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Modelling Western North Sea Palaeogeographies and Tidal Changes During the Flolocene

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Modelling Western North Sea Palaeogeographies and Tidal Changes During the Flolocene Modelling westernNorth Sea palaeogeographiesand tidal changes during the flolocene I. SHENNAN,T K. LAMBECT<,2 R. FLATHER;I B. HORTON,T J. McARTHUR,T J. INNES,T J:.LLo].D;l l,t. RI¡THERFoRDI & R. WINGFIELD4t 1 Environmental Research centre, Department of Geography, (Iniversity oJ'Durham, Durham DHI 3LE, UK (e-mail: [email protected]) 2 Research School of Earth Sciences, The Austrølian National (Jniversity, Canberra ACT 0200, Australia 3' Institute of Oceanographic Sciences, Birkenhead, UK Centre for Coastal and Mqrine Sciences, Proudman Oceanographic Laboratory, Birkenhead L43 7RA, UK a Coastøl and Engineering Geology Group, Brirish Geological Survey, Kingsley Dunhøm Cente, Keyworth,.Nottingham NG12 5GG, UK Abstract: Analysis of cores collected from Late Devensian (Weichselian) and Holocene sediments on the floor of the North Sea provides evidence of the transgression of freshwater environments during relative sea-level rise. Although many cores show truncated sequences, examples from the Dogger Bank, Well Bank and 5 km offshore of north Norfolk reveal transitional sequences and reliable indicato¡s of past shoreline positions. Together with radiocarbon-dated sealevel index points collected from the Holocene sediments of the estuaries and coastal lowlands of easte¡n England these data enable the development and testing of models of the palaeogeographies of coastlines in the western Norti Sea and models of tidal range changes through the Holocene epoch. Geophysical models that incorporate ice-sheet reconstructions, earth rheology, glacio- ' eustasy, and and hydro- isostasy provide predictions ofseaJevel relative to the present for the last lQka at l-ka intervals. These predictions, added to a model of present-day bathymetry, produce palaeogeographic reconstructions fgr e-achtime period. The palaeogeographic maps reveal the transgression of the N¡rrth Sea continental shelf. Key stages include a western embayment off northeast England as early as l0karn; the evolution of a large tidal embayment between eastern England and the Dogger Bank befo¡e 9 ka Bp with connection to the English Channel prior to Skaar; and Dogger Bank as an island at high tide by 7.5kasp and totally submerged by 6karr. Analysis of co¡e data shows that coastal and saltmarsh environments could adapt to rapid rates of sea-level rise and coastline ¡etreat. After 6 ka sp the major changes in palaeogeography occurred inland of the present coast of eastern England. The palaeogeographic models provide the coastline positions and bathymetries for modelling tidal ranges at each l-ka interval. A nested hierarchy of models, from the scale ofthe northeast Atlantic to the east coast ofEngland, uses 26 tidal harmonics to reconstruct tidal regimes. Predictions consistently show tidal ranges smaller than present in the early Holocene, with only minor changes since 6 ka ¡p. Recalibration of previously available sealevel index points using the model results rather than present tidal- range parameters increases the difference between obse¡vations and predictions of relative sea-levelsf¡om the glacio-hydro-isostatic models and reinforces the need to search for better ice-sheetreconstructions. The majority of the continental shelf of the North ing this transgressionthere was the potential for Seawas subaerial at the opening of the Holocene significant erosion, transport and deposition of epoch. Relative seaJevel changes, the combined sediment both on the continental shelf and into result of eustatic sea-level change and glacio- the coastal zone and estuaries. Many sediment and hydro-isostatic landlevel change, caused cores from the offshore have a major hiatus with the transgressionof the former land areas.Ður- much of the Holocene record missing, presum- ably the result of marine erosion during the t Deceased. transgression(Jelgersma 1961). In contrast to the F¡onz:SHENNaN, I. & ANDREwS,J. (eds) HoloceneLand-Ocean Interaction and EnvironmentalChange u-ould theNorth Sea.Geological Society, London, SpecialPublications, 166, 299-319. l-86239-054-1100/$15.00 @ The GeologicalSociety of London 2000. ; 300 I. SHENNAN ET AL. Þ t present land areas,little is known in detail about dependent, such as sand transport paths, seaso- the relative sealevel history of the North Sea and nal stratiflcation, and therefore primary produc- the configuration of the coastline at any one tivity (Austin l99l). time. In 1994, at the start of the Land-Ocean Previous studies of reconstructing both the Interaction Study (LOIS), there were very few palaeocoastlinesof the North Sea and the tides radiocarbon-dated samples of Holocene age were limited by fundamental assumptions about from the UK sector of the North Sea. Only one the input parameters. Bathymetric maps show a or two could be used to fix a past sea level, the low-gradient topography for much of the floor rest were simply limiting values, either indicating of the southern North Sea over which a relatively fully terrestrial or fully marine conditions, with small change in relative sea-level would have no precise relationship to sealevel or the posi- caused a large horizontal shift in the coastline. tion of the coastline at the time of deposition. Prior to geophysical models incorporating ice- Although moredataareavailable from the rest of sheet reconstructions, earth rheology, eustasy, the North Sea (e.g. Behre e, al. 1979; Jelgersma and glacio- and hydro-isostasy (e.g. Lambeck 1979; Lttdwig et al. 1981) the total number of 1991,1993a,b, 1995;Peltier 1996, 1998)the spa- validated index points is over two orders-of- tial and temporal variations of relative sea-level magnitude less than those available from the across the North Sea were very poorly con- surrounding land areas. By integrating data from strained (e.g.Behre et aL.1979;Jansen et al.1979; a range of recent research areas we can start to Jelgersma 1979). This is a severelimitation on the address aspects of understanding long-term envi- palaeogeographic reconstructions of Jelgersma ronmental change that require knowledge of the (1979) and the tidal models of Austin (1991) and Holocene evolution of the North Sea. As long- Hinton (1992, 1995, 1996). Most of the tidal term objectives we need to understand how the models simply used sea-levellowered as a plane changing water depths and coastline positions surface by values indicated by a eustatic curve, limit our knowledge of environmental processes although Hinton (1992, 1995) included a spa- and change. We also need to explain in quan- tially variable isostaticcomponent of up to2m in titative terms the fluxes of sediments into the modelling the southwest North Sea and the estuaries and coastal lowlands from the North Wash (Fig. 1). Sea (e.g. Rees ¿/ al. this volume calculate that The LOIS project enabled different advances to c.75o/oof the l0kmj of Holocene sedimentin the come together and re-address these issues; Shen- Humber Estuary and lowlands had a coastal or nan & Andrews (this volume) describeindividual marine source), the relationships between sea- contributions from the Land-Ocean Evolution level change and coastline advance or retreat, and Perspective Study (LOEPS) component. In order the geographical variations in sea-levelchange. to provide a viable database, the LOEPS core While the majority of samplesused to reconstruct programme undertook sampling both onshore Holocene sea-level change formed close to the and offshore, thus providing new data for the contemporary level of mean high water of spring early Holocene from many coastal locations. tides (MHWST) rather than mean sea-level These new samples also allowed significant (MSL), few studies of Holocene relative sea- improvement of the chronostratigraphy of the level changes include numerical reconstructions western part of the North Sea.Onshore sampling of tidal-range changesthrough time (e.g. Gehrels concentrated on the east coast of England et al. 1995). Most studies standardize the data between Northumberland and north Norfolk using the present tide levels,with some incorpor- (Fig. l). The spatially variable component of ating a tidal element within the error term of the relative sea-levelrise shows an increasing effect reconstructed sea-level(e-g. Shennan 1989;Lam- back through time, reaching c.30m around beck 1993å).As the configuration ofthe coastline l0l4Ckanp for the east coast of England and offshore bathymetry changed, not least with (Fig. l) and much greater in the areas of the connection of the North Sea to the English Scotland, where Late Devensian ice was thicker. Channel, the possibility of significant changesin This component must be included in reconstruc- the tidal prism arises. Initial modelling studies tions of both palaeocoastlines and tìdes. The with both lower and higher sea-levelspredict enlarged database of sealevel index points and changes in the tidal prism (e.g. Belderson ¿¡ ¿i. the possibility of identifying different tide levels 1986; Austin, 1991; Hinton 1992, 1995, 1996; from the stratigraphy (e.g. Horton et al. this Gehrels et al.1995; Scourse& Austin 1995).Tem- volume; Shennan et al. this volume) offers the poral changes in tidal amplitudes are not only potential for testing the output from tidal important for calibrating sea-levelindex points: models. Previous models of Holocene tides in for such changes have profound influences on the North Sea (e.g. Austin 1991; Hinton 1992, sheif-sea processes,which themselves are tide- 1995) predict reduced tide levels compared with PALAEOGEOGRAPHIESAND TIDAL CHANGES 301 Fig. l. Location map of
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