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1

Czwartorzęd Zatoki Pomorskiej i perspektywy surowcowe

Kramarska R., Jegliński W., Kaulbarsz D., Pączek U., Przezdziecki P., Bojakowska I., Koszka-Maroń D., Relisko-Rybak J., Uścinowicz Sz.

Przegląd Geologiczny

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2016

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Vol. 64, nr 8

552--563

EN

This paper summarizes four years of geological research in the Pomerania Bay and Oder Bank. As a result of the synthesis of new and archival data,we have compiled maps, cross-sections and models depicting the geological structure of the Quaternary and its basement, and the relief of structural surfaces. Two main seismostratigraphic sedimentary complexes are distinguished. The first corresponds to Pleistocene glacial and interstadial deposits. The second one is composed of Late Glacial and Holocene lacustrine-swamp and marine sediments. The outline of geochemical condition of the sea bottom is also presented. The content of the elements is always below the acceptable concentration and the origin of the elements is geogenic. Special attention has been given to mineral resources on the bottom surface and to documenting deposits of sand containing heavy minerals. The characterization of areas with sands suitable for beach nourishment and valorization of deposits and prospective areas have also been of great importance. The history of the development of the geological structure and palaeogeography of the area is the summary of the results.

2

Analiza deformacji powierzchniowych wzdłuż południowo-zachodnich wybrzeży Zatoki Gdańskiej z zastosowaniem satelitarnych danych interferometrycznych

Czarnogórska M., Graniczny M., Uścinowicz Sz., Nutricato R., Triggiani S., Nitti D. O., Bovenga F., Wąsowski J.

Przegląd Geologiczny

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2012

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Vol. 60, nr 4

206-211

EN

The paper presents results of SPINUA (Stable Point Interferometry over Unurbanised Areas) Persistent Scatterers Interferometry (PSI) processing chain to study Earth surface deformations along the SW coast of the Gulf of Gdańsk, along the SE part of the Baltic Sea. As the input for SPINUA techniques 40 descending ERS-1/2 SLC (Frame = 251, Track = 36) images from the period 1995-2001 has been used. The area of interest (AOI) includes few cities and several towns, villages and harbors. The low lying coastal areas of the SW part of the Gulf of Gdańsk are at risk of floods and marine erosion. The PSI results, however, did not reveal the presence of a regional scale, spatially consistent pattern of displacements. It is likely that any crustal deformations in the AOI simply do not exceed +2 mm/year, which is the velocity threshold we assumed to distinguish between moving and non-moving persistent scatterers (PS). Importantly, for the most part the urban areas of the main cities (Gdańsk, Gdynia and Sopot) results show ground stability. Nevertheless, significant downward movements up to several mm/year, are locally noticed in the Vistula river delta - alluvial plain system located in the coastal zone east of Gdańsk as well as in the inland area west of the Gdańsk city. Indeed, the highest subsidence rates (-12 mm/year) was observed in the Gdańsk petroleum refinery constructed on alluvial sediments. Thus the anthropogenic loading and consolidation of the recent deposits can locally be an important factor causing ground subsidence.

3

Review and reinterpretation of the pollen and diatom data from the deposits of the Southern Baltic lagoons

Miotk-Szpiganowicz G., Zachowicz J., Uścinowicz Sz.

Polish Geological Institute Special Papers

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2008

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Vol. 23

45-70

EN

According to their origin, geomorphology and hydrology, the fresh/brackish-water bays and coastal lakes of the Southern Baltic coast can be treated as lagoons. They developed at the time of and as a result of the Atlantic (Litorina) transgression of the Southern Baltica. There are many publications about the origin and evolution of the lagoons and lakes along the Polish coast of the Southern Baltic (e.g. Przybyłowska-Lange, 1973a, b, 1974, 1979, 1981; Zaborowska, 1977; Zachowicz, 1977, 1985; Wypych, 1980a, b; Zachowicz et al., 1982; Bogaczewicz-Adamczak, Miotk, 1985a, b; Dąbrowski et al., 1985; Zachowicz, Zaborowska, 1985; Borówka et al., 2001a, b, 2002). Nevertheless, the origin of the lagoons has not been fully explained. In the light of present-day information the results of earliest investigations often need to be reinterpreted. The aim of this work was the correlation of the published and unpublished pollen and diatom diagrams from Late Pleistocene and Holocene sediments of the Southern Baltic lagoons, and their relation with radiocarbon dating. The pollen and diatom diagrams from the area of north-east Germany and the Curonian Lagoon (Kabailiene., 1999; Jahns, 2000; Kaiser et al., 2000; Endtmann, 2002; Bitinas et al., 2002) have been used for comparison. For the palynological sites, the local pollen assemblage zones (L PAZ) have been identified according to Janczyk-Kopikowa (1987). Comparison of the biostratigraphical data allowed us to define the approach time of the formation of the lagoons in their present-day position on the coast as well as to determine the periods of an accelerated sea-level rise and increased frequency of storm surges (so-called marine transgression phases) when the investigated areas had been under the direct influence of the sea. Such influences are visible about 7000, 6000, 5000 and 4000 years BP. This period of marine influences, about 1000-year long, corresponds very well to the same period of climate oscillations mentioned by Stuiver and Braziunas (1993), Stuiver et al. (1995) and Chapman and Shackelton (2000). The influence of the sea in the Post-Litorina period was associated mainly with the inflow of sea water through more or less developed barriers, so they are not synchronous.

4

A critical review and reinterpretation of bio-, litho- and seismostratigraphic data of the Southern Baltic deposits

Zachowicz J., Miotk-Szpiganowicz G., Kramarska R., Uścinowicz Sz., Przedziecki P.

Polish Geological Institute Special Papers

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2008

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Vol. 23

117-138

EN

The aim of this study was the reinterpretation of the published and unpublished Late-Pleistocene and Holocene pollen and diatom diagrams of deposits from the sedimentary basins of the Southern Baltic Sea and the correlation of the distinguished biostratigraphic units with lithological parameters, seismostratigraphic units. Chronostratigraphic subdivision of the Late Pleistocene and Holocene was also made. To facilitate the correlation and reinterpretation of the results of biostratigraphic (palynological and diatom) analyses, new unified and simplified diagrams were drawn using the POLPAL software. Such diagrams were constructed for all the sites under comparison, even for those of no numerical data. In such cases, the published diagrams were scanned and their percentage values were the basis for new diagrams. A review and reinterpretation of biostratigraphic data show an almost complete lack of palynological documentation and diatom diagrams for the Late Pleistocene period and poor documentation for the Early Holocene. Middle and Late Holocene Baltic muds have the best biostratigraphic documentation and radiocarbon dating, which greatly facilitates their location on the geological time scale. Among the Southern Baltic postglacial sediments three lithostratigraphic units were identified. They differ in their lithological features reflecting the conditions prevalent in the sedimentary basin during deposition. It should be noted that these units meet no formal criteria for distinguishing lithostratigraphic units. Similarly, within the Late Pleistocene and Holocene sediments of Southern Baltic deep-water basins, three main seismostratigraphic complexes have been identified. The integrated analysis of seismoacoustic profiles, lithological profiles of cores and reinterpretated biostratigraphic data allow a correlation of the bio-, litho- and seismostratigraphic units with chronostratigraphic units and Baltic evolutionary phases.

5

Terrestrial deposits from the Słupsk bank as an evidence of the late glacial and early holocene Baltic sea level

Uścinowicz Sz., Zachowicz J.

Polish Geological Institute Special Papers

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2005

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Vol. 16

133--141

EN

The site of Late Glacial and Early Holocene peat and limnic sediments at eastern part of Słupsk Bank were investigated by seismoacoustic profiling, lithological, pollen and molluscs analyses, and 14C datings of 3 sediments cores. There is an evidence that from the last deglaciation to the beginning of the Littorina transgression c. 8000-7500 years BP, the Słupsk Bank was a land area, and the maximum water level of the Baltic Ice Lake and the Ancylus Lake was lower then 24-25 m below the present sea level.

PL

Badania sejsmoakustyczne oraz analizy osadów (litologiczne, palinologiczne, malakologiczne), a zwłaszcza datowania radiowęglowe torfów, pozwoliły na szczegółową charakterystykę stanowiska późnoglacjalnych i wczesnoholoceńskich torfów i osadów jeziornych we wschodniej części Ławicy Słupskiej. Wykazano, że od deglacjacji do początków transgresji litorynowej, około 8000-7500 lat BP, Ławica Słupska była lądem, a maksymalny poziom wód w zbiornikach bałtyckiego jeziora lodowego i jeziora ancylusowego nie był wyższy niż 24-25 m poniżej współczesnego poziomu morza.

6

The southern Baltic Sea : test field for international co-operation

Zachowicz J., Kramarska R., Uścinowicz Sz.

Przegląd Geologiczny

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2004

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Vol. 52, nr 8/2

738-743

EN

Selected results of the joint geological investigations of the Southern Baltic are presented, mainly related to geological cartography and environmental geology (e.g., sea bottom contamination). The results of international projects expand the knowledge of bathymetry, seabed sediments in the Polish Exlusive Economic Zone and other data obtained by the Marine Geology Branch of the Polish Geological Institute during its 35 year research activity on the Baltic Sea. The PGI participates in research co-operation with neighbouring Baltic countries (especially Germany, Lithuania, Russia, Sweden, and Finland), but also with geological surveys of Great Britain and the Netherlands conducting joint research in the Polish part of the Baltic Sea.

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Geoindykatory strefy brzegowej : rejestracja i analiza procesów i zjawisk

Graniczny M., Janicki T., Kowalski Z., Uścinowicz Sz., Zachowicz J.

Przegląd Geologiczny

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2004

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Vol. 52, nr 1

47-54

EN

The goal of the project was to evaluate methods for recording and analysing the geoindicators related to the coastal zone. Geoindicators, according to the definition elaborated by the IUGS, are measures (magnitudes, frequencies, rates and trends) of geological processes and phenomena occurring at or near the Earth’s surface and subject to changes over periods of 100 or less years. Shoreline changes are one of the most important geoindicators of processes on the coastal areas because of their importance to economy and nature conservation. Investigations were carried out on the southern and western coast of the Gulf of Gdańsk: in the Vistula river mouth, on cliffed coast south of Gdynia and at the tip of the Hel Peninsula. Shoreline changes in different time scales were identified by analyses of aerial photos, analyses of digital terrain models and GPS measurements.

8

Recent development of the Vistula River outlet

Graniczny M., Janicki T., Kowalski Z., Koszka-Maroń D., Jegliński W., Uścinowicz Sz., Zachowicz J.

Polish Geological Institute Special Papers

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2004

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Vol. 11

103--107

EN

The Vistula River mouth is an unique example of river’s outlet observed since the birth in 1895 to present day. There is a large documentation of morphological changes in the outlet area. In 1895, a 7 kilometres canal was dug into which the waters of the Vistula were let in. Since 1895, most of the water discharge and all sediment transport reach the Gulf through artificial channel c. 20 km east of Gdańsk. During the last 100 years, the shoreline has been shifted seaward c. 1.5 km on the eastern side, to c 2.5 km on the western side of the Vistula mouth. Isobath of 5 m moved seaward c. 3 km and isobaths of 10 and 15 m shifted 2.5 km. During the years 1895-1997, land area accreted to 3,019,000 m2. The volume of the river-outlet cone in the year 2000 was 133.39 mln m3 and the average rate of sediment growth over the 105 years was c. 1.27 mln m3 per year.

9

Rapid sea level changes in the Southern Baltic during late glacial and Early Holocene

Uścinowicz Sz.

Polish Geological Institute Special Papers

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2004

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Vol. 11

9-18

EN

In the area of the southern Baltic Sea, the largest and most violent changes in water level took place in Late Glacial and Early Holocene, during the period between 13.0-8.5 ka BP. These changes depended on the varied glacio-isostatic movements between the northern and southern parts of the Baltic Sea, the glacio-eustatic increase in the ocean level and the closing or opening of the connection between the Baltic Sea basin with the ocean. During the Late Glacial and Early Holocene, the sea level changed within an amplitude as wide as 25-27 m. In some extreme cases, the sea level could have fallen at a rate of about 100-300 mm/a, the sea level rise rate reaching up to about 40-45 mm/a. In Late Glacial and Early Holocene, there were three transgressions: during 12.0-11.2, 11.0-10.3 (the Baltic Ice Lake) and 10.2-9.2 ka BP (the Yoldia Sea and the Ancylus Lake). There were also three regressions, setting on 11.2, 10.3 and 9.2 ka BP. During regressions, depending on the real drainage rate and the local gradient of the bottom inclination, the land possibly grew at a rate of 0.3 to 4 km per year. During transgressions, rate of shoreline migration could reach in some cases up to 150-200 m per year. These processes took place on the surface of the sea bottom currently located at the depth of c. 55 to 25 m below sea level and from 30 to 60 km away from the present-day southern coast of the Baltic Sea. Rapid changes of shoreline position are recorded in progradational barrier structures and in the erosion surfaces of the glacial till and glacio-marine clays.

10

Geological structure of the southern Baltic coast and related hazards

Uścinowicz Sz., Zachowicz J., Graniczny M., Dobracki R.

Polish Geological Institute Special Papers

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2004

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Vol. 15

61-68

EN

Polish coast of the Baltic Sea has a total length of 498 km (without internal lagoons coasts). Quaternary deposits dominate coastal zone, similar to central and northern Poland. According to morphology and geological structure, three types of coast are distinguished: cliffs (c. 101 km), barriers (380 km) and coast similar to wetlands (salt marshes) (c. 17 km). Generally, three types of mass movements can be distinguished on cliff coast: eboulements (rock falls) dominated on the cliffs built mainly by tills, talus and landslip, dominated on sandy cliffs, and typical landslides occurred on cliff stretches with a complex structure where the main role play clay layers being initial slide layers for other deposits. Serious risks are related to erosion of low and narrow barriers, which could be easy broken during storm surges. Storm floods in case of barrier being broken threaten lowlands behind the barriers. Similar flood hazard exists also on lagoon coasts located behind large and relatively stable barriers. It is caused by barographic high water stands, which in extreme cases reach up to 2 m above the mean sea level, and water back flow into straits connecting lagoons with the sea.

PL

Długość polskiego wybrzeża morskiego wynosi 498 km (bez linii brzegowej Zalewów Wiślanego i Szczecińskiego). W budowie geologicznej strefy brzegowej, podobnie jak środkowej i północnej Polski, dominują osady czwartorzędowe. Biorąc pod uwagę geomorfologię i budowę geologiczną wyróżniono trzy zasadnicze typy wybrzeży: klify o łącznej długości ok. 101 km, wybrzeża wydmowe (mierzeje) o łącznej długości ok. 380 km oraz wybrzeża nizinne typu Wetland o długości ok. 17 km. Na wybrzeżach klifowych wyróżniono trzy typy ruchów masowych: obrywy dominujące na klifach, w których występuje glina zwałowa, zsuwy i osypiska dominujące na klifach zbudowanych głównie z osadów piaszczystych oraz typowe osuwiska występujące na klifach o złożonej strukturze geologicznej, gdzie główną rolę odgrywają warstwy ilaste będące powierzchnią poślizgu dla warstw wyżej ległych. Poważne zagrożenia związane są też z erozją niskich i wąskich mierzei, które łatwo mogą być przerwane w czasie sztormów. Nisko położone obszary zaplecza mierzei w takim wypadku zagrożone są powodziami sztormowymi. Podobne zagrożenia powodziowe istnieją też na zapleczu mierzei relatywnie stabilnych - szerokich z wysokimi wałami wydmowymi. Powodzie mogą wystąpić w przypadku wysokich stanów wody spowodowanych spiętrzeniami sztormowymi i barycznymi, dochodzącymi maksymalnie do 2 m ponad średni poziom morza, kiedy dochodzi do wlewów wód morskich do Zalewów i jezior przybrzeżnych.

11

Relative sea level changes, glacio-isostatic rebound and shoreline displacement in the Southern Baltic

Uścinowicz Sz.

Polish Geological Institute Special Papers

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2003

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Vol. 10

5-79

EN

The relative sea level curve was developed for the southern Baltic area, based on a set of 314 radiocarbon datings of different terrestrial and marine sediments, collected at 163 sites located in the Polish part of the Southern Baltic and in the adjacent coastal land area. When developing the curve, relicts of various formations related to the shoreline evolution as well as extents of erosional surfaces, determined from seismoacoustic profiles, were taken into account. During Late Pleistocene and Early Holocene, i.e. between 13.0 and 8.5 ka BP, the southern Baltic sea level rose and fell three times, the amplitude of changes extending over 25-27 m. In some extreme cases, the sea level was falling at a rate of up to about 100-300 mm/a, the rate of rise accelerating to about 35-45 mm/a. In the Late Boreal, c. 8.5 ka BP, the Baltic - its water level by about 28 m lower than the present one - became permanently connected with the ocean. Until the onset of the Atlantic, the sea level had risen to about 21 m below the present sea level (b.s.l.). During 8.0-7.0 ka BP, the sea level was rising, at a rate of about 11 mm/a, to reach 10 m b.s.l. Subsequently during the Atlantic, until its end, the sea level rose to 2.5 m b.s.l., the rate of rise slowing down to about 2.5 mm/a. During the first millenium of the Subboreal, the sea level rose to about 1.3-1.1 m b.s.l., to become - on termination of the Subboreal - about 0.6-0.7 m lower than present. During the Subatlantic, the sea level changes were slight only. The glacio-isostatic rebound began c. 17.5 ka BP, to terminate c. 9.2-9.0 ka BP. The total uplift during that time amounted to about 120 m. The maximum uplift rate of about 45 mm/a occurred c. 12.4-12.2 ka BP. Within the period of c. 9.0 to c. 7.0 ka BP, the southern Baltic experienced forebulge migration, a subsequent subsidence ensuing from c. 7.0 to c. 4.0 ka BP. As from c. 4.0 ka BP, the Earth crust in the area regained its equilibrium. In Late Pleistocene and Early Holocene, the southern Baltic shoreline displaced rapidly and substantially several times, the displacement rate ranging from several tens of metres to a few kilometres per year. The displacement processes involved the seafloor surfaces located at present at 25 to 55 m b.s.l., the shoreline migrating over distances of 30-60 km away from the present coastline. In Middle Holocene, the shoreline moved southwards over a distance ranging from about 60 km in the Pomeranian Bay to about 5 km in the Gulf of Gdańsk. The shoreline location approached the present one at the final phase of the Atlantic. Late Holocene was the period when coast levelling processes were prevailing, the shoreline becoming gradually closer and closer to its present setting.

PL

Krzywą względnych zmian poziomu morza skonstruowano na podstawie 314 dat radiowęglowych osadów pochodzących z różnych środowisk lądowych i morskich. Próbki do datowań pobrano z 163 stanowisk zlokalizowanych na obszarze polskiej części południowego Bałtyku i przyległej strefy brzegowej. Przy konstruowaniu krzywej wykorzystano również relikty różnych form związanych z rozwojem strefy brzegowej oraz zasięgi powierzchni erozyjnych, zlokalizowane na profilach sejsmoakustycznych. W późnym plejstocenie i wczesnym holocenie, między 13,0 i 8,5 tys. lat BP, poziom wody trzykrotnie wzrastał i opadał, a zakres wahań dochodził do 25-27 m. Poziom wody obniżał się w skrajnych przypadkach w tempie do ok. 100-300 mm/rok, a tempo wzrostu dochodziło do ok. 35-45 mm/rok. W późnym boreale, ok. 8,5 tys. lat BP, Bałtyk uzyskał stałe połączenie z oceanem na poziomie niższym od obecnego o ok. 28 m. Do początku okresu atlantyckiego poziom morza wzrósł do ok. 21 m poniżej współczesnego poziomu morza (p.p.m.). W okresie 8,0-7,0 tys. lat BP poziom morza wzrósł do 10 m p.p.m., w średnim tempie ok. 10 mm/rok. Do końca okresu atlantyckiego poziom morza wzrósł do 2,5 m p.p.m., a tempo wzrostu zmalało do ok. 2,5 mm/rok. W pierwszym tysiącleciu okresu subborealnego poziom wody wzrósł do ok. 1,1-1,3 m, a do końca tego okresu do ok. 0,6-0,7 m niższego niż współczesny. W okresie subatlantyckim średni poziom morza zmienił się już nieznacznie. Przebudowa glaciizostatyczna rozpoczęła się ok. 17,5 tys. lat BP i zakończyła ok. 9,2-9,0 tys. lat BP. Całkowity zakres podniesienia (total uplift) w tym okresie wyniósł ok. 120 m. Maksimum prędkości ruchów wznoszących, dochodzące od ok. 45 mm/rok, wystąpiło w okresie ok. 12,4-12,2 tys. lat BP. W okresie od ok. 9,0 do ok. 7,0 tys. lat BP przez obszar południowego Bałtyku migrowało nabrzmienie brzeżne, a w okresie od ok. 7,0 do ok. 4,0 tys. lat BP wystąpiły ruchy obniżajace. Od ok. 4,0 tys. lat BP położenie skorupy ziemskiej wróciło do stanu równowagi. Linia brzegowa południowego Bałtyku w późnym plejstocenie i wczesnym holocenie kilkukrotnie uległa szybkim i znacznym przemieszczeniom. Zmieniła położenie w tempie od kilkudziesięciu metrów do kilku kilometrów rocznie. Procesy te rozgrywały się na powierzchni dna morskiego położonej obecnie na głębokości od ok. 55 do 25 m p.p.m. i w odległości 30-60 km od dzisiejszego wybrzeża. W środkowym holocenie linia brzegowa przemieściła się ku południowi od ok. 60 km w Zatoce Pomorskiej do ok. 5 km w Zatoce Gdańskiej. Położenie linii brzegowej zbliżyło się do współczesnego w końcu okresu atlantyckiego. W późnym holocenie dominowały procesy wyrównywania wybrzeży, a linia brzegowa stopniowo zbliżała się do obecnego położenia.

12

Kenozoik południowego Bałtyku - wybrane zagadnienia

Kramarska R., Uścinowicz Sz., Zachowicz J.

Przegląd Geologiczny

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2002

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Vol. 50, nr 8

709-716

PL

Utwory trzeciorzędowe w obszarze południowego Bałtyku obejmują wycinkowe fragmenty profilu stratygraficznego reprezentowane przez paleocen dolny, eocen górny, oligocen dolny oraz miocen dolny i środkowy. Młodsze ogniwa trzeciorzędu – oligocen dolny oraz miocen dolny i środkowy rozpoznane są dotychczas tylko w bliższym sąsiedztwie brzegu oraz w klifach. Plejstocen jest reprezentowany głównie przez osady zlodowacenia warty i wisły. Pełny profil holocenu występuje jedynie w głębokowodnych basenach sedymentacyjnych. W obszarze płytkowodnym osady młodszego holocenu występują tylko lokalnie. Osady środkowego i późnego holocenu, reprezentowane przez piaski i żwiry morskie, na dużych obszarach leżą bezpośrednio na glinach zwałowych. Długotrwałe okresy denudacji przypadające na koniec trzeciorzędu i początek czwartorzędu, na które nałożyły się procesy plejstoceńskiej egzaracji glacjalnej i erozji subglacjalnej są głównymi czynnikami odpowiedzialnymi za styl budowy geologicznej obszaru i rozwoju rzeźby. Główne elementy współczesnej rzeźby są wynikiem procesów erozyjnych zachodzących podczas holoceńskich transgresji południowego Bałtyku.

EN

Tertiary deposits in the area of the Southern Baltic represent only some parts of the stratigraphic column: Lower Palaeocene, Upper Eocene, Lower Oligocene, and Lower and Middle Miocene. Younger members of the Tertiary are known only from coastal zone area. Pleistocene is represented mainly by deposits of Wartanian and Vistulian glaciations. Full sequence of the Holocene occurs only in deep water basins. In the shallow water area the Early Holocene deposits occur only locally. On large areas Middle and Late Holocene marine deposits are laying directly on top of till. Long-lasting denudation processes at the end of Tertiary and beginning of Pleistocene as well as glacial erosion during the Pleistocene are responsible for the origin of Baltic depression. The main features of present day morphology of the sea floor is a result of marine erosion during the Holocene transgressions.