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The mechanism and timing of the re-entrance of the tidal system is discussed in Baeteman et al. In the seaward part, marine and coastal deposits from the Last Interglacial underlie the Holocene deposits, the fluvial portion being eroded during the middle and late Holocene Baeteman, In the western part of the study area, the Pleistocene deposits, consisting most probably of slope deposits, are very thin and Tertiary deposits Eocene, Kortrijk Formation, formely Ieper Clay, Jacobs and De Ceukelaire, are found in the shallow subsurface.
In general, periglacial aeolian coversands from the Late Pleistocene are absent in this area. This depression is interpreted as a former palaeovalley of an ancient IJzer river. Note that in the coastal plain, the present-day course of the river is located outside the palaeovalley. The small southeast-northwest running valleys in the South reach a depth of about -8 m. The palaeovalley has a very gentle slope with depths of m and m in the central and seaward part, respectively.
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The relief of the pre-Holocene surface contrasts greatly between the western and eastern part. The eastern part has a flat morphology, while the slope is rather steep in the west. A low and small devide in the northwest separates the palaeovalley from an elongated depression. From the data available, it is difficult to ascertain whether this depression also belongs to a valley of an ancient river system, but the presence of basal peat indicates that the depression was not formed by tidal scour processes during the Holocene flooding.
The devide developed into a headland, but as it was low, it was eventually also flooded and the entire area was transformed into a tidal basin. Following this, the isohypse map was geo-registered in a geographical information system GIS and the contour lines were digitized manually. Each polygon represents an elevation range e. A mean value was attributed to each polygon e. As a result the surface appears as a staircase. A TIN is an object used to represent a surface Ianko, Since representation of a surface can be done in different ways e.
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Delaunay triangulation , TIN also implies a specific storage structure of surface data. TIN divides a surface into a set of contiguous, non-overlapping triangles. A height value is recorded for each triangle node. Heights between nodes can be interpolated thus allowing for the definition of a continuous surface.
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TIN can accommodate irregularly distributed as well as selective data sets. With this method it is possible to represent a complex and irregular surface with a small data set, which is the case here. Note that the vertical exaggeration is at least 50 10 being generally the maximum admitted due to the weak elevation difference between the highest and lowest point weakness of gradient. Some artifacts result from the conversion into the TIN representation, such as the connection between the two depressions in the NW part.
The depressions are actually quite distinct, but the size of the most western polygon, the distance between the two depressions, and the difference in elevation are all too small to completely separate them.
So the algorithm behind the TIN links the two depressions and allocates the same value to the new unit. In the smoothed version Fig. Figure 9. Three dimentional elevation model of the pre-Holocene surface. A: TIN representation; B: smoothed representation. The present-day coastline is the seaward boundary of the model. The tidal flat as considered here, comprises subtidal shallow shoals, intertidal sandflats and mudflats, and supratidal salt marshes.
Only the major tidal channels are represented. This would require an even denser boring grid and, moreover, the pattern would still not be realistic. In the reconstruction of the earliest stages of coastal evolution, the course of the tidal channels is chosen arbitrarily because of the scarcity of sufficiently deep boreholes.
The reconstruction of the position of the coastal barriers in the present-day offshore area is impossible since they dissappeared as a result of erosion. Therefore, no attempt was made to show them on the maps for the early Holocene, which does not imply that they did not exist. For the younger time slices however, few data for the coastal barrier are available for the area around Nieuwpoort and the western part of the study area, Baeteman, ; Baeteman, a. However, the presence and position of the coastal barrier was also inferred from associated sedimentary environments, although the major part of the position is chosen arbitrarily.
The present-day shoreline is shown on the maps for reference. Therefore, short periods when tidal sedimentation prevailed, and which are recorded in the sedimentary sequence as an alternation of mud and peat, are not represented. Moreover, the presentation of the latter would require much more detailed maps. Where the density of data points is low, the reconstruction is more schematical. The borehole data and cross-sections which form the basis for the reconstructions, are not presented in this paper.
The significant ones can be consulted in the papers mentioned above. The reconstructions for the western part are redrawn from Baeteman a. The 14C dates are presented in Table 1 and the numbers in the text refer to the site numbers in the Table. Table 1. Radiocarbon ages and calibration dates from the western coastal plain. Baeteman, ; 2. Baeteman, ; 3. Baeteman and Van Strydonck, ; 4. Baeteman, ; 5. Baeteman et al. Baeteman, ; 7. Baeteman, a; 8. Denys, ; 9.
De Ceunynck, ; De Ceunynck et al. Denys and Baeteman, ; Figure Palaeogeographical maps of the IJzer palaeovalley from to cal BP. A headland came into being between the depressions. A tidal channel was installed while at the landward edge of the tidal flat, freshwater marshes with peat accumulation developed. The immediately overlying clastic sediments are fine-grained and indicative of low energy environments.
This illustrates the effect of the morphology of the flooded surface on the distribution of the sediments. The belt of freshwater marsh, shifting upland and inland, was still narrow because the relief prevented it from lateral expansion.
However, the headland in the NW was not yet flooded. Since no tidal flat can exist without a tidal channel, a channel has been drawn arbitrarily in the eastern extension of the tidal flat. The relatively flat relief of the Pleistocene surface resulted in a broader belt of freshwater marshes which also began to develop in two of the small rivers.
The tidal flats extended further inland and the freshwater marshes were pushed upstream due to the RSL rise. The small river valleys, in particular, were characterized by peat growth. The coastal peat bog which developed locally east of the tidal basin has been encroached by the tidal flat, as well as the headland in the NW.
As the map shows, a substantial expansion of the tidal basin towards the west happened together with the tidal channel. Numerous cores record the development of a mudflat on the basal peat at this elevation. The tidal flat now also invaded the small river valleys far south which resulted in poor freshwater drainage since most of the freshwater marshes changed into permanently flooded depressions with accumulation of gyttja.
In this period, the coastal barrier reached the position of the present-day coastline in the west. It is most likely that during this period the tidal scour processes began in that area. Sedimentary records in the area of Nieuwpoort cf.
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Baeteman, show that by this period, the coast had receded far inland. The eastern part of the study area was eventually flooded. This period was characterized by a decrease of the rate of RSL rise resulting in some significant changes. The landward shift of the tidal flat was much reduced, but the tidal channel now occupied the IJzer valley, even far south. This most probably resulted in an improvement of the drainage in view of the alternation of gyttja and peat in the valley fill. The channel also brought the tidal flat far south in the eastern small valley, while in the western ones, freshwater marshes developed over the tidal flat salt marsh.
Because of the reduced rate of RSL rise, peat growth at the outer edge of the tidal flat could last for a much longer time and developed over broader areas. Similar dates of basal peat are found at locations with elevation ranges between -6 and -4 m.