3D and 2D seismic data reveal the base-reflection of the Quaternary in the northwestern German North Sea locally at depths of more than 1000 m. This indicates extremely fast subsidence, with a rate of up to 480 m/Ma during the Quaternary, resulting in a NNW-SSE oriented sedimentary depocentre. Distinct iceberg scour marks, identified in 3D seismic data are used to calibrate quantitative subsidence analysis and to document shallow marine conditions during the Quaternary interglacials. Previously, a number of mechanisms have been proposed to explain the Quaternary subsidence. Here we show that compaction and load-induced subsidence alone explain about 75% of the observed Quaternary subsidence. However, a certain portion of the subsidence needs additional processes to be invoked. The extensive seismic dataset interpreted here makes it possible to exclude a phase of renewed tectonic activity as the origin of the subsidence anomaly. From the orientation and extent of the depocentre, lithosphere buckling and subsidence due to salt movement are considered unlikely. Possibly a post-glacial collapse after the retreat of glaciers in the North Sea Basin, local lower crustal flow, or dynamic topography or a combination of these processes contributed to the residual subsidence.
The widely accepted McKenzie model1 predicts strong subsidence during the extension phase of continental rifts. During the subsequent post-rift phase, subsidence theoretically1 declines exponentially. The Mesozoic/Early Cenozoic subsidence pattern of the North Sea is interpreted as a result of thermally induced subsidence following Late Triassic to Early Cretaceous rifting events accompanied by sediment loading and isostatic adjustments2,3,4,5,6,7. However, during the Quaternary (2.6 Ma), the Central Graben area of the North Sea rift experienced an unusually high degree of subsidence (i.e., anomalous subsidence), at about 140 Ma after the final rifting phase2,3. During these 2.6 Ma, a thick package of more than 1000 m of sediments accumulated in the North Sea Basin, including the northwestern German North Sea (Figs 1 and 2). Various potential mechanisms have been proposed as causes of the anomalously high rate of Quaternary subsidence2,3,8,9,10,10. These include reactivation of faulting in association with a renewed rifting phase2,3, lithosphere buckling due to intraplate stresses8,9,10,11, metamorphic processes at the crust-mantel transition12, and the influence of a mantle thermal anomaly13,14. More generally, other modes of mantle convection are also suggested as causing dynamic topography, i.e. topography deviating from values corresponding to isostatic equilibrium15.
Alongside the distinct offshore subsidence, onshore areas around the North Sea are subject to large-scale uplift16,17,18,19,20,21. In eastern Sweden, an isostatic uplift of about 310 m since the deglaciation of the last glacial maximum has been derived from Holocene shore displacement investigations by radiocarbon-dating22. It is suggested that the topography and landscape in northwestern England have almost entirely formed since the Middle Pliocene, accompanying ~800 m or more of uplift, while further to the south, total uplift since the Middle Pliocene has been estimated to be in the range of 150–200 m23,24. However, it is questionable if the uplift occurred during the Quaternary or actually before the Pleistocene25,26. Nevertheless, the widespread Neogene uplift around the North Sea (and beyond) has been suggested to be linked to local offshore subsidence via enhanced sediment supply9,16 or by lower crustal flow10,17,23,27.
In this study, we calibrate the Quaternary succession in time and (palaeo-) depth by using iceberg scour marks, indicating shallow marine conditions during the interglacial periods. The Quaternary depocentre is regionally interpreted to be in the northwestern German North Sea, supplemented by published depth maps around northwestern offshore Germany. We calculated the well-constrained processes such as compaction and load-induced subsidence, and conclude that only about 25% of the observed subsidence requires additional explanation. This is discussed in the light of earlier suggested mechanisms for the high Quaternary subsidence.
Geological setting of the North Sea Basin
The Cenozoic North Sea Basin developed as an intracratonic sag basin and is centred above Mesozoic rift structures, including the Central Graben28,29,30 (Figs 1 and 2). The Cenozoic depocentre, which is aligned along a NW-SE axis, preserves more than 3 km of Cenozoic, mainly siliciclastic sediments9,31,32.
The Quaternary sedimentary succession reaches a maximum thickness of more than 1000 m along a NNW-SSE trending basin axis in the central North Sea33 (Fig. 1). Because most Quaternary sediments were deposited in a shallow-water environment2,34, the southern part of the North Sea Basin must have locally experienced an extremely high rate of subsidence exceeding average Cenozoic rates by a factor of 10, as revealed by Cenozoic thickness maps2,31,32.
The change between glacial and interglacial periods during the Quaternary resulted in strong sea-level fluctuations, with amplitudes between 100–150 m, and coastline shifts with a vertical range of up to 120 m around the North Sea18,34. Consequently, non-marine conditions were repeatedly established in portions of the southern North Sea during the Pleistocene (Fig. 3), as evidenced by subglacial tunnel valleys39 within the uppermost Quaternary section. Repeated regressive phases coupled with climatic deterioration, led to increased sediment supply mainly from the south, via the rivers Saale, Elbe, Weser, and Rhine, which provided the bulk of the sediments that accumulated in the southern North Sea area during the Quaternary10,33 (Fig. 3).
Interpretation and Results
Eight prominent seismic horizons between 250–1000 ms depth (TWT, approximately 200–1000 m; see chapter Methods and stratigraphic correlation) are interpreted in the study area. All reveal curvilinear and cross-cutting lineations, interpreted as iceberg scour marks (Figs 4 and 5). We consider this to be a robust indication that the surfaces formed under shallow marine conditions with water depths not exceeding 100 m34. The distinct lineations exhibit lengths between 0.1 km and 23 km, widths between 15–50 m, and 6–12 m deep incisions. Such structures are well-documented from a variety of present-day and formerly glaciated marine environments40,41,42,43,44,45 and are certainly the result of scraped iceberg-keels into soft sediments on the seabed. The iceberg scour marks are found at a present-day depth between 300 to 850 m with the majority located at depths between 500–700 m (Fig. 5). They locally cross-cut each other at a wide range of orientations but regionally show a distinct NNW-SSE to N-S orientation (Fig. 5).
A cross-correlation of two of the interpreted horizons with results from a high-resolution 2D-seismic survey, calibrated by well data from the Dutch offshore (see Fig. 2 for location), reveals ages of these horizons of 1.9 and 2.6 Ma. As previously suggested for the Dutch offshore40, the iceberg scour marks in the study area can be attributed to Gelasian (2.6–1.8 Ma) and to Pleistocene (1.8–0.01 Ma) times (Fig. 5). These glacial features on the former sea floor are used in the following as chronological markers, and thus as measures for the Quaternary subsidence pattern and subsidence rates within the German North Sea. Furthermore, interpreted glacial features enable interpretations of the palaeobathymetry and to distinguish between marine and shallow marine conditions.
The present-day depth of the base Quaternary succession in the study area ranges between ~110 m in the southeast, and up to 1100 m towards the central North Sea Basin (Fig. 2). The seismic horizon dated at 2.6 Ma in the Dutch offshore sector40 defines the base Quaternary in the German North Sea (Figs 2 and 4). Based on the calculated Quaternary thickness map, a subsidence rate of approximately 410 m/Ma is derived at the location of well A-9-1. This is in sharp contrast to a calculated subsidence rate of ~140 m/Ma for the main Neogene depocentre (240 m/Ma for the Pliocene) above the Central Graben area. These values show that subsidence was higher during the Quaternary, but also point to a trend of increasing subsidence rates already during the Neogene, particularly during the Pliocene. We derive a subsidence rate of 80 m/Ma for the Palaeogene succession from calculated thickness maps in the most northwestern part of the study area. Although subsidence already started to accelerate in the Neogene, the Quaternary subsidence is still exceptional with a more than ten-fold increase in subsidence compared to average Cenozoic sedimentation rates. The Quaternary isopach map (Fig. 2) further illustrates an increase in subsidence from the southeastern part of the study area (180–265 m/Ma) towards the central North Sea Basin, reaching a maximum rate of 480 m/Ma. The main Quaternary depocentre within the central North Sea follows a distinct NNW-SSE trend. It is clearly offset from the Neogene depocentre and is shifted towards the northwest. We calculated a subsidence rate of ~550 m/Ma for the interval 2.6 Ma–1.9 Ma and ~300 m/Ma for 1.9 Ma–0 Ma, respectively at the location of well A-9-1. The thickness of the Quaternary to Holocene sedimentary succession increases from the southeastern to the northwestern part of the study area, where it reaches a maximum of 1045 m.
In the following we consider a range of mechanisms to explain the Quaternary subsidence pattern which can be addressed on the basis of our comprehensive thickness dataset.
Load-induced subsidence during the Quaternary
In order to decipher the origin of the enormous Quaternary subsidence, first the range of subsidence induced by the load of the sedimentary successions was estimated.
Values for subsidence were calculated, assuming local loading (Airy model) at well locations, using the following equation46:
y is the amount of subsidence in the absence of water load, S* is the sediment thickness (depends on well location), ρs (2080 kg/m3) and ρm (3270 kg/m3) are the mean densities of the sediments and mantle respectively47,48.
Our calculations, based on 29 exploration wells covering the study area, show that subsidence due to sediment loading during the Quaternary ranges between approximately 250 m in the southern part of the study area to a maximum of 550 m at the location of the A-9-1 well, and increases towards the NW to about 665 m (Fig. 2a).
Flexural response of the crust to loading
By taking flexure into account (Fig. 2b), the amount of subsidence due to sediment loading observed in the study area is slightly reduced if compared to the Airy isostasy model46. The flexural response of the lithosphere is modelled as an elastic beam using the following equation49,50: Where D is the strength of the elastic lithosphere, E is Young’s Modulus (70 GPa), ν is Poisson’s ratio (0.25), and T is the thickness of the elastic lithosphere (25 km50).
The 2D flexural model is calculated every 30 km along an about 600 km long SW-NE profile (Fig. 2b). Mean densities of the sediments and mantle are ρs (2080 kg/m³) and ρm (3270 kg/m³), respectively. The maximal subsidence due to sediment loading by flexure is about 610 m, showing a difference of 55 m to the Airy isostasy model46 (Fig. 2b).
Towards the basin edge, where the thickness of the Quaternary decreases to about 100 m, subsidence due to loading using the Airy isostasy model is less than the flexural response of the crust. We consider the thickness of the elastic lithosphere of 25 km50 to be reasonable. To get a feeling for the uncertainties, we additionally modelled with values of 10 km and 30 km flexural crustal thickness. Using 10 km flexural crustal thickness, the local isostasy and the flexural response of the crust are almost identical. By using a constant elastic thickness value of 30 km, the maximal difference between the Airy isostasy model and the flexural response of the crust increases and amounts to about 80 m within the depocentre.
In conclusion, isostasy and flexural modelling show that a large amount (75%) of the observed overall Quaternary subsidence is explained by load-induced subsidence without invoking additional mechanisms.
The compaction of Neogene sediments, and particularly Palaeogene strata underlying the Quaternary succession, is another process that probably contributes to the Quaternary subsidence. Extensive polygonal fault systems51,52 in Neogene and Paleogene successions (Fig. 6) are interpreted here as expressions of compaction, which provides additional regional accommodation space. Based on a 3D basin and petroleum system model53, and by considering a lithology of 75% shale (initial porosity, 70%), 15% silt (initial porosity 55%), and 10% sandstone (initial porosity 41%), compaction values range between 150–250 m for the Neogene and Palaeogene strata. This compaction of Palaeogene and Neogene sediments shows an increasing trend from the southern part of the study area towards the northwest, with maximum compaction below the thickest accumulations of Quaternary sediments53.
Adding these values to the load-induced subsidence (flexure included) of up to 610 m derived here, results in a combined subsidence of up to 810 m. It is concluded that within the errors, most of the deepening and thus accommodation is controlled and can be explained by load-induced subsidence and compaction.
Subsidence due to renewed rifting activity during the Quaternary?
The strong Quaternary subsidence phase has been attributed previously to thermal rejuvenation in association with a renewed rifting phase and tectonic activity2,3. The foundation of this assumption is primarily the observation that the Quaternary depocentre with a thickness of up to 1200 m partly coincides with older tectonic trends such as the Dutch Central Graben (Fig. 1). However, the same does not consistently apply to the German part of the Central Graben (Figs 1 and 2), where the maximum Quaternary thickness attains 700 m, and the main depocentre is considerably offset (50 km) from Mesozoic structures (Figs 1 and 2). In fact, the main Mesozoic rift structure in the German Central Graben area experienced less Quaternary subsidence compared to the neighbouring areas54.
Further southeast and onshore, in northern Central Europe, numerical simulations determined that climate-induced melting of large ice sheets after the Weichselian glaciation was able to trigger fault reactivation and earthquakes around the migrating ice limit55. Even today, the stress due to glacial isostatic adjustment can continue to induce seismicity within the once glaciated region55.
However, in our extensive offshore seismic data there are no indications of renewed tectonic activity (Fig. 7a) e.g. extensional faulting or the development of pull-apart basins2,3. The only exceptions are isolated active salt diapirs and related top diapir fault structures (Fig. 6). Salt-related structures, however, do not coincide spatially with the main Quaternary depocentre but are concentrated in the area of Mesozoic rifting. The Quaternary sedimentary succession is found to be fairly homogenous and is not affected by any significant characteristic tectonically induced fault pattern and/or the reactivation of older Mesozoic tectonic trends. Distinct Mesozoic fault structures, which control the base Upper Cretaceous structural relief, die out upwards within Upper Cretaceous strata. Only a few faults show continuous displacement growth at base Palaeogene, whereas the majority of these faults are associated with salt activity, and a few may be attributed to the abated compressional tectonics at the end of the Late Cretaceous-Early Palaeocene33,56,57,58,59. Admittedly, our seismic data has a vertical seismic resolution of ~10 m and thus is insufficient to image small-scale faults. However, if there are reactivated faults with offsets of only a few meters which are not resolved in our seismic data, than these faults provide a very minor accommodation space in the North Sea Basin. Overall, however, a renewed rifting phase and fault reactivation in the southern North Sea are considered to be an unlikely origin for the Quaternary subsidence.
Subsidence due to salt movement
Salt flow results in the deformation of overlying and adjacent sediments through the formation of rim synclines, characterized by distinct angular unconformities. However, such rim synclines accompanied by differential subsidence patterns are exclusively observed locally around salt diapirs (Fig. 6). Thus, diapirism cannot explain the large-scale subsidence pattern in the North Sea. The effect of subsidence induced by salt expulsion or salt flow is also unlikely because the main Quaternary depocentre does not match the area dominated by salt tectonics or by active salt diapirs (Fig. 2). In contrast to the Central Graben area, the main Quaternary depocentre is found in an area with minor salt.
In the previous sections we have shown that most of the subsidence can be explained by compaction and load-induced subsidence. In contrast, a renewed rifting phase, as well as subsidence due to salt mobilization, are unlikely to have contributed to the Quaternary subsidence pattern.
In the following chapter we discuss qualitatively additional processes that may be invoked as an explanation for about 25% of the observed residual subsidence (Fig. 7b).
Glacial rebound and glacial forebulge collapse
The late Cenozoic uplift of continental areas around the North Atlantic is typically explained by isostatic adjustments following glaciation (Fig. 7c). Unloading due to melting of the Quaternary ice sheets is proposed to result in inflow of mantle in order to re-establish equilibrium, referred to as glacial rebound17,18,21.
However, the timing and magnitude of the glacial rebound are under discussion. Two significant Cenozoic episodes of uplift are reported around the North Atlantic, and the second phase occurred during the late Neogene and the Quaternary16. It is suggested that Neogene uplift in e.g. the eastern Danish North Sea was caused by isostatic adjustment of the crust as a result of accelerated denudation of up to 1000 m of topography, which was driven by climatic changes and long term eustatic lowstand16,31,32. However, there are many observations that indicate that the onset of uplift of landmasses around the North Sea area had already occurred before the first glaciation at 5.1–5.0 Ma2,16,25,26,31,32, questioning a causal relationship. The situation is further complicated by the fact that the offshore areas were ice-covered as well but were obviously experiencing subsidence rather than uplift.
The collapse of a peripheral glacial forebulge60,61, which developed during the Last Glacial Maximum (LGM) around the Fennoscandian ice sheet may have contributed to the isostatic subsidence. The orientation of this forebulge is reconstructed from models and observational data60. It is proposed to have been centered in the North Sea between Norway and Great Britain, extending through northwest Netherlands and northern Germany60,61, fitting the observed subsidence pattern in offshore Germany quite well. The main problem we see in invoking such a process is that the collapse of this peripheral forebulge could have created accommodation space for the post-glacial sediments only from 17 ka BP onward and thus may only explain a small portion of the whole Quaternary subsidence pattern. Quantification is difficult because it depends amongst other things on the glacier thickness and extent during the LGM, which are still widely discussed. By assuming an ice sheet with a thickness of about 2800–3700 m18 covering the Fennoscandian Shield, the roughly estimated collapse-induced accommodation space would be in a range between 50 m to a maximum of 85 m.
Subsidence caused by mantle flow
Small-scale sub-lithospheric mantle convection is suggested to result in an alternating pattern of rapid Neogene uplift and subsidence across north-west Europe13,14 (Fig. 7d). Residual topography, either calculated as deviations from expected water-loaded depths to oceanic basement as a function of plate age or estimated from satellite free-air gravity data, is observed down to wavelengths of about 1300 km15. At least some of these positive (uplift) and negative (subsidence) topographic anomalies are proposed to grow and decay on timescales of millions of years15. It is believed that they are generated and maintained by circulation of the sub-lithospheric mantle, probably involving rapid flow of low-viscosity material in shallow asthenospheric channels15. Nevertheless, at present it appears impossible to either confirm or disprove such a model at the small scale of the North Sea Basin.
Lower crustal processes
Flow in the lower continental crust is considered another mechanism that potentially isostatically compensates for surface loading of the Earth10,17,23,27. Lower crustal flow has e.g. been advocated to explain accelerated phases of basement subsidence in sag basins27. Phases of fast erosion onshore, and deposition of thick sediments offshore, are suggested to induce pressure gradients that drive the flow of the ductile crust from the centre of the former rift zone towards the continental interior27 (Fig. 7e), possibly linking the observed accelerated Quaternary subsidence and the simultaneous onshore surface uplift10.
The North Sea is characterised by a lower topography (i.e. sea level), water and low-density sediments and a thinner crystalline crust under the basin (13–15 km) than the surrounding landmasses with crustal thicknesses between 32–50 km47. Thus, while sediment loading and onshore erosion create a pressure increment directed away from the basin, it is hard to see how the net lithostatic pressure in the lower crust should become higher beneath the basin. Even if lower crustal flow is of local significance in the North Sea10,17, it is unlikely on its own to explain the residual subsidence during the Quaternary relative to the surrounding highs.
Alternatively, metamorphic reactions and alteration of the lower crust were proposed as possible mechanisms for subsidence in the North German Basin and surrounding regions12. During the Early Permian, for instance, an increase in heat flow of 10% is proposed to have triggered lower crustal metamorphic processes within the North German Basin. The resulting transition from greenschist to amphibolite facies is expected to increase rock densities and reduce rock volumes, resulting in increased subsidence12. However, during the Quaternary, there is no indication for a thermal anomaly in the North Sea Basin and this process is equally considered to be unlikely.
Intraplate stresses and lithospheric buckling
Intraplate compressional stresses have been proposed to cause ‘buckling’, or flexure of the lithosphere, resulting, in combination with sediment loading and compression-induced deep lithospheric phase reactions, in enhanced local subsidence8,11,12. 3D flexural modelling suggests that compressive intraplate forces, e.g. from the Atlantic ridge push or the Alpine convergent plate boundary, and subsequent lithospheric buckling can account for up to 700 m of accelerated subsidence in the North Sea8 (Fig. 7f). This model response was forced, however, by a prescribed area of strongly decreased effective elastic thickness (down to 3 km from a background value of 15 km) with no close relationship to the known crustal structure8. The orientation (NNW-SSE) of the main Quaternary depocentre (Figs 1 and 8) was also obtained via the orientation of the weak zone, whereas horizontal stress was modeled as isotropic. We consider such a process to be unlikely to contribute to the residual subsidence due to the orientation of the Quaternary depocentre. If intraplate stress-driven lithospheric buckling affected the North Sea region, then the Quaternary depocentre would be expected to have a NE-SW trend, approximately perpendicular to the observed present-day direction of maximum horizontal stress58,59,63 (Fig. 8). It is also surprising that such an inevitable major tectonic event had no expression in the sedimentary successions by e.g. compressional-related reactivations of faults8,11,64, if buckling of the lithosphere with major compressive forces took place while Quaternary sediments were deposited.
In conclusion, the complex structural evolution of the North Sea since the Caledonian mountain building phase with several subsequent extensional and compressional tectonic events alongside the former suture zones, accompanied by sediment deposition and erosional processes, sea level fluctuations – particularly as a result of glaciation and deglaciation phases during the Quaternary – make it difficult to decipher the origin and to quantify individual processes leading to the differential subsidence. However, the main outcome of this study is that the major portion (~75%) of the observed overall Quaternary subsidence is explained by load-induced subsidence and compaction, with other processes playing a minor role.
Rapid Quaternary subsidence in the North Sea Basin and the origin of the substantial accommodation space created during this period are investigated. Our study is based on 2D and 3D reflection seismic surveys, calibrated by exploration wells, covering northwestern offshore Germany, and is supplemented by results from regional studies. Iceberg scour marks, which are distinct in the seismic data, form our main chronostratigraphic markers. The main results of this study are:
Quaternary reflection surfaces reveal distinct iceberg scour marks in northwestern offshore Germany, indicating shallow water depths (<100 m) during formation. A correlation of two of the horizons with results from a high-resolution 2D-seismic survey, calibrated by well data from the Dutch offshore, reveals ages of 1.9 and 2.6 Ma.
Using the oldest well-calibrated Quaternary horizon, a maximum local subsidence rate of up to 480 m/Ma is derived, which indicates a more than ten-fold Quaternary increase in subsidence relative to average Cenozoic rates.
The present-day depth of this Quaternary surface in northwestern offshore Germany attains a maximum local depth of 1100 m. The Quaternary isopach map illustrates an increasing subsidence trend from the southeastern part of the study area towards the central North Sea Basin. However, this Quaternary depocentre is clearly offset from the Jurassic Central Graben in offshore Germany.
Most of the subsidence can be explained by compaction and load-induced subsidence. Sediment loading explains up to 665 m of subsidence, and thus about half of the observed maximum Quaternary subsidence. Polygonal fault systems in the Lower Neogene and Paleogene successions are interpreted as expressions of compaction below the Quaternary sedimentary succession. A range of compaction between 150–250 m for the Lower Neogene and Palaeogene strata is calculated. Thus, loading by sediment and water in conjunction with compaction explain approximately 75% of the observed total subsidence.
We rule out renewed extensional deformation as an explanation for the remaining 25% of the Quaternary subsidence. With the exception of isolated top diapiric faults above active salt domes, there are no significant indications for Quaternary normal faults in our extensive data. Subsidence due to salt movement is unlikely to be the cause because the Quaternary depocentre is clearly offset from the salt-dominated Mesozoic rift structures.
Intraplate stress-driven lithospheric buckling is also an unlikely cause because the main Quaternary depocentre is elongated along a NNW-SSE axis in the North Sea Basin, parallel to the major horizontal stress, and not perpendicular to it as expected. Mechanisms that cannot be excluded from contributing to the residual subsidence are post-glacial collapse of the glacier forebulge after the retreat of glaciers in the North Sea Basin, local lower crustal flow, and dynamic topography caused by sub-lithospheric mantle processes. Due to the dynamic structural evolution of the North Sea Basin, it remains unclear if there is a single origin or a combination of different processes to explain the 25% of residual subsidence.
Methods and Stratigraphic Correlation
A suite of four commercial 3D seismic surveys covering an area of ~4000 km² in northwestern offshore Germany referred to as the Entenschnabel area, (Fig. 2) have been used to investigate the geomorphology and ice-related glacial features of the Quaternary succession. The time-migrated 3D seismic datasets have a bin size of 12.5 m and are sampled with 4 ms. Two horizons with iceberg scour marks for Quaternary subsidence analysis are used. Iceberg scour marks were interpreted on eight horizons representing the former Quaternary high-latitude sea floor of the North Sea, whose base surface is buried to a present-day depth of more than 1000 m (Figs 4 and 5).
The stratigraphic correlation is based on interpreted seismic horizons from a high-resolution 2D seismic survey (SNST-NL-87-3c, see Fig. 2 for location) from the Dutch offshore area40 which are tied to a detailed age model based on wells A-15-3 and B-13-340 (Figs 2 and 4). 10 horizons are traced through the 3D seismic survey into northwestern offshore Germany, and two of them are presented in this study.
The time-depth conversion of interpreted seismic reflectors is based on a generalized linear relationship that reflects depth due to burial and compaction54. Standard backstripping methods46 and data from ~29 well locations are used for subsidence analysis. However, in exploration wells, the uppermost Cenozoic section is typically not studied in great detail, and the adopted lithologies are mostly generalized.
Sedimentation rates and compaction of the Cenozoic successions are calculated based on a 3D basin and petroleum system model53 and generalized lithologies adopted from well information.
The flexural response of the crust to loading49,50 is calculated using the 2D flexure calculation program Flex2D version 4.4 which is freely available on the website http://www.ux.uis.no/~nestor/work/programs.html.
The multichannel seismic surveys analysed during the current study are not publicly available due to limited data access for the deep subsurface of offshore Germany. 14 depth converted surfaces derived from reflection seismic datasets from the base Zechstein to Present54, and a 3D basin and petroleum system model53 used for compaction and subsidence analysis during the Quaternary, are available online and can be downloaded from the website www.GPDN.de.
McKenzie, D. Some remarks on the development of sedimentary basins. Earth Planet. Sci. Lett. 40, 25–32 (1978).
Kooi, H., Hettema, M. & Cloetingh, S. Lithospheric dynamics and the rapid Pliocene–Quaternary subsidence phase in the southern North Sea Basin. Tectonophysics 192, 245–259 (1991).
Thorne, J. A. & Watts, A. B. Quantitative analysis of North Sea subsidence. Am. Assoc. Pet. Geol. Bull. 73, 88–116 (1989).
Sclater, J. G. & Christie, P. A. F. Continental stretching: an explanation of the post-mid-Cretaceous subsidence of the Central North Sea Basin. Journal of Geophysical Research 85(B7), 3711–3739 (1980).
Barton, P. & Wood, R. Tectonic evolution of the North Sea Basin: crustal stretching and subsidence. Geophysical Journal of the Royal Astronomical Society 79, 987–1022 (1984).
Nielsen, L., Balling, N. & Jacobsen, B. H. Seismic and gravity modelling of crustal structure in the Central Graben, North Sea. Observations along MONA LISA profile 3. Tectonophysics 328(3–4), 229–244 (2000).
Frederiksen, S., Nielsen, S. B. & Balling, N. Post-Permian evolution of the Central North Sea: a numerical model. Tectonophysics 343, 185–203 (2001).
Van Wees, J. D. & Cloetingh, S. 3D flexure and intraplate compression in the North Sea Basin. Tectonophysics 266, 243–259 (1996).
Huuse, M., Lykke-Andersen, H. & Michelsen, O. Cenozoic evolution of the eastern Danish North Sea. Mar. Geol. 177, 243–269 (2001).
Westaway, R. Isostatic compensation of Quaternary vertical crustal motions: coupling between uplift of Britain and subsidence beneath the North Sea. Journal of Quaternary Science. 32(2), 169–182 (2017).
Cloetingh, S. et al. Lithospheric memory, state of stress and rheology: neotectonic controls on Europe’s intraplate continental topography. Quat. Sci. Rev. 24, 241–304 (2005).
Brink, H.-J. The evolution of the North German Basin and the metamorphism of the lower crust. International Journal of Earth Sciences (Geologische Rundschau). 94, 1103–1116 (2005).
Rickers, F., Fichtner, A. & Trampert, J. The Iceland–Jan Mayen plume system and its impact on mantle dynamics in the North Atlantic region: evidence from full-waveform inversion. Earth Planet. Sci. Lett. 367, 39–51, https://doi.org/10.1016/j.epsl.2013.02.022 (2013).
Schoonman, C. M., White, N. J. & Pritchard, D. Radial viscous fingering of hot asthenosphere within the Icelandic plume beneath the North Atlantic Ocean. Earth and Planetary Science Letters 468, 51–61 (2017).
Hoggard, M. J., Winterbourne., J., Czarnota, K. & White, N. Oceanic residual depth measurements, the plate cooling model, and global dynamic topography. J. Geophys. Res. Solid Earth 122, 2328–2372, https://doi.org/10.1002/2016JB013457 (2017).
Japsen, P. & Chalmers, J. A. Neogene uplift and tectonics around the North Atlantic: overview. Global and Planetary Change 24, 165–173 (2000).
Blundell, D. & Waltham, D. A possible glacially-forced tectonic mechanisms for late Neogene surface uplift and subsidence around the North Atlantic. In Proceedings of the Geologists’ Association. 120, 98–107 (2009).
Lambeck, K., Purcell, A., Zhao, J. & Svensson, N.-O. The Scandinavian Ice Sheet: from MIS 4 to the end of the Last Glacial Maximum. Boreas 39, 410–435 (2010).
Nielsen, S. B. et al. Palaeocene initiation of Cenozoic uplift in Norway. In Exhumation of the North Atlantic Margin: Timing, Mechanisms and Implications for Petroleum Exploration (eds Doré, A. G., Cartwright, J. A., Stoker, M. S., Turner, J. P. & White, N.) 45–65 (Geological Society London Special Publications 196, 2002).
Steffen, H., Gitlein, O., Denker, H., Müller, J. & Timmen, L. Present rate of uplift in Fennoscandia from GRACE and absolute gravimetry. Tectonophysics 474, 69–77, https://doi.org/10.1016/j.tecto.2009.01.012 (2009).
Mörner, N.-A. Glacial isostasy: regional –not global: International Journal of Geosciences 6, 577–592 (2015).
Berglund, M. Holocene shore displacement and chronology in Ångermanland, eastern Sweden, the Scandinavian glacio-isostatic uplift centre. Boreas 33, 48–60 (2004).
Westaway, R. Investigation of coupling between surface processes and induced flow in the lower continental crust as a cause of intraplate seismicity. Earth Surface Processes and Landforms 31, 1480–1509, https://doi.org/10.1002/esp.1366 (2006).
Westaway, R. Quaternary uplift of northern England. Global and Planetary Change 68, 357–382, https://doi.org/10.1016/j.gloplacha.2009.03.005 (2009).
Green P. F., Duddy I. R. & Hegarty K. A. Quantifying exhumation from apatite fission-track analysis and vitrinite reflectance data: precision, accuracy and latest results from the Atlantic margin of NW Europe. In Exhumation of the North Atlantic Margin: Timing, Mechanisms and Implications for Petroleum Exploration, (eds Doré, A. G., Cartwright, J., Stoker, M. S., Turner, J. P. & White, N.) 331–354 (Geological Society London Special Publications 196, 2002).
Japsen, P., Green, P. F., Nielsen, L. H., Rasmussen, E. S. & Bidstrup, T. Mesozoic-Cenozoic exhumation in the eastern North Sea Basin: a multi-disciplinary study based on palaeo-thermal, palaeo-burial, stratigraphic and seismic data. Basin Research 19, 451–490 (2007).
Clift, P. D. Coupled onshore erosion and offshore sediment loading as causes of lower crust flow on the margins of South China Sea. Geosci. Lett. 2(1), 1–11 https://doi.org/10.1186/s40562-015-0029-9 (2015).
Ziegler, P. A. & Van Hoorn, B. Evolution of the North Sea rift system. In Extensional Tectonics and Stratigraphy of the North Atlantic Margins (eds Tankard, A. J. & Balkwill, H. R.) 471–500 (Am. Assoc. Petrol. GeoL Mem. 46, 1990).
Huuse, M. & Clausen, O. R. Morphology and origin of major Cenozoic sequence boundaries in the eastern North Sea Basin: top Eocene, near-top Oligocene and the mid-Miocene unconformity. Basin Res. 13, 17–41 (2001).
Wong, T. E., Batjes, D. A. J. & De Jager, J. In Geology of the Netherlands (eds). (354 Royal Netherlands Academy of Arts and Sciences, KNAW, Amsterdam, 2007).
Huuse, M. Cenozoic uplift and denudation of southern Norway: insights from the North Sea Basin. In Exhumation of the North Atlantic Margin: Timing, Mechanisms and Implications for Petroleum Exploration (eds Doré, A. G., Cartwright, J. A., Stoker, M. S., Turner, J. P. & White, N.) 271–290 (Geol. Soc. Spec. Publ., 196, 2002).
Huuse, M. Late Cenozoic palaeogeography of the eastern North Sea Basin: climatic vs. tectonic forcing of basin margin uplift and deltaic progradation. Bulletin of the Geological Society of Denmark 49, 145–170 (2002).
Doornenbal, J. C. & Stevenson, A. G. Petroleum Geological Atlas of the Southern Permian Basin Area (eds) 342 (EAGE Publications, Houten 2010).
De Gans, W. Quaternary. In Geology of the Netherlands (eds Wong, Th.E., Batjes, D. A. J. & de Jager, J.) 173–195 (Royal Netherlands Academy of Arts and Sciences, 2007).
Streif, H. Nordsee und Küstenlandschaft- Beispiel einer dynamischen Landschaftsentwicklung. Akademie der Geowissenschaften zu Hannover e.V. 20, 134–149 (2002).
Huuse, M. & Lykke-Andersen, H. Overdeepened Quaternary valleys in the eastern Danish North Sea: morphology and origin. Quaternary Science Reviews 19, 1233–1253 (2000).
Ehlers, J. et al. Pleistocene glaciation of North Germany. In Quaternery Glaciations-Extent and Chronology 1, Developments in Quaternary Science (eds Ehlers, J. & Gibbard, P. L.) 135–146, (Vol. 2a Elsevier, Amsterdam 2004).
Carr, S., Holmes, R., Van Der Meer, J. J. M. & Rose, J. The last glacial maximum in the north SeaBasin: micromorphological evidence of extensive glaciation. Journal of Quaternary Science 21, 131–153 (2006).
Lutz, R., Kalka, S., Gaedicke, C., Reinhardt, L. & Winsemann, J. Pleistocene tunnel valleys in the German North Sea: spatial distribution and morphology. Zeitschrift der Deutschen Gesellschaft für Geowissenschaften 14, 225–235 (2009).
Kuhlmann, G. & Wong, T. E. Pliocene paleoenvironment evolution as Interpreted from 3D seismic data in the southern North Sea, Dutch offshore sector. Marine and Petroleum Geology 25, 173–189 (2008).
Stoker, M. S. & Long, D. A relict ice-scour erosion surface in the central North Sea. Marine Geology 61, 85–93 (1984).
Hovland, M. & Judd, A. G. In Seabed Pockmarks and Seepages. Impact on Geology, Biology and the Marine Environment (eds) 293 (Graham & Trotman, Boston, 1988).
Rafaelsen, B. et al. Geomorphologie of buried glacigenic horizons in the Barents Sea from 3D seismic data. Geological Society London 203, (259–276 (2002).
Graham, A. G. C., Lonergan, L. & Stoker, M. S. Evidence for Late Pleistocene ice stream activity in the Witch Ground Basin, central North Sea, from 3D seismic reflection data. Quaternary Science Reviews 26, 627–643 (2007).
Dowdeswell, J. A. & Ottesen, D. Buried iceberg ploughmarks in the early Quaternary sediments of the central North Sea: a two-million year record of glacial influence from 3D seismic data. Mar. Geol. 344, 1–9 (2013).
Airy, G. B. On the computation of the effect of the attraction of mountain-masses, as distributing the apparent astronomical latitude of stations in geodetic surveys, Philos. Trans. R. Soc. 145, 101–104 (1855).
Lyngsie, S. B. & Thybo, H. A new tectonic model for the Laurentia–Avalonia–Baltica sutures in the North Sea: a case study along MONA LISA profile 3. Tectonophysics 429, 201–227, https://doi.org/10.1016/j.tecto.2006.09.017 (2007).
Dressel, I., Barckhausen, U. & Heyde, I. A 3D gravity and magnetic model for the Entenschnabel area (German North Sea). International Journal of Earth Sciences, 1–14, https://doi.org/10.1007/s00531-017-1481-x (2017).
Turcotte, D. & Schubert, G. Geodynamics (eds) 435, (Wiley, New York 1982).
Watts, A. B. Isostasy and Flexure of the Lithosphere (ed) 480 (Cambridge University Press, 2001).
Cartwright, J. A. & Dewhurst, D. N. Layer-bound compaction faults in fine-grained sediments:. Geological Society of America Bulletin 110(10), 1242–1257 (1998).
Dewhurst, D. N., Cartwright, J. A. & Lonergan, L. The development of polygonal fault systems by syneresis of colloidal sediments:. Marine and Petroleum Geology (16)8, 793–810 (1999).
Arfai, J. & Lutz, R. 3D basin and petroleum system modelling of the NW German North Sea (Entenschnabel). In Petroleum Geology of NW Europe: 50 Years of Learning – Proceedings of the 8th Petroleum Geology Conference (eds Bowman, M. & Levell, B.), https://doi.org/10.1144/PGC8.35 (2017).
Arfai, J. et al. Late Palaeozoic to Early Cenozoic geological evolution of the northwestern German North Sea (Entenschnabel). New results and insights. Netherlands Journal of Geosciences 93(04), 147–174, https://doi.org/10.1017/njg.2014.22 (2014).
Brandes, C., Steffen, H., Steffen, R. & Wu, P. Intraplate seismicity in northern Central Europe is induced by the last glaciation. Geology 43, 611–614 (2015).
Ziegler, P. A. North Sea rift system. Tectonophysics 208, 55–75 (1992).
Gemmer, L., Nielsen, S. B., Huuse, M. & Lykke-Andersen, H. Post-mid Cretaceous eastern North Sea evolution inferred from 3-D thermo-mechanical modelling. Tectonophysics 350, 315–342 (2002).
Evans, D., Graham, C., Armour, A. & Bathurst, P. In The Millennium Atlas: Petroleum Geology of the Central and Northern North Sea (eds) 989 (The Geological Society of London, 2003).
Kley, J. & Voigt, T. Late Cretaceous intraplate thrusting in central Europe: effect of Africa-Iberia-Europe convergence, not Alpine collision. Geology 36(11), 839–842 (2008).
Kiden, P., Denys, L. & Johnston, P. Late Quaternary sea-level change and isostatic and tectonic land movements along the Belgian–Dutch North Sea coast: geological data and model results. Journal of Quaternary Science 17, 535–546 (2002).
Vink, A., Steffen, H., Reinhardt, L. & Kaufmann, G. Holocene relative sea-level change, isostatic subsidence and the radial viscosity structure of the mantle of north-western Europe (Belgium, the Netherlands, Germany, southern North Sea). Quat. Sci. Rev. 26, 3249–3275, https://doi.org/10.1016/j.quascirev.2007.07.014 (2007).
Anell, I., Thybo, H. & Artemieva, I. M. Cenozoic uplift and subsidence in the North Atlantic region: geological evidence revisited. Tectonophysics 474, 78–105, https://doi.org/10.1016/j.tecto.2009.04.006 (2009).
Heidbach, O., Rajabi, M., Reiter, K., & Ziegler, M. World Stress Map 2016. GFZ Data Services, https://doi.org/10.5880/WSM.2016.002 (2016).
Cloetingh, S. & Burov, E. Lithospheric folding and sedimentary basin evolution: a review and analysis of formation mechanisms. Basin Research 23(3), 257–290 (2011).
OpenStreetMap contributors. Planet dump retrieved from http://openstreetmapdata.com/data/generalized-coastlines (2017).
The authors thank the companies organized in the industrial association BVEG (Bundesverband Erdgas, Erdöl und Geoenergie e.V.), for allowing publication of the datasets for scientific research. We thank Andreas Bahr, Fabian Jähne-Klingberg, Christian Brandes, Ingo Dressel and Holger Steffen for their helpful suggestions. Special thanks go to the editor and the anonymous reviewers for their detailed comments and suggestions, which helped to improve this manuscript.
The authors declare no competing interests.
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Arfai, J., Franke, D., Lutz, R. et al. Rapid Quaternary subsidence in the northwestern German North Sea. Sci Rep 8, 11524 (2018). https://doi.org/10.1038/s41598-018-29638-6
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