Geological Survey of Denmark and Greenland Bulletin 1, 777-811 777 The Middle Jurassic Sortehat Formation of the East Greenland rift basin is a distinctive and laterally per- sistent mudstone-dominated succession sandwiched between the sandstone-dominated Ostreaelv Formation beneath and the sandstones of the Pelion Formation above (Figs 1, 2). The stratigraphic terminology adapted Palynostratigraphy and palaeoenvironment of the Middle Jurassic Sortehat Formation (Neill Klinter Group), Jameson Land, East Greenland Eva B. Koppelhus and Carina F. Hansen The grey–black mudstones of the Sortehat Formation form part of the Middle Jurassic fill of the Jameson Land Basin in East Greenland. The formation is exposed in the southernmost part of the north–south-trending, Mesozoic rift system in East Greenland that was part of the epeiric sea- way between East Greenland and Norway. Sedimentological observations of the Sortehat Formation indicate deposition in an offshore marine setting that was typically low energy and periodically oxygen-deficient but was influenced by storm currents on occasion. Detailed palynological stud- ies of the Sortehat Formation have resulted in the definition of three palynological assemblage zones recognised at four localities, namely Enhjørningen Dal and Pelion (north Jameson Land), the type section at Sortehat (central Jameson Land) and Albuen at Neill Klinter along Hurry Inlet (south-east Jameson Land). In stratigraphic order, these zones are termed the Botryococcus Assemblage Zone, the Nannoceratopsis gracilis – Nannoceratopsis senex Assemblage Zone, and the Sentusidinium pelionense Assemblage Zone. They are recognised on the basis of the iden- tification of approximately 110 species of palynomorphs, including 45 species of spores, 30 of pollen, 22 of dinoflagellate cysts, 10 acritarch species, two species of algae, and some fungal spores. An Aalenian – ?Early Bajocian age is suggested for the Sortehat Formation on the basis of the palynoflora. Interpretation of the palynomorph assemblages suggests that the formation accumulated in a shallow, brackish marine environment. A significant terrestrial input, including the freshwater green alga Botryococcus, is recorded in the lower part of the formation and interpreted as an allochtho- nous accumulation in an offshore marine environment related to transgression of a low-lying coastal plain. A marked shift in the palynomorph assemblage seen by diversification of marine microplankton above the base of the formation, indicates an increase in the marine signal prob- ably related to the onset of highstand conditions following the marine transgression. Keywords: East Greenland, Jameson Land Basin, Middle Jurassic, Aalenian – ?Early Bajocian, palynostratigraphy, sedimentology, palaeoenvironment, transgressive–highstand mudstones, allochthonous Botryococcus assemblage E.B.K., Geological Survey of Denmark and Greenland, Geocenter Copenhagen, Øster Voldgade 10, DK-1350 Copenhagen K, Denmark. Present address: Royal Tyrrell Museum of Palaeontology, Box 7500, Drumheller T0J 0Y0, Alberta, Canada. E-mail: evakoppelhus@hotmail.com C.F.H., Geological Institute, University of Copenhagen, Geocenter Copenhagen, Øster Voldgade 10, DK-1350 Copenhagen K, Denmark. Present address: Skovhegnet 4, DK-3460 Birkerød, Denmark. Geological Survey of Denmark and Greenland Bulletin 1, 777–811 (2003) © GEUS, 2003 in this paper follows the revised scheme of Dam & Surlyk (1998). Although the biostratigraphy and sequence stratigraphy of the sandy formations have been the sub- ject of considerable study in recent years (Engkilde & Surlyk 1993; Engkilde 1994; Dam & Surlyk 1995; Engkilde & Surlyk 2003, this volume; Koppelhus & Dam 2003, this volume), the precise age, the nature of the bound- aries and the depositional history of the Sortehat Formation remain poorly understood. The aim of this paper, therefore, is to present the results of a detailed palynological study of these strata that was undertaken in close co-operation with a sedimentological and sequence stratigraphic study (Hansen 1999). In partic- ular, this paper focuses on establishing the age of the Sortehat Formation, elucidation of the stratigraphic sig- nificance of the formation boundaries and contributing to an understanding of the depositional history of the Sortehat Formation. Regional setting and stratigraphy The Middle Jurassic Sortehat Formation is exposed in the Jameson Land Basin in the southernmost part of the north–south-trending, failed-rift system in East Greenland (Fig. 1). Rifting was initiated in the late Palaeozoic, and 778 25 km 100 km Illoqqortoormiut 22°W24°W 72¡ 72°N 71°N Sortehat Formation Study locality Scoresby Sund Jameson Land Li ve rp oo l L an d Scoresby Land Kong Oscar Fjord Pelion Lepidopteriselv Enhjørningen Dal Albuen Vardekløft Primulaelv Harris Fjeld H u rr y In le t Sortehat Dusén Bjerg Fle m in g Fjo rd Car lsb er g F jor d Liaselv I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I I II I I I I I I I I I I I I I I Hold with Hope Geographical Society Ø Gauss Halvø Traill Ø Kejser Franz Joseph Fjord Kong Oscar Fjord Scoresby Sund Jameson Land Milne Land Liverpool Land 72°N 71°N 73°N 24°WA B N G re en la nd 25 km Normal fault Inferred cross-fault I I G re en la nd Jameson Land Basin Fig. 1. A: Map showing the outcrop of the Sortehat Formation in the Jameson Land Basin; the outcrop pattern is aligned roughly north–south, parallel to the basin axis. B: Structural outline of the southern part of the East Greenland rift basin. The Jameson Land Basin was bounded by faults to the east, west and north, and by the Liverpool Land high towards the east. The nature of the south- ern boundary is unknown. The structural setting suggests an elongate semi-enclosed basin during deposition of the Sortehat Formation. Modified from Engkilde & Surlyk (1993). from Late Permian through Mesozoic times the basin was characterised by relatively uniform thermal subsi- dence interrupted by periods of faulting (Surlyk et al. 1981; Surlyk 1990a). The basin was bounded to the west by a major, approximately north–south-trending fault zone and to the east by faults and the elongated NNE–SSW-trending Liverpool Land high (Fig. 1; Surlyk et al. 1981; Surlyk 1990a). To the north, the basin was bounded by a number of NW–SE-trending cross-faults in Kong Oscar Fjord. The southern boundary is unknown but the basin probably extended further south under the present-day Scoresby Sund. The original extent of the Sortehat Formation is not known in detail, but during Middle Jurassic time it probably covered the present land area of Jameson Land and Scoresby Land (Fig. 1). It was deposited in an elongate, semi-enclosed seaway, connected in the south with the epeiric Jurassic seaway between Greenland and Norway (Surlyk et al. 1981). The Sortehat Formation, as adopted here, was orig- inally erected as the lower member (the Sortehat Member) of the Vardekløft Formation (Surlyk et al. 1973). It was raised to the status of formation by Surlyk (1990b, fig. 3); formal definition of the Sortehat Formation as the uppermost formation of the Neill Klinter Group was undertaken by Dam & Surlyk (1998). The type locality of the Sortehat Formation at Sortehat (Fig. 1A) is identical to that of the former Sortehat Member (Surlyk et al. 1973). 779 Fig. 2. Lithostratigraphy of the Jurassic of Jameson Land, East Greenland showing the stratigraphic position of the Sortehat Formation in the uppermost Neill Klinter Group. Modified from Surlyk (2003, this volume, fig. 5). The boundary between the Ostreaelv Formation and the Sortehat Formation is sharp and erosive in the northern proximal part of the basin and truncates shoreface deposits (indi- cated by the wavy line). At southern localities, the offshore mudstones of the Sortehat Formation gradationally overlie transgressive lower shoreface to offshore deposits. The Sortehat Formation thins towards the south. The heterolithic unit in the lowermost part of the formation also thins towards the south. The upper boundary of the Sortehat Formation is erosional (wavy line) and may record a minor hiatus. Thickness (m) Formation 100–400 60–110 290–420 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 Sandstone Sandstone/mudstone heterolith Mudstone Pelion Fm Ostreaelv Fm Sortehat Fm ? ? NS The Sortehat Formation overlies the sandstone-dom- inated Ostreaelv Formation (Figs 2, 3) which records deposition within a shallow wave, storm and tidally influenced marine embayment (Dam & Surlyk 1995, 1998). The boundary with the overlying black mud- stones of the Sortehat Formation is distinct at all local- ities but changes from a sharp ravinement surface in northern localities to a gradational drowning surface in southern localities (Figs 3, 4; Hansen 1999). The Sortehat Formation is 60–100 m thick and is overlain by the sandy, marine Pelion Formation (Fig. 2); the boundary is sharp throughout the basin. Sedimentologically, the boundary between the Ostreaelv and Sortehat Formations represents a land- wards shift in facies and a rise in relative sea level. The contact is interpreted as a transgressive erosional sur- face (Surlyk 1990a, b; Hansen & Surlyk 1994, Hansen 1999) and marks a basinwide flooding event within an overall transgressive period. The upper boundary of the Sortehat Formation represents a seawards shift in facies related to a fall in sea level and is interpreted as a marine erosional surface formed during forced regres- sion (Surlyk 1990a, b; Engkilde & Surlyk 1993). Facies and depositional setting The Sortehat Formation consists of dark grey to black mudstones with subordinate heterolithic levels (Figs 3, 4). The formation thins southwards away from the north- ern basin margin, from 100 m at Enhjørningen Dal to 60 m at Albuen (Fig. 4). A discrete, heterolithic unit of interbedded mudstones, sandstones and siltstones, 20 m thick, occurs at the base of the formation at the north- ern locality of Enhjørningen Dal; this unit thins to 8 m at the type locality of the Sortehat Formation and ulti- mately wedges out towards the south (Figs 3, 4). Mudstone facies The mudstones of the Sortehat Formation are darker and more fissile in the lowermost part of the formation and generally become lighter upwards, changing from black at the base to dark grey at the top. The dark grey mud- stones, which dominate the formation, commonly appear structureless but locally show bioturbated fabrics, includ- ing subhorizontal traces such as Curvolithus isp. and Planolites-like burrows and, near the top of the for- mation, some vertical traces referred to Diplocraterion isp. The black mudstones, in contrast, show a well- developed coarse parallel lamination formed by an alternation of thin sand/siltstone layers and mudstone layers. The mudstones contain plant debris and cal- careous concretions are present locally. Macrofossils include belemnites and ostreid bivalves. Both mudstone facies are broadly interpreted as hav- ing been deposited from suspension below wave base in an offshore environment. The lack of bioturbation in the black mudstone facies suggests that the sea floor was periodically inhospitable, probably due to poor oxygenation. Sandstone facies The interbedded sandstone layers from the heterolithic levels are very fine- to medium-grained; they locally show well-developed wave ripples but more commonly appear as lenses and streaks of sandstone, 2–15 mm thick, reflecting incipient ripple development (Fig. 3C; cf. the ‘incipient lenses’ of de Raaf et al. 1977). Laterally persistent sandstone layers, 5–30 cm thick, are present locally and show hummocky cross-stratification (Fig. 3C). The trace fossils Ophiomorpha nodusa and Pelecypod- ichnus amygdaloides occur in some of the sandstone layers. The basal heterolithic unit records deposition in the upper offshore – offshore transition zone, influenced by storm sand deposition on a muddy shelf. The persistent hummocky cross-stratified sand sheets represent higher energy storm events above storm wave base. The bio- turbation associated with the sandstones indicates well- aerated bottom-water conditions, at least on occasion. Depositional setting The preliminary interpretation is that the black to dark grey mudstones that dominate the formation were deposited from suspension. In combination with the thin storm sand layers, the mudstones indicate deposition in an offshore environment, probably a muddy, shal- low epeiric sea. The basal thick heterolithic unit at Enhjørningen Dal and Sortehat records northwards shoreface retreat prior to final drowning of the entire basin. A detailed sedimentological and sequence strati- graphic analysis of the Sortehat Formation was pre- sented by Hansen (1999). 780 781 A Fig. 3. A: The Sortehat Formation at the southernmost locality, Albuen, Neill Klinter. The Sortehat Formation consists mainly of dark grey to black mudstones deposited in an offshore environment. The boundary with the underlying fully marine sandy Ostreaelv Formation (arrow) is a particularly distinctive facies boundary within the Mesozoic succession of the East Greenland rift basin and represents a marine flooding event. The profile shown is c. 80 m thick. B: The lower, heterolithic unit of the Sortehat Formation at the northern locality of Enhjørningen Dal (basal boundary marked by arrow; c. 15 m of the Sortehat Formation illustrated). C: In contrast to the shaly appearance at the southern locality of Albuen (see Fig. 3A), this 20 m thick heterolithic unit at Enhjørningen Dal consists of stacked coarsening-upwards units (arrow); the example illustrated here passes up from mudstone (m) to hummocky cross-stratified sandstone (HCS). These stacked units probably record repeated slowing of transgression and shoreline progradation at the northern basin margin. Measuring rule (centre left) is 20 cm long. B C Previous work The age of the Sortehat Formation is not well known. Belemnites have been collected from the formation but to date have not been systematically identified. According to Dam & Surlyk (1998), belemnites from the upper lev- els of the underlying Ostreaelv Formation were col- lected by Rosenkrantz (1934) and studied by Doyle (1991); the belemnite ‘Parabrachybelus’ subadunca- tus from this level probably has a range restricted to the latest Toarcian Levesquei Zone (Doyle 1991). The ammonite Cranocephalites borealis has been found in the basal beds of the Pelion Formation, overlying the Sortehat Formation, indicating an age not younger than early Late Boreal Bajocian for these beds (Surlyk et al. 1973; Callomon 1993). The dark shales of the Sortehat Formation have been subjected to three palynological studies and a geo- chemical study (Fensome 1979; Lund & Pedersen 1985; Krabbe et al. 1994; Underhill & Partington 1994) although none of these studies were based on a comprehensive, closely-spaced sampling programme. Three samples from the Sortehat Formation were analysed for dinofla- gellate cysts by Fensome (1979). One sample (144112) 782 9 8 7 6 0 Sentusidinium pelionense Assemblage Zone Nannoceratopsis gracilis – Nannoceratopsis senex Assemblage Zone Botryococcus sp. Assemblage Zone Perinopollenites elatoides Assemblage Zone 0 100 m 90 80 70 60 50 40 30 20 10 60 m 50 40 30 20 10 60 m 50 40 30 20 10 0 Mudstone Pebbles Belemnites Bivalves Ammonites Logs Concretions Degree of bioturbation Mudstone with sand lenses Sandstone Sandstone with clay laminae Albuen Sortehat Enhjørningen Dal S N < 75 km >< 40 km > Cross-bedded sandstone Hummocky cross-stratified sandstone Pelion Fm Sortehat Fm Ostreaelv Fm Fig. 4. Correlation between the three localities Albuen, Sortehat and Enhjørningen Dal showing the palynological zonation (Assemblage Zones 6–9). The upper part of the Sortehat Formation and the overlying Pelion Formation at the type locality (Sortehat) have been removed by recent erosion. The base and top of the Sortehat Formation are indicated by the dotted line. was from the type section at Sortehat, and two (144229 and 144231) were from a locality north of Dusén Bjerg. Sample 144112 yielded a sparse assemblage of well-pre- served palynomorphs, including Nannoceratopsis gra- cilis. Sample 144229 yielded a dinoflagellate cyst assemblage dominated by N. gracilis. The assemblage in sample 144231 was dominated by the acritarch Veryhachium sortehatense. Fensome (1979) concluded that the palynomorph assemblages determined from the three samples from the Sortehat Formation did not allow for accurate dating. It is worth noting that the dinoflagellate cyst Sentusidinium pelionense was not found in any of the three samples from the Sortehat Formation, but was common in one sample (144111) from the overlying Pelion Formation. Lund & Pedersen (1985) presented the results of a palynological study concerning the Neill Klinter and Vardekløft Groups and the lower part of the Hareelv Formation. Four samples (142832–35) are from the Sortehat Formation. These samples yielded abundant Sentusidinium pelionense but Nannoceratopsis gracilis was not found, whereas the pollen Perinopollenites ela- toides was abundant. Sample 142833 had the lowest number of marine cysts, whereas Botryococcus was common in 142832 and 142835. On the basis of these data, Lund & Pedersen (1985) suggested a Middle–Late Bajocian age for the Sortehat Formation. The Neill Klinter and Vardekløft Groups were also studied palynologically by Underhill & Partington (1994). The material on which their study was based was sam- pled at Liaselv (their section 1), Vardekløft (section 2), and Harris Fjeld/Primulaelv at Neill Klinter, the west- ern slope of Hurry Inlet (section 3; Fig. 1). Twenty sam- ples from the Sortehat Formation were analysed from their sections 1 and 2 (7 samples from section 1, 13 sam- ples from section 2; their fig. 10). An Aalenian–Bajocian age was proposed for the Sortehat Formation. On the basis of these data, Underhill & Partington (1994) sug- gested that the Aalenian–Bajocian record was essentially complete, without apparent biostratigraphic or sedi- mentological evidence of the ‘mid-Cimmerian event’ known from the North Sea area. Underhill & Partington (1994) concluded that the boundary between the Sortehat Formation and the underlying Ostreaelv Formation does not represent an important uncomfor- mity. This is confirmed by recent work (Koppelhus & Dam 2003, this volume) on the uppermost part of the Ostreaelv Formation which has been referred to the Late Toarcian – early Aalenian on the basis of the paly- nological assemblages. The organic geochemistry and the palynofacies of the Sortehat Formation were discussed by Krabbe et al. (1994). Based on the palynofacies study, the succession was divided into three facies: (1) Botryococcus-domi- nated, (2) spore/pollen and brown/blackwood and (3) blackwood-dominated, few spore/pollen. These results, together with the geochemical data, suggest an increase in the salinity of the depositional environment with time (Krabbe et al. 1994). Materials and methods This study is primarily based on material collected by the authors in the 1993 and 1994 field seasons. The Sortehat Formation was investigated along a north–south- trending profile through the Jameson Land Basin, par- allel to the basin axis. Sections were sampled and studied at four localities: Albuen (Neill Klinter along Hurry Inlet) and Sortehat (the type locality of the formation) in the south and Enhjørningen Dal and Pelion in the north- ern part of Jameson Land (Fig. 1; Appendix 1). The boundary between the Ostreaelv and the Sortehat Formations is a well-defined stratigraphic surface and was used as a datum for the sections measured at out- crop; the structural dip of the succession is negligible. The outcrop sections were measured by Jacob staff in metres relative to this surface. Altimeter readings for the datum surface are listed in Appendix 1; sample loca- tions are thus referred to height above sea level, being the sum of the datum altitude (measured by altimeter) and the measured section thickness above the datum. Samples taken from core from the borehole at the type locality of the Sortehat Formation are related to an arbi- trary datum (base of cored section) within the upper Ostreaelv Formation (Appendix 1). Approximately 300 samples were processed at the palynological laboratory of the former Geological Survey of Greenland using standard techniques (Nøhr-Hansen 1993). The palynomorphs were studied using a trans- mitted light microscope. For each sample, 200 speci- mens were counted, and all species were registered in the range chart program SIS. The palynomorphs illus- trated in Plates 1–6 are from the borehole at the type locality of the Sortehat Formation and from a section at Lepidopteriselv; the latter has not been used in the correlation between the three other localities. All the palynomorph taxa recorded in the samples are listed in Appendix 2 with author attributions and dates, and the slides are stored in the collections of the Geological Survey of Denmark and Greenland. 783 Palynological zones: definition The data presented here form part of a broader study encompassing the entire Neill Klinter Group. Nine paly- nological assemblage zones (1–9) have been recog- nised in the group; assemblage zones 1–6 from the Rævekløft, Gulehorn and Ostreaelv Formations are pre- sented in a companion paper (Koppelhus & Dam 2003, this volume). The three assemblage zones of the Sortehat Formation, based on the occurrence of miospores, dinoflagellate cysts and freshwater algae, are named from below: (7) the Botryococcus Assemblage Zone, (8) the Nannoceratopsis gracilis – Nannoceratopsis senex Assemblage Zone and (9) the Sentusidinium pelionense Assemblage Zone. Assemblage Zone 7 is also recognised in the upper levels of the Ostreaelv Formation and is described briefly in Koppelhus & Dam (2003, this vol- ume), but is defined herein. Assemblage Zone 7: Botryococcus new assemblage zone Occurrence. Albuen 438.5–443.5 m Enhjørningen Dal 425.35–445 m Pelion 550–567 m Sortehat (core) 27.82–36.36 m In the cored section from Sortehat, this assemblage occurs in the lower levels of the Sortehat Formation, the base being immediately above the lower boundary of the formation (Figs 4, 5). At Albuen, the assemblage is represented in the uppermost few metres of the Ostreaelv Formation and extends up into the Sortehat Formation (Figs 4, 6; Fig. 6 faces page 794). At Enhjør- ningen Dal, Assemblage Zone 7 is restricted to the lower Sortehat Formation although here the base is some 6 m above the lower boundary of the Sortehat Formation (Figs 4, 7; Fig. 7 faces page 795). 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; Figs 4, 5). Additional sections. Albuen, 438.5 m (sample 397452) – 443.5 m (sample 397468; Figs 4, 6). Enhjørningen Dal, 425.35 m (sample 398341) – 445 m (sample 398417; Figs 4, 7). Base. The base of the assemblage is placed at the first sample in which Botryococcus spp. overwhelmingly dominates the assemblage and the dinoflagellate cysts Nannoceratopsis gracilis and Nannoceratopsis senex and dinoflagellate cysts in general become rare. In the Albuen section (Fig. 6), this event coincides with the first co-occurrence of Callialasporites dampieri (pollen) and Mendicodinium groenlandicum (dinoflagellate cyst) although in other sections (e.g. Sortehat, Enhjør- ningen Dal; Figs 5, 7) these species first occur together some metres below the Botryococcus spp. influx. Top. The upper boundary is defined by the uppermost sample showing the Botryococcus-dominated assem- blage. Above this level, Botryococcus spp. are scarce and Nannoceratopsis gracilis and N. senex become abundant once more. Characteristics. The assemblage is characterised by the overwhelming dominance of the freshwater alga Botry- ococcus spp. and the scarcity of dinoflagellates. Pollen species such as Perinopollenites elatoides, Cerebro- pollenites macroverrucosus and bisaccate pollen are also abundant. Suggested age. Aalenian (see discussion below). Palaeoenvironment. The palynomorph assemblage indi- cates a brackish marine environment. The abundant Botryococcus and the common spores and pollen reflect a significant allochthonous terrestrial input related to transgression (see later discussion). Remarks. The Botryococcus Assemblage is, as the name indicates, dominated by Botryococcus spp. (Plate 4, fig. 4), but spores and pollen also play an important role. The spore flora is diverse, but there are only few specimens of each species, whereas pollen species are less diverse but occur abundantly, such as Perino- pollenites elatoides (Plate 2, fig. 5), bisaccate pollen, Cerebropollenites macroverrucosus (Plate 3, fig. 3) and Corollina torosus (Plate 3, fig. 2). Some of the less abun- dant pollen are stratigraphically significant, such as Quadraeculina anellaeformis (Plate 3, fig. 5) and Callialasporites dampieri (Plate 2, fig. 1). Acritarchs and dinoflagellate cysts occur only rarely. Among the latter are Dissilodinium sp. (Plate 6, fig. 4), Mendicodinium sp., Pareodinia halosa (Plate 4, fig. 6), Mancodinium semitabulatum (Plate 6, fig. 1) and a few specimens of Nannoceratopsis senex (Plate 5, fig. 2) and N. gracilis (Plate 5, fig. 1). 784 785 So rt eh at Middle Jurassic Lower Jurassic Aalenian Toarcian Ostreaelv FormationSortehat Formation 77 .9 8 73 .1 3 69 .5 0 65 .2 4 61 .3 1 57 .4 1 53 .8 6 49 .4 8 45 .0 9 40 .1 1 36 .3 6 32 .0 6 29 .5 6 27 .8 2 26 .2 8 12 .6 5 30 31 43 -1 1 30 31 43 -1 6 30 31 43 -2 0 30 31 43 -2 4 30 31 43 -2 8 30 31 43 -3 3 30 31 43 -3 7 30 31 43 -4 3 30 31 45 -4 9 30 31 43 -5 5 30 31 43 -6 2 30 31 43 -6 7 30 31 43 -6 9 30 31 43 -7 3 30 31 43 -7 5 30 31 43 -7 7 1Baculatisporites spp. 2Manumia delcourtii 3Tripartina variabilis 4Staplinisporites caminus 5Retitriletes semimuris 6Retitriletes clavatoides 7Deltoidospora spp. 8Retitriletes spp. 9Leptolepidites bossus 10Striatella jurassica 11Uvaesporites puzzlei 12Taurocusporites verrucatus 13Concavissimisporites spp. 14Sestrosporites pseudoalveolatus 15Ischyosporites spp. 16Leptolepidites spp. 17Ischyosporites variegatus 18Striatella parva 19Lycopodiacidites rugulatus 20Densoisporites scanicus 21Foraminisporis jurassicus 22Densoisporites velatus 23Polycingulatisporit triangularis 24Megaspore spp. 25Neoraistrickia spp. 26Striatella spp. 27Retitriletes austroclavatoides 28Kraeuselisporites reissingeri 29Apiculatisporites spp. 30Densosporites spp. 31Chasmatosporites hians 32Spheripollenites subgranulatus 33Bisaccate spp. 34Perinopollenites elatoides 35Pinuspollenites minimus 36Cerebropollenites macroverrucosus 37Corollina torosus 38Vesicaspora fuscus 39Quadraeculina anellaeformis 40Cerebropollenties thiergartii 41Chasmatosporites major 42Callialasporites dampieri 43Callialasporites turbatus 44Exesipollenites tumulus 45Callialasporites trilobatus 46Araucariacites australis 47Chasmatosporites apertus 48Eucommiidites troedsonii 49Monosaccate spp. 50Dodekovia tegilla 51Wallodinium laganum 52Nannoceratopsis gracilis 53Scriniocassis weberii 54Nannoceratopsis ambonis 55Nannoceratopsis senex 56Mancodinium semitabulatum 57Dinocyst spp. 58Mendicodinium groenlandicum 59Dissiliodinium spp. 60Pareodinia halosa 61Mendicodinium reticulatum 62Mendicodinium spp. 63Kallosphaeridium spp. 64Pareodinia ceratophora 65Sentusidinium pelionense 66Nannoceratopsis plegas 67Susadinium scrofoides 68Phallocysta eumekes 69Andreedinium arcticum 70Phallocysta elongata 71Scriniocassis spp. 72Acritarch spp. 73Limbicysta bjaerkei 74Veryhachium formosum 75Veryhachium sortehatense 76Lecaniella foveata 77Leiosphaeridia spp. 78Botryococcus spp. 79Tasmanites spp. 80Foraminifera spp. ? R ? ? ? A lp ha be tic al s pe ci es li st 72 A cr ita rc h sp p. 69 A n d re ed in iu m a rc ti cu m 29 A p ic u la ti sp or it es s pp . 46 A ra u ca ri a ci te s a u st ra lis 1 B a cu la ti sp or it es s pp . 33 Bi sa cc at e sp p. 78 B ot ry oc oc cu s sp p. 42 C a lli a la sp or it es d a m p ie ri 45 C a lli a la sp or it es t ri lo b a tu s 43 C a lli a la sp or it es t u rb a tu s 36 C er eb ro p ol le n it es m a cr ov er ru co su s 40 C er eb ro p ol le n ti es t h ie rg a rt ii 47 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 41 C h a sm a to sp or it es m a jo r 13 C on ca vi ss im is p or it es s pp . 37 C or ol lin a t or os u s 7 D el to id os p or a s pp . 20 D en so is p or it es s ca n ic u s 22 D en so is p or it es v el a tu s 30 D en so sp or it es s pp . 57 D in oc ys t sp p. 59 D is si lio d in iu m s pp . 50 D od ek ov ia t eg ill a 48 E u co m m iid it es t ro ed so n ii 44 E xe si p ol le n it es t u m u lu s 80 Fo ra m in ife ra s pp . 21 Fo ra m in is p or is j u ra ss ic u s 15 Is ch yo sp or it es s pp . 17 Is ch yo sp or it es v a ri eg a tu s 63 K a llo sp h a er id iu m s pp . 28 K ra eu se lis p or it es r ei ss in ge ri 76 Le ca n ie lla f ov ea ta 77 Le io sp h a er id ia s pp . 9 Le p to le p id it es b os su s 16 Le p to le p id it es s pp . 73 Li m b ic ys ta b ja er ke i 19 Ly co p od ia ci d it es r u gu la tu s 56 M a n co d in iu m s em it a b u la tu m 2 M a n u m ia d el co u rt ii 24 M eg as po re s pp . 58 M en d ic od in iu m g ro en la n d ic u m 61 M en d ic od in iu m r et ic u la tu m 62 M en d ic od in iu m s pp . 49 M on os ac ca te s pp . 54 N a n n oc er a to p si s a m b on is 52 N a n n oc er a to p si s gr a ci lis 66 N a n n oc er a to p si s p le ga s 55 N a n n oc er a to p si s se n ex 25 N eo ra is tr ic k ia s pp . 64 Pa re od in ia c er a to p h or a 60 Pa re od in ia h a lo sa 34 Pe ri n op ol le n it es e la to id es 70 Ph a llo cy st a e lo n ga ta 68 Ph a llo cy st a e u m ek es 35 Pi n u sp ol le n it es m in im u s 23 Po ly ci n gu la ti sp or it t ri a n gu la ri s 39 Q u a d ra ec u lin a a n el la ef or m is 27 R et it ri le te s a u st ro cl a va to id es 6 R et it ri le te s cl a va to id es 5 R et it ri le te s se m im u ri s 8 R et it ri le te s sp p. 71 S cr in io ca ss is s pp . 53 S cr in io ca ss is w eb er ii 65 S en tu si d in iu m p el io n en se 14 S es tr os p or it es p se u d oa lv eo la tu s 32 S p h er ip ol le n it es s u b gr a n u la tu s 4 S ta p lin is p or it es c a m in u s 10 S tr ia te lla j u ra ss ic a 18 S tr ia te lla p a rv a 26 S tr ia te lla s pp . 67 S u sa d in iu m s cr of oi d es 79 Ta sm a n it es s pp . 12 Ta u ro cu sp or it es v er ru ca tu s 3 Tr ip a rt in a v a ri a b ili s 11 U va es p or it es p u z z le i 74 Ve ry h a ch iu m f or m os u m 75 Ve ry h a ch iu m s or te h a te n se 38 Ve si ca sp or a f u sc u s 51 W a llo d in iu m l a ga n u m 75 50 25 System Stage Palynological Assembl. Zones Lithostratigraphy (m) Sample height Sample number 9 8 7 6 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. 5 . C h ar t sh o w in g th e d is tr ib u tio n o f p al yn o m o rp h s fr o m t h e co re d b o re h o le a t So rt eh at , th e ty p e lo ca lit y o f th e So rt eh at F o rm at io n . Assemblage Zone 8: Nannoceratopsis gracilis – Nannoceratopsis senex new assemblage zone Occurrence. Albuen 444.5–460 m Enhjørningen Dal 446–500 m Pelion 573–577 m Sortehat (core) 40.11–53.86 m Assemblage Zone 8 occurs within the Sortehat For- mation; it thus falls within sequence SQ7 of Dam & Surlyk (1995, 1998). Reference section. Sortehat (core), 40.11 m (sample 303143-55) – 53.86 m (sample 303143-37; Figs 4, 5). Additional sections. Albuen, 444.5 m (sample 397469) – 460 m (sample 397474; Figs 4, 6). Enhjørningen Dal, 446 m (sample 395625) – 500 m (sample 398442; Figs 4, 7). Base. The lower boundary is placed at the first sample in which Botryococcus spp. is rare and Nannoceratopsis gracilis and N. senex are abundant. Top. This is defined by the last sample showing the characteristic assemblage (see below), above which level Nannoceratopsis gracilis becomes less common and Sentusidinium pelionense is the most common dinoflagellate cyst. Characteristics. Botryococcus spp. is rare in this assem- blage whereas Nannoceratopsis gracilis is abundant and there is a general increase in diversity and abundance of dinoflagellate cysts relative to the underlying zone. Suggested age. Aalenian (see discussion below). Palaeoenvironment. The palynological data indicate a brackish marine environment. Remarks. Dinoflagellate cysts are abundant, whereas Botryococcus spp. becomes rare at 40.11 m in the type section at Sortehat (Fig. 5). There are a few acritarchs, such as Veryhachium sorthatense (Plate 4, fig. 2), and some of the same spores and pollen as observed in the Botryococcus Assemblage Zone (Plates 1, 2). Assemblage Zone 9: Sentusidinium pelionense new assemblage zone Occurrence. Albuen 465–502 m Enhjørningen Dal 502–516.75 m Sortehat (core) 57.41–77.98 m Assemblage Zone 9 occurs in the upper Sortehat Formation in the Sortehat section; note that the sam- pled interval in this section is restricted to the Sortehat Formation (Figs 4, 5). At Albuen and Enhjørningen Dal, the assemblage extends through the upper Sortehat Formation and persists up into the overlying Pelion Formation (Figs 4, 6, 7). Assemblage Zone 9 is thus characteristic of the upper levels of sequence SQ7 of Dam & Surlyk (1995, 1998), and at Albuen and Enhjørningen Dal spans the sequence boundary at the base of the Pelion Formation and extends into sequence P1 of Engkilde & Surlyk (2003, this volume). Reference section. Sortehat (core), 57.41 m (sample 303143-33) – 77.98 m (sample 303143-11; Figs 4, 5). Additional sections. Albuen, 465 m (sample 397475) – 502 m (sample 397498; Figs 4, 6). Enhjørningen Dal, 502 m (sample 395679) – 516.75 m (sample 398448; Figs 4, 7). Base. The base of the zone is placed at the sample in which Sentusidinium pelionense is the most common dinoflagellate cyst; Nannoceratopsis gracilis and N. senex are absent or rare. Top. The upper boundary of the assemblage zone is not defined here. The Sentusidinium pelionense Assemblage Zone extends from the upper part of the Sortehat For- mation into the lowermost beds of the Pelion Formation. The full extent of the zone within the Pelion Formation is not known. It is likely, however, that the top of the zone occurs within the lower levels of the Pelion For- mation (S. Piasecki, personal communication 1997). Characteristics. Sentusidinium pelionense is abundant. In some of the investigated sections, S. pelionense is accompanied by Nannoceratopsis gracilis in samples at the boundary between the two palynomorph assemblage zones. In other sections, they do not overlap, i.e. N. gra- cilis is replaced by S. pelionense up-section. 786 Suggested age. Aalenian – ?Early Bajocian (see discus- sion below). Palaeoenvironment. The palynological data indicate that most of the organic material came from a brackish marine source. Remarks. The assemblage contains fewer spores and pollen than the underlying assemblage zone. The most abundant dinoflagellate cysts are Sentusidinium pelion- ense (Plate 6, fig. 5) and Pareodinia halosa (Plate 4, fig. 6) although a few specimens of Phallocysta eumekes were recorded. The acritarch Limbicysta bjaerkei was also found. Palynological results Sortehat At the type locality, the Sortehat Formation is a mini- mum of 50 m thick; the top of the formation is not seen due to recent erosion. Seventy samples were collected and seventeen of these are shown on the distribution chart (Fig. 5). The palynological assemblages from the entire sec- tion fall into three distinct assemblages. There is a dis- tinct change from the Perinopollenites elatoides Zone (Assemblage Zone 6, described by Koppelhus & Dam 2003, this volume) in the underlying Ostreaelv Formation to the Botryococcus Assemblage Zone (Assemblage Zone 7), which is overwhelmingly dominated by the freshwater alga Botryococcus. This change is first observed at 27.82 m (sample 303143-73) just above the lithological boundary between the Sortehat and Ostreaelv Formations at 27.6 m. The Perinopollenites elatoides Zone is characterised by the first appearance of Stap- linisporites caminus, Sestrosporites pseudoalveolatus, Phallocysta eumekes and Wallodinium laganum; Callialasporites dampieri makes its first appearance near the top of the zone. The data from the three Ostreaelv Formation samples from the Sortehat section do not show exactly the same pattern although S. cami- nus and C. dampieri have their first appearance in the uppermost sample from the Ostreaelv Formation and the dinoflagellate cyst W. laganum is very common in sample 303143-80 at 6.64 m (not shown on Fig. 5), approximately 20 m below the boundary between the Ostreaelv and Sortehat Formations. In sample 303143-73 at 27.82 m, 0.22 m above the base of the Sortehat Formation, the freshwater alga Botryococcus appears and the acme extends for approx- imately 9 m before Botryococcus disappears and the dinoflagellate cyst Nannoceratopsis gracilis begins to dominate the assemblage. In three samples (303143-75, 303143-73 and 303143-69) an unidentified dinocyst (Dinocyst sp.) is common to abundant; this dinoflagel- late cyst is similar to one described as Dinoflagellate sp. indet. 2 from Callovian deposits from Spitsbergen where it is said to occur in profusion in some assemblages (Bjærke 1980). This species was also common in the low- ermost sample from the Pelion locality (Fig. 8). N. gracilis continues to be the dominant dinoflagel- late for 14 m to 53.86 m (sample 303143-37) above which there is an acme of Sentusidinium pelionense together with abundant Pareodinia halosa. Albuen The Sortehat Formation at Albuen covers about 60 m and 41 samples have been investigated from this inter- val (Fig. 6). The boundary between the Ostreaelv and Sortehat Formations is at 440 m, but the palynomorph assemblages change between sample 405449 at 434 m and sample 397452 at 438.6 m, several metres below the top of the Ostreaelv Formation, where Botryococcus becomes common, dinoflagellate cysts become rare (Mendicodinium groenlandicum, Nannoceratopsis gra- cilis and Nannoceratopsis senex are present but rare), and pollen are more common than spores. At 443.5 m in sample 397468, 3.5 m above the base of the Sortehat Formation, Botryococcus is abundant for the last time; above this level N. gracilis and N. senex become abun- dant and are accompanied by Sentusidinium pelionense. S. pelionense is only common in one sample (397471), and Pareodinia halosa is common in two other sam- ples, 397475 and 347477. This assemblage changes between 460 m and 465 m, above which level S. pelion- ense is the only common dinoflagellate; this species disappears above 496 m, within the lower levels of the Pelion Formation. The overall dinoflagellate cyst diver- sity decreases from the upper part of the Nannoceratopsis gracilis – Nannoceratopsis senex Assemblage Zone through the Sentusidinium pelionense Assemblage Zone in the upper part of the Sortehat Formation. A few dinoflagellate cysts have been found in most of the samples, and pollen are more common than spores. The samples that span the boundary between the Sortehat Formation and the overlying Pelion Formation yielded an impoverished palynomorph assemblage without any age-diagnostic species. 787 Enhjørningen Dal Enhjørningen Dal is a composite section spanning the top of the Ostreaelv Formation, the entire Sortehat Formation and the lowermost part of the Pelion Formation (Fig. 7). The boundary between the Ostreaelv and Sortehat Formations is at 418 m; the first change in the palynomorph assemblages is observed in sam- ple 398341 at 425.35 m. This lower interval (belonging to the uppermost part of the Ostreaelv Formation and the lowermost part of the Sortehat Formation) is com- pletely dominated by the dinoflagellate species Nanno- ceratopsis gracilis and Nannoceratopsis senex, and by the pollen Perinopollenites elatoides. This interval is accordingly referred to the Perinopollenites elatoides Assemblage Zone (Assemblage Zone 6; Koppelhus & Dam 2003, this volume) which is of Late Toarcian – early Aalenian age. At 425.35 m (sample 398341), Botryococcus appears in abundance and persists in large numbers up to sample 398417 at 445 m. From sample 395625 at 446 m to sample 398442 at 500 m, the palynomorph assemblage contains few Botryococcus; N. gracilis and N. senex are very common in the lower part of this interval. In the upper part of the section, however, from sample 395657 at 476 m to the uppermost sample (398448) at 516.75 m, N. gracilis and N. senex are absent whereas other dinoflagellates are present but rare (e.g. Mancodinium semitabulatum, Phallocysta eumekes, Susadinium scrofoides, Parvocysta barbata, Dissilo- dinium sp. and Mendicodinium sp.). Sentusidinium pelionense is abundant in samples 395679 and 395671, Pareodinia halosa is common in sample 395671 and Kallosphaeridium sp. is abundant in the uppermost sample (398448). Among the pollen at this level, bisac- cates and Cerebropollenites macroverrucosus are espe- cially abundant. Trilete spores seem to decrease in diversity and density compared to the lower part of the section. Pelion Ten samples were investigated from the Pelion local- ity (Fig. 8). They cover the lowermost 27 m of the Sortehat Formation, which is approximately 110 m thick at this locality. Generally, the palynomorph assemblages are rich but the preservation is poor. The assemblage from the lowermost 17 m of the formation (sample 339702 at 550 m to sample 339709 at 567 m) is domi- nated by Botryococcus. In sample 339709, Botryococcus has its last abundant appearance. In this interval, dinofla- gellate cysts are present and locally common (Nanno- ceratopsis gracilis, Mendicodinium groenlandicum and Mendicodinium sp.). The two uppermost samples (sam- ple 339710 at 573 m and sample 339711 at 577 m) yielded an assemblage rich in dinoflagellate cysts includ- ing Nannoceratopsis gracilis, Nannoceratopsis triceras, Nannoceratopsis plegas, Nannoceratopsis triangulata and Mancodinium semitabulatus and some acritarchs. Spores and pollen are common to abundant through- out the 27 m section. Discussion The palynological study reported here has implications both for the age and regional correlation of the Sortehat Formation and for the environmental understanding of the formation, in association with the detailed sedi- mentological and sequence stratigraphic study (Hansen 1999). Age and correlation On the basis of macrofauna in the underlying and over- lying formations (see previous discussion), the age of the Sortehat Formation is constrained between the lat- est Toarcian and the mid-Bajocian; previous palyno- logical work has indicated an Aalenian–Bajocian (Underhill & Partington 1994) or a Middle–Late Bajocian age (Lund & Pedersen 1985). With a view to a more well-founded understanding of the stratigraphy of the Sortehat Formation, the results of this study are com- pared with published palynological data from the North Atlantic region. Although palynological assemblages from the Toarcian–Bajocian interval have been widely reported from this region, few of the sections have been independently dated using ammonites and the Aalenian assemblages, in particular, are commonly dom- inated by terrestrial material. The Aalenian stage is named after Aalen in Germany, where the lowest part of the ‘Braunjura’ crops out at the northern edge of the Swabian Alps. Although no palynological papers have been published on material from the type locality, a dinoflagellate cyst assemblage has been described from two cores from Hausen in south-western Germany, 40 km from the type locality, and the lithological units have been correlated with the ammonite zonation from the Eastern Swabian Alb (Feist- Burkhardt 1990). The palynological assemblages are rich in spores and pollen, and only 5–20% of the total 788 789 Pe lio n Middle Jurassic Aalenian Sortehat Formation 57 7. 00 57 3. 00 56 7. 00 56 5. 00 56 3. 00 55 9. 00 55 7. 00 55 6. 00 55 5. 00 55 0. 00 33 97 11 33 97 10 33 97 09 33 97 08 33 97 07 33 97 06 33 97 05 33 97 04 33 97 03 33 97 02 1Kekryphalospora distincta 2Striatella spp. 3Retitriletes spp. 4Deltoidospora spp. 5Baculatisporites spp. 6Retitriletes clavatoides 7Retitriletes semimuris 8Leptolepidites spp. 9Ischyosporites variegatus 10Sestrosporites pseudoalveolatus 11Striatella parva 12Manumia delcourtii 13Staplinisporites caminus 14Rogalskaisporites cicatricosus 15Todisporites major 16Stereisporites stereoides 17Retitriletes austroclavatoides 18Neoraistrickia spp. 19Polycingulatisporit triangularis 20Striatella seebergensis 21Densoisporites scanicus 22Tripartina variabilis 23Striatella jurassica 24Leptolepidites bossus 25Taurocusporites segmentatus 26Uvaesporites spp. 27Spheripollenites subgranulatus 28Callialasporites spp. 29Callialasporites turbatus 30Cerebropollenites macroverrucosus 31Bisaccate spp. 32Perinopollenites elatoides 33Pinuspollenites minimus 34Corollina torosus 35Quadraeculina anellaeformis 36Callialasporites minus 37Vitreisporites pallidus 38Callialasporites dampieri 39Spheripollenites psilatus 40Exesipollenites tumulus 41Chasmatosporites major 42Alisporites robusta 43Chasmatosporites apertus 44Striate spp. 45Chasmatosporites hians 46Monosulcites spp. 47Cerebropollenties thiergartii 48Callialasporites trilobatus 49Callialasporites segmentatus 50Araucariacites australis 51Phallocysta spp. 52Nannoceratopsis spp. 53Dinocyst spp. 54Nannoceratopsis gracilis 55Mendicodinium groenlandicum 56Nannoceratopsis senex 57Mendicodinium spp. 58Nannoceratopsis plegas 59Nannoceratopsis triceras 60Mancodinium semitabulatum 61Nannoceratopsis triangulata 62Leiosphaeridia spp. 63Acritarch spp. 64Botryococcus spp. 65Miscellaneous spp. 66Fungal spp. A lp ha be tic al s pe ci es li st 63 A cr ita rc h sp p. 42 A lis p or it es r ob u st a 50 A ra u ca ri a ci te s a u st ra lis 5 B a cu la ti sp or it es s pp . 31 Bi sa cc at e sp p. 64 B ot ry oc oc cu s sp p. 38 C a lli a la sp or it es d a m p ie ri 36 C a lli a la sp or it es m in u s 49 C a lli a la sp or it es s eg m en ta tu s 28 C a lli a la sp or it es s pp . 48 C a lli a la sp or it es t ri lo b a tu s 29 C a lli a la sp or it es t u rb a tu s 30 C er eb ro p ol le n it es m a cr ov er ru co su s 47 C er eb ro p ol le n ti es t h ie rg a rt ii 43 C h a sm a to sp or it es a p er tu s 45 C h a sm a to sp or it es h ia n s 41 C h a sm a to sp or it es m a jo r 34 C or ol lin a t or os u s 4 D el to id os p or a s pp . 21 D en so is p or it es s ca n ic u s 53 D in oc ys t sp p. 40 E xe si p ol le n it es t u m u lu s 66 Fu ng al s pp . 9 Is ch yo sp or it es v a ri eg a tu s 1 K ek ry p h a lo sp or a d is ti n ct a 62 Le io sp h a er id ia s pp . 24 Le p to le p id it es b os su s 8 Le p to le p id it es s pp . 65 M is ce lla ne ou s sp p. 60 M a n co d in iu m s em it a b u la tu m 12 M a n u m ia d el co u rt ii 55 M en d ic od in iu m g ro en la n d ic u m 57 M en d ic od in iu m s pp . 46 M on os u lc it es s pp . 54 N a n n oc er a to p si s gr a ci lis 58 N a n n oc er a to p si s p le ga s 56 N a n n oc er a to p si s se n ex 52 N a n n oc er a to p si s sp p. 61 N a n n oc er a to p si s tr ia n gu la ta 59 N a n n oc er a to p si s tr ic er a s 18 N eo ra is tr ic k ia s pp . 32 Pe ri n op ol le n it es e la to id es 51 Ph a llo cy st a s pp . 33 Pi n u sp ol le n it es m in im u s 19 Po ly ci n gu la ti sp or it t ri a n gu la ri s 35 Q u a d ra ec u lin a a n el la ef or m is 17 R et it ri le te s a u st ro cl a va to id es 6 R et it ri le te s cl a va to id es 7 R et it ri le te s se m im u ri s 3 R et it ri le te s sp p. 14 R og a ls k a is p or it es c ic a tr ic os u s 10 S es tr os p or it es p se u d oa lv eo la tu s 39 S p h er ip ol le n it es p si la tu s 27 S p h er ip ol le n it es s u b gr a n u la tu s 13 S ta p lin is p or it es c a m in u s 16 S te re is p or it es s te re oi d es 44 S tr ia te s pp . 23 S tr ia te lla j u ra ss ic a 11 S tr ia te lla p a rv a 20 S tr ia te lla s ee b er ge n si s 2 S tr ia te lla s pp . 25 Ta u ro cu sp or it es s eg m en ta tu s 15 To d is p or it es m a jo r 22 Tr ip a rt in a v a ri a b ili s 26 U va es p or it es s pp . 37 V it re is p or it es p a lli d u s 57 5 56 5 55 5 System Stage Palynological. Assembl. Zones Lithostratigraphy (m) Sample height Sample number 8 7 Fi g. 8 . C h ar t sh o w in g th e d is tr ib u tio n o f p al yn o m o rp h s fr o m t h e lo ca lit y at P el io n . palynomorph content is microplankton. In the Sortehat Formation, where the assemblages are also rich in spores and pollen, microplankton form 25–40% of the total palynomorph content. In the material from south- western Germany, twelve of the eighteen dinoflagel- late cysts recognised have also been identified in the material from the Sortehat Formation. However, none of the four stratigraphically significant species for the Aalenian/Bajocian boundary from Hausen, Carpatho- dinium sp., Dissilodinium giganteum, Dissilodinium sp. A, and Durotrigia daveyi, have with certainty been found in the material from the Sortehat Formation. The closest succession to Jameson Land with known palynological data of Aalenian age is the Stø Formation (Unit C) from the Møre Basin, offshore mid-Norway (Smelror et al. 1994). Ammonites have not been found to confirm the age, but a few foraminifera of little strati- graphic value have been used, together with the pres- ence of the dinoflagellate cyst Phallocysta eumekes, which is restricted to the latest Early Toarcian – Aalenian in Europe (Riding & Thomas 1992). Spores, pollen and dinoflagellate cysts from Unit C are similar to those from the Botryococcus and Nannoceratopsis gracilis – Nannoceratopsis senex Assemblage Zones of the Sortehat Formation. Two thin levels with Botryococcus have been observed in the Stø Formation although not as rich in abundance as in the Sortehat Formation (Smelror et al. 1994). Moreover, the abrupt shift seen in the Sortehat Formation from an assemblage dominated by Botryococcus to one dominated by the dinoflagellate cysts Nannoceratopsis gracilis, Nannoceratopsis senex and Pareodinia halosa is not recognised in the Møre Basin. It should be noted, however that the Botryococcus Assemblage Zone of the Sortehat Formation is not strati- graphically significant but reflects only the palaeo- environmental conditions within the Jameson Land Basin at the time of deposition (see discussion below). Aalenian palynomorph assemblages have also been identified from Arctic Canada and south-east Canada (Johnson & Hills 1973; Davies 1983; Bujak & Williams 1977), Barents Sea (Hammerfest Basin, Nordkap Basin, and Franz Josef Land; Smelror & Below 1992; Smelror 1994), north-west Scotland, north Yorkshire and Gloucestershire in England (Riding 1983, 1984a, b, 1987; Riding et al. 1991; Riding & Thomas 1992), Sweden (Guy-Ohlson 1994; Guy-Ohlson & Norling 1994), the Danish Subbasin (Dybkjær 1991; Seidenkrantz et al. 1993; Poulsen 1994), Øresund and the Baltic Sea (Koppelhus & Nielsen 1994; Koppelhus & Batten 1996), and north-west and south-west Germany (Prauss 1989). The first dinoflagellate cyst zonation of the Jurassic of the Canadian Arctic was made by Johnson & Hills (1973). Their Nannoceratopsis gracilis Range Zone cov- ers the Toarcian–Bajocian. They recorded the ammonite Leioceras opalinum, but the only dinoflagellate cyst in common with the East Greenland material is Nanno- ceratopsis gracilis. Bujak & Williams (1977) erected the Nannoceratopsis gracilis Zone for the Pliensbachian– Aalenian and the Mancodinium semitabulatum Zone for the Bajocian, from successions offshore south-east- ern Canada. Several species are common to the assem- blages from the Sortehat Formation and from the Canadian Arctic but the age has not been confirmed by any marine micro- or macrofauna. Davies (1983) estab- lished eight zones covering the Upper Pliensbachian – Callovian, also from the Canadian Arctic, of which the Dapcodinium coalitum – Phallocysta eumekes Zone, of Late Toarcian – Early Bajocian age, contains species in common with the Sortehat Formation assemblages. Davies (1983) stated that the macrofauna possibly indi- cates a Toarcian – Early Bajocian age. In the Barents Sea area, seven dinoflagellate cyst zones have been recognised in the Toarcian – Lower Oxfordian (Smelror & Below 1992). One of them, the Dodekovia bulla – Nannoceratopsis senex Concurrent Range-Zone, has a number of species (Nannoceratopsis gracilis, Nannoceratopsis senex, Nannoceratopsis triceras, Scriniocassis weberi, Susadinium scrofoides, Pareodinia halosa and Phallocysta eumekes) in common with the assemblages from the Sortehat Formation. The pres- ence of the earliest Aalenian Opalinum Zone on Svalbard has been confirmed on the basis of ammonites. In the United Kingdom, the Aalenian palynomorph assemblages are divided into Sub-biozone c (Opalinum Zone) and Sub-biozone d (Murchisonae and Concavum Zones) of the Nannoceratopsis gracilis Zone (Riding & Thomas 1992; the DSJ10 and DSJ11 Zones of Poulsen & Riding 2003, this volume). These zones are based on the FAD (first appearance datum) and the LAD (last appearance datum) of specific dinoflagellate cyst species. Of the stratigraphically significant species appearing in these zones, Susadinium scrofoides, Wallodinium laganum and other species of the genus Parvocysta have also been found in the material from the Sortehat Formation. Other common but stratigraphically less restricted species are Nannoceratopsis gracilis, Nanno- ceratopsis senex, Mancodinium semitabulatum and Scriniocassis weberi. The palynological zonation in the UK area has been related to the standard ammonite- based zones (Riding & Thomas 1992). 790 In Skåne, southern Sweden, the upper part of the Rya Formation and the lower part of the Vilhelmsfält Formation contain palynomorph assemblages domi- nated by terrestrial material deposited in a freshwater environment, although thin marine and brackish levels occur. Palynological zone III is suggested to be of Aalenian age (Guy-Ohlson & Norling 1994), and shows similarities to the palynomorph assemblages from the three zones of the Sortehat Formation. No ammonites have been found in the Middle Jurassic of southern Sweden but a foraminifera zonation has been established. In the Danish Basin, rocks of Toarcian and early Aalenian age have been identified based on the occur- rence of species of the genus Parvocysta (Poulsen 1994). A miospore and dinoflagellate cyst zonation was erected for the Lower and Middle Jurassic of the Danish Basin (Dybkjær 1991). The Perinopollenites elatoides miospore zone of Dybkjær (1991) covers sediments of Aalenian – Early Bajocian age, whereas the equivalent dinofla- gellate cyst zone includes Nannoceratopsis gracilis and comprises sediments of Late Pliensbachian – Bajocian age. Similar palynomorph assemblages have been reported from the Øresund area (Koppelhus & Batten 1996). A miospore zonation was recommended for the Lower–Middle Jurassic of Bornholm in the Baltic area, where the Callialasporites–Perinopollenites Zone from the Bagå Formation has many species in common with the Sortehat Formation (Batten et al. 1994; Koppelhus & Nielsen 1994). Dinoflagellate cysts (Nannoceratopsis gracilis) have only been found in the lowermost part of this zone. The Callialasporites–Perinopollenites Zone is defined by the first appearance of Callialasporites and the dominance of Perinopollenites elatoides. Unfor- tunately, confirmatory ammonite or microfossil data is lacking in the Danish area to support the proposed Aalenian–Bathonian age, which is based entirely on comparison to other palynological studies in Europe. In the Sentusidinium pelionense Assemblage Zone of the Sortehat Formation, spores and pollen are abundant, and dinoflagellate cysts are locally present. The dinofla- gellate cyst Sentusidinium pelionense has also been found in the Jydegård Formation on Bornholm in the Baltic Sea (Piasecki 1984; Noe-Nygaard et al. 1987). However, with the exception of the presence of S. pelion- ense, the Sentusidinium pelionense Assemblage Zone of the Sortehat Formation is more closely comparable to assemblages from the Norwegian and UK areas than to those of the Danish Basin and Bornholm. Palynomorph assemblages from the Pliensbachian– Callovian of north-west Germany were described by Prauss (1989). The palynomorph assemblage from the Nannoceratopsis plegas Zone of Aalenian age, has a number of species in common with the three zones from the Sortehat Formation, such as Nannoceratopsis gracilis, Mancodinium semitabulatum, Pareodinia halosa, Dodekovia tegillata, Scriniocassis weberi, Phallocysta eumekes and Kallospharidium sp. Unfor- tunately the suggested Aalenian age is not confirmed by ammonites. To conclude this review, the Sortehat Formation paly- nomorph assemblages clearly show close similarities to assemblages of inferred Aalenian age in the North Atlantic region. Few of these studies, however, include independent ammonite data with which to accurately constrain the age of the strata. A notable exception, upon which the age assignment of the Sortehat Formation depends, is the work of Riding (1982), Woollam & Riding (1983) and Riding & Thomas (1992) from the Jurassic of the UK. According to the zonation presented by these workers, the stratigraphically impor- tant palynomorphs recorded from the Sortehat Formation are Mancodinium semitabulatum, Nannoceratopsis ambonis, Phallocysta eumekes and Nannoceratopsis ple- gas. M. semitabulatum, which was recorded through- out the Sortehat Formation, has a range of Late Pliensbachian – Early Bajocian (Woollam & Riding 1983; Riding & Thomas 1992). N. ambonis, which occurs in the lower half of the formation, was initially thought to range from the Aalenian to the Early Bajocian (Riding 1982; Woollam & Riding 1983) but its range has sub- sequently been extended to Late Pliensbachian – Early Bajocian (Riding & Thomas 1992). P. eumekes, which occurs throughout the Sortehat Formation, has a restricted range of Late Toarcian – Aalenian in Europe (Riding & Thomas 1992). However, the species was first described from Bathonian strata in Arctic Canada where it has a range of Toarcian–Bathonian (Dörhöfer & Davies 1980) and is generally considered a more long-ranging species in Boreal regions (Riding 1984c). N. plegas is rare in the Sortehat Formation although its presence in the lower levels of the formation indicates an early Aalenian age for this part of the succession (Riding & Thomas 1992). In association, therefore, these palynomorphs indi- cate an Aalenian – ?Early Bajocian age for the Sortehat Formation. This study thus confirms the age determi- nation of Underhill & Partington (1994), although it is clear from the above review that more detailed studies of both the miospore and the dinoflagellate cyst strati- graphies of the early Middle Jurassic are urgently needed to further resolve the stratigraphy of the Sortehat For- mation. 791 A notable conclusion of this study is that there is no evidence, on palynological grounds, for a significant hia- tus at, or near, the lower boundary of the Sortehat For- mation (see also Koppelhus & Dam 2003, this volume), nor within the Sortehat Formation itself. These obser- vations are particularly pertinent to regional studies of Middle Jurassic uplift in the North Atlantic region (see Underhill & Partington 1994). The stratigraphic signif- icance of the upper boundary of the Sortehat Formation is less well-constrained palynologically, although there is no direct evidence from this study of a major strati- graphic break at this surface. Environmental implications of the palynological data The three palynomorph assemblage zones of the Sortehat Formation can be recognised and correlated through- out the Jameson Land Basin (Fig. 4). Regionally, the Botryococcus Assemblage Zone ranges in thickness from 9–17 m and spans the uppermost part of the Ostreaelv Formation and the lower part of the Sortehat Formation. The zone starts several metres below the boundary between the Ostreaelv and Sortehat Formations in the southernmost locality at Albuen, whereas the appear- ance of the zone coincides with the boundary at the Sortehat type locality. Farther north, at Enhjørningen Dal, this change in the palynomorph assemblage does not occur until 7 m above the formation boundary (Figs 4, 7). At the northernmost locality of Pelion, the change takes place 5 m above the boundary. The green alga Botryococcus is a freshwater form (Guy-Ohlson 1992) with no stratigraphic value as it ranges from the Carboniferous to the present (Tyson 1995; Batten & Grenfell 1996). However, the abundance of Botryococcus in the organic material from the low- ermost Sortehat Formation in Jameson Land is notable. Sedimentologically, the depositional shift from the Ostreaelv Formation to the Sortehat Formation marks a basinwide flooding event within an overall trans- gressive period. As the abundance of Botryococcus is restricted to the section around the flooding surface (base of Sortehat Formation) and extends up to the maximum flooding surface, it seems to be linked to the flooding event (Hansen 1999). The question is whether the abundance of Botryococcus reflects in situ deposi- tion under freshwater conditions that prevailed through- out the basin or if it represents an allochthonous accumulation of algae transported out to sea from inland freshwater environments. The continuous occurrence of dinocysts throughout the Sortehat Formation, albeit in reduced numbers in the Botryococcus Assemblage Zone, suggests a persistent marine influence. Indeed, the reduced number of marine dinoflagellate cysts in this zone may be in part an artefact related to the count- ing procedure such that the abundance of Botryococcus and terrestrial sporomorphs tends to dilute the marine dinoflagellate cysts. Given the co-occurrence of the freshwater alga Botryococcus and the marine dinofla- gellate cysts, the abundance of Botryococcus is here interpreted as an allochthonous accumulation. Seawards transport of material from inland areas suggests either a major freshwater input from rivers or inundation and erosion of coastal areas with seawards transport of land- derived material during transgression. During marine flooding, the initial rise of base-level causes expansion of lakes on low-lying areas within the coastal plain (Wells & Coleman 1987; Dominguez & Wanless 1991; Surlyk et al. 1995). As transgression proceeds, physical communication with the open sea is established, result- ing in the possibility for a large influx of freshwater algae into the marine system. Such an allochthonous origin related to transgression is consistent with the fact that the top of the Botryococcus Assemblage Zone coincides with the maximum flood- ing surface and the end of the transgressive period (Hansen 1999). A similar influx of Botryococcus, related to a flooding event, has been described from the Middle Jurassic Brent Group of the North Sea by Williams (1992), who interpreted this as an allochthonous accu- mulation resulting from the flushing of a freshwater environment into a marine environment. The diversification of the dinoflagellate cysts in the basal part of the Nannoceratopsis gracilis – Nanno- ceratopsis senex Assemblage Zone is suggestive of a general increase in marine influence. This may be related to an increase in salinity during sea-level highstand fol- lowing the transgression, as it is generally suggested that an increased diversity of dinoflagellate cysts points to more open marine conditions (Gorin & Steffen 1991; Leckie et al. 1992). Upwards within the Nannoceratopsis gracilis – Nan- noceratopsis senex Assemblage Zone and through the Sentusidinium pelionense Assemblage Zone, especially at Albuen and partly at Enhjørningen Dal, there is a marked decrease in the diversity of dinoflagellate cyst species, although the assemblage still shows marine influence. A decrease in diversity indicates more stressed and unfavourable environmental conditions, often with unstable salinities (Gorin & Steffen 1991; Leckie et al. 1992; Tyson 1995). 792 Although the strength of the marine signal partly increases up-section, the dinoflagellate cysts are char- acterised by forms tolerant of reduced salinities (e.g. Nannoceratopsis gracilis, Nannoceratopsis senex and Sentusidinium pelionense; Piasecki 1986; Prauss & Riegel 1989; Krabbe et al. 1994). The palynological data there- fore indicate a marine environment, yet restricted in terms of salinity such that brackish conditions prevailed during deposition of the Sortehat Formation. Conclusions The age of the Sortehat Formation is Aalenian to ?Early Bajocian. This age assignment is based on comparison of the three palynomorph assemblage zones (the Botryo- coccus Assemblage Zone, the Nannoceratopsis gracilis – Nannoceratopsis senex Assemblage Zone and the Sentusidinium pelionense Assemblage Zone) with paly- nomorph assemblages in the North Atlantic region that have been recorded either from sections dated directly by ammonites or from sections that can be reliably cor- related to successions with good ammonite control. No major changes have been detected in the miospore and microplankton assemblages across the lower bound- ary of the Sortehat Formation. This confirms the sug- gestion by Underhill & Partington (1994) that the boundary between the Ostreaelv Formation and the Sortehat Formation does not represent a biostrati- graphically significant hiatal surface. The change in depositional environment from the sandy, shallow marine deposits of the Ostreaelv For- mation to the mudstones of the Sortehat Formation records a marine drowning event. This sharp lithologi- cal boundary is broadly coincident with an influx of Botryococcus (the Botryococcus Assemblage Zone). The abundant occurrence of the freshwater green alga Botryococcus together with marine dinoflagellate cysts is suggested to represent an allochthonous accumula- tion of Botryococcus in a marine environment caused by seawards transport of material from an inland fresh- water environment during the marine transgression. In general, there is an increase in the marine signal passing up-section from the Botryococcus Assemblage Zone, as testified by the diversification of marine microplankton in the Nannoceratopsis gracilis – Nanno- ceratopsis senex Assemblage Zone associated with a decrease in the proportion of spores and the disap- pearance of Botryococcus. 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Underhill, J.R. & Partington, M.A. 1994: Use of genetic sequence stratigraphy in defining and determining a regional tectonic control on the “mid-Cimmerian unconformity” – implications for North Sea basin development and the global sea-level chart. In: Weimer, P. & Posamentier, H.W. (eds): Siliciclastic sequence stratigraphy. Recent developments and applications. American Association of Petroleum Geologists Memoir 58, 449–484. Wells, J.T. & Coleman, J.M. 1987: Wetland loss and the subdelta life cycle. Estuarine, Coastal and Shelf Science 25, 111–125. Williams, G. 1992: Palynology as a palaeoenvironmental indica- tor in the Brent Group, northern North Sea. In: Morton, A.C. et al. (eds): Geology of the Brent Group. Geological Society Special Publication (London) 61, 203–212. Woollam, R. & Riding, J.B. 1983: Dinoflagellate cyst zonation of the English Jurassic. Institute of Geological Sciences Report 83/2, 42 pp. London: Her Majesty’s Stationery Office. 795 Manuscript received 16 April 1997; revision accepted 18 January 1999. Appendix 1: Locality information and Geological Survey of Greenland (GGU) numbers of samples used in this study Albuen Location. 70°34′10′′N, 22°38′54′′W. Section datum. The boundary between the Ostreaelv and the Sortehat Formations is the datum for the measured section and is located 440 m above sea level. Sample numbers. GGU 397452–397498, 398501, 398507, 398509, 398513. Sortehat borehole Location. 70°53′50′′N, 22°49′56′′W. Section datum. For the drill-core, an arbitrary datum was defined 80 m below the top of the borehole. The boundary between the Ostreaelv and the Sortehat Formations occurs 27.6 m above this datum. Sample numbers. GGU 303143-11–303143-80. Lepidopteriselv Location. 71°15′12′′N, 22°37′04′′W. Section datum. The boundary between the Ostreaelv and the Sortehat Formations, which forms the datum for the section, lies at c. 810 m above sea level. Sample numbers. GGU 398151–398199. Enhjørningen Dal Two sections were measured in Enhjørningen Dal; Figure 7 is a composite of these sections. The boundary between the Ostreaelv and the Sortehat Formations, at 418 m above sea level, is the datum for the composite section. West Enhjørningen Dal Location. 71°26′53′′N, 23°25′41′′W; the northernmost of two small ravines. Sample numbers. GGU 398203–398299, 398308–398372. East Enhjørningen Dal Location. 71°26′14′′N, 23°21′52′′W; the northernmost of two small ravines. Sample numbers. GGU 395616–395668, 398417–398448. Pelion Location. 71°28′N, 23°19′W. Sample numbers. GGU 339702–339711. These samples were col- lected by Lars Stemmerik in 1990. 796 Appendix 2: List of all recorded palynomorph taxa Miospores: Alisporites robustus Nilsson 1958 Apiculatisporites spp. Araucariacites australis Cookson 1947 Baculatisporites comaumensis (Cookson) Potonié 1956 (Plate 1, fig. 3) B. spp. Bisaccates indeterminate Callialasporites dampieri (Balme) Dev 1961 (Plate 2, fig. 1) C. microvelatus Schulz 1966 (Plate 2, fig. 3) C. minus (Tralau) Guy 1971 C. segmentatus (Balme) Dev 1961 C. trilobatus (Balme) Dev 1961 C. turbatus (Balme) Schulz 1967 (Plate 2, fig. 2) C. spp. Calamospora tener (Leschik) Mädler 1964 Camarozonasporites spp. Cerebropollenites macroverrucosus (Thiergart) Schulz 1967 (Plate 3, fig. 3) C. thiergartii Schulz 1967 Chasmatosporites apertus Nilsson 1958 C. hians Nilsson 1958 (Plate 2, fig. 4) C. major Nilsson 1958 (Plate 2, fig. 6) Chomotriletes minor (Kedves) Pocock 1970 (Plate 4, fig. 1) Cibotiumspora jurienensis (Balme) Filatoff 1975 Conbaculatisporites mesozoicus Klaus 1960 C. spp. Concavissimisporites spp Corollina torosus (Reissinger) Cornet & Traverse 1975 (Plate 3, fig. 2) C. spp. Deltoidospora minor (Couper) Pocock 1970 D. spp. D. toralis (Leschik) Lund 1977 Densoisporites scanicus Tralau 1968 D. velatus Weyland & Krieger 1953 Densosporites spp. Eucommiidites troedsonii Erdtman 1948 Exesipollenites tumulus Balme 1957 (Plate 3, fig. 1) Foraminisporis jurassicus Schulz 1967 Fungal spores Iraqispora labrata Singh 1964 Ischyosporites crateris Balme 1957 I. spp. (Plate 1, fig. 6) I. variegatus (Couper) Schulz 1967 Kekryphalospora distincta Fenton & Riding 1987 Kraeuselisporites reissingeri (Harris) Morbey 1975 Leptolepidites bossus (Couper) Schulz 1967 L. major Couper 1958 L. spp. Limbosporites lundbladii Nilsson 1958 Lycopodiacidites rugulatus (Couper) Schulz 1967 Manumia delcourtii (Pocock) Dybkjær 1991 (Plate 1, fig. 8) Megaspore fragments Monosaccate pollen Monosulcites spp. Murospora spp. Neoraistrickia gristhorpensis (Couper) Tralau 1967 N. taylorii Playford & Dettmann 1965 N. spp. Perinopollenites elatoides Couper 1958 (Plate 2, fig. 5) Pinuspollenites minimus (Couper) Kemp 1970 (Plate 3, fig. 6) Polycingulatisporites circulus Simoncsics & Kedves 1961 Polycingulatisporites triangularis (Bolkhovitina) Playford & Dettmann 1965 Quadraeculina anellaeformis Malyavkina 1949 (Plate 3, fig. 5) Retitriletes austroclavatidites (Cookson) Döring et al. 1963 (Plate 1, fig. 1) R. clavatoides (Couper) Döring et al. 1963 (Plate 1, fig. 2) R. semimuris (Danzé-Corsin & Laveine) McKellar 1974 R. spp. Ricciisporites tuberculatus Lundblad 1954 Rogalskaisporites cicatricosus (Rogalska) Danzé-Corsin & Laveine 1963 Sestrosporites pseudoalveolatus (Couper) Dettmann 1963 Spheripollenites psilatus Couper 1958 S. spp. (Plate 3, fig. 4) S. subgranulatus Couper 1958 Staplinisporites caminus (Balme) Pocock 1970 (Plate 1, fig. 5) S. spp. Stereisporites stereoides (Potonié & Venitz) H.D. Pflug in: Thomson & Pflug 1953 Striatella jurassica Mädler 1964b (Plate 1, fig. 4) S. parva (Li & Shang) Filatoff & Price 1988 S. seebergensis Mädler 1964b S. spp. Striate spp. Taeniasporites rhaeticus Schulz 1967 T. spp. Taurocusporites verrucatus Schulz 1967 T. spp. Tigrisporites spp. Todisporites major Couper 1958 T. minor Couper 1958 Triancoraesporites spp. Trilete spp. Tripartina variabilis Malyavkina 1949 (Plate 1, fig. 7) 797 798 Uvaesporites puzzlei Guy 1971 U. spp. Vesicaspora fuscus (Pautsch) Morbey 1975 Vitreisporites pallidus (Reissinger) Nilsson 1958 Zebrasporites laevigatus (Schulz) Schulz 1967 Phytoplankton: Acritarch spp. Andreedinium arcticum Below 1987 Beaumontella caminuspina (Wall) Below 1987 Botryococcus spp. (Plate 4, fig. 4) Chytroeisphaeridia chytroeoides (Sarjeant) Downie & Sarjeant 1965 Cymatiosphaera spp. Dinocyst spp. Dissilodinium spp. (Plate 6, figs 2, 4) Dodekovia tegillata Prauss 1989 Foraminiferal linings (Plate 4, fig. 3) Fungal spp. Kallosphaeridium spp. Lecaniella foveata Singh 1971 Leiosphaeridia spp. Limbicysta bjaerkei (Smelror) MacRae et al. 1996 Mancodinium semitabulatum Morgenroth 1970 (Plate 6, fig. 1) M. spp. Mendicodinium groenlandicum (Pocock & Sarjeant) Davey 1979 (Plate 6, fig. 3) M. reticulatum Morgenroth 1970 M. spp. Miscellaneous Nannoceratopsis ambonis Drugg 1978 (Plate 5, fig. 3) N. gracilis Alberti emend. van Helden 1977 (Plate 5, fig. 1) N. plegas Drugg 1978 (Plate 5, fig. 4) N. ridingii Poulsen 1992 N. senex van Helden 1977 (Plate 5, fig. 2) N. spp. N. triangulata Prauss 1987 N. triceras Drugg 1978 Pareodinia ceratophora Deflandre 1947 P. halosa (Filatoff) Prauss 1989 (Plate 4, fig. 6) P. spp. Parvocysta barbata Bjærke 1980 P. spp. Phallocysta eumekes Dörhöfer & Davies 1980 P. thomasi Smelror 1991 P. spp. Pterospermella spp Scrinocassis weberi Gocht 1964 S. spp. Sentusidinium pelionense Fensome 1979 (Plate 6, figs 5, 6) S. spp. Susadinium scrofoides (Dörhöfer & Davies) Below 1987 Tasmanites spp. Valensiella ovulum (Deflandre) Eisenack 1963 Veryhachium collectum Wall 1965 V. formosum Stockmans & Williere 1960 V. sortehatense Fensome 1979 (Plate 4, fig. 2) V. spp. Wallodinium laganum Feist-Burkhardt & Monteil 1994 (Plate 4, fig. 5) 799 Plates 1–6 800 Plate 1 Figs 1–4 and 6–8 are from the Lepidopteriselv section, fig. 5 is from the borehole at Sortehat, the type locality of the Sortehat Formation. Scale bar is 10 microns. For each of the illustrated specimens, the EFR (England Finder Reference) is given. Fig. 1. Retitriletes austroclavatidites. Sample 398181, slide 3, EFR E36. Fig. 2. Retitriletes clavatoides. Sample 398181, slide 3, EFR F50. Fig. 3. Baculatisporites comaumensis. Sample 398158, slide 4, EFR S26. Fig. 4. Striatella jurassica. Sample 398158, slide 5, EFR K271. Fig. 5. Staplinisporites caminus. Sample 303143-26, slide 3, EFR J51. Fig. 6. Ischyosporites sp. Sample 398189, slide 4, EFR M40. Fig. 7. Tripartina variabilis. Sample 398189, slide 4, EFR R43. Fig. 8. Manumia delcourtii. Sample 398192, slide 4, EFR W383. 801 1 2 4 3 5 6 7 8 802 Plate 2 Figs 1 and 4–6 are from the borehole at Sortehat, figs 2 and 3 are from the Lepidopteriselv section. Scale bar is 10 microns. Fig. 1. Callialasporites dampieri. Sample 303143-46, slide 3, EFR F222. Fig. 2. Callialasporites turbatus. Sample 398158, slide 4, EFR P25. Fig. 3. Callialasporites microvelatus. Sample 398158, slide 4, EFR H382. Fig. 4. Chasmatosporites hians. Sample 303143-46, slide 3, EFR L42. Fig. 5. Perinopollenites elatoides. Sample 303143-13, slide 3, EFR N25. Fig. 6. Chasmatosporites major. Sample 303143-46, slide 3, EFR K43. 803 1 2 4 3 5 6 804 Plate 3 Figs 1, 2, 5 and 6 are from the Lepidopteriselv section, figs 3 and 4 are from the borehole at Sortehat. Scale bar is 10 microns. Fig. 1. Exesipollenites tumulus. Sample 398181, slide 3, EFR J362. Fig. 2. Corollina torosus. Sample 398158, slide 5, EFR M33. Fig. 3. Cerebropollenites macroverrucosus. Sample 303143-40, slide 3, EFR F24. Fig. 4. Spheripollenites sp. Sample 303143-46, slide 3, EFR W20. Fig. 5. Quadraeculina anellaeformis. Sample 398158, slide 4, EFR S384. Fig. 6. Pinuspollenites minimus. Sample 398158, slide 5, EFR D522. 805 1 2 4 3 5 6 806 Plate 4 Figs 1, 2 and 6 are from the borehole at Sortehat, figs 3–5 are from the Lepidopteriselv section. Scale bar is 10 microns. Fig. 1. Chomotriletes minor. Sample 303143-46, slide 3, EFR K46. Fig. 2. Veryhachium sortehatense. Sample 303143-46, slide 3, EFR H22. Fig. 3. Foraminiferal inner lining. Sample 398158, slide 4, EFR H31. Fig. 4. Botryococcus sp. Sample 398189, slide 4, EFR E492. Fig. 5. Wallodinium laganum. Sample 398194, slide 4, EFR Z39. Fig. 6. Pareodinia halosa. Sample 303143-26, slide 3, EFR M51. 807 1 2 4 3 5 6 808 Plate 5 Fig. 1 is from the Lepidopteriselv section, figs 2–4 are from the borehole at Sortehat. Scale bar is 10 microns. Fig. 1. Nannoceratopsis gracilis. Sample 398158, slide 4, EFR H54. Fig. 2. Nannoceratopsis senex. Sample 303143-40, slide 3, EFR S363. Fig. 3. Nannoceratopsis ambonis. Sample 303143-46, slide 3, EFR J40. Fig. 4. Nannoceratopsis plegas. Sample 303143-40, slide 3, EFR M482. 809 1 2 43 810 Plate 6 Figs 1, 2 and 4–6 are from the borehole at Sortehat, fig. 3 is from the Lepidopteriselv section. Scale bar is 10 microns. Fig. 1. Mancodinium semitabulatum. Sample 303143-46, slide 3, EFR S264. Fig. 2. Dissilodinium sp. Sample 303143-30, slide 3, EFR K324. Fig. 3. Mendicodinium groenlandicum. Sample 398158, slide 5, EFR R39. Fig. 4. Dissilodinium sp. Sample 303143-26, slide 3, EFR C54. Fig. 5. Sentusidinium pelionense. Sample 303143-20, slide 3, EFR M51. Fig. 6. Sentusidinium pelionense. Sample 303143-26, slide 3, EFR E53. 811 1 2 3 4 5 6 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).