Ice ages and marine isotope stages

Continuous records of Quaternary time are available from cores collected from the deep ocean and the Antarctic ice sheet (Fig. 1). For the last 120,000 years, the Greenland ice sheet provides an additional high-resolution record, of particular relevance to the North Atlantic and the study area (e.g. Lowe et al., Reference Lowe, Rasmussen, Björck, Hoek, Steffensen, Walker and Yu2008; Renssen et al., Reference Renssen, Seppä, Crosta, Goosse and Roche2012). Oxygen-isotope signals in ice cores and ocean-floor sediments record global, orbitally forced climatic variations. Observed oxygen-isotope cyclicity is mirrored between the ocean and ice-core records, thus bearing information on climate as reflected in global sea-level and ice-volume changes.

Fig. 1. Chronostratigraphical correlation table for the Quaternary (after Gibbard & Cohen, Reference Gibbard and Cohen2008; modified/updated 2009–2013, http://quaternary.stratigraphy.org/charts.

The ¹⁸O/¹⁶O ratio is conventionally normalised against a standard sample, resulting in the parameter δ¹⁸O. High values of δ¹⁸O indicate large ice volumes during cold lowstand periods known as glacials, and low values signify warm highstand periods known as interglacials (Fig. 1). In the standard subdivisions of δ¹⁸O records in marine isotope stages (MIS), interglacials are assigned odd and glacials even numbers. The MIS ages are constrained by dated palaeomagnetic reversals and volcanic tephras, and systematic orbital cyclicity is used to further constrain ages between these tie points (e.g. Lourens et al., Reference Lourens, Antonarakou, Hilgen, van Hoof, Vergnaud-Grazzini and Zachariasse1996; Lisiecki & Raymo, Reference Lisiecki and Raymo2005). The MIS scheme and its dating serves as a global target curve to correlate (not equate!) stratigraphic units from more discontinuous shallow marine, terrestrial and glacial environments too.

The MIS stack provides a globally integrated signal for the growth and decay of major ice volumes, with the European ice sheets accounting for 15–25% of the global ice-volume variability (e.g. Peltier, Reference Peltier2004). The timing and rate at which European ice sheets grew and decayed differs slightly from those of other ice sheets, notably from the much larger and slower moving one on North America (55–75%). The Scandinavian and British ice sheets reached their maximum extents at 30–25 ka, well before the global Last Glacial Maximum (LGM) around 21 ka, and were relatively quick to melt (e.g. Sejrup et al., Reference Sejrup, Nygård, Hall and Haflidason2009; Carlson & Clark, Reference Carlson and Clark2012; Hughes et al., Reference Hughes, Gibbard and Ehlers2013). The explanation for the earlier timing is to be sought in the vicinity of the North Atlantic and its warm currents, and applies to earlier cycles too.

The oldest known presence of humans in northwest Europe dates from the transition of the Early to the Middle Pleistocene, when the Earth’s climatic system saw profound change in its cyclicity. The latter has become known as the ‘mid-Pleistocene revolution’ (Berger & Jansen, Reference Berger, Jansen, Johannessen, Muench and Overland1994) or, less prosaically, the ‘mid-Pleistocene transition’ (Head et al., Reference Head, Pillans and Farquhar2008). In its broadest definition, this interval extends from about 1.2 Ma to 500 ka, thus spanning considerable time on either side of the internationally defined Early/Middle-Pleistocene boundary at 781 ka (Fig. 1). During the transition, glacial–interglacial cyclicity changed from an orbital-obliquity-paced 41-ka rhythm (i.e. relatively short glacials and comparatively long interglacials) to a slower 100-ka rhythm of much longer glacials alternating with relatively shorter duration interglacials. No evidence has been found for human presence in the North Sea region from before the mid-Pleistocene transition began (Ashton et al., Reference Ashton, Lewis and Stringer2011). This absence cannot be attributed to climate or palaeogeography because in temperate stages both would have been as hospitable before the mid-Pleistocene transition as they were during it.

During the Late Pliocene and Early Pleistocene, sea-level minima were not more than 70 m below preceding highstands. On the transition to the Middle Pleistocene, maximum continental ice volumes and associated high-to-lowstand amplitudes increased significantly. From MIS 22 (c. 800 ka) onwards, glacial sea level appears to have fallen as much as ∼150 m below interglacial levels. These maximum amplitudes were reached for some lowstands within the Cromerian Complex (MIS 20?, MIS 16?), for the Anglian (Elsterian; MIS 12) and for the end of the Saalian (MIS 6). The last glacial lowstand peaked at c. –120 m, some 21,000 years ago, within MIS 2. All maximum lowstands occurred relatively late in the glacials, out of phase with deglaciation in northwest Europe. Relatively early onsets of deglaciation in northwest Europe exposed areas to enhanced input of glacially derived sediment while sea level was still falling in the cooling limb of glacial cycles. Regional climatological effects (relative continentality, also seen in the palynological records, e.g. Turner, Reference Turner1996) and altered functioning of sedimentary systems in these deglaciated but still ‘arctic’ areas had major effects on the proglacial and periglacial landscapes of the southern North Sea basin (e.g. Roebroeks et al., Reference Roebroeks, Hublin, MacDonald, Ashton, Lewis and Stringer2011). These developments influenced Palaeolithic archaeology in two ways, which we regard as being of equal importance: (1) they affected the routes for human migration and settlement, and the trapping of archaeological record at times of postglacial and interglacial recolonisation of our latitudes by palaeohumans, and (2) they have affected the long-term preservation of archaeological record within interglacial deposits at times of post-interglacial habitat deterioration and local extinction of palaeohumans (e.g. Cohen et al., Reference Cohen, MacDonald, Joordens, Roebroeks and Gibbard2012).

Tectonics and glacio-isostasy

The relatively large thickness and completeness of the fill of the North Sea basin, a setting favourable for palaeogeographical mapping, are the result of steady, long-term tectonic subsidence. Averaged over multiple glacial cycles, the basin centre has subsided at rates up to 0.3 m/1000 yr (e.g. Kooi et al., Reference Kooi, Johnston, Lambeck, Smither and Molendijk1998). The degree of subsidence is a function of crustal stress fields between the Alps and the North Atlantic mid-oceanic ridge, which caused reactivation of a Triassic–Jurassic rift system early in the Miocene (25–20 Ma). Quaternary depocentres in the southern North Sea have hosted terrestrial lowland environments such as river and delta plains that from time to time experienced marine inundation (e.g. Rijsdijk et al., Reference Rijsdijk, Passchier, Weerts, Laban, van Leeuwen and Ebbing2005; Hijma et al., Reference Hijma, Cohen, Roebroeks, Westerhoff and Busschers2012). The basin margins appear tectonically stable and are marked by near-zero net subsidence/uplift areas that form the hinge zone of the basin. This hinge zone has received vast amounts of sediment, delivered by rivers originating in upstream areas of uplift. Part of this mostly fluvial input has been stored along the basin margin, in particular in the Lower Rhine Embayment where the rivers Rhine and Meuse enter the North Sea basin. Here, a patchy, dissected and terraced, but still relatively complete, Quaternary record exists. Reconstructions of the positions of the rim of the basin (i.e. the basin hinge line), and the boundary between long-term net subsiding and net uplifting substrate, are based on the occurrence and internal architecture of the terraced Quaternary record (e.g. van den Berg et al., Reference van den Berg, Groenewoud, Lorenz, Brus and Kroonenberg1994; Houtgast & van Balen, Reference Houtgast and van Balen2000; Meyer & Stets, Reference Meyer and Stets2002; Schäfer et al., Reference Schäfer, Utescher, Klett and Valdivia-Manchego2005; Van Balen et al., 2005; Boenigk & Frechen, Reference Boenigk and Frechen2006). The greater part of the fluvially delivered sediment has been transported well into the North Sea basin (Fig. 2).

Fig. 2. Quaternary tectonic and glaciation setting of the North Sea area (after Hijma et al., Reference Hijma, Cohen, Roebroeks, Westerhoff and Busschers2012).

For Palaeolithic archaeological prospection in particular, the tectonic setting matters, through its impact on spatial patterns of preservation and the depths at which deposits from hominin-favoured habitats would preserve (Cohen et al., Reference Cohen, MacDonald, Joordens, Roebroeks and Gibbard2012). For archaeological research and heritage management in the southern North Sea, it is important to realise that the main hinge line separating the Quaternary subsiding tectonic basin from the British–Southern Bight–Belgian older shoulder runs diagonally southeast–northwest through an offshore area between Holland and East Anglia (Fig. 2). In the depocentre, the seafloor substrate is dominated by a thick sequence of fluvial sands deposited by the Rhine and by North German rivers, which have long had their deltas in the present-day North Sea. For this now submerged area, terrestrial lowstand palaeolandscapes would have been comparable to those of the adjacent onshore Netherlands and northern Germany. Outside the North Sea basin proper (Fig. 2), the area between Flanders and East Anglia has been marked by mild uplift. Typical past landscapes would have been similar to palaeolandscapes as reconstructed for onshore Essex and Flanders, and the Southern Bight of the North Sea is underlain by Pleistocene-denudated Paleogene geology (Hijma et al., Reference Hijma, Cohen, Roebroeks, Westerhoff and Busschers2012). Even further south, the Strait of Dover crosscuts the currently inactive Weald–Artois anticlinal structure, with Mesozoic seafloor subcrop. This southern tip of the North Sea lies outside the North Sea tectonic basin. Note that the exact position of the hinge line is difficult to define and pin-point, and the position of the hinge line in the last 1 Ma may not have been exactly that of the last 250 ka or the last 2.5 Ma. One may prefer the term ‘hinge zone’ for that reason. This does not affect the general notion that the Southern Bight and Dover Strait in general are outside the tectonic subsidence area that is the North Sea Basin.

In addition, so-called glacial isostatic adjustment (GIA) forms a second mode of differential vertical crustal movement, operating at the same time scales as the glacial–interglacial cyclicity, driven by the growth and decay of ice-sheets and the associated changes in mass distribution over the earth surface. This induces oscillations in crustal warping that are more or less in phase with the climate and sea-level cycles. Owing to the visco-elastic nature of GIA, part of the adjustment is direct, part is stepped-delayed (e.g. Peltier, Reference Peltier2004; Lambeck et al., Reference Lambeck, Purcell, Funder, Kjær, Larsen and Moller2006; Steffen & Wu, Reference Steffen and Wu2011). During each glaciation, the crust below the ice sheet is depressed by the weight of ice up to 3 km thick (Fig. 3). In compensation, the peripheral area around the area of crustal depression experiences upwarping (forebulging). During deglaciation, and for some continued relaxation time thereafter, the suppressed areas rebound while in the periphery the forebulge collapses. The loading and unloading of shelf areas with the weight of sea water causes further perturbating warping effects (hydro-isostasy). Glacio and hydro-isostasy together controlled the timing and speed of transgression, the positioning of migrating coastlines of specific times and the depths at which sedimentary indicators of former sea levels from along palaeocoastlines are found preserved today (e.g. Lambeck, Reference Lambeck1995; Sturt et al., Reference Sturt, Garrow and Bradley2013), of relevance to Palaeolithic and Mesolithic submerged archaeology alike.

Fig. 3. Cartoon illustrating the ice thickness and GIA magnitude for Scandinavia, the North Sea basin and the periglacial foreland of northwest Europe (after Cohen et al., Reference Cohen, Stouthamer, Hoek, Berendsen and Kempen2009; abridged).

A further phenomenon related to GIA is the gravity effect of the presence of ice sheets and deepening oceanic water bodies. Regional accumulation of mass affects the geoid and increases the elevation of large ice-proximal water bodies relative to those of their distal counterparts. In the North Sea, the lowstand associated with the LGM was not at the global –120 m, but some tens of metres higher (e.g. Peltier, Reference Peltier2004; Steffen & Wu, Reference Steffen and Wu2011). The vertical positions at which palaeo-coastlines are currently encountered is controlled by syn-depositional geodetic and post-depositional GIA effects combined, complicating the environmental and palaeolandscape reconstructions for the North Sea area, during the last deglaciation (e.g. Lambeck, Reference Lambeck1995) and during earlier glacial–interglacial cycles (e.g. Lambeck et al., Reference Lambeck, Purcell, Funder, Kjær, Larsen and Moller2006).

GIA explains both the complex patterns and the differential timing of Holocene transgression along the North Sea coast, as seen along Britain and from Flanders to the German Bight. The magnitude of warping varies spatially and causes palaeocoastlines of the same early Holocene age to differ many metres in elevation when traversing the study area (Vink et al., Reference Vink, Steffen, Reinhardt and Kaufmann2007). These processes and conditions will have differed between glacial cycles, but in general the farther south within the study area, the more comparable the spatial patterns of GIA between successive larger glaciations. GIA in these distal ice-peripheral areas is relatively strongly affected by crustal properties that have remained constant through time, such as the presence of major fault systems bounding the North Sea basin (Lambeck et al., Reference Lambeck, Purcell, Funder, Kjær, Larsen and Moller2006). In ice-proximal northerly peripheral regions, variation in ice-load patterns makes GIA patterns differ more strongly from one glaciation to the next. Asymmetry of the peripheral forebulge (inset of Fig. 3) causes this. Particularly when geoid-change is accounted for in the datum to which the forebulge vertical displacements are expressed, it shows a restricted area of steep northern flank, a somewhat broader area with the warping crest and a much-stretched southward-decaying tail. Ice-mass differences between glacials change the centroid-position of the steep flank much more than they change it for the broader crest zone, and they hardly affect the centroid of the gentle southern flank.

GIA is, again, a process that affected post-glacial migration and recolonisation as well as long-term preservation, of relevance to the Palaeolithic of past interglacials (e.g. Hijma et al., Reference Hijma, Cohen, Roebroeks, Westerhoff and Busschers2012; Cohen et al., Reference Cohen, MacDonald, Joordens, Roebroeks and Gibbard2012), in very similar ways as it is affecting the latest Palaeolithic and Mesolithic archaeology of the current interglacial (e.g. Lambeck, Reference Lambeck1995; Smith et al., Reference Smith, Harrison, Firth and Jordan2011; Sturt et al., Reference Sturt, Garrow and Bradley2013), as well as younger coastal plain as well as even younger coastal-plain accumulation and archaeology (Kiden et al., Reference Kiden, Denys and Johnston2002; Cohen, Reference Cohen, Giosan and Bhattacharaya2005; Gouw & Erkens, Reference Gouw and Erkens2007; Hijma & Cohen, Reference Hijma and Cohen2011).

Patterns of differential crustal movement have strongly influenced the preservation of lowland depositional records, especially over periods of 10⁴ to 10⁶ years. Long-term subsidence creates conditions favourable to the preservation of interglacial deposits with possible archaeological remains over many subsequent glacial–interglacial cycles. In these types of settings, Early Palaeolithic sites can still be discovered today.

Before 500 ka, glaciations were not able to overprint the effects of tectonics and glacio-isostasy on the overall landscape. Various lowland environments aligned to subsidence depocentres and maintained relatively stable positions during the Cromerian Complex Stage between 1 Ma and 500 ka ago (Fig. 1). In highstand interglacial stages, this explains aspects of accumulation and preservation of the Early Palaeolithic record along the North Sea’s southern shores (Cohen et al., Reference Cohen, MacDonald, Joordens, Roebroeks and Gibbard2012). In lowstand glacial stages, the strong tectonic control on valley positioning made that major valley diversions were exceptional events. From 500 ka onward, however, the effects of extreme glaciations began to dominate those related to long-term subsidence. Direct and indirect glaciation impacts led to disruption and rerouting of river systems into and within the basin, thus providing strong control of the location of depositional systems, especially during the Anglian and Saalian glacial maxima (Gibbard, Reference Gibbard1988; Busschers et al., Reference Busschers, Kasse, van Balen, Vandenberghe, Cohen, Weerts, Wallinga and Bunnik2007, Reference Busschers, van Balen, Cohen, Kasse, Weerts, Wallinga and Bunnik2008; Hijma et al., Reference Hijma, Cohen, Roebroeks, Westerhoff and Busschers2012).

Glacially disturbed valley networks traverse and skim tectonic depocentres and uplifting areas rather than following differential-subsidence-controlled paths. Although the positioning of depositional centres associated with major valleys and river mouths was no longer tectonically controlled, vertical crustal movements continued to control preservation. The resulting record consists of buried deposits in areas of subsidence (e.g. Busschers et al., Reference Busschers, Kasse, van Balen, Vandenberghe, Cohen, Weerts, Wallinga and Bunnik2007) and preserved terraces along the basin rim, where uplift made interfluve areas out of former valley floors (e.g. Boenigk & Frechen, Reference Boenigk and Frechen2006). These contain Palaeolithic records, which require comparison and correlation to independently dated coastal and offshore sites (e.g. Parfitt et al., Reference Parfitt, Barendregt, Breda, Candy, Collins, Coope, Durbidge, Field, Lee, Lister, Mutch, Penkman, Preece, Rose, Stringer, Symmons, Whittaker, Wymer and Stuart2005, Reference Parfitt, Ashton, Lewis, Abel, Coope, Field, Gale, Hoare, Larkin, Lewis, Karloukovski, Maher, Peglar, Preece, Whittaker and Stringer2010; Preece & Parfitt, Reference Preece and Parfitt2012) to develop and test theories on migration patterns, habitat tracking and palaeohuman evolution (e.g. Hopkinson, Reference Hopkinson2007; Hublin, Reference Hublin2009; Cohen et al., Reference Cohen, MacDonald, Joordens, Roebroeks and Gibbard2012).

Chronostratigraphic division schemes

Seventeen major phases of alternating cold and temperate climate have been recognised in the terrestrial and shallow-marine record of the North Sea basin. Not all of them can be linked to a single MIS (Fig. 1; NW European Stages). Most glacials and interglacials are marked by multiple climate-driven phases of shorter duration (e.g. Lowe et al., Reference Lowe, Rasmussen, Björck, Hoek, Steffensen, Walker and Yu2008): relatively cold stadials and relatively warm interstadials. The Greenland ice-core record of the Late Pleistocene corroborates the subdivision made on the basis of the oceanic sediment-based isotopic record. The Greenland ice core also shows sub-Milankovitch oscillations that were relatively strong in amplitude and rather quick in alternation: several degrees of abrupt warming followed by slow cooling, over periods spanning between 500 and 2000 years (e.g. Lowe et al., Reference Lowe, Rasmussen, Björck, Hoek, Steffensen, Walker and Yu2008).

The last two glacials (Britain: the Wolstonian ‘Tottenhill’ substage and the Devensian; the Netherlands and Germany: the Saalian Drenthe substage and the Weichselian; southern North Sea: Saalian Drenthe substage, Last Glacial; Fig. 1) are most easily linked to the MIS record and correlated between sub-regions. For glacials and interglacials before (Britain: during the Anglian and Early Wolstonian; the Netherlands: Elsterian and Early Saalian; southern North Sea: Anglian and Early Saalian) linkage has been less easy. Linkage relies on stratigraphical reasoning, which combines arguments of biostratigraphic correlation with lithostratigraphic tracing, and aims to correlate records in the North Sea towards sites with numerical age constraints (e.g. Litt, Reference Litt, Sirocko, Claussen, Sánchez-Goñi and Litt2007; but sites with direct dating evidence are sparse) and to sites that directly recorded marine oxygen isostope signals (e.g. Toucanne et al., Reference Toucanne, Zaragosi, Bourillet, Gibbard, Eynaud, Giraudeau, Turon, Cremer, Cortijo, Martinez and Rossignol2009; but this requires tracing of signal over relatively long distances).

In the stratigraphical framework, the northwest European Holsteinian interglacial stage may be associated with either MIS 9 or MIS 11, whereas the British equivalent, the Hoxnian, correlates to a part of MIS 11 (most likely MIS 11c). The pollen-based palynological signals in deposits of these two interglacials are very similar in the North Sea region, which hinders stratigraphical correlations based on that type of information alone. This includes correlation to glacial–interglacial sequences in the Netherlands and the Lower Rhine Embayment (e.g. Zagwijn & van Staalduijnen, Reference Zagwijn and van Staalduinen1975; Kukla, Reference Kukla1978) and North Germany (e.g. Geyh & Müller, Reference Geyh and Müller2005), tracing of glaciogenic sedimentary signals to the shelf and deep-sea record of the coast of Norway and Scotland (e.g. Sejrup et al., Reference Sejrup, Nygård, Hall and Haflidason2009), and proglacial tracing of sedimentary signals to the shelf and deep-sea record of the English Channel and the Western Approaches (Toucanne et al., Reference Toucanne, Zaragosi, Bourillet, Gibbard, Eynaud, Giraudeau, Turon, Cremer, Cortijo, Martinez and Rossignol2009). Subglacially produced tills in the North Sea basin can also be tied to sequences of terraced river deposits that show mineralogical changes through time, induced by river course changes, and include several dated marker beds left by volcanic events (Boenigk & Frechen, Reference Boenigk and Frechen2006). Figure 1 contains our currently preferred correlations, but several issues remain unresolved, in part because direct dating evidence is sparse. This sparseness complicates open archaeological questions on the timing and nature of Lower to Middle Palaeolithic behavioural and evolutionary changes (Hopkinson, Reference Hopkinson2007).

On a different level, but equally uncertain, are the precise timing of the onset of the last interglacial and its duration, as registered in pollen records across terrestrial Europe. The broad correlation of the Eemian/Ipswichian to the beginning of MIS 5 (substage MIS-5e) is universally accepted (Fig. 1). The precise onset of the Eemian (base of pollenzone E1), however, somewhat lagged the start of MIS 5 (mid-point Termination II, Fig. 1) and may be diachronic across Atlantic Europe (e.g. Sánchez-Goñi et al., Reference Sánchez-Goñi, Eynaud, Turon and Shackleton1999; Sier et al., Reference Sier, Roebroeks, Bakels, Dekkers, Brühl, de Loecker, Gaudzinski-Windheuser, Hesse, Jagich, Kindler, Kuijper, Laurat, Mücher, Penkman, Richter and van Hinsbergen2011). The timing of regional maximum transgression of the North Sea also lags behind that of the global eustatic sea-level curve owing to glacio-isostatic adjustments in the periphery of the Scandinavian-British ice sheet (e.g. Lambeck et al., Reference Lambeck, Purcell, Funder, Kjær, Larsen and Moller2006) and to North Atlantic ocean-siphoning effects (e.g. Mitrovica & Milne, Reference Mitrovica and Milne2002). By influencing the regional climate, Late Saalian and Eemian regional developments in Greenland and the North Atlantic presumably delayed the interglacial climatic optimum relative to the global average signal, following similar mechanisms as in the Holocene (Renssen et al., Reference Renssen, Seppä, Crosta, Goosse and Roche2012), by at least the amount of lag time observed for the Holocene (2000 years), and given the instability of the Eemian Greenland ice sheet (NEEM community members, 2013) potentially longer. This will have controlled the regional vegetational development of the study area, used as a means of time control, stage-wise within the Eemian (e.g. pollenzones E1 to E6). The timing of the transgression further affected the regional climatic gradients and the distributions of sedimentary environments, in ways similar to those seen during the Holocene. The question is how the yet unknown lengths of regional climate-change and transgression delays (i.e. the degree to which these differed for the Eemian relative to the Holocene) propagate into and complicate palaeogeographical intercomparison of the last interglacial and the Holocene for the North Sea region. The simple approach has been to portray the Eemian as a clone of the Holocene. If both the climatic and the transgressive transitions in the Eemian of northwestern Europe occurred longer after the globally recognised beginning of the last interglacial (Termination II in Fig. 1) than their equivalent transitions did in the Holocene (following Termination I), this would be hard to identify in the current record because of numeric dating accuracy. Yet our current global climate-system understanding does predict this to be the case (text and references above). Uncertainty in the timing of climate change and transgression propagates to studies of Neanderthal habitat tracking and migration pathways in the North Sea basin, and between mainland Europe and Britain. It sets palaeogeographical reconstruction challenges that exceed the resolution that the currently established chronostratigraphical approaches (i.e. Fig. 1) can provide.

Lithostratigraphic division schemes

In the past decade, the various (national) lithostratigraphic subdivision schemes for the southern North Sea basin and its surrounding countries have been modified considerably (e.g. Doppert et al., Reference Doppert, Ruegg, van Staalduinen, Zagwijn, Zandstra, Zagwijn and van Staalduinen1975; van Adrichem Boogaert & Kouwe, 1993; Bowen, Reference Bowen1999; Gullentops et al., Reference Gullentops, Bogemans, de Moor, Paulissen and Pissart2001; Laga et al., Reference Laga, Louwye and Geets2001; McMillan, Reference McMillan2002, Reference McMillan2005; Ebbing et al., Reference Ebbing, Weerts and Westerhoff2003; Westerhoff et al., Reference Westerhoff, Wong, de Mulder, de Mulder, Geluk, Ritsema, Westerhoff and Wong2003; Rijsdijk et al., Reference Rijsdijk, Passchier, Weerts, Laban, van Leeuwen and Ebbing2005; Weerts et al., Reference Weerts, Westerhoff, Cleveringa, Bierkens, Veldkamp and Rijsdijk2005). Differences between these schemes exist for various reasons.

First, onshore lithostratigraphic systems are difficult to correlate with offshore seismostratigraphic units. Second, the politico-geographical division of the North Sea continental shelf is a complicating factor. Even the originally common scheme developed by the British, Belgian, Dutch, German and Danish geological surveys while jointly mapping the North Sea has been abandoned by some partners. Third, researchers have worked with and have chosen to formalise division schemes on different scales, which is understandable given the differences in geological setting. Many deposits that rank as ‘Formations’ in the British system, for example, equate to ‘Members’ in the Dutch system (Westerhoff et al., Reference Westerhoff, Wong, de Mulder, de Mulder, Geluk, Ritsema, Westerhoff and Wong2003), and also between onshore and offshore schemes different hierarchical slotting decisions are made. Quite a few of these lithostratigraphic units are specifically associated with remnants of various landscapes formed at different times. Seismo-lithostratigraphic ‘Formations’ recognised offshore, on the other hand, are particularly inclusive. They match the scale of onshore Dutch ‘Formations’ and ‘Subgroups’ and onshore British ‘Subgroups’ and ‘Groups’.

A final reason for regional differences in schemes and for correlation problems between onshore and offshore litho- (seismo-) stratigraphic units applies only to deposits in the older part of the Quaternary. There is a loss of discriminating lithological detail when units are traced from the basin margin (river valley) to the basin centre (alternating submerged shallow-marine environments and emerged fluvial plains) because the deposits of multiple sources become increasingly mixed and consequently lose many of their unique provenance-indicative fingerprints. The higher rates of subsidence near the basin depocentre increase the chance that multiple erosional levels are preserved. Towards the basin margins, recycling is increasingly severe, with fewer and fewer recycling episodes being preserved in separate layers. In areas with little or no net deposition, an amalgamated record of multiple recycling events is commonly all that remains, making it difficult to reconstruct palaeogeography.

Features from glacial times

The harshest Pleistocene glacials caused erosion and widespread reworking, creating and mobilising sediment. The North Sea area was (partly) covered by land ice for only a brief part of these glacials. For a much larger part of the time, terrestrial ‘periglacial’ conditions were dominant. Near the depocentre, the glacial depositional record is relatively complete, which is of particular significance to the study of the Early and Middle Palaeolithic.

Sub-glacial landforms: These include depositional (‘till sheets’) and erosional features (tunnel valleys, tongue basins). The former occupy laterally extensive areas throughout the glaciated region. The latter are elongated and remarkably deep features presumably formed by pressurised, super-cooled sub-glacial flows of water controlled by ice-sheet hydrology (e.g. Moreau et al., Reference Moreau, Huuse, Janszen, van der Vegt, Gibbard and Moscariello2012). Relatively small-scale tunnel valleys occur on Chalk bedrock of East Anglia (Anglian age; Woodland, Reference Woodland1970) and immediately offshore (Anglian/Wolstonian/Devensian age). Up to seven generations (from up to five glacial cycles, MIS 12 to MIS 4; Stewart & Lonergan, Reference Stewart and Lonergan2011) have been recognised in the North Sea, where they are much larger. The largest of the tunnel valleys (Anglian/Elsterian age) are infilled by glacio-lacustrine sediments that accumulated during deglaciation, and by lacustrine and marine deposits from post-glacial times (Laban, Reference Laban1995; Lee et al., Reference Lee, Busschers and Sejrup2012; Moreau et al., Reference Moreau, Huuse, Janszen, van der Vegt, Gibbard and Moscariello2012). The valleys are therefore important containers of palaeoenvironmental information. Positive-relief sub-glacial landforms (e.g. eskers), which may have been temporary palaeosurfaces, are relatively rare in the North Sea basin.

Ice-marginal landforms: These features form immediately next to ice margins. They are most strongly developed where land ice reached its maximum extent and near former ice limits associated with temporary re-advances, but occur all over formerly glaciated areas. The distribution of depositional positive-relief features (ice-pushed ridges, deltas, delta-moraines, ice-marginal fans and kames, sandar) – especially where associated with erosional subglacial ice-marginal landforms such as tongue basins (see above) – can be used in reconstructions of past ice-margin changes. Large-scale Saalian morainic and ice-pushed ridges mark terrestrial still-stand positions at several sites across the North Sea basin (e.g. van den Berg & Beets, Reference van den Berg, Beets and van der Meer1987; Busschers et al., Reference Busschers, van Balen, Cohen, Kasse, Weerts, Wallinga and Bunnik2008). Where the ice fronts were submerged, sediment-rich meltwater created deltas or fan-like accumulations that form ridge-like delta-moraines where coalesced, such as in the Anglian of Norfolk (Cromer Ridge; Gibbard & van der Vegt, Reference Gibbard, van der Vegt, Dixon and Markham2012). Depressions created by ice scour tend to occur upstream of ice-pushed constructional landforms. In some aspects they are comparable to the tunnel valleys discussed above, but their relation with surrounding ice-pushed ridge topography signals a different genesis (pushing material towards the sides, e.g. van den Berg & Beets, Reference van den Berg, Beets and van der Meer1987, rather than eroding it and moving it longitudinally). In the North Sea, most Anglian and Saalian ice-marginal landforms have been eroded by processes associated with deglaciation and periglacial stages, and locally by Devensian ice. The scant and discontinuous morphological evidence for ice-margin positions is a major obstacle in Quaternary palaeogeographical studies of the North Sea area.

Proglacial features: Continental ice sheets have released considerable volumes of meltwater and sediment into the North Sea area. Outwash systems, such as sandar fans and ice-marginal rivers, formed during advance as well as recession. When meltwater could not freely drain, it ponded to form proglacial lakes, in which case the outwash systems developed into fan-deltaic and subaquatic variants. Direct blockage and proglacial ponding also affected rivers that flowed towards the ice front in northerly directions. To the east (e.g. Winsemann et al., Reference Winsemann, Asprion and Meyer2004) and west (e.g. Gibbard, Reference Gibbard and Preece1995) of the present-day North Sea, river valleys relatively close to the ice front were temporarily occupied by proglacial or ice-dammed lakes. The largest-scale ponding occurred when Scandinavian and British ice fronts joined and blocked northward meltwater drainage. Allegedly, the largest proglacial lake thus formed occupied much of the southern North Sea basin during part of the Anglian/Elsterian Stage (Fig. 4). Its existence and size are primarily inferred from erosional geomorphological evidence, however, and direct evidence in the form of fine-grained lacustrine facies has never been found in the North Sea basin proper. Poor preservation of proglacial sedimentary evidence is a major problem in studies on North Sea glaciations older than 150,000 years. Although it is thought that lakes formed along the ice margin of all the major glaciations, and changed in response to the ice-margin mobility through time, all existing reconstructions are highly speculative (Murton & Murton, Reference Murton and Murton2012).

Fig. 4. Drainage basin and delta of the Miocene–Pliocene–Early Pleistocene Eridanos river system (after Overeem et al., Reference Overeem, Weltje, Bishop-Kay and Kroonenberg2001). Background map depicts former terrestrial environment in Middle-Pleistocene-glacial excavated areas that are nowadays seas.

Preservation of glacio-lacustrine deposits differs strongly for the two end-member types of proglacial lake that exist. Whereas many sub-glacially eroded features contain distal glacio-lacustrine infill (commonly continuing upward into postglacial fill), proglacial lakes from times of maximum glaciation left a predominantly erosional record. Water levels in these latter lakes were unstable because the outlet levels changed continuously following short-lived phases of maximum lake level and extent. Partial lake drainage during ice-margin reconfigurations at maximum glaciation and during initial deglaciation stages reduced water depths and reduced the areal extent of lakes south of the ice front. Where distal lake beds fell dry, newly established fluvial channels caused widespread erosion of the accumulated lake deposits. Former lake shorelines and abandoned lake deltas are heavily dissected, if at all present, and terraces formed during lake stages cannot easily be distinguished from normal fluvial terraces produced in the same river valleys. Sediment provenance in wide river plains and shallow-lake braided-river delta plains is the same, sediment body thickness is very similar and sedimentological structures in part of the deposits may be differentiating, but to prove that demands very detailed study in multiple large outcrops (i.e. monitoring exposures in active quarries over years). Tracing sedimentary units downstream may be a way to distinguish ‘continuous’ valley trains from ‘widening and terminating’ delta lobes (Cohen et al., Reference Cohen, Gibbard, Busschers, Dehnert and Preusser2005; Busschers et al., Reference Busschers, van Balen, Cohen, Kasse, Weerts, Wallinga and Bunnik2008), but to do so across the hinge zone means switching from terrace record (dissected exposures) to buried deposits (boreholes), which in the case of the study area are in turn deformed by ice-margin activity (displaced, glacio-tectonised exposures), again complicating matters. The incomplete record of proglacial features, increasingly fragmentary for older glaciations, thus complicates palaeogeographical reconstructions and has limited reconstructions for, for example, the Anglian to the conceptual level (Fig. 5).

Fig. 5. Proglacial lake extent leading to initial breaching of the Strait of Dover, as envisaged for the early stages of maximum Anglian glaciation (from Cohen et al., Reference Cohen, Gibbard, Busschers, Dehnert and Preusser2005; Gibbard, Reference Gibbard2007). With a quote from Belt (Reference Belt1874).

Periglacial river valleys: During lowstands, lakes and rivers occupied the lowest parts of the landscape, and regional groundwater tables in the adjacent lowlands were within a few metres of the surface, well above coeval sea level. The North Sea floor during glaciation maxima was a polar landscape dissected by rivers. Its hydrology was affected not only by precipitation and groundwater flow, but also by permafrost (year-round frozen substrate) development and melt. Abundant mammoth bones and other mammal skeletal remains dredged from the North Sea floor (e.g. van Kolfschoten & Laban, Reference van Kolfschoten and Laban1995) are evidence of less hostile circumstances and indicate that the most severe polar-desert conditions were relatively short-lived. For much of the periglacial times, the present-day North Sea probably was a dry grassy steppe-tundra, perhaps with patches of boreal forest at times. It is likely that the river valleys were hospitable sanctuaries for herds of mammals during the harshest times, providing drinking water, and being slightly warmer and more fertile than the surrounding upland. Repeated sea-level (base-level) fall during the past 1 Ma is reflected in river incision and in increased denudation of emergent surfaces. Sediment removed from periglacial land areas was deposited in shrinking and expanding marine basins. Close to the coast, valley gradients were gentle, valleys wide and river incision was limited. The dominance of stacked braid-belt architectures throughout the basin, evidence of extensive reworking rather than just incision or aggradation (e.g. Busschers et al., Reference Busschers, Kasse, van Balen, Vandenberghe, Cohen, Weerts, Wallinga and Bunnik2007; Hijma & Cohen, Reference Hijma and Cohen2011), suggests the ‘low-shouldered, delta-capped’ palaeovalleys and associated in situ archaeological remnants to have a relatively high preservation potential, at least below present onshore areas. Offshore along the North Sea’s erosive exit route across Southern Bight basin shoulder terrain preservation of the palaeovalley units is far less favourable (e.g. Hijma et al., Reference Hijma, Cohen, Roebroeks, Westerhoff and Busschers2012). In these areas, relatively coarse reworked lag deposits lay at relatively shallow depths below the seafloor, within reach of dredging (e.g. Hijma et al., Reference Hijma, Cohen, Roebroeks, Westerhoff and Busschers2012), which paradoxically have produced a richer ex situ paleontological and Palaeolithic record than better preserved periglacial areas to the north (e.g. Mol et al., Reference Mol, Post, Reumer, van der Plicht, de Vos, van Geel, van Reenen, Pals and Glimmerveen2006). Further west into the southern North Sea, in the hinge zone and outside the North Sea basin, localised palaeovalley infill from British river systems have been encountered below gravel lags from the youngest stages (e.g. Bridgland & D’Olier, Reference Bridgland, D’Ollier and Preece1995), which may well host a complementary record to the bone-gravel-lag from the Lower Rhine in the North Sea.

Periglacial landscapes outside valleys: Permafrost was common in areas exposed to terrestrial processes during lowstand conditions. Seasonal freezing and thawing gave rise to complex suites of depositional and erosional landforms. Typically, the erosional forms reflect the removal of material by wind, water and mass-flow processes, especially where and when vegetation cover was patchy or absent. Frost-dominated processes acted on the different substrates in different ways. Chalk, for example, is susceptible to mass flow and to cold-water dissolution under periglacial conditions. Dry valleys, dolines and solutional pipes are common. Arenaceous Pliocene and Early Pleistocene terrains are prone to deflation. Clayey intercalations are not deflated easily, which in the lowlands of the southwest Netherlands left Early Pleistocene plateaux with a Middle to Late Pleistocene periglacial veneer (Westerhoff et al., Reference Westerhoff, Weerts, Menkovic and Westerhoff2009). Where undercut by migrating channels in valleys, periglacial freezing cycles and meltwater production on steepened hill slopes promoted mass wasting of the clayey strata. On the depositional side, wind-blown dust (loess) and sand accumulated across extensive regions. In the North Sea basin, sandy aeolian deposits are widespread, derived in part from nearby sources in local periglacial river systems (e.g. van Huissteden et al., Reference van Huissteden, Vandenberghe, van der Hammen and Laan2000). The southern rim of the North Sea basin is the northern edge of the European loess belt. Here, silt is the dominant wind-blown deposit, originating from the fluvial plains of the larger rivers (e.g. Antoine et al., Reference Antoine, Catt, Lautridou and Sommé2003).

The periglacial interfluve landscape provided the initial conditions for soil and hydrological and vegetation and faunal developments each time the climate ameliorated from cold to temperate. There was a direct control on human habitats in terrestrial settings outside deltas and coastal plains (see below). For Palaeolithic and Mesolithic archaeology in and around the North Sea, the periglacial geomorphological activity in the interfluve areas further caused (1) fresh substrate to be exposed at accessible locations along secondary drainage systems (local rivers, brooks, doline lakes, hollows, small caves) and landmark landforms (plateau areas, low cuesta escarpments), and (2) cold-stage aeolian and colluvial cover to be developed over temperate stage surfaces. Typically, the temperate stages inherit the periglacial interfluve drainage networks and substrate exposures. This has enabled humans to trace discoveries of suitable quantities of flint in gravels of active rivers upstream to the substrate source areas where these were entrained from older terrace gravels (coarser grained strata from older terraces) and even to the original bedrock sources itself. Whereas proglacial activity and big river activity have altered the long-distance migration paths of palaeohumans in a progressive way (next section), interfluve activity in equally progressive ways affected resource accessibility around and in the youngest eroded parts of the southern North Sea (Cohen et al., Reference Cohen, MacDonald, Joordens, Roebroeks and Gibbard2012; Hijma et al., Reference Hijma, Cohen, Roebroeks, Westerhoff and Busschers2012). The aeolian and colluvial periglacial cover of temperate surfaces is an important element of the local preservation of archaeology. Progressive changes in the effectiveness of especially aeolian cover (notably in relation to growth of the Channel River) affect site taphonomy and differences therein between upwind England and downwind continental Europe (Hijma et al., Reference Hijma, Cohen, Roebroeks, Westerhoff and Busschers2012). Such differences, however, would hold more strongly for upland areas surrounding the North Sea and the English Channel, than for the buried landscapes below the Southern North Sea floor (that we see as source region for loess predominantly), within the ecotone of habitat availability (Parfitt et al., Reference Parfitt, Ashton, Lewis, Abel, Coope, Field, Gale, Hoare, Larkin, Lewis, Karloukovski, Maher, Peglar, Preece, Whittaker and Stringer2010).

Features from temperate (interglacial) times

After each glaciation, climate amelioration and associated sea-level rise forced significant faunal and vegetation changes, as well as dramatic modification of hydrological regimes. The rising sea transformed large terrestrial areas into open sea and coastal zones. In areas not submerged, depositional styles of river valleys changed, and soil-formation processes intensified. Erosion and reworking were less widespread during interglacials than under periglacial conditions, but few interglacial terrestrial deposits survive in the long term. They are easily and preferentially eroded during subsequent glacials, making interglacial (and interstadial) palaeolandscapes and in situ archaeological remnants rare in comparison to their periglacial counterparts, but exceptions exist. Holocene deposits are one such exception, of course, because they are part of a still accumulating interglacial record. Over time scales longer than an interglacial, only the deepest fills of tidal, estuarine and fluvial channels have relatively high preservation potential. This also stretches to buried drowned valleys, of which the relatively early and deepest drowned segments in the highstand coastal zone (Hijma & Cohen, Reference Hijma and Cohen2011) may have better odds of survival than segments farther inland (e.g. Busschers et al., Reference Busschers, Kasse, van Balen, Vandenberghe, Cohen, Weerts, Wallinga and Bunnik2007) and seaward (Hijma et al., Reference Hijma, Cohen, Roebroeks, Westerhoff and Busschers2012). In the southern North Sea, this is of demonstrated relevance for near-coastal Mesolithic site coverage (Weerts et al., Reference Weerts, Otte, Smit, Vos, Schiltmans, Waldus, Borst, Bebermeier, Hebenstreit, Kaiser and Krause2012; Moree & Sier, Reference Moree and Sier2014) and may also be of relevance in research on Palaeolithic interglacial re-dispersal routes (cf. Cohen et al., Reference Cohen, MacDonald, Joordens, Roebroeks and Gibbard2012).

Interglacial deposits filling glacial-scour features: Interglacial landforms and deposits preserved in deep glacial-scour features, limited to those warm periods that immediately followed the few episodes of glaciation of the North Sea area, tend to be preserved. Where such features host subaquatic deposits that accumulated in metres-deep lake waters, this provides excellent by-proxy records for palaeoenvironmental reconstruction. The deposits have hence been targeted in the past by Quaternary stratigraphers and many studied locations have become classic sites (being the namesakes of many of the regional stratigraphic units in Fig. 1). It is unlikely that humans lived in these infilling glacial-scour features. For archaeology the palaeoenvironmental information is of contextual importance only, unless lakeshore deposits have also been preserved. In areas that are initially lake but were later transgressed by the sea, the odds for preservation of deposits from lake shore settings are relatively high. This would hold for most such lakes in the present North Sea region (e.g. Briggs et al., Reference Briggs, Thomson, Gaffney, Gaffney, Thomson and Fitch2007; Murton & Murton, Reference Murton and Murton2012) and could also hold for Eemian equivalent environments at depth below the Holocene coastal plain (e.g. Peeters et al., Reference Peeters, Busschers and Stouthamer2014).

The seafloor: On transgression and inundation by the North Sea, newly submerged areas became subject to tidal currents and to wave action, and were obviously no longer inhabitable palaeolandscapes. Sandy substrates were most easily reworked by currents and waves into bank features (see Cooper et al., Reference Cooper, Townend and Balson2008 for an overview). Fields of sand waves, ubiquitous in the present-day North Sea, must have been common during each highstand. Sand-wave migration and shoreface erosion left ravinement surfaces, lags of coarse clasts that may include archaeological artefacts and mammal remains. The ravinement surface of the last interglacial is an important stratigraphical marker under the North Sea. Mollusc assemblages of the Holocene, Eemian and older interglacial North Seas differ in composition, aiding their stratigraphical distinction (e.g. Meijer & Preece, Reference Meijer and Preece1995; Rijsdijk et al., Reference Rijsdijk, Kroon, Meijer, Passchier, van Dijk, Bunnik and Janse2013). For archaeology, it is mostly the degree to which marine ravinement eroded terrestrial palaeosurfaces that matters. Over considerable areas of North Sea floor, the Holocene marine ravinement did erode the inherited Last Glacial periglacial surface and Early Holocene soils within them. There are, however, considerable areas where in the first stages of transgression sedimentation had dominated, and Early Holocene soil and covering peats have been preserved at some depth (typically 1–4 m) below the seafloor. In such areas, the surfaces stand a chance of escaping future marine reworking because the reworking is restricted in depth and only affects the transgressive cover. In these cases it is not the erosion-scarred seafloor that is the drowned landscape, but a more pristine, better protected buried landscape found somewhere below the seafloor (Ward & Larcombe, Reference Ward and Larcombe2008; Weerts et al., Reference Weerts, Otte, Smit, Vos, Schiltmans, Waldus, Borst, Bebermeier, Hebenstreit, Kaiser and Krause2012; Moree & Sier, Reference Moree and Sier2014).

Coastal features and the drowned landscape below: In the highly dynamic environments of the coastal zone, preservation of transgressed surfaces is a function of sediment supply at the time of transgression, besides eventual water depth in the subsequent highstand stage. This appears to hold both for sand-dominated systems such as the Holland Barrier coast (Beets & van der Spek, Reference Beets and van der Spek2000) and for extensive mixed-load river mouth areas that indent, underlay and dissect it, where the lowstand surface was covered with fines as part of the transgressive developments (Hijma & Cohen, Reference Hijma and Cohen2011). The modern Dutch barrier coast, formed from the Middle Holocene onward, owes its position and width in part to the abundance of fluvial Pleistocene sand reworked shoreward from the low-gradient offshore North Sea floor. Near the coastline, erosion was partly a function of the shoreface and nearshore gradient. Steep gradients render a coast vulnerable to wave attack and destruction of palaeosurfaces.

The present North Sea coast of East Anglia down to the Thames Estuary, with its cliffs, bluffs and estuaries that originated from drowned valleys, differs from that of Flanders, Holland, the Wadden Islands and large parts of the German Bight. From northwest France to Denmark, the coast of mainland Europe is fringed by a series of sandy barriers that protect muddy back-barrier lagoons, swampy deltas, tidal inlets and estuaries resulting from marine incursions. However, the Weser and Elbe estuaries can be viewed as estuaries in drowned (Pleistocene) valleys. These latter estuaries formed in deeply incised valleys in the Saalian till.

Large parts of the lowland on the continental European side of the North Sea contain remnants of former back-barrier coastal landscapes (tidal basin, lagoon, marsh and peatland). The Pleistocene substrate of the western and northern Netherlands shows the marks of a tidally modified fluvial palaeolandscape that extends far, but discontinuously, below the North Sea, all the way to the Dogger Bank (Fig. 2; Gaffney et al., Reference Gaffney, Thomson and Fitch2007). Although coastal processes such as shoreface erosion and tidal-inlet scouring have modified the drowned fluvial palaeolandscape, large-scale palaeosurface patterns have survived in many places. The inherited Pleistocene morphology has influenced the development and spatial distribution of archaeologically relevant coastal features such as barriers, beach plains and river outlets. All rivers in the North Sea area have been strongly affected by Holocene sea-level rise. It changed patterns of fluvial sedimentation up to c. 150 km from the coast in the low-gradient bigger rivers, played a role in the formation and demise of distributaries (and thus sediment delivery to the coast; Beets & van de Spek, Reference Beets and van der Spek2000; Berendsen & Stouthamer, Reference Berendsen and Stouthamer2000; Hijma & Cohen, 2012), and governed peat formation in active and abandoned alluvial plains (and thus accommodation and preservation of palaeosurfaces and sedimentary layers including any contained archaeology and palaeoenvironmental information; Cohen, Reference Cohen, Giosan and Bhattacharaya2005; Gouw & Erkens, Reference Gouw and Erkens2007). This also took place in earlier interglacials (e.g. Busschers et al., Reference Busschers, Kasse, van Balen, Vandenberghe, Cohen, Weerts, Wallinga and Bunnik2007).

Estuaries and tidal inlets can scour to depths many tens of metres below sea level. Estuaries and tidal inlets along the modern Netherlands coast in their present form result from Medieval storm surges, and many do not have a strong valley-inherited morphology. Most of them have very limited direct spatial relations with equivalent palaeoenvironments from older stages. Unlike these modern features, Early to Middle Holocene estuaries did occupy valley-inherited positions (e.g. Beets & van der Spek, Reference Beets and van der Spek2000; Vos et al., Reference Vos, Bazelmans, Weerts and van der Meulen2011; Hijma & Cohen, Reference Hijma and Cohen2011), and these environments contain the mesolithic wetland archaeological record (Verhart, Reference Verhart1988; Weerts et al., Reference Weerts, Otte, Smit, Vos, Schiltmans, Waldus, Borst, Bebermeier, Hebenstreit, Kaiser and Krause2012; Moree & Sier, Reference Moree and Sier2014). In the later Holocene, however, deltaic avulsions have successively shifted river-mouth positions (Berendsen & Stouthamer, Reference Berendsen and Stouthamer2000), at first away from inherited positions and in some cases returning later on.

As on the Belgian–Netherlands side, the deepest parts of English fills have the best chance of survival. Preserved bases of older generations of estuarine and inlet fills provide palaeogeographically relevant information, and may hold archaeological and palaeontological material. In the Southern Bight, the estuaries along the Essex coast are of a different nature to those on the Flemish–Dutch side. The British estuaries have transformed from valley into estuary, and back, several times over multiple glacial–interglacial cycles. In the absence of major subsidence, sediments of older stages have been preserved as terraces along the valley margins (e.g. Roe & Preece, Reference Roe and Preece2011). Estuaries are amongst the richest coastal habitats in terms of readily available nutrition and palaeohumans may well have exploited them since relatively early in their evolutionary history (Cohen et al., Reference Cohen, MacDonald, Joordens, Roebroeks and Gibbard2012, and sources therein).

On the British side of the North Sea, coasts with cliff and bluff erosion that irreversibly exposes older strata are common. Their formation is driven by storm-related wave action and by precipitation-related destabilisation of rock or sediment. Palaeo-cliff lines (currently submerged as well as inland) indicate that final highstand features may survive during subsequent glacials. They are excellent palaeo-coastline indicators. Cliff-line retreat during interglacial highstands (lasting some 10,000 years on average) was several kilometres, judging from present retreat rates. Rates differ with the cliff's geological composition (Weald–Artois: chalk; East Anglia: till) and exposure to waves. The higher parts of these cliffs are also denuded under periglacial circumstances, while colluvium accumulates at their base. The repeated alternation of marine and periglacial conditions may have promoted long-term cliff retreat. In the depocentre part of the North Sea therefore, palaeocliffs should not be expected to be a common feature. In the Southern Bight, former cliff lines can be projected seaward from the present position and possibly explain concentrations of finds from within the marine ravinement bed. Where cliff retreat exposes older interglacial strata, potentially archaeologically relevant units and palaeosurfaces become newly exposed (e.g. East Anglia; Parfitt et al., Reference Parfitt, Ashton, Lewis, Abel, Coope, Field, Gale, Hoare, Larkin, Lewis, Karloukovski, Maher, Peglar, Preece, Whittaker and Stringer2010). Where palaeo-cliff lines formed in flint-containing material, they are archeologically relevant from a natural-resource perspective (e.g. southern England; Bates et al., Reference Bates, Parfitt and Roberts1997).

Inland interglacial features: During temperate periods, the landscape of western Europe was characterised by the establishment of a dense broad-leaf forest that colonised interfluve and valley areas alike (e.g. West, Reference West, Rose and Schlüchter1989, Reference West and Turner1996). The biodiversity of both fauna and flora increased markedly during each phase of climate amelioration. Interglacial mammalian assemblages typically included a wide range of taxa, many of which are now associated with warmer regions. Abundant remains of beaver, aurochs, deer, elephant, bear, rhinoceros, hyena and lion have been found in units from different interglacials (e.g. Schreve, Reference Schreve2001; Schreve & Bridgland, Reference Schreve and Bridgland2002). Preserved records of small rodents and freshwater molluscs are useful in providing time frames for these units, also in fluvially and marine reworked contexts (e.g. Mayhew et al., Reference Mayhew, Dieleman, Slupik, van den Hoek Ostende and Reumer2014). The bones of birds, fish and amphibians are important palaeoenvironmental indicators too (e.g. Joordens et al., Reference Joordens, Wesselingh, de Vos, Vonhof and Kroon2009; Finlayson et al., Reference Finlayson, Carrión, Brown, Finlayson, Sánchez-Marco, Fa, Rodríguez-Vidal, Fernández, Fierro, Bernal-Gómez and Giles-Pacheco2011). Representatives of the genus Homo were widespread throughout the region during several warmer phases. In addition to the biota, preserved forest-type palaeosols and remnants of peat blankets are diagnostic of interglacial conditions (e.g. Zagwijn, Reference Zagwijn1996; Stremme, Reference Stremme1998; Turner, Reference Turner2000). They reflect inland palaeolandscapes that were remarkably stable. The interglacial land surface was either cloaked in dense vegetation on rich forest soils or covered by peat blankets in areas with poor drainage, generally preventing soil erosion and slope instability. Flood response in rivers was mitigated because precipitation was trapped rather than discharged directly in the form of runoff. Most rivers occupied stable channels between wooded floodplains, flooded only following snowmelt and rain storms in the hinterland (e.g. Busschers et al., Reference Busschers, Kasse, van Balen, Vandenberghe, Cohen, Weerts, Wallinga and Bunnik2007; Lewin & Gibbard, Reference Lewin and Gibbard2010; Peeters et al., Reference Peeters, Busschers and Stouthamer2014).

Periods of stability, marking the warmest parts of interglacials, were preceded and followed by phases of steady change, related to climate amelioration and deterioration. Records of regional vegetation succession and accompanying faunal colonisation and decolonisation form some of the clearest evidence of changing palaeolandscape dynamics. The permanent loss of some taxa and the arrival of new forms has been used as an effective means of discriminating between past interglacials. As man is a terrestrial species, all these inland matters affected archaeology in numerous ways while the rivers were creating their sedimentary record (syn-depositional, short-term preservation; cf. Cohen et al., Reference Cohen, MacDonald, Joordens, Roebroeks and Gibbard2012). For long-term preservation, it then matters what marine drowning and glaciation have done to the fluvial deposits (post-depositional, long-term preservation), which has been reviewed above.

Loss of the Eridanos river system

A major Middle-Pleistocene development in the North Sea area was the demise of the large Eridanos river system (Fig. 4). The Eridanos system existed in the Miocene, Pliocene and Early Pleistocene. Its drainage basin extended as far east as the modern Baltic Sea and Finland, into the headlands of the large Russian rivers Volga and Dnieper today. Increasingly severe glacial minima following the Mid-Pleistocene climatic transition, associated with progressively more extensive glaciations, brought about major changes in these upstream parts of the Eridanos tributary network. Erratic Scandinavian gravel first arrived late in the Early Pleistocene (Doppert et al. Reference Doppert, Ruegg, van Staalduinen, Zagwijn, Zandstra, Zagwijn and van Staalduinen1975; Bijlsma, Reference Bijlsma1981; Gibbard, Reference Gibbard1988), not long before most source areas were lost, strongly reducing northern fluvial sediment supply to the North Sea area.

From then on, northern Germany was occupied by ice-marginal river systems each time the Baltic Sea area was covered by ice, delivering smaller but still considerable amounts of sediment to the southern North Sea basin. During interglacials and glacials with relatively minor glaciation, however, the North Sea no longer received major fluxes of sediment from easterly sources. The reduction in sediment supply had a significant long-term impact on the central North Sea area. By c. 1 Ma, Eridanos sediment had filled sizable parts of the available accommodation space and successive highstand coastlines were located far seaward of today's Wadden Islands (Overeem et al., Reference Overeem, Weltje, Bishop-Kay and Kroonenberg2001). After 1 Ma, a growing sediment deficit moved the highstand coastline south and east, increasingly close to its present-day position. Zagwijn (Reference Zagwijn1974, Reference Zagwijn, Oele, Schüttenhelm and Wiggers1979) dubbed this highstand situation ‘Ur-Frisia’. It is synchronous to the ‘Costa del Cromer’ dubbed-situation (Roebroeks, Reference Roebroeks2005) of the earliest known human presence in the area.

In the south of the former Eridanos depocentre, the loss of northern and eastern sediment supply was compensated by enhanced sediment influx from the Rhine, which transported ever more and coarser sand and gravel liberated from central Europe during increasingly severe glaciations. The Rhine supplied enough material to balance subsidence and to create a delta plain in the western Netherlands depocentre during every interglacial of the last 1 Ma, not unlike what happened in the preceding 1 Ma. Meanwhile, the Rhine was relocating its centre of deposition from a western position in the present North Sea towards the northwest Netherlands. Halfway through the Middle Pleistocene, it had completely avulsed to the northern Netherlands (Busschers et al., Reference Busschers, van Balen, Cohen, Kasse, Weerts, Wallinga and Bunnik2008).

The loss of the Eridanos sediment source mattered for coastal configurations of the northern Netherlands region and adjacent areas, especially in the Cromerian Complex Stage (roughly 1 Ma to 0.5 Ma). These coastal configurations changed at the time of the oldest known interglacial coastal presence of Palaeolithic humans along the southern North Sea rim. Highstand coastlines were located farther north and west from the present-day coastline early in the Cromerian Complex than towards the end of it (Zagwijn, Reference Zagwijn1974). On the English side of the North Sea, where the oldest European Palaeolithic sites have been found (Parfitt et al., Reference Parfitt, Ashton, Lewis, Abel, Coope, Field, Gale, Hoare, Larkin, Lewis, Karloukovski, Maher, Peglar, Preece, Whittaker and Stringer2010), the reverse is true. Up to the Anglian glaciation, the coastal plain of East Anglia returned to more or less the same position during every interglacial cycle within the Cromerian Complex (Cohen et al., Reference Cohen, MacDonald, Joordens, Roebroeks and Gibbard2012).

Creation of the Dover Strait drainage outlet

High-resolution bathymetric data have spawned renewed interest in the genesis of shelf-valley systems in the English Channel and in the origin of the Dover Strait (e.g. Gupta et al., Reference Gupta, Collier, Palmer-Felgate and Potter2007; Gibbard, Reference Gibbard2007; Mellett et al., Reference Mellett, Hodgson, Plater, Mauz, Selby and Lang2013). Spillage of vast volumes of accumulated meltwater from proglacial lakes carved out the later sea strait and left the enigmatic scars still visible on the English Channel floor today (Belt, Reference Belt1874; Gibbard, Reference Gibbard1988). It induced severe proglacial erosion and meant that the Channel River (Fleuve Manche), the shelf region of the Western Approaches and the abyssal fans below it were fed more water and sediment than before (e.g. Toucanne et al., Reference Toucanne, Zaragosi, Bourillet, Gibbard, Eynaud, Giraudeau, Turon, Cremer, Cortijo, Martinez and Rossignol2009). Following the opening of the Strait of Dover, the area between southwest Britain and mainland Europe stopped delivering sediment to the North Sea depocentre, at least during lowstands. The present-day shallow-marine and coastal regimes in the Southern Bight, with cliffs, estuaries, ravinement surfaces and other features (see the section on features from temperate (interglacial) times above), owe their existence to the (pro)glacial erosion triggering the opening of the Dover Strait.

Although theories on the timing and pacing of the opening of the Strait still have to be substantiated by other than erosional geomorphological evidence, the hypothesis that this started in the Anglian and is related to massive spillage of proglacial water from the North Sea Basin towards the south (Gibbard, Reference Gibbard1988, Reference Gibbard and Preece1995) has far-reaching bearings on northwest Europe’s Middle and Late-Pleistocene archaeological record and on the history of man as inferred from it. These bearings are not found as much in the would-be catastrophic events, which are attributed a key role in the formation of the Strait of Dover in some versions of the hypothesis (e.g. Gupta et al., Reference Gupta, Collier, Palmer-Felgate and Potter2007), and neither are they found in the interpretation that it must all have happened during a specific single glaciation (e.g. Belt, Reference Belt1874), or must have happened as a stepwise process spread over more than one glaciation (Busschers et al., Reference Busschers, van Balen, Cohen, Kasse, Weerts, Wallinga and Bunnik2008; Hijma et al., Reference Hijma, Cohen, Roebroeks, Westerhoff and Busschers2012). Rather, they come from the simple concept (not hypothesis) that terrestrial upland in the Strait of Dover and Southern Bight disappeared in the Middle Pleistocene and was replaced by a new exit route for river waters and entrance route for marine waters into this region outside the North Sea Basin proper (i.e. an open Strait of Dover).

As it stands, it appears that the Dover Strait became the permanent fluvial exit route for the Thames much earlier in the Middle Pleistocene than for the Rhine, and that marine exchange between the English Channel and the North Sea was strong in the Eemian, and much smaller or absent in the preceding interglacials (Meijer & Preece, Reference Meijer and Preece1995; Hijma et al., Reference Hijma, Cohen, Roebroeks, Westerhoff and Busschers2012). As this appears to have happened ‘halfway’ through the period of Palaeolithic occupancy in the North Sea region, it not only affects distribution of coastal archaeology from during the younger half of the archaeological record, but also comparison of sites and distribution across the period. Understanding the palaeogeographical change is vital in separating human-evolutionary from landscape-related aspects in the routes of re-dispersal between successive temperate intervals and overall distribution of palaeo-humans (Hijma et al., Reference Hijma, Cohen, Roebroeks, Westerhoff and Busschers2012). Timing the palaeogeographical change is vital to understanding whether behavioural changes as inferred from archaeological records occurred independently from the large-scale landscape changes or not (e.g. Cohen et al., Reference Cohen, MacDonald, Joordens, Roebroeks and Gibbard2012). Importantly, further carving and deepening of the opened Dover Strait continued in the last glacial (Antoine et al., Reference Antoine, Catt, Lautridou and Sommé2003; Hijma et al., Reference Hijma, Cohen, Roebroeks, Westerhoff and Busschers2012; Mellett et al., Reference Mellett, Hodgson, Plater, Mauz, Selby and Lang2013; Rijsdijk et al., Reference Rijsdijk, Kroon, Meijer, Passchier, van Dijk, Bunnik and Janse2013), at the time of Neanderthal presence in the region (Hublin et al., Reference Hublin, Weston, Gunz, Richards, Roebroeks, Glimmerveen and Anthonis2009). From that time onwards there is a noticeable increase in aeolian deposition and loess-related archaeology from the grown, permanent Channel River (see the section on features from glacial times above).

Shifting interglacial coastlines

Coastal processes in younger glacial–interglacial cycles were strongly influenced by the footprint of glaciations of the North Sea basin itself, and by extra-basinal developments related to the opening of the Dover Strait and the shifting of Rhine depocentres after the loss of the Eridanos. First, glaciations accentuated the topography that would later be inundated by postglacial transgressive seas. Regional and local highs, for example, were future coastal headlands, and glacial basins transformed into embayments. On a larger scale, the scouring in the Strait of Dover area, and the subsequent establishment of river valleys extending into the English Channel, brought extra transgressive pathways and altered the tidal circulation and amplification patterns during highstands (Uehara et al., Reference Uehara, Scourse, Horsburgh, Lambeck and Purcell2006; Smith et al., Reference Smith, Harrison, Firth and Jordan2011). Whilst all river mouths and coasts were transgressed ‘from the north’ before these changes, southern river systems in youngest cycles were transgressed ‘from the south’, through the Strait of Dover. Along coastal re-dispersal routes, migration of groups of palaeohumans will have changed in response to these palaeogeographical changes (Cohen et al., Reference Cohen, MacDonald, Joordens, Roebroeks and Gibbard2012).

Accurate reconstruction of interglacial coastlines during transgression, highstand and sea-level fall is difficult. For rapid transgressions, typical of early deglaciation phases, coastline positions can be regarded as the intersection of reconstructed water-level and basin-floor topography. Complications related to river-mouth configuration and coastal sedimentation are then ignored. For highstands, the volume and distribution of sediment that is mobilised and transported towards the coastal zone (from onshore and offshore) and the duration of the highstand are major factors determining the coastal configuration. Great volumes of sediment have been transported toward coasts and into estuaries along partly unknown sediment-transport pathways generated by cross-shore (storm) wave fields and longshore and cross-shore tidal currents. Much of the sediment was derived from the seabed (i.e. inherited lowstand glacial, fluvioglacial and periglacial sediment; see the section on landforms and other morpho-sedimentary features above) and from eroding headlands, but additional material was provided from onshore sources by rivers.

In the tectonically subsiding parts of the North Sea area, ice-marginal headlands have played a prominent and recurrent role in controlling the position of successive highstand barrier systems. The promontory related to the overridden ice-marginal feature between Texel (in the northwest Netherlands) and the Dogger Bank was present in the Eemian as well as the Holocene. The ice-marginal structure forms the shallowest area of the North Sea between mainland Europe and Britain, and must have been a land bridge in latest Saalian (c. 130,000 years ago) and Lateglacial/earliest Holocene times (up to c. 9000 years ago), as rising sea level drowned the continent. During lowstands, it was the divide between ‘Rhine/Meuse’ and ‘Elbe/Weser’ drainage. The modern, slightly concave coastline of the western Netherlands is the result of progressive promontory erosion in the last interglacial and the Holocene, combined with complete infilling of embayments with peat and remobilised clastic sediment during the Eemian (marginal marine), Weichselian (falling-stage deltaic) and Holocene (marginal marine). Promontory erosion was interrupted during the last lowstand, but major remobilisation of sand by periglacial fluvial and polar-desert (aeolian) processes had its own indirect effect on Holocene barrier formation, explaining part of the differences between Eemian and Holocene coastal configurations. Clearly, inherited topography is in fact quite short-lived as the dominant control on transgressive coasts. Sediment supply and redistribution are the main controls during highstands and falling base level. In the basin, the control of sedimentary activity is helped by background tectonic subsidence, which makes promontories sink and stimulates new deposition. For coastal areas to the south of the North Sea depocentre (notably in southeast England and Flanders), topographic inheritance has been the main control during transgressions and highstands, and fluvial erosion the main control during lowstands. In this part of the study area, highstand coastal configurations show ever deeper estuaries and increased inland tidal reach. The positions of most valleys (estuaries when drowned), however, has remained unchanged from one interglacial to the next.