This history can encompass a distinct sea bed evolution, including migration of underwater bars. It is worth noting that as a consequence, local sediment transport rates depend on the shape of the sea bottom, which is the upper limit of the dynamic layer. In view of the above findings, one can imagine Buparlisib in vivo that relatively small sediment resources in the dynamic layer can ‘saturate’ the water flow with sand grains in a short time scale (a matter of minutes). It is doubtful, however, whether the small sediment resources in the dynamic layer can feed the water flow satisfactorily and maintain the sandy ‘saturation’ for a longer time, exceeding the wave period, i.e. at scales of minutes, hours and days. Further,
one may ask what influence local sand resources exert on coastal evolution along adjacent shore sections in the long term – over months and years. As already mentioned, the dynamic layer’s parameters are governed by the coupled impact of waves and currents, causing sediment motion in the coastal zone. In non-tidal seas, including the Baltic, the most spectacular geomorphologic effects are related to longshore sediment transport.
This is so intensive that, according to some researchers (see e.g. Pruszak 2003), it gives rise to the longshore movement of sand with a net rate of more than 100 000 m3 year−1. It is assumed in theoretical calculations selleck antibody that the amount of Org 27569 sediment set in motion depends only on hydrodynamic forcing and sea bed grain diameters. The analysis of Racinowski & Baraniecki (1990) shows, however, that computationally obtained longshore sediment transport rates reflect only longshore transport ability and should be interpreted as the ‘maximum mass or volume of sand that can be displaced along the shore in given coastal hydrodynamic conditions’. It has also been pointed out by Mielczarski (2006) that the longshore sediment transport rate, determined conventionally on the basis of the longshore component of wave energy, is actually the ‘transport ability of wave motion’, the real usefulness of which depends on the amount
of sandy sediments accumulated in the nearshore dynamic layer. The southern Baltic coast is dominated by beaches and dunes: consisting mostly of Holocene sands, they make up about 80% of the Polish shoreline. Locally, there is also peat and mud on the sandy shores, usually in the form of interbeddings under the beach or dune surface. Cliff shores, making up the remaining 20% of the Polish coast, are basically built of Pleistocene formations, mainly till and silt, but also sand, gravel and pebbles. Small amounts of Holocene sands can be found at the toes of the cliffs (see Figure 2). The Polish shore in the eastern part of the Gulf of Gdańsk, from the Polish–Russian border to the Vistula river mouth, is an example of a beach-dune coast. Here, stable accumulative shores, with wide beaches and high dunes, are predominant.