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NORWEGIAN JOURNAL OF GEOLOGY Vol 99 Nr. 4 https://dx.doi.org/10.17850/njg99-4-1

Correlation of the Upper Oligocene–Miocene deltaic to shelfal succession onshore Denmark with similar deposits in the northern North Sea and Norwegian Sea shelf based on Sr isotope-, bio- and seismic stratigraphy—a review

Tor Eidvin1, Erik Skovbjerg Rasmussen2, Fridtjof Riis1, Karen Dybkjær2 & Kari Grøsfjeld3

1Norwegian Petroleum Directorate (NPD), Professor Olav Hanssens vei 10, P. O. Box 600, NO–4003 Stavanger, Norway. 2Geological Survey of Denmark and Greenland (GEUS), Øster Voldgade 10, DK–1350, Copenhagen K, Denmark. 3Geological Survey of Norway, Leif Eirikssons vei 39, P. O. Box 6315 Torgarden, NO–7491 Trondheim, Norway

E-mail corresponding author (Tor Eidvin): [email protected]

The almost complete, mainly deltaic, upper Paleogene and Neogene succession in Jylland, Denmark, was previously investigated for 87Sr/86Sr ratios in 143 samples from 18 localities. In the present paper, strontium-isotope data from the Upper Oligocene–Lower Miocene parts and foraminiferal and pyritised diatoms data from 94 of these samples were used to correlate with previously published data from Norwegian wells and boreholes and one borehole in the British sector of the North Sea. For the Middle–Upper Miocene parts of the succession the correlation is based mainly on Bolboforma data. The ages of the geological formations in the Danish succession correlate readily with lithological units in the Norwegian North Sea, the Norwegian Sea shelf and the East Shetland Platform, which have all been investigated applying similar methods. The Bolboforma assemblages have their origin in the North Atlantic and the Norwegian Sea and confirm the presence of an open strait in the northern North Sea. This strait was the only seaway passage into the North Sea Basin during the Miocene. The glauconitic Utsira Formation sand (approximately 5.7–4.2 Ma), in the threshold area close to the outlet to the Norwegian Sea, overlies erosional unconformities comprising hiati of 21 my in some areas and 13 my in other areas. We believe that the unconformity below the Utsira Formation was mainly related to a fall in sea level in the Late Miocene, contemporaneous with that partly responsible for the Messinian salinity crisis. Bolboforma and dinoflagellate cysts stratigraphy indicate that the base of the Molo Formation in its southern distribution area (Draugen Field, Trøndelag Platform) is of Late Miocene age (close to 9 Ma). This part of the Molo Formation was contemporaneous with the middle/upper part of the Kai Formation.

Keywords: Sr isotope stratigraphy, foraminiferal stratigraphy, Bolboforma stratigraphy, upper Paleogene-Neogene correlation, Denmark, North Sea, Norwegian Sea shelf, Norwegian Sea.

Received 30. May 2019 / Accepted 25. September 2019 / Published online 30. October 2019

Introduction understanding the palaeogeography and infill history of the North Sea basin. A proper dating of the sedimentary A correlation between the well-dated outcropping Upper units and recognition of the extent of hiatuses are Oligocene–Miocene succession in Denmark (Eidvin et necessary for this purpose. al., 2014a) and the offshore succession in the Norwegian North Sea, East Shetland Platform and Norwegian Sea Thin-walled calcareous microfossils such as foraminifera shelf (Eidvin, 2016; Eidvin et al., 2013, 2014b) is a key for and Bolboforma are generally sparse in the Danish

Eidvin, T., Rasmussen, E.S., Riis, F., Dybkjær, K. & Grøsfjeld, K. 2019: Correlation of the Upper Oligocene–Miocene deltaic to shelfal succession onshore Denmark with similar deposits in the northern North Sea and Norwegian Sea shelf based on Sr isotope-, bio- and seismic stratigraphy – a review. Norwegian Journal of Geology 99, 543–573. https://dx.doi.org/10.17850/njg99-4-1.

543 544 T. Eidvin et al. onshore upper Paleogene and Neogene successions. This Eidvin et al. (2014a) presented a comparison and is either due to their dissolution by humic acid in the a discussion of the Danish strontium-isotope and pore water or they were not present in the most marginal dinocyst data. They concluded that the Sr isotope ages marine environments. However, from the stratigraphic from the lower part of the Danish Miocene succession, borehole Rødding (DGU nr. 141.1141) in southern i.e., the latest Oligocene–Early Miocene Brejning to Jylland (Fig. 1), Eidvin et al. (2013) were able to retrieve Odderup formations, agree with the age estimates based foraminifera, Bolboforma and mollusc shells from most on dinocysts. However, the 87Sr/86Sr ratios of fossil sections (Figs. 1 & 2). In several sites, investigated for carbonates from the Middle–Upper Miocene, Hodde fossil dinoflagellate cysts (dinocysts) by Dybkjær & to Gram formations consistently indicate ages older Piasecki (2010), thick-walled tests of molluscs have than those recorded by the dinocysts (Fig. 2). Post- been quite resistant to dissolution. These are present depositional processes as an explanation for this offset where foraminifera are absent, and Eidvin et al. (2014a) are inconsistent with the good preservation of the shell succeeded to retrieve molluscs and/or mollusc fragments material. There is also restricted reworking. Eidvin et al. from a number of samples for strontium isotope analyses (2014a) suggested that limited oceanic exchange with the from these sites (Table 1). inner North Sea Basin might have caused the observed Sr isotope ratios.

Boreholes/wells 100 km Exposures Frida-1 Studied localities Lone-1 North Sea Jylland 50 km S-1 Tove-1 57°N Limfjorden Sweden Salling

Lyby Strand Harre-1 Denmark Præstbjerg

Fasterholt Jylland 55°N Sdr. Vium Jensgård Fakkegrav Dykær Vejle Fjord Føvling Brejning Bøgeskov Sjælland Gram-2 Rødding Fyn Gram

53°N Lille Tønde Hørup Hav Klintinghoved Germany 8°E 10°E 12°E

Figure 1. Map of onshore and offshore Denmark showing wells, boreholes and outcrops analysed for dinocysts (Dybkjær & Piasecki, 2010), Bolboforma and foraminifera (Eidvin et al. 2013). It also shows the sites where shell material has been Sr dated. Small circles: Outcrops and boreholes which formed the basis for the dinocyst study (Dybkjær & Piasecki, 2010). Large circles: Outcrops and boreholes that formed the basis for the dinocystFig. study 1 (Dybkjær & Piasecki, 2010) as well as the present Sr isotope study. NORWEGIAN JOURNAL OF GEOLOGY Correlation of the Upper Oligocene–Miocene deltaic to shelfal succession onshore Denmark with similar deposits 545 Continues Analysed fossils Six mollusc fragments mollusc Six One mollusc fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One One mollusc fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One Two mollusc fragments mollusc Two fragments mollusc Two Two mollusc fragments mollusc Two Three mollusc fragments mollusc Three fragments mollusc Three fragments mollusc Three Comments Same sample as above as sample Same above as sample Same above as sample Same above as sample Same Same sample as above as sample Same above as sample Same Same sample as the two above the two as sample Same 24.78 24.83 22.43 22.63 24.76 24.99 23.99 23.93 23.20 24.53 23.81 23.99 24.22 22.80 24.05 22.06 22.28 21.99 23.41 23.99 24.16 22.68 22.67 22.91 22.79 22.48 22.22 23.03 23.39 22.93 mean value) mean M., 2004; 2004; & M., H. (Ma; Age 25.53 25.57 23.46 23.69 25.51 25.68 24.84 24.42 24.23 25.32 24.70 24.84 25.03 23.86 24.89 22.88 23.25 22.76 24.41 24.84 24.98 23.74 23.72 23.97 23.85 23.52 23.14 24.08 24.54 23.99 mean value) mean M., 1997; 1997; & M., H. (Ma; Age 2S error 0.000009 0.000008 0.000008 0.000008 0.000008 0.000008 0.000008 0.000008 0.000009 0.000008 0.000008 0.000008 0.000009 0.000009 0.000009 0.000009 0.000008 0.000008 0.000009 0.000009 0.000008 0.000008 0.000008 0.000009 0.000008 0.000008 0.000009 0.000009 0.000008 0.000008 Sr 87/86 0.708163 0.708161 0.708287 0.708275 0.708164 0.708155 0.708202 0.708231 0.708243 0.708174 0.708212 0.708202 0.708190 0.708265 0.708199 0.708313 0.708297 0.708318 0.708232 0.708202 0.708193 0.708272 0.708273 0.708259 0.708266 0.708284 0.708302 0.708252 0.708233 0.708258 Corrected Lithostratigraphy/sample level Lithostratigraphy/sample Brejning Fm Brejning Fm Brejning Fm Brejning Fm Brejning Fm Brejning Fm Brejning Fm Brejning Fm Brejning 76.8–76.4 m (bucket) Fm? Brejning 44.25 m (core) Fm, Brejning 44.25 m (core) Fm, Brejning 37.25 m (core) Fm, Brejning 31.25 m (core) Fm, Brejning 243 m (DC) Fm, Fjord Vejle 241 m (DC) Fm, Fjord Vejle Fm Fjord Vejle Fm Fjord Vejle Fm Fjord Vejle 230 m Fm, Fjord Vejle Brejning Fm Brejning Fm Brejning Fm Brejning Fm Brejning 170 m (core) Fm, Fjord Vejle 170 m (core) Fm, Fjord Vejle 170 m (core) Fm, Fjord Vejle 68.8–68.4 m (bucket) Fm, Fjord Vejle 19.75 m (core) Fm, Fjord Vejle 238 m (DC) Fm, Fjord Vejle 236 m (DC) Fm, Fjord Vejle Strontium-isotope analyses (all samples are analysed at the University in Bergen if not stated otherwise. All Sr ratios were corrected to NIST 987 = 0.710248. Numerical ages derived from the SIS SIS the from derived ages Numerical 987 = 0.710248. NIST to corrected were ratios Sr All otherwise. stated if Bergen not in University the at analysed are samples (all analyses 1. Strontium-isotope Table cuttings). DCditch – Technology. and Standard for Institute – National NIST 2004). (1997, McArthur & of Howarth Tables Look-up Localities Fakkegrav (outcrop) Fakkegrav (outcrop) Fakkegrav (outcrop) Bøgeskov (outcrop) Bøgeskov (outcrop) Jensgård (outcrop) Jensgård (outcrop) Strand Lyby (outcrop) Strand Lyby (boreh.) Hav Hørup core) (borehole, Harre (boreh.) Harre (boreh.) Harre (boreh.) Harre Rødding (boreh.) Rødding (boreh.) Salling 1 (outcrop) Salling 1 (outcrop) Salling 1 (outcrop) Rødding (boreh.) Brejning (outcrop) Brejning (outcrop) Brejning Dykær (outcrop) Dykær (outcrop) (boreh.) Fasterholt (boreh.) Fasterholt (boreh.) Fasterholt (boreh.) Hav Hørup (boreh.) Harre Rødding (boreh.) Rødding (boreh.) Table 1. Continued 546 T. Eidvin et al. Corrected Age (Ma; H. & M., 1997; Age (Ma; H. & M., 2004; Localities Lithostratigraphy/sample level 2S error Comments Analysed fossils 87/86Sr mean value) mean value)

Rødding (boreh.) Vejle Fjord Fm, 228 m 0.708262 0.000009 23.92 22.86 One mollusc fragment Rødding (boreh.) Vejle Fjord Fm, 225 m 0.708230 0.000009 24.44 23.45 One mollusc fragment Rødding (boreh.) Vejle Fjord Fm, 222 m 0.708276 0.000008 23.67 22.62 One mollusc fragment Rødding (boreh.) Vejle Fjord Fm, 220 m 0.708263 0.000009 23.90 22.84 One mollusc fragment Rødding (boreh.) Vejle Fjord Fm, 218 m 0.708380 0.000009 21.26 21.09 One mollusc fragment Rødding (boreh.) Vejle Fjord Fm, 216 m 0.708387 0.000009 21.13 20.97 One mollusc fragment Salling 2 (outcrop) Klintinghoved Fm 0.708462 0.000009 19.96 19.66 One mollusc fragment Salling 2 (outcrop) Klintinghoved Fm 0.708447 0.000007 20.19 19.87 One mollusc fragment Salling 2 (outcrop) Klintinghoved Fm 0.708439 0.000008 20.31 19.98 Same sample as the two above Two mollusc fragments Klinting-hoved (outcrop) Klintinghoved Fm 0.708389 0.000008 21.10 20.93 One mollusc fragment Klinting-hoved (outcrop) Klintinghoved Fm 0.708371 0.000008 21.44 21.24 Same sample as above One mollusc fragment Klinting-hoved (outcrop) Klintinghoved Fm 0.708370 0.000009 21.46 21.25 One mollusc fragment Klinting-hoved (outcrop) Klintinghoved Fm 0.708398 0.000009 20.95 20.75 One mollusc fragment Sønder Vium (boreh.) Klintinghoved Fm, 283.3 m (core) 0.708395 0.000008 21.00 20.81 One mollusc fragment Sønder Vium (boreh.) Klintinghoved Fm, 268.5 m (core) 0.708459 0.000008 20.01 19.70 One mollusc fragment Prestbjerg (boreh.) Klintinghoved Fm, 155–154 m (core) 0.708351 0.000008 21.89 21.52 One fragment of a shark tooth Prestbjerg (boreh.) Klintinghoved Fm, 155–154 m (core) 0.708349 0.000009 21.93 21.55 One fragment of a shark tooth Prestbjerg (boreh.) Klintinghoved Fm, 155–154 m (core) 0.708374 0.000009 21.38 21.19 One fragment of a shark tooth Hørup Hav (boreh.) Klintinghoved Fm, 62.75–62.3 m (bucket) 0.708331 0.000009 22.39 21.80 One mollusc fragment Hørup Hav (boreh.) Klintinghoved Fm, 54.8–54.3 m (bucket) 0.708323 0.000009 22.63 21.92 One mollusc fragment Hørup Hav (boreh.) Klintinghoved Fm, 52.0–51.35 m (bucket) 0.708265 0.000008 23.86 22.80 One mollusc fragment Hørup Hav (boreh.) Klintinghoved Fm, 50.9–50.45 m (bucket) 0.708365 0.000009 21.56 21.32 One mollusc fragment Hørup Hav (boreh.) Klintinghoved Fm, 49.3–49.1 m (bucket) 0.708348 0.000009 21.96 21.56 One mollusc fragment Hørup Hav (boreh.) Klintinghoved Fm, 43.0 m (bucket) 0.708438 0.000008 20.32 20.00 One mollusc fragment Rødding (boreh.) Klintinghoved Fm, 185 m (DC) 0.709012 0.000008 5.65 5.67 Probably caved One mollusc fragment Sønder Vium (boreh.) Arnum Fm, 112 m (core) 0.708555 0.000008 18.50 18.44 One mollusc fragment Sønder Vium (boreh.) Arnum Fm, 112 m (core) 0.708560 0.000008 18.43 18.38 One mollusc fragment Sønder Vium (boreh.) Arnum Fm, 111.15 m (core) 0.708580 0.000008 18.18 18.12 One mollusc fragment Sønder Vium (boreh.) Arnum Fm, 111.15 m (core) 0.708543 0.000007 18.66 18.59 One mollusc fragment Sønder Vium (boreh.) Arnum Fm, 111.0–109.5 m (core) 0.708572 0.000008 18.28 18.23 One mollusc fragment Sønder Vium (boreh.) Arnum Fm, 111.0–109.5 m (core) 0.708611 0.000008 17.83 17.74 One mollusc fragment Sønder Vium (boreh.) Arnum Fm, 90.0–88.5 m (core) 0.708529 0.000008 18.86 18.77 One mollusc fragment NORWEGIAN JOURNAL OF GEOLOGY Correlation of the Upper Oligocene–Miocene deltaic to shelfal succession onshore Denmark with similar deposits 547 Analysed fossils One smallOne gastropod smallOne gastropod One bryozo fragment One One mollusc fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One One mollusc fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One fragment mollusc One Two mollusc fragments mollusc Two fragments mollusc Two Caved Caved Caved Caved Reworked Comments 17.70 17.70 17.57 18.28 20.24 18.80 19.12 19.97 11.14 11.39 15.78 15.59 13.59 16.02 16.53 16.39 17.11 32.37 15.49 16.19 15.59 10.84 15.32 15.82 17.74 17.60 18.56 16.04 16.43 16.09 16.19 18.80 mean value) mean M., 2004; 2004; & M., H. (Ma; Age 17.79 17.79 17.68 18.56 20.53 18.89 19.27 20.29 11.27 11.49 16.23 15.97 13.59 16.51 16.95 16.84 17.35 32.13 15.83 16.67 15.97 11.01 15.54 16.29 17.83 17.62 18.64 16.53 18.87 16.57 16.67 18.89 mean value) mean M., 1997; 1997; & M., H. (Ma; Age 2S error 0.000009 0.000010 0.000009 0.000009 0.000008 0.000008 0.000009 0.000009 0.000009 0.000011 0.000008 0.000008 0.000008 0.000008 0.000009 0.000009 0.000009 0.000009 0.000008 0.000009 0.000009 0.000009 0.000008 0.000008 0.000008 0.000009 0.000009 0.000008 0.000007 0.000009 0.000008 0.000009 Sr 87/86 0.708614 0.708614 0.708624 0.708558 0.708424 0.708527 0.708502 0.708440 0.708852 0.708846 0.708734 0.708746 0.708805 0.708718 0.708688 0.708696 0.708655 0.707898 0.708752 0.708708 0.708746 0.708860 0.708764 0.708731 0.708611 0.708622 0.708545 0.708717 0.708694 0.708714 0.708708 0.708527 Corrected Lithostratigraphy/sample level Lithostratigraphy/sample Arnum Fm, 82.85–82.35 m (DC) Fm, Arnum Arnum Fm, 81.35–80.8 m (DC) Fm, Arnum 67.9–67.45 m (DC) Fm, Arnum 135 m (DC) Fm, Arnum 132 m (DC) Fm, Arnum 129 m (DC) Fm, Arnum 127 m (DC) Fm, Arnum 124 m (DC) Fm, Arnum 120 m (DC) Fm, Arnum 100 m (DC) Fm, Arnum 99 m (DC) Fm, Arnum 94 m (DC) Fm, Arnum 92 m (DC) Fm, Arnum 91 m (DC) Fm, Arnum 69 m (core) Odderup Fm, 69 m (core) Odderup Fm, 69 m (core) Odderup Fm, 81 m (DC)Odderup Fm, 78 m (DC)Odderup Fm, 72 m (DC)Odderup Fm, 69 m (DC)Odderup Fm, 65 m (DC)Odderup Fm, 64 m (DC)Odderup Fm, 41 m (DC)Odderup Fm, Arnum Fm, 90.0–88.5 m (core) Fm, Arnum 71.15 m (core) Fm, Arnum 71.15 m (core) Fm, Arnum 51.80 m (core) Fm, Arnum 51.80 m (core) Fm, Arnum 51.80 m (core) Fm, Arnum 51.50 m (core) Fm, Arnum 87.6 m (DC) Fm, Arnum Lille Tønde (boreh.) Lille Tønde (boreh.) Lille Tønde Rødding (boreh.) Rødding (boreh.) Rødding (boreh.) Rødding (boreh.) Rødding (boreh.) Rødding (boreh.) Rødding (boreh.) Rødding (boreh.) Rødding (boreh.) Rødding (boreh.) Rødding (boreh.) (boreh.) Føvling (boreh.) Føvling (boreh.) Føvling Rødding (boreh.) Rødding (boreh.) Rødding (boreh.) Rødding (boreh.) Rødding (boreh.) Rødding (boreh.) Rødding (boreh.) Localities Sønder Vium (boreh.) Vium Sønder (boreh.) Vium Sønder (boreh.) Vium Sønder (boreh.) Vium Sønder (boreh.) Vium Sønder (boreh.) Vium Sønder (boreh.) Vium Sønder (boreh.) Lille Tønde (boreh.) Lille Tønde 548 T. Eidvin et al.

Table 2. Comparison of the Oligocene to Pleistocene time scale of The purpose of the present paper is to correlate the Berggren et al. (1995) and Cohen et al. (2013, updated 2018). Please note data from the Danish succession (published in Eidvin that after Berggren et al. (1995), series/epochs, sub-series/sub-epochs and stages/ages are all formal chronostratigraphic units. After Cohen et al., 2014a) with similar data in wells in the northern et al. (2013, updated 2018), series/epochs and stages/ages are formal North Sea (Figs. 1–3; published in Eidvin, 2016 and chronostratigraphic units. Eidvin et al., 2013, 2014b). Since Eidvin et al. (2014a) showed that the strontium-isotope data from the Middle–Upper Miocene part of the Danish succession Berggren et Cohen et al. (2013, are not reliable and cannot be trusted, we have only al. (1995) updated 2018) used the strontium-isotope data from the Upper Sub-series/ Stages/ Stages/ Ma Oligocene–Lower Miocene part of this succession sub-epochs ages ages (Table 1). For the Middle–Upper Miocene part, the Series/epochs 0 correlation is based on comparing the Bolboforma and Pleistocene 1.85 foraminiferal assemblages in the Rødding borehole cene Upper/ Gelasian 2.6 Pleisto- Gelasian with similar assemblages in the Norwegian and British Late Piacenz. 3.5 Piacenz. 3.6 wells and boreholes and the deep-sea record (Figs. Lower/ 4–8). Dinocyst correlation is also used in some areas. Zanclean Zanclean Early 5.32 Eidvin et al. (2013, 2014b) have substantiated the

Pliocene 5.33 5 approximate synchronicity of the upper Paleogene Messinian Messinian 7.12 7.25 and Neogene delta and distal sediments in different parts of the North Sea (Figs. 9–12). In the present paper we present a more detailed correlation. Tortonian Tortonian Upper/Late 10 In a number of previous studies, more than 2000 11.2 11.62 samples, in more than 55 Norwegian wells and boreholes and one British well, have been analysed Serravalian Serravalian 13.82 for benthic and planktonic foraminifera, Bolboforma and pyritised diatoms. As an additional control, and in 14.8 Middle Langhian 15 order to increase the stratigraphic resolution, around Miocene Langhian 16.0 1500 samples from the same wells and boreholes, were 16.4 analysed for 87Sr/86Sr ratios (Eidvin, 2016; Eidvin et al., 2013, 2014b). Most of the analysed samples were ditch Burdigalian Burdigalian cuttings, whereas sidewall cores and conventional core samples were available in some wells. Figures 1 20.5 20.4 20 and 2 in Eidvin et al. (2013) and figures 17 and 18 in Eidvin et al. (2014b) show the location of the analysed

Lower/Early Aquitanian Aquitanian sidewall cores, conventional core samples and ditch 23.0 cuttings. Caved material is often a problem when 23.8 analysing ditch cuttings, whereas reworked material is 25 always a problem regardless of types of samples. This Chattian is discussed in the papers where the detailed results Chattian of the analysis are presented (Eidvin, 2016; Eidvin & Rundberg, 2007; Eidvin et al. 2007, 2013, 2014b and

Upper/Late 27.8 28.5 papers referred to in Eidvin et al. 2013, 2014b). These papers compare the ages provided by Sr isotope 30 correlations with ages given by biostratigraphic Oligocene Rupelian Rupelian correlations and discuss the uncertainties. In the northern North Sea, common soft-sediment

Lower/Early deformation and sand injection in the lower part of 33.7 33.9 the Utsira Formation, which are mainly restricted to the depocentres (Riis & Eidvin, 2015, 2016), may also Priabonian 35 Priabonian complicate the dating of the sediments. All wells have 37 been tied to high-quality seismic data. The strontium 37.8 data, which are used for the correlations in the present paper, are based on fossil tests interpreted to be in situ or having an age which does not deviate very much from the depositional age.

The 87Sr/86Sr ratios were converted to age estimates Table 2 using the Strontium isotope stratigraphy (SIS) look-up NORWEGIAN JOURNAL OF GEOLOGY Correlation of the Upper Oligocene–Miocene deltaic to shelfal succession onshore Denmark with similar deposits 549

Sequence Ma Epoch Age Lithostratigraphy boundaries and

Period SW NE Sr-datings (Ma) 5 Plio. Zanclean Marine silt and clay Marine sand Messinian Brackish water silt and clay Fluvial sand and gravel Marbæk Fm Coal Hiatus Upper Sequence boundaries: ♦ ♦ Tortonian E 17.2 -10.3 10 Gram Fm D

Måde Group Måde C B Ørnhøj Fm A Serravallian 17.1♦-15.3♦ Hodde Fm Middle

15 Langhian Miocene Miocene

Neogene Fasterholt Mb 17.4 -15.8 Odderup Fm Stauning Mb

Arnum Fm 20.5-16.6 Vandel Mb Burdigalian Resen Mb Bastrup Fm 23.9-20.0 Ribe Group 20 Lower Klintinghoved Fm

Kolding Fjord Mb Addit Mb Aquitanian Hvidbjerg Mb Vejle Fjord Fm Billund Fm 24.4-22.8 Skansebakke Mb Brejning Fm Øksenrade Mb Brejning Fm 25.7-23.5

25 Chattian Upper Oligocene Paleogene

♦ = These ages are considerably older than the ages obtained from dinocyst correlations according to Eidvin et al. (2014a).

Figure 2. Lithostratigraphy of the Danish uppermost Oligocene–Miocene (from Rasmussen et al., 2010). The column to the right shows the palynological stratigraphy of Dybkjær & Piasecki (2010) and the main results of the strontium-isotope datings of mollusc tests from outcrop Fig.and borehole 2 samples. Please note that the stratigraphy of Rasmussen et al. (2010) and Dybkjær & Piasecki (2010) is based on the time scale of Gradstein et al. (2004). The strontium-isotope stratigraphy is based on the look-up table of Howarth & McArthur (1997) which again is based on the time scale of Berggren et al. (1995). The use of Howarth & McArthur’s (1997) table is to facilitate correlation with successions on the Norwegian continental shelf. In the strontium-isotope analyses (Table 1), age estimates based on Howarth & McArthur (2004) are also listed.

table of Howarth & McArthur (1997; Eidvin et al., 2013, on the tables of Howarth & McArthur (1997, 2004) are Fig. 3). Consequently, to facilitate correlation with listed (Table 1). There is currently no SIS look-up table successions on the Norwegian continental shelf, we have that is based on the new time scale of Cohen et al. (2013, also converted the Sr ratios to age estimates using the updated 2018). Table 2 shows that, for the post-Eocene, same look-up table in the present paper. This look-up absolute ages for the time scales of Berggren et al. (1995) table is based on the time scale of Berggren et al. (1995), and Cohen et al. (2013, updated 2018) do not deviate and this time scale is used throughout the present paper. very much. The most important difference is that in The dinocyst zonation of Dybkjær & Piasecki (2010) is Cohen et al. (2013, updated 2018), the base Pleistocene is based on the time scale of Gradstein et al. (2004). In the moved from 1.85 to 2.588 Ma. paper of Eidvin et al. (2014a) age estimates are based on the revised look-up table of Howard & McArthur (2004), which in turn is based on the time scale of Gradstein et al. (2004). In the present paper, age estimates based 550 T. Eidvin et al.

0˚ LEGEND 9° 18˚ Wells and boreholes analysed for Sr isotopes Other wells/boreholes investigated or referred to Shelf break N Hutton sand (Oligocene - Pleistocene; mapped) Utsira Formation (Upper Miocene - Lower Pliocene; mapped) Molo Formation (Upper Miocene - Lower Pliocene) Thick Skade Formation (Lower Miocene; mapped) 4° Thin and distal Skade Formation (Lower Miocene; mapped) Eir formation (informal; Middle Miocene; mapped) Lower Miocene (Burdigalian - early Langhian) delta sand (Denmark; mapped) 6704/12-GB1 6610/3-1 Lowermost Miocene (Aquitanian) 6610/2-1 S delta sand (Denmark; mapped) Oligocene sands (conceptual model) 6607/5-2 6609/5-1 6607/5-1 6610/7-2 Lower Oligocene argillaceous wedge unit (conceptual model) 6610/7-1 North Sea Oligocene play (NOL-1) according to the NPD (mapped) 6609/11-1

6510/2-1 6507/5-1, /5-J-1 H 6508/5-1 Possible drainage route to Oligocene- Miocene deposit 6507/12-1

Based on onshore morphology and oshore deposition patterns 49-23 6403/5-GB-1 6407/9-2 64˚ 6407/9-1 Based on provenance studies, onshore 6407/9-5 morphology and oshore 6404/11-1 deposition patterns

6305/4-1 6305/5-1

Present water divide

Paleo water divide

Areas with abundant river captures SWEDEN

36/1-2 34/2-4 35/3-1 Fig. 13 34/4-6 34/7-1 34/4-7 34/8-1 34/8-3 A 34/7-2 35/11-1 Shetland 34/10-17 35/11-14 S 29/3-1 31/3-1 30/6-3 NORWAY 30/5-2

60˚ Eroded

25/1-8 S 25/2-10 S 9/09a-A23 Partly eroded

25/10-2 24/12-1 26/10-1 59° 16/1-2 16/1-4 16/2-14 16/3-5

15/9-A-23 15/9-13 15/12-3

Fig. 12

2/2-2 9/12-1 11/10-1 DENMARK C-1X Nini 1 Resen 2/4-C-11 Holstebro Fjand Sorring 4° UlfborgMausing Frida 1 R-1X 56˚ Lone 1 Hjøllund

Rødding 0˚ 0 25 50 100 kilometres 9°

Fig. 3 NORWEGIAN JOURNAL OF GEOLOGY Correlation of the Upper Oligocene–Miocene deltaic to shelfal succession onshore Denmark with similar deposits 551

Figure 3. Map showing wells and boreholes containing Oligocene to in the eastern North Sea Basin throughout this period. Lower Pliocene deposits analysed for strontium isotopes, the location During the Middle Miocene, the regional subsidence of of the interpreted seismic profiles (Figs. 12 &13) and the Oligocene to » the central North Sea Basin accelerated while the basin Lower Pliocene sandy deposits in the North Sea, Norwegian Sea and on the Norwegian Sea shelf mentioned in the text (the sites indicated flanks became uplifted (Ziegler, 1990; Knox et al., 2010; in Figure 1 are not included; modified after Eidvin et al., 2013). The Rasmussen & Dybkjær, 2014). In Denmark, this resulted extent of the Oligocene sands and wedge units are according to Rundberg in flooding of the margins and deposition of marine mud & Eidvin (2005). The extent of the Utsira, Eir (informal) and Skade on top of the Lower Miocene deltaic deposits. Resumed formations in the North Sea is according to the NPD (unpublished data). delta progradation took place during the Late Miocene The extent of the Molo Formation is after Bullimore et al. (2005), and the (Sørensen et al., 1997), and at this time the deltas extent of the Hutton sand (informal) is after Gregersen & Johannessen (2007). The extent of the North Sea Oligocene play (NOL-1) is according reached the central part of the Danish North Sea Basin to the Norwegian Petroleum Directorate web page (www.npd.no). The (Rasmussen et al., 2005, 2008). The Norwegian–Danish provenance study is after Olivarius (2009) and the topographic map is Basin was probably a land area during the Pliocene. after Olesen et al. (2010). However, the evidence for that has been destroyed by Quaternary uplift and erosion (Japsen, 1993).

The North Sea Basin is an epicontinental basin, confined Geological setting by the Scandinavian and British landmasses, with a marine connection in the north to the Norwegian– The Norwegian–Danish Basin was formed during the Greenland Sea (Figs. 3 & 8). In the Norwegian sector, Permian–Triassic rifting (Ziegler, 1982, 1990; Berthelsen, the basin comprises several major, Mesozoic highs and 1992). The basin is bounded to the northeast by the grabens of which the Central Graben in its south-central so-called Sorgenfrei–Tornquist Zone and the southern region and the Viking Graben in the north are dominant boundary is formed by the Ringkøbing–Fyn High. (see figure 7 in Eidvin et al., 2013 or figure 15 in Eidvin Reactivation of fault blocks took place in the Jurassic and et al. 2014b). Tectonism ceased in the Cretaceous and especially salt movements were associated with the Mid- the basin was subjected to post-rift subsidence and Cimmerian tectonic phase (Vejbæk & Andersen, 1987; became filled by sediments sourced by the surrounding Berthelsen, 1992; Thybo, 2001). Regional subsidence topographical highs. In the Paleocene–Eocene, the characterised the basin from the Early Cretaceous. This surrounding landmasses were uplifted and the North period was still dominated by a paralic depositional Sea Basin deepened. Deltaic sequences prograded into setting. During the Late Cretaceous, inversion of former the deep basin from the Shetland Platform and West graben structures occurred, and resumed reactivation Norway. Progradation continued in the Oligocene and of salt structures probably commenced (Mogensen Miocene, but the source area was then mainly confined & Korstgård, 1993). The Late Cretaceous period was to the Shetland Platform (Eidvin & Rundberg, 2001, dominated by deposition of marine chalk, and adjacent 2007; Gregersen & Johannessen, 2007; Rundberg & to the Sorgenfrei–Tornquist Zone a 1–2 km-thick Eidvin, 2005; Eidvin et al., 2013). The depocentres succession of chalk was formed. However, in the typically contain 200–600 m of Oligocene to Lower marginal areas of the Fennoscandian Shield, e.g. Scania, Pliocene sands. uplift of basement resulted in progradation of siliciclastic delta systems (Erlström, 1994). Continued subsidence in The Norwegian Sea and its continental shelf and the North Sea characterised the Paleogene. Marine chalk, slope contain various structural elements (see figure and later on marine clay, accumulated in the basin. Along 6 in Eidvin et al., 2013 or figure 10 in Eidvin et al., the Sorgenfrei–Tornquist Zone, minor uplift/inversion 2014b). The Møre and Vøring basins are characterised of the flanks occurred in the Late Paleocene (Nielsen by exceptionally thick Cretaceous successions and a et al., 2005). Deposition of marine clay continued complex Cretaceous and Cenozoic tectonic history into the Eocene. Minor reactivation of salt structures (Blystad et al., 1995; Brekke, 2000). In Oligocene to Early commenced at the Eocene/Oligocene boundary. From Pliocene times, the Møre and Vøring basins were located the Oligocene, mud-dominated, mica-rich, marine in a distal position relative to sediment supply from sediments were deposited. During the latest Early Scandinavia, and pelagic ooze makes up a significant part Oligocene, sandy deltaic deposits started to accumulate of the succession. Large compressional structures were in the northeastern part of the basin in the Norwegian formed during Eocene and Middle Miocene tectonism. sector of the North Sea (Eidvin et al., 2013). The change The Trøndelag Platform has remained tectonically stable from clay-dominated to mud- and sand-dominated, since the Late Cretaceous. In the Late Miocene to Early mica-rich sediments was associated with progradation Pliocene, there was a pronounced progradation of coastal of sediments sourced in the Southern Scandes. Inversion sediments along the inner Norwegian Sea continental of the Norwegian–Danish Basin took place at the shelf (represented by the sandy Molo Formation, Oligocene–Miocene boundary (Rasmussen, 2009, 2013). typically 100–200 m thick). Farther west on the present Early Miocene uplift of the Southern Scandes and a continental shelf, deposition of fine-grained clastic decreasing water depth in the Norwegian–Danish basin sediment and pelagic ooze prevailed, and contouritic resulted in progradation of sand-rich deltaic deposits deposits are common (Laberg et al., 2005). 552 T. Eidvin et al.

N. Pachyd. (D.)

ACOSTAENSIS ACOSTAENSIS

(LAD) N. (LAD) N. (FAD)

derma (S.) derma N. Pachy- N. N. N. ensis Lower Atlan- tica (D) Acosta- N. mayeri tica (S.) N. atlant. (D.) FORAM. N. Atlan- PLANKT. lata gori ensis B. fra- B. compr. SITE 642+643 FORMA B. reticu- CALCAREOUS B. laevis macheri B. baden- BOLBO- B. metz- MICROFOSSILS (BASED ON FADs) Müller & Spiegler 1993) (Spiegler & Jansen 1989, 6000 4000 No. IRD/g sed Jansen (1996). Sr data only from the the from only data Sr (1996). Jansen 2000 SITE 644/642 no data & VØRING PLATEAU 0 9 8 7 10 6b 11 12 NSA 9 12b 8c 12a 8b 8a 7b 7a 6b 11 10 15 14 NSB 12c 16x 13a 13b (King 1989) 9c 9b 9a 13 12 11 10 16a NORTH SEA NORTH NSP (BASED ON LADs) 15c 16b 14b 14a 15d 15b 15a 4 6 8 0 2

10 12 14 16 18 20 22 24 26 28 30 32 34

(Ma)

Upper Middle Lower Upper Lower Upper Lower

Pliocene Miocene Oligocene cene SUB- Pleisto- SERIES SERIES/ This vertical scale (in Ma) differs from that of the three wells which are in metres. This vertical scale (in Ma) differs Marine mudstone Marine sandstone Glauconitic sandstone/mudstone Neogloboquadrina assembl. (dex.) pachyderma Lower Neogl. assembl. (dex.) atlantica

23.8 23.1

(Ma) 5.3 5.4 5.9 6.1 10.1 12.1 11.3 15.5 15.9 15.7 17.1 17.4 17.9 18.1 19.3 19.4

assembl. assemblage assemblage

assemblage assemblage assemblage macheri

assemblage assemblage

bulloides reticul. B.

(sin.) atlantica puncticulata fragori metz-

Globorotalia zealandica Globorotalia

rina - badenen.

Diatom sp. 4 sp. Diatom 3 sp. Diatom

Neogloboquad. Globorotalia Bolboforma Bolbo.

Globige- PA Bolboforma

assemblage

assemblage assemblage assemblage saxonica assembl. seminuda assemblage

subglobosa grossus

Uvigerina tenuipustulata Uvigerina Uvigerina venusta Uvigerina

Plectofrondicularia alsatica Turrilina Globocassidul. Cibicides

assem. Uviger. assem. semior. guerchi Astiger. Rotalia.

bulimoi.

staesch. saproph.

Pliocene Miocene

Lower Miocene Lower Lower Pliocene Lower Upper Miocene Upper Oligocene Upper

Middle S Upper

Lower

Oligoc.

Group

Utsira Formation Utsira Formation Skade Hordaland Group Hordaland

land

Nordland L Nord- Well 25/10-2 (Sea floor = 111.6 mRKB)(Sea floor = 111.6 = Strontium isotope ages in million years ago = Depth in metres below the rig floor L S Lithostratigraphic = units PA = Series / subseries assemblages fossil or foraminiferal Planktonic = PB assemblages foraminiferal Benthic = mRKB Sr (Ma)

14.5- 15.3

5.5 5.8 9.0 17.8 -19 18.2-8.3 18.7-19.2 25.1

(Ma)

assembl. assembl. (dextral) assembl. (dextral) atlantica assemblage ciperoensis Globigerina

assemblage assemblage

ticulata bulloides

reticulata badenensis

Neogloboquadrina Lower - zealandica Globorotalia

talia punc- talia rina Diatom sp. 4 sp. Diatom 3 sp. Diatom

Bolboforma Bolboforma Globoro- PA Globige-

assembl.

Bolbofor-

ma fragori ma

assemblage assemblage saxonica assemblage staeschei guerichi assemblage assemblage feldensis

laria seminuda laria

Uvigerina pygmea langen- pygmea Uvigerina

Uvigerina venusta Uvigerina Astigerina - tenuipustulata Uvigerina Turrilina alsatica Turrilina

Plectofrondicu- PB - langeri pygmea Uvigerina

grossus pseudo. assembl. assembl.

Cibicides

Monspel.-

Pliocene

Upper Miocene Upper Miocene Lower Middle Miocene Middle Upper Oligocene Upper S Lower

Upper

Pliocene

Skade Formation Skade Group Hordaland SOUTHERN VIKING GRABEN Formation Utsira Nordland Group Nordland L Well 24/12-1 Well Group Nordland (Sea floor mRKB) = 135 m 740 520 720 820 760 620 780 920 700 480 460 940 580 440 640 840 980 560 680 880 540 860 500 660 800 600 960 900 1120 1140 1180 1160 1100 1240 1220 1020 1260 1200 1040 1080 1060 1000 assembl. assembl. assembl. Bolboforma metzmacheri B. spinosa/ rotunda B. Bolboforma - badenensis B. reticulata

Sr 15.5 16.0 15.8 16.0 16.2 19.3 20.5 19.6 21.1 23.7 23.9 24.4 24.4 24.9

(Ma) ?

Undefined Undefined

laevis forma

Bolbo-

assem.

assembl. assem.

assemblage staeschei guerich Astigerina Undefined seminuda sp. A sp.

Plectofr.- PB Nonion

canui

hauerii assem. Cerato- Pararot. bulimina

Miocene Lower Miocene Lower Upper S

Upper

Middle Oligoc.

Miocene

Formation Formation

(onshore) Odderud Formation Odderud Formation Arnum Bastrup Formation Bastrup

Klintinghoved Vejle Fjord Vejle the and zonation Sea (1989) North King’s to 25/10-2 calibrated 24/12-1 and wells and borehole Rødding the between analyses of strontium-isotope results main selected and assemblages of fossil Correlation L

Fm Fm Fm ning Brej- Gram Hodde Ørnhøj Fm DENMARK RØDDING BOREHOLE m 70 20 40 50 30 80 60 90 Fig. 4 110 170 210 120 140 130 150 180 240 160 190 100 250 220 230 200 Upper Oligocene and Lower Miocene are shown from the Rødding borehole, since only these particular data are considered to be reliable from this borehole. borehole. this from reliable be to considered are data particular these only since borehole, Rødding the from shown are Miocene Lower and Oligocene Upper Figure 4. Figure Rundberg (2007) and Eidvin et al. (2013). All the the All (2013). al. et Eidvin (2007) and & Rundberg Eidvin in found are discussions and results analysis Detailed 1993). & Spiegler, (Müller Plateau Vøring the 643 on 642 and Sites of ODP the zonation Bolboforma Fronval (1991) and & Sjøholm Jansen IRD curve is The after situ. in to close or situ in be to interpreted tests fossil on based are data strontium the but cuttings, ditch are samples Lorem ipsum Lorem NORWEGIAN JOURNAL OF GEOLOGY Correlation of the Upper Oligocene–Miocene deltaic to shelfal succession onshore Denmark with similar deposits 553

Palaeoclimate seaboard of the Norwegian–Greenland Sea before 2.75 Ma (Fronval & Jansen, 1996).

The global deep-sea δ18O record shows that a cool climate prevailed early in the Late Oligocene, but a warming trend started in the later part of Late Oligocene (Fig. Description of correlated areas and 9). This warming trend is also detected in NW Europe deposits (Utescher et al., 2009; Larsson et al, 2011); consequently, a warm temperate and humid climate persisted in the North Sea realm during the Oligocene. This warm Overview climate continued during the Early Miocene. The mean annual temperature was 19 to 20°C and the winters were The depocentre in the Norwegian–Danish Basin and frost free. The precipitation was in the order of 1300 to Jylland (the eastern North Sea Basin) received sediments 1500 mm per year (Utescher et al., 2009; Larsson et al., from the Southern Scandes mountains, with a general 2010, 2011; Rasmussen, 2013). Minor deteriorations progradation from north to south during the period. The in climate, the so-called Mi events (glaciation events in depocentre in the basinal areas of the UK and Norwegian Antarctica; Miller et al., 1998), resulted in short-spanned sectors of the North Sea, north of 58°N, received decreases in air temperature in the order of 2–5°C sediments from the Scotland–Shetland area. Because of (Larsson et al., 2010, 2011; Sliwinska et al., 2014). The the sedimentary infilling there was a gradual shallowing global mid Miocene Climatic Optimum apparently did of the northern North Sea basin in the Oligocene to the not have any distinct influence on the air temperature Pliocene. In other local depocentres along the coast of in the Danish North Sea area (Larsson et al., 2011). Norway, deposition of sandy sediments took place only In the Late Miocene and Pliocene, a minor climatic occasionally (Eidvin et al., 2013). deterioration occurred in Central Europe (Utescher et al., 2009), but in southern Scandinavian this decline is not observed during the Late Miocene (Larsson et al., 2011). Onshore Denmark (eastern North Sea Basin) Data from Central England also indicate that a relatively warm climate persisted during the Late Miocene (Pound In Jylland, Denmark, large areas have upper Paleogene & Riding, 2015). Also on Iceland, a warm temperate, and Neogene successions below the Quaternary glacial humid climate existed during the mid to early Late deposits. The Lower Miocene succession is characterised Miocene, with a shift to a cool temperate climate during by coarse-grained, dominantly sand-rich, fluvio-deltaic the latest Late Miocene (Denk et al., 2005). deposits interfingering with marine clay (Larsen & Dinesen 1959; Rasmussen & Dybkjær, 2005; Hansen A study of continuous late Neogene sediment sections & Rasmussen, 2008; Rasmussen et al., 2010). The delta from ODP Site 907 on the Iceland Plateau and ODP Sites was sourced from the Southern Scandes in Norway and 642, 643 and 644 on the Vøring Plateau (Norwegian Sea; Central Sweden and prograded towards the south and Fig. 8) showed a gradual and stepwise cooling of the southwest (Figs. 3 & 8). The deltaic succession, referred deep water of the Iceland–Norwegian Sea with major to the Ribe Group, is composed of three discrete units cooling events at approximately 11 and 6.4 Ma (Fronval referred to sequences B, C and D by Rasmussen (2004) & Jansen, 1996). The oldest ice-rafted debris (IRD) and is approximately 200 m thick with a gross thickness detected is dated to approximately 12.6 Ma. IRD from of sand up to 150 m. The abrupt incursion of sand in this event is also recorded in borehole 6704/12-GB1 on the southern part of the Norwegian–Danish Basin in the Vøring Plateau (Fig. 3; Eidvin et al., 1998, 2013). This the earliest Miocene is interpreted to be the result of an coincides with a decrease in mean annual temperature inversion of the basin and a possible coincident uplift of at middle and high latitudes, an intensification of the source area. The Ribe Group is succeeded by the mud- North Atlantic deep-water production, and a change in dominated Måde Group (Lower Nordland Group). The circulation patterns within the Iceland–Norwegian Sea, Måde Group was deposited in a fully marine depositional as indicated by a shift from extensive biogenic opal ooze setting that lasted from Middle–Late Miocene time in the deposition to carbonate accumulation on the Vøring eastern North Sea Basin. Onshore, the Måde Group is up Plateau. IRD records from both the Iceland Plateau and to 140 m thick and is subdivided into three sequences; E, the Vøring Plateau suggest further intensifications of F1 and F2 (Møller et al., 2009; Rasmussen, 2017). the Northern Hemisphere glaciations at approximately 6 Ma (Messinian). The onset of the large-scale Northern These deposits have been studied palynologically in more Hemisphere glaciations is dated to 2.75 Ma on the Vøring than fifty boreholes (including some offshore boreholes) Plateau and 2.9 Ma on the Iceland Plateau (Fronval and about twenty-five outcrops (Fig. 1). Dinocysts occur & Jansen, 1996). The different timing could imply in nearly all of the deposits. The palynological studies that the growth of the large ice sheets did not occur have resulted in a dinocyst zonation scheme of nineteen simultaneously in Greenland and Scandinavia. There is dinocyst zones spanning from the Oligocene–Miocene no evidence for the existence of glaciers along the eastern transition to the Pliocene (Dybkjær & Piasecki, 2010). 554 T. Eidvin et al.

N. PACHYD. (D.) ACOSTAENSIS ACOSTAENSIS

(LAD) N. (LAD) N. (FAD)

DERMA (S.) DERMA N. PACHY- N. N. ENSIS LOWER TICA (D) TICA TICA (S.) TICA ACOSTA- FORAM. N. ATLANT. (D.) N. ATLANT. N. ATLAN- PLANKT. N. MAYERI N. ATLAN- LATA GORI ENSIS B. FRA- B. COMPR. SITE 642+643 FORMA CALCAREOUS BOLBO- B. METZ- B. BADEN- B. LAEVIS MICROFOSSILS MACHERI B. RETICU- (BASED ON FADs) Müller & Spiegler 1993) (Spiegler & Jansen 1989, 6000 4000 No. IRD/g sed 2000 SITE 644/642 no data VØRING PLATEAU 0 9 8 7 11 10 6b 12 NSA 9 8c 12b 12a 11 10 8b 8a 7b 7a 6b 15 14 NSB 12c 16x 13b 13a (King 1989) 9c 13 12 11 10 9b 9a 16a NORTH SEA NORTH NSP (BASED ON LADs) 15c 14a 16b 15d 15b 15a 14b 4 6 8 0 2

10 12 14 16 18 20 22 24 26 28 30 32 34

(Ma)

UPPER MIDDLE LOWER UPPER LOWER UPPER LOWER

PLIOCENE MIOCENE OLIGOCENE SUB- CENE SERIES SERIES/ PLEISTO- This vertical scale differs Ma) (in from the that of three wells which are in metres. ?

25.8 14.4 15.5 16.4 26.2

(Ma)

12.9 13.1 17.7 18.0 18.5 19.2 20.8 21.4 21.4 22.1 21.8 22.5 22.1 23.5 24.0 24.4 23.6 24.8 24.9 24.3 24.2 25.9

assemblage praebulloides

(sinistral) assemblage (sinistral) . assembl triloba

Neogloboquadrina atlantica Neogloboquadrina quadrilobatus quadrilobatus Globigerina angustiumbilicata - Globigerina - angustiumbilicata Globigerina

Globigerina bulloides - bulloides Globigerina PA Globigerinoides

derma

N. pachy-

ass. (dex.) ass. (dex.) grossus

assemblage assemblage assemblage girandana assemblage assemblage inflata

Cibicides

subnodosum hannai soldanii Gyroidina boueanus Bulimina elongata - Elphidium - elongata Bulimina

hannai - hannai

Elphidiella - osnabrugensis Almaena Florilus Astigerina guerichi staeschei - - staeschei guerichi Astigerina Elphidium PB Elphidiella

antiqua

Bolivina

cf.

Miocene

Upper Oligocene Upper Lower Miocene Lower Upper Pliocene Upper S Middle

Marine mudstone Marine sandstone Glauconitic sandstone/mudstone

Well 25/1-8Well S

Hordaland Group Hordaland Skade Formation Skade Nordland Group Nordland = Strontium isotope ages in million years ago = Depth in metres below the rig floor (Sea floor mRKB) = 127 L L S Lithostratigraphic = units PA = Series / subseries assemblages fossil or foraminiferal Planktonic = PB assemblages foraminiferal Benthic = mRKB Sr (Ma) m 410 710 740 470 770 320 620 230 260 350 650 200 830 530 380 440 590 560 680 290 860 500 890 800 900 ?

26.2

4.5 5.2 13.3 13.4 13.4 19.4 19.9 20.6 20.3 20.5 20.5 20.5 22.1 23.3 23.9 24.1 23.9

(Ma)

ass. reticulata Assemblage assembl. bilicata

Bolboforma

Undefined assemblage 3 sp. Diatom

ass. angustium- Globigerina bulloides Globigerina

badenensis - - badenensis

Globigerina PA Bolboforma

boq.

ticulata assem. Neoglo- atlantica Globige.

quadrilo.

Globoro-

talia punc-talia triloba triloba (sin.) ass. (sin.) ass. elongata assemblage staeschei assemblage assembl. girardana assem. alsatica assemblage hannai

Bulimina guerichi Asterigerina subnodosum Elphidium Gyroidina soldanii Gyroidina Turrilina Cibicides grossus - Elphidiella - grossus Cibicides PB

assem.

assem. seminuda assem. F. boue- F.

E. pyg. - C.t.

Rotalia. Elph. ex. G. s. mam. Plectofron. anus - S. bullimoi. bulloides

Miocene

Lower Miocene Lower

SOUTHERN VIKING GRABEN Pliocene Upper Upper Oligocene Upper S Middle

Plio-

cene cene Lower Oligo- Lower

Well 25/2-10 S 25/2-10 Well Group Hordaland Group Hordaland Skade Formation Skade Nordland Group Nordland (Sea floor mRKB) = 141 Nordland L tion Utsira Forma- m 310 610 910 370 970 670 520 820 760 730 700 280 790 260 850 430 550 460 490 580 940 340 640 400 880 1120 1150 1180 1210 1270 1240 1420 1450 1330 1480 1030 1360 1390 1300 1090 1060 1000 ? assembl. assembl. assembl. Bolboforma metzmacheri Bolboforma - badenensis B. reticulata B. spinosa/ B. rotunda

15.5 16.0 15.8 16.0 16.2 19.3 20.5 19.6 21.1 23.7 23.9 24.4 24.4 24.9

(Ma)

Undefined Undefined

laevis forma

Bolbo-

assem.

assembl. assem.

assemblage staeschei guerich Astigerina Undefined seminuda sp. A sp.

Nonion PB Plectofr.-

canui

hauerii assem. Cerato- Pararot. bulimina

Miocene Lower Miocene Lower Upper S

Upper

Middle Oligoc.

Miocene

Formation Formation

(onshore) Arnum Formation Arnum Odderup Formation Odderup Bastrup Formation Bastrup

Klintinghoved Fjord Vejle L Fm Fm Fm ning Brej- Gram Hodde Ørnhøj Fm DENMARK RØDDING BOREHOLE m 70 20 40 50 30 80 60 90 110 170 210 120 140 130 150 180 240 160 190 100 250 220 230 200 Fig. 5 NORWEGIAN JOURNAL OF GEOLOGY Correlation of the Upper Oligocene–Miocene deltaic to shelfal succession onshore Denmark with similar deposits 555

Figure 5. Correlation of fossil assemblages and selected, main results of in alternation with thinner mudstones. In most parts, strontium-isotope analyses between the Rødding borehole and wells 25/2- the deposits are probably turbiditic in origin and were 10 S and 25/1-8 S calibrated to King’s (1989) North Sea zonation and the » probably deposited in quite deep parts of the shelf. The Bolboforma zonation of the ODP Sites 642 and 643 on the Vøring Plateau (Müller & Spiegler, 1993). Detailed analysis results and discussions are sandy successions in the wells 25/2-10 S and 25/1-8 S found in Eidvin & Rundberg (2007) and Eidvin et al. (2013). All the and the British well 9/09a-A 23 (Fig. 3) contain common samples are ditch cuttings, but the strontium data are based on fossil mollusc fragments and lignite coal and have probably tests interpreted to be in situ or close to in situ. The IRD curve is after been deposited in mainly shallow water (Eidvin et al., Jansen & Sjøholm (1991) and Fronval & Jansen (1996). Sr data only from 2013; Eidvin, 2016). All of these wells are situated within the Upper Oligocene and Lower Miocene are shown from the Rødding the deltaic Hutton sand area as defined by Gregersen & borehole, since only these particular data are considered to be reliable from this borehole. Johannessen (2007). As seen in figure 3, the Hutton sand extends into the Norwegian sector and continues into the deeper water Skade Formation. The Skade sands pinch out towards the lower slope of the Norwegian margin Central and northern North Sea to the east. It has been suggested that the sandy deposits are a result of an Early Miocene tectonic uplift event According to Eidvin et al. (2013), during late Rupelian affecting the East Shetland Platform, possibly associated to Chattian, sediments in the northernmost part of the with a renewed compressional tectonic phase along the North Sea Basin were sourced from the northwestern part northwestern European margin (Rundberg & Eidvin, of the South Scandes Dome, which was a topographic 2005). high throughout the Paleogene. In the northeastern part of the northern North Sea off Nordfjord, sandy During the Middle Miocene, sediments continued to gravity-flow sediments were deposited (Ull formation, be deposited from the East Shetland Platform. In the an informal name suggested by Eidvin et al., 2013). northern North Sea, these deposits form a part of the Farther south off Hordaland and Sogn and Fjordane, a Hutton sand succession in the UK sector and represent distinct wedge of Rupelian organic-rich mudstones was the basal part of the Nordland Group occurring as an formed along the coast. Deltaic complexes prograded infilling unit within the Viking Graben in the Norwegian southwards into the Norwegian–Danish Basin (Vade sector. The sediments are sandy on the East Shetland Formation and the sand-rich part of the Lark Formation, Platform and in the western and northern parts of the and the Dufa and Freja members in Danish waters). In Viking Graben. In the eastern and southern parts and the latest Rupelian to Chattian there was a large input south of the Viking Graben, the deposits are mainly of sandy sediments from the Shetland Platform into the silty and clayey. Sandy Middle Miocene sediments are northern North Sea. Most of the sediments were laid recorded in wells 25/1-8 S, 25/2-10 S (western Viking down in the southern Tampen area (the informal Ull Graben), 26/10-1 (southeastern Viking Graben), 9/09a-A formation). Farther south, Chattian deposits are recorded 23 (East Shetland Platform, UK sector), 16/3-5 (southern below the Skade Formation in the Frigg Field area, i.e., Viking Graben, may be part of an injectite), 15/9-13 within the area belonging to the Hutton Sand according (southern Viking Graben) and 30/5-2 and 30/6-3 (170 m to Gregersen & Johannessen (2007). Elsewhere, in the thick; northern Viking Graben; Fig. 3; Eidvin et al., 2013; central and northern North Sea, mainly argillaceous Eidvin, 2016). Especially the Middle Miocene section in sediments were deposited. well 25/1-8 S was probably deposited at a very shallow- marine site. In the shallow-marine environment it may In large parts of the Viking Graben (northern North be difficult to distinguish these sands from sands of Sea), a sandy section, sourced from the East Shetland the Utsira Formation above and the Skade Formation Platform, makes up a great proportion of the Lower below, and they are believed to act as one aquifer Miocene Skade Formation. More than 500 exploration system (Halland et al., 2011, updated 2019; Eidvin et al., wells have penetrated the Lower Miocene deposits, and 2013). In spite of being noisy, seismic data show that selected wells have been investigated for benthic and in the Middle Miocene or possible Lower Miocene, an planktonic foraminifera, pyritised diatoms and 87Sr/86Sr eastward-prograding delta system was developed in the ratios (marked with red dots in Fig. 3; Eidvin et al., Frigg area. Wells 25/1-8 S and 9/09a-A 23 penetrated the 2013). One well from the East Shetland Platform, in sandy deposits in the delta plain while well 25/2-10 S was the British North Sea sector, has also been investigated drilled east of the clinoform belt. A thick depocentre of (Eidvin, 2016). The Skade Formation reaches a Middle Miocene sands was developed east and north maximum thickness of up to 400 m (Eidvin et al., of the Frigg area in a more distal shelf environment 2013). In the British sector, the Lower Miocene sandy (sands penetrated in wells 30/5-2 and 30/6-3; figure 12 in deposits constitute a part of the Hutton sand succession. Eidvin et al., 2013). The Middle Miocene sandy sections Hutton sand is an informal term used in the UK sector appear to form mappable units which are clearly younger by several oil companies to describe all sands above than the Skade Formation and older than the Utsira the Lower Eocene Balder Formation in the Northern Formation in the Viking Graben. Eidvin et al. (2013) North Sea (British Geological Survey, 2000). The Skade tentatively introduced the name Eir formation, after an Formation comprises a succession of amalgamated sands Æsir (god) in Norse mythology, for these units in the 556 T. Eidvin et al.

N. PACHYD. (D.) ACOSTAENSIS ACOSTAENSIS

are in metres.

(LAD) N. (LAD) N. (FAD)

DERMA (S.) DERMA N. PACHY- N. N. ENSIS LOWER TICA (D) TICA TICA (S.) TICA ACOSTA- FORAM. N. ATLANT. (D.) N. ATLANT. N. ATLAN- PLANKT. N. MAYERI N. ATLAN- LATA GORI ENSIS B. FRA- B. COMPR. SITE 642+643 FORMA CALCAREOUS BOLBO- B. METZ- B. BADEN- B. LAEVIS MICROFOSSILS MACHERI B. RETICU- (BASED ON FADs) Müller & Spiegler 1993) (Spiegler & Jansen 1989, 6000 4000 No. IRD/g sed 2000 SITE 644/642 no data VØRING PLATEAU 0 9 8 7 11 10 6b 12 NSA 9 8c 12b 12a 11 10 8b 8a 7b 7a 6b 14 15 NSB 12c 16x 13b 13a (King 1989) 9c 13 12 11 10 9b 9a 16a NORTH SEA NORTH NSP (BASED ON LADs) 15c 14a 15d 16b 15b 15a 14b 4 6 8 0 2

10 12 14 16 18 20 22 24 26 28 30 32 34

(Ma)

UPPER MIDDLE LOWER UPPER LOWER UPPER LOWER

PLIOCENE MIOCENE OLIGOCENE SUB- CENE SERIES SERIES/ PLEISTO- This vertical scale (in Ma) differs from that of the three wells which This vertical scale (in Ma) differs ?

N. PACHYD. (D.) ACOSTAENSIS ACOSTAENSIS

are in metres.

(LAD) N. (LAD) N. (FAD)

Sr 6000

16.4 14.4 15.5 26.2 25.8

(Ma)

12.9 21.8 22.5 23.5 24.0 24.4 23.6 24.8 24.9 24.3 24.2 25.9 13.1 17.7 18.0 18.5 19.2 20.8 21.4 21.4 22.1 22.1

assemblage praebulloides (sinistral) assemblage (sinistral) . assembl triloba

Neogloboquadrina atlantica Neogloboquadrina quadrilobatus quadrilobatus

4000 Globigerina - angustiumbilicata Globigerina Globigerina bulloides - bulloides Globigerina PA Globigerinoides

derma

N. pachy-

ass. (dex.) ass. (dex.) grossus

assemblage assemblage assemblage girandana assemblage assemblage No. IRD/g sed inflata

2000 Cibicides hannai subnodosum soldanii Gyroidina boueanus SITE 644/642 Elphidium - elongata Bulimina

no data

hannai - hannai

Elphidiella - osnabrugensis Almaena Florilus Astigerina guerichi staeschei - - staeschei guerichi Astigerina Elphidium PB Elphidiella

antiqua

VØRING PLATEAU

0 Bolivina

cf.

Miocene

Lower Miocene Lower Oligocene Upper

Upper Pliocene Upper 9 8 7 Middle 11 10 6b 12 S NSA

Marine mudstone Marine sandstone Glauconitic sandstone/mudstone

Well 25/1-8Well S

Skade Formation Skade Group Hordaland Nordland Group Nordland = Strontium isotope ages in million years ago 9 = Depth in metres below the rig floor (Sea floor mRKB) = 127 8c 12b 12a 11 10 8b 8a 7b 7a 6b 15 14 NSB L 12c 16x 13b 13a (King 1989) L age) on based shelf; (Norw. units lithostratigraphic corresponding Suggested = SLU Lithostratigraphic = units S PA = Series / subseries assemblages fossil or foraminiferal Planktonic = PB assemblages foraminiferal Benthic = mRKB Sr (Ma) 9c 13 12 11 10 9b 9a 16a NORTH SEA NORTH NSP (BASED ON LADs) 15c 14a 15b 15a 16b 15d 14b m 4 6 8 0 2 10 12 14 16 18 20 22 24 26 28 30 32 34

(Ma) 410

710 740 470 770 320 620 230 260 350 650 200 830 530 380 440 590 560 680 290 860 500 890 800 900 ?

UPPER MIDDLE LOWER UPPER LOWER LOWER SOUTHERN VIKING GRABEN UPPER

PLIOCENE MIOCENE OLIGOCENE SUB- CENE SERIES SERIES/ PLEISTO- This vertical scale (in Ma) differs from that of the three wells which This vertical scale (in Ma) differs ?

Sr 4.1+5.0+10.0+10.1 14.6+17.1 2x18.6+18.7 19.0+19.5+19.7+20.3 19.1+19.4+20.1+20.3 20.2+21.5+21.8 22.6+23.5+23.6 20.4+22.7+23.6 28.9 29.2 29.4 30.4+31.0+31.1

(Ma)

2x13.5+14.6 24.3+2x24.5+27.6 25.1+25.2+25.3+27.7+28.1 25.9+26.9 25.3+25.6+26.8 25.1+26.9+27.4+27.6+29.0 30.0 13.0+13.9 16.4+2x17.1 17.5+18.6+18.7 2x24.9+25.3

assembl.

asemblage bulloides assemblage praebulloides Globigerina

bulloides

Undefined

nensis

rina Globigerina prae- Globigerina Globigerina angustiumbilicata - angustiumbilicata Globigerina

B. bade- B. PA Globige-

derma fined

Unde-

(sin) ass. (sin)

N. pachy- N.

assemblage assemblage

assembl. staeschei

assemblage girardana soldanii Gyroidina

boueanus subnodosum Astigerina guerichi Astigerina

Elphidium PB Florilus

fined

Unde-

assembl. H. ordic. H. E. hannai E.

E. excav. -

Pliocene

Miocene

Lower Upper Oligocene Upper Oligocene Lower

Sr Miocene Lower

16.4 14.4 15.5 26.2 25.8

(Ma) - Miocene

12.9 Middle 21.8 22.5 23.5 24.0 24.4 23.6 24.8 24.9 24.3 24.2 25.9 13.1 17.7 18.0 18.5 19.2 20.8 21.4 21.4 22.1 22.1

assemblage S praebulloides

(sinistral) assemblage (sinistral) . assembl triloba

cene Upper

U. Plio. Neogloboquadrina atlantica Neogloboquadrina

Pleisto- quadrilobatus Globigerina angustiumbilicata - Globigerina - angustiumbilicata Globigerina

Form. (inform.) Form. Group tion

(Ull Formation (informal) Formation (Ull Globigerina bulloides - bulloides Globigerina

PA Globigerinoides Skade Formation Skade Group Hordaland

Group (Eir Group land derma Forma-

(Sea floor mRKB) = 173 N. pachy- Group Hordaland

ass. (dex.) ass. (dex.) grossus

assemblage assemblage girandana assemblage assemblage inflata assemblage Nordland Nord- Utsira

Cibicides 9/09a-A23Well (UK)

SLU

hannai soldanii Gyroidina boueanus Bulimina elongata - Elphidium - elongata Bulimina subnodosum

hannai - hannai tiated

Elphidiella - osnabrugensis Almaena Florilus Astigerina guerichi staeschei - - staeschei guerichi Astigerina Elphidium

Hutton Sand (informal) Sand Hutton Lark Formation Lark

PB Elphidiella antiqua

feren- Bolivina

cf.

L Undif- Miocene

Upper Pliocene Upper Miocene Lower Oligocene Upper S Middle

Marine mudstone Marine sandstone Glauconitic sandstone/mudstone

Well 25/1-8Well S

Skade Formation Skade Group Hordaland Nordland Group Nordland = Strontium isotope ages in million years ago m = Depth in metres below the rig floor (Sea floor mRKB) = 127 L 410 710 740 470 770 320 620 920 250 260 350 650 830 950 530 380 440 590 560 680 290 860 500 890 800 960 EAST SHETLAND PLATFORM ? L age) on based shelf; (Norw. units lithostratigraphic corresponding Suggested = SLU Lithostratigraphic = units S PA = Series / subseries assemblages fossil or foraminiferal Planktonic = PB assemblages foraminiferal Benthic = mRKB Sr (Ma) m 410 710 740 470 770 320 620 230 260 650 350 200 830 530 380 440 590 680 560 290 860 500 890 800 900 ? SOUTHERN VIKING GRABEN assembl. assembl. assembl.

Sr 4.1+5.0+10.0+10.1 14.6+17.1 2x18.6+18.7 19.0+19.5+19.7+20.3 19.1+19.4+20.1+20.3 20.2+21.5+21.8 22.6+23.5+23.6 20.4+22.7+23.6 28.9 29.2 29.4 30.4+31.0+31.1

(Ma)

2x13.5+14.6 24.3+2x24.5+27.6 25.1+25.2+25.3+27.7+28.1 25.9+26.9 25.3+25.6+26.8 25.1+26.9+27.4+27.6+29.0 30.0 13.0+13.9 16.4+2x17.1 17.5+18.6+18.7 2x24.9+25.3

assembl.

Bolboforma metzmacheri assembl. Bolboforma - badenensis B. reticulata B. spinosa/ B. rotunda

asemblage bulloides assemblage praebulloides Globigerina

bulloides

Undefined

nensis

rina Globigerina prae- Globigerina Globigerina angustiumbilicata - angustiumbilicata Globigerina

B. bade- B. PA Globige-

derma fined

Sr Unde-

(sin) ass. (sin) 15.5 16.0 15.8 16.0 16.2 19.3 20.5 19.6 21.1 23.7 23.9 24.4 24.4 24.9

N. pachy- N.

(Ma) assemblage assemblage

assembl. staeschei

Undefined Undefined assemblage girardana soldanii Gyroidina

boueanus subnodosum Astigerina guerichi Astigerina

Elphidium PB Florilus PA

fined

laevis forma

Unde-

Bolbo-

assem. assembl.

H. ordic. H. E. hannai E.

E. excav. -

Pliocene assembl. assem.

Miocene

assemblage staeschei guerich Astigerina Undefined Lower Lower Miocene Lower Oligocene Upper Oligocene Lower

seminuda sp. A sp.

Miocene - Miocene Middle

Plectofr.- S Nonion Upper PB

canui cene

U. Plio.

hauerii

assem.

Cerato- Pararot. Pleisto- bulimina

Form. (inform.) Form. Group tion

(Ull Formation (informal) Formation (Ull

Miocene

Lower Miocene Lower

Skade Formation Skade Group Hordaland

Group (Eir Group land Forma-

(Sea floor mRKB) = 173 Upper

S Group Hordaland Nordland Nord-

Well 9/09a-A23Well (UK) Utsira

SLU

Upper

Middle

Oligoc.

Miocene

Formation Formation

tiated

(onshore) Arnum Formation Arnum Hutton Sand (informal) Sand Hutton Odderup Formation Odderup Bastrup Formation Bastrup Lark Formation Lark

feren- Vejle Fjord Vejle Klintinghoved

L L Undif- zonation Sea (1989) North King’s to 25/1-8 S calibrated 9/09a-A 23 (UK) and wells and borehole Rødding the between analyses of strontium-isotope results main selected and assemblages of fossil Correlation Fm Fm Fm ning Brej-

Gram Hodde Ørnhøj Fm DENMARK RØDDING BOREHOLE m m 410 710 740 470 70 770 20 320 40 620 920 50 30 250 80 60 90 260 350 650 950 830 530 380 440 590 560 680 290 860 890 500 800 960 EAST SHETLAND PLATFORM 110 170 210 120 140 130 150 180 240 160 190 100 250 220 230 200 Fig. 6 Spiegler, 1993). Detailed analysis results and discussions are found in Eidvin et al. (2013) and Eidvin (2016). All the samples samples the All (2016). Eidvin (2013) and al. et Eidvin in found are discussions and results analysis Detailed 1993). & Spiegler, (Müller Plateau Vøring the 643 on 642 and Sites of ODP the zonation Bolboforma the and the from only data Sr (1996). & Jansen Fronval (1991) and & Sjøholm Jansen IRD curve is The after situ. in to close or situ in be to interpreted tests fossil on based mainly are data strontium the but cuttings, ditch are borehole. this from reliable be to considered are data particular these only since borehole, Rødding the from shown are Miocene Lower and Oligocene Upper Figure 6. Figure ? assembl. assembl. assembl. Bolboforma metzmacheri Bolboforma - badenensis B. reticulata B. spinosa/ B. rotunda

15.5 16.0 15.8 16.0 16.2 19.3 20.5 19.6 21.1 23.7 23.9 24.4 24.4 24.9

(Ma)

Undefined Undefined

laevis forma

Bolbo-

assem.

assembl. assem.

assemblage staeschei guerich Astigerina Undefined seminuda sp. A sp.

Plectofr.- PB Nonion

canui

hauerii assem. Cerato- Pararot. bulimina

Miocene Lower Miocene Lower Upper S

Upper

Middle Oligoc.

Miocene

Formation Formation

(onshore) Arnum Formation Arnum Odderup Formation Odderup Bastrup Formation Bastrup

Klintinghoved Vejlefjord L Fm Fm Fm ning Brej- Gram Hodde Ørnhøj Fm DENMARK RØDDING BOREHOLE m 70 20 40 50 30 80 60 90 110 170 210 120 140 130 150 180 240 160 190 100 250 220 230 200 Fig. 6 NORWEGIAN JOURNAL OF GEOLOGY Correlation of the Upper Oligocene–Miocene deltaic to shelfal succession onshore Denmark with similar deposits 557

Norwegian sector, representing a new formation in the Material and methods Nordland Group (Fig. 10).

During the Late Miocene to Early Pliocene, the northern Strontium isotope analyses North Sea apparently formed a narrow seaway between the deeper water in the Møre Basin and the central North Eidvin et al. (2014a) obtained 87Sr/86Sr ratios of 143 Sea. The central North Sea received large amounts of samples from 18 localities from the Upper Oligocene coarse sand (Utsira Formation). The Utsira Formation to Upper Miocene Danish succession. Fifty-four of represents a huge sedimentary depositional system in the these samples were from the Rødding well (Fig. 1). The northern North Sea (about 450 km long and 90 km wide; analyses were mainly carried out on fragments of mollusc Fig. 3), comprising one large sandy depocentre (250–300 shells, tests of foraminifera and Bolboforma, in addition m in the southern Viking Graben) and an area with to one sample representing a shark tooth. The collected 80–100 m-thick sandy deposits in the northern Viking shell material was supplemented with mollusc shells Graben (figure 11 in Eidvin et al., 2013; Halland et al., picked from the collection of Leif Banke Rasmussen, 2011, updated 2019). The western central area of the stored at the Geological Museum in Copenhagen Viking Graben comprises a large deltaic system which (Rasmussen, 1966). The results were presented in Eidvin prograded eastwards in the Early and Middle Miocene. et al. (2014a). However, since the strontium isotope Here, Upper Miocene to Lower Pliocene sediments of data from the Middle–Upper Miocene are uncertain, as the Utsira Formation are thin or absent due to lack of mentioned above, only strontium isotope data from the accommodation space (Fig. 10). Numerous wells have Upper Oligocene–Lower Miocene part (94 samples from penetrated these deposits, and several of these have been 18 localities) have been used for the correlation in the investigated for benthic and planktonic foraminifera, present paper. These are listed in Table 1. Bolboforma and 87Sr/86Sr ratios (marked with red dots in Fig. 3; Eidvin et al., 2013). Apparently, the progradation of the delta front stopped in the Middle/Late Miocene. Biostratigraphy The sediments were transported to the delta slope and the shallow shelf beyond the delta, suggesting a relative Micropalaeontological investigations in the Rødding fall in sea level. In the Tampen area to the north, the borehole were based on analyses of planktonic and Utsira Formation is represented by a thin glauconitic benthic foraminifera and Bolboforma. Pyritised diatoms unit dated to the latest Miocene to Early Pliocene. There, were also used to establish a stratigraphy for the Upper it is overlying Oligocene and Lower Miocene deposits. Oligocene–Lower Miocene part (see Eidvin et al., 2013). Offshore western Norway, north of the Troll Field a sandy deltaic system developed. This delta was probably The fossil assemblages are mainly correlated with the fed by the Sognefjorden paleo-valley (Fig. 13). In the micropalaeontological zonation for Cenozoic sediments western part of the Norwegian sector blocks 30 and 25, of King (1983, 1989). The zonations based on Bolboforma the Utsira Formation merges with parts of the Hutton species (Spiegler & Müller, 1992; Müller & Spiegler, sand (see Fig. 3). 1993; Spiegler, 1999) from ODP and DSDP drillings in the Norwegian Sea and the North Atlantic are very important for dating the Middle–Upper Miocene part Norwegian Sea shelf of the column. Correlation with these zones yields the most accurate age determinations, because the zones are In the Late Miocene, coastal plains and deltas of the calibrated with both nannoplankton and palaeomagnetic Molo Formation built out along the inner continental data. shelf of the Norwegian Sea (Eidvin et al., 2013; Grøsfjeld et al., in press and unpublished dinocyst data (personal observations)). In the northern distribution area off Vesterålen, this has been interpreted to be due to a relative sea-level fall probably mainly caused by uplift Correlation of the coastal zone/mainland (Grøsfjeld et al., in press). Here, in the northeastern part of the distribution of the Molo Formation (well 6610/3-1), the progradation of The strontium isotope analyses of samples from the coastal sand initiated in the Tortonian (Grøsfjeld et al., in Danish Brejning, Vejle Fjord, Klintinghoved, Arnum press). In the southern part of its distribution, the Molo and Odderup formations gave ages between 25.7 (Late Formation (Draugen Field, Trøndelag Platform) contains Oligocene) and 15.5 Ma (early Middle Miocene; Fig. glauconite sand (Eidvin et al., 2013). On the shelf to the 2). These sediments, which have also been analysed west, clayey and hemipelagic sediments accumulated, for foraminifera and pyritised diatoms in the Rødding whereas on the slope and rise pelagic ooze was deposited borehole (Figs. 1 and 3; Eidvin et al., 2013), can be (middle/upper part of the Kai Formation). correlated with deposits from a number of lithological units in the Norwegian North Sea and the East Shetland

558 T. Eidvin et al.

ACOSTAENSIS ACOSTAENSIS

N. PACHYD. (D.)

(LAD) N. (LAD) N. (FAD)

DERMA (S.) DERMA N. PACHY- N. N. ENSIS LOWER TICA (D) TICA TICA (S.) TICA ACOSTA- FORAM. N. ATLANT. (D.) N. ATLANT. N. ATLAN- PLANKT. N. MAYERI N. ATLAN- LATA GORI ENSIS B. FRA- B. COMPR. SITE 642+643 FORMA CALCAREOUS BOLBO- B. METZ- B. BADEN- B. LAEVIS MICROFOSSILS MACHERI B. RETICU- (BASED ON FADs) Müller & Spiegler 1993) (Spiegler & Jansen 1989, 6000 4000 No. IRD/g sed 2000 SITE 644/642 no data VØRING PLATEAU 0 9 8 7 12 11 10 6b NSA 9 12b 8c 12a 11 10 8b 8a 7b 7a 6b 15 14 NSB 12c 16x 13b 13a (King 1989) 9c 13 12 11 10 9b 9a 16a NORTH SEA NORTH NSP (BASED ON LADs) 15c 16b 14b 15d 15b 15a 14a 4 6 8 0 2

10 12 14 16 18 20 22 24 26 28 30 32 34

(Ma)

UPPER MIDDLE LOWER UPPER LOWER UPPER LOWER

PLIOCENE MIOCENE OLIGOCENE SUB- CENE SERIES SERIES/ PLEISTO- are in metres. differs in vertical whichThis are the wells three of from Ma) scale that (in

6.0+6.4 (Ma)

assemblage

assemblage assembl. (sin.) atlantica assemblage fragori B. assemblage

metzmachheri

Globigerina bulloides Globigerina Neogloboquadrina - subfragori Bolboforma sp. Cenosphaera

PA Bolboforma

assemblage tabilis

ass. telegdi

assemblage assembl. pygmeus assemblage assemblage

tammina spec- tammina

Cibicides

Cibicides grossus Cibicides Eponides saxonica venusta Uvigerina communis Mattinottiella

Spiroplec- PB pygmeus- E.

Eocene Lower Pliocene Lower Pliocene

Upper Miocene Upper

Lower - Middle - Lower Upper Miocene - - Miocene Upper S Upper

Log Log

Well 6508/5-1 Formation Formation

(Sea floor = 435 mRKB) Formation Kai Brygge L Naust Helgeland Basin m 1170 1140 1130 1130 1150 1310 1180 1210 1160 1190 1370 1270 1240 1320 1250 1280 1220 1260 1200 1350 1330 1290 1380 1340 1360 1400 1390 1300 = Strontium isotope ages in million years ago = Depth in metres below the rig floor L S Lithostratigraphic = units PA = Series / subseries assemblages fossil or foraminiferal Planktonic = PB assemblages foraminiferal Benthic = PD Dinoflagellate zones = mRKB Sr (Ma) NORWEGIAN SEA SHELF SEA NORWEGIAN

Sr 5.7 5.2 30.3

5.8 (Ma) assemblage assembl.

(sinistral) assemblage (sinistral)

metzmacheri Undefined sp. 4 sp.

Neogloboquadrina atlantica Neogloboquadrina

Bolboforma

PA Diatom

loides G. bul-

assem.

assemblage assemblage assemblage

assemblage assemblage fined

pseudotepida subglobosa bulimoides

Elphidiella hannai Elphidiella Eponides pygmeus Eponides Unde-

Globocassidulina Rotaliatina PB Monspeliensina

Miocene Miocene

Upper Pliocene Upper Lower Oligocene Lower Lower Pliocene Lower

Lower S Upper

Log

Marine mudstone Marine sandstone Glauconitic sandstone/mudstone

Well 6407/9-5 Well Molo Formation Molo Formation Brygge Naust Formation Naust (Sea floor mRKB) = 319 L Trøndelag Platform Trøndelag m 710 740 810 670 750 770 720 760 820 780 730 700 630 790 650 850 830 640 680 840 860 660 690 800 assembl. assembl. assembl. Bolboforma metzmacheri Bolboforma - badenensis B. reticulata B. spinosa/ B. rotunda

15.5 16.0 15.8 16.0 16.2 19.3 20.5 19.6 21.1 23.7 23.9 24.4 24.4 24.9

(Ma)

Undefined Undefined

laevis forma

Bolbo-

assem.

assembl. assem.

assemblage staeschei guerich Astigerina Undefined seminuda sp. A sp.

Plectofr.- PB Nonion

canui

hauerii assem. Cerato- Pararot. bulimina

Miocene Lower Miocene Lower Upper S

Upper

Middle Oligoc.

Miocene

Formation Formation

(onshore) Odderup Formation Odderup Formation Arnum Bastrup Formation Bastrup

Klintinghoved Fjord Vejle L Fm Fm Fm ning Brej- Gram Hodde Ørnhøj Fm DENMARK RØDDING BOREHOLE m Fig. 7 70 20 40 50 30 80 60 90 110 170 210 120 140 130 150 180 240 160 190 100 250 220 230 200 NORWEGIAN JOURNAL OF GEOLOGY Correlation of the Upper Oligocene–Miocene deltaic to shelfal succession onshore Denmark with similar deposits 559

Figure 7. Correlation of Bolboforma between the Rødding borehole metzmacheri assemblage are recorded in the Ørnhøj and and wells 6407/9-5 and 6508/5-1, calibrated to King’s (1989) North Sea Gram formations. In well 24/12-1, a Bolboforma fragori zonation and the Bolboforma zonation of the ODP Sites 642 and 643 on » assemblage is recorded from the lowermost part of the the Vøring Plateau (Müller & Spiegler, 1993). Detailed analysis results and discussions are found in Eidvin et al. (2007, 2013). All the samples Utsira Formation. In well 25/10-2 a Bolboforma fragori are ditch cuttings, but the strontium data are mainly based on fossil tests assemblage and a Bolboforma metzmacheri assemblage interpreted to be in situ or close to in situ. The IRD curve is after Jansen are recorded from the lower part of the Utsira Formation & Sjøholm (1991) and Fronval & Jansen (1996). Sr data only from the (see also Eidvin et al., 2013). These assemblages correlate Upper Oligocene and Lower Miocene are shown from the Rødding with a Bolboforma fragori/Bolboforma subfragori Zone borehole, since only these particular data are considered to be reliable (accurately dated to 11.7–10.3 Ma, earliest Late Miocene), from this borehole. Bolboforma laevis Zone (10.3–10.0 Ma, Late Miocene; B. laevis is also present in the B. fragori/Bolboforma subfragori Zone) and Bolboforma metzmacheri Zone Platform, which have been investigated applying similar (10.0–8.7 Ma, Late Miocene) on the Vøring Plateau methodology. These include the Hutton sand (informal; (Quale & Spiegler, 1989; Spiegler & Müller, 1992; Müller East Shetland Platform), clay-rich deposits of the & Spiegler, 1993). Hordaland Group (central, southeastern and northern North Sea), the sandy Skade Formation (northern North Based on Sr and benthic foraminiferal data, the Brejning Sea) and the sandy Eir formation (informal; Figs. 10 & Formation in the Rødding borehole correlates with 11). Some of these correlations are visualised in detail the Upper Oligocene part of the Hordaland group in (Figs. 4–7). wells 25/2-10 S and 25/1-8 S in the southern Viking Graben and King’s (1989) NSB Zone 8 from the Figure 4 shows that, based on Sr isotope and benthic North Sea (Fig. 5). The Vejle Fjord, Klintinghoved and foraminiferal data, the Brejning Formation in the Bastrup formations and the lower part of the Arnum Rødding borehole correlates with the Upper Oligocene Formation in the Rødding borehole correlate with the part of the Hordaland Group in wells 24/12-1 and Skade Formation in well 25/2-10 S. The Vejle Fjord, 25/10-2 in the southern Viking Graben and King’s Klintinghoved and Bastrup formations and the whole (1989) NSB Zone 8 from the North Sea. The Vejle Fjord of the Arnum Formation correlate with the Skade Formation in the Rødding borehole correlates with the Formation in well 25/1-8 S. All of these units correlate Lower Miocene part of the Hordaland Group, below the in turn with the NSB 9 Zone and NSB 10 Zone of King Skade Formation, in well 24/12-1, the Lower Miocene (1989). part of the Hordaland Group, lower part of the Skade Formation in well 25/10-2 and the lower main part of the According to Figure 5, the correlation of the Hodde NSB Zone 9 of King (1989). The Klintinghoved, Bastrup, Formation in the Rødding borehole is based mainly on Arnum and Odderup formations correlate with the main Bolboforma assemblages. The Bolboforma badenensis– part of the Skade Formation in well 24/12-1 and the Bolboforma reticulata assemblage correlates with similar upper main part of the Skade Formation in well 25/10-2 assemblages in the sandy lowermost part of the Nordland and King’s (1989) NSB Zone 10 and the upper part of Group (suggested to be named the Eir formation by NSB Zone 9. Eidvin et al., 2013) situated between the Skade and Utsira formations in wells 25/2-10 S and 25/1-8 S. These The correlation of the Hodde, Ørnhøj and Gram assemblages correlate in turn with the Bolboforma formations in the Rødding borehole is based on badenensis–Bolboforma reticulata Zone of Müller & Bolboforma assemblages. Similar Bolboforma Spiegler (1993) from the Vøring Plateau (Norwegian Sea; assemblages, in the Hodde and Gram formations, Fig. 8), dated to slightly older than 14 to 11.7 Ma (Middle are recorded from the Gram, Lille Tønde and Borg-1 Miocene). Sediments with the same age as the Ørnhøj boreholes on the Ringkøbing High and in the North and Gram formations in the Rødding borehole are not German Basin (southern Jylland) by Laursen & present in the wells 25/2-10 S and 25/1-8 S (Fig. 5). Kristoffersen (1999, Fig. 8). Figure 4 shows that the Bolboforma badenensis–Bolboforma reticulata Figure 6 shows that, based mainly on Sr data, the Vejle assemblage in the Hodde Formation correlates with Fjord, Klintinghoved, Bastrup, Arnum and Odderup similar assemblages in the fine-grained lowermost part formations in the Rødding borehole correlate with the of the Nordland Group situated between the sandy Skade upper main part of the Hutton sand in well 9/09a-A 23. and Utsira formations in wells 24/12-1 and 25/10-2 (see also Eidvin et al., 2013). These assemblages correlate The Hodde Formation, based on the Bolboforma in turn with the Bolboforma badenensis–Bolboforma badenensis–Bolboforma reticulata assemblage in the reticulata Zone of Müller & Spiegler (1993) from the Rødding borehole, is correlated with a similar assemblage Vøring Plateau (Norwegian Sea; Fig. 8), which has been in well 9/09a-A 23. These assemblages correlate again dated accurately to slightly older than 14 to 11.7 Ma with the Bolboforma badenensis–Bolboforma reticulata (Middle Miocene; Spiegler & Müller, 1992). Bolboforma Zone of Müller & Spiegler (1993) from the Vøring of a Bolboforma laevis assemblage and a Bolboforma Plateau (Norwegian Sea; Fig. 8) which, as noted above, 560 T. Eidvin et al. has been dated accurately to slightly older than 14 to the North Sea was not in contact with an open ocean 11.7 Ma (Middle Miocene; Spiegler & Müller, 1992). The towards the east, west and south (Fig. 8). According to Ørnhøj and Gram formations in the Rødding borehole Løseth & Henriksen (2005) and Løseth et al. (2013) are tentatively correlated with the uppermost part of the a compressional phase and related major regression Hutton sand in well 9/09a-A 23. would have led to an isolation of the North Sea Basin. This compressional phase is shown as terminating Figure 6 also shows that, based on Sr and benthic approximately at the top Miocene (their figure 17). This foraminiferal data, most of the lower part of the Hutton partly reflects their estimate of the age of the Utsira sand in well 9/09a-A 23 correlates with the Hordaland Formation to the Early Pliocene. An opening to the south, Group in well 25/1-8 S and King’s (1989) NSB Zone in addition an opening to the north, formed first as late 8 from the North Sea. Based on the same kind of data, as in the late Pleistocene when repetitive mega-floodings, the middle part of the Hutton sand in well 9/09a-A 23 caused by breaching of rock dams at the Dover Strait, correlates with the Skade Formation in well 25/1-8 S instigated catastrophic drainages of large pro-glacial and the NSB 9 Zone and NSB 10 Zone of King (1989). lakes in the southern North Sea Basin. Two periods with Based on Sr and benthic foraminiferal data, Figure 6 catastrophic floods, after 450,000 but before 180,000 also shows that the Middle Miocene part of the Hutton years ago, formed bedrock-floored valleys. Thus, Britain sand in well 9/09a-A 23 correlates with the lower part of was isolated from continental Europe during high sea- the Nordland Group in well 25/1-8 S. Sediments with a level stands during the Eemian and Holocene (Sanjeev et similar age as the uppermost part of the Hutton sand in al., 2007; Gibbard, 2007, Gibbard & Cohen, 2015). well 9/09a-A 23 are not present in well 25/1-8 S. A major sea-level fall within the Late Miocene is Figure 7 shows that, based on Sr and pyritised diatoms indicated by a number of features, including deep (Diatom sp. 4 assemblage), the Klintinghoved and channelling beneath the Tortonian Deurne Member Bastrup formations and lower part of the Arnum in Belgium (Houthuys, 2014; Vandenberghe, 2014), Formation in the Rødding borehole correlate with the incision of Upper Miocene delta systems within the upper part of the Brygge Formation in well 6407/9-5 central North Sea (Møller et al., 2009) and the rapid (Trøndelag Platform) and Zone NSP 10 of King (1989) progradation of the Eridanos Delta into the central North from the North Sea. This correlation is verified by Sea Basin (Overeem et al., 2014; Kuhlmann et al., 2006; unpublished dinocyst data (personal observations). Patruno et al., 2019). However, there are no stratigraphic The upper part of the Gram Formation in the Rødding or sedimentological data suggesting a closure of the borehole is of a similar age as the lower part of the Molo basin. The incision of the pre-Deurne Member channels Formation in well 6407/9-5 and the middle part of the implies strong tidal currents, which are unlikely to have Kai Formation in well 6508/5-1 (Helgeland Basin; see been generated in a closed sea. In addition, in the thick Fig. 14), which again correlates with the Bolboforma and apparently continuous Upper Miocene succession in metzmacheri Zone (10.0–8.7 Ma, Late Miocene) on the central North Sea there are no signs of stratification, the Vøring Plateau (Spiegler & Müller, 1992; Müller & reduced salinity or lowered oxygenation which can Spiegler, 1993; also verified by unpublished dinocyst data be deduced from the sediments or the microfauna. (personal observations)). The key evidence is provided by the plankton. Several Bolboforma zones, described from and accurately dated in scientific boreholes from the Norwegian Sea and North Atlantic, up to and including the B. metzmacheri Discussion Zone (c. 10.0–8.7 Ma, through the Serravallian to mid Tortonian; Spiegler & Müller, 1992; Müller & Spiegler, 1993), are represented in the central North Sea Basin, The idealised palaeogeography for the Middle–Late onshore southern Denmark and in other onshore areas Miocene advocated by Løseth & Henriksen (2005) shows (King, 1989; Laursen & Kristoffersen, 1999; Eidvin & a situation with a large land area stretching from present- Rundberg, 2007; Eidvin et al., 2013), indicating the day Shetland Island to southern Norway (their figure existence of an open connection to the North Atlantic/ 15). Our divergent views on the geological history have Nordic seas throughout this period. The succeeding led to a discussion in geoscience journals including the B. intermedia Zone (c. 8.8–5.9 Ma: late Tortonian and following articles: Eidvin et al. (2013, 2014b), Løseth Messinian; Spiegler & Müller, 1992) is also identified et al. (2013), Rundberg & Eidvin (2016ab), Løseth et al. (though rarely) in both onshore and offshore areas (2016b), Løseth & Øygarden (2016), Eidvin & Rundberg (Chris King, personal communication). Planktonic (2016a, b) and Løseth (2016). In the present paper foraminifera are represented throughout almost all we want to document and elaborate our view more this interval in some areas. A succession of pteropod thoroughly. zones is identified through the early Tortonian (Gürs & Jansen, 2002). Planktonic foraminifera are represented According to several authors, including Knox et al. (quite commonly) through the Upper Miocene in the (2010) and Rasmussen et al. (2008), during the Miocene central North Sea Basin (e.g., well 2/4-C-11 (Eidvin et NORWEGIAN JOURNAL OF GEOLOGY Correlation of the Upper Oligocene–Miocene deltaic to shelfal succession onshore Denmark with similar deposits 561

14 13 Fig. 13 12 11

10 9 8 7 6

5 Fig. 13 4 3 1 2

Tortonian - Zanclean delta 1: Lille Tønde borehole 2: Borg-1 borehole Lower Miocene delta and fan deposits 3: Gram borehole Drainage routes 4: Rødding borehole Hypothetical drainage routes 5: Well 2/4-C-11 6: Well 24/12-1 Wells and boreholes shown in 7: Well 25/10-2 the correlation diagrams 8: Well 9/09a-A 23 (UK) (Figs. 4-7) 9: Well 25/2-10 S Scienti c deep-sea boreholes 10: Well 25/1-8 S Boreholes investigated by 11: Well 6407/9-5 Laursen and Kristoersen (1999) 12: Well 6508/5-1 Well investigated by Eidvin et al. 13: ODP Site 644 (1999, 2013) 14: ODP Site 642 Figure 8. Palaeogeographic reconstruction of the North Sea Basin and adjacent areas in the Miocene (after Knox et al., 2010; Rasmussen et al., 2008; Dybkjær & Piasecki, 2010). The extents of the Miocene deltas and fan deposits and possible drainage routes in Denmark are from figure 3. Hypothetical drainage routes for the Hutton sand and Skade Formation are modified from Halland et al. (2014) and Gjeldvik et al., (2011). The approximateFig. positions 8 of the wells and boreholes from the correlation diagrams in Figures 4–7 are indicated with red dots and numbers. Other wells and boreholes are indicated with black, green and blue dots. 562 T. Eidvin et al. High OD 1511005 Global sea level sea Low events Climate Temperature (°C) Temperature 0 10°

Nor. - Greenl. Sea 8° 1 6° 4° 2 2° O (‰) 18 0° 3 δ Partial or ephemeral ice sheets scale and permanentFull ice sheets New IRD data from ODP 913 Site Greenland) East (off IRD data from the Ridge Lomonosov 4

IRD Lomonosov Ridge 5 Molo Brygge Brygge basins Brygge Kai Møre/Vøring Brygge Kai Naust N Eidvin (2005), Rasmussen et al. (2008) and Eidvin et al. (2013). On the right-hand side of the diagram some some diagram of the side right-hand On the (2013). al. et Eidvin and (2008) al. et Rasmussen (2005), Eidvin & Eir (inf.) Skade Northern North Sea Utsira Glauconitic Utsira Mb Utsira Glauconitic

Ull (informal) Ull

Grid

Nordland Hordaland Diatom ooze Vade Lark Southern North Sea Horda Freja Dufa Odderup Billund Bastrup Søvind Marbæk Clay and hemipelagicClay Gram Denmark Hodde Viborg Branden Arnum Brejning Vejle FjordVejle Klintinghoved Sand

General view of the Late Paleogene and Neogene lithostratigraphy modified after Rundberg Rundberg after modified lithostratigraphy Neogene and Paleogene view Late of the General Pliocene Miocene Oligocene Eocene

Age Neogene Paleogene Cenozoic Fig. 9 Fig. Figure 9. Figure palaeoclimatic data are added including a global deep-sea oxygen curve, bottom-water paleo-temperatures in the world’s oceans, periods with ice-sheets in Antarctica and the northern hemisphere (after Zachos et al., al., et Zachos (after hemisphere northern the and Antarctica in ice-sheets with periods oceans, world’s the in paleo-temperatures bottom-water curve, oxygen deep-sea a global including added are data palaeoclimatic 2006; al., et Backman Ocean; (Artic Ridge Lomonosov the on 2007) and al., et Eldrett 913 (off Greenland; East Site ODP of IRD at deposition with Periods (1998). al. et Hardenbol curve after sea-level a global 2001) and indicated also are 2008) John, St. 2006; al., et Moran NORWEGIAN JOURNAL OF GEOLOGY Correlation of the Upper Oligocene–Miocene deltaic to shelfal succession onshore Denmark with similar deposits 563 N 62° Hiatus Hiatus Utsira Fm Glauconitic (5.7-4.2 Ma) 24.1-23.4 Ma 32.7-31.5 Ma 27.2-25.7 Ma Ull fmUll (informal) Utsira Fm 5.5-5.2 Ma 8.7 Ma Viking Graben 12.2-10.4 Ma 14.1-13.0 Ma Eir fm (informal) 13.4-12.9 Ma 13.3-10.9 Ma 5.2-4.5 Ma Hiatus Frigg Area Frigg Skade Fm 19-16.4 Ma 24-23.9 Ma 15.9-15.5 Ma 5.3 Ma 11.3 Ma Utsira Fm 5.0-4.1 Ma Viking Graben 14.7 Ma 11.8-11.5 Ma 10.9-10.7 Ma 16.7-14.7 Ma 58° Vade Fm 26-26.3 Ma 57° 27.2-26.4 Ma 29.2-30.3 Ma gian Danish Basin Central Graben/Norwe-Central

56°30’ S 5.7-3.7 Ma 5.6-5.2 Ma 6.6 Ma 7.4 Ma 15.5 Ma 16.7 Ma 20.7 Ma 25.3 Ma 27.9 Ma

NORDLAND GROUP NORDLAND GROUP HORDALAND Gr. Late Late Early Early Epoch Hiatus Middle Eocene/ Pleistoc. Pliocene Miocene Miocene Miocene Oligocene Oligocene Post-Eocene lithostratigraphy of the Norwegian North Sea including main results of the strontium isotope analyses based on fossil tests interpreted to be in situ (after Eidvin et al., 2013). al., et Eidvin (after situ in be to interpreted tests fossil on based analyses isotope of strontium the results main including Sea North ofNorwegian the lithostratigraphy Post-Eocene

5 15 10 20 30 25 Age (Ma) Figure 10. Figure

Fig. 10 564 T. Eidvin et al.

0.70910

0.70900

0.70890

0.70880 Utsira Fm Odderup Fm

0.70870 Eir fm (informal) Arnum Fm

0.70860 Klintinghoved Fm

87Sr / 8687Sr Sr 0.70850 Skade Fm

0.70840 Vejle Fjord Fm Hutton sand Brejning Fm 0.70830 (informal)

0.70820

0.70810 Miocene 5.32 to 23.8

0.70800 5 10 15 20 25 Numerical Age, Ma

FigureFig. 11. 11 Curve showing strontium-isotope evolution of seawater from 25 to 5 Ma (from Howarth & McArthur, 1997). For clairity, the obtained 87Sr/86Sr ratios (y-axis) and corresponding ages (x-axis; mean values) for the Norwegian Skade, Eir (informal) and Utsira formations, the Danish Brejning, Vejle Fjord, Klintinghoved, Arnum and Odderup formations and the British Hutton sand (informal; from Figs. 2, 6 & 10) are indicated with different colours. al., 1999, 2013)). The late Tortonian (7.5 Ma) transition in the Nordland Group in well 25/2-10 S. The lack of the from dextral to sinistral Neogloboquadrina atlantica top of the assemblage in the latter well is probably due is also identified in the central North Sea (Spiegler & to a break in the stratigraphy. Towards the west, the B. Jansen, 1989; King, 1989). Dinocyst assemblages also badenensis-B. reticulata assemblage is recorded in the UK indicate continuing oceanic connections, and there is no well 9/09a-A 23 on the East Shetland Platform. As seen in stratigraphical break in the Miocene–Pliocene succession Figure 14, in the scientific boreholes at ODP Sites 642 and in Denmark (Dybkjær & Piasecki, 2010). 644 on the Vøring Plateau the occurrence of B. badenensis and B. reticulata is estimated to be slightly older than 14 In the correlation chapter and Figures 4–7 we described to c. 11.7 Ma (Middle Miocene; Spiegler & Müller, 1992; the correlations of Bolboforma assemblages from the Müller & Spiegler, 1993). Ringkøbing–Fyn High, in the southeast, through the Central and Viking grabens to the Norwegian Sea shelf and Higher up in the sections at ODP Sites 642 and 644, Vøring Plateau (Norwegian Sea) in the north (see Fig. 8). Spiegler & Müller (1992) and Müller & Spiegler (1993) described a B. fragori/B. subfragori Zone from Figure 14 synthesises the Bolboforma correlation. sediments with an age of approximately 11.7–10.3 Ma The Bolboforma badenensis-Bolboforma reticulata (earliest Late Miocene). Between the B. badenensis-B. assemblage, the oldest assemblage, is recorded from the reticulata Zone and the B. fragori/B. subfragori Zone they Hodde Formation in the Gram-1 borehole (Laursen & described a very thin Bolboforma compressispinosa Zone. Kristoffersen, 1999) and the Rødding borehole (both Immediately above the B. fragori/B. subfragori Zone, from the Ringkøbing–Fyn High). Laursen & Kristoffersen Spiegler & Müller (1992) and Müller & Spiegler (1993) (1999) also recorded this assemblage farther south described a Bolboforma laevis Zone extending up to from the Borg-1 and Lille Tønde boreholes in the North sediments estimated to c. 10 Ma in age. B. laevis and B. German Basin (Fig. 8; not included in Fig. 14). The clodiusi are also common in the B. fragori/B. subfragori assemblage is not recorded in well 2/4-C-11 (Central Zone (Quale & Spiegler, 1989; Müller & Spiegler, 1993). Graben) since there is a local hiatus in the Middle Miocene in that area, possibly due to salt tectonics and polygonal Laursen & Kristoffersen (1999) recorded B. clodiusi faulting (Eidvin et al., 2013). In the Viking Graben, the assemblages from the Gram Formation in the Borg-1 and B. badenensis-B. reticulata assemblage is recorded from Lille Tønde boreholes (North German Basin) and the the Nordland Group, including the lowermost part of the Gram-1 borehole (Ringkøbing-Fyn High; Fig. 8). Eidvin Utsira Formation, in wells 24/12-1 and 25/10-2 as well as et al. (2013) recorded a B. laevis assemblage from the

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a g r je b d a NORWEGIAN JOURNAL OF GEOLOGYG B Correlation of the Upper Oligocene–Miocene deltaic to shelfal succession onshore Denmark with similar deposits 565

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0 m 0 0 2 2 - 1 / 6 3 r d e n Correlation panel of the Oligocene to Pliocene succession from central Jylland, Denmark, into the North Sea and northward to just west of Stadt, western Norway. The datum (horizontal blue line) is the base base is the line) blue (horizontal datum The Norway. western of Stadt, west just to northward and Sea North the into Denmark, Jylland, central from succession Pliocene to of Oligocene the panel Correlation a

me d em b nn a m en e s U c ig o l O Figure 12. Figure Fig. 12 (2010, al. et Eidvin after location, 3 for Fig. also (see unconformity Miocene Middle so-called the to corresponds line of blue 58°30´N the North sector. Norwegian southern and Danish the in Formation of Hodde the 2013)). 566 T. Eidvin et al. Northern Viking Graben - 61°N

Line NVGTI-92-105 34/7-1 34/8-3A 35/11-1 W E

TWT (ms) 400 – SEAFLOOR

600 – PLEISTOCENE

800 – PLEISTOCENE PROGRADING COMPLEX

1000 – TAMPEN SPUR MEMBER (informal) UTSIRA FORMATION SAND

middle Miocene - lower Pliocene 1200 – BASAL PLEISTOCENE LOWER MIOCENE mid-Miocene unconformity Messinian 1400 – unconformity? OLIGOCENE UTSIRA FORMATION (GLAUCONITE; Intra Oligocene unc. Messinian - Zanclean)

0 10 20 25 km

Figure 13. East–west transect of the northern North Sea at about 61°N illustrating the main sequences and sedimentary architecture of the post-Eocene strata (see Fig. 3 for location; modified after Eidvin & Rundberg, 2001, Rundberg & Eidvin, 2005 and Eidvin et al., 2013). Fig. 13

Ørnhøj and Gram formations in the Rødding borehole All these observations clearly show that planktonic (Ringkøbing-Fyn High; Fig. 14). A B. fragori-B. subfragori deep-sea forms, which have their origin in the North assemblage is recorded from the Nordland Group in well Atlantic and the Norwegian Sea, have been brought by 2/4-C-11 (Central Graben). B. fragori assemblages are ocean currents through an open strait into the northern recorded from the Utsira Formation in the wells 24/12-1 and central North Sea during the entire Serravallian, and 25/10-2 (Viking Graben; Fig. 14). In well 25/2-10 S Tortonian, Messinian and Zanclean time interval (Viking Graben), sediments with a similar age as the B. (approximately 14.5–3.5 Ma). fragori assemblage are eroded. Deposited in a shelf setting, the sandy Utsira Formation Above the B. laevis Zone in the boreholes at ODP Sites (about 12.5–3.5 Ma; Eidvin et al., 2013) overlies Middle 642 and 644, Spiegler & Müller (1992) and Müller & Miocene shales (about 15–12.5 Ma; Eidvin et al., 2013) Spiegler (1993) described a B. metzmacheri Zone from in a large area in the Norwegian sector of the North sediments with an age of c. 10–8.7 Ma (Late Miocene). Sea. The Utsira Formation thins and appears to be B. metzmacheri assemblages are recorded in the Gram condensed towards the west, shaling out towards the Formation from the Borg-1 and Lille Tønde boreholes south, east and north. It appears to consist of a lower (North German Basin; Laursen & Kristoffersen, 1999), unit (approximately 12.5–6 Ma), which is mainly from the Gram-1 and Rødding boreholes (Ringkøbing– restricted to the depo-centres and being commonly Fyn High), from the Nordland Group in well 2/4-C-11 strongly affected by soft-sediment deformation, and (Central Graben), from the Utsira Formation in well an upper unit (approximately 5–3.5 Ma) which is less 25/10-2 (Viking Graben), from the lower part of the deformed and has a wider distribution (Riis & Eidvin, Molo Formation in well 6407/9-5 (Trøndelag Platform) 2015, 2016). In the northernmost part of the Norwegian and from the middle part of the Kai Formation in well North Sea (Tampen area) there is a 10–50 m-thick sheet 6508/5-1 (Helgeland Basin; Figs. 8 & 14). of glauconite sand (approximately 5.7–4.2 Ma; Fig. 15; Eidvin & Rundberg, 2001; Eidvin, 2009; Eidvin & Planktonic foraminifera of Late Miocene age (Spiegler Øverland, 2009; Eidvin et al., 2013). The glauconite sand & Jansen, 1989; Figs. 4–7), as sinistral and dextral coiled overlies an erosional unconformity. Løseth & Henriksen N. atlantica, Globigerina bulloides and Globorotalia (2005) suggested that the erosion was related to Middle puncticulata, occur in the upper part of the Utsira Miocene uplift and they correlated it to the uplift of Formation in the wells we have investigated in the Viking southern Scandinavia. Our alternative interpretation is Graben and in the Nordland Group in the Central that there was Early–Middle Miocene uplift along the Graben (Eidvin et al., 2013). margin of the Møre Basin which created a submarine

NORWEGIAN JOURNAL OF GEOLOGY Correlation of the Upper Oligocene–Miocene deltaic to shelfal succession onshore Denmark with similar deposits 567

N. PACHYD. (D.) N. PACHYD.

N. ACOSTAENSIS N. (LAD) ACOSTAENSIS N. (FAD)

(S.) DERMA

(D) N. PACHY- N. N. ENSIS LOWER TICA TICA TICA (S.) ACOSTA- FORAM. N. ATLAN- (D.) N. ATLANT. PLANKT. N. MAYERI N. ATLAN- LATA GORI ENSIS B. FRA- B. COMPR. SITE 642+643 FORMA CALCAREOUS BOLBO- B. METZ- B. BADEN- B. LAEVIS MICROFOSSILS MACHERI B. RETICU- (BASED ON FADs) Müller and Spiegler 1993) (Spiegler and Jansen 1989, 6000 4000 No. IRD/g sed 2000 SITE 644/642 no data Vøring Plateau Vøring (Norwegian Sea) 0 0 2 4 6 8 This vertical scale (in Ma) differs from that of the eight This vertical scale (in Ma) differs wells which have metres. 10 12 14

(Ma)

ass. fragori B. assemblage assemblages

subfragori - - subfragori metzmacheri

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Bolboforma Bolboforma

units

Formation

Kai Formation Kai Naust Fm Naust

Lithostratigraphic Brygge

Log

Basin Depth (mRKB) Depth 6508/5-1 1130 1150 1200 1250 1300 1350 1400 Helgeland

assemblage

assemblage macheri assemblages

Bolboforma Bolboforma metz- Bolboforma

Formation units Molo Formation Molo

Brygge Lithostratigraphic Depth (mRKB) Depth 725 750 775 800 Platform 6407/9-5 Trøndelag

Bolboforma metzmachheri Bolboforma fragori - B. subfragori, B. laevis and B. clodiusi assemblages Bolboforma badenensis - B. reticulata assemblage

assemblages forma assemblage reticulata

Bolboforma Bolboforma badenensis - Bolbo- - badenensis Bolboforma (1996). & Jansen

Colour Key

Formation units

Nordland Group Nordland

Lithostratigraphic Utsira Depth (mRKB) Depth 480 500 550 600 25/2-10 S

Viking Graben

assemblages assemblage

Bolboforma Bolboforma badenensis Bolboforma

units Hutton sand (informal) sand Hutton Lithostratigraphic

East Depth (mRKB) Depth 310 350 390 Platform Shetland

9/09a-A23 (UK) 9/09a-A23

Sjøholm (1991) and Frondval Frondval (1991) and & Sjøholm

assemblage assemblages

assemblage assem. reticulata B.

metzmacheri

Bolboforma

Bolboforma fragori Bolboforma

B. badenensis - badenensis B. Bolboforma

units

Utsira Formation Utsira Nordland Group Nordland

Lithostratigraphic Depth (mRKB) Depth

25/10-2

620 650 700 750 800

assem.

assemblages assemblage

ass. reticulata

fragori - fragori

Bolboforma

Bolboforma badenensis Bolboforma Bolboforma Bolbof.

units

Formation

Nordland Group Nordland

Lithostratigraphic Utsira

Viking Graben Depth (mRKB) Depth 24/12-1 680 700 750 800 850

CORRELATION OF BOLBOFORMA ASSEMBLAGES OF BOLBOFORMA CORRELATION

assemblages ass. metzmacheri assem. subfragori B.

Bolboforma Bolboforma - fragori Bolboforma

Group units

Nordland Group Nordland

Lithohstratigraphic Hordaland Depth (mRKB) Depth 2/4 - C-11 1530 1550 1600 1650 1700

Central Graben

assemblages ass. reticulata B.

assemblage laevis Bolboforma Bolboforma B. badenensis - badenensis B.

Bolbof- metzma.

units Formation Formation

Gram Formation Gram Hodde Formation Hodde

Lithostratigraphic Ørnhøj Odderup Depth (mRKB) Depth

Rødding 21 25 30 35 40 45

assembl. assem. metzmacheri ned assem. reticulata B. assemblages

clodiusi

Bolboforma Bolboforma Unde- - badenensis Bolboforma

Bolbofor.

Formation?

units

Gram Formation Gram Formation Hodde

Lithostratigraphic Odderup

m below surface below m Sample depth Sample 39 44 47 50 5.3 7.3 9.0 Gram-1 11.3 13.1 15.1 17.0 19.0 21.5 23.5 25.5 27.5 29.5 31.4 32.7 34.7 35.7 Ringkøbing - High Fyn Fig. 14 Correlation of Middle and Upper Miocene Bolboforma assemblages from the wells in Figures 4–7 and from other selected wells and boreholes to the Bolboforma zonation of the ODP Sites 642 Sites of ODP the zonation Bolboforma the to boreholes and wells selected other from 4–7 and Figures in wells the from assemblages Bolboforma Miocene Upper and of Middle 14. Correlation Figure Jansen curveIRD is after The 1993). Spiegler, & (Müller Plateau Vøring the on 643 and 568 T. Eidvin et al.

(Naust Formation (Naust equivalent) X X X !X %J+X%6>AUA6)X >AFL+D>XADJ4X V )3B¥ 5.1 Ma (Utsira Formation) 5.1 Approximately Ma29-26 Group) (Hordaland ~ Spur Tampen member (informal) Ma> 2.75 ?e

5.7 Ma r 3 3 `¥ b¥ ¥ b¥ _¥ _¥ ¥ Ma 5.1+5.5 ¥ r 3 3 ae ¥ `¥

C) Approximately Group) Ma (Hordaland 23-18 61 °

be 3 Måløy

¥ Florø ¥ J ¥ ,133 ¥ => 3f¥ Ede + 23 `¥ ¥ ,

! SAND

J de¥ BASAL

b¥ 23 LOWER +3 3 ! MIOCENE b¥ GELASIAN GELASIAN 3 J¥ OLIGOCENE PROGRADING ¥ GLAUCONITIC _¥

3 r ° ° 3 4 ce 4 ¥ Te `e M

e 3 5.0 Ma $3

`¥ h¥ $3 $3 03 ¥ %3 34/8-3 A 34/8-9 S 34/4-7 34/2-4 r 34/8-1

G ° 3 34/4-6 °

3 2 ce 2 34/7-1 34/8-A-1 H ¥ 34/7-2

3hf ¡" ¡;~f¡Q~YqNh~{¡VhOfOy¡~a¡Yqq¡d~y¡gY¡Lh{V¡NYN¡Pq~Qp¡ "(¡¡ Yqq¡d~y¡gY¡D{~Y¡NYN¡Pq~Qp¡ ""¡ N{V¡ "'¡ N{V¡Yqq ""¡ ~{¡

gY¡{~gY{¡GNyY{¡D ¡=~Y¡~h h~{¡~a¡Q~{Y{l ~{Nq¡R~Y¡i{¡Yqv¡ "()$¡ N{V¡ "( / u8¡ 6B¡. fNyyN¡N¡ q~f ¡2Yg¡i{¡yYY¡PYq~¡ 61 ° hfc ~~ ¡ [Q¥ Fig. 15 Fig. A) B) NORWEGIAN JOURNAL OF GEOLOGY Correlation of the Upper Oligocene–Miocene deltaic to shelfal succession onshore Denmark with similar deposits 569

Figure 15. (A) Log correlation diagram of wells from the Visund area Kai Formation in well 6508/5-1 (Fig. 14), in the lower (block 34/8), wells from the Snorre area (blocks 34/4 and 34/7) and middle part of the Kai Formation in well 6607/5-1 well 34/2-4 on the northern Tampen Spur (northernmost North Sea; » and in the middle to upper part of the Kai Formation modified after Eidvin & Rundberg, 2001). (B) Distribution of Utsira Formation sands in the Snorre and Visund Field areas at Tampen. in well 6609/5-1 (Eidvin et al., 2013 and unpublished Light and dark yellow areas show the outlines of the main Utsira data) suggest that the Molo Formation, in its southern quartzose sands. Hatched area (with green stars) shows the assumed distribution area, correlates with the middle/upper part outline of the thin glauconitic member extending beyond the main of the Kai Formation. Utsira sand. Red lines indicate top Oligocene truncation, whereas red arrows show sediment transport directions (note also well 34/7-2 in the Tordis Field area; modified after Eidvin & Rundberg, 2001; Rundberg & Eidvin, 2005). (C) Global sea-level curves of Hardenbol et al. (1998; light-grey shading) and Miller et al. (2005; black line), Conclusions as well as the 4th-order eustatic cycles of Esteban et al. (1996; dark- grey shading; modified after Pérez-Asensio, 2013). Please note that the glauconitic Utsira Formation sand was deposited coevally with Strontium-isotope data (87Sr/86Sr ratios) from the Upper the period of transgression after the Messinian lowstand. Oligocene–Lower Miocene succession in Jylland, Denmark (94 samples from 18 localities; Eidvin et al., 2014a), were utilised for correlation with Norwegian wells and boreholes (Eidvin, 2016 and Eidvin et al., 2013, topographic high where probably only small amounts of 2014b) together with foraminiferal and pyritised diatom Miocene sediments accumulated. The erosion that gave data. Dinocyst correlation is also used in some areas. For rise to the unconformity could have been mainly related the Middle–Upper Miocene parts of the succession the to a sea-level drop in the Late Miocene, concurrent with correlations are based mainly on Bolboforma data from the Messinian salinity crises (Fig. 15). This interpretation a stratigraphic borehole at Rødding in southern Jylland. is consistent with our view that there was an open seaway in the North Sea throughout the Middle Miocene. It is The Sr isotope investigations of samples from the noted that the unconformity itself is affected by soft- Danish, Brejning, Vejle Fjord, Klintinghoved, Arnum sediment deformation. The pre-deformational tectonic and Odderup formations gave ages between 25.7 structure is not easy to reconstruct in the seismic data. and 15.5 Ma. These sediments can be correlated with deposits from a number of sedimentological units in Based on the marine palynomorphs in two ditch- the Norwegian North Sea, Norwegian Sea shelf and cutting samples at 1190 and 1180 m in well 34/4-6 in the one well on the East Shetland Platform in UK waters. glauconitic Utsira Formation, De Schepper & Mangerud These include clay-rich deposits of the Hordaland (2017) assigned a maximum age of 3.0 Ma for the upper Group (central, southeastern and northern North Sea), part of this formation and a minimum age of 4.6 Ma for Hutton sand (informal; East Shetland Platform), the the lowermost part. However, as the sediments represent sandy Skade Formation (northern North Sea) and the ditch-cutting samples and it was difficult to differentiate Brygge Formation (Norwegian Sea shelf). A Bolboforma between reworked, in situ and caved specimens, they assemblage in the Hodde Formation in the Rødding considered this age to be uncertain. borehole was correlated with sandy and fine-grained deposits in the lower part of the Nordland Group, Strontium-isotope ages based on tests of foraminifera situated between the Skade and Utsira formations, in the which have their last occurrence in the Late Miocene Viking Graben and the upper part of the Hutton sand to Early Pliocene in the North Sea (King, 1989), picked (informal) on the East Shetland Platform. Bolboforma from ditch-cutting samples and a sidewall core in wells assemblages in the Ørnhøj and Gram formations in from the Snorre and Visund fields, gave ages of 5.7–5.2 the Rødding borehole were correlated with the lower Ma. Records from a sidewall core from the Tordis Field part of the sandy Utsira Formation (northern North gave ages of 4.7 and 4.2 Ma (Fig. 15). These ages are Sea), the lower part of the Molo Formation (in its substantiated by the fact that glauconite was precipitated, southern distribution area), middle/upper part of the most commonly, during periods with transgression Kai Formation (Norwegian Sea shelf) and with the ODP on outer shelves at 200–300 metres water depths boreholes on the Vøring Plateau (Norwegian Sea; Figs. (Odin & Matter, 1981 and Van Houten & Purucker, 2, 4–7, 10, 11 & 14). This demonstrates that there must 1984). According to Hardenbol et al. (1998) a global have existed a seaway between the North Sea and the transgression started in the middle of the Messinian and Norwegian Sea during the Middle, Late Miocene and a regression in the middle Zanclean. Early Pliocene.

According to Løseth & Henriksen (2005) and Løseth et al. (2016a. 2017), the Molo Formation postdates the Kai Formation. The occurrences of the Bolboforma Acknowledgements. The authors are especially grateful to the late Chris King for very important discussions. Many thanks also to Rune Goa metzmacheri assemblage in the lower part of the Molo (NPD) for drawing most of the figures, Tone Tjelta Hansen (NPD) Formation in well 6407/9-5, in the middle part of the for technical assistance, Stephan Piasecki (Natural History Museum 570 T. Eidvin et al.

of Denmark) for collecting molluscs, David Roberts (Geological Eidvin, T. 2016: Biostratigraphy and Strontium Isotope Stratigraphy Survey of Norway, NGU) for improving the language, Yuval Ronen (SIS) of Lower Oligocene to Pleistocene in Well 9/09-A 23 (Bruce (University of Bergen) for executing the strontium isotope analyses Field, UK) including Hutton sand (informal). Norwegian Petroleum and Robert Williams (NPD) for discussions. We acknowledge Morten Directorate, 1–15. Smelror (NGU) and Roel Verreussel (TNO Geological Survey of the http://www.npd.no/Global/Norsk/3-Publikasjoner/ Netherlands) for their constructive review and NPD, GEUS and the Forskningsartikler/9-09a-A23-figurer.pdf. Natural History Museum of Denmark for permission to publish this Eidvin, T. & Rundberg, Y. 2001: Late Cainozoic stratigraphy of the manuscript. Tampen area (Snorre and Visund fields) in the northern North Sea, with emphasis on the chronology of early Neogene sands. 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