Geological Survey of Denmark and Greenland Bulletin 22, 2010, pp. 92 GEOLOGICAL SURVEY OF DENMARK AND GREENLAND BULLETIN 22· 2010 Lithostratigraphy of the Upper Oligocene – Miocene succession of Denmark Erik Skovbjerg Rasmussen, Karen Dybkjær and Stefan Piasecki GEOLOGICAL SURVEY OF DENMARK AND GREENLAND MINISTRY OF CLIMATE AND ENERGY Bulletin 22_ GSB191-Indhold 04/03/11 12.40 Side 1 Geological Survey of Denmark and Greenland Bulletin 22 Keywords Lithostratigraphy, Miocene, Upper Oligocene, North Sea, Denmark Cover Upper shoreface sands of the Billund Formation in the Addit gravel pit, central Jylland showing prominent burrows (Ophiomorpha isp.); illustrated section is 40 cm high. Photo: Tom Pallesen. Frontispiece Outcrop of the Kolding Fjord Member, Klintinghoved Formation at Hagenør, Lillebælt. The succession is dominated by organic-rich, lagoonal, silty clay and sand beds deposited as washover fans on the back-barrier flat. Photo: Peter Warna-Moors. Chief editor of this series: Adam A. Garde Editorial board of this series: John A. Korstgård, Department of Earth Sciences, University of Aarhus; Minik Rosing, Geological Museum, University of Copenhagen; Finn Surlyk, Department of Geography and Geology, University of Copenhagen Scientific editor of this volume: Jon R. Ineson Editorial secretaries: Jane Holst and Esben W. Glendal Referees: Dan Evans (UK) and Claus Heilmann-Clausen (DK) Illustrations: Stefan Sølberg Digital photographic work: Benny M. Schark Layout and graphic production: Henrik Klinge Pedersen Printers: Rosendahls · Schultz Grafisk a/s, Albertslund, Denmark Manuscript received: 15 December 2009 Final version approved: 1 November 2010 Printed: 31 December 2010 ISSN 1604-8156 ISBN 978-87-7871-291-2 Citation of the name of this series It is recommended that the name of this series is cited in full, viz. Geological Survey of Denmark and Greenland Bulletin. If abbreviation of this volume is necessary, the following form is suggested: Geol. Surv. Den. Green. Bull. 22, 92 pp. Available from Geological Survey of Denmark and Greenland (GEUS) Øster Voldgade 10, DK-1350 Copenhagen K, Denmark Phone: +45 38 14 20 00, fax: +45 38 14 20 50, e-mail: geus@geus.dk or at www.geus.dk/publications/bull © De Nationale Geologiske Undersøgelser for Danmark og Grønland (GEUS), 2010 For the full text of the GEUS copyright clause, please refer to www.geus.dk/publications/bull Bulletin 22_ GSB191-Indhold 04/03/11 12.40 Side 2 Bulletin 22_ GSB191-Indhold 04/03/11 12.40 Side 3 4 Contents Abstract . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 5 Introduction . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 7 Geological setting . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 9 Previous studies . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 11 Previous lithostratigraphic subdivision . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 11 Vejle Fjord Formation . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 11 Klintinghoved, Ribe and Arnum Formations . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 12 Arnum, Hodde, Gram and Sæd Formations . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 12 Odderup Formation (terrestrial Miocene) . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 12 Sequence stratigraphy and onshore–offshore correlation . . . . . . . . . . . . . . . . . . . . . . . . . . 13 Data and methodology . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 14 Revised lithostratigraphy . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 16 Brejning Formation . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 16 Sydklint Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 20 Øksenrade Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 21 Ribe Group . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 24 Vejle Fjord Formation . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 27 Skansebakke Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 32 Billund Formation . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 34 Hvidbjerg Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 36 Addit Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 40 Klintinghoved Formation . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 45 Kolding Fjord Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 50 Bastrup Formation . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 53 Resen Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 55 Arnum Formation . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 56 Vandel Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 58 Odderup Formation . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 59 Stauning Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 61 Fasterholt Member . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 63 Måde Group . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 65 Hodde Formation . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 66 Ørnhøj Formation . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 68 Gram Formation . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 70 Marbæk Formation . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 72 Stratigraphic architecture . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 75 Palaeogeography . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 80 Acknowledgements . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 87 References . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 88 Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 4 5 Abstract Authors’ address Geological Survey of Denmark and Greenland, Øster Voldgade 10, DK-1350 Copenhagen K, Denmark. E-mail: esr@geus.dk *Present address: University of Copenhagen, Øster Voldgade 10, DK-1350 Copenhagen K, Denmark. Rasmussen, E.S., Dybkjær, K. & Piasecki, S*. 2010: Lithostratigraphy of the Upper Oligocene – Miocene succession of Denmark. Geological Survey of Denmark and Greenland Bulletin 22, 92 pp. This paper presents a revised lithostratigraphic scheme for the uppermost Upper Oligocene – Miocene succession of Denmark. The marine Oligocene Brejning Clay Member is upgraded to formation sta- tus and includes the Sydklint Member and the Øksenrade Member (new). The shallow marine and deltaic deposits of mainly Early Miocene age are included in the Ribe Group (new) while the fully marine Middle and Upper Miocene clay-rich deposits are referred to the Måde Group (new). The Ribe Group is subdivided into 6 formations: the Vejle Fjord Formation is revised and includes the Skansebakke Member, the Billund Formation (new) includes the Addit and Hvidbjerg Members (new), the Klintinghoved Formation is redefined formally and includes the Koldingfjord Member (new), the Bastrup Formation (new) includes the Resen Member (new), the Vandel Member is a new member in the Arnum Formation (revised), the Odderup Formation is redefined and includes the Stauning Member (new) and the coal- bearing Fasterholt Member. The Måde Group is subdivided into the Hodde, Ørnhøj (new), Gram and Marbæk (new) Formations. Subdivision of the Upper Oligocene – Miocene succession into two groups, the Ribe and Måde Groups, is compatible with the North Sea lithostratigraphic framework where they correlate with the upper part of the Hordaland Group and the Nordland Group, respectively. The revised lithostratigraphic framework correlated in three dimensions provides rigorous con- straints on the palaeogeographic interpretation of the Late Oligocene – Miocene period. Three major deltaic units (Billund, Bastrup and Odderup Formations) prograded from the north and north-east into the North Sea Basin during the Early – early Middle Miocene. Delta progradation was punctuated by deposition of marine clay and silt associated with minor transgressive events (Vejle Fjord, Klintinghoved and Arnum Formations). During the Middle–Late Miocene, marine depositional conditions dominated (Hodde, Ørnhøj and Gram Formations). A fourth and final progadational event (Marbæk Formation) commenced in the latest Tortonian heralding the emergence of present-day Denmark (including the North Sea sector). Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 5 6 Fig. 1. Map showing the location of the study area in Jylland, western Denmark, and the boreholes, outcrops and seismic data used. Towns and villages mentioned in the text are indicated. The index map (lower right) shows the localities in the Fredericia–Kolding area. 56°N Fig. 77 Fig. 78 57°N 56°N 55°N 8°E 10°E Fig. 79 Borehole Outcrop Town Seismic lines Seismic sections shown in figures 25 km Voervadsbro Sdr. Vissing ÅrhusSilkeborg Føvling Rømø Sylt Ribe Ribe Gram Arnum-1 Rødding Estrup Bastrup Lillebælt HvidbjergPjedsted Vejle Fjord Horsens Fjord Limfjorden Kvong Forumlund Marbæk Sjelborg Måde Esbjerg Borg-1 Løgumkloster Vollerup Vester Sottrup Hørup HavSønderborg Klintinghoved TinglevSæd V. Torsted Lundgård Hodde Vorbasse Grindsted Billund Billund Vandel Gadbjerg Almstok Egtved Andkær Skansebakke Vejle Horsens Søvind JuelsmindeSanatoriet Fakkegrav Brejning Brejning Hoved Jensgård Dykær StakrogeOdderupSkjern Assing Mølleby Hammerum Herning Isenvad Fasterholt Søby Store Vorslunde Give Brande Hjøllund Fjelstervang Fjand Ulfborg Ørnhøj, Lille Spåbæk Abildå Holstebro Klosterhede Vind Stensig Stauning Sdr. Vium Resen Brøndum Lyby Mogenstrup Gyldendal Søndbjerg Lodbjerg Skyum Skyum Bjerge Skanderup Thisted Silstrup Klovbakker Mors Sunds Ikast Bording Mausing Sorring Sofienlund Hinge Ølst Gl. Rye Morsholt Salten Addit Addit Mark Uldum Lindved Hovslund Hellevad Struer Skive Viborg Vonsild Kolding Fjord Flensborg Fjord Lillebæ lt Middelfart Fredericia Øksenrade Fænø Hindsgavl Galsklint Kolding Røjle Klint Børup Rønshoved Hagenør Lillebælt North Sea UK Norway Sweden Germany Poland Denmark Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 6 7 Sediments of Miocene age crop out in Denmark along the east coast of Jylland and in the Limfjorden area (Fig. 1); a few inland cliffs in central Jylland also expose Miocene deposits, especially in river scars and road cuts. Excavation for raw materials for construction, i.e. gravel, sand and clay, has resulted in open pits that expose Miocene deposits, mainly in western and central Jylland. During the last decade, the increasing need for water for domestic pur- poses and irrigation has initiated intensive drilling pro- grams and the acquisition of high-resolution seismic data from the Miocene succession. The renewed interest in the Miocene has resulted in financial support for field investi- gations, so it has been possible to re-study all Danish out- crops exposing Miocene deposits. A high-resolution biostratigraphic subdivision of the Miocene succession has been developed, based on dinofla- gellate cysts (dinocysts) (Dybkjær & Piasecki 2010). This new dinocyst zonation has provided a robust framework within which the studied boreholes have been correlated. It has also made it possible to integrate all seismic and bore- hole data with the new, detailed sedimentological descrip- tions and interpretations of the outcrops (Friis et al. 1998; Rasmussen & Dybkjær 2005; E.S. Rasmussen et al. 2006) in order to construct a depositional model for the Miocene succession. Associated studies, for example of the climatic conditions (Larsson et al. 2006; Larsson-Lindgren 2009; T. Utescher, personal communication 2009) and sediment provenance (Knudsen et al. 2005; Olivarius 2009), have further added to the understanding of the depositional sys- tem. The lithostratigraphy presented here encompasses the upper Upper Oligocene – Miocene succession found onshore Denmark. It is bounded beneath by a major unconformity between Upper Eocene – lower Upper Oligocene clay-rich deposits and silt- and sand-rich deposits of late Late Oligocene – Miocene age. The top of the successsion is defined by the Quaternary unconformity. During the study of the succession, it was necessary to establish a number of informal lithostratigraphic units that are now widely used in the mapping of aquifers both in Denmark and Germany, and are increasingly adopted in the literature (Rasser et al. 2008; Knox et al. 2010). It is therefore timely to formally define these units and redefine existing lithostratigraphic units in order to construct a consistent lithostratigraphic framework. The Miocene succession was deposited during a period of worldwide tectonism (Potter & Szatmari 2009) and marked climatic change (e.g. Zachos et al. 2001; Miller et al. 2005; Utescher et al. 2009). Two of the most distinct phases in the Alpine orogeny commenced in the Miocene, the Late Oligocene – Early Miocene Savian Phase and the Middle Miocene Betic Phase (Ziegler 1982; Oszczypko 2006; Ribero et al.1990). The opening of the North Atlantic was characterised by the final change in spreading from the Aegir Ridge to the Kolbeinsey Ridge and increasing spreading rates in the Early Miocene have been detected (Mosar et al. 2002; Doré et al. 2008). In the Middle Miocene, a major tectonic reorganisation occurred (Ziegler 1982; Doré et al. 2008). The climate was warm temperate in the Early – early Middle Miocene, but changed to a cold temperate climate in the Late Miocene. The Miocene succession studied here was deposited in the eastern part of the North Sea Basin (Fig. 2). The onshore portion of this basin under focus here is a stratigraphically complete fluvial – deep shelf transect that is recorded in detail by outcrop, borehole and seismic data; it provides a nat- ural laboratory for the study of the development of fluvio- deltaic depositional systems, the tectonic impact on basin evolution and the consequences of climatic changes includ- ing glacio-eustatic sea-level changes. In addition to creat- ing a robust and consistent framework for practical applications, therefore, the lithostratigraphic revision pre- sented here is a prerequisite for future research into Miocene climatic, tectonic and eustatic evolution. Introduction Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 7 8 Fig. 2. Palaeogeographic reconstruction of North-West Europe during the Early Miocene (modified from E.S. Rasmussen et al. 2008); configuration based on Mosar et al. (2002). 100 km Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 8 9 The evolution of the North Sea Basin was strongly influ- enced by the collision between the African and European tectonic plates, volcanism in central Europe and the open- ing of the North Atlantic (Ziegler 1982; 1990; Ziegler et al. 1995; Martinsen et al. 1999; Faleide et al. 2002; E.S. Rasmussen et al. 2005, 2008; Rasmussen 2009a; Gabrielsen et al. 2010). Interaction of these factors with changing eustatic sea level resulted in final closure of the southern connection with the Tethyan ocean during Early–Middle Miocene times (Harzhauser & Piller 2007); subsequently, the only connection to the Atlantic was through a strait between Norway and Shetland (Fig. 2). The depositional basin of the eastern North Sea area which covered present-day Denmark, was bounded towards the north-east by the Fennoscandian Shield (Fig. 3; Bertelsen 1978; Vejbæk 1997). The transition to the basin was con- trolled by the SE–NW-trending Sorgenfrei–Tornquist Zone. The basin was subdivided into two subbasins: the Norwegian –Danish Basin and the North German Basin, with the ESE–WNW-striking Ringkøbing–Fyn High sep- arating the subbasins. The Ringkøbing–Fyn High is fur- ther segmented into a number of N–S-trending elements such as the Brande Trough (Fig. 3). These structural ele- ments were formed during Permian rift tectonics and later reactivated in the Jurassic and during Late Cretaceous and Early Paleocene inversion tectonics (Ziegler 1990; Liboriussen et al. 1987; Mogensen & Jensen 1994; Vejbæk & Andersen 2002). Reactivation of some of the older struc- tures occurred in the Oligocene as well as in the Miocene (E.S. Rasmussen 2004a, 2009a; Japsen et al. 2007). During the Middle Miocene, the North Sea Basin experienced increased regional subsidence (Ziegler 1982, 1990; Vejbæk 1992; Koch 1989; Michelsen et al. 1998; Clausen et al. 1999; E.S. Rasmussen 2005). In the late Pliocene – early Plei - stocene, the North Sea Basin was tilted towards the south- west (Japsen 1993; Japsen & Bidstrup 1999; Japsen et al. 2002; E.S. Rasmussen et al. 2005). The North Sea Basin was located in the northern west- erly wind belt. The climate was warm temperate to tropi- cal in the early part of the Paleogene (Buchardt 1978; Heilmann-Clausen & Surlyk 2006; Zachos et al. 2001). A dramatic change occurred at the Eocene–Oligocene tran- sition where a distinct climatic cooling took place. The early Oligocene icehouse climate resulted in a marked eusta- tic sea-level drop due to growth of ice caps, primarily on Antartica (Buchardt 1978; Prentice & Matthew 1988; Miller et al. 1991, 1996, 1998, 2005; Zachos et al. 2001). However, by the end of the Oligocene a subtropical climate prevailed in the North Sea Basin area (T. Utescher, personal communication 2009; Larsson et al. 2010). At the bound- ary between the Palaeogene and the Neogene, a marked, but transient, climatic cooling occurred with buildup of widespread ice caps on Antarctica. This climatic event resulted in a major, global sea-level fall (Miller et al. 1998; Zachos et al. 2001). The Early Miocene climate in the North Sea Basin area was characterised by an oscillation between cool temperate and warm temperate climates (Mai 1967; Larsson et al. 2006). An overall increase in temper- ature culminated at the Early to Middle Miocene transi- tion, the so-called ‘Mid-Miocene climatic optimum’ (Buchardt 1978; Zachos et al. 2001). In the North Sea Basin area, a warm temperate to subtropical climate pre- vailed (Mai 1967; Friis 1975; Utescher et al. 2000, 2009). Geological setting Fig. 3. Structural elements in the study area. Modified from Berthelsen (1992). 57°N 56°N 55°N 58°N 8°E 12°E10°E Norway Denmark Sweden Germany Ringkøbing – Fyn High Sorgenfrei–Tornquist Zone 50 km Faults Positive structural elements Norwegian–Danish Basin Fennoscandian Shield Rødd ing G ra be n Brande Trough Tønder Graben Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 9 10 At the termination of the Middle Miocene, a marked drop in global temperature commenced and during most of the Late Miocene the North Sea Basin area was characterised by a cool temperate climate (Buchardt 1978; Utescher et al. 2000, 2009; Zachos et al. 2001; Larsson-Lindgren 2009). Fine-grained siciliclastic sediments of mainly deep marine origin were deposited in Denmark and the North Sea Basin during the post-Danian Palaeogene (Heilmann-Clausen et al. 1985; Heilmann-Clausen 1995; Schiøler et al. 2007). A general sea-level lowstand and tectonic re-organisation during the Oligocene resulted in erosion or non-deposition, especially in the central and southern part of the study area. In the northern part of the North Sea Basin, prodeltaic, clay-dominated wedges were laid down. In the latest Oligocene, renewed transgression resulted in the deposi- tion of glaucony-rich clay. This was followed by deposition of deltaic and coastal-plain sand and clay in the Early Miocene. Three major deltaic progradational pulses occurred during the Early Miocene; the third and final pulse was char- acterised by extensive coal deposition. Subsequent to depo- sition of the dominantly fluvio-deltaic deposits in the Early to early Middle Miocene, full marine, clay-rich sedimen- tation dominated during the remaining part of the Middle and Late Miocene. Late Pliocene – early Pleistocene tilting of the eastern North Sea area (Japsen 1993; Japsen & Bidstrup 1999; Japsen et al. 2002; E.S. Rasmussen et al. 2005), combined with periodic growth of ice caps in the northern hemi- sphere, resulted in base-level fall and marked erosion of the substratum; Middle and Upper Miocene deposits are thus missing in the eastern and northern parts of Jylland (Fig. 4). Lower Miocene Oligocene Eocene Middle–Upper Paleocene Lower Paleocene (Danian) Upper Cretaceous Lower Cretaceous and older Middle–Upper Miocene 50 km57°N 56°N 55°N 8°E 12°E 10°E Fig. 4. Pre-Quaternary subcrop map of Denmark. Modified from Sorgenfrei & Berthelsen (1954) and Håkansson & Pedersen (1992). Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 10 11 J.G. Forchhammer (1794–1865) wrote the first account of the geology of Denmark (Forchhammer 1835; see also Garboe 1961) and described the Diluvial ‘Rullestens - dannelse’ (loosely translated as ‘boulder formation’) which he recognised throughout Denmark; this unit was partly included in the Tertiary. The lower part was named the ‘amber–brown-coal formation’ (translated from Danish) and included fossiliferous strata of ‘the western system’, which was recognised in west and central Jylland as well as farther south in Germany, for example on the island of Sylt (Fig. 1). This ‘western system’ undoubtedly included the marine Miocene as recognised today. Beyrich (1853) studied molluscs collected by Forchhammer from Sylt and informed Forchhammer in 1854 that he had identified these as a Miocene fauna (Garboe 1961). Molluscs from south-west Jylland (e.g. Esbjerg and Gram) were also iden- tified as being of Miocene age, and the results were presented at the 11th Scandinavian Research Meeting in Copenhagen in 1873 (Mørch 1874). The palaeontologist J.P.J. Ravn (1866–1951) established the first Miocene (and Oligocene) stratigraphy of Denmark based on his comprehensive study of the fossil faunas in dark brown and grey, mica-rich clay which occurred widely in Jylland. The resulting stratigraphic scheme of the Lower, Middle and Upper Miocene and associated deposits (Ravn 1906) was published one year before his monograph on the Oligocene and Miocene mollusc faunas (Ravn 1907). Ravn realised that Lower Miocene marine faunas were missing and therefore suggested that the widespread brown-coal deposits represented the Lower Miocene. He also included part of the mica-rich clay and sand succession of the Lillebælt region in south-east Jylland in the Lower Miocene, based on mixed Oligocene–Miocene faunas. The botanist N.E.K. Hartz (1867–1937) studied the succession that includes brown-coal deposits. Exposures of brown coals were scarce at that time, but he concluded that the coals and the asso- ciated mica-rich sediments are all freshwater deposits (Hartz 1909) and he found no evidence to contradict the Early Miocene age suggested by Ravn (1906). The Geological Survey of Denmark (DGU) performed two drilling campaigns in 1917 and 1921 under the lead- ership of V. Milthers, and more brown-coal deposits were located. Later, on the initiative of K. Milthers, DGU drilled almost 9000 boreholes during the years between 1941 and 1949 (L.B. Rasmussen 1988). In the last campaign (1958–1963), more than 2000 boreholes were drilled, mak- ing a total of approximately 11 000 boreholes (L.B. Rasmussen 1988). In addition to engineering data, these extensive programmes also yielded geological results such as the volume, numbers and extent of brown-coal seams. The Middle–Upper Miocene succession was not well under- stood prior to the Second World War but the second drilling campaign revealed the overall stratigraphy and approxi- mate thickness of these strata (Milthers 1949; Heller 1960). These workers proposed the existence of two discrete coal- bearing units (probably broadly equivalent to the Ribe and Odderup Formations of later workers, see below) under- lying c. 100 m of Middle Miocene marine sediments (the Arnum Formation of later workers). Previous lithostratigraphic subdivision Prior to this study, the Upper Oligocene – Miocene suc- cession of onshore Denmark had been subdivided lithos- tratigraphically into a number of formal and informal units. The origin of these terms is discussed briefly below to pro- vide the background to the lithostratigraphic revision pre- sented in this bulletin. Vejle Fjord Formation The mixed Oligocene–Miocene fauna reported by Ravn (1907) from the Lillebælt region (Fig. 1) impelled Eriksen (1937) to study the same succession in this region for fos- sils; he found a sparse mollusc fauna in the Brejning expo- sure on the south coast of Vejle Fjord and in neighbouring cliffs. The fauna in the lower, glauconitic strata was of Oligocene age, but the sparse fauna in the overlying black, micaceous clay was suggested to be of Early Miocene age. The uppermost beds of the succession, comprising mica- ceous, grey sand, were barren of fossils. Larsen & Dinesen (1959) studied the same strata in two exposures and for- mally established the Vejle Fjord Formation which con- sisted of the glauconitic Brejning Clay and the overlying, black to grey, micaceous clay and sand of the Vejle Fjord Clay and Vejle Fjord Sand, respectively. Analysis of the foraminifer fauna in the Brejning Clay clearly indicated an Upper Oligocene affinity whereas a contrasting foraminifer fauna in the overlying, basal Vejle Fjord Clay was suggested to indicate an Early Miocene age (Larsen & Dinesen 1959). These data supported the results based on the mollusc fauna, indicating that most of the formation, i.e. the Vejle Previous studies Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 11 12 Fjord Clay and Vejle Fjord Sand”, should be referred to the Lower Miocene. The Oligocene–Miocene transition was thus placed near the shift from the glauconitic Brejning Clay to the black pyritic clay of the Vejle Fjord Clay. In the following years, the Vejle Fjord Clay and Vejle Fjord Sand were systematically excluded from most Mio - cene stratigraphic schemes (e.g. L.B. Rasmussen 1961). It was not until much later that Danish stratigraphers incor- porated the Vejle Fjord Formation and the foraminifer stratigraphy in a Miocene stratigraphic scheme, although maintaining the Vejle Fjord Formation and Klintinghoved Formation (see below) as separate geographic entities (Buchardt-Larsen & Heilmann-Clausen 1988). Farther north in Jylland, Christensen & Ulleberg (1973) defined the Sofienlund Formation which was divided into four members: the Ulstrup Clay, the Sofienlund Clay, the Sofienlund Silt and the Sofienlund Sand. The foraminifer content of the Sofienlund Formation suggested a Chattian age for the two lower members and a post-Chattian age for the upper two members (Christensen & Ulleberg 1973). The lithology and biostratigraphy clearly indicate that these sediments should have been referred to the previously estab- lished Vejle Fjord Formation. A similar view was stated by Larsen & Kronborg (1994), according to whom the lower two members are equivalent to the Brejning Clay whereas the upper two members equate to the Vejle Fjord Clay and Vejle Fjord Sand. The Sofienlund Formation is abandoned herein. The Sydklint Member was erected in north-west Jylland and provisionally referred to the basal Vejle Fjord Formation by Heilmann-Clausen (1997); this member is re-assigned to the Brejning Formation in this bulletin. Klintinghoved, Ribe and Arnum Formations The fossil mollusc fauna of the Lower and Middle Miocene, exemplified by fauna from the coastal cliff at Klintinghoved and seven deep wells in southern Jylland, was studied by Sorgenfrei (1940, 1958). The Klintinghoved Formation (of present usage) was not defined formally, but arose from extensive palaeontological work on the outcrop of a glacial, dislocated and folded raft of sediments that was considered to be of Early Miocene age (Sorgenfrei 1940). Sorgenfrei (1957) included the ‘Klintinghoved Mica Clay’ as a formal formation in his ‘Formations of Denmark’ in Lexique Stratigraphique. Two new formations were defined on the basis of the deep wells, the Ribe and Arnum Formations; the marine clay of the Arnum Formation was referred to the Middle Miocene on the basis of the fauna (Sorgenfrei 1958). The faunally barren Ribe Formation, composed of quartzitic sand, was recorded below the fossiliferous Arnum Formation in one well near the town of Ribe. In the Danish American Prospecting Company (DAPCO) well at Arnum, Sorgenfrei (1958) tentatively referred quartz-rich gravel and sand, below mud and sand of the Arnum Formation, to the Ribe Formation and underlying clays to the Klintinghoved Formation based solely on the lithological succession, in the absence of a mollusc fauna. Arnum, Hodde, Gram and Sæd Formations In the comprehensive stratigraphic work by L.B. Rasmussen (1958, 1961, 1966, 1968), focus was on the upper Arnum Formation, and the Hodde and Gram Formations; the lat- ter two formations were formally erected (L.B. Rasmussen 1961). He continued and extended Sorgenfrei’s work, pro- ducing a biostratigraphic zonation of this stratigraphic interval. L.B. Rasmussen (1966) referred the Gram Formation (including the silt interval encountered in the borehole at Sæd) to the Upper Miocene and the Hodde Formation to the Middle Miocene (Fig. 5), assignments that have been largely confirmed by later work. L.B. Rasmussen (1961; see also Laursen et al. 1998) suggested that sandy strata overlying the Gram Clay in south-west Jylland could be of Messinian (latest Miocene) age based on a mollusc fauna that was considered to be incompatible with the upper Gram Clay faunas; the Sæd Formation, overlying the Gram Formation, was thus pro- posed. Hinsch (1990) re-evaluated this mollusc fauna, how- ever, demonstrating equivalence to the Tortonian fauna in the uppermost Gram Formation; this is supported by dinoflagellate floras in the same strata (Piasecki 2005). The Sæd Formation is therefore abandoned in the present paper. Odderup Formation (terrestrial Miocene) The Odderup Formation was erected by L.B. Rasmussen (1961) as the brown-coal and quartz-sand succession between the marine clays of the Arnum Formation and the overlying Hodde Formation. The observation of brown-coal or coal fragments and quartz sands below the marine Arnum Formation in certain wells, however, complicated the strati- graphic concept, but L.B. Rasmussen (1961) envisaged two major prograding deltaic units (Ribe and Odderup Formations) subdividing the marine Miocene into three major units (Klintinghoved Formation, Arnum Formation, Hodde–Gram Formations, see Fig. 5). The geology of the Søby–Fasterholt area was published by Koch (1989) in a comprehensive resumé of palaeo - Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 12 13 botanical, sedimentological and stratigraphic studies, includ- ing an analysis of the brown-coal seams. In this area, the Odderup Formation is bounded by marine strata of the Arnum Formation beneath and the overlying marine suc- cession of the Hodde and Gram Formations. That part of the Odderup Formation containing brown coals was defined as the Fasterholt Member. Sequence stratigraphy and onshore–offshore correlation In a study of the Cenozoic of the Danish North Sea, Michelsen (1994; Michelsen et al. 1998) divided the late Palaeogene–Neogene succession into 3 allostratigraphic units: Units 5 to 7. The succession was further subdivided into 11 depositional sequences. The unconformities recog- nised in the offshore geophysical data were not directly correlated onshore using seismic data, but were correlated to the onshore lithostratigraphic units based on the bio - stratigraphic data available at that time. The Danish off- shore stratigraphy was integrated with the UK and Nor we- gian stratigraphy: Units 5 and 6 were correlated with the upper Hordaland Group (Lark Formation of Schiøler et al. 2007) whilst Unit 7 was correlated with the Nordland Group. Sequence stratigraphy was applied to the onshore Mio - cene succession in southernmost Jylland based on the analy- sis of petrophysical logs from 6 wells combined with seismic data (E.S. Rasmussen 1996). The succession was divided into 6 depositional sequences ranging in age from the lat- est Oligocene to the latest Miocene. Precise dating of these sequences was precluded by a general lack of biostrati- graphic data but the sequence stratigraphic framework was correlated with the existing lithostratigraphy. E.S. Rasmussen (2004b) introduced a new sequence stratigraphic subdivi- sion, this time based on 16 new boreholes, outcrops and multichannel seismic data distributed in central and south- ern Jylland. This resulted in subdivision of the upper Oligocene – Miocene succession into 6 depositional sequences, a framework similar to that of E.S. Rasmussen (1996), although the ages of the sequences were refined on the basis of dinoflagellate cyst stratigraphy that was estab- lished over this period and formalised recently (Piasecki 1980, 2005; Dybkjær & Rasmussen 2000, 2007; Dybkjær 2004a, b; Dybkjær & Piasecki 2008, 2010). Fig. 5. Miocene lithostratigraphy of western Denmark as defined by L.B. Rasmussen (1961). Hodde Formation Arnum Formation Klintinghoved Formation Upper Miocene Middle Miocene Lower Miocene Lithostratigraphy Gram Formation West East Chrono- stratigraphy Marine deposits Fluvio-deltaic deposits Odderup Formation Ribe Formation Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 13 14 Data and methodology 10 15 20 a b NN12 N N 1 1 NN10 NN9 NN8 NN6 NN5 NN4 NN3 NN2 NN1 NP25 NN7 L at e M id d le E ar ly M io ce n e Oligocene A ge ( M a) Epoch Stage (Ages in Ma) N an n o p la n kt o n zo n at io n Dinoflagellate cysts zonation: Denmark (Dybkjær & Piasecki 2010) Dinoflagellate events Zonation Messinian Tortonian Serravallian Langhian Burdigalian Aquitanian Chattian 23.03 20.43 15.97 13.65 11.61 7.25 5.33 Amiculosphaera umbracula Barssidinium evangelinae Selenopemphix armageddonensis Hystrichosphaeropsis obscura Palaeocystodinium spp. Gramocysta verricula Achomosphaera andalousiense Unipontidinium aquaeductum Unipontidinium aquaeductum Systematophara spp. Cannosphaeropsis passio Distatodinium biffii Deflandrea phosphoritica, common Chiropteridium galea Caligodinium amiculum Thalassiphora pelagica Thalassiphora rota Cordosphaeridium cantharellus Exochosphaeridium insigne Homotryblium spp. abundant Labyrinthodinium truncatum Labyrinthodinium truncatum Cousteaudinium aubryae Cousteaudinium aubryae Ectosphaeropsis burdigalensis Exochosphaeridium insigne Sumatradinium hamulatum Palaeocystodinium miocaenicum Palaeocystodinium miocaenicum Cerebrocysta poulsenii H. obscura (H. o.) G. verricula (G. v.) A. andalousiense (A. a.) U. aquaeductum (U. a.) L. truncatum (L. t.) A. umbracula (A. u.) C. cantharellus (C. c.) E. insigne (E. i.) C. aubryae (C. au.) C. galea (C. g.) D. phosphoritica (D. p.) S. hamulatum (S. h.) T. pelagica (T. p.) C. amiculum (C. am.) Homotryblium spp. (H. spp) Maximum occurrence First stratigraphic occurrence Last stratigraphic occurrence Fig. 6. Dinocyst zonation for the upper- most Oligocene – Miocene succession onshore Denmark, from Dybkjær & Piasecki (2010). The ages of the stage boundaries are from Gradstein et al. (2004), the nannoplankton zonation from Martini (1971). NN: Neogene nanno- plankton zone. NP: Palaeogene nanno- plankton zone. Dinoflagellate events indicated in black define zone boundaries, those indicated in grey are additional diag- nostic events. Twenty-five outcrops, one cored borehole at Sdr. Vium (DGU no. 102.948) and c. 50 boreholes, drilled using the airlift drilling technique, were available for the study (Fig. 1). Most of the boreholes were drilled in order to solve stratigraphic problems, but some were drilled in order to test seismic facies interpretations. All boreholes are identi- fied by their DGU borehole numbers, whereas outcrops are referred to by the nearest locality name. All 25 outcrops and the cored borehole were described sedimentologically and samples taken for biostratigraphy. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 14 15 The grain size and mineralogy of the airlift borehole sam- ples, each representing one metre, were described. In addi- tion, c. 40 samples per borehole were taken for bio- stratigraphic (dinocyst) analysis. The description of the Fasterholt Member, including the sedimentary logs, is based on Koch (1989). In boreholes drilled using the airlift drilling technique, problems are experienced in retrieving fine-grained sand to the surface, and thus the recovery is commonly low or even zero in such intervals. As an aid to lithological identifica- tion, however, a gamma-ray log was obtained from all 50 boreholes. This petrophysical log is typically used to dif- ferentiate between sand and clay in siliciclastic sections, although sands rich in heavy minerals, glaucony and mica can give anomalous readings. In the correlation panels pre- sented in this study (see Plates 1–9), the borehole litholo- gies were described by the first author, with the following exceptions: Fjand (DGU no. 76.635), Fjelstervang (DGU no. 84.2649), Lindved (DGU no. 116.1569), Løgumkloster (DGU no. 159.739), Ribe (DGU no. 140.42), Rømø (DGU no. 148.52), Tinglev (DGU no. 168.1378), Uldum (DGU no. 1444), Ulfborg (DGU no. 73.971),Vester Sottrup (DGU no. 169.799) and Vollerup (DGU no. 160.1378). Lithological descriptions of the latter boreholes are from the ‘Jupiter’ well database at the Geological Survey of Denmark and Greenland (GEUS). All sample depths from boreholes are adjusted using the gamma-ray log in order to get true depths of the samples. Thus there may be a dis- Fig. 7. Revised lithostratigraphic framework of the uppermost Oligocene – Miocene of onshore Denmark, as presented here. R.: Resen. Plio.: Pliocene. Plio. Zanclean Messinian Tortonian M åd e G ro u p R ib e G ro u p Serravallian M io ce n e N eo ge n e 10 15 20 25 Chattian Langhian Burdigalian Aquitanian O lig o ce n e U p p er U p p er M id d le L o w er 5 P al ae o ge n e P er io d SW NE EpochMa Age Dinocyst zonation Lithostratigraphy H. o. G. v. A. a. U. a. L. t. A. u. C. c. E. i. C. au. C. g. D. p. S. h. T. p. C. am. H. spp Marbæk Fm Gram Fm Ørnhøj Fm Hodde Fm Arnum Fm Stauning Mb Odderup Fm Bastrup Fm Fasterholt Mb Vandel Mb Resen Mb Resen Mb R. Mb Klintinghoved Fm Vejle Fjord Fm Brejning Fm Brejning Fm Skansebakke Mb Kolding Fjord Mb Øksenrade Mb Not included in this study Billund Fm Hvidbjerg Mb Addit Mb Sydklint Mb Marine silt and clay Marine sand Fluvial sand and gravel Hiatus Brackish-water silt and clay Coal Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 15 16 crepancy (usually less than 4 m) between depths indicated in the Jupiter database (measured depth: MD) and the depths assigned to the lithostratigraphic units in this study. The measured depth of cuttings samples is, however, indi- cated in the text. Approximately 1000 km of 2D high-resolution seismic data have been used to correlate between boreholes and to investigate the overall architecture of the Miocene succes- sion. The correlations are also guided by dinocyst studies of most of the boreholes included here. These studies have resulted in a detailed dinocyst zonation (Fig. 6; Dybkjær & Piasecki 2008, 2010). The geological age assigned to each lithostratigraphic unit is based primarily on this dinocyst stratigraphy (Fig. 7). The lithostratigraphy of the uppermost Oligocene – Mio - cene succession of onshore Denmark is herein formally revised according to the guidelines presented by Salvador (1994). Nine lithostratigraphic units are revised and/or elevated in rank, 13 new lithostratigraphic units are erected. The Oligocene to lowermost Miocene Brejning Clay Member, previously referred to the Vejle Fjord Formation, is elevated to formation status; it includes the Sydklint Member and the Øksenrade Member. The Miocene suc- cession is subdivided into two groups, the Ribe and Måde Groups. The Ribe Group consists of the Vejle Fjord, Billund, Klintinghoved, Bastrup, Arnum, and Odderup Formations. The Vejle Fjord Formation includes the Skansebakke Member, the Billund Formation includes the Hvidbjerg and Addit Members, the Klintinghoved Formation includes the Kolding Fjord Member, the Bastrup Formation includes the Resen Member, the Arnum Formation includes the Vandel Member and the Odderup Formation includes the Stauning and Fasterholt Members. The Måde Group com- prises the Hodde, Ørnhøj, Gram, and Marbæk Formations (Fig. 7). It should be noted that particularly distinctive portions of individual formations are defined as members, but the formations are not subdivided at member level in their entirety. Lithostratigraphic definition of units in complex inter- digitating lithologies requires clear recognition of the litho- logical (or petrophysical in subsurface data) bounding criteria for formations and members. In this study, the fol- lowing criteria were adopted. The sand-rich formations (e.g. Billund, Bastrup, Odderup Formations) possess over 75% sand and have a minimum thickness of 5 m; inter- calated mudstone packets over 5 m thick are referred to the coeval marine, mud-rich formation (i.e. the Vejle Fjord Formation in the case of the sand-rich Billund Formation). Similarly, the marine, mud-dominated formations may contain subordinate sands; sand-rich intervals (with over 75% sand) that exceed 5 m in thickness are referred to the coeval sand formation. Salvador (1994) and subsequent lithostratigraphic guide- lines (NACSN 2005) discourage the use of stratigraphically alternating formations in interdigitating depositional sys- tems; the practical disadvantages in outcropping terranes are clear. In subsurface lithostratigraphy, however, this prac- tise is adopted on occasion (e.g. Johnson & Lott 1993) and is utilised here to emphasise the genetic integrity of the deltaic sandy systems. Brejning Formation new formation History.The Brejning Formation corresponds to the Brejning Clay Member of the Vejle Fjord Formation of Larsen & Dinesen (1959). Name. After the town of Brejning, south of Vejle Fjord (Fig. 1). Type and reference sections. The exposure at Skansebakke, Brejning (55°40´19.74´´N, 9°41´33.84´´E) forms the type section for the Brejning Formation (Larsen & Dinesen 1959, fig. 12). At low tide, the Brejning Formation is exposed in the basal, south-eastern part of the Skansebakke profile at Brejning. A borehole at Brejning encountered a c. 4 m thick (–0.4 to –4.65 m) section referred to the Brejning Formation (Larsen & Dinesen 1959). The refer- ence section is the outcrop at Dykær, Juelsminde (Fig. 8). Other exposures of the formation are found at Sanatoriet and Fakkegrav in the Vejle Fjord area, and at Jensgård at the mouth of Horsens Fjord. In central Jylland, the for- mation crops out at the Sofienlund clay pit; in the Lim- Revised lithostratigraphy Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 16 fjorden area, the formation is exposed at Lyby and Mogenstrup. Periodically, the formation is exposed at Søvind, Sønder Vissing, and in the Ølst and Hinge clay pits. The reference borehole section is the interval from 100.90 to 96.50 m (101–97 m MD) in the Andkær borehole (DGU no. 125.2017; Fig. 8). Thickness.The Brejning Formation is normally 2–4 m thick, but is over 20 m thick in a number of wells (Plates 2, 5), and a 50 m thick succession referred to the Brejning Formation was encountered in the Borg-1 borehole (Plate 9). Lithology. The Brejning Formation consists of greenish to brown, glaucony-rich clay with scattered pebbles (Fig. 9). In the upper part, there is an increased content of organic matter, silt and sand. Siderite concretions are also com- mon in the upper part of the formation. The clay mine - ralogy is dominated by illite, but smectite, kaolinite and gibbsite are also present (Friis 1994; E.S. Rasmussen 1995). Mica is common in the upper part of the formation. Log characteristics. High gamma-ray readings characterise the Brejning Formation (Fig. 8); the lower part, in partic- ular, may show extremely high gamma-ray values due to 17 Fig. 8. Reference sections for the Brejning Formation. The primary reference section is the Dykær outcrop located south-west of Juelsminde and the secondary reference section is the interval from 100.9 to 96.5 m in the Andkær borehole. The accompanying legend is applicable to all outcrop and borehole logs shown in this study. Vejle Fj.: Vejle Fjord. 0 1 2 m Cl Si F MC P Sand 100 101 95 m.b.s. GR 96 97 98 99 O lig o ce n e L o w er M io ce n e O lig o ce n e B re jn in g Fm M io ce n e V ej le F j. Fm B re jn in g Fm E o ce n e Sø vi n d F m V ej le F jo rd F m Dykær outcrop Andkær borehole DGU no. 125.2017 Lithology Clay/silt Heterolith Fine Medium Coarse Gravel Coal Sedimentary structures Erosional surface Parallel bedding Planar cross-bedding Trough cross-bedding Hummocky cross-bedding Swaley cross-bedding Inclined heterolithic bedding Cross-lamination Wavy bedding Flaser bedding Backflow ripples Climbing ripples Double clay layers Concretion Collapse structures Biogenic structures Bioturbation Ophiomorpha Rootlets Fossils Bivalve Plant Wood Sponge spicules Diatoms Metres below surface Gamma ray Sand Clast Clast m.b.s. GR 40 cps 120 Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 17 18 the high content of glaucony (e.g. Rødding borehole, Plate 8), although expanded sections (e.g. Borg borehole, Plate 9) may show uniform intermediate values. Fossils. The marine clay of the Brejning Formation contains a rich mollusc fauna (Ravn 1907; Eriksen 1937; Schnetler & Beyer 1987, 1990). Marine microfossils, such as foraminifers (Larsen & Dinesen 1959; Ulleberg 1987, 1994; Laursen & Kristoffersen 1999), calcareous nanno- fossils (von Salis Perch-Nielsen 1994) and dinocysts (Dybkjær 2004a, b; Rasmussen & Dybkjær 2005), are rep- resented, and foraminifers and dinocysts are abundant and diverse. In the upper part of the formation, a gradual change/detoriation in the mollusc fauna was interpreted to reflect a shallowing-upward trend. Similarly, in the Dykær and Jensgård exposures, the abundance and diversity of foraminifers (Larsen & Dinesen 1959) and dinocysts decrease in the upper part of the formation whereas the abun- dance and diversity of spores, pollen and freshwater algae increase (Dybkjær 2004a, b; Rasmussen & Dybkjær 2005). Echinoids, crinoids, asteroids, anthozoans, otoliths, sharks’ teeth, brachiopods, crustaceans and bryozoans have also been found. Depositional environment. The Brejning Formation was deposited in a fully marine, sediment-starved environment (Larsen & Dinesen 1959; Schnetler & Beyer 1990; E.S. Rasmussen 1995; Rasmussen & Dybkjær 2005). The water depth was probably more than 200 m in the Norwe- gian–Danish Basin based on otoliths (Schnetler & Beyer 1990) and benthic foraminifera (C. Morigi, personal com- munication 2009). The heights of clinoforms (offshore Denmark) associated with early Oligocene delta progradation indicate a minimum water depth of 200 m (Danielsen et al. 1997), and since the Late Oligocene was warmer than the Early Oligocene (Zachos et al. 2001), relatively deep water probably prevailed within the Norwegian–Danish Basin during deposition of the Brejning Formation. Schnetler & Beyer (1990) reported a mixed mollusc fauna, some ele- ments indicating deep marine conditions and some indica- tive of shallow water; the shallow marine fauna is most likely reworked, i.e. transported down the delta or shelf slope to the basin floor. On the Ringkøbing–Fyn High, shal- lower water prevailed. The upward increase in silt and sand indicates progradation of the shoreline in the latest Oligocene associated with a relative sea-level fall (Rasmussen & Dybkjær 2005). Boundaries. In southern and western Jylland, the Brejning Formation rests with a sharp and erosional boundary on the Eocene Søvind Marl Formation (Fig. 9; Heilmann- Clausen et al. 1985). In this area, the boundary is marked by a distinct change in colour and grain size from the green- ish grey clay of the Søvind Marl Formation to the green- ish brown and commonly silty Brejning Formation. The boundary may locally be intensively bioturbated and con- sequently more gradational. In central and northern Jylland, the boundary is defined where dark brown clay of the Branden Formation (lower Upper Oligocene) is overlain by greenish glaucony-rich clay of the Brejning Formation. The base of the Brejning Formation is marked by a promi- nent shift to higher values on the gamma-ray log in the Andkær borehole, but may locally be more gradational due to glaucony-filled burrows in the upper part of the Søvind Marl Formation. The upper boundary is typically sharp and characterised by a change from greenish, dark brown, glaucony-rich clayey silt of the Brejning Formation to dark brown clayey silt of the overlying Vejle Fjord Formation. A change in the degree of consolidation is also observed at the boundary in most parts of Jylland from the well-consolidated sedi- ments of the Brejning Formation to the relatively loose sediments of the Vejle Fjord Formation. A gravel layer com- monly occurs immediately above the upper boundary. At the type locality, the upper boundary is recognised by a dis- Fig. 9. The Brejning Formation at Øksenrade showing the lower part of the formation and the lower boundary with the underlying, light greenish-grey Middle Eocene Søvind Marl Formation (photo- graph courtesy of Peter Warna-Moors). Red penknife for scale, c. 10 cm long. Brejning FmBrejning Fm Søvind Marl FmSøvind Marl Fm Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 18 tinct decrease in the content of glaucony passing from the Brejning Formation to the Vejle Fjord Formation (Larsen & Dinesen 1959). The scattered glaucony grains found in the Vejle Fjord Formation are reworked (E.S. Rasmussen 1987). In central east Jylland, the boundary is commonly characterised by a marked change from the sand deposits of the Øksenrade Member to the dark brown, clayey silt of the Vejle Fjord Formation. 19 N Brejning Fm (Oligocene) Brejning Fm (Miocene) Øksenrade Mb Sydklint Mb Vejle Fjord Fm Skansebakke Mb Billund Fm Addit Mb Hvidbjerg Mb Klintinghoved Fm Kolding Fjord Mb Bastrup Fm Resen Mb Arnum Fm Vandel Mb Odderup Fm Stauning Mb Fasteholt Mb Hodde Fm, Ørnhøj Fm, Gram Fm Marbæk Fm A B D G E C F H 50 km Fig. 10. The distribution of uppermost Oligocene – Miocene formations and members in Denmark. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 19 20 Distribution. The Brejning Formation is present in much of central and southern Jylland but is typically absent on the Ringkøbing–Fyn High (Fig. 10A). Due to the diachro- nous nature of the upper boundary (see below), the youngest beds referred to the Brejning Formation are only present in southern and western Jylland. The northern and eastern limit closely follows that of the Miocene deposits (Fig. 3). Biostratigraphy. The Deflandrea phosphoritica Dinocyst Zone of Dybkjær & Piasecki (2010) is recorded in the Brejning Formation. In addition, the Chiropteridium galea Zone is recorded in the upper part of the formation in the south- ern parts of Jylland. Geological age. The Brejning Formation is of late Chattian to early Aquitanian (latest Late Oligocene to earliest Early Miocene) age. The dinocyst stratigraphy indicates that the upper boundary of the Brejning Formation is diachro- neous. In central parts of Jylland, the boundary broadly cor- relates with the Oligocene –Miocene boundary (E.S. Rasmussen 2004b; Rasmussen & Dybkjær 2005; Dybkjær & Rasmussen 2007). In the southern part of Jylland, depo- sition of the glaucony-rich clay of the Brejning Formation apparently continued into the early Aquitanian. Subdivision. The Brejning Formation includes the Sydklint Member and the new Øksenrade Member. Sydklint Member History. A thin diatomite layer of Oligocene age, uncon- formably overlying the Lower Eocene Fur Formation and overlain by Upper Oligocene micaceous clay, was observed in the cliff section at Silstrup, near Thisted, by Heilmann- Clausen (1982). Although noted by Bøggild (1918), he apparently considered the layer to represent a glaciotec- tonically derived slice of the Fur Formation (see Heilmann- Clausen 1997). The silicoflagellate assemblage in the diatomite layer was described by von Salis (1993). The lithology of the Oligocene diatomite layer and the contact to the underlying Fur Formation were described in more detail by Heilmann-Clausen (1997) who also proposed a model for the genesis of the diatomite. Heilmann-Clausen (1997) formally defined the unit as the Sydklint Member, which he provisionally referred to the Vejle Fjord Formation. Cl Si F MC P Sand Sydklint outcrop 0 1 m U p p er O lig o ce n e E o ce n e B re jn in g Fm Fu r Fm S. M b Fig. 11. Type section of the Sydklint Member. Modified after Heil- mann-Clausen (1997); for legend, see Fig. 8, p. 17. S.: Sydklint. Fig. 12. Contact between the light grey Lower Eocene Fur For - mation and the brown Upper Oligocene Sydklint Member at Silstrup Sydklint. A thin glauconitic layer occurs at the boundary between the two units. Thalassinoides burrows extend from the glauconitic layer down into the topmost Fur Formation. Knife for scale. GlauconyGlaucony Fig. 13. Photomicrograph of a vertical thin-section through the diatomaceous Sydklint Member. 100 μm Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 20 21 Name. After the coastal cliff of Silstrup Sydklint, south of Thisted (Fig. 1). Type section. The type section is the coastal cliff of Silstrup Sydklint (56°55´15.49´´N, 8°39´20.76´´E; Fig. 11). Thickness. The member is up to 28 cm thick. Lithology. The Sydklint Member includes a basal 1–8 cm thick clay layer rich in coarse-grained glaucony and reworked clasts of the Fur Formation (Figs 11, 12). Sporadic extra- basinal pebbles and a single 25 cm large, partly glauconi- tised gneiss clast have been found in the basal layer. The glaucony-rich basal layer is succeeded by 20 cm of brown, clayey diatomite (Fig. 13). Log characteristics. The member is only recognised at out- crop, and log data are not available. Fossils. The Sydklint Member contains well-preserved sili- ceous and organic-walled microfossils, including diatoms, silicoflagellates, sponge spicules, dinocysts, pollen and spores (Fig. 13). Depositional environment. The Sydklint Member was deposited in a marine, probably shelf environment. Boundaries. The Sydklint Member has a sharp lower bound- ary separating the glaucony-rich basal layer from the under- lying Fur Formation. An omission suite of shallow Thalassinoides burrows extends 5–8 cm down into the top- most Fur Formation. The upper boundary is gradational over a few centimetres. Distribution.The Sydklint Member is only known from out- crops at Silstrup Sydklint and nearby Klovbakker at Sundby, Mors. Biostratigraphy. The member is referred to the silicoflagel- late Distephanus speculum haliomma Subzone of Bukry (1981) by von Salis (1993) and to the Deflandrea phos- phoritica Dinocyst Zone of Dybkjær & Piasecki (2010) by Heilmann-Clausen (C. Heilmann-Clausen, personal com- munication 2010). Geological age. The Sydklint Member is of late Chattian (lat- est Late Oligocene) age. Øksenrade Member new member History. The succession defined here as the Øksenrade Member was termed ‘Middelfart malm’ by L.B. Rasmussen (1975). Equivalent oolitic ironstones cropping out at Jensgård at the mouth of Horsens Fjord were described by Friis et al. (1998). Name. After Øksenrade Skov, just north of the coastal type locality (Fig. 1). Type and reference sections. The type section is the coastal cliff facing Fænø Sund, south of Øksenrade Skov, Middel- fart (55°29´39.61´´N, 9°42´47.29´´E; Fig. 14). The ref- erence section is the interval from 212 to 210 m (214–212 m MD) in the borehole at Gadbjerg (Fig. 14; DGU no. 115.1474). Fig. 14. Type and reference sections of the Øksenrade Member (Ø.). The type section is the Øksenrade outcrop located south-west of Middelfart; the top of the member is not seen. The reference section is the interval from 212 to 210 m in the Gadbjerg borehole; for legend, see Fig. 8, p. 17. Øksenrade outcrop 0 1 2 3 4 m Cl Si F MC P Sand 230 220 210 200 m.b.s. GR Gadbjerg borehole DGU no. 115.1474 L o w er M io ce n e U p p er O lig o ce n e U p p er O lig o ce n e B re jn in g Fm Ø ks en ra d e M b E o ce n e V ej le F jo rd F m Ø . B re jn in g Fm Sø vi n d M ar l Fm 40 cps 100 Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 21 22 Thickness. The member is c. 1 m thick at the type locality (Fig. 14), but the top is not seen; boreholes indicate a max- imum thickness of 5 m (Fig. 14; Plate 8). Lithology. The Øksenrade Member is composed of reddish ooids and grey, well-sorted, fine-grained quartz sand (Figs 15, 16) and ranges lithologically from a sand with dis- persed ooids to a sandy ooid grainstone. At Jensgård, the Øksenrade Member consists of planar cross-bedded sand, sets are up to 40 cm thick and typically show asymptotic toesets. The foresets are inclined towards the north. The ooids are composed of concentric layers of goethite, com- monly with a core of glaucony grains or pellets (H. Friis, personal communication 2010); at the type section, shells or quartz grains also form ooid cores. The cement consists of siderite with some calcite; the iron content of the sedi- ment is up to 30% (E.S. Rasmussen 1987). Moulds of mollusc shells are common. Log characteristics. The Øksenrade Member is typified by relatively low gamma-ray readings (Fig. 14) but distinct spikes may occur due to horizons rich in glaucony. Fossils. The Øksenrade Member is characterised by abun- dant moulds of mollusc shells (L.B. Rasmussen 1975; Gravesen 1990). Depositional environment. The Øksenrade Member was deposited above storm wave base as indicated by cross-bed- ding (Rasmussen & Dybkjær 2005). The bivalve and gas- tropod faunas (L.B. Rasmussen 1975) also indicate a shallow-water depositional environment. The transgressive lag that is locally found on the Ringkøbing–Fyn High at the base of the Vejle Fjord Formation is indicative of expo- sure and terrestrial sedimentation prior to transgressive reworking (Rasmussen & Dybkjær 2005). Such a shal- lowing and local emergence at the transition from the Oligocene to the Miocene is also indicated by the presence of freshwater algae in the upper part of the Brejning Formation (Rasmussen & Dybkjær 2005). Boundaries. The Øksenrade Member rests with a sharp ero- sional boundary on the undifferentiated Brejning Forma- tion beneath (Figs 15, 16). The lower boundary is also marked by a change from dark brown, clayey silt with scat- Fig. 15. Brejning Formation and the Øksenrade Member in the coastal cliff at Øksenrade Skov, south-west of Middelfart. This outcrop consti- tutes the type section of the Øksenrade Member; spade for scale (c. 1.3 m long). Øksenrade Mb Brejning Fm Øksenrade Mb Brejning Fm Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 22 23 tered sand lenses to fine-grained, reddish sand; on the gamma-ray log, this facies shift is reflected by a shift towards lower values. The upper boundary is characterised by a marked change from the sand deposits of the Øksenrade Member to dark brown, clayey silts of the Vejle Fjord Formation; this boundary is marked by a prominent shift on the gamma-ray log from low to high values. Distribution. The Øksenrade Member is present in east Jylland and the extreme western part of Fyn, from Horsens in the north to Middelfart in the south (Fig. 10A). The west- ernmost limit is defined by exposures at Gadbjerg near Give where the member occurs on a footwall crest at the boundary fault of the Brande Trough. Biostratigraphy. No samples from this member have been analysed for palynology; the mollusc fauna is non-specific. Geological age. Based on stratigraphic context, the Øksenrade Member is considered of latest Chattian (latest Late Oligocene) age. Fig. 16. Boundary between the Brejning Formation and the Øksen - rade Member, marked by a distinct colour change from dark brown clayey silt to red sand. Lens cap for scale. Øksenrade Mb Brejning Fm Øksenrade Mb Brejning Fm Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 23 24 History. Non-fossiliferous sand and gravel encountered below 125.6 m in a borehole at Ribe were defined as the Ribe Formation by Sorgenfrei (1958). The borehole ter- minated at a depth of 127 m and thus the base of the for- mation was never defined. L.B. Rasmussen (1961) suggested that a succession of quartz gravel and sand with some lig- nite between 255.7 and 144.5 m in the Arnum-1 borehole should be referred to the Ribe Formation. He further indi- cated that the fluvio-deltaic, brown-coal-bearing succes- sion around Silkeborg and Skanderborg may be correlative with the Ribe Formation. In this stratigraphic revision, however, the fluvio-deltaic deposits at Silkeborg are referred to the Vejle Fjord and Billund Formations. The Ribe Formation was included in the stratigraphic chart of L.B. Rasmussen (1961) where it was suggested to encompass the fluvio-deltaic deposits below the Odderup Formation. The age of the formation was indicated as Early to early Middle Miocene (Fig. 4). During the last decade, detailed biostratigraphic and sequence stratigraphic studies of the Lower Miocene suc- cession have been carried out (E.S. Rasmussen 2004b; Dybkjær 2004a; Rasmussen & Dybkjær 2005; E.S. Rasmussen et al. 2006; Dybkjær & Piasecki 2010). These studies have revealed that the stratigraphy of the Lower Miocene deposits is more complicated than formerly believed. The fluvio-deltaic sediments that are so charac- teristic of the Lower Miocene – lower Middle Miocene succession are thus here defined as the Ribe Group. The introduction of the Bastrup Formation, which replaces the Ribe Formation in southern Jylland, is also consistent with the new lithostratigraphy of Schleswig-Holstein, northern Germany (Rasser et al. 2008; Knox et al. 2010). Here the Bastrup Formation was adopted to represent Lower Miocene fluvio-deltaic sands of Burdigalian age, based on a study of the Kasseburg cored borehole near Hamburg (K. Gürs, personal communication 2006; Rasser et al. 2008; Knox et al. 2010). The Ribe Group correlates with the upper part of the Hordaland Group as applied in the North Sea region, Ribe Group new group Store Vorslunde borehole DGU no. 104.2325 220 210 200 190 180 170 160 150 140 130 120 110 100 90 80 70 60 50 40 30 20 10 0 m.b.s. GR R ib e G ro u p V ej le F jo rd F m B ill u n d F m K lin ti n gh o ve d F m B as tr u p F m A rn u m F m O d d er u p F m B r. Fm L o w er M io ce n e O lig o . 0 cps 80 Fig. 17. The full development of the Ribe Group is illustrated by the interval from 219 to 1 m in the Store Vorslunde borehole, north-east of Vejle; for legend, see Fig. 8, p. 17. Br.: Brande. Oligo.: Oligocene. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 24 25 including offshore Denmark in the Norwegian–Danish Basin (Deegan & Scull 1977; Hardt et al. 1989; Schiøler et al. 2007). Name. After the town of Ribe (Fig. 1). Type area. The type area of the Ribe Group is central and east Jylland. In the gravel pit at Voervadsbro in central Jylland (Fig. 1), both marine sand and fluvial sand and gravel of the Ribe Group are exposed. In the Store Vorslunde borehole (Fig. 17; DGU no. 104.2325) a complete section through the group is represented in the interval from 219 to 1 m (220–1 m MD). The group crops out at Klintinghoved in southern Jylland, at Rønshoved, Hagenør, Børup, Hindsgavl, Galsklint, Hvidbjerg, Brejning, Sanatoriet, Fakkegrav, Dykær and Jensgård in eastern Jylland, at Addit, Salten, Isenvad and Abildå in central Jylland and at Gyldendal, Søndbjerg, Lyby, Skyum Bjerge, Skanderup and Lodbjerg in the Limfjorden area. Thickness. The group is 218 m thick in the Store Vorslunde borehole. A thickness of c. 200 m is common in the Norwegian–Danish Basin and in most places on the Ringkøbing–Fyn High. In the Tinglev borehole, located in the Tønder Graben, more than 200 m has been penetrated without reaching the lower boundary of the group (Plate 1). Reduced thicknesses are seen in the eastern part of Jylland, partly due to erosion during the Pleistocene. Lithology. The group consists of three cycles of alternating mud-rich and sand-rich units with some intercalation of coal beds, especially in the upper cycle (Odderup Forma- tion); each cycle, 50 to 100 m thick, represents a coarsen- ing-upward cycle. The sands are typically medium- to coarse-grained, quartz-rich with a variable mica content. Various types of cross-bedding, including tabular, trough, hummocky and swaley cross-stratification, characterise the sand-rich units. The sand grains are normally sub- to well- rounded. Well-rounded pebbles of quartz, quartzite and Fig. 18. Quartz-rich sand and pebbles from the Miocene fluvio-deltaic deposits; photographs courtesy of P. Warna-Moors. A: Pebbles of quartz, quartzite and chert; these are commonly found near sequence boundaries, associated with transgressive lags or within fluvial channels. Note that the clasts are up to 3 cm in diameter. B: Granules and coarse-grained sand of the Billund Formation. C: Fine- and medium-grained sand of the Billund Formation. A B C Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 25 26 chert up to 4 cm in size (Fig. 18) commonly occur in the upper part of the units near sequence boundaries (in trans- gressive lags or fluvial channels). Fossils occur only spo- radically in the sand-rich units. The micaceous, mud-rich portions of the group are typ- ically homogeneous, with some intercalation of laminated mud intervals as well as discrete sand layers. The sand lay- ers are commonly hummocky cross-stratified or represent tidal rhythmites. The clay mineral association is dominated by illite, kaolinite and gibbsite (Fig. 19); pyrite is a very com- mon authigenic mineral. The coal beds are found associated with cross-stratified fluvial sands and muds, and also cap shoreface/beach sands and lagoonal muds. The coal beds are limited to the Norwegian–Danish Basin where they typically reach thick- nesses of 2–3 m; the thickest succession has been recorded in the Fasterholt area, where there is a cumulative thick- ness of about 9 m of coal. Lithological details of the respec- tive formations of the Ribe Group are given below under the individual formation descriptions. Log characteristics. The typical log pattern shows three cycles of decreasing-upward gamma-ray values (Fig. 17). The gamma-ray log is generally characterised by a serrated pat- tern, but distinct gamma-ray spikes are common in the lower part of each cycle; in the upper cycle (the Arnum and Odderup Formations), high gamma-ray spikes occur throughout the succession. In the northern part and also locally in the southern part, decreasing gamma-ray values are commonly observed in the upper part of each cycle. For more detailed descriptions, see the individual units below. Fossils. Molluscs occur abundantly in the marine and near- shore deposits and plant fossils are locally abundant in the terrestrial deposits. More detailed descriptions of the fauna/flora are given below in the definitions of the for- mations and members. Depositional environment. The Ribe Group was deposited by delta systems prograding from the north and north-east towards the south and south-west. Deposition of the first cycle (Billund Formation) was strongly controlled by the topography formed during Early Miocene inversion tec- tonism (Rasmussen & Dybkjær 2005; Hansen & Rasmus- sen 2008; E.S. Rasmussen 2009a). During the deposition of this cycle, the so-called Ringkøbing and Brande lobes were focussed particularly within structural lows, the Brande Trough and the Rødding Graben (Hansen & Rasmussen 2008). East of the main delta lobes, spit and barrier-com- plexes developed due to shore-parallel transport of sand that was delivered from the river mouths of the delta sys- tems (Rasmussen & Dybkjær 2005; Hansen & Rasmusen 2008). Fluvial sands interpreted as braided river system deposits (Hansen 1985; Jesse 1995; E.S. Rasmussen et al. 2006) dominate in the northern part. The second cycle (Bastrup Formation) shows a more evenly distributed progradational pattern across Jylland. Due to the lack of outcrops of this part of the Miocene suc- cession, detailed sedimentology has not been carried out. Judging from borehole data, there are no indications of widespread spit and barrier complexes. As for the first cycle, fluvial systems dominate the upper part of the succession. Log and seismic data (E.S. Rasmussen et al. 2007; E.S. Rasmussen 2009b) indicate that a meandering fluvial sys- Fig. 19. X-ray diffractogram of the clay fraction from muds of the Vejle Fjord Formation (Ribe Group). Note that gibbsite is present indicating that the source area was heavily weathered. Full line = untreated samples, dotted line = glycolated samples and dashed line = samples heated to 500°C. Modified from E.S. Rasmussen (1995). dA: lattice separation (in angstrom). 5 20°1020 15 5 73 10 18 dA (0 0 2 ) G ib b si te (0 0 1 ) G ib b si te (0 0 1 ) K ao lin it e (0 0 2 ) Ill it e (0 0 1 ) Ill it e (0 0 1 ) Sm ec ti te Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 26 27 tem was widespread, although local or periodic develop- ment of braided fluvial systems may have taken place. The third and final cycle (the Odderup Formation) was deposited in a prograding coastal plain with widespread coal formation within the Norwegian–Danish Basin, whereas clean fluvial sand dominates the Ringkøbing–Fyn High area. Boundaries. The lower boundary is commonly sharp, being defined where greenish to brownish, glaucony-rich clay and silt is overlain by dark brown, organic-rich mud. Over much of Jylland, the boundary is also marked by a change in the degree of consolidation, from the well-consolidated sediments of the Oligocene Brejning and Branden Formations to poorly consolidated Ribe Group sediments. The boundary may be marked by a gravel lag or sand bed. Due to intense bioturbation, the boundary may be locally blurred. In central east Jylland, the boundary is charac- terised by a marked change from the sand deposits of the Øksenrade Member to dark brown clayey silt of the Vejle Fjord Formation of the Ribe Group. The upper boundary is sharp, being marked by a thin gravel layer that separates the white, fine-grained sand of the uppermost Ribe Group (Odderup Formation) from the dark brown mud of the suc- ceeding Måde Group. This is reflected by a prominent shift on the gamma-ray log towards high gamma-ray values. Distribution.The Ribe Group is present over most of Jylland. The northern and eastern limits of the group closely fol- low the lower boundary of the Miocene deposits (Fig. 4) Geological age. The Ribe Group is of Aquitanian – early Langhian (Early Miocene – earliest Middle Miocene) age. Subdivision. The Ribe Group is divided into six forma- tions: the Aquitanian Vejle Fjord and Billund Formations, the uppermost Aquitanian – lower Burdigalian Klin - tinghoved and Bastrup Formations and the upper Burdigalian – lower Langhian Arnum and Odderup For - mations (Fig. 7). Vejle Fjord Formation redefined formation General. The marine, clay-dominated Vejle Fjord Formation interdigitates north-eastwards with the fluvio-deltaic, sand- rich Billund Formation. These two formations thus alter- nate up-section in some boreholes (e.g. Plates 2–8). Fig. 20. Type section of the Vejle Fjord Formation and the Skansebakke Member at Skansebakke, Brejning; for legend, see Fig. 8, p. 17. 0 1 2 3 4 5 6 7 8 m Cl Si F MC P Sand Skansebakke outcrop V ej le F jo rd F m Sk an se b ak ke M b L o w er M io ce n e Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 27 28 Dykær outcrop 0 1 2 3 4 5 6 7 8 9 10 m 10 11 12 13 14 15 16 Cl Si F MC P Sand Cl Si F MC P Sand B ill u n d F m L o w er M io ce n e H vi d b je rg M b B ill u n d F m V ej le F jo rd F m B re jn in g Fm L o w er M io ce n e O lig o ce n e Sk an se b ak ke M b H vi d b je rg M b Fig. 21. Primary reference section of the Vejle Fjord Formation at Dykær, south-west of Juelsminde; for legend, see Fig. 8, p. 17. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 28 29 History. The Vejle Fjord Formation was defined by Larsen & Dinesen (1959). The formation was originally defined as the succession from the base of the Brejning Clay Member to the top of the Vejle Fjord Sand Member. For strati- graphic and practical reasons, the Brejning Clay Member is herein removed from the Vejle Fjord Formation and ele- vated to the status of formation (see above); redefinition of the Vejle Fjord Formation is therefore necessary. Revision is also needed because of the large amount of data acquired during the last decade, which has shed new light on the depo- sitional system (Dybkjær & Rasmussen 2000; Rasmussen & Dybkjær 2005). Sediments referred by Christensen & Ulleberg (1973) to the upper Sofienlund Formation are assigned here to the Vejle Fjord Formation; the Sofienlund Formation is abandoned. Name. After Vejle Fjord in east Jylland (Fig. 1). Type and reference sections. The type section is the Skanse- bakke outcrop at Brejning 55°40´19.74´´N, 9°41´33.84´´E; Figs 1, 20). The outcrop reference section is defined at Dykær near Juelsminde (Figs 1, 21). Other exposures in the Vejle Fjord area are Brejning Hoved, Sanatoriet, Fakkegrav and Jensgård. It is further exposed at Hindsgavl near Middelfart, and the formation crops out at Skyum Bjerge, Lyby, Mogenstrup and Skanderup (Mors) in the Limfjorden area (Fig. 1). The secondary reference section is the Store Vorslunde borehole (DGU no. 104.2325) (Fig. 22), in the interval from 219 to 160 m (220–161 m MD). Thickness. The formation is c. 20 m thick at the type local- ity though neither the base nor the top are seen; the for- mation is about 18 m thick in the nearby Andkær borehole (see Plate 1). In the western part of Jylland, it may reach a thickness of up to c. 100 m, as exemplified by the Holstebro borehole (Plate 4). Lithology. The Vejle Fjord Formation consists mainly of dark brown clayey silt (Fig. 23). In some areas, it is dom- inated by laminated, greenish-grey sand and dark brown, clayey silt. Sand stringers up to a few centimetres thick may occur. Locally, the formation is composed of wave- influenced heterolithic mud and sand showing hum mocky cross-stratification (Figs 24, 25); the heterolithic succes- sion is commonly characterised by double clay layers and climbing ripples. Soft-sediment deformation structures occur locally. Trace fossils occur in places in the Vejle Fjord Formation. Log characteristics. The formation is characterised by inter- mediate gamma-ray values (Fig. 22). The log pattern is ser- rated and shows both decreasing- and increasing-upward trends throughout the succession. Fossils. The Vejle Fjord Formation contains an impoverished mollusc fauna (Ravn 1907; Eriksen 1937; Schnetler & Fig. 22. Secondary reference section of the Vejle Fjord Formation: the interval from 219 to 160 m in the Store Vorslunde borehole, north-east of Vejle; for legend, see Fig. 8, p. 17. Store Vorslunde borehole DGU no. 104.2325 220 210 200 190 180 170 160 150 140 m.b.s. GR V ej le F jo rd F m B ill u n d F m B ra n d e Fm L o w er M io ce n e O lig o ce n e 0 cps 80 Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 29 30 Beyer 1987, 1990). The foraminifer fauna (Larsen & Dinesen 1959; Laursen & Kristoffersen 1999) and the dinocyst flora (Dybkjær 2004 a, b; Rasmussen & Dybkjær 2005) are similarly impoverished within this formation, although the abundance of dinocysts is locally very high, albeit restricted to a few species. Depositional environment. The Vejle Fjord Formation was deposited in a brackish to fully marine depositional envi- ronment. Brackish-water conditions predominated within the Norwegian–Danish Basin in the early phase of depo- sition as a consequence of the elevated Ringkøbing–Fyn High (Rasmussen & Dybkjær 2005; E.S. Rasmussen 2009a). As sea level rose during the Early Miocene, fully marine con- ditions were re-established and the water depth was c. 100 m in the Norwegian–Danish Basin and probably less than 30 m on the Ringkøbing–Fyn High. Most of the Vejle Fjord Formation was deposited in a prodelta environment. The thickest developments of the formation are associated with inter-lobe depositional environments. Boundaries. The lower boundary is typically sharp, being characterised by a change from greenish dark brown, glau- cony-rich, clayey silt to dark brown, clayey silt. A change in the degree of consolidation is observed at the boundary over much of Jylland, relatively loose sediments of the Vejle Fjord Formation overlying well-consolidated sediments of the Brejning Formation. A gravel layer is commonly found at the lower boundary. At the type locality, the lower bound- ary is marked by a distinct decrease in the content of glau- cony (Larsen & Dinesen 1959); the scattered glaucony grains found in the Vejle Fjord Formation are reworked (E.S. Rasmussen 1987). In central east Jylland, the boundary is commonly characterised by a marked change from the sand deposits of the Øksenrade Member (upper Brejning Formation) to dark brown, clayey silt of the Vejle Fjord Formation. Recognition of the lower boundary of the for- mation in subsurface data is based on both lithological and petrophysical data. The gamma-ray response at the bound- ary is variable. Where the upper Brejning Formation is mud-rich, as in the reference section for the formation (Fig. 8), gamma-ray values fall at the boundary to intermediate levels. In contrast, where the upper Brejning Formation is sand-rich (e.g. Fig. 14), or where the Vejle Fjord Formation overlies deltaic sands referred to the Billund Formation (e.g. Stakroge and Assing Mølleby boreholes, Plate 3), the Fig. 23. Type section of the Vejle Fjord Formation at Skansebakke, Brejning; spade for scale (c. 1.3 m long). Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 30 31 lower boundary is defined by an abrupt increase in gamma- ray values. Although in a number of wells the boundary can be difficult to position based on log data alone, litho- logical evidence (e.g. the presence of a gravel layer, glau- cony content, clay colour and consolidation) can aid identification (e.g. Resen and Mausvig boreholes, Plate 5). The upper boundary is typically defined where clayey, organic-rich silty sediments of the Vejle Fjord Formation are succeeded by sand-rich deposits (> 75% sand) with a minimum thickness of 5 m; the overlying sands are referred either to the Billund Formation or to the Kolding Fjord Member of the Klintinghoved Formation (e.g. Plate 6). On the gamma-ray log, this boundary may show a marked decrease in gamma-ray readings where overlain by a dis- crete sand unit, or a gradual but steady decrease in gamma- ray readings reflecting a transitional, interbedded, sand- rich unit at the base of the overlying formation. Where the Billund Formation is absent in south and west Jylland, the Vejle Fjord Formation is succeeded by the clay-rich Klintinghoved Formation, and the boundary can be diffi- cult to locate in detail. In the Rødding and Føvling bore- holes (Plate 8), for example, the two formations are lithologically very similar although the clayey silts of the Vejle Fjord Formation may be slightly more consolidated. The boundary can typically be picked on the gamma-ray log, however, at a minor or moderate upward increase in values, commonly capping a weak coarsening-upward suc- cession (decreasing-upward gamma-ray values). Fig. 24. Hummocky cross-stratified sand in the upper part of the Vejle Fjord Formation at Jensgård, east of Horsens (Fig. 1); the dipping, weakly deformed attitude of these strata is due to glaciotec- tonics. Fig 25. Hummocky cross-stratified sand with burrows (Scolicia isp.) from the Vejle Fjord Formation at Skyum (Fig. 1). Note that the sand layer is only burrowed in the upper part. Most of the Vejle Fjord Formation was deposited as alternating sand and clayey, silt layers, but due to bioturbation any stratification was later destroyed and only the thicker storm sand layers were preserved. Knife blade for scale. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 31 Distribution. The formation is present over much of Jylland with the exception of the southern and westernmost parts (Fig. 10B). The northern and eastern limit closely follows the overall outcrop pattern of the Miocene deposits (Fig. 4). Biostratigraphy. The Chiropteridium galea and the Homo- tryblium spp. Dinocyst Zones of Dybkjær & Piasecki (2010) are recorded in the Vejle Fjord Formation. Geological age. The Vejle Fjord Formation is of Aquitanian (earliest Early Miocene) age. Subdivision. The Vejle Fjord Formation includes the Skansebakke Member. Skansebakke Member revised member History. Sediments referred here to the Skansebakke Member were formerly assigned to the Vejle Fjord Sand Member by Larsen & Dinesen (1959); the member is renamed here in accordance with modern lithostratigraphic guidelines. Name. After the outcrop of the type section at Skansebakke, Brejning, on the south coast of Vejle Fjord. Type and reference sections. The type section is the outcrop at Skansebakke (55°40´19.74´´N, 9°41´33.84´´E; Fig. 1). It is also exposed at Brejning Hoved, Sanatoriet, Fakkegrav and Dykær. The reference section is the interval from 91.10 to 79 m (92–79 m MD) in the Andkær borehole (DGU no. 125.2017; Fig. 26). Thickness. At the type locality, the member is c. 7 m thick (top not seen); the member is c. 12 m thick at Brejning Hoved and 7 m thick at Sanatoriet. Lithology. The Skansebakke Member consists of alternat- ing layers of fine-grained, well-sorted, yellowish sand and brownish clay (Fig. 27). The sand beds are sharp-based and homogenous to evenly laminated. The sand beds are com- monly capped by wave- and current-ripples. The trace fos- sils Arenicolites isp. and Macaronichnus isp. are common, and Ophiomorpha isp. is sporadically distributed (Friis et al. 1998). The pyrite content is relatively high compared to the overlying Billund Formation, resulting in the yellowish colour in exposed sections (M. Olivarius, personal com- munication 2010). Log characteristics. The member is characterised by low gamma-ray readings with a serrated pattern (Fig. 26), reflect- ing the alternation of sand and mud beds. Fossils. The Skansebakke Member contains an impover- ished mollusc fauna (Ravn 1907; Eriksen 1937). The foraminifer fauna (Larsen & Dinesen 1959) and the dinocyst flora (Dybkjær 2004 a, b; Rasmussen & Dybkjær 2005) are also impoverished within this member. Depositional environment. The Skansebakke Member is interpreted as having been deposited in a lagoonal deposi- tional environment (Larsen & Dinesen 1959; Friis et al. 1998; Rasmussen & Dybkjær 2005). The sand beds were deposited as washover fans on a backbarrier flat during the main degradation of minor spit and barrier systems formed along elevated parts of the Ringkøbing–Fyn High. Boundaries. The lower boundary is placed at the base of the first significant sand layer separating dark brown, clayey silt from a succession dominated by interbedded yellowish fine-grained sand and dark brown to brown, silty clay. On the gamma-ray log, the lower boundary is placed at a minor, but distinct decrease in gamma-ray readings. The upper boundary is defined by the distinct change from yellow- ish, fine-grained sand to white, fine- to medium-grained 32 Andkær borehole DGU no. 125.2017 100 90 80 70 m.b.s. GR V ej le F jo rd F m L o w er M io ce n e O li. B j. Fm B ill u n d F m H vi d b je rg M b Sk an se b ak ke M b 20 cps 100 Fig. 26. The reference section of the Skansebakke Member is the interval from 91.10 to 79 m in the Andkær borehole. Note that the sand-rich nature of the interval indicated by the gamma-ray log is not reflected by the lithological sample data; for legend, see Fig. 8, p. 17. Bj.: Brejning. Oli.: Oligocene. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 32 33 sand of the Hvidbjerg Member (Billund Formation). This boundary is only documented in the Andkær borehole where the gamma-ray log changes from serrated, low–inter- mediate gamma-ray readings of the Skansebakke Member to more consistently low gamma-ray values of the Hvidbjerg Member. Distribution. The Skansebakke Member is restricted to cen- tral east Jylland and is exposed along the coast of Vejle Fjord (Fig. 10B). In the subsurface, this member is only recognised in the Andkær borehole. Biostratigraphy. The Chiropteridium galea and the Homo- tryblium spp. Dinocyst Zones of Dybkjær & Piasecki (2010) are recorded in the Skansebakke Member. Geological age. The Skansebakke Member is of Aquitanian (earliest Early Miocene) age. Fig. 27. Alternating fine-grained sand and clay of the Skansebakke Member at Skansebakke. The clay was deposited in a lagoon and the sand was deposited as washover fans during the degradation of a barrier island associated with an Early Miocene transgression. Spade for scale (c. 1.3 m long). Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 33 34 Billund Formation new formation Name. After the town of Billund (Fig. 1). Type and reference sections. The type section of the Billund Formation is the interval from 235 m to 184 m (235–185 m MD) in the Billund borehole (DGU no. 114.1857, 55°43´08.53´´N, 9°08´33.98´´E; Fig. 28). The reference section is the interval from 160 to 126 m (161–128 m MD) in the Store Vorslunde borehole (DGU no. 104.2325; Fig. 28). Thickness. In the type section, the formation is 51 m thick; the maximum thickness of 77 m has been found in the Hammerum borehole (Plate 6). Lithology. The Billund Formation is primarily known from the subsurface but is exposed at a number of localities. In the Lillebælt area, the formation is exposed at Børup, Galsklint, Hindsgavl, Røjle and Rønshoved and in the Vejle Fjord region at Dykær, Fakkegrav and Hvidbjerg. In cen- tral Jylland, the formation can be observed at Addit, Salten and Voervadsbro, and at Søndbjerg and Lyby in northern Jylland. It is composed of fine- to coarse-grained sand with some gravel or pebble-rich beds (Fig. 29). The formation consists of almost pure quartz sand and includes clasts of quartzitic sandstone with subordinate mica and heavy min- erals. Clasts of well-rounded chert occur locally. Pebbly horisons are common in the upper part and at the base of fluvial channels; clasts up to 4 cm occur in erosional scours within steep clinoform units. The formation is charac- terised by both coarsening-upward and fining-upward depo- sitional patterns. Fine-grained sand units which are commonly hummocky cross-stratified, occur in the lower part of the formation and in eastern sections. The upper part is commonly dominated by swaley cross-stratified sand or sharp-based sand with a homogeneous or laminated lower part capped by wave ripples. The trace fossils Ophiomorpha isp. and Skolithos isp. are common (Fig. 29; Friis et al. 1998; Rasmussen & Dybkjær 2005). In the northern area, the formation is dominantly com- posed of cross-bedded sand with a range of set thicknesses. Soft sediment deformation structures are commonly seen. Some sections show an interval of interbedded, fine-grained, wave-rippled sands, muds and coals, sandwiched between two sand bodies with an overall sheet geometry. Root hori- zons and tree stumps are locally present (Weibel 1996; E.S. Rasmussen et al. 2007). In the eastern area, where the for- mation crops out, the sands are characterised by hum- mocky and swaley cross-stratification and homogeneous to laminated sand beds commonly capped by wave rip- ples; tidal bundles are also present (Fig. 30). The interbed- ded muds and heteroliths are dark brown in the northern part due to a high content of organic matter. In the south- ern area, the mud is light brown and typically thinner bed- ded, occurring interbedded with storm sand beds. Log characteristics. The formation is generally characterised by low gamma-ray values. In some boreholes, the lower part is characterised by a serrated lower part with gener- Fig. 28. Type and reference sections of the Billund Formation. The type section is the interval from 235 to 184 m in the Billund bore- hole and the reference section is the interval from 160 to 126 m in the Store Vorslunde borehole; for legend, see Fig. 8, p. 17. Bra.: Brande. Olig.: Oligocene. Billund borehole DGU no. 114.1857 Store Vorslunde borehole DGU no. 104.2325 L o w er M io ce n e O lig o . V ej le F jo rd F m B ra . F m K lin ti n gh o ve d F m B ill u n d F m L o w er M io ce n e E o ce n e V ej le F jo rd F m B ill u n d F m Sø vi n d F m 240 230 220 210 200 190 180 170 160 220 210 200 190 180 170 160 150 140 130 120 110 100 m.b.s. m.b.s. GRGR 20 cps cps 100 0 80 Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 34 35 ally higher gamma-ray values (e.g. Hammerum borehole, Plate 6). In the type borehole, the Billund Formation shows consistently low gamma-ray readings (Fig. 28). Fossils. The Billund Formation contains fossil wood (Weibel 1996), leaves and seeds (Ravn 1907) but also marine mol- luscs (e.g. in the ‘Brøndum Blokke’; Friis 1995). Foraminifers and dinocysts are present locally (Laursen & Kristoffersen 1999; E.S. Rasmussen et al. 2006). Depositional environment. The Billund Formation was deposited as a delta system prograding from the north and north-east towards the south and south-east. The well-con- strained palaeogeographical setting is based on high-reso- lution seismic data and facies distribution (Rasmussen & Dybkjær 2005; Hansen & Rasmussen 2008). Progradation took place in association with an Early Miocene inversion phase (E.S. Rasmussen 2009a), and the distribution of the delta lobes was consequently strongly controlled by the antecedent topography. Two major lobes, the Ringkøbing and Brande lobes, were mapped by Hansen & Rasmussen (2008). The Billund delta complex was deposited as wave- dominated deltas (Rasmussen & Dybkjær 2005; Hansen & Rasmussen 2008; E.S. Rasmussen 2009b). The south- eastward longshore currents that prevailed during the Early Miocene resulted in deposition of spit and barrier complexes south-east of the main delta lobes (Hvidbjerg Member). The most coarse-grained part was deposited in steeply dipping clinoformal packages deposited during falling sea-level (Hansen & Rasmussen 2008; E.S. Rasmussen 2009b) and within incised valleys (Addit Member). Boundaries. The lower boundary is defined by a change from clayey, organic-rich silty sediments of the Vejle Fjord Formation to sand-rich deposits; as noted earlier, recogni- tion of the Billund Formation requires a minimum sand thickness of 5 m and a sand–mud ratio of over 75%. Locally, for example in the type section at Billund, sand referred to the Billund Formation overlies the Eocene Søvind Marl; in such sections, the base of the formation is a significant Fig. 29. Marine sand and fluvial gravel and sand of the Billund Formation exposed at Voervadsbro. Note the Skolithos burrows (centre) indi- cating a marine depositional environment. The lower boundary of the fluvial deposits (Addit Member) is at the base of the gravel layer (dashed line). The illustrated section is 2 m high. Addit Mb Billund Fm Addit Mb Billund Fm Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 35 36 hiatal surface. On the gamma-ray log, the lower boundary is identified by a marked decrease in gamma-ray readings. In some sections (e.g. Store Vorslunde, Fasterholt bore- holes, Plate 2), the shift from mud- to sand-rich deposits is gradational and reflected by a gradual but steady decrease in gamma-ray readings; the boundary is placed according to the criteria described above. The upper boundary is placed at the change from sand- rich deposits of the Billund Formation to the predomi- nantly dark brown, silty clays of the Klintinghoved Formation or the Vejle Fjord Formation. At outcrop, the boundary is often erosive and overlain by a gravel lag or sand layer showing a fining-upward trend; the base of the gravel lag or sand layer forms the upper boundary. On the gamma-ray log, the upper boundary shows a variety of motifs. In boreholes where the sandy Billund Formation is succeeded by mud-dominated facies of the Klintinghoved Formation, the boundary is defined at an abrupt increase in values. Where the lower Klintinghoved Formation includes gravel and sand layers succeeded by mud-rich facies (e.g. Egtved borehole, Plate 7), the boundary is placed at the base of a prominent shift to lower gamma-ray val- ues that is succeeded by a general upward increase in val- ues. Where gamma-ray readings are strongly serrated, the boundary is placed at the base of the most coarse-grained sand or gravel layer found in the lithological descriptions. Distribution. The Billund Formation is distributed in cen- tral Jylland (Fig. 10C). Although beyond the formal bound- aries of the formation, a sand-rich succession reported from the subsurface of the North Sea may represent the west- ernmost lobe of the Billund delta complex (Hansen & Rasmussen 2008). Biostratigraphy. The Chiropteridium galea and the Homo- tryblium spp. Dinocyst Zones of Dybkjær & Piasecki (2010) are recorded in the Billund Formation. Geological age. The Billund Formation is of Aquitanian (earliest Early Miocene) age. Subdivision. The Billund Formation includes two mem- bers: the Hvidbjerg Member and the Addit Member. Hvidbjerg Member new member General. The new Hvidbjerg Member represents a partic- ular facies variant of the Billund Formation, dominated by spit deposits. The diagnostic features are only convincingly recognised at outcrop; the member is thus only recognised in the Vejle Fjord area in outcrops and closely adjacent boreholes. The member also crops out at Søndbjerg and Lyby in the Limfjorden area (Fig. 1). History. The succession of white sands at Hvidbjerg Strand was studied by Larsen & Dinesen (1959); these authors refrained from including the ‘Hvidbjerg Sand’ in the Vejle Fjord Formation due to contrasting heavy mineral suites in these two units. Name. After the outcrop at Hvidbjerg Strand on the south coast of Vejle Fjord (Fig. 1). Type and reference sections. The type section of the Hvidbjerg Member is the coastal exposure at Hvidbjerg Strand on the south coast of Vejle Fjord (55°38´24.58´´N, 9°44´39.22´´E; Figs 31, 33). Other exposures are at Sanatoriet, Fakkegrav and Dykær in the Vejle Fjord area, at Pjedsted north-west of Fredericia and at Hindsgavl, Galsklint, Børup and Rønshoved in the Lillebælt area. The sand crops out at two localities in the Limfjorden area, at Søndbjerg and Lyby. The reference section is the interval Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 36 37 from 79 to 58 m (79–58 m MD) in the Andkær borehole (DGU no. 125.2017; Fig. 32). Thickness. The member is 28 m thick in the type section at Hvidbjerg (Fig. 31). In the outcrops of the Lillebælt area, it can attain 13 m but is rarely thicker than 6 m. In the subsurface, the member is recognised in the Andkær borehole (reference section, 21 m thick) and the Lillebælt borehole (c. 11 m). Lithology. The Hvidbjerg Member consists of white, fine- to medium-grained sand with a few pebble layers (Fig. 33). The sand beds are dominated by sharp-based, structureless to evenly laminated sand capped by wave ripples. Hummocky and swaley cross-stratification are common in the southern area, near Lillebælt (Fig. 34). Trough and tab- ular cross-stratified sand beds occur locally as well as tidal bundles. The cross-bedding indicates bipolar current direc- tions towards the north-east and south-west. Thin, light brown clay layers are common in the southern part. North of Hvidbjerg, a dark brown, mud-dominated unit up to 3 m thick is recognised, locally capped by wood debris. The trace fossils Ophiomopha isp. and Skolithos isp. occur locally. The Hvidbjerg Member differs from the remainder of the Billund Formation in relation to its better sorting and its dominantly aggradational stacking pattern (e.g. Rasmussen & Dybkjær 2005). Log characteristics. The member is characterised by low gamma-ray readings (Fig. 32). High gamma-ray readings may be recorded where clay-rich, lagoonal deposits occur. Fossils. A relatively rich dinocyst assemblage occurs in the Hvidbjerg Member (Dybkjær 2004a; Rasmussen & Dyb- kjær 2005). Depositional environment. Deposition took place in a storm- dominated shoreface environment associated with spit development, south-east of the main Billund delta lobes. The core of a spit system crops out at Hvidbjerg. North of Hvidbjerg, shoreface sands alternate with mud-rich lagoon- al deposits (Fig. 21). Tidal inlet deposits are observed at Dykær and Pjedsted where flood- and ebb-dominated sys- tems, respectively, are recorded (Fig. 30). Boundaries.The member overlies the Vejle Fjord Formation; the lower boundary is marked by a change from black, organic-rich, clayey silt to white sand. At Hvidbjerg, the lower boundary is erosional (Fig. 31). Where the member is superimposed on the Skansebakke Member of the Vejle Fjord Formation, the lower boundary is identified by a change from yellowish sands of the Skansebakke Member to white sands of the Hvidbjerg Member. On the gamma- ray log, the boundary is characterised by a distinct shift towards low gamma-ray readings. The upper boundary is placed at the change from sand- rich deposits of the Hvidbjerg Member to the predominantly dark brown, silty clay of the Klintinghoved Formation. The boundary is often erosional and overlain by a gravel lag or sand layer showing a fining-upward trend; the gravel lag commonly contains of clasts up to 4 cm in diameter. The base of the gravel lag forms the upper boundary of the member. The gamma-ray readings may be characterised by an abrupt increase followed by a gradual decrease in values or a marked decrease in gamma-ray readings suc- Fig. 30. Tidal bundles in the Hvidbjerg Member exposed at Pjedsted, north-west of Fredericia (Fig. 1). The cross-bedding dips towards the south-west and thus reflects ebb current flow. Note the clay drapes and preserved bottom sets (arrows) recording sedimentation during neap tides. The cross-bedded section thus represents a neap–spring–neap cycle (i.e. c. one and a half months). The section is 1.5 m high. Photograph courtesy of Ole Rønø Clausen. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 37 38 Hvidbjerg outcrop 0 1 2 3 4 5 6 7 8 9 10 m 10 11 12 13 14 15 16 17 18 19 20 Cl Si F MC P Sand 20 21 22 23 24 25 27 26 28 Cl Si F MC P Sand Cl Si F MC P Sand L o w er M io ce n e B ill u n d F m V ej le F jo rd F m H vi d b je rg M b L o w er M io ce n e B ill u n d F m H vi d b je rg M b L o w er M io ce n e B ill u n d F m H vi d b je rg M b Fig. 31. Type section of the Hvidbjerg Member from the coastal exposures at Hvidbjerg, south-east of Vejle (Fig. 1); for legend, see Fig. 8, p. 17. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 38 39 ceeded by a gradual increase (e.g. Andkær borehole, Fig. 32); the boundary is placed at the lowest gamma-ray response. Distribution. The Hvidbjerg Member is present in east Jylland and has also been found at Søndbjerg in north- west Jylland (Fig. 10C). Biostratigraphy. The Chiropteridium galea and the Homo - tryblium spp. Dinocyst Zones of Dybkjær & Piasecki (2010) are recorded in the Hvidbjerg Member. Geological age. The Hvidbjerg Member is of Aquitanian (earliest Early Miocene) age. Fig. 33. The c. 27 m of white sand exposed at Hvidbjerg represents deposition on a spit system east of the main delta lobe of the Billund Formation. Note the stratification defined by the most bioturbated parts of the succession; photograph illustrates the upper levels of the Hvidbjerg Member shown in Fig. 31. Andkær borehole DGU no. 125.2017 90 80 70 60 50 m.b.s. GR L o w er M io ce n e B ill u n d F m K lin ti n gh o ve d F m V ej le F jo rd F m H vi d b je rg M b Sk an se b ak ke M b 20 cps 100 Fig. 32. Reference section of the Hvidbjerg Member in the Andkær borehole (79–58 m); for legend, see Fig. 8, p. 17. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 39 Addit Member new member History. Sand-rich fluvial and coal-bearing deposits in the Silkeborg area were first studied by Hartz (1909). He cor- related the succession with Lower Miocene coal-bearing deposits in Schleswig-Holstein. L.B. Rasmussen (1961) indicated that the fluvio-deltaic sediments of the Silkeborg–Skanderborg area could be of similar age to the Ribe Formation as defined from the Arnum-1 well in south- ern Jylland. Studies of the succession in gravel pits south of Silkeborg were carried out during the 1970s and 1980s, focusing on the depositional environment and diagenesis (Friis 1976, 1995; Hansen 1985; Hansen 1995; Jesse 1995). These studies referred the deposits to the Middle Miocene Odderup Formation, although Friis (1995) was aware of the problems inherent in this correlation. Re-investigation of the Salten inland cliff and the gravel pits at Addit and Voervadsbro, including biostratigraphic analysis based on dinocysts, revealed that the succession is Early Miocene in age and should be correlated with the Vejle Fjord Formation – Billund Formation depositional phase (E.S.Rasmussen et al. 2006). Name. After the village of Addit, south-south-west of Århus (Fig. 1). Type and reference sections. The type section of the Addit Member is defined as the Dansand gravel pit at Addit (56°02´26.33´´N, 9°37´59.62´´E; Fig. 35). The member is also exposed in the Voervadsbro gravel pit which forms the primary reference section (Fig. 36), and in the inland cliff at Salten. The secondary reference section is the inter- val from 117 to 55 m (119–55 m MD) in the Addit Mark borehole (DGU no. 97.928; Fig. 37). Thickness. In the type section, the Addit Member is over 33 m thick; neither top nor base are seen. In the Addit borehole nearby (Fig. 1), the member is 50 m thick (Plate 6) and 62 m was penetrated in the borehole at Addit Mark (Fig. 37; Plate 6). Where well developed in central and north-east Jylland, the member is typically 20–50 m thick (see Plates 1, 2, 5, 6). Lithology. The succession is typically composed of two sand- and gravel-rich units separated by fine-grained, sandy and clayey sediments, commonly with intercalated coal layers (Figs 35, 36, 38; Plates 1, 6), though the middle hetero- geneous unit may be absent or poorly developed. The sands consist almost solely of quartz and quartzitic sandstone lithic grains, with minor content of mica and heavy min- erals; clasts of well-rounded chert may occur. The two sand- rich units are characterised by fining-upward trends and possess sheet geometry. The lower part of each unit con- sists of trough cross-stratified, coarse-grained sand and gravel alternating with large-scale cross-stratified sand (Figs 35, 36, 39). Upwards, these sand-rich units are progressively dominated by tabular co-sets of cross-stratified sand. The sand-rich succession may be capped by fine-grained, cross- bedded sand showing lateral accretion structures. The coal- bearing, fine-grained sand and clay layer, sandwiched between the coarser units, consists of cross-bedded sand and alternating thin, rippled, fine-grained sand and clay layers. Bioturbation is observed rarely. Wood fragments are abun- 40 Fig. 34. Hummocky cross-stratified sand of the Billund Formation (Hvidbjerg Mem- ber) overlying interbedded, hummocky cross-stratified sands and clays of the Vejle Fjord Formation; Hindsgavl, near Middlefart (Fig. 1). Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 40 41 Addit outcrop 0 1 2 3 4 5 6 7 8 9 10 m 10 11 12 13 14 15 16 17 18 19 20 Cl Si F MC P Sand 20 21 22 23 24 25 26 27 28 29 30 30 31 32 33 Cl Si F MC P Sand Cl Si F MC P Sand Cl Si F MC P Sand B ill u n d F m L o w er M io ce n e A d d it M b B ill u n d F m L o w er M io ce n e A d d it M b B ill u n d F m L o w er M io ce n e A d d it M b B ill u n d F m L o w er M io ce n e A d d it M b Fig. 35. Type section of the Addit Member in the Addit gravel pit, south-east of Silke- borg (Fig. 1); for legend, see Fig. 8, p. 17. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 41 42 Voervadsbro outcrop 0 1 2 3 4 5 6 7 8 9 10 m 10 11 12 13 14 15 16 17 18 19 20 Cl Si F MC P Sand 20 21 22 23 26 25 24 Cl Si F MC P Sand Cl Si F MC P Sand B ill u n d F m A d d it M b B ill u n d F m A d d it M b B ill u n d F m L o w er M io ce n e L o w er M io ce n e L o w er M io ce n e A d d it M b Fig. 36. Primary reference section of the Addit Member in the Voervadsbro gravel pit, south-east of Silkeborg (Fig. 1), where the lower part of the member is exposed; for legend, see Fig. 8, p. 17. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 42 dant at certain horizons and petrified wood is common at Voervadsbro (Weibel 1996). Log characteristics. The member is characterised by low gamma-ray readings, especially in the lower part (Fig. 37). The sand-rich part is commonly characterised by a slight upward increase in gamma-ray values. A moderate–high gamma-ray response commonly characterises the middle part of the member, reflecting the clay-rich and coal-bear- ing deposits at this level. Fossils. The Addit Member contains fossil wood (Weibel 1996), leaves and seeds (Ravn 1907). Dinocysts occur very sporadically in the Addit Member (Dybkjær 2004a, b; E.S. Rasmussen et al. 2006). Depositional environment. The lower sands of the member were deposited as migrating three-dimensional dunes (main channel) and migrating unit and compound bars in a braided fluvial system (Hansen 1985; Hansen 1995; E.S. Rasmussen et al. 2006). The upper part of the member was deposited as migrating two-dimensional dunes; sedi- mentary structures such as cross-bedded sand beds with preserved bottomsets and normally graded foresets indicate tidal influence (Pontén & Plink-Björklund 2007). The upper part of the sand succession, showing lateral accre- tion, was laid down in a point bar of a meandering fluvial system. The fine-grained middle part of the member was deposited in a flood plain and lake environment that was occasionally flooded by the sea as indicated by the rare presence of dinocysts and Ophiomorpha trace fossils. Boundaries. Where the Addit Member directly overlies the Vejle Fjord Formation, the lower boundary is marked by an abrupt change from dark brown, silty clay or clayey silt to grey, coarse-grained sand and gravel (Fig. 37; Plates 1, 2, 6). Where the Addit Member overlies the Hvidbjerg Member, the boundary is marked by an erosional bound- ary where white, fine- to medium-grained sand is overlain by gravel (Fig. 29). On the gamma-ray log, the lower bound- ary is shown as a prominent shift on the gamma-ray log where the Addit Member overlies the Vejle Fjord Formation. Where the member overlies the Hvidbjerg Member, the lower boundary is placed at the change of gamma-ray read- ing from a gradual upward decrease in gamma-ray readings to consistently low or decreasing-upward gamma-ray read- ings. The upper boundary is placed at the change from sand- rich deposits of the Addit Member to predominantly dark brown, silty clays of the Klintinghoved Formation. The boundary may be erosional, being overlain by a gravel lag or sand layer showing a fining-upward trend; the gravel lag commonly contains clasts up to 4 cm in diameter. The base of the gravel lag or sand layer forms the upper bound- ary of the member. The gamma-ray log is commonly char- acterised by an abrupt increase in gamma-ray values (e.g. 43 Fig. 37. Secondary reference section of the Addit Member in the Addit Mark borehole (117–55 m); for legend, see Fig. 8, p. 17. K.: Klintinghoved. 140 0 cps 90 130 120 110 Addit Mark borehole DGU no. 97.928 100 90 80 70 60 m.b.s. GR V ej le F jo rd F m L o w er M io ce n e B ill u n d F m K . F m A d d it M b Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 43 Resen, Plate 5; Isenvad, Plate 6). Locally, a decrease in gamma-ray readings is succeeded by a gradual increase in gamma-ray values (e.g. Hammerum, Sunds, Plate 2). Here the boundary is placed at the lowest gamma-ray readings. Distribution. The Addit Member is found in the central and northern parts of Jylland. It is especially well developed in the area south of Silkeborg, in an elongate zone striking from Resen (south-west of Viborg) to the area between Herning and Ikast (Figs 1, 10C). Biostratigraphy. The Homotryblium spp. Dinocyst Zone of Dybkjær & Piasecki (2010) is recorded in the Addit Member. Geological age. The Addit Member is of Aquitanian (earli- est Early Miocene) age. 44 Fig38 Coal bedCoal bed QuaternaryQuaternary Fig. 38. Addit Member at the Addit gravel pit showing the two fining- upward sand- and gravel-rich units and the intercalated coal unit. The height of the section is 40 m. Fig. 39. Cross-bedded sand and gravel of the Addit Member in the Addit gravel pit deposited as a mid-channel bar in a braided fluvial system. The height of the section is 3 m. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 44 Klintinghoved Formation redefined formation General. The marine clay-rich deposits of the Klintinghoved Formation interdigitate towards the north-east with the more proximal sand-rich deltaic sediments of the Bastrup Formation. These formations thus alternate up-section in certain boreholes (e.g. Plates 1, 2, 6). History. The mollusc fauna of marine clay-rich deposits at Klintinghoved was described by Sorgenfrei (1940). The deposits were defined as the Klintinghoved Formation in a later publication (Sorgenfrei 1958). The Klintinghoved Formation was included in the stratigraphy of L.B. Rasmussen (1961). Name. After Klintinghoved cliff, Flensborg Fjord (Figs 1, 42). Type and reference sections. Following Sorgenfrei (1958), the type section is the outcrop at Klintinghoved cliff (54°53´23.15´´N, 9°49´43.62´´E; Figs 40, 42). The ref- erence section is designated in the cored Sdr. Vium bore- hole (DGU no. 102.948; 54°53´23.18´´N, 9°49´43.94´´E) from 288 to 132 m (Figs 40, 41). Thickness. At Klintinghoved, the exposed section is 3.5 m thick; neither base nor top of the formation is seen. In the subsurface, the formation is 10–50 m thick in central Jylland, thickening to over 125 m in the west and south- west (e.g. Sdr. Vium, Fig. 40). Lithology. The formation consists of dark brown, silty clay with subordinate intercalated sand beds (Figs 43, 44). The sand beds are sharp based and homogenous to finely lam- inated; double clay layers are recognised locally. In the cored borehole at Sdr. Vium, the formation is dominated by dark brown mud with intercalated sand beds (Figs 40, 41, 45). The sand beds typically show sharp lower bound- aries, and are commonly structureless in the lower part passing upward into laminated sand. Log characteristics. The formation is characterised by mod- erate to high gamma-ray values (Fig. 40). The log pattern is highly serrated, reflecting interbedded muds and sands at various levels, and shows a general decrease in gamma- ray response upwards. Fossils. The Klintinghoved Formation contains a rich mol- lusc fauna (Sorgenfrei 1958). Shark teeth also occur and marine microfossils such as foraminifers (Laursen & Kristoffersen 1999) and dinocysts (Dybkjær & Rasmussen 2000; Dybkjær 2004a; Rasmussen & Dybkjær 2005) are abundant and diverse. 45 Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 45 46 Klintinghoved outcrop 0 1 2 3 m Cl Si F MC P Sand Sdr. Vium borehole DGU no. 102.948 300 200 m.b.s. 200 190290 280 270 260 250 240 230 220 210 Cl Si F MC P Sand Not cored No GR log available Cl Si F MC P Sand L o w er M io ce n e K lin ti n gh o ve d F m L o w er M io ce n e K lin ti n gh o ve d F m L o w er M io ce n e K lin ti n gh o ve d F m 160 150 140 130 120 110 L o w er M io ce n e A rn u m F m B as tr u p F m K lin ti n gh o ve d F m GR 40 100 cps Fig. 40. Type and reference sections of the Klintinghoved Formation. The type section is defined at Klintinghoved, east of Sønderborg, where 3.5 m of the formation is exposed. The reference section is the interval from 288 to 132 m in the Sdr. Vium borehole. The inter- vals outlined in red are shown in detail in Fig. 41; for legend, see Fig. 8, p. 17. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 46 47 Depositional environment.The Klintinghoved Formation was deposited in shelf, delta slope and lower shoreface envi- ronments. Water depths were in the order of 15 to 60 m, but locally up to 100 m based on the height of clinoforms seen on seismic data. The depositional environment was strongly influenced by storms and tidal processes. Boundaries. The lower boundary is, in the northern part, characterised by a change from sand-rich deposits of the Billund Formation to the predominantly dark brown, silty clay of the Klintinghoved Formation (e.g. Store Vorslunde, Fasterholt, Sunds and Resen boreholes, Plate 2). In the southern part where the Klintinghoved Formation overlies the Vejle Fjord Formation, the boundary is not marked by significant changes in lithology, although the Vejle Fjord Formation tends to be slightly more consolidated. On the gamma-ray log, a weak to marked shift to higher gamma- ray values defines the boundary, especially where the Klin- tinghoved Formation overlies the Billund Formation (e.g. Rødding, Almstok, Store Vorslunde, Fasterholt, Sunds and Resen boreholes, Plate 2). At outcrop, the lower boundary is often erosional and overlain by a gravel lag, as seen at Rønshoved and Børup (Rasmussen & Dybkjær 2005); the gravel lag commonly contains clasts up to 4 cm in di ameter. The upper boundary is either sharp, exemplified by the Bastrup borehole (Fig. 52; Plate 8), or gradational as in the Almstok borehole (Fig. 52; Plate 2). In the Bastrup bore- hole, the upper boundary is placed where grey mud is sharply overlain by grey, medium-grained sand. In bore- holes where a more gradational development occurs, the boundary is marked by a change from alternating beds of sand and mud to a clean sand unit at least 5 m thick and comprising at least 75% sand. On the gamma-ray log, the 275 274 273 272 271 270 269 268 267 266 265 Cl Si F MC P Sand 140 139 138 137 136 135 134 133 Cl Si F MC P Sand Sdr. Vium borehole DGU no. 102.948 Sdr. Vium borehole DGU no. 102.948 m.b.s m.b.s Fig. 41. Detailed sedimentological logs of representative intervals of the Klintinghoved Formation in the reference section (for loca- tion, see Fig. 40; for legend, see Fig. 8 on page 17). Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 47 48 Double clay layersDouble clay layers Fig. 42. The Klintinghoved cliff, viewed from the east (cliff is c. 10 m high). The location of the type section of the Klintinghoved Formation is arrowed. Fig. 43. Alternating clay and bioturbated and laminated sand of the Klintinghoved Formation at the type locality. Note the double clay layers in the sand indicating tidal influence on deposition. Fig. 44. Interlaminated, dark brown clayey silt and thin, fine-grained sand of the Klintinghoved Formation at the type locality. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 48 boundary is generally characterised by a minor decrease in gamma-ray values followed by a consistent decrease in val- ues upwards, as seen in the Almstok borehole (Fig. 52; Plate 2) and in the Holstebro and Klosterhede boreholes (Plate 4). In the Bastrup borehole, the upper boundary is characterised by a distinct decrease in gamma-ray values. In western Jylland where Klintinghoved Formation is over- lain by the Arnum Formation (e.g. Kvong, Sdr. Vium bore- holes, Plate 4), the boundary is placed at a distinct increase in gamma-ray readings separating coarsening-upward units of the Klintinghoved and Arnum Formations. Distribution. The Klintinghoved Formation is distributed in the northern part of central Jylland and in western and southern Jylland (Fig. 10D). Biostratigraphy. The Thalassiphora pelagica and Sumatra- dinium hamulatum Dinocyst Zones of Dybkjær & Piasecki (2010) are recognised in the Klintinghoved Formation. Geological age. The Klintinghoved Formation is of late Aquitanian to early Burdigalian (Early Miocene) age. Subdivision. The Klintinghoved Formation includes the new Kolding Fjord Member. 49 Fig. 45. Core sections from the Sdr. Vium borehole, illustrating interbedded, dark brown silty clays and sharp-based sands of the Klintinghoved Formation. A: 272.70 m (base of illustrated sec- tion); B: 250.45 m (base). The sand beds are normally graded and homogenous to weakly laminated in the lower part. Note the double clay layers (B, arrow) indicating tidal influence on sedi- mentation. 1 cm A B Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 49 Kolding Fjord Member new member History. Sand and organic-rich clayey sediments exposed at Lillebælt were studied by Radwanski et al. (1975), E.S. Rasmussen (1995) and Friis et al. (1998). In these studies, the sediments were referred tentatively to the Vejle Fjord Formation of previous usage. However, a biostratigraphic study by Dybkjær & Rasmussen (2000) revealed that the sediments were significantly younger than the Vejle Fjord Formation (as recognised here) and equivalent in age to the Klintinghoved Formation (L.B. Rasmussen 1961). Name. The Kolding Fjord Member crops out at a number of localities along Lillebælt and Kolding Fjord. It is named after Kolding Fjord, where the type locality of Rønshoved is situated. Type and reference sections. The type section is the exposure at Rønshoved on the southern side of Kolding Fjord (55°29´26.90´´N, 9°38´36.10´´E; Figs 1, 46). Other local- ities where the member is exposed are Hagenør, Børup, Galsklint and Fænø in the Lillebælt and Kolding Fjord area (Fig. 1). A minor outcrop is also recognised at Gyldendal, Limfjorden. The reference section is the out- crop at Hagenør (Figs 1, 47). Thickness. The Kolding Fjord Member is 11 m thick at Rønshoved and c. 8 m at Hagenør (Figs 46, 47). Although rarely exceeding 10 m, developments up to 20 m thick are recognised locally (e.g. Vonsild and Vind boreholes, Plates 1, 8). Lithology. The member is composed of white to yellow, fine- to medium-grained sand with a few thin, brown clay layers. At the type section, the basal unit is a gravel layer c. 10 cm thick that contains clasts up to 4 cm in diameter. The clasts consist of almost pure quartz and quartzitic sand- stone. The succeeding sandy part of the member in the type section is dominated by hummocky and swaley cross- stratified silt and fine-grained sand (Figs 46, 48). The more clayey part is dominated by heterolithic mud which shows hummocky cross-stratification and clear rhythmicity i.e. double clay layers and alternating sand- and mud-rich units. Layers up to 2 m thick of dark brown, organic-rich, clayey silt may be intercalated in the sand (Figs 49, 50). Homo- 50 Rønshoved (east) outcrop 0 1 2 3 4 5 6 7 8 9 10 m Cl Si F MC P Sand K lin ti n gh o ve d F m L o w er M io ce n e K o ld in g Fj o rd M b B ill u n d F m H vi d b je rg M b 10 11 12 13 Cl Si F MC P Sand K lin ti n gh o ve d F m L o w er M io ce n e K o ld in g Fj o rd M b Fig. 46. Type section of the Kolding Fjord Member at Rønshoved, east of Kolding; for legend, see Fig. 8, p. 17. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 50 geneous sand beds capped by wave-ripples are also com- mon on top of lagoonal deposits (Fig. 51); wave-ripple crests are oriented north-west–south-east. Trace fossils, including Macaronichnus isp., Ophiomorpha nodosa and echinoid burrows, are common in the Kolding Fjord Member (Radwanski et al. 1975). Log characteristics. The member is characterised by low to moderate gamma-ray values. The log pattern is serrated; high gamma-ray values are registered where lagoonal, clay-rich deposits dominate. Fossils. The Kolding Fjord Member contains a dinocyst assemblage of variable richness (Dybkjær & Rasmussen 2000; Rasmussen & Dybkjær 2005). Depositional environment. Deposition took place on a storm- dominated coast in a lower and upper shoreface environ- ment (Friis et al. 1998; Rasmussen & Dybkjær 2005). The fine-grained, heterolithic part was deposited in a lagoonal environment with some tidal influence. The upper part of the member was deposited as washover fans on the back-bar- rier flat during the final degradation of the barrier complex. Boundaries. In the type section, the lower boundary is ero- sional and, as in other exposures (e.g. Børup, Galsklint) and borehole sections (e.g. Stakroge, Plate 3), is defined by a distinct change from the sandy deposits of the Billund Formation to gravel-dominated layers of the lowermost Kolding Fjord Member. In such cases, the gamma-ray log shows a marked decrease in values at the boundary (Plate 3). In the Vonsild borehole, however, located near the type and reference sections, the lower boundary is recognised by a prominent increase in gamma-ray readings, due to the presence of fine-grained, lagoonal sediments in the lower part of the member (Plates 1, 8). It is acknowledged that identification of this boundary may be difficult on the gamma-ray log where shoreface sands occur both beneath and above the boundary and the transgressive lag is thin. The upper boundary is characterised by a change from the sand-dominated succession of the Kolding Fjord Member to dark brown, clayey silts of the Klintinghoved Formation. The gamma-ray log shows a distinct increase in gamma-ray values. Distribution. The member is recognised in east Jylland and south-west of Holstebro in west Jylland (Fig. 10D). Biostratigraphy. The Thalassiphora pelagica and Sumatra- dinium hamulatum Dinocyst Zones of Dybkjær & Piasecki (2010) occur in the Kolding Fjord Member. Geological age. The Kolding Fjord Member is of late Aquitanian to early Burdigalian (Early Miocene) age. 51 Hagenør outcrop 0 1 2 3 4 5 6 7 8 m Cl Si F MC P Sand K lin ti n gh o ve d F m L o w er M io ce n e Q u at . K o ld in g Fj o rd M b Fig. 47. Reference section of the Kolding Fjord Member at Hage- nør; for legend, see Fig. 8, p. 17. Quat.: Quaternary. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 51 52 Fig. 48. Heterolithic deposits of the Kolding Fjord Member sharply overlain (at 5.3 m in Fig. 46) by hummocky cross-stratified sand at Rønshoved in the type section. The heterolithic succession is characterised by alternating hummocky cross-stratified sand and sandy clay and various types of ripple-laminated sand. About 3 m of the section is shown. Fig. 49. Exposure of the Kolding Fjord Member in the reference section at Hagenør. The lower part of the Hagenør outcrop is characterised by two organic-rich, clayey silt deposits separated by bioturbated sand (see Fig. 47). The upper part of the exposure is dominated by alter- nating sand and clay layers; the sand beds are typically sharp based, homogenous to weakly laminated in the lower part and capped by wave- or current-ripples. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 52 Bastrup Formation new formation General. The new Bastrup Formation is recognised pri- marily in the subsurface. This fluvio-deltaic, sand-domi- nated formation interdigitates in a complex manner with the more distal, marine, mud-rich Klintinghoved Formation. These formations thus alternate up-section in certain bore- holes (e.g. Plates 1, 2, 6). Name. After Bastrup village, south-west of Kolding (Fig. 1). Type and reference sections. The type section is the interval from 108 to 84 m (110–84 m MD) in the Bastrup bore- hole (DGU no. 133.1298; 55°24´21.58´´N, 9°14´47.40´´E; Fig. 52). The reference section is the interval from 160 to 111 m (160–111 m MD) in the borehole at Almstok (DGU no. 114.1858; Fig. 52). Thickness. The thickness of the Bastrup Formation is 24 m in the type section, but the formation is commonly c. 50 m thick (see reference section, Fig. 52 and Plates 2, 3). A maximum thickness of 100 m was penetrated in the borehole at Løgumkloster (Plate 3). Lithology. The Bastrup Formation consists predominantly of grey, medium- to coarse-grained sand with intercalated gravel layers; the diameter of gravel clasts rarely exceeds 2 cm. Petrologically, the sand is dominated by quartz and quartzite lithic grains with minor content of mica and heavy minerals. In a few boreholes, however, a high con- centration of mica has been recorded (e.g. Estrup). Dark brown, organic-rich, silty clay is locally present. The for- mation is characterised by both coarsening-upward and fining-upward depositional patterns. The upper part of the formation is commonly characterised by a 15–30 m thick fining-upward succession consisting of coarse-grained to fine- grained sand. In the north, gravel commonly forms the 53 Fig. 50. Close-up of lagoonal facies in the Kolding Fjord Member at Hagenør. The light brown deposits that are capped by sand ripples and sandwiched between dark lagoonal clays contain marine paly- nomorphs and represent a short marine incursion; the strike of the ripple crests is NW–SE. The illustrated section is c. 2 m high. Fig. 51. Close-up of the alternating sand and clay layers of the Kolding Fjord Member exposed in the upper part of the Hagenør reference section. Spade handle for scale. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 53 base of the fining-upward units. Clay-rich sediments with subordinate intercalations of coal are often sandwiched between sand-rich units. Log characteristics. The formation is characterised by low gamma-ray values (Fig. 52). The log pattern is serrated and shows both decreasing- and increasing-upward trends through the succession. The decreasing trend is associated with delta progradation and the increasing-upward trend is associated with channel-fill deposits (i.e. point bars) which are common in the upper levels of the formation, and can locally be demonstrated on seismic data (E.S. Rasmussen et al. 2007). Fossils. A sparse foraminifer assemblage occurs in the dis- tal part of the Bastrup Formation (Laursen & Kristoffersen 1999). The dinocyst flora is variable overall, being rich at some levels and very sparse/impoverished at other levels (Dybkjær 2004a; Dybkjær & Piasecki 2010). Depositional environment. Deposition took place in deltaic and fluvial environments. Well developed point bars and fluvial channels are common in the upper part (E.S. Rasmussen et al. 2007; E.S. Rasmussen 2009b). The inter- calated mud represents floodplain deposition. Boundaries. The lower boundary is either sharp, for exam- ple in the type section of the Bastrup borehole or grada- tional as in the Almstok reference section (Fig. 52). In the type section, the lower boundary is placed where grey mud is sharply overlain by grey, medium-grained sand; on the gamma-ray log, this lower boundary is defined at a marked decrease in gamma-ray values. A gravel layer is commonly present at the base of the Bastrup Formation. In grada- tional sections showing interbedded sands and muds, becoming sandier upwards, the boundary is defined at the base of the first significant sand interval (at least 5 m thick) in which the sand to mud ratio is greater than 75%. In such gradational sections, the log response reflects the transi- tional nature of the boundary, showing a minor decrease in gamma-ray values followed by a consistent overall decrease upwards (e.g. the Almstok borehole, Fig. 52). The upper boundary is defined by a sharp transition from grey and white sand of the Bastrup Formation to dark brown, silty clay of the Arnum Formation. In central Jylland, the Arnum Formation is developed as a grey to white silt, which rests with a sharp boundary on the sand-rich Bastrup Formation. On the gamma-ray log, this upper boundary is typically identified by a prominent shift to higher values. Distribution. The formation is present in southern and cen- tral Jylland. Towards the north-east, the formation is trun- cated and it pinches out towards the south-west (Fig. 10E). Biostratigraphy. The Sumatradinium hamulatum and Cordo- sphaeridium cantharellus Dinocyst Zones of Dybkjær & Piasecki (2010) occur in the Bastrup Formation. Geological age. The Bastrup Formation is of early Burdigalian (Early Miocene) age. Subdivision. The Bastrup Formation includes the new Resen Member. 54 Bastrup borehole DGU no. 133.1298 120 110 100 90 80 70 m.b.s. GR GR Almstok borehole DGU no. 114.1858 170 160 150 140 130 120 110 100 m.b.s. L o w er M io ce n e B as tr u p F m R es en M b K lin ti n gh o ve d F m A r. Fm O d d er u p. F m St au n in g M b L o w er M io ce n e B as tr u p F m K lin ti n gh o ve d F m A rn u m F m R es en M b 0 cps 120 0 150 cps Fig. 52. Type and reference sections of the Bastrup Formation. The type section is from 108 to 84 m in the Bastrup borehole. The reference sec - tion is from 160 to 111 m in the Almstok borehole; for legend, see Fig. 8 on page 17. Ar.: Arnum. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 54 Resen Member new member General. This member is recognised widely in the Bastrup Formation, representing fluvial-dominated facies that com- monly are inferred to be incised into the undifferentiated Bastrup Formation deltaic facies. It is mainly recognised in the subsurface, but coal was formerly mined in a pit near Resen, south of Skive (Fig. 1). Name. After the village of Resen, south of Skive, where a brown-coal pit was mined (Fig. 1). Type and reference sections. The type section is the com- posite interval from 124 to 112 m and from 97 to 70 m (125–113 m MD, 97–71 m MD) in the borehole at Hammerum, east of Herning (DGU no. 85. 2429; 56°07´55.45´´N, 9°05´33.52´´E; Figs 1, 53). The reference section is the interval from 104 to 67 m (105– 67 m MD) in the Egtved borehole, south-west of Vejle (DGU no. 124.1159; Figs 1, 53). Thickness. The member is 39 m thick in the type section (Fig. 53) and is typically in the range 10–40 m thick (Plates 2, 3, 6, 7). Lithology. The member consists of grey, medium- to coarse- grained sand with intercalated gravel layers. Dark brown, organic-rich, silty clay with some coal is present locally. The member is typically characterised by 10–30 m thick fining-upward successions; a number of boreholes show stacked, fining-upward cycles that may be separated by intervals referred to the Bastrup Formation (undifferenti- ated). Log characteristics. The member is characterised by low gamma-ray readings. The log pattern is serrated and, where simply developed (e.g. Billund, Plate 2), shows an increas- ing trend upwards, reflecting the origin of these sand-rich units as channel fill deposits. In some boreholes, such chan- nel sands are separated by finer-grained deposits showing moderate–high gamma-ray values (Fig. 53). Fossils. The dinocyst flora is variable overall, being rich at some levels and very sparse/impoverished at other levels (Dybkjær 2004a; Dybkjær & Piasecki 2010). Depositional environment. Deposition took place in fluvial environments, and well-developed point bars and fluvial channels are common (E.S. Rasmussen et al. 2007; E.S. Rasmussen 2009b). The intercalated mud represents flood- plain deposition and some marine influence has also been recognised, especially in the southern part. The most exten- sive coal formation was within freshwater lakes and mires developed in the rim synclines around salt diapirs, e.g. the Sevel and Mønsted salt structures south of Skive (Japsen & Langtofte 1991). Boundaries. The Resen Member is bounded both by sand- rich units (e.g. Bastrup Formation beneath, Vandel Member above) and by mud-rich units (Klintinghoved Formation beneath, Arnum Formation above). Where succeeding the Klintinghoved Formation, the boundary is sharp and placed where dark brown, clayey silts of the Klintinghoved Formation are sharply overlain by grey, medium- to coarse- grained sands, locally with a basal gravel layer. On the gamma-ray log, this relationship is recorded by an abrupt shift to lower values (Fig. 53). In sections where the Resen Member succeeds the undifferentiated Bastrup Formation, the boundary is defined at the base of coarser sand/gravel deposits at a shift from decreasing-upward gamma-ray val- ues (Bastrup Formation) to increasing-upward gamma-ray values (Resen Member channel sands). 55 Fig. 53. Type and reference sections of the Resen Member. The composite section (124–112 m, 97–70 m) in the Hammerum bore- hole is designated as the type section. The reference section is the interval from 104 to 67 m in the Egtved borehole; for legend, see Fig. 8, p. 17. A.: Arnum. Klint.: Klintinghoved. Od.: Odderup. Res.: Resen. Hammerum borehole DGU no. 85.2429 130 cps 120 110 100 90 80 70 60 m.b.s. Egtved borehole DGU no. 124.1159 110 20 cps 80 100 90 80 70 60 m.b.s. GRGR B as tr u p F m O d . F m L o w e r M io ce n e R e se n M b R e s. M b B as tr u p F m A . F m K lin t. F m K lin t. F m L o w e r M io ce n e R e se n M b 0 60 Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 55 56 The upper boundary is typically defined by a sharp tran- sition from grey and white sands of the Resen Member to dark brown, silty clay of the Arnum Formation; on the gamma-ray log this is reflected by an abrupt increase in values. In central Jylland, the upper boundary is charac- terised by a sharp change from grey and white sand to grey and white silt of the Vandel Member. On the gamma-ray log, this facies transition is reflected by an increase in gamma-ray values that continues up through the Vandel Member. Distribution. The member is present in southern and cen- tral Jylland (Fig. 10E; Plates 1, 2, 6). Towards the north- east, the member is truncated and it pinches out towards the south-west. Biostratigraphy. The Sumatradinium hamulatum and Cordo- sphaeridium cantharellus Dinocyst Zones of Dybkjær & Piasecki (2010) occur in the Resen Member. Geological age. The Resen Member is of early Burdigalian (Early Miocene) age. Arnum Formation revised formation General. The marine clay-dominated Arnum Formation is only recognised in the subsurface where it shows complex interdigitation with the nearshore sand-rich Odderup Formation. These two formations thus altenate up-section in some boreholes (Plates 1–9). History. The Arnum Formation was defined by Sorgenfrei (1958) to encompass the dark micaceous marine clays occurring stratigraphically above the Ribe Formation (of previous usage). Name. After Arnum village in southern Jylland (Fig. 1). Type and reference sections. The Arnum Formation was pen- etrated in two boreholes at Arnum (DGU no.150.13, DGU no.150.25b; both at 55°14´48.07´´N, 8°58´18.48´´E) from 107 to 40 m and from 107.5 to 40 m respectively (Sorgenfrei 1958); together these sections form the type sec- tion. The composite interval 132–111 m and 98–51 m in the cored borehole, Sdr. Vium (DGU no. 102.948) is des- ignated as the reference section (Fig. 54). A secondary ref- erence section is defined as the interval from 55 to 37 m (56–39 m MD) in the Store Vorslunde borehole (DGU no. 104.2325; Fig. 55). Thickness. The formation is c. 93 m thick in the type bore- hole (Sorgenfrei 1958). The formation is commonly only a few tens of metres thick in the north-east of the area but thickens west and south (Plates 4, 7, 9); about 130–150 m were encountered in the Borg-1 and Rømø boreholes and nearly 200 m in the Forumlund borehole (Plate 4). Lithology. The Arnum Formation consists of dark brown, silty clay with occasional shell beds. Thin laminated, fine- grained sand beds are common. The sand beds commonly display a sharp lower boundary succeeded by laminated and low-angle cross-bedded sand capped by wave lami- nated sand. Micro-hummocky cross-stratification is com- mon. Some of the wave-rippled sand beds have sharp erosive upper boundaries overlain by mud (Fig. 56A–C). Thin sand beds and silt layers may have a high content of heavy minerals; glaucony is present and locally forms discrete lamina (Fig. 56D). Log characteristics. The formation is characterised by mod- erate–high gamma-ray values (Figs 54, 55). The log pat- tern is serrated (reflecting subordinate interbedded sands) and commonly shows an overall decreasing trend upwards. Discrete gamma-ray peaks may be related to silt and sand beds rich in heavy minerals. Fossils. The Arnum Formation contains a rich assemblage of marine molluscs (Sorgenfrei 1958; L.B. Rasmussen 1961). Rich foraminifer and dinocyst assemblages also occur in this formation (Laursen & Kristoffersen 1999; Dybkjær & Piasecki 2010). Depositional environment. The Arnum Formation was deposited in a fully marine shelf environment. The water depth is unknown, but the concentration of heavy miner- als and the presence of scours and wave-rippled sand may indicate rather shallow water with frequent reworking and sorting of sediments. Boundaries. The Arnum Formation is typically bounded by sand-rich formations, the Bastrup Formation or Vandel Member beneath and the Odderup Formation, both beneath and above. In the former case, the lower boundary is defined by a sharp transition from grey and white sand of the Bastrup Formation to dark brown, silty clay of the Arnum Formation, recorded on the gamma-ray log as an abrupt increase in values. In central Jylland, the lower boundary is defined at the change from grey and white sand to grey Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 56 and white silt of the Vandel Member. In western and south- ern sections, the Bastrup Formation is absent and the clay- rich Arnum Formation succeeds silty clays of the Klintinghoved Formation (Fig. 54). This boundary may be difficult to locate but is typically placed where the consis- tently decreasing-upward gamma-ray trend of the upper- most Klintinghoved Formation is succeeded by the ‘noisy’, serrated pattern of the Arnum Formation (e.g. Fig. 54; Kvong borehole, Plate 4). The upper boundary is placed at the base of the first sig- nificant occurrence of grey fine-grained sand, commonly with a high content of heavy minerals, that is thicker than 5 m with a sand/mud ratio of at least 75%. On the gamma- ray log, the upper boundary with the Stauning Member may be difficult to recognise but is marked by a shift from ser- rated and moderate–high gamma-ray values to low–mod- erate values, albeit still serrated in nature (e.g. Stauning borehole, Plate 6). At Rømø, in the far south-west (Plate 9), the Odderup Formation is absent and the Arnum Formation is overlain by the Hodde Formation (Måde Group); the boundary is placed at the shift from consis- tent moderate–high gamma-ray values to increasing-upward values. 57 100 90 80 70 60 50 60 m.b.s. m 160 150 140 130 120 110 Cl Si F MC P Sand Cl Si F MC P Sand L o w er M io ce n e L o w er M io ce n e A rn u m F m A rn u m F m A rn u m F m O d d er u p F m St au n in g M b B as tr u p F m K lin ti n gh o ve d F m Sdr. Vium borehole DGU no. 102.948 121 120 m.b.s. 127 126 125 124 123 122 Cl Si F MC P Sand Sdr. Vium borehole DGU no. 102.948 40 cps 100 Store Vorslunde borehole DGU no. 104.2325 60 50 40 30 m.b.s. GR L o w er M io ce n e A rn u m F m O d d er u p F m B as . F m 0 cps 80 Fig. 55. The secondary reference section for the Arnum Formation is the interval from 55 to 37 m in the Store Vorslunde borehole; for legend, see Fig. 8, p. 17. Bas.: Bastrup. Fig. 54. The primary reference section of the Arnum Formation is the composite interval (132–111 m, 98–51 m) in the cored Sdr. Vium borehole; for legend, see Fig. 8, p. 17. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 57 Distribution. The formation is recognised in Jylland, south- west of a line from Struer to Horsens (Figs 1, 10F). Biostratigraphy. The Cordosphaeridium cantharellus, Exocho- sphaeridium insigne, Cousteaudinium aubryae and Labyrin- thodinium truncatum Dinocyst Zones of Dybkjær & Piasecki (2010) occur in the Arnum Formation. Geological age. The Arnum Formation is of Burdigalian to early Langhian (Early – early Middle Miocene) age. Subdivision. The Arnum Formation includes the new Vandel Member. Vandel Member new member General. The lack of exposure of this member precludes detailed description and environmental interpretation. It is defined as a discrete member of the Arnum Formation since it forms a recognisable marker interval between the coarse siliciclastics of the Bastrup Formation beneath and the mud-rich facies of the Arnum Formation above. Name. After the village of Vandel, east of Billund (Fig. 1). Type and reference sections. The type section is the inter- val from 114 to 102 m (112–102 m MD) in the Vandel Mark borehole (DGU no.115.1371; 55°42´47.99´´N, 9°10´54.82´´E; Figs 1, 57). The reference section is the interval from 100 to 97 m (100–97 m MD) in the Grindsted borehole (DGU no. 114.2038; Fig. 57). Thickness. The thickness of the member rarely exceeds the 12 m recorded in the borehole at Vandel Mark (Plate 7). Lithology. In both the Vandel and the Grinsted boreholes, log and/or cuttings data indicate a lowermost sand or gravel layer, fining upwards into mud-rich deposits. The diag- nostic feature of the Vandel Member, however, is the occur- rence of grey to white silt with a high content of heavy min- e rals; clasts of reworked reddish Eocene clay may be present. 58 Fig. 56. Slabbed core sections from the Sdr. Vium borehole showing typical lithologies of the Arnum Formation. A: Dark brown clayey silt interbedded with hummocky cross-stratified sand; 59.20 m (base of illustrated core). B: Hummocky cross-stratified sand bed bounded by dark brown silty clays; 73.40 m (base). C: Heterolithic deposits showing double clay layers (arrows); 95.60 m (base). Note the small-scale faults cutting the succession, possibly due to contemporaneous seismic activity. D: Bioturbated clay with a 1 mm lamina rich in glaucony; 125.00 m (base). 1 cm 1 cm DA GlauconyGlaucony B C 1 cm 1 cm Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 58 Log characteristics. The member shows intermediate gam- ma-ray readings overall with subordinate low values near the base (sandy beds) and localised high peaks (? heavy mineral sands). Fossils. No fossils have been recorded. Depositional environment.The depositional setting is unclear but the member caps fluvio-deltaic deposits (Resen Member) of the Bastrup Formation. The absence of fossils could point towards a floodplain depositional environment. Boundaries. The lower boundary is defined by a lithologi- cal shift from grey sand to grey and white silt as observed in borehole cuttings samples. This boundary is difficult to position on the gamma-ray log alone; a minor increase in values is observed in the type section (Fig. 57), followed by a weak increasing-upward trend. The upper boundary is placed at the top of the interval of white to grey silt. A slight, but distinct decrease in gamma-ray values is recognised at the upper boundary in the type section. Distribution. The member is recognised in central Jylland (Fig. 10F). Biostratigraphy. The Vandel Member is barren of dinocysts, but the Cordosphaeridium cantharellus Dinocyst Zone (Dybkjær & Piasecki 2010) occurs in the lithostratigraphic units below and above. Geological age. The Vandel Member is of Burdigalian (late Early Miocene) age. Odderup Formation redefined formation History. The Odderup Formation was defined by L.B. Rasmussen (1961), from the borehole at Odderup Brickworks where the succession of brown coal and quartz sand from 40.3 to 28.2 m was defined as the type section. Koch (1989) subsequently erected the Fasterholt Member and included this in the Odderup Formation. The forma- tion is redefined here, based on the more extensive subsurface database now available, to include the marine sand-dom- inated succession, commonly rich in heavy minerals, that is associated with the largely terrestrial sediments recognised in the early work. Name. After Odderup village in western Jylland (Fig. 1). Type and reference sections. Following L.B. Rasmussen (1961), the type section is the borehole at Odderup (DGU no. 103.150; 55°52´19.05´´N, 8°37´42.28´´E) from 40.3 to 28.2 m. The formation is exposed at the Abildaa Brown Coal Museum near Ørnhøj but only the brown-coal-bear- ing Fasterholt Member is present here. The primary refer- ence section is the interval from 37 to 1 m (39–1 m MD) in the borehole at Store Vorslunde (DGU no. 104.2325). The secondary reference section illustrates the alternation of the Odderup and Arnum Formations that is observed in a number of boreholes (Plates 2–9); the Odderup Formation is represented in the intervals from 118 to 110 m (118–111 m MD) and 90 to 41 m (90– 42 m MD) in the Rødding borehole (DGU no. 141.1141; Fig. 58). Thickness. The formation is c. 12 m thick at the type sec- tion and about 36 m thick in the primary reference sec- tion. In central Jylland, it commonly exceeds 40 m (Plates 2, 7) and an exceptionally thick development was recorded in the Tinglev borehole (c. 165 m; Plates 1, 9). Lithology. The formation consists of fine- to coarse-grained sand with some intercalation of clay beds and brown coal. The formation consists of quartz and clast of quartzites 59 Vandel Mark borehole DGU no. 115.1371 Grindsted borehole DGU no. 114.2038 120 110 100 90 m.b.s. GR GR 110 0 100 100 90 80 m.b.s. B as tr u p F m V an d el M b R es en M b St . M b V a. R es en M b A rn u m F m O d d . F m L o w er M io ce n e A rn u m F m B as tr u p F m L o w er M io ce n e 0 cps cps 120 Fig. 57. Type and reference sections of the Vandel Member. The type section is the interval from 114 to 102 m in the Vandel Mark borehole. The reference section is the interval from 100 to 97 m in the Grindsted borehole; for legend, see Fig. 8, p. 17. Odd.: Odderup. St.: Stauning. Va.: Vandel Mb. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 59 with minor content of mica. Heavy minerals are locally very common. The sand is characterised by low-angle cross- bedding dipping towards the south-west, and is enriched in heavy minerals (Fig. 59). The fine-grained part of the formation is dominated by hummocky cross-stratified sand and homogenous to laminated sand. The Odderup Formation is characterised by a succes- sion of sand with subordinate clay layers; the Odderup Formation is differentiated from the Arnum Formation in being sand-dominated with a sand/mud ratio of at least 75% and a minimum thickness of 5 m. Log characteristics. The formation is characterised by low to moderate gamma-ray values (Fig. 58); an overall decreas- ing-upward gamma-ray trend is typical. High gamma-ray values are associated with beds rich in heavy minerals. Fossils. Marine molluscs as well as dinocysts occur in the south-western sections of the Odderup Formation (Stauning Member; Piasecki 1980; Dybkjær & Piasecki 2010). Foraminifers reported from coarser-grained (more proxi- mal) intervals (Laursen & Kristoffersen 1999) may be the result of caving from higher strata. Fossil seeds, leaves and wood are abundant in coal beds and lacustrine sands and muds of the terrestrial Fasterholt Member. Depositional environment. The Odderup Formation was deposited in the lower to upper shoreface and swash zone of a prograding coastal-plain (Odderup Formation undif- ferentiated and Stauning Member). The coals and associ- ated sediments are the deposits of freshwater lakes, lagoonal swamps and mires (Fasterholt Member; Koch 1989). Boundaries. The lower boundary is placed where fossilifer- ous, dark brown, silty clays with subordinate, fine-grained sand layers referred to the Arnum Formation are overlain by a significant thickness (> 5 m) of grey fine-grained sand (sand: mud > 75%), commonly with a high content of heavy minerals. On the gamma-ray log, the lower bound- ary may be an abrupt shift to lower values, particularly where the Fasterholt Member directly overlies the Arnum Formation. This boundary may be more difficult to locate where the Stauning Member forms the lowermost Odderup Formation but the increase in the proportion of sand at this level is generally reflected by a fall in the gamma-ray val- ues (e.g Ulfborg borehole, Plate 5). The upper boundary is a marked change in lithology from the white, fine- to medium-grained sand of the Odderup Formation to the dark brown, clayey silt of the Hodde Formation. The boundary is typically sharp but locally is marked by a gravel layer, the base of which defines the boundary. The gamma-ray log typically shows a promi- nent shift (to higher values) at the boundary. 60 Rødding borehole DGU no. 141.1141 Store Vorslunde borehole DGU no. 104.2325 120 0 150 cps cps 110 100 90 80 70 60 50 40 30 30 40 20 10 0 m.b.s.m.b.s. GR GR O d d er u p F m A . F m Fa . L o w er M io ce n e O d d er u p F m A . F m A rn u m F m St au n in g M b St au n in g M b O d d er u p F m H o d d e Fm L o w er M io ce n e M id d le M io ce n e 0 40 80 Fig. 58. Reference sections of the Odderup Formation; for legend, see Fig. 8, p. 17. The primary reference section is the interval from 37 to 1 m in the Store Vorslunde borehole. The secondary reference section is the composite interval (118–110 m, 90–41 m) in the Rødding borehole. A.: Arnum. Fa.: Fasterholt Mb. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 60 Distribution. The Odderup Formation is distributed in west, central and southern Jylland (Fig. 10G). Biostratigraphy. The Cordosphaeridium cantharellus, Exocho- sphaeridium insigne, Cousteaudinium aubryae and Labyrin- thodinium truncatum Dinocyst Zones of Dybkjær & Piasecki (2010) occur in the marine parts of the Odderup Formation. Geological age. The Odderup Formation is of Burdigalien to early Langhian (Early to earliest Middle Miocene) age. Subdivision. The Odderup Formation includes the new Stauning Member and the Fasterholt Member (Koch 1989). Stauning Member new member History. Knudsen et al. (2005) recognised that fine-grained sand layers with a high content of heavy minerals occurred in the Arnum Formation in a number of boreholes in south and central Jylland; these sand layers were informally referred to as the ‘Stauning Sand’. On gamma-ray logs, the sand beds are characterised by extremely high gamma-ray values. Exploration for these heavy mineral sands was intensive during the latter part of the 1990s in the Stauning and Give areas. Name. After the village of Stauning (Fig. 1) where the mem- ber subcrops Quaternary deposits at relatively shallow depths. Type and reference sections. The type section of the Stauning Member is defined in the interval from 95 to 76 m (95–76 m MD) in the Vandel Mark borehole (DGU no. 115.1371; 55°42´47.99´´N, 9°10´54.82´´E; Fig. 60). The reference section is the intervals from 118 to 110 m (118–111 m MD) and 90 to 63 m (90–64 m MD) in the Rødding borehole (DGU no. 141.1141; Fig. 60). Thickness. Intervals referred to the Stauning Member com- monly range from 10 to 40 m in thickness (e.g. Plates 2, 3), but over 100 m has been found in the extreme south- ern part of the study area, for example in the Tinglev bore- hole (Plate 9). Lithology. Intervals assigned to the Stauning Member, by definition, have a sand/mud ratio of at least 75% and are more than 5 m thick. The member is typically composed of grey to white, fine-grained sand, with a high content of heavy minerals, intercalated with dark brown, clayey silt (Fig. 61). Log characteristics. The member typically shows a highly ser- rated gamma-ray log (e.g. Plate 6, Stauning borehole) although some sections show more stable low gamma-ray values (e.g. Tinglev borehole, Plate 9). Extremely high gamma-ray readings (e.g. Kvong borehole, Plate 4; Løvlund borehole, Plate 7) are found in association with concen- trations of heavy minerals. Fossils. Marine molluscs occur in the Stauning Member (Knudsen 1998) as well as foraminifers and dinocysts (Laursen & Kristoffersen 1999; Dybkjær & Piasecki 2010). 61 Fig. 59. Exposure (Isenvad gravel pit) of the Odderup Formation showing low- angle cross-bedded sand with concen- trations of dark heavy minerals; the sand was deposited in the swash zone of a beach. The height of the illustrated section is 0.4 m. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 61 Depositional environment. The Stauning Member was deposited as storm sand layers on the inner shelf, the sands being primarily of storm origin. Boundaries.The lower boundary is placed at the base of sand- dominated (>75% sand) successions at least 5 m thick, overlying the mud-rich Arnum Formation. In some wells, this boundary is marked by a general upward decrease in the background gamma-ray values (e.g. Hellevad borehole, Plate 1; Føvling borehole, Plate 3) but anomalous exam- 62 Vandel Mark borehole DGU no. 115.1371 100 90 80 70 60 50 40 30 m.b.s. Rødding borehole DGU no. 141.1141 120 0 150 110 100 90 80 70 60 50 40 m.b.s. GRGR O d d er u p F m H . O d d er u p F m O d d er u p F m O d d er u p F m St au n in g M b St au n in g M b St au n in g M b A rn u m F m A r. Fm A rn u m F m M id d le M io ce n e L o w er M io ce n e L o w er M io ce n e 0 60 cps cps 120 Fig. 60. Type and reference sections of the Stauning Member; for legend, see Fig. 8, p. 17. The type section is the interval from 95 to 76 m in the Vandel Mark Borehole. The reference section is the composite interval (118–110 m, 90–63 m) in the Rødding bore- hole. Ar.: Arnum. H.: Hodde Fm. 10 cm A B CA B C Fig. 61. Cores of the Stauning Member showing homogenous to laminated, grey sand with some intercalated dark brown muds. Note the high content of shells in C (arrows), especially in the lower part of the sand beds. A: 15.72 m (base of illustrated core); B: 23.73 m (base); C: 26.94 m (base). Cores from a shallow borehole to investigate the heavy mineral potential of Stauning Member sands; 2 km due west of Skjern. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 62 ples are also observed (e.g. Rødding borehole, Fig. 60), possibly due to the heavy mineral content of the sands. The upper boundary is defined where the fine-grained sand-rich succession is overlain by dark brown, silty clay of the Arnum Formation or medium- to coarse-grained sand of the Odderup Formation. Where the Odderup Formation succeeds the Stauning Member, the upper bound- ary is commonly reflected by a shift from a dominantly ser- rated gamma-ray log pattern to a steady and gradually decreasing gamma-ray log pattern (e.g. Plates 1, 2). Distribution. The Stauning Member is found in southern, central and western Jylland (Fig. 10G). Biostratigraphy. The Cordosphaeridium cantharellus, Exocho sphaeridium insigne, Cousteaudinium aubryae and Labyrin- thodinium truncatum Dinocyst Zones of Dybkjær & Piasecki (2010) are recognised in the Stauning Member. Geological age. The Stauning Member is of Burdigalian to early Langhian (Early to earliest Middle Miocene) age. Fasterholt Member History. The Fasterholt Member was defined by Koch (1989). Brown-coal-bearing layers were mentioned by Forchhammer (1835) and brown-coal beds that crop out in the banks of the Skjern Å (river) were reported by Dalgas (1868) and Hartz (1909). Extensive mining of brown coal occurred during the two world wars and large prospecting programs were carried out in connection with the demands for local energy resources (Milthers 1939; Milthers 1949). Name. After the village of Fasterholt (Fig. 1). Type and reference sections.The formation has previously been exposed in several brown-coal pits in central and western Jylland and the Fasterholt brown-coal pit (56°00´52.60´´N, 9°06´16.05´´E) is the type locality of Koch (1989; Figs 1, 62). The member is only exposed today in a small pit at Abildå near Ørnhøj (Fig. 1). The reference section is defined in the Store Vorslunde borehole (DGU no. 104.2325) from 15 to 13 m (15–13 m MD; Fig. 62). Thickness. The member is c. 8.5 m thick in the type sec- tion and is commonly about 10 m thick elsewhere in cen- tral Jylland (Plate 2). It is not recognised in south-west Jylland (Fig. 10G). Lithology. The Fasterholt Member consists of interbedded sands, clays and brown coals. In the type section, it con- sists of three sedimentary units, each typically showing a fining-upward trend from a basal sandy lower part passing upward into silty clay and capped by a brown-coal layer (Fig. 62). Fossils. Marine fossils are absent but spores and pollen, fos- sil seeds, leaves and wood occur abundantly (Christensen 1975, 1976; Friis 1975, 1979; Koch 1977, 1989; Koch & Friedrich 1970; Koch et al. 1973; Wagner & Koch 1974). Depositional environment. The member is interpreted to represent deposition in a terrestrial setting that included lacustrine and mire environments (Koch 1989). The con- 63 Fig. 62. Type and reference sections of the Fasterholt Member; for legend, see Fig. 8, p. 17. The type section is the Fasterholt Brown Coal Pit, north-west of Brande; this section is no longer exposed. The log is redrawn from Koch (1989). The reference section is the interval from 15 to 13 m in the Store Vorslunde borehole. A.: Arnum Fm. Fa.: Fasterholt Mb. Fasterholt outcrop 0 1 2 3 4 5 6 7 8 9 10 Cl Si F MC P Sand Store Vorslunde borehole DGU no. 104.2325 40 30 20 10 0 m.b.s.m GR O d d er u p F m L o w er t o M id d le M io ce n e Fa st er h o lt M b O d d e ru p F m A . L o w er t o M id d le M io ce n e F a. 0 40 cps 80 Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 63 centration of brown coals in the depocentre of the Norwegian–Danish Basin, particularly adjacent to pre- existing faults indicates a structural control on the deposi- tion. Boundaries. The lower boundary is sharp, being placed where white sands are overlain by a succession dominated by silty clay and brown coal, with intercalated sands. The lower boundary may be marked by a dense root horizon with tree stumps. On the gamma-ray log, the boundary is characterised by a prominent shift towards high gamma- ray values. The upper boundary is also sharp, being typically marked by the incoming of the sand-rich upper part of the Odderup Formation; this lithological change is indicated on the gamma-ray log by a distinct shift to lower readings. Where overlain by clay-rich sediments of the Arnum Formation (e.g. Vind borehole, Plate 4) or the Hodde Formation (e.g. Fjelstervang borehole, Plate 3), the gamma-log values show an abrupt increase. Distribution. The Fasterholt Member is restricted to cen- tral Jylland (Fig. 10G). Biostratigraphy. In the absence of marine fossils, the Faster- holt Member is stratigraphically constrained by the pres- ence of the C. aubryae Dinocyst Zone below (in the marine Odderup or Arnum Formations) and the L. truncatum Dinocyst Zone above (in the overlying Arnum Formation) (Dybkjær & Piasecki 2010). Geological age. Due to the absence of marine fossils, the Fasterholt Member is dated indirectly by the biostratigra- phy of the under- and overlying marine strata. The age of the Fasterholt Member is thus constrained to Burdigalian to early Langhian (Early to earliest Middle Miocene). 64 Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 64 History.The succession defined here as the Måde Group was referred by L.B. Rasmussen (1961) to the ‘Måde serien’; this encompassed the marine, clay-dominated younger Miocene deposits. As described by L.B. Rasmussen (1961), the suc- cession is characterised by a basal gravel layer which is over- lain by black, mica-rich mud followed by a thin green ish, glaucony-rich clay, grey clay and finally by fine- to medium- grained sand. Relative to the North Sea litho stratigraphy, the Måde Group correlates with the Nordland Group (Deegan & Scull 1977; Hardt et al. 1989; Schiøler et al. 2007). Name. After a local area west of Esbjerg (Fig. 1) that was renowned for its brickworks based on Upper Miocene clays; the last brick factories were closed in the 1970s. Type area. The type area of the Måde Group is south-west Jylland. The group is exposed at the Gram clay-pit (Fig. 1) where both the Gram and Marbæk Formations can be seen. At Ørnhøj (Lille Spåbæk), the Hodde and Ørnhøj For- mations are exposed and the Marbæk Formation crops out in coastal cliffs at Sjelborg and Marbæk, north-west of Esbjerg (Fig. 1). The full development of the group is illus- trated by the cored borehole Sdr. Vium (DGU no. 102.948; 51–24 m, Fig. 63) and the Tinglev borehole (DGU no. 168.1378) from 197 to 50 m (197– 49 m MD; Fig. 63). Thickness. The group is typically about 25 m thick in the western part of Jylland, but in southernmost Jylland, for example in the Tinglev borehole, nearly 150 m has been penetrated (Fig. 63; Plate 9). Lithology. The Måde Group is dominated by dark brown, organic-rich mud (Fig. 64). The lower part is composed of alternating fine-grained sand and silty clay with a basal gravel layer (Hodde Formation). Upwards, the succession becomes more fine-grained with scattered incursions of glaucony. This is succeeded by greenish brown, glaucony- rich clay, typically 3 m thick (Ørnhøj Formation). In the upper part of the glaucony-rich section, goethification of glaucony grains is common (Dinesen 1976). This is over- lain by a succession of brown clays rich in pyrite that becomes siltier upwards with thin (c. 5 cm thick), fine- grained storm sand beds occurring in the upper part. The uppermost Måde Group consists of fine- to medium- grained sand. Log characteristics. The group is characterised by moderate to high gamma-ray readings (Fig. 63). Extremely high gamma-ray values may be recorded in the lower levels of the group, the upper part showing a gradual decrease in gamma-ray readings (see Fig. 63). 65 Måde Group new group Sdr. Vium borehole DGU no. 102.948 60 50 40 30 m.b.s. Tinglev borehole DGU no. 168.1378 200 0 800 cps 190 180 170 160 150 140 130 120 110 100 90 80 70 60 50 m.b.s. GRGR M åd e G ro u p R ib e G ro u p A rn u m F m H o d . F m Ø . F m G ra m F m M id d le M io ce n e U p p er M io ce n e L . M io . M id d le M io ce n e U p p er M io ce n e M åd e G ro u p R ib e G rp O d d er u p F m H o d d e Fm * G ra m F m M ar b æ k Fm 20 cps 140 Fig. 63. The full development of the Måde Group is illustrated by the interval from 51 to 24 m in the cored Sdr. Vium borehole and the interval from 197 to 50 m in the Tinglev borehole; for legend, see Fig. 8, p. 17. Hod.: Hodde. L. Mio.: Lower Miocene. Ø and *: Ørnhøj Fm. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 65 Fossils. The Måde Group contains rich and diverse mollusc faunas, crustaceans and vertebrates. Shark teeth are com- mon. Foraminifers and dinocysts are abundant (see details below in the description of the individual formations). Depositional environment. The Måde Group was deposited on a marine shelf. When the flooding of the land was at its maximum, during the deposition of the glaucony-rich Ørnhøj Formation and the lower part of the Gram Formation, the water depth was over 100 m (Laursen & Kristoffersen 1999). The upper part of the group was deposited in front of a prograding coastline in an offshore to shoreface setting. Boundaries. The lower boundary is sharp, being marked by a thin gravel layer separating the white, fine-grained sand of the Ribe Group from the dark brown mud of the Måde Group. The upper boundary is a sharp erosional bound- ary separating mud and fine-grained sand of the Måde Group from Quaternary deposits, the boundary commonly being characterised by a distinct change in lithology and colour of the deposits. Distribution. The Måde Group is restricted to the western and southern part of Jylland (Fig. 10H) and is found locally around Herning and in the Brande–Give area (Fig. 1). Geological age. The Måde Group is of early Langhian to lat- est Tortonian (early Middle to Late Miocene) age. Subdivision. The Måde Group is divided into four forma- tions: the Hodde, Ørnhøj, Gram and Marbæk Formations. Hodde Formation History. The Hodde Formation was defined by L.B. Rasmussen (1961) from the Hodde-1 borehole; it was exposed during the construction (1941–43) of the 66 Fig. 65. Reference sections of the Hodde Formation; for legend, see Fig. 8, p. 17. The primary reference section is the interval from 51 to 44.9 m in the cored Sdr. Vium borehole. The secondary reference section is the interval from 50 to 39 m in the Føvling borehole. G.: Gram Fm. Hod.: Hodde. L. Mio.: Lower Miocene. U.: Upper Miocene. Ør. and Ørn.: Ørnhøj. Sdr. Vium borehole DGU no. 102.948 60 60 cps 100 50 40 30 m.b.s. Føvling borehole DGU no. 132.1835 60 60 180 cps 50 40 m.b.s. GRGR M id d le M io ce n e U p p er M io ce n e Ø rn . F m G ra m F m H o d . F m A rn u m F m M id d le M io ce n e U . L . M io . H o d d e Fm Ø r. Fm G . O d d er u p F m Marine Middle–Upper Miocene deposits (Måde Group) Continental lower Middle Miocene deposits (Ribe Group) Continental lower Middle Miocene deposits (Ribe Group) Fig. 64. The open pit at Lille Spåbæk, Ørnhøj (Fig. 1) where the Hodde, Ørnhøj and Gram Formations were exposed in the late 1970s. These three formations, togeth- er with the Marbæk Formation, constitute the Måde Group. The cliff is c. 10 m high. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 66 Karlsgårde channel, near Hodde, but this exposure does not exist today. Name. After the village of Hodde in south-west Jylland (Fig. 1). Type and reference sections. The type section was defined by L.B. Rasmussen (1961) as the interval from 23.4 to 13.8 m in the Hodde-1 borehole (DGU no. 113.33; 55°41´04.11´´N, 8°40´14.27´´E). The formation is exposed at Lille Spåbæk near Ørnhøj, south of Holstebro (Fig. 1). The primary reference section is the interval from 51 to 44.90 m in the cored borehole at Sdr. Vium (DGU no. 102.948; Fig. 65). A secondary reference section is the Føvling borehole (DGU no. 132.1835) from 50 to 39 m (Fig. 65). Thickness. The formation is 9.6 m thick (23.4–13.8 m) in the type section and is typically 5–10 m thick where pre- sent, but thickens in southernmost Jylland; more than 40 m was penetrated in the Rømø borehole (Plate 9). Lithology. The Hodde Formation consists of dark brown, organic-rich, bioturbated silty clay with thin sand lenses (Figs 66, 67); the pyrite content is high. The basal part of the formation is composed of a thin gravel layer. In the upper part of the formation, laminated, silty clay is common and glaucony may occur. Trace fossils are common in the Hodde Formation (Asgaard & Bromley 1974). Log characteristics. The formation is typified by moderate to high gamma-ray values (Fig. 65); a gradual upward increase in gamma-ray response is characteristic. Locally, the upper part shows low gamma-ray readings, for exam- ple in the Føvling borehole (Plate 8). Fossils. The Hodde Formation typically contains a limited fauna of marine molluscs (L.B. Rasmussen 1966) but a 67 Fig. 66. The upper part of the Hodde Formation at Lille Spåbæk, Ørnhøj, dominated by dark brown silty clay. Fig. 67. Close-up of the Hodde Formation at Lille Spåbæk, Ørnhøj. The Hodde Formation is composed of dark brown silty clay; the yellowish stripes are due to weathering of pyrite. The illustrated section is 0.5 m high. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 67 richer fauna occurs locally in shell-beds associated with the basal gravel bed. Marine microfossils, such as foraminifers and dinocysts, occur abundantly (Laursen & Kristoffersen 1999; Piasecki 1980, 2005; Dybkjær & Piasecki 2010). Depositional environment. The depositional environment is interpreted as fully marine (L.B. Rasmussen 1961). The basal coarse-grained transgressive lag indicates deposition on a marine shoreface during the initial transgressive phase. The increase in glaucony in the upper part indicates a near ces- sation of sediment influx to this part of the North Sea in the Serravallian. Boundaries. There is a marked change in lithology from the white, fine- to medium-grained sand of the Odderup Formation to the overlying dark brown, clayey silt of the Hodde Formation. The boundary is sharp and is commonly characterised by a gravel layer, the base of which (where present) defines the boundary. The gamma-ray log shows a prominent shift to high values at the lower boundary. The upper boundary is defined by an abrupt change from dark brown, clayey silt of the Hodde Formation to greenish brown clay of the Ørnhøj Formation. On the gamma-ray log, this is reflected by a distinct shift towards higher gamma-ray values. Distribution. The Hodde Formation is recognised in south- ern and western Jylland (Fig. 10H). The formation occurs locally as far east as Bording and Give in central Jylland in depressions associated with salt structures. Biostratigraphy. The upper part of the Labyrinthodinium truncatum Dinocyst Zone and the Unipontidinium aquae- ductum Dinocyst Zone (Dybkjær & Piasecki 2010) are recorded in the Hodde Formation. Geological age. The Hodde Formation is of early Langhian to mid-Serravallian (Middle Miocene) age. Ørnhøj Formation new formation History. Formerly referred to as the ‘Glauconitic Clay mem- ber’ of the lower Gram Formation of previous usage (L.B. Rasmussen 1956, 1961). Name. After the village of Ørnhøj (Fig. 1) where the for- mation is still exposed in some of the old brown-coal pits in the neighbourhood. Type and reference sections. The formation is partly exposed at Lille Spåbæk, west of Ørnhøj (Figs 1, 64). The type sec- tion is the interval from 44.90 to 40 m in the cored bore- hole at Sdr. Vium (DGU no. 102.948; 55°49´04.02´´N, 8°24´46.52´´E; Fig. 68). The reference section is the inter- 68 Fig. 68. The type and reference sections of the Ørnhøj Formation; for legend, see Fig. 8, p. 17. The type section is the interval from 44.9 to 40 m in the cored Sdr. Vium borehole. The reference section is the interval from 39 to 36 m in the Føvling borehole. G: Gram Fm. Ho.: Hodde. L. Mio.: Lower Miocene. M.: Middle. Odd.: Odderup. Ø.: Ørnhøj Fm. *: Upper Miocene. Føvling borehole DGU no. 132.1835 Sdr. Vium borehole DGU no. 102.948 60 60 cps 240 50 40 30 20 10 0 m.b.s. GR m.b.s. GR 45 120 cps 160 44 43 42 41 40 39 38 Glaucony Cl Si F MC P Sand Ø rn h ø j Fm Ø . G H o . F m O d d . F m G ra m F m M id d le M io ce n e M . M io ce n e * Q u at er n ar y L . M io . U p p er M io ce n e Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 68 val from 39 to 36 m (39–36 m MD) in the Føvling bore- hole (DGU no. 132.1835; Fig. 68). Thickness. The formation is 4–5 m thick in the type and reference boreholes, but in general it rarely exceeds more than 2 m in thickness (Plates 4, 8, 9). Lithology. The Ørnhøj Formation is composed of green and brown clay (Fig. 69). High concentrations of green glaucony pellets of fine sand grade occur commonly. In the upper part of the formation, goethification of glau- cony is common. Log characteristics. The formation is characterised by high gamma-ray values. Fossils. The Ørnhøj Formation is barren of macro- and microscopic calcareous fossils but a diverse assemblage of dinocysts is present (Piasecki 1980, 2005; Dybkjær & Piasecki 2010). Depositional environment. The Ørnhøj Formation was deposited in a fully marine, sediment-starved depositional setting that favoured the formation of glaucony. The water depth was probably more than 100 m, based on the esti- mates of water depth during deposition of the Gram Formation (see below). The Ørnhøj Formation represents the most widespread transgression during the Miocene (E.S. Rasmussen 2004b; Knox et al. 2010). The goethifi- cation of glaucony in the upper part is interpreted as a result of a sea-level fall (Dinesen 1976; Eder et al. 2007) with associated wave action at the sea floor. Concentration of glaucony in depositional bars at Ørnhøj (J. Frederiksen, personal communication 2009) supports the interpreta- tion of wave action at the sea floor. Boundaries. The lower boundary is characterised by an abrupt change from the dark brown, clayey silts of the Hodde Formation to greenish brown clays of the Ørnhøj Formation (Fig. 69). The gamma-ray log shows a promi- nent shift in gamma-ray response towards high values. The upper boundary is defined by the change from greenish brown or brown, glaucony-rich clay to dark brown clay. At the boundary there is an abrupt change from glau- cony-impregnated pellets and shells to pyritised pellets. On the gamma-ray log, the upper boundary is defined at a decrease in gamma-ray values; locally a very prominent decrease is observed, for example in the Stensig borehole (Plate 4). Distribution. The Ørnhøj Formation is recognised in south- ern and western Jylland. The formation is locally recog- nised in the subsurface as far east as Bording and Give in central Jylland, where it occurs in depressions associated with salt structures (Fig. 10H). Biostratigraphy. The Achomosphaera andalousiense and Gramo- cysta verricula Dinocyst Zones of Dybkjær & Piasecki (2010) are recorded in the Ørnhøj Formation. Geological age. The Ørnhøj Formation is of late Serravallian (late Middle Miocene) age. 69 Ørnhøj Fm Hodde Fm Ørnhøj Fm Hodde Fm Fig. 69. The Ørnhøj Formation at Lille Spåbæk, Ørnhøj. The lower boundary with the Hodde Formation beneath is seen in the lower part of the section. Knife for scale, c. 20 cm long. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 69 Gram Formation redefined formation History. The Gram Formation was defined by L.B. Rasmussen (1956). In the original definition of the Gram Formation, three members were recognised: the Glauconite Clay, Gram Clay and Gram Sand members (L.B. Rasmussen 1956). The Glauconite Clay member of previous usage is herein redefined as the new Ørnhøj Formation and the Gram Sand member as the Marbæk Formation; the rede- fined Gram Formation thus equates to the Gram Clay member of L.B. Rasmussen (1956). Name. After the town of Gram (Fig. 1). Type and reference sections. The type section is at the dis- used pit of the Gram brickworks (55°18´24.90´´N, 9°03´31.26´´E; Fig. 1), now the Midtsønderjyllands Museum of Gram, where a 13.1 m thick section of the Gram Formation is exposed (Figs 70, 71). The reference section is the interval from 40 to 24 m in the cored bore- hole Sdr. Vium (DGU no. 102.948; Fig. 71). Thickness. A 13.1 m section is seen at the type section, but neither the base nor the top is exposed. In the reference section, the formation is about 16 m thick. The formation thickens south-westward and 105 m was penetrated in the Tinglev borehole (Plate 1). Lithology. The Gram Formation consists of dark brown clay, which becomes more silty upwards. In the upper part, a few, fine-grained, wave-rippled sand beds, c. 5 cm thick, are intercalated with the clays (Figs 70, 71). Siderite con- cretions are common in the lower part of the formation. Pyrite is common both as pyritised pellets and in trace fos- sils; the latter include common Trichichnus ispp. (Rasmussen & Larsen 1989; Bromley 1996). Log characteristics. The formation is characterised by mod- erate gamma-ray values (Fig. 71). The log pattern is ser- rated and shows a general decreasing-upward trend in gamma-ray values through the succession (Fig. 63). Fossils. The Gram Formation is characterised by abundant and diverse mollusc faunas, in association with marine ver- tebrates (whales and sharks) and crustaceans (crabs), the lat- ter in concretionary nodules (L.B. Rasmussen 1966, 1968; Bendix-Almgreen 1983; Hoch 2008; Schnetler 2005; Steeman, 2009). Foraminifers and dinocysts are abundant (Laursen & Kristoffersen 1999; Piasecki 1980, 2005). Depositional environment. The Gram Formation was deposited in a fully marine environment with water depths of more than 100 m (Laursen & Kristoffersen 1999; C. Morigi, personal communication 2010). The incoming of storm beds in the upper part is interpreted to reflect progra- dation of the shoreline (Rasmussen & Larsen 1989). Boundaries. The lower boundary is defined at the change from greenish brown or brown, glaucony-rich clay to dark brown clay, associated with an abrupt change from glau- cony-impregnated pellets and shells to pyritised pellets. On the gamma-ray log, this is reflected by a decrease in gamma-ray values. 70 Fig. 70. Fine-grained, partly bioturbated sand interbeds in the upper part of the Gram Formation, Gram clay pit. The sand beds are commonly wave-rippled. The illustrated section is 0.30 m high. Facing page: Fig. 71. Type and reference sections of the Gram Formation; for legend, see Fig. 8, p. 17. The type section is at the Gram clay pit near Gram, where 13.1 m of the forma- tion is exposed. The reference section is the interval from 40 to 24 m in the cored Sdr. Vium borehole. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 70 71 U p p er M io ce n e G ra m F m U p p er M io ce n e G ra m F m Ø rn h ø j Fm U p p er M io ce n e U p p er M io ce n e U p p er M io ce n e M ar b æ k Fm G ra m F m G ra m F m 0 1 2 3 4 5 6 7 8 9 10 m m.b.s. GR 11 10 12 13 1 2 41 40 39 38 37 36 35 34 33 32 31 30 31 80 100 cps 29 28 27 26 25 24 Cl Si F MC P Sand Cl Si F MC P Sand Cl Si F MC P Sand 110 140 cps Cl Si F MC P Sand Gram outcrop Sdr. Vium borehole DGU no. 102.948 Covered interval (< 2m) 0 Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 71 72 The upper boundary is placed where interbedded clay and thin sand layers are succeeded by amalgamated sand beds. On the gamma-ray log, the upper boundary is identi- fied by a marked shift to consistently low gamma-ray values. Distribution. The Gram Formation is recognised in the subsurface of southern and western Jylland (Fig. 10H). The formation occurs locally as far east as Bording and Give in central Jylland in depressions associated with salt structures. Biostratigraphy. The Amiculasphaera umbracula and Hystri- chosphaeropsis obscura Dinocyst Zones of Dybkjær & Piasecki (2010) are recorded in the Gram Formation. Geological age. The Gram Formation is of Tortonian (Late Miocene) age. Marbæk Formation new formation History. Sands exposed in the cliffs at Sjelborg and Marbæk, north-west of Esbjerg (Fig. 1), and sandy sediments in the upper part of the Sæd borehole (DGU no. 167.445) were tentatively referred to the Pliocene by Jørgensen (1945). New studies of these sections (Piasecki et al. 2003), however, indicated that these deposits are Tortonian in age. The sand was informally named the Gram Sand member (Gram Formation of previous usage) by L.B. Rasmussen (1956). Name. After the coastal cliff at Marbæk, north-west of Esbjerg (Fig. 1). Type and reference sections. The type section is the exposure at Marbæk cliff (55°32´56.49´´N, 8°18´57.49´´E; Figs 1, 72). The reference section is the interval from 62 to 50 m (62–49 m MD) in the Tinglev borehole (DGU no.168.1378; Fig. 73). Thickness. The Marbæk Formation is c. 16 m thick in the Marbæk cliff (Fig. 72); neither the base nor the top is exposed. In the pit at the Gram brickworks, 1.5 m of the formation is exposed in the bank of a stream (Fig. 71). In Marbæk outcrop 0 1 2 3 4 5 6 7 8 9 10 10 11 12 13 14 15 Cl Si F MC P Sand Cl Si F MC P Sand ? ? ? ? ? m U p p er M io ce n e M ar b æ k Fm U p p er M io ce n e M ar b æ k Fm Fig. 72. Type section of the Marbæk Formation in the coastal cliff at Marbæk, north-west of Esbjerg, where c. 16 m of the formation are exposed; for legend, see Fig. 8, p. 17. Iron-stained fractures are conspicuous at 7–9 m in this section. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 72 73 the Tinglev borehole, the formation is 10 m thick (Fig. 73, Plate 1), though the top is an unconformity with Quaternary sediments. Lithology. In the type section, the formation is dominated by white, often reddish, fine- to medium-grained, mica-rich sand with a few thin intercalated coarse-grained sand or gravel layers and, in the lower part, subordinate silt-rich intervals (Figs 72, 74). The sand beds show parallel lami- nation with subordinate cross-bedding; hummocky cross- stratification is common (Fig. 75). A silt-rich interval shows double clay layers. The uppermost white sand at Sjelborg consists of homogenous sand capped by wave-ripples (Fig. 76). The pyrite content is very high in the Marbæk For- mation (Olivarius 2009) and the distinctive red colour of the succession at the Marbæk outcrop is due to oxidation of the pyrite. Fossils. Rare, poorly preserved molluscs have been found in the Marbæk Formation (Jørgensen 1945). Dinocysts occur in the lower part of the formation but become scarce upwards (Piasecki et al. 2003). Depositional environment. The formation was deposited in a storm-dominated environment within the upper and Tinglev borehole DGU no. 168.1378 90 80 70 60 50 m.b.s. GR U p p e r M io ce n e M ar b æ k F m G ra m F m 0 800 cps Fig. 73. Reference section for the Marbæk Formation is the inter- val from 62 to 50 m in the Tinglev borehole; for legend, see Fig. 8, p. 17. Fig. 74. Oblique view of the Marbæk Formation at Marbæk, north-west of Esbjerg. Two persons (upper right) for scale. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 73 74 lower shoreface. Double clay layers indicate some tidal influence. Boundaries. The lower boundary is defined where alter- nating thin clay and sand layers are overlain by amalgamated sand beds; this boundary is not observed at outcrop. On the gamma-ray log, this boundary is identified by a marked shift to steady low gamma-ray values. The upper boundary is placed at a distinct, erosional unconformity separating the mica-rich sands from tills and yellowish, coarse-grained sands and gravels of Quaternary age. Distribution. The formation is limited to the far west and south of Jylland. Biostratigraphy. The Hystrichosphaeropsis obscura Dinocyst Zone of Dybkjær & Piasecki (2010) is recorded in the lower part of the Marbæk Formation. Geological age. The lower part of the Marbæk Formation is of Tortonian (Late Miocene) age, equivalent to the upper- most part of the Gram Formation. The absence of fossils in the upper levels of the formation precludes precise dat- ing of this part. Fig. 75. Hummocky cross-stratified sand of the Marbæk Formation at Marbæk; the illustrated section is 50 cm high. Fig. 76. Although deformed by glacial tectonics, the Marbæk Formation sands display homogenous and wave-rippled facies typical of upper shoreface deposits. The illustrated section is 0.4 m high; Sjelborg. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 74 75 The overall stratigraphic architecture of the Miocene suc- cession is best revealed by integration of seismic data with outcrop and borehole data. Thus, in the grid of correla- tion panels presented here (Plates 1–9), the borehole and outcrop data provide the critical, stratigraphic constraints whilst the sedimentary architecture between wells is based in large part on the seismic data. Inspection of seismic sections (Figs 77–79) reveals that the lower part of the Miocene succession is composed of two discrete, progradational successions (Fig. 77). The first succession includes the Vejle Fjord and Billund Formations and the second succession includes the Klintinghoved and Bastrup Formations. These packages are often characterised by a seismic reflection pattern that shows both oblique–par- allel and sigmoidal clinoforms. The height of clinoforms ranges between 60 m and 100 m, and dips of the clino- forms commonly vary between 3° and 10° (Fig. 77). Clinoformal packages may alternate with units of more or less transparent seismic character (Fig. 78). This part of the succession is interpreted to represent prograding delta lobes with alternating sand-rich and mud-rich units (E.S. Rasmussen et al. 2007; Hansen & Rasmussen 2008; E.S. Rasmussen 2009b; Fig. 80, Plates 1–9). On top of each pro- grading unit, erosional valleys and channels occur and some channels are characterised by having a shingled reflection pattern (E.S. Rasmusssen 2009b). These features were formed by incision and are commonly filled with sand. The shingled reflection pattern is interpreted to represent point bars of meandering river systems (E.S. Rasmussen et al. 2007; E.S. Rasmussen 2009b). In between these delta lobes, seismic reflectors are parallel, commonly of low amplitude (Fig. 78); this seismic character is considered to reflect the presence of mud-dominated inter-lobe deposits (Hansen & Rasmussen 2008). In northern and central Jylland, a successive southward migration of delta lobes can be demonstrated (e.g. Plate 2), defining an ascending shoreline trajectory (Fig. 78) indicating progradation dur- ing rising sea level (e.g. Helland-Hansen & Gjelberg 1994). In the northern part of the study area, the Lower Miocene is dominated by a parallel to subparallel reflection pattern capping the clinoforms (Fig. 79). Boreholes penetrating this part of the succession indicate alternating mud- and sand-rich units (Fig. 79). Gravel pits and outcrops around Silkeborg indicate a dominance of braided fluvial systems Stratigraphic architecture 0 100 200 T W T ( m se c) 300 (offset 4 km) NorthSouth Store Vorslunde BillundAlmstok 2 km 5 0 m Top delta lobe Top Bastrup Top Billund/Vejle Intra Odderup Base Miocene Internal reflector/surface Clinoforms Incised valleys Base Quaternary Bastrup Delta complexBastrup Delta complex Resen MbResen Mb Addit MbAddit Mb Arnum FmArnum Fm Arnum Fm Arnum Fm Arnum FmArnum Fm Arnum Fm Billund Delta complexBillund Delta complex Odderup coastal plain Odderup coastal plain Odderup FmOdderup Fm Vejle Fjord FmVejle Fjord Fm Vejle Fjord Fm Vejle Fjord Fm Klinting- hoved Fm Klinting- hoved Fm Fig. 77. S–N-trending seismic section tieing the Almstok, Billund and Store Vorslunde boreholes (for location, see Fig. 1). Sand-rich delta lobes characterised by an oblique–parallel reflection pattern are indicated in yellow. Note the alternation of these sand-rich delta deposits and more clay-rich inter-lobe deposits, a characteristic feature of the Vejle Fjord–Billund Formations and the Klintinghoved–Bastrup Formations. The upper part of the section is dominated by a parallel to subparallel reflection pattern which is characteristic of the Arnum–Odderup Formations and indicates a change in sedimentation style. Seismic data courtesy of COWI a/s. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 75 76 100 200 300 400 500 Hammerum 200 150 100 50 0 Isenvad (Offset 300 m) 150 100 50 Billund Fm BillundFmAddit Mb Addit Mb Klintinghoved Fm Resen MbResen Mb Billund Fm BillundFm Vejle Fjord Fm Vejle Fjord Fm Addit Mb Addit Mb Klintinghoved Fm Resen MbResen Mb Odderup FmOdderup Fm Bastrup FmBastrup Fm EastWest 1 km T W T ( m se c) 1 km Resen Mb Bastrup Fm Delta lobe Delta lobe Billund Fm Resen Mb Bastrup Fm Delta lobe Delta lobeDelta lobe Billund FmBillund Fm Addit MbAddit Mb Addit MbAddit Mb Delta lobe Billund Fm Vejle Fjord FmVejle Fjord Fm NorthSouth 5 0 m Klinting- hoved Fm Klinting- hoved Fm Fig. 79. W–E-striking seismic section at Ikast (for location, see Fig. 1). The section shows a cross-section of the Billund and Bastrup delta systems as indicated by dipping reflectors both towards the west and east. In this area, the fluvial systems of the Addit and Resen Members, shown in red, are particularly well developed. Seismic courtesy of Rambøll a/s; for legend, see Fig. 77). Fig. 78. Detailed seismic section of the Store Vorslunde area (for location, see Fig. 1). Sand-rich parts of the deltas are indicated in yellow, sand-rich fluvial deposits of the Addit and Resen Members are shown in red. Seismic data courtesy of COWI a/s; for legend see Fig. 77. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 76 77 in this area (Hansen 1985; Hansen 1995; Jesse 1995; E.S. Rasmussen et al. 2007), and based on subsurface data such braided fluvial systems dominated in northern Jylland and parts of central Jylland from Addit to Hammerum (Plate 6). In a narrow NW–SE-striking belt across central Jylland, the seismic data show an oblique–parallel reflection pattern. This represents progradation during falling sea level (Hansen & 2008, E.S. Rasmussen 2009b). In southern Jylland, there is a tendency towards a combined aggradational– progradational stacking pattern (Plate 1), reflecting progra- dation during rising sea level. Above these two progradational units of the Billund/Vejle Fjord system and the Klintinghoved/Bastrup system (i.e. above the top Bastrup reflector in Figs 77–79), a parallel to subparallel reflection pattern dominates the Miocene succession (Fig. 77); this correlates with the Arnum and Odderup Formations. The change in seismic character indicates a change in depositional environment from pro- grading ‘Gilbert-type’ deltas to aggrading shelf and coastal plain deposits. This is illustrated on correlation panels by progressive outbuilding of the Odderup Formation towards the south-west contemporaneously with the accumulation of the marine Arnum Formation (Fig. 80; Plate 4). Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 77 78 78 Billund DGU no. 114.1857 Estrup DGU no. 132.1838 Vorbasse DGU no. 123.1167 Rødding DGU no. 141.1141 Almstok DGU no. 114.1858 Sto DG Løgumkloster DGU no. 159.739 Odderup Fm Arnum Fm Arnum Fm Arnum Fm Bastrup Fm Bastrup Fm Billund Fm Odderup Fm Odderup Fm Arnum Fm Vejle Fjord Fm Klintinghoved Fm Brejning Fm Stauning Mb Stauning Mb Stauning Mb Stauning Mb Vandel Mb Stauning Mb Stauning Mb Resen MbResen Mb Resen Resen MbBastrup Fm Hodde Fm Ørnhøj FmGram Fm Odderup Fm Addit Mb Addit Mb Billund Fm Klintinghoved Fm Fasterholt Mb Resen Mb Resen Mb Resen Mb Arnum Fm Bastrup Fm Bastrup Fm Bastrup Fm Billund Fm Vejle Fjord Fm Klintinghoved Fm Isenvad DGU no. 86.2056 A D Stauning DGU no. 93.1125 B West Assing Mølleby DGU no. 94.2821 Arnum Fm Bastrup Fm Bastrup Fm Arnum Fm Billund Fm Vejle Fjord Fm Stauning Mb Kolding Fjord Mb Gram Fm Hodde Fm Ørnhøj Fm Stensig DGU no. 93.1062 Hammerum DGU no. 85.2429 Hjøllund DGU no. 86.2118 50 m ? A South B A Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 78 79 Resen DGU no. 65.1643 Sunds DGU no. 85.2452 Billund DGU no. 114.1857 Almstok DGU no. 114.1858 Store Vorslunde DGU no. 104.2325 Hammerum DGU no. 85.2429 Fasterholt DGU no. 95.2730 Klyngholt Bastrup Fm Bastrup Fm Billund Fm Billund Fm Billund Fm Brejning Fm Vejle Fjord Fm Odderup Fm Odderup FmOdderup Fm Arnum Fm Stauning Mb el Mb Stauning Mb Stauning Mb n Mb Resen Mb Resen Mb Resen Mb Addit Mb Fasterholt Mb Fasterholt Mb Hodde Fm Ørnhøj Fm Gram Fm Addit Mb Billund Fm Billund Fm Billund FmBillund Fm hoved Fm Vejle Fjord Fm Arnum Fm Vejle Fjord Fm Isenvad DGU no. 86.2056 Addit Mark DGU no. 97.928 Addit gravel pit DGU no. 97.1000 Morsholt DGU no. 108.148 East Hjøllund DGU no. 86.2118 Brejning Fm Depositional environments Sand (marine) Sand/gravel (continental) Clay (marine) Clay (lagoonal) Clay (continental) Coal 50 m Base Quaternary Top Bastrup Fm / Klintinghoved Fm Top Billund Fm / Vejle Fjord Fm Main boundaries Top Brejning Fm Top Paleocene clay Top Odderup Fm / Arnum Fm North B A Fig. 80. Two typical correlation panels showing the overall architecture of the Miocene succes- sion in Jylland. A: S–N-trending section from Løgumkloster to Resen. Note the change in the depositional style from the forestepping delta lobes of the markedly progradational Billund and Bastrup Formations to the more regular, aggrading – weakly prograding system of the Odderup Formation. B: W–E-striking section from Stauning to Morsholt. Note that the main delta lobes pinch out both to the east and to the west. The two correlation panels are also shown in Plates 2 and 6, together with detailed borehole logs. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 79 The Late Oligocene was characterised by a warm climate and thus a period with a high sea level (Utscher et al. 2000, 2009; Zachos et al. 2001; Miller et al. 2005; Larsson et al. 2006; Larsson-Lindgren 2009). The North Sea was located in the northern westerly wind belt (Galloway 2002) and consequently the north-eastern part of this sea, which cov- ered present-day Denmark, was dominated by wave processes due to the long fetch across the North Sea (Fig. 2). Most of present-day Denmark was covered by the sea in the Late Oligocene and the deposition of the fully marine Brejning Formation took place. There is no evidence for the north- ern position of the coastline at this time, but structural ele- ments such as the Sorgenfrei–Tornquist Zone or the Fennoscandian Shield were probably important features in controlling the location and trend of the shoreline; the position of the coastline is conservatively placed in the fringe area of the Fennoscandian Shield (Fig. 81A). Locally in northern Jylland, the diatomite of the Sydklint Member was formed associated with submarine exposure of Eocene diatomites. Climatic cooling and initial uplift of the 80 Palaeogeography 100 km 100 km A B Fig. 81. A: Palaeogeographic reconstruction of the latest Late Oligocene (Brejning Formation). The exact location of the shoreline is uncer- tain, but most of present-day Jylland was submerged at that time. Water depth in northern Jylland was over 200 m and extensive formation of glaucony indicates some distance to the shoreline. B: Palaeogeographic reconstruction of the earliest Early Miocene (earliest Aquitanian; Vejle Fjord Formation). Due to Early Miocene inversion (reactivation) of the Ringkøbing–Fyn High and salt structures, a barrier formed between the eastern part of the Norwegian–Danish Basin and the North Sea Basin. This resulted in brackish water conditions north-east of the Ringkøbing–Fyn High. Small spit systems developed east of these structures. The degradation of these spit systems during the Early Miocene transgression resulted in the formation of the Skansebakke Member. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 80 Norwegian–Danish Basin at the end of the Oligocene (E.S. Rasmussen 2009a) resulted in a fall in relative sea level at the Oligocene–Miocene transition. This led to deposition of the Øksenrade Member which was deposited in shallow water on the Ringkøbing-Fyn High. At Dykær, subaerial conditions prevailed for a period (Rasmussen & Dybkjær 2005). The transition from the Oligocene to the Miocene was characterised by a short, but marked sea-level fall associ- ated with ice cap growth on Antarctica (Miller et al. 1996). Coincident with this, inversion of the Norwegian–Danish Basin and reactivation of the Sorgenfrei–Tornquist Zone and the Ringkøbing–Fyn High commenced (E.S. Rasmussen 2009a). This resulted in a marked change in the deposi- tional regime in the eastern North Sea Basin from deposi- tion of dominantly fully marine, clay-rich sediments at the basin floor and toe-of-shelf slope, to sedimentation of coarse-grained, sand-rich, shallow marine, deltaic deposits (Larsen & Dinesen 1959; L.B. Rasmussen 1961; Spjeldnæs 1975; Friis et al. 1998; Michelsen et al. 1998; E.S. Rasmussen 1996, 2004a, b). During the earliest Miocene, the palaeogeography was controlled by structural highs and lows (Fig. 81B). Elevated parts of the Ringkøbing–Fyn High formed a barrier across present-day southern Jylland. Salt diapirs within the Norwegian–Danish Basin acted as cores of minor islands. A large silled basin formed north of the Ringkøbing–Fyn High where brackish water conditions prevailed. During 81 100 km 100 km A B Fig. 82. A: Palaeogeographic reconstruction of the Early Miocene (Aquitanian; Billund and Vejle Fjord Formations). The sea level continued to rise during this phase and flooded the Ringkøbing–Fyn High. Due to high sediment supply to the basin, however, the shoreline prograd- ed southward. This favoured the formation of spit/barrier complexes south-east of the main delta lobes; represented by the Hvidbjerg Member of the Billund Formation. The river system during the Early Miocene was dominantly braided in character. B: Palaeogeographic reconstruc- tion of the Early Miocene (late Aquitanian; Billund Formation). During this period, relative sea level fell and progradation of the shoreline is reflected by amalgamation of beach ridges along the coast. Distinct incision and formation of broad valleys commenced at the same time. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 81 the lowstand of sea level, sands were transported along the structures and deposited as spits and barrier islands east of the structures (Fig. 81B). In this brackish water basin, the lower part of the Vejle Fjord Formation was deposited. A subsequent rise of sea level in the early Aquitanian resulted in flooding of the Ringkøbing–Fyn High. This led to degra- dation of the barrier complexes and deposition of the Skansebakke Member. At the time of maximum flooding, the shoreline withdrew to a position north of Århus in the east and near Thisted in the north-west. The high sedi- ment supply to the North Sea Basin, however, resulted in progradation of sand-rich delta complexes from the north and north-east, as recorded by the Billund Formation (Fig. 82A). The sediments were probably conveyed through three major river systems (Olivarius 2009). The western river was probably connected to the Setesdal valley in present- day Norway and was the source for the sediments deposited in the delta located off the present west coast of Denmark, the so-called Ringkøbing lobe (Hansen & Rasmussen 2008). The central river was sourced from the north, probably from the southern part of present-day Norway and the northern part of present-day central western Sweden. The eastern river drained the area covered by the present-day central Sweden. The central and eastern river system merged in central Jylland and resulted in the deposition of the Brande lobe of the Billund Formation (Hansen & Rasmussen 2008). The river systems were braided and their deposits constitute the Addit Member. On entering the 82 Fig. 83. A: Palaeogeographic reconstruction of the Early Miocene (early Burdigalian; Klintinghoved Formation and Kolding Fjord Member). Global climatic warming resulted in a relative rise in sea level. The shoreline was characterised by estuaries and associated barrier complexes and the accumulation of braided fluvial deposits in incised valleys. B: Palaeogeographic reconstruction of the Early Miocene (early Burdigalian; Klintinghoved Formation). During the most widespread flooding in the early Burdigalian, most of western and central Jylland was covered by the sea and the clay-rich Klintinghoved Formation was deposited. 100 km 100 km A B Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 82 sea, the sands were deposited in wave-dominated deltas (Rasmussen & Dybkjær 2005; Hansen & Rasmussen 2008). Some of the sand at the delta mouth was reworked and trans- ported eastward by longshore currents to be deposited as spit and barrier complexes of the Hvidbjerg Member (Fig. 82A). Development of lagoonal environments was common during this time. Due to a global climatic deterioration in the late Aquitanian (Zachos et al. 2001), sea level began to fall and the delta complexes were forced south-westward; deposition of a coastline characterised by amalgamated beach ridges took place (Fig. 82B). A resumed transgression occurred at the beginning of the Burdigalian. This transgression was the result of a global warming (Zachos et al. 2001). According to T. Utescher (per- sonal communication 2008), the average air temperature rose 2°C. Widespread barrier-island complexes formed east of the main delta systems due to strong erosion of the main delta and eastward transport of erosional materials. These barrier-island complexes correspond to the Kolding Fjord Member (Fig. 83A). During maximum flooding of the sea and associated with the progradation of the succeeding delta complex, mud was deposited in the Danish area. This constitutes the Klintinghoved Formation (Fig. 83B). The succeeding delta complex, the Bastrup Formation, pro- graded south-westward (Fig. 84A) and periodically this progradation occurred during a sea-level fall. The coastline was dominated by beach ridges (Fig. 84B). In mid- Burdigalian times, the delta complexes of the Bastrup 83 Fig. 84. A: Palaeogeographic reconstruction of the Early Miocene (early Burdigalian; Bastrup Formation). Progradation occurred during rising relative sea level which formed optimal conditions for a shoreline dominated by lagoons and barrier islands. The fluvial system was domi- nated by meandering river systems. B: Palaeogeographic reconstruction of the Early Miocene (Burdigalian; Bastrup Formation). During this period, relative sea level fell and the prograding shoreline was characterised by amalgamation of beach ridges parallel to the coast. Distinct incision on land and formation of broad valleys commenced at the same time. 100 km 100 km A B Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 83 Formation reached the southern part of Denmark (Fig. 85A). During sedimentation of the Bastrup Formation, the fluvial regime changed character, to be dominated by meandering rivers, especially in the latter phase of progra- dation. Sand deposits of these rivers are referred to the Resen Member. A distinct global climatic warming, the ‘Mid Miocene climatic optimum’, occurred at the end of the Early Miocene (late Burdigalian) (Zachos et al. 2001). This resulted in a sea-level rise and renewed transgression. The mud laid down during this transgression and in front of the suc- ceeding prograding coastline is represented by the Arnum Formation (Fig. 85B). At the time of maximum flooding, the coastline was located across the northern part of pre- sent-day north-west Jylland and continued south-eastwards through central Jylland. Despite a subtropical climate (Friis 1975), and hence globally high sea levels during the latest part of Early and early Middle Miocene, progradation resumed (Fig. 86A). This was due to tectonism and uplift of the hinterland and consequently increased sediment sup- ply to the North Sea Basin (E.S. Rasmussen 2004b). Sand of the prograding coastline is represented by the Odderup Formation (Fig. 86B). Fine-grained storm-sand layers deposited in front of the coastline are included in the Stauning Member. As a consequence of the prograding coastline of the Odderup Formation and coincident rising sea level due to the warmer climate, conditions for brown coal formation were optimal. A preliminary study (T. 84 Fig. 85. A: Palaeogeographic reconstruction of the Early Miocene (Burdigalian; Bastrup Formation) when most of Jylland was land; progra- dation took place during rising sea level. B: Palaeogeographic reconstruction of the late Early Miocene (late Burdigalian; Arnum Formation). The shoreline was located across the northern part of Jylland at the time of maximum flooding. 100 km 100 km A B Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 84 Utescher, personal communication 2009) indicated that widespread coal formation was also associated with increased precipitation in the area. The coal was formed on the coastal plain especially adjacent to pre-existing faults (Koch 1989) and predominantly north of the Ringkøbing–Fyn High. These widespread coal layers are referred to the Fasterholt Member (Koch 1989). Due to the overall rising sea level during the Mid Miocene climatic optimum, and partly also due to ‘auto retreat’ (see Muto & Steel 2002), a major transgression occurred in the middle Langhian (early Middle Miocene). The transgres- sion was further amplified by increased subsidence of the North Sea Basin during the Middle and Late Miocene (Koch 1989; Michelsen et al 1998; Clausen et al. 1999; E.S. Rasmussen 2004b; E.S. Rasmussen et al. 2005). Mud-rich sediments of the Hodde Formation were deposited during this transgression. There is no evidence of the formation of barrier-island complexes during the transgression which suggests a very rapid flooding of the low relief landscape represented by the coal-rich Odderup Formation. Despite major global climatic deterioration (cooling) in the early Serravallian (Middle Miocene; Zachos et al. 2001), flood- ing of this part of the North Sea Basin continued as a con- sequence of the accelerating subsidence of the basin. During the most widespread flooding of the area, glaucony-rich sedi - ments of the Ørnhøj Formation accumulated, indicating a long distance to the coastline. The location of the coast- line during this maximum transgression is uncertain. 85 Fig. 86. A: Palaeogeographic reconstruction of the late Early Miocene (late Burdigalian; Odderup Formation). At this time, the climate became subtropical and the global sea level continued to rise. High sediment supply, however, forced the shoreline to prograde. These condi- tions favoured formation of lagoons and swamp lakes which were optimal for the formation of coal-rich deposits. B: Palaeogeographic recon- struction of the early Middle Miocene (early Langhian; Odderup Formation). During the maximum regression of the shoreline, most of Jylland was land and only the south-western part was submerged. Lagoonal and swamp conditions prevailed north of the Ringkøbing–Fyn High, probably favoured by increased subsidence in this area. 100 km 100 km A B Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 85 Boreholes in central Jylland do not indicate any influx of coarse-grained siliciclastic deposits, so at a minimum, the coastline was displaced to the southern boundary of the Fennoscandian Shield (Fig. 87A). Parts of the shield may, however, have been flooded during the highest rate of rel- ative sea-level rise. Coincident with the subsidence of the North Sea Basin, the Norwegian mainland was uplifted (Løseth & Henriksen 2005; Rundberg & Eidvin 2005; Eidvin & Rundberg 2007; E.S. Rasmussen et al. 2008). This resulted in enhanced sediment supply to the basin where progradation took place. Mud of the Gram Formation was deposited in an open shelf environment (Fig. 87B). Thin storm-sand layers are intercalated in the upper Gram For - mation indicating an approaching coastline (Rasmussen & Larsen 1989). Near the end of the Tortonian (Late Mio - cene), shoreface sediments of the Marbæk Formation were deposited in the central–western part of present-day Denmark (Fig. 88). Progradation of the coastline continued through the Late Miocene and a delta/coastline was formed in the cen- tral part of the Central Graben area (Rasmussen 2005; Møller et al. 2009). The termination of the Miocene was characterised by a sea-level fall of c. 90 m, which is indi- cated by deep incision of equivalent strata in the offshore Cenozoic record of Denmark (Møller et al. 2009). 86 Fig. 87. A: Palaeogeographic reconstruction of the Middle Miocene (Serravallian; Ørnhøj Formation). Despite climatic deterioration in the Middle Miocene, most of Jylland was flooded and the shoreline was located in the northern part of Jylland. Due to very low sedimentation rates, optimal conditions existed for the formation of glaucony. B: Palaeogeographic reconstruction of the Late Miocene (Tortonian; Gram Formation). In the latest part of the Miocene, uplift of Scandinavia and the Alpine mountains resulted in extremely high sediment supply into the North Sea Basin. This led to marked progradation from both the north and south. 100 km A 100 km B Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 86 Acknowledgements This project would not have been possible without the enthusiastic participation of the geologists working in the municipalities of Vejle, Ringkøbing, Ribe, Århus and Sønderjylland (subsequently restructured into MC Ribe, MC Ringkøbing, MC Århus and Region Syddanmark). The fundamental sedimentological and stratigraphic research on which this study is based was supported financially by the Carlsberg Foundation. Statens Naturvidenskabelige Forskningsråd (Danish Natural Science Research Council) generously supported the drilling of the cored borehole at Sdr. Vium. Keld Rømer Rasmussen kindly provided the gamma-ray log from the Addit gravel-pit borehole. Tibor Czako and K. Ingemann Schnetler are thanked for fruit- ful discussions on Miocene geology. Claus Heilmann- Clausen is thanked for guidance to the localities in the Limfjorden area. The authors thank Claus Heilmann- Clausen and Dan Evans for thorough and constructive reviews; Claus Heilmann-Clausen also provided data and descriptions from the Sydklint Member. 87 100 km Fig. 88. Palaeogeographic reconstruction of the Late Miocene (Tortonian; Marbæk Formation). The marked progradation of the shoreline during the Late Miocene resulted in subaerial conditions over most of Jylland and deposition of shoreface deposits only in the extreme western part of Jylland. At the end of the Miocene, the shore- line was located c. 250 km west of the present-day west coast of Jylland. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 87 Asgaard, U. & Bromley, R.G. 1974: Sporfossiler fra den Mellem Miocæne transgression i Søby–Fasterholt området. Dansk Geologisk Forening Årskrift 1973, 11–19. Bendix-Almgreen, S.E. 1983: Carcharodon megalodon from the Upper Miocene of Denmark, with comments on elasmobranch tooth enameloid: coronoïn. Bulletin of the Geological Society of Denmark 32, 1–32. Bertelsen, F. 1978: The Upper Triassic – Lower Jurassic Vinding and Gassum Formations of the Norwegian–Danish Basin. Danmarks Geologiske Undersøgelse Serie B 3, 26 pp. Berthelsen, A. 1992: Mobile Europe. In: Blundell, D., Freeman, R. & Mueller, St. (eds): A continent revealed: the European geotra- verse, 11–32. Cambridge: Cambridge University Press. Beyrich, E. 1853: Die Conchylien des norddeutschen Tertiär - gebirges. 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Ziegler, P.A. 1982: Geological atlas of western and central Europe, 130 pp. The Hague: Shell Internationale Petroleum Maat - schappij B.V. Ziegler, P.A. 1990: Geological atlas of western and central Europe, 2nd edition, 239 pp. The Hague: Shell Internationale Petroleum Maatschappij B.V. Ziegler, P.A., Cloetingh, S. & van Wees, J.D. 1995: Geodynamics of intraplate compressional deformation: the Alpine foreland and other examples. Tectonophysics 252, 7– 59. 92 Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 92 Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 93 De Nationale Geologiske Undersøgelser for Danmark og Grønland (GEUS) Geological Survey of Denmark and Greenland Øster Voldgade 10, DK-1350 Copenhagen K Denmark The series Geological Survey of Denmark and Greenland Bulletin started in 2003 and replaced the two former bulletin series of the Survey, viz. Geology of Greenland Survey Bulletin and Geology of Denmark Survey Bulletin. Some of the twenty-one volumes published since 1997 in those two series are listed on the facing page. The present series, together with Geological Survey of Den - mark and Greenland Map Series, now form the peer-reviewed scientific series of the Survey. Geological Survey of Denmark and Greenland Bulletin 1 The Jurassic of Denmark and Greenland, 948 pp. (28 articles), 2003. Edited by J.R. Ineson & F. Surlyk. 500.00 2 Fish otoliths from the Paleocene of Denmark, 94 pp., 2003. By W. Schwarzhans. 100.00 3 Late Quaternary environmental changes recorded in the Danish marine molluscan faunas, 268 pp., 2004. By K.S. Pedersen. 200.00 4 Review of Survey activities 2003, 100 pp. (24 articles), 2004. Edited by M. Sønderholm & A.K. Higgins. 180.00 5 The Jurassic of North-East Greenland, 112 pp. (7 articles), 2004. Edited by L. Stemmerik & S. Stouge. 160.00 6 East Greenland Caledonides: stratigraphy, structure and geochronology, 93 pp. (6 articles), 2004. Edited by A.K. Higgins and F. Kalsbeek. 160.00 7 Review of Survey activities 2004, 80 pp. (19 articles), 2005. Edited by M. Sønderholm & A.K. Higgins. 180.00 8 Structural analysis of the Rubjerg Knude Glaciotectonic Complex, Vendsyssel, northern Denmark, 192 pp., 2005. By S.A.S. Pedersen. 300.00 9 Scientific results from the deepened Lopra-1 borehole, Faroe Islands, 156 pp. (11 articles), 2006. Edited by J.A. Chalmers & R. Waagstein. 240.00 10 Review of Survey activities 2005, 68 pp. (15 articles), 2006. Edited by M. Sønderholm & A.K. Higgins. 180.00 11 Precambrian crustal evolution and Cretaceous–Palaeogene faulting in West Greenland, 204 pp. (12 articles), 2006. Edited by A.A. Garde & F. Kalsbeek. 240.00 12 Lithostratigraphy of the Palaeogene – Lower Neogene succession of the Danish North Sea, 77 pp., 2007. By P. Schiøler, J. Andsbjerg, O.R. Clausen, G. Dam, K. Dybkjær, L. Hamberg, C. Heilmann-Clausen, E.P. Johannessen, L.E. Kristensen, I. Prince & J.A. Rasmussen. 240.00 13 Review of Survey activities 2006, 76 pp. (17 articles), 2007. Edited by M. Sønderholm & A.K. Higgins. 180.00 14 Quaternary glaciation history and glaciology of Jakobshavn Isbræ and the Disko Bugt region, West Greenland: a review, 78 pp., 2007. By A. Weidick & O. Bennike. 200.00 15 Review of Survey activities 2007, 96 pp. (22 articles), 2008. Edited by O. Bennike & A.K. Higgins. 200.00 16 Evaluation of the quality, thermal maturity and distribution of potential source rocks in the Danish part of the Norwegian–Danish Basin, 66 pp., 2008. By H.I. Petersen, L.H. Nielsen, J.A. Bojesen-Koefoed, A. Mathiesen, L. Kristensen & F. Dalhoff. 200.00 17 Review of Survey activities 2008, 84 pp. (19 articles), 2009. Edited by O. Bennike, A.A. Garde & W.S. Watt. 200.00 18 Greenland from Archaean to Quaternary. Descriptive text to the 1995 Geological map of Greenland, 1:2 500 000. 2nd edition, 126 pp., 2009. By N. Henriksen, A.K. Higgins, F. Kalsbeek & T.C.R. Pulvertaft. 280.00 19 Lithostratigraphy of the Cretaceous–Paleocene Nuussuaq Group, Nuussuaq Basin, West Greenland, 171 pp., 2009. By G. Dam, G.K. Pedersen, M. Sønderholm, H.H. Midtgaard, L.M. Larsen, H. Nøhr-Hansen & A.K. Pedersen. 300.00 20 Review of Survey activities 2009, 106 pp. (23 articles), 2010. Edited by O. Bennike, A.A. Garde & W.S. Watt. 220.00 21 Exploration history and place names of northern East Greenland, 368 pp., 2010. By A.K. Higgins. 200.00 22 Lithostratigraphy of the Upper Oligocene – Miocene succession of Denmark, 92 pp., 2010. By E.S. Rasmussen, K. Dybkjær & S. Piasecki. Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 94 Geological Survey of Denmark and Greenland Map Series 1 Explanatory notes to the Geological map of Greenland, 1:500 000, Humboldt Gletscher, Sheet 6, 48 pp., 2004. By P.R. Dawes 280.00 2 Explanatory notes to the Geological map of Greenland, 1:500 000, Thule, Sheet 5 (1991), 97 pp. + map, 2006. By P.R. Dawes. 300.00 3 Explanatory notes to the Geological map of Greenland, 1:100 000, Ussuit 67 V.2 Nord, 40 pp. + map, 2007. By J.A.M. van Gool & M. Marker. 280.00 4 Descriptive text to the Geological map of Greenland, 1:500 000, Dove Bugt, Sheet 10, 32 pp. + map, 2009. By N. Henriksen & A.K. Higgins 240.00 5 Descriptive text to the Geological map of Greenland, 1:100 000, Kangaatsiaq 68 V.1 Syd and Ikamiut 68 V.1 Nord, 41 pp. + 2 maps, 2010. By A.A. Garde & J.A. Hollis. Geology of Greenland Survey Bulletin (discontinued) 179 The Citronen Fjord massive sulphide deposit, Peary Land, North Greenland: discovery, stratigraphy, mineralization and structural setting, 40 pp., 1998. By F.W. van der Stijl & G.Z. Mosher. 200.00 180 Review of Greenland activities 1997, 176 pp. (26 articles), 1998. Edited by A.K. Higgins & W.S. Watt. 200.00 181 Precambrian geology of the Disko Bugt region, West Greenland, 179 pp. (15 articles), 1999. Edited by F. Kalsbeek. 240.00 182 Vertebrate remains from Upper Silurian – Lower Devonian beds of Hall Land, North Greenland, 80 pp., 1999. By H. Blom. 120.00 183 Review of Greenland activities 1998, 81 pp. (10 articles), 1999. Edited by A.K. Higgins & W.S. Watt. 200.00 184 Collected research papers: palaeontology, geochronology, geochemistry, 62 pp. (6 articles), 1999. 150.00 185 Greenland from Archaean to Quaternary. Descriptive text to the Geological map of Greenland, 1:2 500 000, 93 pp., 2000. By N. Henriksen, A.K. Higgins, F. Kalsbeek & T.C.R. Pulvertaft. 225.00 186 Review of Greenland activities 1999, 105 pp. (13 articles), 2000. Edited by P.R. Dawes & A.K. Higgins. 225.00 187 Palynology and deposition in the Wandel Sea Basin, eastern North Greenland, 101 pp. (6 articles), 2000. Edited by L. Stemmerik. 160.00 188 The structure of the Cretaceous–Palaeogene sedimentary-volcanic area of Svartenhuk Halvø, central West Greenland, 40 pp., 2000. By J. Gutzon Larsen & T.C.R. Pulvertaft. 130.00 189 Review of Greenland activities 2000, 131 pp. (17 articles), 2001. Edited by A.K. Higgins & K. Secher. 160.00 190 The Ilímaussaq alkaline complex, South Greenland: status of mineralogical research with new results, 167 pp. (19 articles), 2001. Edited by H. Sørensen. 160.00 191 Review of Greenland activities 2001, 161 pp. (20 articles), 2002. Edited by A.K. Higgins, K. Secher & M. Sønderholm. 200.00 Geology of Denmark Survey Bulletin (discontinued) 36 Petroleum potential and depositional environments of Middle Jurassic coals and non-marine deposits, Danish Central Graben, with special reference to the Søgne Basin, 78 pp., 1998. By H.I. Petersen, J. Andsbjerg, J.A. Bojesen-Koefoed, H.P. Nytoft & P. Rosenberg. 250.00 37 The Selandian (Paleocene) mollusc fauna from Copenhagen, Denmark: the Poul Harder 1920 collection, 85 pp., 2001. By K.I. Schnetler. 150.00 Prices are in Danish kroner exclusive of local taxes, postage and handling Note that information on the publications of the former Geological Survey of Denmark and the former Geological Survey of Greenland (amalgamated in 1995 to form the present Geological Survey of Denmark and Greenland) can be found on the Survey’s website: www.geus.dk Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 95 Bulletin 22_ GSB191-Indhold 04/03/11 12.41 Side 96