{"refrec":{"BRefID":9298,"RR":"<b>Depuydt, F.</b> (1972). De Belgische strand- en duinformaties in het kader van de geomorfologie der zuidoostelijke Noordzeekust. <i>Verhandelingen van de Koninklijke Vlaamse Academie voor Wetenschappen, Letteren en Schone Kunsten van Belgie, Klasse der Wetenschappen</i>, 34(122). Koninklijke Academie voor Wetenschappen, Letteren en Schone Kunsten van België: Brussel. 228, 7 maps pp.","BEntID":9298,"PublicFlag":1,"CheckedFlag":0,"wosflag":0,"vabbflag":0,"RefStringPartII":". <i>Verhandelingen van de Koninklijke Vlaamse Academie voor Wetenschappen, Letteren en Schone Kunsten van Belgie, Klasse der Wetenschappen</i>, 34(122). Koninklijke Academie voor Wetenschappen, Letteren en Schone Kunsten van België: Brussel.  228, 7 maps pp.","DocTypID":5,"DocType":"Book/Monograph","MarineFlag":1,"FreshFlag":0,"BrackishFlag":1,"TerrestrialFlag":0,"Authorstring":"Depuydt, F.","OrigTitleTranslFlag":1,"Authorstringtrunc":"Depuydt, F.","Englishabstract":"The study of \"<i>Belgian beach- and dune-formation in the framework of the geomorphology on the south-eastern North Sea coast</i>\", tries to find an explanation for the micro- and macro-morphology of the sandcoast in general, and to give an insight in the genesis of the Belgian coast-dunes in particular . The problems (both static and dynamic coastmorphology) are studied with the help of terrain-observations, amplified with map-analysis and the study of historical documents, as well as with the help of sedimentological analyses. Chapter one of the <i>\"Morphological analysis of beach and dune\"</i> (part I) deals with the micro-forms of the Belgian and northern French coast (north-east of Sangatte -cf. map 1 and 4 in annex) which were then compared with those of the remaining northern coasts up to Skagen (northern-most point of Jutland in Denmark). The startingpoint for this analysis is the beach- and dune-strip of the Westhoek (between De Panne and the French-Belgian border -cf. map 2), which is the most developed dune-strip of the analyzed French-Belgian coast and which was already dealt with in a previous study (F. Depuydt, 1967). Concerning the <i>beach</i>, the ultimate small and large values of its slope and its width are to be found along the Belgian and northern French coast, where the differences in tide are also largest (more than 4 rn). The width of the beach (between low-tide and high-tide) varies from about 200 m to 1500 m and this under a global angle of inclination of 2 % to 0,32 % with an average value that is less than 1 % for northern France. Locally the greatest part of the side-face of the beach has a beach-angle which doesn't even reach 0,15 % (mostly westward of Dunkirk). Due to this fact, extensive beach-pools are preserved (photographs 3, 4 and 5), strangely enough the silt-sediment is very small here ( &lt; 0,3 %). Transport of sand and formation of embryonal dunes are almost absent on these naturally wide beaches, of which the angle of inclination is less than 0,60 %. In Holland, Germany and Denmark, the wide and shelving sandbeaches are rarer, especially on the mainland. The angle of inclination varies between 1 % and 2% (cf. map 4A, 5A and 6A). As the difference in tide decreases in a northerly direction, there is also a decrease in frequency of subsequent active beachwalls; which on the other hand could be noticed along the French-Belgian coast. Typical for Denmark are the stone-beaches, in the vicinity of the moraine-cliffs, and the fossil sea-terraces, which can clearly be distinguished in the present beachcliffs. Going from the south (France) towards the north (Denmark), the quantity of shells and shell-waste gradually diminishes. North of Bergen (northern Holland), the shell-waste even becomes rare. The morphology of the <i>dunes</i> differs quite strongly from one beach-zone to the other. Southwest of Dunkirk, the dunevolume is very small. Only low duneridges follow in succession. In between, there are rather extensive, moist and thickly overgrown dunedepressions. Between Nieuwpoort and the Scheldt-estuary the actual dunelandscape is limited to a narrow, high duneridge. The dunezone between Dunkirk (Aa-estuary) and Nieuwpoort (mouth of the Yzer) reaches the width of 2200 m, and is the only zone of the northern French, Belgian and Dutch coast to have these systematical, wide parabolic dunes (cf. map 2A and 4A). Behind a carved foredune, which reaches the height of 12 m above floodmark, there are even two rings of parabolic dunes in succession and stretching parallel with the coastline between Bray-Dunes and Koksijde. The most southern paraboles (twelve or so) are 500 to 1300 m wide, and their axes indicate the same direction as the resulting wind-vector (N 75°). The southern arms of these parabolic dunes are in a direct line with each other, but the northern arms are mainly covered with a fresh rambling dune. This wandering dune is nothing but the southern arms of the smaller northern paraboli","AbstractOtherLang":"Each of the outward physical factors of influence puts a typical stamp upon the grain-size distribution: -In comparison with the erosion sand, the sedimentary sand approximates more perfectly a normal Gauss-distribution, it has a finer mean grain-size and moreover, it is better sorted. -Considered as a whole, the topography it inversely proportioned to the mean grain-size and sorting degree; but it is directly proportioned to the degree of skewness -The slopes against the wind have coarser grains than those below the wind. -The vegetation, which improves the positive sandbalance, has the effect of decreasing the average grain-size. As a conclusion to part two, the characteristics of the sediments of <i>beach</i> and <i>dune</i> are contrasted to each other, and as a result of this, their morpho-dynamic differences are indicated. Map 7 shows very clearly the importance of the grain-size distribution of the source sediment for the configuration of the grains which were transported or selected from this sediment. As was clearly shown for the Belgian and for the Dutch beach areas, the sand is really a selection of sand-grains from well-defined classes of the source-material which are to be found deeper in the sea. In that way the parameters truely indicate well-defined characteristics of the mechanism of transport on the beach, as we tried to illustrate above. As the granulometrical parameters of the dunesand come close to those of the beachsand and, as it is difficult to believe (see further on) that the transport competence of the wind locally shows the same characteristics as that of the seawaves along the same beach, it becomes obvious that the granulometry of the dunesand is completely dominated by its source sediment: the beachsand. Nevertheless, it has been possible to indicate some typical characteristics of the eolian transport mechanism, beginning with sediments which had been subjected to eolian activity for a rather long time, because the sand was found a further distance from the sea or in fossile sedimentary deposits. In this way it is not astonishing that the correlation diagrams of the figures 21, 22, 25 and 28 show absolutely no significant distinction between beach- and dunesand; a fact that has been mentioned to the contrary by other authors (E. Von Engelhardt, 1940; C. Mason and R. L. Folk, 1958; G. Friedman, 1961 and B. K. Sahu,1964) and sometimes it has wrongly been quoted as an exclusive and unmistakable characteristic of beach- and dunesand respectively. The stretching transition of the generalized cumulative beachsand-curve to the generalized dunesand-curve is mainly shown in the swelling out of the coarser grain-size classes to \"normal\" classes, which were only an admixture fraction in the beachsand. Next to the typical coarse tail the fine sandtruncation also disappears in the eolian material, which implies that the kurtosis value decreases and that the skewness becomes less negative. The amount of stretching of the curve remains rather constant for a given beachzone; this also implies that in this particular beach-zone the quotient <i>mean X<sub>sigma</sub> /phi<sub>sigma</sub></i> fluctuates around a constant value, that varies however from coast to coast. The eolian transport energy does not run parallel with the marine one along the whole of the beach studied, as is shown in figure 28: on one hand the mean wave energy (somewhat greater than the mean wind velocity) varies more from coast to coast (cf. X<sub>phi</sub>-histogram), but locally on the other hand it has somewhat smaller fluctuations around its mean value (cf.<i> sigma<sub>phi</sub></i>-diagram of figure 28 and the <i>sigma<sub>phi</sub></i> values of figure 22). The reasons for this are: -for the sea: on one hand the local differences in fetch, tide-activity, coast-currents, coastline-tracé and-morphology, and coast-evolution; on the other hand the relatively small influence of big gusts of wind on the wave intensity. -f","BibLvlCode":"MS","StandardTitle":"De Belgische strand- en duinformaties in het kader van de geomorfologie der zuidoostelijke Noordzeekust","OrigTitleLangCode":"nl","OrigTitleLangCodeExtended":"dut","OrigTitleLangID":41,"DateLastModified":{"date":"2025-12-25 01:30:18.003955","timezone_type":1,"timezone":"+01:00"},"UserAccessRight":null,"UserAccID":null,"AuthorKeywords":null,"OtherDescriptors":null,"Notes":null,"AnaPub":null,"MonPub":1972,"DateUpdate":"2025-12-17","DateCreate":"2001-05-17","SecASFANote":null,"ConfID":null,"PeerRev":0,"VlizCoreFlag":1,"WoScode":null,"VABBcode":null,"OpenAcc":0},"refs":null,"anarec":null,"monrec":{"MonID":9298,"ISBN":null,"PubliDate":1972,"IssueDate":null,"Volume":"34","Issue":"122","Pagination":"228, 7 maps","Place":"Brussel","Edition":null,"BRefXtra":null,"BRefXtraRR":null,"SerID":248745,"SerRR":"Verhandelingen van de Koninklijke Vlaamse Academie voor Wetenschappen, Letteren en Schone Kunsten van Belgie, Klasse der Wetenschappen. 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