Krzysztof Petelski

Annales Societatis Geologorum Poloniae (2011), vol. 81:105–114.

THE IN FLU ENCE OF SUB-QUA TER NARY BASE MENT

ON THE RE LIEF IN THE EAST ERN PART

OF THE POM ER A NIAN LAKELAND, POLAND

In sti tute of Ge og ra phy, Pom er a nian Acad emy in S³upsk, Partyzantów 27, 76–200 S³upsk, Po land, e-mail: kpetelski@box43.pl

Petelski, K., 2011. The in flu ence of sub-Qua ter nary base ment on the re lief in the east ern part of the Pom er a nian Lakeland, Po land. Annales Societatis Geologorum Poloniae, 81: 105–114.

Ab stract: Geo log i cal map ping works, con ducted on 1:50,000 litho-petrographic map sheets of the South Bal tic coast and the east ern part of the Pomerania Lakeland, show a clear re la tion ship be tween large land forms of this area, like: subglacial chan nels, Wie¿yca Hill, the ice lobe that ac cu mu lated Gardno mo raine de pos its, and sub-Qua ter nary re lief. These land forms came into ex is tence as a re sult of re ac ti va tion of pre-ex ist ing fault zones in the sub-Caino zo ic base ment, due to the ice mass load ing dur ing suc ces sive Pleis to cene ice-sheet ad vances. Subglacial chan nels de vel oped and thick tills and ice-dammed lake de pos its were ac cu mu lated in the re gion. The subglacial chan nels and morainic belts are now dom i nat ing land forms in the Pom er a nian Lakeland.

Key words: re lief of the top of sub-Qua ter nary de pos its, subglacial chan nels, Kaszuby Lakeland, Bytów Lake-land, Gardno Low Lake-land, Po land.

Manu script re ceived 15 February 2010, ac cepted 28 April, 2011

IN TRO DUC TION

Geo log i cal map ping works, con ducted by the au thor for over thirty years in the South Bal tic coast and the east ern part of the Pom er a nian Lakeland, from the ¯u³awy Wiœlane bor der to Bytów, S³upia River val ley, S³upsk and Lake Gardno (Fig. 1), made it pos si ble to draw some con clu sions about the li thol ogy of Qua ter nary sed i ments. They show a clear re la tion ship be tween the pres ent-day to pog ra phy and sub-Qua ter nary re lief of this area. My hy poth e sis is that the sub-Qua ter nary re lief is not the one in her ited from Neo gene and preglacial times, but it formed dur ing the suc ces sive Pleis to cene ice-sheet ad vances.

RE SEARCH METH ODS

I con ducted geo log i cal map ping works on 12 sheets of the 1:50,000 De tailed Geo log i cal Map of Po land (DGMP) to ex am ine the geo log i cal ar chi tec ture of Qua ter nary sed i -ments (Petelski, 1998, 1999, 2000a, b, 2001, 2002, 2003a,b, 2005, 2006, 2008, 2009). Geo log i cal struc ture of Qua ter -nary de pos its was stud ied by spe cial re search bore holes. The or i gin of gla cial de pos its and stra tig ra phy of tills was in ter preted based on lithological and petrographic in ves ti -ga tions (Lisicki, 2003). Anal y sis of the bore holes drilled for the DGMP and all ar chi val bore holes ever drilled in this area en abled for the con struc tion of re lief maps of the top of

sub-Qua ter nary strata. Geo phys i cal re sis tiv ity sur veys were per formed along geo log i cal cross-sec tions. They con firmed the pres ence of sub-Qua ter nary land forms de scribed in the pa per. Zones of glaciotectonic dis tur bances in the study area were iden ti fied and ana lysed as well.

GEO LOG I CAL SET TING

OF THE SUB-QUA TER NARY BASE MENT

VS. THE RE LIEF OF THE EAST ERN PART

OF THE POMERANIAN LAKELAND

The east ern part of the Pom er a nian Lakeland, span ning the Kaszuby and Bytów lakelands, is a highly el e vated area (over 200 m a.s.l.) of morainic pla teaus with some cul mi na -tions at tain ing 230–250 m a.s.l. There oc curs the high est point of the Eu ro pean Low lands – Wie¿yca (329 m a.s.l.). The sur faces of the morainic pla teaus are com posed of tills. The area is transected by four sys tems of large subglacial chan nels; from the east these are: the D¹browskie and Patul- skie lakes val ley, Raduñskie lakes val ley, Gowidliñskie Lake val ley and Jasieñ Lake val ley. A few tens of metres high prom i nent es carp ments bound the val leys. The val leys’ bot toms or wa ter lev els of the val leys’ lakes lie 60–70 m lower than the sur faces of the sur round ing morainic pla teaus. Tak ing into ac count the depths of the lakes, the dif -fer ences in el e va tion be tween the pla teau sur face and the val ley bot tom range from 80 to 100 m.

The morainic pla teaus of the Kaszuby and Bytów lake-lands de scend south wards to the el e va tion of 160–150 m a.s.l. They ad join here a zone of outwash plains de pos ited dur ing the Pom er a nian Phase of the Vistulian (Weichselian) Gla ci ation. To wards the north, the pla teau ar eas de scend and pass into coastal morainic pla teaus of Damnica and ¯arnowiec. The coastal pla teaus are sit u ated at much lower el e va -tions (100 m a.s.l.) than the morainic ar eas of the lakelands.

The morainic pla teaus are com monly re ferred to as lakeland ridges. This term is jus ti fied not only by the high el e va tions of these ar eas but also by their subsurface geo -log i cal struc ture. The sub-Qua ter nary bed rock of this re gion lies at higher el e va tions than it does in the ar eas sit u ated to the south and north of the lakeland ridge. The top of Mio -cene strata that un der lie the Qua ter nary suc ces sion in the lakeland ridge is lo cated at el e va tions rang ing from 100 m a.s.l. in the Bytów Lakeland to 60–80 m a.s.l. in the

Kaszuby Lakeland (Fig. 2). The top of Mio cene strata de scends north wards. In the South Bal tic coast, it lies at el e va -tions rang ing from 20 m b.s.l. to 60 m b.s.l. To the south of the lakeland ridge, in the outwash plains area, the top of Mio cene strata de scends to 20–40 m a.s.l.

In pre vi ous pa pers (Zaborski, 1933; Oko³owicz, 1956; Piasecki, 1958, 1962; Pachucki, 1961; Sylwestrzak, 1961, 1972, 1973, 1978; Galon, 1967, 1968; Roszko, 1968; Beniuszys, 1968; Szukalski, 1968; Augustowski, 1969) con -cern ing the re lief and geo log i cal struc ture of the east ern part of the Pom er a nian Lakeland, li thol ogy of Qua ter nary sed i -ments and their re la tion ship to the subsurface geo log i cal struc ture of the area was ne glected. The ex cep tions are the works de voted to the Gdañsk re gion, pre sented by Mojski (1979, 2002), who in di cated a clear re la tion ship be tween the pres ent-day topography of the area and the re lief and geo log i cal struc ture of Neo gene strata.

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Fig. 1. Lo ca tion of ar eas dis cussed in the pa per: 1 – lo ca tion of the sheets of the De tailed Geo log i cal Map of Po land, scale 1:50,000, pre pared by the au thor, 2 – lo ca tion of geo log i cal crosssec tions, 3 – lo ca tion of lake val leys pre sented in the pa per, 4 – lo ca tion of in di vid -ual fig ures

Geo log i cal works con ducted by my self on 12 sheets of the DGMP re vealed a re la tion ship be tween large subglacial chan nels and the sub-Qua ter nary base ment re lief.

The Raduñskie Lake tun nel val ley and the D¹browskie and Patulskie lake tun nel val ley (Fig. 3) oc cur in the area where the deep Raduñska and Patulska subglacial chan nels (faultbounded val leys) are in cised in the top of the Mio -cene. The val leys’ bot toms are sit u ated at 80–120 m b.s.l. el e va tion and lie 140–180 m lower than the sur round ing ar -eas where the top of the Mio cene is lo cated at 60 m a.s.l. The trend of these subglacial chan nels and their geo log i cal struc ture is doc u mented by 30 ar chi val bore holes and re -search bore holes drilled for the pur poses of the DGMP. The Qua ter nary sec tion drilled in the Patulska val ley is over 308 m thick (a bore hole at Szymbark, sheet Egiertowo of the DGMP). The bot toms of both val leys are lined with de pos its of the old est (Narewian; Menapian) gla ci ation. The Raduñ-ska val ley is filled with gla cial de pos its, in clud ing ice-dam-med lake silts and clays, Narewian–Menapian, Sanian– Elsterian 2, Odranian–Saalian 1 and Wartanian–Saalian 2 till ho ri zons, and glaciofluvial sands. Flu vial sed i ments of the Lubawa (Saalian 1/Saalian 2) Inter gla cial com prise only a 4 m-thick se ries of the en tire 266-m-thick depositional suc ces sion fill ing the val ley.

The Patulska val ley, in con trast to the Raduñska val ley, is filled mainly by very thick tills of the Odranian (Saalian 1) Gla ci ation (56.0 m) and Wartanian (Saa(Saalian 2) Gla ci -ation (in clud ing Lower Stadial (76.0 m) and Mid dle Stadial (20.0 m)), as well as by glaciofluvial sands. Flu vial sed i

ments in this 308mthick sec tion are merely 8.0 m in thick -ness, and are rep re sented by the Mazovian (Holsteinian) Inter gla cial sands.

The fill ing of both the val leys proves that they were sites of subglacial de po si tion through out the en tire Qua ter -nary pe riod. No signs of ero sion is ob served in the val leys’ bot toms, thus they were not river val leys dur ing inter gla cial pe ri ods.

Deep val leys cut into the sub-Qua ter nary base ment formed and de vel oped in the Qua ter nary. Dur ing Neo gene and preglacial (Early Pleis to cene) times, vari a tions in the re lief of the top of Mio cene strata were the same as to day. Such high vari a tions in the el e va tion of the top of the Mio -cene would have had to be re duced by gla cial ero sion and ac cu mu la tion. At the site of the pres ent-day deep Raduñska and Patulska val leys, there were prob a bly shal low top o -graphic de pres sions, most likely river val leys. Dur ing the Narewian (Menapian) ice-sheet ad vance, the val leys be -came filled with tills and glaciofluvial sands.

The cov er ing of the area by the ad vanc ing ice sheet re -sulted in re ac ti va tion of pre-ex ist ing fault zones within the sub-Ce no zoic base ment. Af ter the ice re treat, iso static re bound of the Earth’s crust oc curred in the area that was pre vi -ously de formed due to ice load ing. The up lift con tin ued with dif fer ent speed along the pre-ex ist ing fault zones, re sult ing in the for ma tion of a horst. The am pli tude of ver ti cal move -ments along the fault lines at tained a few tens of metres.

The same sit u a tion oc curred dur ing the suc ces sive ice-sheet ad vances. Al ways at the same sites, along the fault

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Fig. 2. Re lief of the top of subQua ter nary strata in the Kaszuby and Bytów lakelands; lo ca tion of geo log i cal crosssec tions from Fig -ures 3 and 4: 1 – edges in re lief of the top of sub-Qua ter nary strata, M – Mio cene sands, Ol – Oligocene sands and silts, E – Eocene sands

zones, subglacial chan nels de vel oped dur ing the fol low ing glaciations. Thick till se ries were de pos ited in these val leys, which were sub se quently de formed by glaciotectonic pro -cesses. The trend of the val leys co in cides with that of photolineaments iden ti fied by Ba¿yñski et al. (1984) and Graniczny et al. (1987, 1995) in di cat ing that these land forms are as so ci ated with the tec tonic struc ture of the base -ment.The Wie¿yca Hill is lo cated upon a fault zone at the bound ary be tween the Patulska val ley and the area of the up lifted top of Mio cene strata (up to 60 m a.s.l. in el e va tion; Fig. 3). The hill is a large cre vasse-fill landform at tain ing the el e va tion of over 250 m a.s.l., whose in di vid ual peaks ex ceed 300 m a.s.l. and the sum mit is at 329 m a.s.l. (the high est hill of the Eu ro pean Low lands). The thick ness of sand-gravel-boul der sed i ments com pos ing the Wie¿yca Hill ex ceeds 53 m.

The for ma tion of such a large cre vasse-fill landform was pos si ble ow ing to its lo ca tion upon a fault zone where a set of cre vasses de vel oped in the ice sheet when its front was to the south of the study area and the ice mass was rel a -tively thick.

To the east of Wie¿yca, the NE–SW-trending Mar-szewo val ley is sit u ated. It is deeply in cised (60–70 m) into the sur round ing Przywidz Pla teau that rises to the el e va tion of over 200 m a.s.l. To the east, be tween Kolbudy and Czerniewo, the pla teau is bor dered by a high (70–80 m) edge slop ing to wards the ¯u³awy Wiœlane Low land. The trend of the Marszewo val ley and the pla teau-bound ing edge is closely re lated to the an cient land forms ob served in the sub-Qua ter nary base ment.

The N–Strending an cient edge is 100 m high. It sep a -rates the area of el e vated top of Mio cene strata (40 m a.s.l.) in the Kaszuby Lakeland from the area where the top of the Mio cene is sit u ated at the el e va tion be low 60 m b.s.l. in the ¯u³awy Wiœlane re gion. At the foot of the edge, there is a thick com plex (60 m) of Narewian (Menapian), Nidanian

(Elsterian 1), Sanian 1 and Sanian 2 (Elsterian 2) tills. The an cient Marszewo val ley is in cised to a depth of 80 m be low the top of Mio cene strata that lies at 40 m a.s.l. (Fig. 4). Its bot tom is lined with the Augustovian (Bavelian s.l.) Inter gla cial flu vial sands and grav els over lain by Nidanian Gla ci ation de pos its (tills interlayered by icedammed lake sed i -ments, 53 m in thick ness).

The val leys of the Raduñskie lakes and D¹browskie and Patulskie lakes, as well as the Marszewo val ley and the edge of the Kaszuby Lakeland be tween Kolbudy and Czerniewo clearly fol low the di rec tion of preex ist ing land forms ob -served in the sub-Qua ter nary base ment. Sed i ments of the old est gla ci ation (Menapian) and South-Pol ish (Elsterian) glaciations of all these land forms fill the val leys (re lief de -pres sions) in the top of Neo gene strata.

In the ar eas where the top of sub-Qua ter nary base ment is sit u ated at high el e va tions, sed i ments of the old est and South-Pol ish glaciations are ab sent. Gla cial de po si tion started here with the Mid dle-Pol ish (Saalian) Glatiation (Odranian and Wartanian) sed i ments that smoothed the rough re lief of older gla ci ation pe ri ods. Geo log i cal cross-sec tions through the Raduñskie, D¹browskie and Patulskie lake val leys (Fig. 3), the Marszewo val ley, and the Kaszuby Lakeland be tween Kolbudy and Czerniewo (Fig. 4) dif fer in the num ber of iden ti fied till ho ri zons, which was proved based on litho-petrographic in ves ti ga tions con ducted for the DGMP.

A sim i lar type of geo log i cal struc ture is ob served in the east ern part of the Bytów Lakeland where the course of the Jasieñ Lake val ley is re lated to the trend of an an cient val ley ob served in the subQua ter nary base ment. A more in ter est -ing is sue is the prob lem of the bound ary be tween the Odra and Vistula ice lobes of the Pom er a nian Phase of the Main Stadial of the Vistulian (Weichselian) Gla ci ation. The bound ary is drawn across the Bawernica morainic pla teau ris ing above 200 m a.s.l. (Keilhack, 1898; Oko³owicz,

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Fig. 3. Geo log i cal cross-sec tion through the Raduñskie lakes val ley and the D¹browskie and Patulskie lakes val ley. Cr – Cre ta ceous, Ol – Oligocene, M – Mio cene; Glaciations: A – Narevian (Menapian), N – Nidanian (Elsterian 1), S – Sanian 1 (Elsterian 2), G – Sanian 2 (Elsterian 2), O – Odranian (Saalian 1), W – Wartanian (Saalian 2), B – Vistulian (Weichselian); 1 – peat, 2 – sands, 3 – clays, 4 – tills, 5 – Neo gene and Palaeogene sands, 6 – Cre ta ceous chalk and marl

1956; Sylwestrzak, 1972; Petelski, 1998), where in di vid ual peaks ex ceed 225 m a.s.l. The Bawernica pla teau co in cides with the area where the top of Neo gene strata lies at very high el e va tions (over 100 m a.s.l.). An cient subglacial chan -nels oc cur on both sides of the el e vated sub-Qua ter nary bed rock. Their bot toms are at depths of 30–40 m a.s.l. These an cient chan nels are as so ci ated with large subglacial chan -nels ob served at the sur face: the Jasieñ Lake subglacial channel run ning to the west of the Bawernica morainic pla teau, and the Gowidliñskie Lake subglacial chan nels oc cur -ring to the east of the pla teau.

In the cen tral part of the Bytów Lakeland, north of Miastko, the morainic pla teau is dis sected by deep val leys and its el e va tion ex ceeds 200 m a.s.l. The val ley bot toms lie 80–100 m be low the pla teau sur face. The courses of the val -leys co in cide with the trends of an cient val leys in the sub-Qua ter nary base ment (Petelski et al., 2009).

The an cient val leys of the Bytów Lakeland, like those in the Kaszuby Lakeland, are filled with sed i ments of the old est gla ci ation and the South Pol ish glaciations. No de -pos its of these ages have been found in ar eas of the el e vated top of Neo gene strata. Sed i ments of the Odranian, Warta-nian and Vistulian glaciations cover both the study area and the an cient de pres sions in the sub-Qua ter nary sur face, smooth ing the rough re lief of the sub-Qua ter nary bed rock.

SOUTH BAL TIC COASTLAND

I con ducted geo log i cal in ves ti ga tions in the Gardno Low land, Reda–£eba ice-mar ginal val ley and ¯arnowiec Lake re gion of the Bal tic coastland (Petelski, 1975, 1976, 1978, 1985, 1990; Petelski & Jurys, 1989).

Since the be gin ning of the 20th cen tury, many dis cus -sions have been made on the for ma tion of the Reda–£eba ice-mar ginal val ley. How ever, Petelski and Sadurski (1987a, b, 1988) in di cated a re la tion ship be tween these land forms

and an cient val leys that ex isted in the presentday icemar -ginal val ley through out the en tire Qua ter nary pe riod. They also pointed out to the re la tion ship be tween these land forms and the ¯arnowiec Lake tun nel val ley, which was a sub-gla cial chan nel dur ing the Qua ter nary. The for ma tion and sig nif i cance of the ¯arnowiec Lake tun nel val ley at the site where a fault cuts the Palaeozoic base ment have been con -firmed by many au thors (cf. Dadlez, 1990; Znosko, 1998).

A dif fer ent sit u a tion ex isted in the Gardno Low land where one of the best-doc u mented lobal pat terns in Po land ex ists. Al though the area was de scribed al ready in the 20th cen tury lit er a ture (Borne, 1857; Jentzsch, 1914; Bülow, 1924, 1930, 1932; Hartnack, 1926; Halicki, 1947; Giedrojæ- Juraha, 1949; Rosa, 1963, 1964, 1968; Bartkowski, 1965; Roszko, 1968; Sylwestrzak, 1972, 1973, 1979; Petelski, 1975, 1976, 1978, 1985; Petelski & Jurys, 1989; Mojski & Or³owski, 1978; Tobolski, 1984, 1989; Rotnicki, 1987, 1994, 1999; Rotnicki & Borówka, 1990, 1994; Wojcie-chowski, 1988, 1990; Florek & Or³owski, 1991; Dobrzyñ-ski et al., 1991; Jasiewicz, 1998, 1999; Czerniawska, 1999, 2004), re con struc tion of a rel a tively de tailed im age of both the li thol ogy of the Qua ter nary se ries and the re lief of the top of Neo gene strata was pos si ble in 2003–2006 only (Pe-telski, 2005, 2006; Fig. 5). Geo log i cal stud ies car ried out in this area over the last years have shown a clear re la tion ship be tween the re lief of the area and the re lief of the subQua -ter nary base ment.

The dom i nant landform of the sub-Qua ter nary base -ment is an ex ten sive val ley. It be gins south of S³upsk and then runs across S³upsk to W³ynkówko, where it turns northeastwards to Smo³dzino and then to wards the north be neath the Bal tic Sea floor. The bot tom of the val ley is un -even; it slopes at dif fer ent an gles. In S³upsk, it is lo cated at a depth of more than 140 m b.s.l. (Fig. 6), be tween W³yn-kówko and Smo³dzino – be low 120 m b.s.l. (Fig. 7), whereas north of Smo³dzino it reaches a depth of 257 m b.s.l. The width of the landform var ies be tween 2 and 3 km.

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The val ley is sur rounded by ar eas where the top of Neo gene strata is sit u ated at el e va tions of 0 to 20 m a.s.l. The only re gion where the top of Neo gene strata oc curs at lower el e va -tions (40–60 m b.s.l.) is the north ern part of the study area.

The ba sic el e ments of the pres ent-day re lief of the study area co in cide with the trend of both the an cient de pres sions ob served in the top of the Neo gene and the ac com pa ny ing glaciotectonic de for ma tion zones. The po si tion of the ice lobe that ac cu mu lated Gardno mo raine de pos its was con -trolled by a de pres sion in the top of Neo gene strata, which ac com pa nies the above-men tioned val ley. The course of the north ern edge of the Damnica morainic pla teau co in cides with the trend of the south ern edge of an an cient val ley run -ning be tween W³ynkówko and Smo³dzino. The subglacial chan nel, con tain ing the S³upia River be tween Kawkowo and W³ynkówko, runs along an an cient val ley ob served in the top of Neo gene strata.

As in the case of the Kaszuby and Bytów lakelands where the an cient val leys are filled with sed i ments of the old est gla ci ation and the SouthPol ish glaciations, the val -ley run ning from S³upsk through W³ynkówko and Smo³-dzino, and far ther north wards un der the Bal tic Sea floor, is filled with Narewian, Nidanian, Sanian 1 and Sanian 2 de -pos its. No flu vial sed i ments have been found here. In the val ley sec tion that crosses the S³upsk re gion, the sed i ments are rep re sented by Narewian, Sanian 1 and Sanian 2 tills inter- bed ded by glaciofluvial sands and grav els. They are strongly glaciotectonically de formed and rep re sent an ex -am ple of the val ley-side glaciotectonics (Dadlez &-amp; Jaro-szewski, 1994). Be tween W³ynkówko and Smo³dzino, the val ley is filled with a thick (88 m) com plex of till ho ri zons (also strongly glaciotectonically de formed) de pos ited dur -ing the Narewian, Nidanian, Sanian and Odranian glacia-tions, with no in ter ven ing sed i ments ob served. To the north of Smo³dzino, the bot tom of the val ley is at 263 m b.s.l el e -va tion. It is filled with thick till se ries of the fol low ing glaciations: Narewian (72 m), Nidanian (24 m) and Sanian (59 m). The tills are sep a rated by glaciofluvial sands, whose thick ness is small as com pared to the till thick ness. In the area out side the an cient val ley, where the top of the Neo gene is at higher el e va tions, the gla cial suc ces sion com -mences with the Odranian or Wartanian sed i ments which lev elled the vari able re lief of the top of the Neo gene. Geo -log i cal cross-sec tions pre sented in Fig ures 6 and 7 dif fer in the num ber of iden ti fied tills, as doc u mented by litho-petro-graphic in ves ti ga tions of the DGMP. Geo log i cal struc ture and tec tonic set ting of the sub-Qua ter nary base ment were thor oughly ex plored in the South Bal tic area by geo phys i cal meth ods in clud ing high-res o lu tion seis mic sur veys (Kra-marska et al., 1999; Krzywiec et al., 2003). There is a clear re la tion ship be tween the Cre ta ceous–Caino zo ic lithologies and the ori en ta tion of fault zones in the Palaeozoic base ment. There fore, the oc cur rence of glaciotectonic de for ma -tion zones in the S³upsk re gion (Figs 6, 7) is sup posed to be con strained by the block-type tec ton ics of the Cre ta ceous suc ces sion.

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Fig. 5. Re lief of sub-Qua ter nary strata in the Gardno Low land and S³upsk re gion; lo ca tion of geo log i cal crosssec tions from Fig -ures 6 and 7. 1 – geo log i cal cross-sec tion lines, 2 – edges of morainic pla teau, 3 – morainic pla teau, 4 – Gardno fron tal mo -raines, 5 – edges in re lief of the top of sub-Qua ter nary strata

CON CLU SIONS

The or i gin of the an cient val leys from the South Bal tic coastland and Kaszuby and Bytów lakelands is the same and con sists in re ac ti va tion of fault zones pre-ex ist ing in the sub-Caino zo ic base ment due to the ice mass load ing dur ing suc ces sive ice-sheet ad vances. These ar eas were sub se -quently the sites of de vel op ment of subglacial chan nels

where thick till ho ri zons and ice-dammed lake sed i ments ac cu mu lated.

The trend of the val leys co in cides with photolineaments iden ti fied by Ba¿yñski et al. (1984), in di cat ing that these land forms are re lated to the tec tonic struc ture of the base -ment. Ac cord ing to Dadlez (1976, 1989, 1990) and Znosko (1998), the ¯arnowiec Lake tun nel val ley is lo cated on a fault zone within the Palaeozoic basement.

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Fig. 6. Geo log i cal cross-sec tion through the Damnica Pla teau and S³upia River val ley. For ex pla na tions see Fig. 3

The Gardno val ley, in par tic u lar its north ern sec tion whose bot tom is at 263 m b.s.l. el e va tion, can be com pared with an cient val leys de scribed from the floor of the South Bal tic Sea (Kramarska et al., 1999) where high-res o lu tion re flec tion seis mic data re vealed their re la tion to the fault zones of the Palaeozoic basement.

Iso static move ments of the Earth’s crust along the re ju -ve nated fault zones caused re ac ti va tion of the pre-ex ist ing subglacial chan nels dur ing suc ces sive Pleis to cene glacia-tions. It is worth not ing, how ever, that the pro cess was more in tense in Mid-Pleis to cene times, prob a bly due to neotecto-nic move ments of the Kuyavian and Mazovian phases (Baraniecka, 1975) that were su per im posed on the iso static crustal move ments. The vari a tions in the geo log i cal struc -ture style (dis con tin u ous de for ma tion in the Raduñskie lake tun nel val ley, D¹browskie and Patulskie lake tun nel val ley, and in the zone of strong glaciotectonic de for ma tion in the S³upsk tun nel val ley; quiet de po si tion in the Marszewo tun -nel val ley) were caused by vari able in ten sity of iso static crustal move ments in the study area. Large and deep tun nel val leys, filled with strongly de formed sed i ments, developed in areas of intense vertical crustal motions.

All the subglacial chan nels are filled with sed i ments of the old est gla ci ation and the South-Pol ish glaciations. These sed i ments are ab sent from the sur round ing ar eas where the top of Neo gene strata was be ing up lifted and the sed i ments have been re moved. The Up per Pleis to cene de pos its cover the whole of the study area, lev el ling dif fer en ti ated re lief of the top of Neogene strata.

The bound ary be tween the Odra and Vistula ice lobes of the Pom er a nian Phase of the Main Stadial of the Vistu-lian Gla ci ation runs across the Bawernica morainic pla teau. This is an area of highly el e vated top of Neo gene strata (above 100 m a.s.l.). The up lift ing move ments of this area fa voured sep a ra tion of the ice into two ice lobes: the Odra and Vistula lobes.

The in flu ence of the re lief of the subQua ter nary base -ment on the pres ent-day to pog ra phy of this area is much stronger than pre vi ously thought. The lo ca tions of large subglacial chan nels and high top o graphic edges, the po si -tion of the high est cul mi na -tion of the Pom er a nian Lakeland (Wie¿yca) and the bound ary be tween the Odra and Vistula ice lobes are all re lated to the re lief of the top of Neo gene strata. The re lief formed as a re sult of ver ti cal move ments of the Earth’s crust during the Pleistocene.

REF ER ENCES

Augustowski, B., 1969. Œrodowisko geograficzne województwa gdañskiego w zarysie. (In Pol ish). Wy¿sza Szko³a Pedago-giczna, Gdañsk.

Baraniecka, M., 1975. The dependences of the de vel op ment of Qua ter nary de pos its upon the struc ture and dy nam ics of the base ment in the cen tral part of the Pol ish Low lands. (In Pol -ish, Eng lish sum mary). Biuletyn Instytutu Geologicznego, 288: 5–97.

Bartkowski, T., 1965. RzeŸba, budowa geologiczna, geomorfologia i stosunki wodne województwa koszaliñskiego. (In Pol -ish). Instytut Zachodni, Poznañ.

Ba¿yñski, J., Doktór, S. & Graniczny, M., 1984. Mapa

foto-geologiczna Polski. (In Pol ish). Instytut Geologiczny, War-szawa.

Beniuszys, S., 1968. Geo log i cal struc ture of the Hill Wie¿yca in the light of re cent stud ies. (In Pol ish, Eng lish sum mary). Kwartalnik Geologiczny, 12: 403–409.

Borne, V. D., 1857. Zur Geognosie der Provinz Pommern. Zeitschrift der Deutschen Geologischen Gesellschaft, 9: from 473.

Bülow, K., 1924. Die Diluviallandschaft im nordostlichen Hinter-pommern. Jahrbuch der Preussischen Geologischen Landes-anstalt, Bd. 45: 317–344.

Bülow, K., 1930. Erdgeschichte und Landschaftsgestaltung im Kreis Stolp in Pommern. Eulitz, Stolp.

Bülow, K., 1932. Randlagen und Ruckzug des letzten Eises in Hinterpommern. Zeitschrift der Deutschen Geologischen Gesellschaft, 84: 241–251.

Czerniawska, J., 1999. Ice-dammed de pos its in the lower ³upawa river val ley. (In Pol ish, Eng lish sum mary). In: Borówka, R. (ed.), Ewolucja geosystemów nadmorskich po³udniowego Ba³tyku. Wydawnictwo Naukowe Bogucki, Poznañ – Szcze-cin: 63–67

Czerniawska, J., 2004. Zone of ice-con tact sed i men ta tion of ice-dammed lake and gla cial de pos its in the north ern part of for mer ice-dammed lake in the lower £upawa val ley from the Gardno Phase pe riod. (In Pol ish, Eng lish sum mary). In: Kostrzewski, A. (ed.), Geneza, litologia i stratygrafia osadów czwartorzêdowych, Tom IV, Geografia, 68: 37–47, Poznañ. Dadlez, R., 1976. Out line of Sub-Caino zo ic ge ol ogy in the South

Bal tic Ba sin. (In Pol ish, Eng lish sum mary). Biuletyn Instytutu Geologicznego, 185: 21–50.

Dadlez, R., 1989. Deep sub stra tum of the south ern Bal tic and ad ja -cent ar eas – a tec tonic out line. (In Pol ish, Eng lish sum mary). Studia i Materia³y Oceanologiczne, 56: 33–38.

Dadlez, R., 1990. Tec ton ics of the South ern Bal tic. (In Pol ish, Eng lish sum mary). Kwartalnik Geologiczny, 34: 1–20. Dadlez, R. & Jaroszewski, W., 1994. Tektonika. (In Pol ish). PWN,

Warszawa.

Dobrzyñski, S., Florek, E., Florek, W. & Or³owski, A., 1991. Plejstocen Œrodkowego Pomorza i pobrze¿a Ba³tyku w œwie-tle termoluminescencyjnych wskaŸników wieku osadów. (In Pol ish). Przegl¹d Geologiczny, 39 (5-6): 301–306.

Florek, W. & Or³owski, A., 1991. O wieku maksimum transgresji jeziora Gardno. (In Pol ish). Przegl¹d Geologiczny, 39 (5-6): 298–301.

Galon, R., 1967. Czwartorzêd Polski Pó³nocnej. (In Pol ish). In: Galon, R. & Dylik, J. (eds), Czwartorzêd Polski. PWN, Warszawa: 106–166.

Galon, R., 1968. The course of deglaciation in the Peribalticum. (In Pol ish, Eng lish sum mary). In: Ostatnie zlodowacenie skandynawskie w Polsce. Prace Geograficzne Instytutu Geo-grafii PAN, 74: 201–216.

Giedrojæ-Juraha, S., 1949. Moreny czo³owe okolic jeziora Gardno. (In Pol ish). Czasopismo Geograficzne, 20: 239–244. Graniczny, M., Doktór, S. & Kucharski, R., 1987. Korelacja

danych teledetekcyjnych i geofizycznych za pomoc¹ technik cyfrowych. (In Pol ish). Przegl¹d Geologiczny, 35 (8-9): 453– 461.

Graniczny, M. Doktór, S. & Kucharski, R., 1995. Sprawozdanie z opracowania mapy liniowych elementów strukturalnych Polski w skalach 1:200 000 i 1:500 000 na podstawie kom-pleksowej analizy komputerowej zdjêæ geofizycznych i tele-detekcyjnych. (In Pol ish). Un pub lished re port, Pañstwowy Instytut Geologiczny, Warszawa.

Halicki, B., 1947. Projekt Nadmorskiego Parku Narodowego. (In Pol ish). Wiadomoœci Muzeum Ziemi, 3: 77–91.

Hartnack, W., 1926. Die Küste Hinterpommerns unter besonderer Berücksichtigung der Morphologie. Jahrbuch Geogr. Ges., Beih. II zum 43/44, Stolp.

Jasiewicz, J., 1998. Stratygrafia osadów gardzieñskiej moreny czo³owej. (In Pol ish). In: Kostrzewski, A. (ed.), Geneza, litologia i stratygrafia osadów czwartorzêdowych, Tom III, Geografia, 64: 49–51, Poznañ.

Jasiewicz, J., 1999. Glaciotectonic struc ture of du plex (Gardno phase and mo raine, Dêbina cliff, west of Rowy). (In Pol ish, Eng lish sum mary). In: Borówka, R. (ed.), Ewolucja geosyste- mów nadmorskich po³udniowego Ba³tyku. Wydawnictwo Naukowe Bogucki, Poznañ – Szczecin: 87–93.

Jentzsch, A., 1914. Beobachtungen am Ostseestrand im Hinter-pommer und Westpreussen. Jahrbuch der Preussischen Geo-logischen Landesanstalt, Bd. 35: 131–145.

Keilhack, K., 1898. Die Stillstandeslagen des letzten Inlandeises und die hydrographische Entwicklung des pommerschen Küstengebietes. Jahrbuch der Preussischen Geologischen Landesanstalt, 19: 90–152.

Kramarska, R., Krzywiec, P., Dadlez, R., Jegliñski, W., Papiernik, B., Przezdziecki, P. & Zientara, P., 1999. Geo log i cal map of the Bal tic Sea bot tom with out Qua ter nary de pos its, 1:500,000. (In Pol ish, Eng lish sum mary). Pañstwowy Instytut Geologiczny, Gdañsk–Warszawa.

Krzywiec, P., Kramarska, R. & Zientara, P., 2003. Strikeslip tec ton ics within the SW Bal tic Sea and its re la tion ship to the in -ver sion of the Mid-Pol ish Trough – ev i dence from high-res o lu tion seis mic data. Tectonophysics, 373: 94–105. Lisicki, S., 2003. Lithotypes and lithostratigraphy of tills of the

Pleis to cene in the Vistula drain age ba sin area, Po land. (In Pol ish, Eng lish sum mary). Prace Pañstwowego Instytutu Geologicznego, 177: 1–105.

Mojski, J.E., 1979. An out line of Pleis to cene stra tig ra phy and struc ture of its base ment in Gdañsk area. (In Pol ish, Eng lish sum mary). Biuletyn Instytutu Geologicznego, 312: 5–50. Mojski, J.E., 2002. Czwartorzêd regionu gdañskiego. (In Pol ish).

Przegl¹d Geologiczny, 50 (8): 705–708.

Mojski, J. E. & Or³owski, A., 1978. Pleis to cene subgla cial chan nel from the vi cin i ties of S³upsk. (In Pol ish, Eng lish sum -mary). Kwartalnik Geologiczny, 22: 171–179.

Oko³owicz, W., 1956. Morfogeneza wschodniej czêœci Pojezierza Pomorskiego. (In Pol ish). Biuletyn Instytutu Geologicznego, 100: 355–393.

Pachucki, C., 1961. Moreny czo³owe ostatniego zlodowacenia na obszarze Peribalticum. (In Pol ish). Rocznik Polskiego Towa-rzystwa Geologicznego, 31: 303–318.

Petelski, K., 1975.On the geo log i cal struc ture of the Gardno ter mi -nal mo raine as seen in the cliff ex po sures be tween Dêbina and Poddêbie in west Pomerania. (In Pol ish, Eng lish sum mary). Zeszyty Naukowe Wydzia³u Biologii i Nauk o Ziemi Uniwer-sytetu Gdañskiego, 5: 169–179.

Petelski, K., 1976. Glacidynamic dis tur bances in the floor of the boul der clay mid dle ho ri zon in cliff out crops found near the vil lage Dêbina in west Pomerania. (In Pol ish, Eng lish sum -mary). Zeszyty Naukowe Wydzia³u Biologii i Nauk o Ziemi Uniwersytetu Gdañskiego, 6: 87–99.

Petelski, K., 1978. Dead ice ac cu mu la tion forms in ter mi nal ba sin of the Gardno lobe. (In Pol ish, Eng lish sum mary). Kwartalnik Geologiczny, 22: 621–634.

Petelski, K., 1985. Geo log i cal fea ture of Gardno lobe front mo -raine and end trough. (In Pol ish, Eng lish sum mary). Biuletyn Instytutu Geologicznego, 348: 89–121.

Petelski, K., 1990. Nowe dane o budowie geologicznej i genezie pradoliny Redy – £eby. (In Pol ish). In: Mojski, J. E. & Sadurski, A. (eds), Przewodnik 61 Zjazdu Polskiego

Towa-rzystwa Geologicznego, Gdañsk 13-15 wrzeœnia 1990. Wydawnictwo AGH, Kraków: 26–29.

Petelski, K., 1998. Szczegó³owa Mapa Geologiczna Polski 1:50000, arkusz Pomysk Wielki. (In Pol ish). Pañstwowy Instytut Geologiczny, Warszawa.

Petelski, K., 1999. Szczegó³owa Mapa Geologiczna Polski 1:50000, arkusz Egiertowo. (In Pol ish). Pañstwowy Instytut Geologiczny, Warszawa.

Petelski ,K., 2000a. Szczegó³owa Mapa Geologiczna Polski 1:50000, arkusz Koœcierzyna. (In Pol ish). Pañstwowy Instytut Geologiczny, Warszawa.

Petelski, K., 2000b. Szczegó³owa Mapa Geologiczna Polski 1:50000, arkusz Egiertowo – Wielki Klincz. (In Pol ish). Pañstwowy Instytut Geologiczny, Warszawa.

Petelski, K., 2001. Szczegó³owa Mapa Geologiczna Polski 1:50000, arkusz Dzier¿¹¿no. (In Pol ish). Pañstwowy Instytut Geologiczny, Warszawa.

Petelski, K., 2002. Szczegó³owa Mapa Geologiczna Polski 1:50000, arkusz Smo³dziñski Las. (In Pol ish). Pañstwowy Instytut Geologiczny, Warszawa.

Petelski, K., 2003a. Szczegó³owa Mapa Geologiczna Polski 1:50000, arkusz Skarszewy. (In Pol ish). Pañstwowy Instytut Geologiczny, Warszawa.

Petelski, K., 2003b. Szczegó³owa Mapa Geologiczna Polski 1:50000, arkusz Godziszewo. (In Pol ish). Pañstwowy Instytut Geologiczny, Warszawa.

Petelski, K., 2005. Szczegó³owa Mapa Geologiczna Polski 1:50000, arkusz Smo³dzino. (In Pol ish). Pañstwowy Instytut Geologiczny, Warszawa.

Petelski, K., 2006. Szczegó³owa Mapa Geologiczna Polski 1:50000, arkusz S³upsk. (In Pol ish). Pañstwowy Instytut Geologiczny, Warszawa.

Petelski, K., 2008. Szczegó³owa Mapa Geologiczna Polski 1:50000, arkusz Miastko. (In Pol ish). Pañstwowy Instytut Geologiczny, Warszawa.

Petelski, K., 2009. Szczegó³owa Mapa Geologiczna Polski 1:50000, arkusz Karsin. (In Pol ish). Pañstwowy Instytut Geologiczny, Warszawa.

Petelski, K. & Jurys, L., 1989. Gen e sis of the north ern edge of S³upsk morainic pla teau be tween Wrzeœæ and G³ówczyce. (In Pol ish, Eng lish sum mary). Studia i Materia³y Oceanolo-giczne, 56: 251–256.

Piasecki, D., 1958. Wycieczka B-3 na Pojezierze Kaszubskie. (In Pol ish). In: Przewodnik XXXI Zjazdu Polskiego Towarzystwa Geologicznego w Gdañsku. Polskie Towarzystwo Geolo-giczne, Gdañsk: 33–38.

Petelski, K., Piotrowski, A. & Schiewe, M., 2009. The in flu ence of the con fig u ra tion of the Neo gene sed i ments roof re lief on the geo log i cal fea ture of the Qua ter nary sed i ments and the con -tem po rary re lief of the Bytów Lake Dis trict and Polanowska Up land. (In Pol ish, Eng lish sum mary). In: Kostrzewski, A. & Paluszkiewicz, R. (eds), Geneza, litologia i stratygrafia utwo- rów czwartorzêdowych, T. V, UAM, Seria Geografia, 88: 417–422, Poznañ.

Petelski, K. & Sadurski, A., 1987a. The gen e sis of the Reda-£eba ice mar ginal val ley in the light of the heatmass trans fer the -ory. (In Pol ish, Eng lish sum mary). Czasopismo Geogra-ficzne, 58: 439–456.

Petelski, K. & Sadurski, A., 1987b. Kreda jeziora wskaŸnikiem rozpoczêcia holoceñskiej wymiany wód podziemnych. (In Pol ish). Przegl¹d Geologiczny, 35 (3): 143–147.

Petelski, K. & Sadurski, A., 1988. Geo log i cal and hydrogeological char ac ter is tics of the catch ment area of the ket tle – lake Orle. Folia Quaternaria, 58: 13–30.

Piasecki, D., 1962. Fizjografia dorzecza Raduni i morfogeneza jej

doliny. (In Pol ish). Zeszyty Geograficzne WSP w Gdañsku, IV: 51–119.

Rosa, B., 1963. Über die morphologische Entwicklung der Küste Polen im Lichte der alten Strandformen. (In Pol ish, Ger man sum mary). Studia Societatis Scientiarum Torunensis, Sectio C, 5: 1–172.

Rosa, B., 1964. On al lu vial and biogenic de pos its fill ing the floors of the rivers of the Pol ish coastal zone, their con nec tion with the trans gres sion of the sea and their sig nif i cance in the in ves -ti ga -tion of the neotectonics of this re gion. (In Pol ish, Eng lish sum mary). Zeszyty Naukowe Uniwersytetu Miko³aja Koper-nika w Toruniu, 10, Geografia, 3: 83–108.

Rosa, B., 1968. The South Balic area dur ing the last gla ci ation and the Ho lo cene. (In Pol ish, Eng lish sum mary). Prace Geogra-ficzne Instytutu Geografii PAN, 74: 121–155.

Roszko, L., 1968. Re ces sion of last in land ice from Polands ter ri -tory. (In Pol ish, Eng lish sum mary). Prace Geograficzne Instytutu Geografii PAN, 74: 65–100.

Rotnicki, K., 1987. Paleogeografia i geomorfologia obszaru S³o-wiñskiego Parku Narodowego – stan badañ i ich perspek-tywy. (In Pol ish). In: S³owiñski Park Narodowy: Konferencja poœwiêcona XX-leciu SPN-u, S³upsk-Smo³dzino, 13-14.09. 1987, p. 18–26.

Rotnicki, K., 1994. Geo mor phol ogy and main prob lems of the Up -per Qua ter nary of the Gardno – £eba Coastal Plain. In: Rot-nicki, K. (ed.), Changes of the Pol ish Coastal Zone, POL ISH COAST’94. IGU Com mis sion on Coastal Sys tems, Sym po -sium on Changes of Coastal Zone, Gdynia, Po land, Aug. 27th - Sept. 1st, 1994, p. 75–81.

Rotnicki, K., 1999. Prob lem of the Ho lo cene trans gres sions at the Pol ish Bal tic mid dle coast in the light of new data from the Gardno-£eba Coastal Plain. (In Pol ish, Eng lish sum mary). In: Borówka, R. K. (ed.), Ewolucja geosystemów nadmorskich po³udniowego Ba³tyku. Wydawnictwo Naukowe Bogucki, Poznañ – Szczecin: 121–139.

Rotnicki, K. & Borówka, R., 1990. Nowe dane dotycz¹ce straty-grafii osadów m³odoczwartorzêdowych Niziny Gardzieñsko – £ebskiej na obszarze po³o¿onym miêdzy jeziorami Gardno i

£ebsko. (In Pol ish). Sprawozdania Komisji Geograficzno-Geologicznej Poznañskiego Towarzystwa Przyjació³ Nauk, 107: 125–128.

Sylwestrzak, J., 1961. Morfologia Rynny Raduñskiej. (In Pol ish). Zeszyty Geograficzne WSP w Gdañsku, 3: 107–116. Sylwestrzak, J., 1972. Stosunki geomorfologiczne Wysoczyzny

Kamieniecko-Sierakowskiej. (In Pol ish). Rozprawy Wydzia³u III Gdañskiego Towarzystwa Naukowego, 9: 279–300. Sylwestrzak, J., 1973. Rozwój sieci dolinnej na tle recesji l¹dolodu

w pó³nocnowschodniej czêœci Pomorza. (In Pol ish). Un pub -lished Dr. Sc. the sis, Uni ver sity of Gdañsk, Gdañsk: 1–204. Sylwestrzak, J., 1978. The de vel op ment of the val ley sys tem in

Pomorze to wards the close of the Pleis to cene. (In Pol ish, Eng lish sum mary). Ossolineum, Gdañsk: 5–161.

Szukalski, J., 1968. Zagadnienie predyspozycji pod³o¿a czwar-torzêdu w obrêbie Wzgórz Szymbarskich. (In Pol ish). Zeszyty Geograficzne WSP w Gdañsku, 10: 107–119.

Tobolski, K., 1984. Littorina trans gres sion on the Gardno-£eba Plain in the light of the dis tri bu tion of biogenic sed i ments. (In Pol ish, Eng lish sum mary). Sprawozdania Komisji Geogra-ficzno-Geologicznej Poznañskiego Towarzystwa Przyjació³ Nauk, 100: 188–191.

Tobolski, K., 1989. Bal tic Ho lo cene trans gres sions in the light of palaeo eco logi cal in ves ti ga tion of the Gardno-£eba Low land. (In Pol ish, Eng lish sum mary). Studia i Materia³y Oceanolo-giczne, 56: 257–265.

Wojciechowski, A., 1988. Littorina trans gres sion in Lake Gardno in the light of lithofacies anal y sis. (In Pol ish, Eng lish sum -mary). Sprawozdania Komisji Geograficzno-Geologicznej Poznañskiego Towarzystwa Przyjació³ Nauk, 106: 48–51. Wojciechowski, A, 1990. Lithofacies anal y sis of Gardno Lake de

-pos its. (In Pol ish, Eng lish sum mary). Wydawnictwo Nau-kowe Uniwersytetu Adama Mickiewicza, Geografia, 49: 1– 118, Poznañ.

Zaborski, B., 1933. Zarys morfologii pó³nocnych Kaszub. (In Pol -ish). Instytut Ba³tycki, Toruñ.

Znosko, J., 1998. At las tektoniczny Polski 1:500 000. (In Pol ish). Pañstwowy Instytut Geologiczny, Warszawa.