u sp ol le n it es m in im u s 26 Q u a d ra ec u lin a a n el la ef or m is 3 R et it ri le te s a u st ro cl a va to id es 10 R et it ri le te s cl a va to id es 2 R et it ri le te s se m im u ri s 14 R et it ri le te s sp . 18 R og a ls k a is p or it es c ic a tr ic os u s 9 S ta p lin is p or it es c a m in u s 4 S te re is p or it es s te re oi d es 21 S tr ia te lla j u ra ss ic a 17 S tr ia te lla s ca n ic a 11 S tr ia te lla s ee b er ge n si s 44 Ta sm a n it es s p. 16 T ig ri sp or it es m ic ro ru gu la tu s 22 To d is p or it es m a jo r System Stage Palynological Assembl. Zones Lithostratigraphy Elis Bjerg Mb Upper Pliensbach. (m) Sample height Sample number 22 5 23 5 21 5 20 5 12 Fi g. 8 . P al yn o m o rp h d is tr ib u tio n c h ar t fo r th e u p p er m o st p ar t o f th e R æ ve kl ø ft F o rm at io n a n d t h e E lis B je rg M em b er ( G u le H o rn F o rm at io n ) at G o n io m ya kl ø ft ( fo r lo ca tio n , se e Fi g. 1 ). Fo r le ge n d , se e Fi g. 4 . Characteristics. Terrestrial palynomorphs dominate the assemblage together with Botryococcus sp., as in Assemblage Zone 1; the spore Kekryphalospora dis- tincta appears for the first time. The difference between this assemblage and that of Assemblage Zone 1 is the appearance of dinoflagellate cysts, including Manco- dinium semitabulatum, Nannoceratopsis senex, N. gra- cilis, N. plegas, N. triangulata and Parvocysta barbata and the presence of more acritarchs, including Limbicysta bjaerkei. Suggested age. A Late Pliensbachian age is suggested based on the first appearance of the spore Kekry- phalospora distincta in sample 405411 (236.50 m) in the Albuen section (Fig. 3A); this species is known to have a range from Late Pliensbachian to Early Bajocian (Fenton & Riding 1987). Palaeoenvironment. Although influenced by brackish to marine waters, there is still a strong terrestrial signal. Remarks. The spore Kekryphalospora distincta is also known from assemblages of Pliensbachian age from the Danish area (Anholt borehole, Øresund borehole 15 and the Korsodde section on Bornholm; Seidenkrantz et al. 1993; Koppelhus & Nielsen 1994; Koppelhus & Batten 1996). The appearance of Nannoceratopsis tri- angulata is particularly noteworthy as this species has previously only been recorded from NW Germany where it occurs in the uppermost Toarcian (Prauss 1987). The appearance of Limbicysta bjaerkei and Parvocysta barbata is unexpected at this level, as they are known to have their first appearance in the Bifrons Zone (late Early Toarcian) in the North Sea and Svalbard and on the mid-Norwegian shelf (Bjærke 1980a; Riding & Thomas 1992; I. Throndsen, personal communication 1996). However, these anomalous occurrences were also recognised at this level in the Neill Klinter Group by Underhill & Partington (1994); L. bjaerkei was recorded in their section 3 between 360 m and 370 m. Two explanations are possible: either P. barbata and L. bjaerkei have a longer range than recently reported or the sediments are younger than expected. In Assemblage Zone 2, acritarchs are more common than in the underlying zone and in the succeeding zones; this pattern is known from the Lower Jurassic in England and Wales (Wall 1965). Assemblage Zone 3: Chasmatosporites – Cerebropollenites thiergartii – Botryococcus new assemblage zone Occurrence. Albuen 246–284.7 m Astartekløft 266–328 m Lepidopteriselv 674–700 m Assemblage Zone 3 is confined to the uppermost part of the Elis Bjerg Member (Gule Horn Formation) in the Albuen and Lepidopteriselv sections; relative to the sequence stratigraphic scheme of Dam & Surlyk (1995, 1998), the assemblage occurs within the upper levels of sequence SQ3, below sequence boundary SB4 in these sections (Fig. 3A). At Astartekløft, however, the assemblage spans the boundary between the Elis Bjerg Member and the succeeding Albuen Member, thus strad- dling the sequence boundary (SB4) between sequences SQ3 and SQ4 (Fig. 10). It should be noted, however, that recognition of assemblage Zone 3 is based on only two widely spaced samples at the Astartekløft locality (Fig. 10). Reference section. Albuen, 246 m (sample 405418) – 284.7 m (sample 405427; Figs 3A, 4). Additional section. Astartekløft, 266 m (sample 346614) – 328 m (sample 346627; Fig. 10) Base. The base is placed at the first sample in which dinoflagellate cysts are absent or rare, succeeding sam- ples of Assemblage Zone 2 characterised by a number of dinoflagellate species. Top. The top of the assemblage is placed at the last sam- ple showing the assemblage described below; above this level, the palynomorph assemblage is dominated by bisaccate pollen. Characteristics. This zone is also dominated by terres- trial material. A number of spores have their first appear- ance, such as Striatella jurassica, Kraeuselisporites reissingeri, Taurocusporites verrucatus and Densoi- sporites velatus. The pollen species and Botryococcus sp. are very consistent; only few dinoflagellate cysts and acritarchs were recorded. Suggested age. A Late Pliensbachian age is proposed based on the absence of marker species indicative of 737 a younger age. The miospore assemblage is a contin- uation of Assemblage Zone 2. Palaeoenvironment. The palynology displays an over- whelmingly terrestrial signal; there is very little evi- dence of marine influence. Remarks. Cerebropollenites thiergartii is common through much of the zone but becomes rare towards the top of the zone and in succeeding zones. Assemblage Zone 4: Bisaccates new assemblage zone Occurrence. Albuen 287–297.8 m Astartekløft 339–340 m This assemblage zone is restricted to the Albuen Member (Gule Horn Formation) at both Albuen and Astartekløft (Figs 3A, 3B, 4, 9, 10); it thus falls within sequence SQ4 of Dam & Surlyk (1995, 1998). Reference section. Albuen, 287 m (sample 405428) – 297.8 m (sample 405434; Figs 3A, 3B, 4). Additional section. Astartekløft, 339 m (sample 405472) – 340 m (sample 405473; Figs 9, 10). Base. The base is defined by the first sample domi- nated overwhelmingly by bisaccate pollen, to the exclu- sion of most other palynomorphs. Top. The top of the zone is defined by the last sample composed predominantly of bisaccate pollen; the suc- ceeding sample, defining the base of the overlying Assemblage Zone 5, is characterised by the first appear- ance of Spheripollenites subgranulatus. Characteristics. This assemblage zone is characterised by very poor preservation of the few palynomorphs present and by the absence of marine palynomorphs. Bisaccate pollen are common in most of the samples. The spores, pollen and Botryococcus sp. that were abundant in the Assemblage Zones 1–3 are absent in this zone. Suggested age. A Late Pliensbachian age is assigned to this zone, as for Assemblage Zone 3 (see above). Palaeoenvironment. Taken at face value, the palyno- morph data suggest that the sediments of the Albuen Member were deposited in a more distal position rel- ative to the source than that suggested by the previous assemblage zones. Amongst all palynomorphs, bisac- cate pollen are known to be found farthest away from the source, because of their ability to be transported by air. However, bisaccate pollen are also known to have a thick wall and therefore may be preferentially pre- served. Thus, although lack of marine palynomorphs could be interpreted in terms of a non-marine envi- ronment, it could also have resulted from selective destruction of the more thin-walled marine paly- nomorphs during intrusion of Palaeogene igneous sills and dykes in the Albuen Member. Remarks. This interval was not recognised in previous studies by Lund & Pedersen (1985) and Underhill & Partington (1994). Assemblage Zone 5: Spheripollenites subgranulatus – Cerebropollenites macroverrucosus – Luehndea spinosa new assemblage zone Occurrence. Albuen 359–375.5 m Astartekløft 341–383 m Moskusoksekløft 359 m (single sample) Primulaelv 451 m (single sample) In the Albuen reference section, Assemblage Zone 5 was only recorded from the lower Nathorst Fjeld Member of the Ostreaelv Formation; it should be noted that the underlying Astartekløft Member (also Ostreaelv For- mation) was not sampled in this section so the potential downwards range of the assemblage is poorly con- strained (Figs 3B, 3C, 4). At Astartekløft itself, however, Assemblage Zone 5 extends from the lowermost Astartekløft Member up into the Nathorst Fjeld Member (Figs 9, 10). Relative to the sequence stratigraphic scheme of Dam & Surlyk (1995, 1998), Assemblage Zone 5 occurs within sequence SQ5, beginning imme- diately above the sequence boundary (SB5) in the Astartekløft section (Fig. 9) and extending up to some 10 m beneath the flooding surface at Albuen (Fig. 3C). Reference section. Albuen, 359 m (sample 405466) – 375.5 m (sample 405458; Figs 3B, 3C, 4). 738 739 M Si Pb Sand 335 345 355 365 m 375 Drowning surface SB5 M Si Pb Sand 385 m qz qz R es tr ic te d sh el f Sh or ef ac e Astartekløft Su bt id al s an d sh ee t N at ho rs t Fj el d M em be r A st ar te kl øf t M em be r A ss em bl ag e Z on e 5 A Z 4 A ss em bl ag e Z on e 5 A lb ue n M em be r 341270 341269 405472 405473 405474 405475 405476 405477 405478 405483 405479 Fig. 9. Sedimentological log through the upper- most Albuen Member (Gule Horn Formation) and the Astartekløft and Nathorst Fjeld Members (Ostreaelv Formation) at Astartekløft (for location, see Fig. 1). Sequence boundary (SB5), palynomorph assemblage zones (AZ) and sample numbers are indicated. For legend, see Fig. 3. 740 A st ar te kl ø ft Lower Jurassic Toarcian Ostreaelv Formation Astartekløft MemberNathorst Fjeld Member Upper Pliensbachian Gule Horn Formation Elis Bjerg MemberAlbuen Member 38 3. 00 37 2. 00 34 9. 00 34 5. 00 34 2. 00 34 1. 50 34 1. 00 34 0. 00 33 9. 00 32 8. 00 26 6. 00 34 12 70 34 12 69 40 54 79 40 54 77 40 54 76 40 54 75 40 54 74 40 54 73 40 54 72 34 66 27 34 66 14 1Stereisporites stereoides 2Densoisporites velatus 3Retitriletes austroclavatoides 4Conbaculatisporites mesozoicus 5Calamospora tener 6Lycopodiacidites rugulatus 7Baculatisporites sp. 8Deltoidospora spp. 9Chomotriletes sp. 10Rogalskaisporites cicatricosus 11Kraeuselisporites reissingerii 12Retitriletes sp. 13Triletes sp. 14Striatella jurassica 15Ischyosporites variegatus 16Foraminisporis jurassicus 17Kekryphalospora distincta 18Manumiadel courtii 19Leptolepidites sp. 20Striatella seebergensis 21Cingulizonates inequalis 22Cerebropollenites thiergartii 23Chasmatosporites hians 24Quadraeculina anellaeformis 25Corollina torosus 26Chasmatosporites major 27Perinopollenites elatoides 28Bisaccate spp. 29Pinuspollenites minimus 30Chasmatosporites apertus 31Vesicaspora fuscus 32Spheripollenites subgranulatus 33Cerebropollenites macroverrucosus 34Chasmatosporites sp. 35Corollina meyeriana 36Striate spp. 37Taeniasporites rhaeticus 38Nannoceratopsis senex 39Nannoceratopsis plegas 40Mancodinium semitabulatum 41Nannoceratopsis gracilis 42Nannoceratopsis triangulata 43Mendicodinium reticulatum 44Kallosphaeridium sp. 45Nannoceratopsis triceras 46Leiosphaeridia spp. 47Micrhystridium spp. 48Botryococcus spp. ? R R R A lp ha be tic al s pe ci es li st 7 B a cu la ti sp or it es s p. 28 Bi sa cc at e sp p. 48 B ot ry oc oc cu s sp p. 5 C a la m os p or a t en er 33 C er eb ro p ol le n it es m a cr ov er ru co su s 22 C er eb ro p ol le n it es t h ie rg a rt ii 30 C h a sm a to sp or it es a p er tu s 23 C h a sm a to sp or it es h ia n s 26 C h a sm a to sp or it es m a jo r 34 C h a sm a to sp or it es s p. 9 C h om ot ri le te s sp . 21 C in gu liz on a te s in eq u a lis 4 C on b a cu la ti sp or it es m es oz oi cu s 35 C or ol lin a m ey er ia n a 25 C or ol lin a t or os u s 8 D el to id os p or a s pp . 2 D en so is p or it es v el a tu s 16 Fo ra m in is p or is j u ra ss ic u s 15 Is ch yo sp or it es v a ri eg a tu s 44 K a llo sp h a er id iu m s p. 17 K ek ry p h a lo sp or a d is ti n ct a 11 K ra eu se lis p or it es r ei ss in ge ri i 46 Le io sp h a er id ia s pp . 19 Le p to le p id it es s p. 6 Ly co p od ia ci d it es r u gu la tu s 40 M a n co d in iu m s em it a b u la tu m 18 M a n u m ia d el co u rt ii 43 M en d ic od in iu m r et ic u la tu m 47 M ic rh ys tr id iu m s pp . 39 N a n n oc er a to p si s p le ga s 41 N a n n oc er a to p si s gr a ci lis 38 N a n n oc er a to p si s se n ex 42 N a n n oc er a to p si s tr ia n gu la ta 45 N a n n oc er a to p si s tr ic er a s 27 Pe ri n op ol le n it es e la to id es 29 Pi n u sp ol le n it es m in im u s 24 Q u a d ra ec u lin a a n el la ef or m is 3 R et it ri le te s a u st ro cl a va to id es 12 R et it ri le te s sp . 10 R og a ls k a is p or it es c ic a tr ic os u s 32 S p h er ip ol le n it es s u b gr a n u la tu s 1 S te re is p or it es s te re oi d es 36 St ri at e sp p. 14 S tr ia te lla j u ra ss ic a 20 S tr ia te lla s ee b er ge n si s 37 Ta en ia sp or it es r h a et ic u s 13 Tr ile te s sp . 31 Ve si ca sp or a f u sc u s In te rv al n ot s am pl ed In te rv al n ot s am pl ed System Stage Palynological Assembl. Zones Stratigraphy (m) Sample height Sample number 26 5 27 0 32 5 33 0 33 5 34 0 34 5 35 0 37 5 38 0 37 0 45 3 U nc er ta in de te rm in at io n Ve ry r ar e R ar e Fe w C om m on A bu nd an t ? R Fi g. 1 0. P al yn o m o rp h d is tr ib u tio n c h ar t fo r th e E lis B je rg a n d A lb u en M em b er s (G u le H o rn F o rm at io n ) an d t h e A st ar te kl ø ft a n d N at h o rs t Fj el d M em b er s (O st re ae lv F o rm at io n ) at A st ar te kl ø ft ( fo r lo ca tio n , se e Fi g. 1 ). Additional section. Astartekløft, 341 m (sample 405474) – 383 m (sample 341270; Figs 9, 10). Base. The base of the assemblage is defined by the first appearance, in abundance, of Spheripollenites sub- granulatus; at Albuen, this coincides with the first appearance of Luehndea spinosa, although this species was not recorded in the Astartekløft section. Top. This is defined by the uppermost sample showing the palynomorph assemblage characteristic of the zone (i.e. sample 405458 at Albuen). The succeeding sample shows an acme of Perinopollenites elatoides, defining the base of Assemblage Zone 6. The top of the assemblage is not seen in the Astartekløft section (Fig. 9). Characteristics. In Assemblage Zone 5, the pollen Spheripollenites subgranulatus appears in abundance for the first time; this species was only recorded in one sample below this level, in sample 346627 at 328 m in the Astartekløft section (Figs 9, 10). The assemblage is also marked by the reappearance of abundant Nanno- ceratopsis senex and N. gracilis. The pollen Cerebro- pollenites macroverrucosus and to a lesser degree Corollina torosus are more common than in the under- lying assemblage. Spherical bodies of uncertain affin- ity are also abundant (on the distribution chart they are registered under micromiscellanea). Suggested age. An Early–Late Toarcian age is proposed based on the presence and acme of Spheripollenites subgranulatus which is known to be abundant in Toarcian strata in the Danish Basin and the North Sea (Dybkjær 1991; Batten et al. 1994; Koppelhus & Nielsen 1994; Koppelhus & Batten 1996). Palaeoenvironment. This assemblage contains elements indicative of both brackish and marine conditions. Remarks. In Germany, the North Sea area and the Danish Basin, the dinoflagellate cyst Luehndea spinosa is known to appear within the Margaritatus, Spinatus and Tenuicostatum Zones which span the Late Pliensbachian to Early Toarcian (Morgenroth 1970; Riding & Thomas 1992; Poulsen 1996). The abundant spherical bodies of unknown affinity are also known from Svalbard, the North Sea and the Baltic Sea in upper Pliensbachian and Toarcian strata (Bjærke 1980b; Dybkjær 1991; Koppelhus & Nielsen 1994); on the mid-Norway shelf, these forms are known to occur in Lower Toarcian strata (I. Throndsen, personal communication 1996). This zone correlates with Assemblage Zone B of Lund & Pedersen (1985). It has not been possible to recognise this assemblage in the data presented by Underhill & Partington (1994). Comparison with the Microcysta erugata taxa range-zone of Smelror & Below (1992) has been attempted, but the two zones have very few species in common. Assemblage Zone 6: Perinopollenites elatoides new assemblage zone Occurrence. Albuen 377.5–434 m Enhjørningen Dal 414–424.67 m Sortehat (core) 12.65–26.28 m In the Albuen section, Assemblage Zone 6 extends from the upper Nathorst Fjeld Member through the Skævdal Member and much of the Trefjord Bjerg Member (all Ostreaelv Formation; Figs 3C, 4). Relative to the sequence stratigraphic scheme of Dam & Surlyk (1995, 1998), the assemblage occurs within sequences SQ5 and SQ6, spanning the sequence boundary SB6 (Figs 3C, 4). Data for the Enhjørningen Dal and Sortehat sections is pre- sented in the companion paper by Koppelhus & Hansen (2003, this volume). In the Sortehat core, Assemblage Zone 6 is confined to the upper Ostreaelv Formation (Trefjord Bjerg Member); the top of the assemblage lies immediately beneath the boundary between the Ostreaelv and Sortehat Formations. At Enhjørningen Dal, however, Assemblage Zone 6 spans the boundary between these two formations, extending some 6 m up into the Sortehat Formation (Koppelhus & Hansen 2003, this volume). Reference section. Albuen, 377.5 m (sample 341243) – 434 m (sample 405449; Figs 3C, 4). Base. The base of the zone is placed at the sample in which Perinopollenites elatoides reaches its acme; it is accompanied by abundant Chasmatosporites hians and C. major. Top. The upper boundary of Assemblage Zone 6 is placed at the last sample showing the palynomorph assemblage described here; above this level, Botry- ococcus sp. becomes very dominant, defining the base of Assemblage Zone 7. 741 Characteristics. The zone is characterised particularly by the acme of Perinopollenites elatoides. The spores Staplinisporites caminus and Sestrosporites pseudoalveo- latus have their first appearance within the zone together with the dinoflagellate cysts Phallocysta eumekes, Wallodinium laganum, Scriniocassis sp. and Dissilio- dinium sp. The dinoflagellate cysts Nannoceratopsis gracilis and N. senex continue to be common in most of the samples. Botryococcus sp. re-appears at 392 m (sample 405456; Fig. 3C) and continues to be common to the top of this zone. Suggested age. A Late Toarcian – early Aalenian age is suggested based on the first appearances of the spores Staplinisporites caminus and Sestrosporites pseudoalveo- latus together with the dinoflagellate cysts Phallocysta eumekes, Wallodinium laganum, Scriniocassis sp. and Dissiliodinium sp. The occurrence of abundant Perino- pollenites elatoides is a feature of Aalenian sediments in the Danish Basin and on Bornholm (Dybkjær 1991; Koppelhus & Nielsen 1994). Palaeoenvironment. The palynomorphs indicate that the palaeoenvironment was influenced by both fresh, brackish and marine waters, suggesting a nearshore environment. Remarks. The two species Chasmatosporites hians and C. major are very abundant in the lowermost sample in this interval, higher up they become rare. In offshore mid-Norway, C. hians has a maximum appearance after the Spheripollenites acme (I. Throndsen, personal com- munication 1996). The pollen Callialasporites dampieri is known to appear in the uppermost Toarcian and lowermost Aalenian in north-west Scotland (Riding et al. 1991). This zone correlates with Assemblage Zone C in Lund & Pedersen (1985) and the assemblage found in sample B2/57 at approximately 460 m in Primulaelv by Underhill & Partington (1994). The dinoflagellate cyst Wallodinium laganum appears for the first time in this zone and is only known from the Late Toarcian Levesquei Zone in northern Germany and England (Feist-Burkhardt & Monteil 1994). The ammonite Dactylioceras sp. occurs at the base of the Skævdal Member at Nathorst Fjeld, suggesting an Early Toarcian Tenuicostatum Zone age for the lower part of the assem- blage zone. Assemblage Zone 7: Botryococcus This assemblage is formally defined in the companion paper by Koppelhus & Hansen (2003, this volume); a summary is given here. Occurrence. Albuen 438.5–443.5 m Enhjørningen Dal 424.86–445 m Pelion 550–567 m Sortehat (core) 27.82–36.36 m At Albuen, this assemblage is represented in the upper- most few metres of the Trefjord Member (Ostreaelv Formation) and extends up into the Sortehat Formation (Figs 3C, 4); additional data for the uppermost Trefjord Member and the overlying Sortehat Formation in the Albuen section are given in Koppelhus & Hansen (2003, this volume). In the cored section from Sortehat, the assemblage occurs in the lower levels of the Sortehat Formation, the base of the zone being immediately above the base of the formation (Koppelhus & Hansen 2003, this volume). At Enhjørningen Dal, Assemblage Zone 7 is also restricted to the lower Sortehat Formation although here the base is some 6 m above the lower boundary of the Sortehat Formation. Detailed discus- sion and the full dataset are given in Koppelhus & Hansen (2003, this volume). Assemblage Zone 7 occurs within the lower levels of sequence SQ7 of Dam & Surlyk (1995, 1998). Reference section. Sortehat (core), 27.82 m (sample 303143-73) – 36.36 m (sample 303143-62). Additional sections. See Koppelhus & Hansen (2003, this volume). Base. The base of the assemblage is placed at the first sample in which Botryococcus sp. overwhelmingly dom- inates the assemblage. In the Albuen section (Figs 3C, 4), this event coincides with the first co-occurrence of Callialasporites dampieri (pollen) and Mendicodinium groenlandicum (dinoflagellate cyst) although in other sections (e.g. Enhjørningen Dal, Sortehat; Koppelhus & Hansen 2003, this volume) these species first occur together some metres below the Botryococcus sp. influx. Top. The upper boundary is defined by the uppermost sample showing the Botryococcus-dominated assem- blage. Above this level, Botryococcus sp. disappear and Nannoceratopsis gracilis and N. senex become abundant once more. 742 Characteristics. The assemblage is characterised by the overwhelming dominance of Botryococcus sp. and the scarcity of dinoflagellates. Suggested age. An Aalenian age is proposed based on the abundance of Callialasporites dampieri. Pollen from the genus Callialasporites are known to appear first in sediments of Late Toarcian and Aalenian age in Sweden and the Danish area (Guy-Ohlson 1988; Koppelhus & Nielsen 1994). Palaeoenvironment. The fresh and brackish water alga Botryococcus is known from recent environments to produce blooms at certain times of the year. The colonies float at the water surface under calm conditions and sub- sequently sink when the water is disturbed. When they die, they float within the surface waters and can be transported by wind far from the area where they were produced. Palaeoenvironmental interpretation based solely on the presence of Botryococcus is therefore dan- gerous; the degree to which the Botryococcus in this succession is allochthonous is unknown. Further dis- cussion of the environmental implications of this assem- blage is given by Koppelhus & Hansen (2003, this volume). Additional palynological results As noted earlier, definition of the six assemblage zones described here is based primarily on the section at Albuen, the palynostratigraphy of which is thus pre- sented in detail above. In addition to this reference sec- tion, however, a series of other sections were included in the study, some of which yield important supple- mentary data for the definition of the assemblage zones (see above). The palynostratigraphic results from these additional localities, spread widely in the Jameson Land Basin (Fig. 1), are described below, broadly from south to north. Rævekløft At Rævekløft, nine samples were collected, six from the Rævekløft Formation (405435–405440) and three from the Elis Bjerg Member (Gule Horn Formation, 405441–405443; Fig. 11). The samples collected from the Rævekløft Formation are separated by a gap of c. 100 m from those collected in the Elis Bjerg Member and the boundary between the two units was not exposed. All the samples yielded abundant poorly pre- served palynomorphs. Terrestrial material dominates together with the freshwater alga Botryococcus sp. Bisaccate pollen are the most abundant palynomorphs in all the samples. A few acritarchs and questionable dinoflagellate cysts were found. Based on the presence of the spores Deltoidospora and Baculatisporites, the pollen Cerebropollenites thiergartii and Pinuspollenites minimus and the lack of dinoflagellate cysts, the sam- ples 405435–405440 (?upper Rævekløft Formation) are assigned to Assemblage Zone 1. In the samples 405441–405443 (Elis Bjerg Member), the dinoflagellate cysts Nannoceratopsis senex and Mancodinium semi- tabulatum appear for the first time, indicating that the assemblage belongs to Assemblage Zone 2. Suggested age. An Early Pliensbachian age is suggested for Assemblage Zone 1, based on the presence of Cere- bropollenites thiergartii together with Pinuspollenites minimus; a Late Pliensbachian age is proposed for Assemblage Zone 2 based on the occurrences of Nanno- ceratopsis senex and Mancodinium semitabulatum. Tancrediakløft Only one sample (341229; Rævekløft Formation) was studied from this locality. The sample contained only black material which was not identifiable. Qupaulakajik Only one sample (341254; Albuen Member, Gule Horn Formation) was studied from this locality. The paly- nomorphs were black and indeterminate. Goniomyakløft Five samples were studied (Figs 7, 8). The sample 405467, from the uppermost part of Rævekløft Formation, yielded an assemblage rich in poorly preserved palynomorphs, dominated by terrestrial material. However, several spec- imens of the dinoflagellate cyst genus Dapcodinium were found together with a single specimen of Tas- manites. The former are similar to Dapcodinium priscum, but not identical to specimens of this species described from Northwest Europe. The assemblage is suggested to belong to Assemblage Zone 1. 743 744 Lower Jurassic Upper Pliensbachian Gule Horn Formation 12 Elis Bjerg Member Lower Pliensbachian Rævekløft Fm 21 0. 00 20 9. 00 20 8. 00 12 2. 00 12 1. 00 12 0. 00 11 9. 00 11 8. 50 11 8. 00 40 54 43 40 54 42 40 54 41 40 54 40 40 54 39 40 54 38 40 54 37 40 54 36 40 54 35 1Rogalskaisporites cicatricosus 2Conbaculatisporites mesozoicus 3Lycopodiacidites rugulatus 4Deltoidospora spp. 5Retitriletes clavatoides 6Retitriletes semimuris 7Retitriletes sp. 8Baculatisporites sp. 9Tigrisporites microrugulatus 10Foraminisporis jurassicus 11Kraeuselisporites reissingeri 12Tripartina variabilis 13Stereisporites stereoides 14Densoisporites scanicus 15Retitriletes austroclavatoides 16Todisporites minor 17Kekryphalospora distincta 18Cibotiumsporites jurienensis 19Striatella parva 20Todisporites major 21Striatella jurassica 22Chasmatosporites hians 23Cerebropollenites thiergartii 24Vesicaspora fuscus 25Quadraeculina anellaeformis 26Perinopollenites elatoides 27Pinuspollenites minimus 28Bisaccate spp. 29Cerebropollenites macroverrucosus 30Chasmatosporites major 31Chasmatosporites apertus 32Corollina torosus 33Monosulcites punctatus 34Taeniasporites rhaeticus 35Nannoceratopsis senex 36Acritarch spp. 37Veryhachium sp. 38Leiofusa jurassica 39Leiosphaeridia spp. 40Botryococcus spp. 41Tasmanites sp. R A lp ha be tic al s pe ci es li st 36 A cr ita rc h sp p. 8 B a cu la ti sp or it es s p. 28 Bi sa cc at e sp p. 40 B ot ry oc oc cu s sp p. 29 C er eb ro p ol le n it es m a cr ov er ru co su s 23 C er eb ro p ol le n it es t h ie rg a rt ii 31 C h a sm a to sp or it es a p er tu s 22 C h a sm a to sp or it es h ia n s 30 C h a sm a to sp or it es m a jo r 18 C ib ot iu m sp or it es j u ri en en si s 2 C on b a cu la ti sp or it es m es oz oi cu s 32 C or ol lin a t or os u s 4 D el to id os p or a s pp . 14 D en so is p or it es s ca n ic u s 10 Fo ra m in is p or is j u ra ss ic u s 17 K ek ry p h a lo sp or a d is ti n ct a 11 K ra eu se lis p or it es r ei ss in ge ri 38 Le io fu sa j u ra ss ic a 39 Le io sp h a er id ia s pp . 3 Ly co p od ia ci d it es r u gu la tu s 33 M on os u lc it es p u n ct a tu s 35 N a n n oc er a to p si s se n ex 26 Pe ri n op ol le n it es e la to id es 27 Pi n u sp ol le n it es m in im u s 25 Q u a d ra ec u lin a a n el la ef or m is 15 R et it ri le te s a u st ro cl a va to id es 5 R et it ri le te s cl a va to id es 6 R et it ri le te s se m im u ri s 7 R et it ri le te s sp . 1 R og a ls k a is p or it es c ic a tr ic os u s 13 S te re is p or it es s te re oi d es 21 S tr ia te lla j u ra ss ic a 19 S tr ia te lla p a rv a 34 Ta en ia sp or it es r h a et ic u s 41 Ta sm a n it es s p. 9 T ig ri sp or it es m ic ro ru gu la tu s 20 To d is p or it es m a jo r 16 To d is p or it es m in or 12 Tr ip a rt in a v a ri a b ili s 37 Ve ry h a ch iu m s p. 24 Ve si ca sp or a f u sc u s R æ ve kl øf t 20 0 20 5 21 0 12 5 12 0 11 5 System Stage Palynological Assembl. Zones Lithostratigraphy (m) Sample height Sample number In te rv al n ot s am pl ed Fi g. 1 1. P al yn o m o rp h d is tr ib u tio n c h ar t fo r th e R æ ve kl ø ft F o rm at io n a n d G u le H o rn F o rm at io n ( E lis B je rg M em b er ) at R æ ve kl ø ft ( fo r lo ca tio n , se e Fi g. 1 ). F o r le ge n d , se e Fi g. 4 . Sample 405468 was collected just beneath the bound- ary between the Rævekløft Formation and the suc- ceeding Elis Bjerg Member (Gule Horn Formation). This sample yielded a similar palynomorph assemblage to that described above but included the first appearance of the dinoflagellate cyst Mancodinium semitabula- tum. It is suggestive of the somewhat younger As- semblage Zone 2. The samples 405469–405471 are from the Elis Bjerg Member. They lack recognisable dinofla- gellate cysts although acritarchs and some question- able dinoflagellate cysts were found together with Crassosphaera sp., foraminiferal inner linings and abun- dant Botryococcus sp. This assemblage is also suggested to belong to Assemblage Zone 2. Suggested age. An ?Early–Late Pliensbachian age is pro- posed, based on the appearance of Mancodinium semi- tabulatum. Astartekløft Fourteen samples from the northern and southern side of Astartekløft were investigated palynologically (Figs 9, 10; note that the barren samples are not shown on Fig. 10). The lowermost samples, 346614 at 266 m and 346627 at 328 m, are from the lower Elis Bjerg Member (Gule Horn Formation) and the lower Albuen Member (Gule Horn Formation), respectively (Fig. 10). These samples are dominated by Botryococcus sp. and bisac- cate pollen, together with common Cerebropollenites thiergartii and Chasmatosporites hians, and are referred to Assemblage Zone 3. The two samples 405472 and 405473 from the upper Albuen Member (Figs 9, 10) contain abundant bisac- cate pollen; this and the lack of other palynomorphs indicate Assemblage Zone 4. Samples 405474 and 405475 are from the lowermost beds of the Astartekløft Member; they record the first appearance of Spheripollenites subgranulatus, together with abundant Cerebropollenites macroverrucosus and the re-appearance of the dinoflagellate cyst Nanno- ceratopsis senex. Sample 405477, also from the Astarte- kløft Member, lacks Spheripollenites subgranulatus but Nannoceratopsis senex is common. In sample 405483 from the Astartekløft Member, the organic material is black and indeterminate and thus this sample does not appear on Figure 10. In sample 341269, from the Nathorst Fjeld Member, Spheripollenites subgranulatus is abun- dant, and in the uppermost sample (341270), also from the Nathorst Fjeld Member, Spheripollenites subgranu- latus is absent but Nannoceratopsis senex is abundant together with Cerebropollenites macroverrucosus. It is suggested that the assemblages recorded between sam- ple 405474, at the base of the Astartekløft Member, and the uppermost sample 341270, in the Nathorst Fjeld Member, are compatible with Assemblage Zone 5 as defined from the Albuen section. Suggested age. The lowermost part of the succession is referred to the Upper Pliensbachian based on the abun- dance of Cerebropollenites thiergartii and Chasmato- sporites hians. An Early Toarcian age for the uppermost part is based on the first appearance and abundance of both Spheripollenites subgranulatus and Cerebro- pollenites macroverrucosus. Moskusoksekløft Only one sample (341260; Nathorst Fjeld Member, Ostreaelv Formation) was investigated from this local- ity; it yielded the dinoflagellate cysts Nannoceratopsis senex and N. triangulata and the pollen Spheripollenites subgranulatus and Cerebropollenites macroverrucosus (Fig. 12A). This assemblage is referred to Assemblage Zone 5. Suggested age. An Early Toarcian age is proposed based on the presence of Spheripollenites subgranulatus and Cerebropollenites macroverrucosus together with Nanno- ceratopsis senex and N. triangulata. Harris Fjeld One sample (346741) was studied from this locality, from the lower part of Elis Bjerg Member (Fig. 12B). The palynological assemblage is dominated by poorly preserved bisaccate pollen and the assemblage was deemed too poor to determine to which assemblage zone it belongs. Primulaelv Three samples (346746, 346745, 346753) were analysed from this locality (Fig. 12C), the first two from the Elis Bjerg Member and the third from the lowermost mud- stones of the Skævdal Member. The lowermost sample is tentatively referred to Assemblage Zone 1, based on a very poor assemblage of bisaccates, Pinuspollenites 745 746 Sy st em Lo w er Ju ra ss ic St ag e To ar ci an Pa ly no lo gi ca l A ss em bl . Z on es Li th os tr at ig ra ph y N at ho rs t Fj el d M b O st re ae lv F or m at io n Sa m pl e he ig ht 359.00 Sa m pl e nu m be r 341260 1 D el to id os p or a sp p. 2 St ri at el la ju ra ss ic a 3 Is ch yo sp or ite s va ri eg at us 4 B ac ul at is p or ite s sp . 5 Sp he ri p ol le ni te s su bg ra nu la tu s 6 C er eb ro p ol le ni te s m ac ro ve rr uc os us 7 C or ol lin a to ro su s 8 Bi sa cc at e sp p. 9 C or ol lin a m ey er ia na 10 C ha sm at os p or ite s m aj or 11 C er eb ro p ol le ni te s th ie rg ar tii 12 N an no ce ra to p si s se ne x 13 N an no ce ra to p si s tr ia ng ul at a 14 C ym at io sp ha er a sp . 15 Fo ra m in ife ra s pp . 16 B ot ry oc oc cu s sp p. Alphabetical species list 4 Baculatisporites sp. 8 Bisaccate spp. 16 Botryococcus spp. 6 Cerebropollenites macroverrucosus 11 Cerebropollenites thiergartii 10 Chasmatosporites major 9 Corollina meyeriana 7 Corollina torosus 14 Cymatiosphaera sp. 1 Deltoidospora spp. 15 Foraminifera spp. 3 Ischyosporites variegatus 12 Nannoceratopsis senex 13 Nannoceratopsis triangulata 5 Spheripollenites subgranulatus 2 Striatella jurassica A: Moskusoksekløft 5 B: Harris Fjeld Sy st em ? St ag e Li th os tr at ig ra ph y ? Pa ly no lo gi ca l A ss em bl . Z on es ? El is B je rg M b G ul e H or n Fm Sa m pl e he ig ht 269.00 Sa m pl e nu m be r 346741 1 B a cu la ti sp or it es s p. 2 Ly co p od ia ci d it es r u gu la tu s 3 D el to id os p or a s pp 4 R og a ls k a is p or it es c ic a tr ic os u s 5 Bi sa cc at e po lle n 6 C h a sm a to sp or it es h ia n s 7 Pe ri n op ol le n it es e la to id es 8 Pi n u sp ol le n it es m in im u s 9 C er eb ro p ol le n ti es t h ie rg a rt ii 10 Ve si ca sp or a f u sc u s Alphabetical species list 1 Baculatisporites sp. 5 Bisaccate pollen 9 Cerebropollenites thiergartii 6 Chasmatosporites hians 3 Deltoidospora spp. 2 Lycopodiacidites rugulatus 7 Perinopollenites elatoides 8 Pinuspollenites minimus 4 Rogalskaisporites cicatricosus 10 Vesicaspora fuscus C: Primulaelv 451.00 310.00 346753 346746 1 D el to id os p or a s pp . 2 B a cu la ti sp or it es s p. 3 S tr ia te lla j u ra ss ic a 4 M eg as po re s pp . 5 R et it ri le te s sp . 6 K ek ry p h a lo sp or a d is ti n ct a 7 K ra eu se lis p or it es r ei ss in ge ri i 8 Is ch yo sp or it es v a ri eg a tu s 9 M a n u m ia d el co u rt ii 10 Bi sa cc at e sp p. 11 C er eb ro p ol le n it es t h ie rg a rt ii 12 C or ol lin a t or os u s 13 C h a sm a to sp or it es h ia n s 14 Pi n u sp ol le n it es m in im u s 15 S p h er ip ol le n it es s u b gr a n u la tu s 16 C er eb ro p ol le n it es m a cr ov er ru co su s 17 C h a sm a to sp or it es a p er tu s 18 C h a sm a to sp or it es m a jo r 19 N a n n oc er a to p si s sp . 20 N a n n oc er a to p si s se n ex 21 M a n co d in iu m s em it a b u la tu m 22 N a n n oc er a to p si s gr a ci lis 23 B ot ry oc oc cu s sp p. Alphabetical species list 2 Baculatisporites sp. 10 Bisaccate spp. 23 Botryococcus spp. 16 Cerebropollenites macroverrucosus 11 Cerebropollenites thiergartii 17 Chasmatosporites apertus 13 Chasmatosporites hians 18 Chasmatosporites major 12 Corollina torosus 1 Deltoidospora spp. 8 Ischyosporites variegatus 6 Kekryphalospora distincta 7 Kraeuselisporites reissingerii 21 Mancodinium semitabulatum 9 Manumia delcourtii 4 Megaspore spp. 22 Nannoceratopsis gracilis 20 Nannoceratopsis senex 19 Nannoceratopsis sp. 14 Pinuspollenites minimus 5 Retitriletes sp. 15 Spheripollenites subgranulatus 3 Striatella jurassica Sy st em St ag e Pa ly no lo gi ca l A ss em bl . Z on es Li th os tr at ig ra ph y L. P lie ns ba ch ia n G ul e H or n Fm El is B je rg M b To ar ci an O st re ae lv F m N at h. F . M b Sk æ v. M b Lo w er Ju ra ss ic (m ) Sa m pl e he ig ht Sa m pl e nu m be r Interval not sampled 450 445 315 3101 5 Rare Few Common Abundant Fig. 12. Palynomorph distribution charts (for locations, see Fig. 1). A, Ostreaelv Formation (Nathorst Fjeld Member) at Moskusoksekløft. B, Gule Horn Formation (Elis Bjerg Member) at Harris Fjeld. C, Gule Horn Formation (Elis Bjerg Member) and Ostreaelv Formation (Nathorst Fjeld (Nath. F.) and Skævdal (Skæv.) Members) at Primulaelv. minimus and common Botryococcus sp. The second sample (346745) was barren and thus does not appear on the distribution chart (Fig. 12C). The uppermost sample is referred to Assemblage Zone 5 on the basis of abundant Spheripollenites subgranulatus, Cerebro- pollenites macroverrucosus and Nannoceratopsis senex. Suggested age. A Late Pliensbachian age is tentatively suggested for the lowermost sample (346746) based on a very poor assemblage in which only bisaccates and Pinuspollenites minimus are common. An Early Toarcian age is suggested for the uppermost sample (346753) based on abundant Spheripollenites subgranulatus, Cerebropollenites macroverrucosus and Nannoceratopsis senex. Lepidopteriselv Ten samples (139137–139146) were studied from this section and all of them are rich in palynomorphs (Fig. 13, following page 744). These samples were collected by Claus Heinberg and Tove Birkelund in 1974, and they were thus not assigned to the recently-defined mem- bers. However, comparing their field notes with our sedimentological logs, it has been possible to assign the samples to the Elis Bjerg Member. The samples 139237–139240 are rich in the spores Deltoidospora and Baculatisporites, the pollen Pinus- pollenites minimus and Cerebropollenites thiergartii, bisaccate pollen and Botryococcus sp. In sample 139141, the dinoflagellate cyst Nannoceratopsis senex is very abundant and Botryococcus sp. is rare. Samples 139142–139146 are again rich in spores and pollen and Botryococcus sp. whereas dinoflagellate cysts are rare. The palynological results allow us to suggest that the lowermost five samples (139137–139141) belong to Assemblage Zone 2. This is based on the common occurrence of Cerebropollenites thiergartii and Nanno- ceratopsis senex. The next five samples (139142–139146) are referred to Assemblage Zone 3 based on the pres- ence of Cerebropollenites thiergartii, Pinuspollenites minimus and bisaccate pollen and the fact that dinofla- gellate cysts are rare. 747 Liaselv Sy st em Lo w er Ju ra ss ic St ag e U pp er P lie ns ba ch ia n Pa ly no lo gi ca l A ss em bl . Z on es Li th os tr at ig ra ph y G ul e H or n Fo rm at io n El is B je rg M em be r (m ) 325 315 305 295 Sa m pl e he ig ht 325.00 299.00 293.00 Sa m pl e nu m be r 346665 346662 346667 1 B a cu la ti sp or it es s p. 2 D el to id os p or a s pp . 3 Ly co p od ia ci d it es r u gu la tu s 4 R et it ri le te s se m im u ri s 5 N eo ra is tr ic k ia s p. 6 S tr ia te lla s ee b er ge n si s 7 D en so is p or it es s ca n ic u s 8 R et it ri le te s sp . 9 Bi sa cc at e sp p. 10 Pi n u sp ol le n it es m in im u s 11 Pe ri n op ol le n it es e la to id es 12 C er eb ro p ol le n it es t h ie rg a rt ii 13 C h a sm a to sp or it es h ia n s 14 C er eb ro p ol le n it es m a cr ov er ru co su s 15 Q u a d ra ec u lin a a n el la ef or m is 16 C h a sm a to sp or it es m a jo r 17 Ve si ca sp or a f u sc u s 18 C or ol lin a t or os u s 19 N a n n oc er a to p si s se n ex 20 M en d ic od in iu m s p. 21 M a n co d in iu m s em it a b u la tu m 22 D in oc ys t sp p. 23 A cr ita rc h sp p. 24 B ot ry oc oc cu s sp p. ? Alphabetical species list 23 Acritarch spp. 1 Baculatisporites sp. 9 Bisaccate spp. 24 Botryococcus spp. 14 Cerebropollenites macroverrucosus 12 Cerebropollenites thiergartii 13 Chasmatosporites hians 16 Chasmatosporites major 18 Corollina torosus 2 Deltoidospora spp. 7 Densoisporites scanicus 22 Dinocyst spp. 3 Lycopodiacidites rugulatus 21 Mancodinium semitabulatum 20 Mendicodinium sp. 19 Nannoceratopsis senex 5 Neoraistrickia sp. 11 Perinopollenites elatoides 10 Pinuspollenites minimus 15 Quadraeculina anellaeformis 4 Retitriletes semimuris 8 Retitriletes sp. 6 Striatella seebergensis 17 Vesicaspora fuscus 2 Uncertain determination Very rare Rare Few Common Abundant ? R Fig. 14. Palynomorph distribution chart for the Gule Horn Formation (Elis Bjerg Member) at Liaselv (for location, see Fig. 1). Suggested age. A Late Pliensbachian age is proposed for the samples 139137–139146 based on the presence of Cerebropollenites thiergartii, Pinuspollenites minimus, Nannoceratopsis species and Mancodinium semitabu- latum. Liaselv Three samples (346662, 346665, 346667) were analysed from the Elis Bjerg Member (Fig. 14); in general, preser- vation of the palynomorphs is very poor. All three sam- ples are dominated by bisaccate pollen and Botryococcus sp. and it is suggested that they belong to Assemblage Zone 2. Suggested age. A Late Pliensbachian age has been sug- gested because of the abundance of Pinuspollenites minimus and bisaccates. Horsedal and the Deltoidospora Assemblage Four samples (346696, 346700, 346701, 346703) were analysed from the Horsedal Member at Horsedal (Figs 15, 16). Sample 346696 was barren. Sample 346700, from a coal bed, yielded an assemblage composed pre- dominantly of laevigate spores (pteridophyte spores) of the genus Deltoidospora. Such an assemblage has not been recorded before in samples from the Neill Klinter Group at Albuen or at any other locality in Jameson Land and Scoresby Land. The assemblage totally lacks microplankton. Sample 346701 yielded a more diverse assemblage, but is dominated by bisaccate pollen and Botryococcus sp. The uppermost sample, 346703, yielded only bisaccate pollen. It has not, based on the present material, been pos- sible to place this assemblage within any of the assem- blage zones defined above from the Albuen succession. The assemblage is thus defined as a new assemblage, named the Deltoidospora Assemblage, which is presently only recognised at Horsedal in the Horsedal Member of the Ostreaelv Formation. Suggested age. This assemblage is not age specific; it could occur within any stage of the Jurassic. Palaeoenvironment. This assemblage is indicative of an enclosed swamp area (lagoon, pond, small lake) with a dense vegetation of ferns. Ranunkeldal Seven samples were analysed from this section (Figs 5, 6). Samples 341167–341170 were sampled in the upper- most part of the Kap Stewart Group and samples 748 M Si Pb Sand 815 820 346700 825 346703 346701 830 m Horsedal W av e- a nd s to rm -d om in at ed la go on D el to id os p or a A ss em bl ag e O st re ae lv F or m at io n H or se da l M em be r Fig. 15. Sedimentological log through part of the Horsedal Member (Ostreaelv Formation) in Horsedal (for location, see Fig. 1). Sample numbers are indicated; arrows denote grain-size trends. For legend, see Fig. 3. 341171–341173 are from the Elis Bjerg Member of the Gule Horn Formation. Preservation of the palynomorphs from all these samples is very poor. However, the paly- nomorph assemblages are dominated by the laevigate spore Deltoidospora sp., bisaccate pollen, Chasmato- sporites hians, Cerebropollenites thiergartii and Quadrae- culina anellaeformis. Botryococcus sp. is present in all samples, but is only abundant in the uppermost sam- ple. In sample 341168, a dinoflagellate cyst has been found; it is similar to Mendicodinium reticulatum, but shows some anomalous features. The occurrence of this dinoflagellate cyst suggests that the environment was influenced by brackish waters, at least for a short time. A single Nannoceratopsis gracilis cyst was observed in sample 341171 from 306 m. In this sample, a Tasmanites was found together with a poorly preserved foraminiferal inner-lining. In the uppermost sample, several Leiofusa jurassica were recorded. The palynomorph assemblages from the Kap Stewart Group in Ranunkeldal are suggested to belong to a separate assemblage zone. The samples from the Elis Bjerg Member are referred to Assemblage Zone 1. Suggested age. A ?Late Sinemurian age is suggested for the Kap Stewart Group samples because of the occur- rence of the dinoflagellate comparable to Mendico- dinium reticulatum. This species has been found on Bornholm, Denmark in sediments of latest Sinemurian and earliest Pliensbachian age (Batten et al. 1994; Koppelhus & Nielsen 1994). A Pliensbachian age is sug- gested for the Elis Bjerg Member samples because of the presence of Nannoceratopsis gracilis. Palaeoenvironment. A non-marine, freshwater envi- ronment is indicated for the Kap Stewart Group sam- ples, although the presence of a dinoflagellate cyst in sample 341168 suggests the influence of brackish water, albeit only temporarily. The samples from the Elis Bjerg Member indicate marine influence. Depositional environments and assemblage zones The palynological results presented above provide an additional dataset with which to constrain palaeoenvi- ronmental and sequence stratigraphic interpretations. In the following section, the individual palynological assemblage zones, together with the Deltoidospora Assemblage, are discussed in relation to the sedimen- tological and stratigraphic data. Assemblage Zone 1: Cerebropollenites thiergartii – Pinuspollenites minimus – Botryococcus This assemblage zone is characteristic of the sedimen- tary succession referred to sequence SQ2 of Dam & Surlyk (1995, 1998) at Qupaulakajik, Albuen and 749 Horsedal Sy st em St ag e Li th os tr at ig ra ph y O st re ae lv F or m at io n H or se da l M em be r Pa ly no lo gi ca l A ss em bl ag e ? ? D el to id os p or a (m ) 825 815 Sa m pl e he ig ht 828.00 823.00 813.00 Sa m pl e nu m be r 346703 346701 346700 1 D el to id os p or a s pp . 2 B a cu la ti sp or it es s p. 3 C a la m os p or a t en er 4 R et it ri le te s sp . 5 N eo ra is tr ic k ia s p. 6 R et it ri le te s a u st ro cl a va to id es 7 Ly co p od ia ci d it es r u gu la tu s 8 D en so is p or it es s ca n ic u s 9 C h a sm a to sp or it es m a jo r 10 Pe ri n op ol le n it es e la to id es 11 C er eb ro p ol le n it es t h ie rg a rt ii 12 S p h er ip ol le n it es p si la tu s 13 C er eb ro p ol le n it es m a cr ov er ru co su s 14 C h a sm a to sp or it es h ia n s 15 Pi n u sp ol le n it es m in im u s 16 Bi sa cc at e sp p. 17 Ve si ca sp or a f u sc u s 18 Q u a d ra ec u lin a a n el la ef or m is 19 Pa re od in ia h a lo sa 20 M en d ic od in iu m s p. 21 N a n n oc er a to p si s sp . 22 B ot ry oc oc cu s sp p. ? Alphabetical Species List 2 Baculatisporites sp. 16 Bisaccate spp. 22 Botryococcus spp. 3 Calamospora tener 13 Cerebropollenites macroverrucosus 11 Cerebropollenites thiergartii 14 Chasmatosporites hians 9 Chasmatosporites major 1 Deltoidospora spp. 8 Densoisporites scanicus 7 Lycopodiacidites rugulatus 20 Mendicodinium sp. 21 Nannoceratopsis sp. 5 Neoraistrickia sp. 19 Pareodinia halosa 10 Perinopollenites elatoides 15 Pinuspollenites minimus 18 Quadraeculina anellaeformis 6 Retitriletes austroclavatoides 4 Retitriletes sp. 12 Spheripollenites psilatus 17 Vesicaspora fuscus Uncertain determination Rare Few Common Abundant ? Fig. 16. Palynomorph distribution chart for the Horsedal Member (Ostreaelv Formation) in Horsedal (for location, see Fig. 1). Goniomyakløft, which consists of the upper part of the Rævekløft Formation and the lowermost part of the Elis Bjerg Member (Fig. 17). It is also present in the lower part of sequence SQ3 at Primulaelv, however, and in the lowermost part of the Elis Bjerg Member in Ranunkel- dal, just above the Kap Stewart Formation. The base of the assemblage zone thus coincides with the base of sequence SQ1 (i.e. SB1) and the zone extends up into the lowermost part of sequence SQ3 of Dam & Surlyk (1995, 1998). At the studied locations, the upper part of the Rævekløft Formation consists of cross-bedded, fossiliferous medium- to very coarse-grained sandstones (Fig. 7), interpreted to represent fields of dunes or shoreface ridges on the shoreface (Dam & Surlyk 1995, 1998). In the Elis Bjerg Member, the assemblage is pre- sent in subtidal sand sheet, shoreface and offshore tran- sition deposits (Figs 3A, 5). The Rævekløft Formation is capped by an important drowning surface that defines the base of the Elis Bjerg Member (Figs 7, 17; Dam & Surlyk 1995, 1998). The palynological assemblage is uniform, being dom- inated by bisaccate pollen and the freshwater to brack- ish alga Botryococcus sp. Spores include common Deltoidospora and Baculatisporites sp., and locally Lycopodiacidites rugulatus. Among the pollen, Pinus- pollenites minimus and Cerebropollenites thiergartii are common. Acritarchs are rare and dinoflagellate cysts are absent with the exception of one Nannoceratopsis gra- cilis cyst and the undetermined dinoflagellate cyst (cf. Mendicodinium reticulatum) from the Ranunkeldal section. The assemblage probably reflects a vegetation with few fern species and several gymnosperm species. These grew close to a fresh or brackish water envi- ronment, where the Botryococcus algae lived. When seen in the light of the strong marine indicators pro- vided by the macrofossils, sedimentary structures and ichnology, it is suggested that this palynomorph assem- blage is dominantly allochthonous, having been trans- ported from a terrestrial to a shallow marine environ- ment. Similar palynomorph assemblages are known from other areas, for example in the uppermost Sinemurian and lowermost Pliensbachian of Bornholm in the Baltic Sea (Koppelhus & Nielsen 1994). Assemblage Zone 2: Nannoceratopsis–Botryococcus The assemblage zone is characteristic of the middle part of the Elis Bjerg Member at Albuen, Lepidopteriselv and Liaselv in subtidal sand sheet and storm-dominated shoreface deposits, but also occurs in similar deposits in the lower part of the member at Goniomyakløft and the upper part of the member at Qupaulakajik (Figs 2, 17). The assemblage zone is most characteristic of the lower part of sequence SQ3 of Dam & Surlyk (1995, 1998), but is also locally present in the uppermost part of sequence SQ2 (Fig. 17). The top is placed below the transition from subtidal sand sheet deposits to tidal channel deposits of the Elis Bjerg Member (Fig. 3A). The palynomorph assemblage is dominated by the same spores, pollen and Botryococcus sp. that charac- terise Assemblage Zone 1, but the incoming of Nanno- ceratopsis senex, N. gracilis, Parvocysta barbata and Mancodinium semitabulatum together with Limbicysta bjaerkei and a few more acritarchs indicates an increase in marine influence. In most of the samples, there are between three and seven different dinoflagellate cyst species and between one and five acritarch species. The marine interpretation of this palynomorph assem- blage zone is in agreement with the sedimentological and ichnological data, which also indicate a shallow marine environment (Dam & Surlyk 1995, 1998). Assemblage Zone 3: Chasmatosporites – Cerebropollenites thiergartii – Botryococcus The assemblage is characterised by rare dinoflagellate cysts such as Mendicodinium reticulatum and Nanno- ceratopsis spp. A few acritarchs are present, together with abundant pollen and Botryococcus. The assemblage is present in the upper part of the Elis Bjerg Member, but may extend into the lowermost part of the Albuen Member (Fig. 17). Assemblage Zone 3 is dominantly pre- sent in stacked tidal channel and wave- and storm-dom- inated shoreface deposits (Fig. 3A; Dam & Surlyk 1995, 1998), whereas the sample from the Albuen Member was from heterolithic lower shoreface deposits. The base of the assemblage zone is placed just below the transition from subtidal sand sheet deposits to tidal channel deposits. At Albuen, the top of the zone occurs just beneath the boundary between tidal channel deposits of the Elis Bjerg Member and storm-dominated offshore transition deposits of the Albuen Member; this boundary has been interpreted as a coalesced sequence boundary and transgressive surface (Dam & Surlyk 1995, 1998). At Astartekløft, however, the lowermost sam- ple in the Albuen Member is also referred to Assemblage Zone 3 (Fig. 10). 750 751 0 50 10 0 15 0 km 50 m H ST H ST H ST H ST H ST T ST T ST SQ 6 SQ 5 SQ 7 SQ 4 SQ 3 SQ 2 SQ 1 T re fjo rd B je rg Qupaulakajik/ Rævekløft Albuen Goniomyakløft Astartekløft Moskusoksekløft Harris Fjeld (N) Nathorst Fjeld Dusén Bjerg T id al c ha nn el s an d su bt id al s ho al s Rhætelv Horsedal Halten Terrace, Norway Lepidopteriselv/ Liaselv Primulaelv Harris Fjeld (S) A st ar te kl øf t/ H or se da l Sk æ vd al M b Fm Sortehat Ostreaelv Gule Horn A lb ue n El is B je rg R æ ve kl øf t T ST T ST T ST H ST T ST T STLS T N at ho rs t Fj el d/ H ar ri s Fj el d/ Le pi do pt er is el v So ut h N or th Sh or ef ac e T er m in al lo be La go on O ffs ho re t ra ns iti on Fa ci es a ss oc ia tio n bo un da ry Se qu en ce b ou nd ar y M aj or fl oo di ng s ur fa ce N ot Ile R or T ilj e Å re A ss em bl ag e Z on e 4 A ss em bl ag e Z on e 3 A ss em bl ag e Z on e 2 A ss em bl ag e Z on e 1 D el to id os p or a A ss em bl ag e A ss em bl ag e Z on e 7 A ss em bl ag e Z on e 6 A ss em bl ag e Z on e 5 Fi g. 1 7. N o rt h –s o u th c o rr el at io n p an el o f th e Lo w er – lo w er M id d le J u ra ss ic N ei ll K lin te r G ro u p o f Ja m es o n L an d , E as t G re en la n d s h o w in g th e d is tr ib u tio n o f th e p al yn o lo gi ca l a ss em - b la ge z o n es r ep o rt ed h er e re la tiv e to th e m ai n s eq u en ce s tr at ig ra p h ic e le m en ts a n d th e d ep o si tio n al e n vi ro n m en ts . T h e co rr el at iv e fo rm at io n s o f th e H al te n T er ra ce , o ff sh o re N o rw ay , ar e sh o w n o n t h e ri gh t- h an d s id e o f th e fi gu re . N o te t h at p al yn o lo gi ca l d at a ar e sc ar ce n o rt h o f A st ar te kl ø ft . T h e d o tt ed v er tic al l in es i n d ic at e th e lo ca lit ie s o n w h ic h t h e se q u en ce st ra tig ra p h ic i n te rp re ta tio n o f D am & S u rl yk ( 19 98 ) is b as ed . A ss em b la ge Z o n es 8 a n d 9 i n t h e So rt eh at F o rm at io n a re n o t in d ic at ed ; th e re ad er i s re fe rr ed t o K o p p el h u s & H an se n (2 00 3, t h is v o lu m e) . Fi gu re m o d if ie d f ro m D am & S u rl yk ( 19 98 ). S Q , se q u en ce ; LS T , lo w st an d s ys te m s tr ac t; T ST , tr an sg re ss iv e sy st em s tr ac t; H ST , h ig h st an d s ys te m s tr ac t. The shift from Assemblage Zone 2 to Assemblage Zone 3 records a change from a marine setting to an environment with a strongly terrestrial character, albeit with evidence of periodic marine influence. This flo- ral/faunal change is compatible with the sedimento- logical record (Dam & Surlyk 1995, 1998), which indicates a change from subtidal sand sheet deposition in a shallow marine environment to a tidal channel environment, where a larger degree of terrestrial influ- ence is to be expected. Assemblage Zone 4: Bisaccates This palynomorph assemblage is very uniform, being dominated overwhelmingly by bisaccate pollen. The combined data from the Albuen and Astartekløft sec- tions suggest that the assemblage characterises much of the Albuen Member of the Gule Horn Formation. At Albuen, the base of the assemblage zone occurs imme- diately above the coalesced sequence boundary and transgressive surface that separates the Elis Bjerg and Albuen Members (Fig. 3B; SB4 of Dam & Surlyk 1995, 1998); at Astartekløft, in contrast, Assemblage Zone 3 straddles this sequence boundary, Assemblage Zone 4 being recognised only in the uppermost levels of the Albuen Member (Fig. 10). The upper levels of the Albuen Member proved inac- cessible at Albuen and were not sampled; the top of the zone is placed at the uppermost sample, some 12 m below the top of the member. At Astartekløft, however, detailed sampling across the boundary between the Albuen and Astartekløft Members demonstrated that the boundary between Assemblage Zones 4 and 5 coin- cides closely with this surface which is interpreted as a sequence boundary (Figs 9, 10, 17; SB5 of Dam & Surlyk 1995, 1998). The Albuen Member is heterolithic, being composed of alternating mudstones and well-sorted fine-grained sandstones deposited in a storm-dominated lower shoreface environment (Dam & Surlyk 1995, 1998). A few coarse-grained pebbly sheets, moulded into large symmetrical ripples, and massive sandy mudstones deposited from debris flows are commonly interbed- ded with the heterolithic deposits. It is well-known that bisaccate pollen is commonly concentrated in distal marine settings, beyond the reach of other terrestrial palynomorphs. On this basis, this assemblage could therefore be interpreted to reflect an offshore marine environment, beyond the depositional range of other land-derived elements. The sedimento- logical data, however, testify to a lower shoreface envi- ronment (Dam & Surlyk 1998), and other land-derived elements should therefore be present. The absence of marine palynomorphs is also difficult to explain. As discussed earlier, such thin-walled forms may have been selectively destroyed by thermal effects caused by the intrusion of volcanics into the sediments. Alternatively, the lack of marine palynomorphs could reflect partial iso- lation of the embayment resulting in the development of a fresh to brackish water environment; this could also explain the lack of tidal indicators in this member. Assemblage Zone 5: Spheripollenites subgranulatus – Cerebropollenites macroverrucosus – Luehndea spinosa The base of Assemblage Zone 5 in the Albuen section is characterised by the sudden incoming of Spheri- pollenites subgranulatus and the reappearance of dinofla- gellate cysts together with a more diverse pollen flora and the freshwater alga Botryococcus sp. In sample 405466 at 259 m in the Albuen section (Figs 3B, 4A), Luehndea spinosa appears for the first time together with common spherical dinocysts that are of unknown affin- ity, but have been recorded from Spitsbergen, the Danish Subbasin and Bornholm, Denmark (Bjærke 1980a; Dybkjær 1991; Koppelhus & Nielsen 1994). At Astartekløft, the lower zone boundary is placed just above the sequence boundary between the Albuen and Astartekløft Members (Figs 9, 17; SB5 of Dam & Surlyk 1995); the upwards extent of the zone is poorly constrained at this locality. At Albuen, the upper bound- ary of the zone is placed approximately 10 m below the drowning surface that separates the heavily bio- turbated shoreface sandstones of the Nathorst Fjeld Member from bioturbated shelf deposits of the Skævdal Member (Fig. 3C). At Primulaelv, a single sample shows that this assemblage is also present just above the drown- ing surface (Fig. 17). Along Neill Klinter, the Astartekløft Member includes three facies associations, tidal chan- nel, subtidal sand sheet and storm-dominated sandy shoal associations (Fig. 3B). The tidal channel and sub- tidal sand sheet deposits are similar to those of the Elis Bjerg Member, discussed above under Assemblage Zones 2 and 3. The storm-dominated sandy shoal deposits form a laterally continuous succession, com- posed of well-sorted fine- to medium-grained sand- stone beds (Dam & Surlyk 1995, 1998). The Nathorst Fjeld Member forms a single coarsening-upwards succession consisting of alternating silty mudstones and 752 thin laminae of very fine- to fine-grained sandstones, grading upwards into fine- to coarse-grained sand- stones. The sandstones are cross-bedded, wave ripple cross-laminated, hummocky cross-stratified and bio- turbated. The coarsening-upwards succession reflects an increase in energy with time and is interpreted to record progressive shallowing from an offshore transi- tion setting to a shoreface environment. The Spheripollenites subgranulatus – Cerebropollenites macroverrucosus – Luehndea spinosa assemblage com- prises a mixture of spores, pollen, a few dinoflagellate cyst species and acritarchs and the freshwater alga Botryococcus. The assemblage zone indicates a brack- ish to marine environment with a large input of terres- trial material. This is in accordance with the sedi- mentological data indicating various environments in a marginal shallow marine setting. Assemblage Zone 6: Perinopollenites elatoides Assemblage Zone 6, which is typical of the Skævdal and the Trefjord Bjerg Members (Fig. 17) is characterised by the abundance of the pollen Perinopollenites elatoides and the absence or scarcity of Spheripollenites sub- granulatus. Overall, the palynomorph assemblage is dominated by different pollen species but dinoflagel- late cysts are also significant, including Dissiliodinium sp., Phallocysta eumekes, Pareodinia halosa, and Kallospharidium sp.; acritarchs are also present. At Albuen, in the south-eastern part of the basin, the lower boundary is placed some 10 m below the drown- ing surface that defines the top of the Nathorst Fjeld Member (Figs 3C, 17). The upper boundary of the assemblage zone at Albuen is placed at 434 m in the upper Trefjord Bjerg Member. Succeeding samples, just below the boundary between the Trefjord Bjerg Member and the Sortehat Formation, are referred to Assemblage Zone 7, which is characteristic of the lower Sortehat Formation (Figs 3C, 17). At 437 m, between these two sampled levels, is an erosional surface that is draped by well-rounded quartzite pebbles up to 3 cm across; this surface is defined as a sequence boundary (SB7 of Dam & Surlyk 1998). The Skævdal Member consists of bioturbated muddy sandstones and deposition probably took place in a low-energy shelf environment (Dam & Surlyk 1995, 1998). Primary physical structures only occur locally and include wave ripple cross-lamination, cross-lami- nation and cross-bedding. Stratigraphic variations in the mud content suggests that the heavily bioturbated muddy sandstones were originally deposited as het- eroliths (Dam & Surlyk 1995, 1998). The Skævdal Member is truncated by a prominent basinwide erosional unconformity, in places draped by a lag conglomerate. The unconformity marks a basin- wide seawards shift in facies and is interpreted as a sequence boundary (SB6 of Dam & Surlyk 1995, 1998). At Albuen, the sequence boundary is overlain by sub- tidal cross-bedded sandstones of the Trefjord Bjerg Member deposited in an extensive subtidal dune field. The palynomorph Assemblage Zone 6 is indicative of deposition in a marine environment with a large input of terrigenous material. This is in accordance with the sedimentological data that indicate a shallow marine environment (Dam & Surlyk 1995, 1998). Assemblage Zone 7: Botryococcus This assemblage is characterised by abundant Botry- ococcus. In a few samples near the lower boundary of the zone, both Botryococcus and dinoflagellate cysts occur in abundance, but the latter become rare upwards within the zone; the top of the zone is marked by the re-appearance of dinoflagellate cysts and the disap- pearance of Botryococcus. The depositional environment of this assemblage zone is discussed in detail in an accom- panying paper (Koppelhus & Hansen 2003, this volume). Deltoidospora Assemblage This assemblage is restricted to the Horsedal Member in the northern part of the basin (Figs 15–17). This member is made up of minor coarsening-upwards suc- cessions, 1–6 m thick, deposited in wave-dominated beaches or delta systems that prograded into an exten- sive lagoonal environment (Dam & Surlyk 1995, 1998). The palynomorph assemblage is overwhelmingly dominated by laevigate spores (pteridophyte spores) of the genus Deltoidospora and is suggestive of an enclosed swamp area (lagoon, pond, small lake) with a dense vegetation of ferns. This is in close agreement with the depositional environment suggested by sedimentary facies analysis (Dam & Surlyk 1995, 1998). Discussion and conclusions Seven palynological assemblage zones have been recog- nised in the Rævekløft, Gule Horn and Ostreaelv 753 Formations of the Neill Klinter Group (Fig. 17). Six of these are defined in this paper; the uppermost zone is defined by Koppelhus & Hansen (2003, this volume) in an accompanying paper as it is most characteristic of the overlying Sortehat Formation, the uppermost for- mation of the Neill Klinter Group (Koppelhus & Hansen 2003, this volume). In addition, an assemblage termed the Deltoidospora Assemblage is defined here from the Horsedal section. The seven palynological assemblage zones were all recognised primarily on the basis of data from the Albuen section but additional data from other localities suggest that the zones may have a basinwide distri- bution (Figs 17, 18). The palynological assemblages contain a diverse palynoflora, including 136 species. The assemblages indicate that the Neill Klinter Group spans the Early Pliensbachian to early Aalenian, without any major breaks in the stratigraphic record. The study 754 AZ7 AZ6 AZ5 AZ4 AZ5 AZ3 AZ3 AZ2 AZ1 SB7 SB6 SB5 SB4 SB3 SB2 SB1 A al en ia n To ar ci an La te P lie ns ba ch ia n So rt eh at F m O st re ae lv F m N ei l K lin te r G ro up G ul e H or n Fm R æ ve kl øf t Fm K S Si n. Ea rl y Pl ie ns - ba ch ia n Sk æ vd al M b N at ho rs t Fj el d M b A st ar te kl øf t M b El is B je rg M b A lb ue n M b Tr ef jo rd Bj er g M b ? AZ2 AZ5 AZ3 AZ2 AZ2 AZ1 AZ1 AZ2 AZ4 AZ1 AZ5 A lb ue n A st ar te kl øf t R æ ve kl øf t G on io m ya kl øf t Le pi do pt er is el v Li as el v R an un ke ld al H ar ri s Fj el d Pr im ul ae lv M os ku so ks ek lø ft AZ1 Fig. 18. Correlation diagram showing the stratigraphic distribution of the palyno- logical assemblage zones (AZ1–7) at the studied locations (see Fig. 1). Note that the boundaries between Assemblage Zones 1 and 2 and between Assemblage Zones 3 and 4 are ‘diachronous’ relative to sequence boundaries SB3 and SB4 respectively. KS, Kap Stewart Group; Sin., Sinemurian. 755 shows that the palynomorph flora of the Neill Klinter Group is strongly influenced by the amount of organic matter derived from land plants and freshwater envi- ronments, yet the brackish and marine microplankton play a very important role in the interpretation of the environment and in establishing a palynostratigraphy for the group. Comparing the sequence stratigraphic framework developed by Dam & Surlyk (1995, 1998) with the dis- tribution of the palynological assemblages, it is clear that some of the major sequence stratigraphic and litho- logical boundaries are reflected by changes in the assem- blages. Assemblage Zones 1–3 are characteristic of sequences SQ1–3. Figures 17 and 18 illustrate that the boundary between Assemblages 1 and 2 is diachro- nous on a regional scale with respect to the important sequence stratigraphic surfaces (e.g. SB3). Given that the sole difference between these two zones is the pres- Boreal ammonite zones Palyno-events in East Greenland Palyno-events on the mid-Norwegian shelf OpalinumA al en ia n Pl ie ns ba ch ia n Lo w er Lo w er U pp er U pp er T oa rc ia n Levesquei Thouarsense Variabilis Bifrons Falciferum Tenuicostatum Spinatum Margaritatus Davoei Ibex Jamesoni Pareodinia halosa common Botryococcus spp. acme Callialasporites dampieri FAD Wallodinium laganum FAD Pareodinia halosa FAD Perinopollenites elatoides acme Abundant Cerebropollenites macroverrucosus Luehndea spinosa FAD Cerebropollenites thiergartii becomes rare Spheripollenites acme Only bisaccate pollen Cerebropollenites thiergartii dinoflagellate cysts Parvocysta sp. FAD Mancodinium semitabulatum Nannoceratopsis senex/gracilis FAD Abundant Botryococcus spp. Wallodinium laganum acme Callialasporites dampieri FAD Increasing Parvocysta sp. Comparodinium sp. FAD abundant Perinopollenites elatoides Nannoceratopsis gracilis/senex acme Sphaeromorph clusters acme Chasmatosporites sp. N. gracilis/senex acme Sphaeromorph clusters acme Chasmatosporites sp. N. gracilis/senex acme Sphaeromorph clusters acme Chasmatosporites sp. N. gracilis/senex acme Spheripollenites acme Abundant–common L. spinosa Luehndea spinosa FAD C. thiergartii present but becomes rare in younger sediments Mancodinium semitabulatum N. senex/gracilis FAD Abundant–common Botryococcus spp. Common acritarchs Fig. 19. Diagram showing major palyno- events in the Neill Klinter Group compared to the Early Jurassic palyno- events recorded from the Halten Terrace, mid-Norwegian shelf (I. Throndsen, personal communication 1996). FAD, first appearance datum. 756 ence/absence of marine dinoflagellates, such diachrone- ity is not surprising. It can be attributed to variations in terrestrial input and the dominance of the freshwater plume laterally along the basin margin. The transition from Assemblage Zone 2 to Assemblage Zone 3 is marked by a decrease in dinoflagellate cysts which coincides with a gradual overall change from a dominance of subtidal sand sheet deposits to a domi- nance of tidal channel deposits in the upper part of the Elis Bjerg Member (Figs 3A, 17; Dam & Surlyk 1998). The strengthening of the terrestrial signal recorded by the change in the palynological assemblage is thus in accordance with the sedimentological record. At Albuen, sequence boundary SB4 separates Assemblage Zones 3 and 4; at Astartekløft, however, a sample from a few metres above the sequence bound- ary is referred to Assemblage Zone 3. This may be due to reworking of the uppermost sediments of the Elis Bjerg Member in the underlying sequence. Palynological data from the Astartekløft section suggest that SB5 separates Assemblage Zones 4 and 5, whereas the transition from Assemblage Zone 5 to 6 appears to be diachronous (Fig. 17). Sequence boundary SB7 separates Assemblage Zones 6 and 7 (Fig. 17). With respect to the sequence strati- graphic interpretation given by Dam & Surlyk (1995), an important conclusion of this study is that Assemblage Zone 7, characteristic of the lower part of the overly- ing Sortehat Formation (Koppelhus & Hansen 2003, this volume), also occurs in the uppermost few metres of the Trefjord Bjerg Member at Albuen, above a later- ally persistent erosional surface with a conglomerate lag (Figs 3C, 17). At other localities, a thin conglomerate layer separates the Trefjord Bjerg Member and the Sortehat Formation. Dam & Surlyk (1995) interpreted the Trefjord Bjerg Member – Sortehat Formation bound- ary as a coalesced sequence boundary and transgres- sive surface. However, the palynological data suggest that at Albuen the sequence boundary should be placed beneath this boundary, at the conglomerate-draped ero- sional surface, and thus that the uppermost sandstones (c. 3 m thick) of the Trefjord Bjerg Member represent a thin lowstand or transgressive package (Figs 3C, 17). Moreover, the palynological data suggest that the inferred major flooding surfaces in the sequence stratigraphic analysis (i.e. base Albuen Member and base Sortehat Formation), may in fact record partial isolation of the embayment from the seaway between Norway and Greenland causing a freshwater to brackish environment to develop. This would also explain the lack of tidal indicators in the Albuen Member. If this is the case, the Albuen Member does not represent transgressive and highstand deposits in a sequence stratigraphic sense, but rather a period of physical isolation of the basin from the sea. The palynostratigraphy has proven to be an impor- tant tool in confirming the high-resolution sequence stratigraphic correlation between East Greenland and the Halten Terrace of the mid-Norwegian shelf pro- posed by Dam & Surlyk (1995). This detailed palyno- logical study should make it possible to correlate to other localities in the North Atlantic and to the mid-Norwegian area and the northern part of the North Sea. The pat- tern of events seen in the East Greenland material is mirrored by data from the Halten Terrace. Thus, accord- ing to I. Throndsen (personal communication 1996), the Pliensbachian is characterised by common to abundant Botryococcus; this is followed by the incoming of the dinoflagellate cysts Nannoceratopsis gracilis, N. senex and Mancodinium semitabulatum together with com- mon to abundant Cerebropollenites thiergartii pollen and abundant bisaccate pollen in the Upper Pliensbachian (Fig. 19). The dinoflagellate cyst Luehndea spinosa occurs in the uppermost Pliensbachian and lowermost Toarcian together with Nannoceratopsis gracilis and N. senex followed by an acme of Spheripollenites sub- granulatus together with the sphaeromorph clusters. In the Upper Toarcian, the dinoflagellate cyst Parvocysta complex appears together with abundant Perinopollenites elatoides pollen and the first Callialasporites dampieri appear together with the dinoflagellate cyst Wallodinium in the lowermost Aalenian. Acknowledgements The work carried out in connection with this project by E.B.K. was supported by a grant from the EFP-93 Projects 1313/93-0010 and 0017. The work of G.D. has been supported by BP Exploration Operating Company Limited, London, and the Carlsberg Foundation. The manuscript was read by Karen Dybkjær, James B. Riding, Jon R. Ineson and Finn Surlyk who offered many help- ful suggestions. In particular, we thank Ingar Throndsen who placed unpublished data from the Halten Terrace at our disposal, Henrik Nøhr-Hansen for patient assis- tance with the range charts and Jon R. Ineson for care- ful editing of the manuscript. References Batten, D.J., Koppelhus, E.B. & Nielsen, L.H. 1994: Uppermost Triassic to Middle Jurassic palynofacies and palynomiscel- lanea in the Danish Basin and Fennoscandian Border Zone. Cahiers de Micropaléontologie 9, 21–45. Bjærke, T. 1980a: Mesozoic palynology of Svalbard V. 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Ziegler, P.A. 1988: Evolution of the Arctic – North Atlantic and the western Tethys. American Association of Petroleum Geologists Memoir 43, 198 pp. 758 Manuscript received 21 February 1997; revision accepted 1 June 2000. 759 Appendix 1: List of all recorded palynomorph taxa Miospores: Anapiculatisporites sp. A. telephorus (Pautsch) Klaus 1960 Annulispora folliculosa (Rogalska) de Jersey 1959 Apiculatisporites parvispinosus (Leschik) Schulz 1963 A. sp. Araucariacites australis Cookson 1947 Baculatisporites sp. (Plate 1, fig. 12) B. wellmanii (Couper) Krutzsch 1959 Bisaccates indeterminate (Plate 2, fig. 9) Callialasporites dampieri (Balme) Dev 1961 (Plate 2, fig. 5) C. microvelatus Schulz 1966 C. minus (Tralau) Guy 1971 (Plate 2, fig. 3) C. sp. C. turbatus (Balme) Schulz 1967 Calamospora tener (Leschik) Mädler 1964 Camarozonozporites rudis (Leschik) Klaus 1960 C. sp. Campenia sp. Cerebropollenites macroverrucosus (Thiergart) Schulz 1967 (Plate 3, fig. 4) C. sp. C. thiergartii Schulz 1967 (Plate 3, fig. 1) Chasmatosporites apertus Nilsson 1958 (Plate 3, fig. 5) C. elegans Nilsson 1958 C. hians Nilsson 1958 C. major Nilsson 1958 (Plate 3, fig. 7) C. minor Nilsson 1958 C. sp. Chomotriletes minor (Kedves) Pocock 1970 C. sp. Cibotiumspora jurienensis (Balme) Filatoff 1975 Cingulizonates inequalis (Mädler) Lund 1977 Conbaculatisporites mesozoicus Klaus 1960 C. sp. Corollina meyeriana (Klaus) Venkatachala & Goczan 1964 C. sp. C. torosus (Reissinger) Cornet & Traverse 1975 (Plate 3, fig. 2) Deltoidospora minor (Couper) Pocock 1970 D. spp. (Plate 1, fig. 1) Densoisporites scanicus Tralau 1968 (Plate 1, fig. 9) D. velatus Weyland & Krieger 1953 Densosporites sp. D. variabilis (Waltz) Potonié & Kremp 1956 Eucommiidites major Schulz 1967 E. troedsonii Erdtman 1948 Exesipollenites tumulus Balme 1957 Foraminisporis jurassicus Schulz 1967 Fungal spores Iraquispora sp. Ischyosporites crateris Balme 1957 (Plate 1, fig. 7) I. sp. I. variegatus (Couper) Schulz 1967 (Plate 2, fig. 1) Kekryphalospora distincta Fenton & Riding 1987 (Plate 1, fig. 3) Kraeuselisporites reissingeri (Harris) Morbey 1975 (Plate 1, fig. 5) Leptolepidites major L. sp. (Plate 1, fig. 4) Limbosporites lundbladii Nilsson 1958 Lycopodiacidites rugulatus (Couper) Schulz 1967 (Plate 2, fig. 4) Manumia delcourtii (Pocock) Dybkjær 1991 (Plate 2, fig. 2) Marattisporites scabratus Couper 1958 Megaspore fragments Monosaccate pollen Monosulcites punctatus Orlowska-Zwolinska 1966 (Plate 2, fig. 6) Murospora sp. Neoraistrickia gristhorpensis (Couper) Tralau 1967 N. sp. N. taylori Playford & Dettmann 1965 Ovalispollis ovalis Krutzsch 1955 Perinopollenites elatoides Couper 1958 (Plate 3, fig. 3) Perinosporites thuringiacus Schulz 1962 Pinuspollenites minimus (Couper) Kemp 1970 (Plate 2, fig. 8) Polycingulatisporites circulus Simoncsics & Kedves 1961 P. triangularis (Bolkhovitina) Playford & Dettmann 1965 Quadraeculina anellaeformis Malyavkina 1949 (Plate 2, fig. 7) Retitriletes austroclavatoides (Cookson) Döring et al. 1963 R. clavatoides (Couper) Döring et al. 1963 R. semimuris (Danzé-Corsin & Laveine) McKellar 1974 R. sp. (Plate 1, fig. 8) Ricciisporites tuberculatus Lundblad 1954 Rogalskaisporites cicatricosus (Rogalska) Danzé-Corsin & Laveine 1963 (Plate 1, fig. 10) Sculptisporites aulosenensis (Schulz) Koppelhus 1992 Sestrosporites pseudoalveolatus (Couper) Dettmann 1963 Spheripollenites psilatus Couper 1958 S. subgranulatus Couper 1958 (Plate 3, figs 6, 8) Staplinisporites caminus (Balme) Pocock 1970 (Plate 1, fig. 11) Stereisporites antiquasporites (Wilson & Webster) Dettmann 1963 Stereisporites stereoides (Potonié & Venitz) H.D. Pflug in: Thomson & Pflug 1953 S. sp. Striatella jurassica Mädler 1964 S. parva (Li & Shang) Filatoff & Price 1988 S. scania (Nilsson) Filatoff & Price 1988 S. seebergensis Mädler 1964 (Plate 1, fig. 2) S. spp. Striate pollen 760 Taeniasporites rhaeticus Schulz 1967 T. sp. Taurocusporites verrucatus Schulz 1967 (Plate 1, fig. 6) Tigrisporites microrugulatus Schulz 1967 T. sp. Todisporites major Couper 1958 T. minor Couper 1958 T. sp. Triletes sp. Tripartina variabilis Malyavkina 1949 Uvaesporites argenteaeformis (Bolkhovitina) Schulz 1967 U. sp. Vesicaspora fuscus (Pautsch) Morbey 1975 Vitreisporites pallidus (Reissinger) Nilsson 1958 V. sp. Vittatina sp. Zebrasporites interscriptus (Thiergart) Klaus 1960 Phytoplankton: Acritarch spp. Baltisphaeridium sp. Beaumontella caminuspina (Wall) Below 1987 B. delicata (Wall) Below 1987 B. sp. Botryococcus spp. (Plate 6, figs 6, 7) Celyphus rallus Batten 1985 (Plate 7, fig. 1) C. spp. Crassosphaera sp. Cymatiosphaera sp. Dapcodinium sp. Dinocyst sp. (Plate 4, figs 8, 9) Dissiliodinium sp. (Plate 6, figs 4, 5) Kallosphaeridium sp. Lecaniella foveata Singh 1971 (Plate 7, fig. 5) L. spp. Leiofusa jurassica Cookson & Eisenack 1958 (Plate 7, fig. 2) Leiosphaeridia spp. Limbicysta bjaerkei (Smelror) MacRae et al. 1996 (Plate 6, figs 1–3) Luehndea spinosa Morgenroth 1970 (Plate 5, fig. 5) Mancodinium semitabulatum Morgenroth 1970 (Plate 5, figs 1, 2) M. sp. Mendicodinium groenlandicum (Pocock & Sarjeant) Davey 1979 M. reticulatum Morgenroth 1970 (Plate 5, figs 3, 4) M. sp. Micrhystridium exilium Wall 1965 M. fragile Deflandre 1937 M. intromittum Wall 1965 M. lymensis Wall 1965 M. spp. M. stellatum Deflandre 1942 M. wattonense Wall 1965 Nannoceratopsis ambonis (Drugg) Riding 1984 (Plate 4, fig. 4) N. dictyoambonis Riding 1984 N. gracilis Alberti emend. van Helden 1977 (Plate 4, figs 1, 3) N. plegas Drugg 1978 N. senex van Helden 1977 (Plate 4, fig. 2) N. sp. N. triangulata Prauss 1987 N. triceras Drugg 1978 Pareodinia halosa (Filatoff) Prauss 1989 (Plate 4, fig. 7) Parvocysta barbata Bjærke 1980 P. nasuta Bjærke 1980 P. sp. Phallocysta eumekes Dörhöfer & Davies 1980 (Plate 4, figs 5, 6) P. elongata (Beju) Riding 1994 Pterospermella spp. Scriniocassis sp. Susadinium scrofoides (Dörhöfer & Davies) Below 1987 Tasmanites sp. Tetraporina compressa Kondrat’ev 1963 (Plate 7, fig. 6) Valvaeodinium armatum Morgenroth 1970 V. spp. Veryhachium collectum Wall 1965 (Plate 7, fig. 3) V. formosum Stockmans & Williere 1960 (Plate 7, fig. 4) V. irregulare de Jekhowsky 1961 V. reductum (Deunff) de Jekhowsky 1961 V. sp. V. trispinosum (Eisenack) Deunff 1954 Wallodinium laganum Feist-Burkhardt & Monteil 1994 (Plate 5, fig. 6) W. spp. Others: Foraminifera spp. Foraminiferal linings (Plate 7, fig. 7) Haplophragmoides spp. Miscellaneous 761 Plates 1–7 762 Plate 1 Palynomorphs from the Neill Klinter Group at the Albuen section. The scale bar is 10 microns. For each of the illustrated specimens (Plates 1–7), the England Finder Reference (EFR) is given. Fig. 1. Deltoidospora sp. Sample 405414-3, EFR S291. Fig. 2. Striatella seebergensis. Sample 405466-3, EFR D34. Fig. 3. Kekryphalospora distincta. Sample 405466-3, EFR J383. Fig. 4. Leptolepidites sp. Sample 405423-3, EFR T40. Fig. 5. Kraeuselisporites reissingeri. Sample 405419-3, EFR D294. Fig. 6. Taurocusporites verrucatus. Sample 405466-3, EFR H273. Fig. 7. Ischyosporites crateris. Sample 405449-3, EFR W29. Fig. 8. Retitriletes sp. Sample 405420-3, EFR P50. Fig. 9. Densoisporites scanicus. Sample 405449-3, EFR P19. Fig. 10. Rogalskaisporites cicatricosus. Sample 405419-3, EFR L513. Fig. 11. Staplinisportes caminus. Sample 405449-3, EFR J462. Fig. 12. Baculatisporites sp. Sample 405414-3, EFR T353. 763 1 2 3 4 5 6 10 11 12 7 8 9 764 Plate 2 Palynomorphs from the Neill Klinter Group at the Albuen section. The scale bar is 10 microns. Fig. 1. Ischyosporites variegatus. Sample 405464-3, EFR G43. Fig. 2. Manumia delcourti. Sample 405449-3, EFR V244. Fig. 3. Callialasporites minus. Sample 405449-3, EFR J291. Fig. 4. Lycopodiacidites rugulatus. Sample 405401-4, EFR Z263. Fig. 5. Callialasporites dampieri. Sample 405449-3, EFR J203. Fig. 6. Monosulcites punctatus. Sample 405414-3, EFR T31. Fig. 7. Quadraeculina anellaeformis. Sample 405414-3, EFR K431. Fig. 8. Pinuspollenites minimus. Sample 405420-2, EFR V212. Fig. 9. Bisaccate sp., full dimensions 90 x 70 microns. Sample 405418-3, EFR P462. 765 1 2 4 7 9 8 5 6 3 766 Plate 3 Palynomorphs from the Neill Klinter Group at the Albuen section. The scale bar is 10 microns. Fig. 1. Cerebropollenites thiergartii. Sample 405401-4, EFR U252. Fig. 2. Corollina torosus. Sample 405466-3, EFR D171. Fig. 3. Perinopollenites elatoides. Sample 405453-3, EFR G243. Fig. 4. Cerebropollenites macroverrucosus. Sample 405454-3, EFR Y303. Fig. 5. Chasmatosporites apertus. Sample 405401-4, EFR Y363. Fig. 6. Spheripollenites subgranulatus. Sample 405459-3, EFR N293. Fig. 7. Chasmatosporites major. Sample 405423-3, EFR F51. Fig. 8. Spheripollenites subgranulatus. Sample 405459-3, EFR N20. 767 1 4 7 8 5 6 2 3 768 Plate 4 Palynomorphs from the Neill Klinter Group at the Albuen section. The scale bar is 10 microns. Fig. 1. Nannoceratopsis gracilis. Sample 405449-3, EFR N20. Fig. 2. N. senex. Sample 405466-3, EFR K211. Fig. 3. N. gracilis. Sample 405414-3, EFR O404. Fig. 4. N. ambonis. Sample 405453-3, EFR F383. Fig. 5. Phallocysta eumekes. Sample 405426-3, EFR V47. Fig. 6. P. eumekes. Sample 405459-3, EFR Y56. Fig. 7. Pareodinia halosa. Sample 405454-3, EFR V314. Fig. 8. Dinoflagellate sp. Sample 405419-3, EFR D40. Fig. 9. Dinoflagellate sp. Sample 405453-3, EFR E272. 769 1 4 7 5 8 2 3 6 9 770 Plate 5 Palynomorphs from the Neill Klinter Group at the Albuen section. The scale bar is 10 microns. Fig. 1. Mancodinium semitabulatum. Sample 405466-3, EFR H531. Fig. 2. M. semitabulatum. Sample 405411-3, EFR H37. Fig. 3. Mendicodinium reticulatum. Sample 405422-3, EFR M292. Fig. 4. M. reticulatum. Sample 405420-3, EFR F381. Fig. 5. Luehndea spinosa. Sample 405466-3, EFR F554. Fig. 6. Wallodinium laganum. Sample 405452-3, EFR F573 771 1 2 3 4 5 6 772 Plate 6 Palynomorphs from the Neill Klinter Group at the Albuen section. The scale bar is 10 microns. Fig. 1. Limbicysta bjaerkei. Sample 405456-3, EFR N244. Fig. 2. L. bjaerkei. Sample 405449-3, EFR E221. Fig. 3. L. bjaerkei. Sample 405405-3, EFR R484. Fig. 4. Dissiliodinium sp. Sample 405454-3, EFR P204. Fig. 5. Dissiliodinium sp. Sample 405456-3, EFR H304. Fig. 6. Botryococcus sp. Sample 405401-4, EFR X334. Fig. 7. Botryococcus sp. Sample 405401-4, EFR T242. 773 1 2 4 6 7 5 3 774 Plate 7 Palynomorphs from the Neill Klinter Group at the Albuen section. The scale bar is 10 microns; this scale bar is not applicable to figure 7. Fig. 1. Celyphus rallus. Sample 405466-3, EFR E21. Fig. 2. Leiofusa jurassica. Sample 405414-3, EFR O404. Fig. 3. Veryhachium collectum. Sample 405414-3, EFR O403. Fig. 4. V. formosus. Sample 405408-3, EFR L353. Fig. 5. Lecaniella foveata. Sample 405454-3, EFR W401. Fig. 6. Tetraporina compressa. Sample 405419-3, EFR K504. Fig. 7. Foraminiferal lining, 132 microns in diameter. Sample 405464-3, EFR P292. 775 1 2 543 6 7 Albuen (A) Lo w er Ju ra ss ic M A To ar ci an O st re ae lv F or m at io n G ul e H or n Fo rm at io n Sk æ vd al M em be r N at ho rs t Fj el d M em be r A lb ue n M b A s El is B je rg M em be r Tr ef jo rd B je rg M b L. P lie ns ba ch ia n U pp er P lie ns ba ch ia n 439.00 438.50 434.00 432.00 431.50 428.00 425.90 416.50 411.50 402.00 392.00 379.40 377.50 375.50 369.50 367.50 366.20 365.00 363.00 361.30 359.00 297.80 295.40 294.20 292.20 290.75 290.20 287.80 287.00 284.70 283.40 273.80 271.00 267.40 264.27 264.25 256.50 253.40 250.50 249.00 247.40 246.00 241.00 240.00 238.20 238.00 236.80 231.70 229.80 229.50 229.40 229.00 222.50 215.50 213.00 211.00 341248 397452 405449 341247 405450 405451 405452 405453 405454 405455 405456 405457 341243 405458 405459 341245 405460 341241 405462 405464 405466 405434 405433 405432 405431 405430 405429 341236 405428 405427 405426 405425 341235 405424 405423 405422 341234 405421 405420 341233 405419 405418 405417 405416 405414 405413 405411 405410 405408 341232 405406 405405 405404 405403 405402 405401 1 Ro ga lsk ai sp or ite s ci ca tr ic os us 2 Co nb ac ul at isp or ite s m es oz oi cu s 3 Ly co po di ac id ite s ru gu la tu s 4 D el to id os po ra s pp . 5 Re tit ril et es c la va to id es 6 Re tit ril et es s em im ur is 7 Re tit ril et es s p. 8 Ba cu la tis po rit es s p. 9 Ti gr isp or ite s m ic ro ru gu la tu s 10 Fo ra m in isp or is ju ra ss ic us 11 Kr ae us el isp or ite s re iss in ge ri 12 Tr ip ar tin a va ria bi lis 13 St er ei sp or ite s st er eo id es 14 D en so isp or ite s sc an ic us 15 Re tit ril et es a us tr oc la va to id es 16 To di sp or ite s m in or 17 Ke kr yp ha lo sp or a di st in ct a 18 Ci bo tiu m sp or ite s ju rie ne ns is 19 St ria te lla p ar va 20 To di sp or ite s m aj or 21 St ria te lla ju ra ss ic a 22 Le pt ol ep id ite s sp . 23 Z eb ra sp or ite s in te rs cr ip tu s 24 St er ei sp or ite s an tiq ua sp or ite s 25 U va es po rit es a rg en te ae fo rm is 26 Tr ile te s sp . 27 St ria te lla s pp . 28 St ria te lla s ee be rg en sis 29 Ch om ot ril et es s p. 30 M eg as po re fr ag m en ts 31 An ap ic ul at isp or ite s sp . 32 An ap ic ul at isp or ite s te le ph or us 33 N eo ra ist ric ki a sp . 34 Ta ur oc us po rit es v er ru ca tu s 35 D en so isp or ite s ve la tu s 36 Sc ul pt isp or ite s au lo se ne ns is 37 U va es po rit es s p. 38 To di sp or ite s sp . 39 M an um ia d el co ur tii 40 Is ch yo sp or ite s va rie ga tu s 41 Is ch yo sp or ite s cr at er is 42 St ap lin isp or ite s ca m in us 43 Po lyc in gu la tis po rit es tr ia ng ul ar is 44 Se st ro sp or ite s ps eu do al ve ol at us 45 Po lyc in gu la tis po rit es c irc ul us 46 N eo ra ist ric ki a ta ylo rii 47 Le pt ol ep id ite s m aj or 48 Li m bo sp or ite s lu nd bl ad ii 49 M ur os po ra s p. 50 Ch as m at os po rit es h ia ns 51 Ce re br op ol le ni te s th ie rg ar tii 52 Ve sic as po ra fu sc us 53 Q ua dr ae cu lin a an el la ef or m is 54 Pe rin op ol le ni te s el at oi de s 55 Pi nu sp ol le ni te s m in im us 56 Bi sa cc at e sp p. 57 Ce re br op ol le ni te s m ac ro ve rr uc os us 58 Ch as m at os po rit es m aj or 59 Ch as m at os po rit es a pe rt us 60 Co ro llin a to ro su s 61 M on os ul ci te s pu nc ta tu s 62 Ch as m at os po rit es s p. 63 Ch as m at os po rit es e le ga ns 64 M on os ac ca te s pp . 65 Vi tr ei sp or ite s pa llid us 66 Ca llia la sp or ite s da m pi er i 67 Ca llia la sp or ite s sp . 68 Ar au ca ria ci te s au st ra lis 69 Eu co m m iid ite s tr oe ds on ii 70 Ce re br op ol le ni te s sp . 71 Sp he rip ol le ni te s su bg ra nu la tu s 72 Ca m pe ni a sp . 73 Ca llia la sp or ite s m ic ro ve la tu s 74 Ca llia la sp or ite s m in us 75 Ex es ip ol le ni te s tu m ul us 76 Ca llia la sp or ite s tr ilo ba tu s 77 Ca llia la sp or ite s tu rb at us 78 Eu co m m iid ite s m aj or 79 Ri cc iis po rit es tu be rc ul at us 80 Ta en ia sp or ite s sp . 81 St ria te s pp . ? ? ? R R ? ? R R R R R R R R Alphabetical species list 31 Anapiculatisporites sp. 32 Anapiculatisporites telephorus 68 Araucariacites australis 8 Baculatisporites sp. 56 Bisaccate spp. 66 Callialasporites dampieri 73 Callialasporites microvelatus 74 Callialasporites minus 67 Callialasporites sp. 76 Callialasporites trilobatus 77 Callialasporites turbatus 72 Campenia sp. 57 Cerebropollenites macroverrucosus 70 Cerebropollenites sp. 51 Cerebropollenites thiergartii 59 Chasmatosporites apertus 63 Chasmatosporites elegans 50 Chasmatosporites hians 58 Chasmatosporites major 62 Chasmatosporites sp. 29 Chomotriletes sp. 18 Cibotiumsporites jurienensis 2 Conbaculatisporites mesozoicus 60 Corollina torosus 4 Deltoidospora spp. 14 Densoisporites scanicus 35 Densoisporites velatus 78 Eucommiidites major 69 Eucommiidites troedsonii 75 Exesipollenites tumulus 10 Foraminisporis jurassicus 41 Ischyosporites crateris 40 Ischyosporites variegatus 17 Kekryphalospora distincta 11 Kraeuselisporites reissingeri 47 Leptolepidites major 22 Leptolepidites sp. 48 Limbosporites lundbladii 3 Lycopodiacidites rugulatus 39 Manumiadel courtii 30 Megaspore fragments 64 Monosaccate spp. 61 Monosulcites punctatus 49 Murospora sp. 33 Neoraistrickia sp. 46 Neoraistrickia taylorii 54 Perinopollenites elatoides 55 Pinuspollenites minimus 45 Polycingulatisporites circulus 43 Polycingulatisporites triangularis 53 Quadraeculinaanellae formis 15 Retitriletes austroclavatoides 5 Retitriletes clavatoides 6 Retitriletes semimuris 7 Retitriletes sp. 79 Ricciisporites tuberculatus 1 Rogalskaisporites cicatricosus 36 Sculptisporites aulosenensis 44 Sestrosporites pseudoalveolatus 71 Spheripollenites subgranulatus 42 Staplinisporites caminus 24 Stereisporites antiquasporites 13 Stereisporites stereoides 81 Striate sp. 21 Striatella jurassica 19 Striatella parva 28 Striatella seebergensis 27 Striatella sp. 80 Taeniasporites sp. 34 Taurocusporites verrucatus 9 Tigrisporites microrugulatus 20 Todisporites major 16 Todisporites minor 38 Todisporites sp. 26 Triletes sp. 12 Tripartina variabilis 25 Uvaesporites argenteaeformis 37 Uvaesporites sp. 52 Vesicaspora fuscus 65 Vitreisporites pallidus 23 Zebrasporites interscriptus 400 380 360 300 280 260 240 220 420 Interval not sampled Sy st em St ag e Pa ly no lo gi ca l A ss em bl . Z on es Li th os tr at ig ra ph y (m ) Sa m pl e he ig ht Sa m pl e nu m be r 7 6 5 4 3 2 1 Uncertain determination Very rare Rare Few Common Abundant ? R Fig. 4A. Terrestrial palynomorph distribution chart for the Gule Horn and Ostreaelv Formations at Albuen (for location, see Fig. 1). M, Middle Jurassic; A, Aalenian; As, Astartekløft Member. Albuen (B) 439.00 438.50 434.00 432.00 431.50 428.00 425.90 416.50 411.50 402.00 392.00 379.40 377.50 375.50 369.50 367.50 366.20 365.00 363.00 361.30 359.00 292.20 287.80 287.00 284.70 283.40 273.80 271.00 267.40 264.27 264.25 256.50 253.40 250.50 249.00 247.40 246.00 241.00 240.00 238.20 238.00 236.80 231.70 229.80 229.50 229.40 229.00 222.50 215.50 213.00 211.00 341248 397452 405449 341247 405450 405451 405452 405453 405454 405455 405456 405457 341243 405458 405459 341245 405460 341241 405462 405464 405466 405431 341236 405428 405427 405426 405425 341235 405424 405423 405422 341234 405421 405420 341233 405419 405418 405417 405416 405414 405413 405411 405410 405408 341232 405406 405405 405404 405403 405402 405401 1 N an no ce ra to ps is se ne x 2 N an no ce ra to ps is sp . 3 N an no ce ra to ps is gr ac ilis 4 M en di co di ni um r et ic ul at um 5 Be au m on te lla c am in us pi na 6 N an no ce ra to ps is tr ia ng ul at a 7 N an no ce ra to ps is pl eg as 8 M an co di ni um s em ita bu la tu m 9 Pa rv oc ys ta b ar ba ta 10 M en di co di ni um g ro en la nd ic um 11 Be au m on te lla d el ic at a 12 M en di co di ni um s p. 13 Lu eh nd ea s pi no sa 14 D in oc ys t sp . 15 Va lva eo di ni um a rm at um 16 Va lva eo di ni um s pp . 17 N an no ce ra to ps is am bo ni s 18 D iss ilio di ni um s p. 19 Pa rv oc ys ta s p. 20 Ph al lo cy st a eu m ek es 21 N an no ce ra to ps is tr ic er as 22 Pa re od in ia h al os a 23 Ka llo sp ha er id iu m s p. 24 Sc rin io ca ss is sp . 25 Ph al lo cy st a el on ga ta 26 W al lo di ni um s pp . 27 A cr ita rc h sp p. 28 Le io fu sa ju ra ss ic a 29 Le io sp ha er id ia s pp . 30 M ic rh ys tr id iu m ly m en sis 31 M ic rh ys tr id iu m s pp . 32 Ve ry ha ch iu m fo rm os um 33 Li m bi cy st a bj ae rk ei 34 Ve ry ha ch iu m c ol le ct um 35 Te tr ap or in a co m pr es sa 36 Le ca ni el la fo ve at a 37 Ve ry ha ch iu m r ed uc tu m 38 Ve ry ha ch iu m ir re gu la re 39 M ic rh ys tr id iu m in tr om itt um 40 M ic rh ys tr id iu m w at to ne ns e 41 M ic rh ys tr id iu m fr ag ile 42 Ve ry ha ch iu m tr isp in os um 43 M ic rh ys tr id iu m s te lla tu m 44 Cy m at io sp ha er a sp . 45 Be au m on te lla s p. 46 Pt er os pe rm el la s pp . 47 Bo tr yo co cc us s pp . 48 Ta sm an ite s sp . 49 Le ca ni el la s pp . 50 Fu ng al s po re s 51 Ce lyp hu s sp p. 52 H ap lo ph ra gm oi de s sp p. 53 M is ce lla ne ou s sp p. ? ? ? ? ? ? ? Alphabetical species list 27 Acritarch spp. 5 Beaumontella caminuspina 11 Beaumontella delicata 45 Beaumontella sp. 47 Botryococcus spp. 51 Celyphus spp. 44 Cymatiosphaera sp. 14 Dinocyst sp. 18 Dissiliodinium sp. 50 Fungal spores 52 Haplophragmoides spp. 23 Kallosphaeridium sp. 36 Lecaniella foveata 49 Lecaniella spp. 28 Leiofusa jurassica 29 Leiosphaeridia spp. 33 Limbicysta bjaerkei 13 Luehndea spinosa 53 Miscellaneous spp. 8 Mancodinium semitabulatum 10 Mendicodinium groenlandicum 4 Mendicodinium reticulatum 12 Mendicodinium sp. 41 Micrhystridium fragile 39 Micrhystridium intromittum 30 Micrhystridium lymensis 31 Micrhystridium spp. 43 Micrhystridium stellatum 40 Micrhystridium wattonense 17 Nannoceratopsis ambonis 3 Nannoceratopsis gracilis 7 Nannoceratopsis plegas 1 Nannoceratopsis senex 2 Nannoceratopsis sp. 6 Nannoceratopsis triangulata 21 Nannoceratopsis triceras 22 Pareodinia halosa 9 Parvocysta barbata 19 Parvocysta sp. 25 Phallocysta elongata 20 Phallocysta eumekes 46 Pterospermella spp. 24 Scriniocassis sp. 48 Tasmanites sp. 35 Tetraporina compressa 15 Valvaeodinium armatum 16 Valvaeodinium spp. 34 Veryhachium collectum 32 Veryhachium formosum 38 Veryhachium irregulare 37 Veryhachium reductum 42 Veryhachium trispinosum 26 Wallodinium spp. Sy st em St ag e Pa ly no lo gi ca l A ss em bl . Z on es Li th os tr at ig ra ph y (m ) Sa m pl e he ig ht Sa m pl e nu m be r Interval not sampled 1 2 3 4 5 6 7 Lo w er Ju ra ss ic M A To ar ci an O st re ae lv F or m at io n G ul e H or n Fo rm at io n Sk æ vd al M em be r N at ho rs t Fj el d M em be r A lb ue n M b A s El is B je rg M em be r Tr ef jo rd B je rg M b L. P lie ns ba ch ia n U pp er P lie ns ba ch ia n 400 380 360 300 280 260 240 220 420 Uncertain determination Very rare Rare Few Common Abundant ? R Fig. 4B. Marine palynomorph distribution chart for the Gule Horn and Ostreaelv Formations at Albuen (for location, see Fig. 1). M, Middle Jurassic; A, Aalenian; As, Astartekløft Member. Lepidopteriselv Lo w er Ju ra ss ic U pp er P lie ns ba ch ia n G ul e H or n Fo rm at io n El is B je rg M em be r 700.00 695.00 685.00 679.00 674.00 654.00 653.00 648.00 642.00 638.00 139146 139145 139144 139143 139142 139141 139140 139139 139138 139137 1 Ba cu la tis po rit es s p. 2 D el to id os po ra s pp . 3 Ca la m os po ra te ne r 4 To di sp or ite s m aj or 5 Ro ga lsk ai sp or ite s ci ca tr ic os us 6 St ria te lla p ar va 7 Re tit ril et es a us tr oc la va to id es 8 Re tit ril et es c la va to id es 9 N eo ra ist ric ki a sp . 10 St er ei sp or ite s st er eo id es 11 Re tit ril et es s em im ur is 12 Kr ae us el isp or ite s re iss in ge rii 13 Re tit ril et es s p. 14 Ti gr isp or ite s m ic ro ru gu la tu s 15 Ap ic ul at isp or ite s pa rv isp in os us 16 Co nb ac ul at isp or ite s m es oz oi cu s 17 D en so isp or ite s sc an ic us 18 Ly co po di ac id ite s ru gu la tu s 19 Ira qu isp or a sp . 20 Ti gr isp or ite s sp . 21 Tr ip ar tin a va ria bi lis 22 Ke kr yp ha lo sp or a di st in ct a 23 An ap ic ul at isp or ite s sp . 24 M ar at tii sp or ite s sc ab ra tu s 25 D el to id os po ra m in or 26 An nu lis po ra fo llic ul os a 27 Ap ic ul at isp or ite s sp . 28 St ria te lla ju ra ss ic a 29 D en so sp or ite s sp . 30 D en so sp or ite s va ria bi lis 31 Ca m ar oz on os po rit es r ud is 32 M ur os po ra s p. 33 Q ua dr ae cu lin a an el la ef or m is 34 Bi sa cc at e sp p. 35 Pe rin op ol le ni te s el at oi de s 36 Ch as m at os po rit es h ia ns 37 Pi nu sp ol le ni te s m in im us 38 Ch as m at os po rit es a pe rt us 39 Ce re br op ol le ni te s th ie rg ar tii 40 Co ro llin a to ro su s 41 M on os ul ci te s pu nc ta tu s 42 Ce re br op ol le ni te s m ac ro ve rr uc os us 43 Ve sic as po ra fu sc us 44 Ch as m at os po rit es m aj or 45 Ar au ca ria ci te s au st ra lis 46 Sp he rip ol le ni te s ps ila tu s 47 Ca llia la sp or ite s tu rb at us 48 Ca llia la sp or ite s m in us 49 Eu co m m iid ite s tr oe ds on ii 50 M on os ac ca te s pp . 51 Co ro llin a sp p. 52 Vi tta tin a sp . 53 M en di co di ni um r et ic ul at um 54 M an co di ni um s em ita bu la tu m 55 N an no ce ra to ps is se ne x 56 N an no ce ra to ps is tr ia ng ul at a 57 N an no ce ra to ps is gr ac ilis 58 N an no ce ra to ps is sp . 59 M ic rh ys tr id iu m in tr om itt um 60 Ve ry ha ch iu m tr isu lc um 61 M ic rh ys tr id iu m fr ag ile 62 Le ca ni el la s pp . 63 M ic rh ys tr id iu m ly m en sis 64 Ve ry ha ch iu m s p. 65 Bo tr yo co cc us s pp . 66 Ta sm an ite s sp . ? R R ? R ? R ? Alphabetical species list 23 Anapiculatisporites sp. 26 Annulispora folliculosa 15 Apiculatisporites parvispinosus 27 Apiculatisporites sp. 45 Araucariacites australis 1 Baculatisporites sp. 34 Bisaccate spp. 65 Botryococcus spp. 3 Calamospora tener 48 Callialasporites minus 47 Callialasporites turbatus 31 Camarozonosporites rudis 42 Cerebropollenites macroverrucosus 39 Cerebropollenites thiergartii 38 Chasmatosporites apertus 36 Chasmatosporites hians 44 Chasmatosporites major 16 Conbaculatisporites mesozoicus 51 Corollina sp. 40 Corollina torosus 25 Deltoidospora minor 2 Deltoidospora spp. 17 Densoisporites scanicus 29 Densosporites sp. 30 Densosporites variabilis 49 Eucommiidites troedsonii 19 Iraquispora sp. 22 Kekryphalospora distincta 12 Kraeuselisporites reissingerii 62 Lecaniella spp. 18 Lycopodiacidites rugulatus 54 Mancodinium semitabulatum 24 Marattiisporites scabratus 53 Mendicodinium reticulatum 61 Micrhystridium fragile 59 Micrhystridium intromittum 63 Micrhystridium lymensis 50 Monosaccate spp. 41 Monosulcites punctatus 32 Murospora sp. 57 Nannoceratopsis gracilis 55 Nannoceratopsis senex 58 Nannoceratopsis sp. 56 Nannoceratopsis triangulata 9 Neoraistrickia sp. 35 Perinopollenites elatoides 37 Pinuspollenites minimus 33 Quadraeculina anellaeformis 7 Retitriletes austroclavatoides 8 Retitriletes clavatoides 11 Retitriletes semimuris 13 Retitriletes sp. 5 Rogalskaisporites cicatricosus 46 Spheripollenites psilatus 10 Stereisporites stereoides 28 Striatella jurassica 6 Striatella parva 66 Tasmanites sp. 14 Tigrisporites microrugulatus 20 Tigrisporites sp. 4 Todisporites major 21 Tripartina variabilis 64 Veryhachium sp. 60 Veryhachium trisulcum 43 Vesicaspora fuscus 52 Vittatina sp. Sy st em St ag e Pa ly no lo gi ca l A ss em bl . Z on es Li th os tr at ig ra ph y (m ) Sa m pl e he ig ht Sa m pl e nu m be r 700 675 650 3 2 Uncertain determination Very rare Rare Few Common Abundant ? R Fig. 13. Palynomorph distribution chart for the Gule Horn Formation (Elis Bjerg Member) at Lepidopteriselv (for location, see Fig. 1).