Landform Analysis, Vol. 1: 7-18 (1997)

The evolution of fluvial systems in the Upper Vistulian and Holocene in the territory of Poland

Leszek Starkel

Polish Academy ofSciences, lllstitllte ofGeography. Depllrlll1em ofGeomOlphology and Hydrology, uf. Sw. Jana 22.31-018 Krakoll'. Po/and

Abmllcl: The location of Polish temtory at the junction of a shield - platform, Hercynian and Alpine Europe creates the possibility ofstudying a great diversity in the evolution oftluvial systems. As well a~ the climatic change from pcriglacial LA to temperate. an important role was played by th~ drainage of the whole territory towards the north and by the hlocking of valleys by the advances of the Scandinavian iee sheet. Studies of the evolution of fluvial systems started at the end of the -­,H' 19th century, but detailed investigations initiated in the 1970s provided a good background for stratigraphic and paleogeographic reconstructions. In Ihe tcrritory of Poland. several WoE oriented zones of various sequences and trends of evolution have been distinguished. In the southern and middle parts ofextraglacial Poland climatic changes arc registered in the erosional and depositional sequences. These are especially well expressed in the valleys of mountain rivers whieh show changeable flood frequency and different tectonic tendencies. In the upland and lowland zones, there is a very distinct phase ofcontinental climate. In the zone oflhe last glaciation, systems of ice marginal streamways were developed in association with a lIew superimposed valley pattern, composed of transversal gaps and young, expanding fluvial systems. The pcriglacial episode was reflected in the valley floors in thc zone ofolder ice sheet advances. During the Lilorina transgression. a wide belt was submerged. but this sea level rise is not reflected in any ohvious evolution of the valley reaches upstream.

KeJ' ~Wd5: fluvial system, Upper Vistulian, Holocene

History of research

It is now over one century ago when Zar~czny (1894), Introduction Lonmicki (1903) and Friedberg (1903) recognised two various Upper Pleistocene and Holocene alluvial fills in the upper Poland occupies an area at the junctiun uf thn:e main Vistula basin and iL" lower COUI1iC. km.sch (1901) and Kei1hal;k tectonic units of the European continent: the NE part of the (1904) studied the retreat ofthe last ice sheet and the foonation Fennoscandian Shield and Russian Platform, the western of ice marginal streamways. region of Hercynian horsts and grabens and the southern, During the inter-war period the group of terraces in the Alpine zone of young mountains and foredeeps. The whole Middle Vistula valley was related to supposed ice retreat The accuracy of references in this volume is the territory slopes to the north, so the main direction ofdrainage (Lencewicz, 1927). Their number was multiplied in the gap responsibility of the authors to whom queries is tuwards the Baltic depression. This belt. less than 1000 km ufLower Vistula which was fOffiled after ice retreal from the should be addressed. . wide, was exposed to the Upper Quaternary climatic Pomeranian marginal zone (Galon, 1934, 1953). In the upper fluctu

7 L. Starkef The evofution offluviaf systems in the Upper Vistulian. ..

elaborated the concept ofthe trnnsfonnation ofriver channel profile itselfregulates the dominance oferosion upstream and overloading of ri ... ers (SlarkeL 1968). The tendency of panems from braided to meandering, as associated with aggrndation downstream. A great number oftribotaries may mountain regions to uplift and ofsubmontane depressions to envirorunental changes during the late Vistulian. also ha...e some impact on the river regime in the section subside may be renected in a trend towards erOSIon or In the19708 the numberofsites dated by radiocarbon and downstream oftheir jWlCtiOns. The length ofvarious reaches aggradation (liszkowski, 1982). In the lowland areas. the palynological methods increased rapidly. Parnllel alluvial fills facilitates the gradual smoothing of the impact originating existence of glacial rebound is difficult to prove, due to its of VislUlian age (Mamakowa & Starkel. 1974) as well as upstream; on the contrary, any disturbancedownsrream needs superposition on other isostatic !rends (Brykczyitski. 1986). Holocene age (Ralska-Jasiewiczowa & Starke1, 1975) were a long time to be transmitted upstream. docwnented. Later, several national and international projects An eust.atic (aclor(nuctualionsofthe newly fomlOO Baltic started (among them IGCP·158) which surveyed bundreds of The pre-e.risting relief(inhcrited from the previous stages SBaltic Sea was preceded by the Baltic Ice Lake. the radiocarbon and other datings which indicated that the The main drainage courses eross ...arious geomorphic level of which is considered to be more than 80 III below its stratigmphy was in need of revision and enabled extensive zones starting from the Carpathians (up to I0CKl-2500 In a.s.l.) present level. The Yoldia transgression started from ca 80 m paleogeographic reconstructions to be made (Fig. I). Among and'Sudc:ten Mts. (1:l00-1600 m a.s.!.). a submontane a.s.1. (KcSan (Szumanski, 1983), Middle Warta (Kozarski, 1991; the Tertiary and rejuvenated in the Quatemary. Excluding promoted new conditions for the development of dehas Kozarski er 01., 1988) and Prosna ... alleys (Rotnicki. 1987. vaJ Icy heads and narrower. structure- controlled gapsorgorges, (Mojski. 1990). 1991; Rotnicki & Mlynarczyk. 1989). Starkcl (1983)proroscd their floors are wide, with preJoicrved fragments of older Fig. J. Areas of detailed studies on laIc Pleistocene and a general model ofcut and fill fonnalion. Great importance Quaternary allovial as well as glacifluvial. eolian orother fills. Anthropogenic fadors, appearing in the Neolilhic Holocc:nc: fluvial systems. was placed on the widespread introduction of In the lowlands 3 zones may bedistinguished: (I)a zone Forest clearance Started in the Neolithic. first on a local I. valley rc:..c:hes sun'c:yed in det:l.ll. 2· olher localities and shoM "'llIey reaches mentioned in this summary dendrochronological (Kntpiec, 1992) and ofpre-penultimatc glaciation with extensive pcriglacial plains scale, then on a regional one (Starkel. 1990) causing changes palaeomalacologic.al dating methods (Alexandrowicz, 1987). and a well organised drainage pattern. (2) a zone ofpenultimate in the rate of overnank deposition. coarsening of sediment In the ...arious upland regions detailed studies ofthc age (Wanhe) glaciation with well developed periglacml features and finally. in the last centuries. the lransformation in the cold stage aggradation (Klimaszewsld; 1971. Starl.:c1, 1%8). ofthe terrace sequence were undertaken. emphasising the role and remains ofthe glacial order in the drainage pattern. (3) a channel pattern (KJimek & Starl.:cl. 1974; Starkel, I995c). In the Warsaw Basin. the sequence ofterrnces was associated of loess deposition (Jersak er aJ.• 1992; Snieszko.1985) and zoneofthe lasl glacianon with the valleypattern superimposed However, this is not a main subject ofthis paper. with ice retmll phases (RoZycki. 1967). Detailed surveys of climatic fluctuations during !he cold stage (Turlc:owska, 1988; on the meltout- dcpositional relieflefi after ice retreat (Fig. 2). ice marginal streamways and the VtStula system gaveevidence Superson. 1996). Regional differentiation in the e\'olution of on the age ofthe drainage evolution in Northern Poland (Galon.. In the coastal zone the role ofsea level fluctuations was Climatic changes, rt'flecled in variationsofthe hydrological 1967; Kozarski. 1962; Roszko. 1968). Falkowski (1975) in ...estigated (Mojski, 1990; Flon:k, 1991). Most results relating regime and sedimenlload flu\ial systems to the Vistulian-Holocene transition are swnmarised in the The course of climatic changes during last 30 ka IS volume related to the (GCP project 253 - Tennination of relati...ely well kno....'Il over Polish territory (Maruszczak. 1987. The combination ofthese ...arious factors caused a regional Pleistoccne (Starkel & Gl(bica, 1995; Turkowska. 1995; Manikowska, 1995). The shift from oceanic to continental differentiation in the evolution of fluvial systems which has Kozarski, 1995; Mojski, 1995, and others). climate dated about 25-20 ka BP, later well expresst:d in the been discussed several times by the Author (Starkel. 1968. extension ofpcmlafrost and acolian acti... ity between 20 and 1977,1979,1990.1994. 1995b, 1995d; Fig. 3). Areal distribution of various factors in the 15 ka BP. is especially clear. Amelioration ofclimate towards a temperature humid type was realised in three relatively abrupt Uppl'r mountain reaches , evolution of fluvial systems ,, changes ca 14.5 ka. 13.0kaand 10.0 ka BP. All these ...ariations In the mountains. the channel gradient (slope) dcpend on , show some metachronous shift in time going rrom the Sand various factors and in the mature wide Carpathian and Sudetic -' The following factors discussed below are considered in SE towards the nonh. In the wesl-east transect some differences valleys it fluctuates between 2 and 1rn6a. Thetectonictendency the evolution ofthe fluvial systems: in continentality are dctectable. expressed in two loess facies and lithology ofbedrock arc ...ery important. The aggradatJon I) the size ofcatchment and the longitudinal profile ofvalley (Jersak, 1979). as well as in the Holocene vegetation history during the cold stage, rcflected in the interfingering ofslope floors and river channels; (Ra1ska-Jasiewiczowa.1983). and flu ... ial sediment with a distinct erosional break dunng the 2) the pre..existing relief(inherited from the previous stages inlerpleniglacial is a common featw"e. This is registered by ofthe Quaternary); Thc last advance and retrcat ofthe Snndinavian ice sheet ovcrbank sediments with dated organic intercalations 3)climatic changes, reflected in variations ofthe hydrological Aboot45%of Polish territory was covered by the last ice (Klimaszewski, 1971: Starkel. 1968). In reaches which have regime and sediment load; sheet between ca 22 and 14 ka BP. River valleys wereblocked a rising tendency e.g. in the transversal gaps oflhe Dunajec 4) the last advance and retreat ofthe Scandina\'ian ice sheet; by ice. rivers were diverted from their courses and. together (Fmehlich etaf.. 1972) or Wislok (Zuchiewicz. 1987), several 5) differences in neotectonic movements; with meltwater. were flowing to the west. following ice steps were cut in alluvia and then in bedrock which reflect 6} an eustatic factor(floctuations ofthe newly fonned Baltic marginal streanlways (Galon. 1968). Together with ice melting late-glacial and Holocene phases ofincision. In the subsiding Sea); (depending on the type of deglaciation), new areas became Orawa· Nowy Targ Basin. this dissection started long before 7) anthropogenic factors, appearing in the Neolithic. free ofice and a new drainage pattern started to be organised the late Vistulian. Organic deposition started on an erosional Fig. 2. Types of river valley evolution. I - zone of prc-pcnultimale glacial ion wHh e/(tensive pcriglBeial still W1derthc periglacial climate (Kozarski. 1980, 1995). Later, step during the Oolling interstadial (Klimaszewski, 1967). features. 2 . zOne of the Walla glaciation WIth pcriglacial fealures The size ofcatchment and the longitudinal profile ofvalley this panem became reorganised during the melting of ice Peatbogs located in the abandoned channel have been and relllailU of glacial order in the drainage pattern. 3 . zOne of last noon: lllld river channels blocks and the progressive amelioration ofthc climate. recognised in the Upper San val1l=y at Tarnawa. Three distinct glaciation. superimposed valley pauern with expressed periglacial The territory of Poland is drained by two large rivers: flood phases, two in the foml ofo... c:rbank deposits during the features. 4 - zone ofyounger phase~ with ~llpcrimposcd young Vi.~lula 1 1 valley paUern. 5 - valley reaches wilh uplift lendency. 6 _valley (194424 km ) and Oder (118 861 km ). The remaining Differences ill I1coteclonic Illo,"'cments Younger Dryas and betwecn 8.7-7.8 ka fiP and the third one reaches with possible subsiding tendency. 7 . ice marginal are small ri ...ers which directly reach the Baltic Sea. In the In the evolution ofsome regions, the tectonic factor may as a submergence during early Sub-boreal have also been Slreamways (pradolinu). 8 - main sandul valleys. 9 - valley gaps great river basins there are ... arious well de...e1oped reaches. be important. During timcs ofpcriglacial climate its role was identified (Ralska·Jasiewiczowa & SWkel. 1975). aeron marginal mnes. 10 - delt:l.. 11 - area submerged during which are controlled by various factors. but the equilibrium affected by extensi...e slope degradation and seasonal LlflH'if.a lrafl$gJcl;!;ion. 12· ice marginS during various phases.

8 9 11 I L. Starkel The evolution offluvial systems in the Upper Vistulian...

Foothill reaches 28 ka BP, and 10-12 m high with a braided pattern (Mamakowa In the wide belt of the Carpathian Foothills the older & Starkel, 1974; Starkel, 1995a), deep pre-late Vistulian I. --- - Vistulian terrace is buried by the loess orsolifluction sediments incision (Klimek. 1992) and several Holocene fills .-=-:'-===:. ====- -=~ (Swke1, 1977; Lanczont, 1995) and the oldest deposil~ in the (Alexandrowicz el al., 1981). This reach shows a distinct deeply incised abandoned palacochannels are dated as AJlerOd tendency towards deepening and narrowing ofthe floodplain. , 0 =~~- . 0 • 0 YO (Mamakowa, 1962; W6jeik, 1987; Klimek. 1992). The The trend opposite to aggradation was recOb'llised in the IPo o distinction ofyoWlger fills is relatively poor, but the presence subsiding Oswil{eim Basin in the foreland of the Silesian o 0 o 0 of buried oak trunks from the last two millennia indicate a Beskid (Niedzialkowska Cl aI" 1985), 8 I o 0 0 0 0 dominant role of aggradation connected with deforestation 2) Wide valley floors (5-10 km) which have a well developed 802-AT1 S8/SA, (Starkel, 1995a; Knyliec. 1996). In the minor river catchments loess terrace, remnants ofa lower sandy level with dunes and I under several metres of loamy deposits are buried organic a f100dplain which has several fills and a distinct tendency to ?7:!:.4 kaTL sediments from the Atlantic phase or even older (er. StarkeL avulsions, As a result, wide fragments of valley floor with ,,,, 1960, 1995b), abandoned systems ofpalaeochanneis from the Younger Dryas I I I I S8-SA ) I IIII ViduLa AL (Kalicki, 1991), late Atlantic (Starkel el al., 1991) or early 11 I Submontanc basins Subboreal (Kalicki el al.. 1996) have been preserved. The 180 0 140 ::~'-1 =_~=_ _~~~r'101 ~~46r~:~~=,===_ 1• I Late Quaternary alluvial fills are generally recognised, avulsions were typical also in the earlier times, which is II. = . __ YO o,o~ '" __ but we are still searching for a deposilional representative of indicated by islands ofhigher terraces separating two younger ·0. o' · ..' ,,;;,--_~~~ •.... .,...... - the coldest phase 25-15 ka BP. The interplcniglacial terrace valley (cf. Starkel, 1990). The outlet ofthe Raba rivcr(G«bica. . • 0 0 ~".'.' ' •. \...... Y "Y""'I,,V',N.." o 0'0V-0 '0-0"', 0 0 'o'~"o' .- .. t-t-t-'f....! buried by loess (Mamakow3 & Srodon, 1977; G«bica, 1995) 1995) possessed similar landfomls. '-.....·L.~·_0-1~S4~11;~.~:~::1:>0 has also been generally recognised, two fills being dated 30 3) In case of narrower gaps, as for the Vistula reach m the o . 0 . o. ka BP (StarkeL 1995a) with late-glacial dWlCS. and then several Cracow Gate or the gap ofthe Middle Vistula across the South YOWlgcr fills, among them a distinct level with late-glacial large Polish Uplands, the river energy due to confined meandering palaeomeanders and/or a braided pattern. with several was manifested in the vertical variations. Therefore. in both generations of smaller palaeochannels and, finally. a lower valley reaches, the channel deposits represent the youngest floodplain with larger channels (ef. StarkeL 1983; Kalicki. members and, on the narrow benches, overbank deposits 13670.110 I 5170~21 lE'UIWIC E 8... 1991). The concept of phases with higher flood frequency separated by fossil soil horiwns art: preserved (cf. Rutkowski. C7~ovO~'~23:;; I llll-X"- during the Holocene responsible for the fomlation ofseveral 1987; Poiaryski & Kalicki, 1995; Fig. 3, I). - l IIII-Ih, 4 Ill. fills and channel avulsions originated in this region (Starkel, Vistula 1983, 1985); this was slightly revised after new discoveries o o (Kalicki, 1991; Starkel ct al., 1996). The following phases (after the Younger Dryas): 8.7-7.8 ka BP, 6.6-6.0, 5.5-4.9, a.s.1 4.4-4.1,3.2-3.0,2.7-2.6,2.2-1.8 ka BP; V-VI century AD, 300 m '0 X-XII and XV-XVllI century AD are distinguished there. a.I.I. sw Due to the varying width of valley floors and distance mlDD o from the mountains, sediments and foons are different and several types have been distinguished (Starke1, 1990; Starkel, co, ,,0 1995b; G~bica. 1995; Starkel et al., 1996) (Fig. 3 I and 1I). TR1 TP-2 TH-2 TH-4 '0 0 TH-' TH-3 TH4 Tf'1 TP-2 TP-O ,0/ 0 I) A sequence ofalluvial fans at the mountain front, with two distinct upper pleniglacial terraces, IS m high, younger than [11900'500, I I48llOt260 I 11Ol,QO"BO I 0/ 0 200 " 0 I 0 ...'. '921, P.C. \ ~~~,j o' / 0 60 I CO , ' =-0-1000 IV. o :ij', .. ,, o . O' ~', 0 o O' . ·~ .•_:.:o·" 0 ~.~. h' ~ " i>- ~~t?~~~~~~'';'~O?,'~'~'~O~~''~'~'~~'. ~~'t';".0,'' 0,·0·.·.',y /.,0,00 0 0 0 ~ 0 o· 0 ."""-----~ .. 0 01 0 I 0 "'1f:"70 b0 0 0 0 ~7};7#P"/7~ '" 01 0 0 ~/o 0 0 0 0 0 0 10 0 010 0 ~ 0 0 o~ 0 114390"60 1110500mO I 6360.,50

Fig. 3. Selected generalised cross-sections of river valleys in the Vistula catchment. 1- Wisloka valley at the Carpathian foreland (arter StarkcI. 1995b), 11 - Vistula valley at the Grobla forest- the western part of SoU!h-Poli~h Sandomicrz Basin (after Starkel et al., 1991), In . Vistula valley in the narrow gap across the Uplands SOOkm 400 200 100 o (after Pozaryski & Kalieki, 1995), IV - Vistula valley in the Plock Basin - upSlrcam of maximal extend of last ice sheet (after Florck el al., 1987). I- bedrock, 2 . gravels, 3 - sands and gra"cls, 4 . sands, 5 - palaeocharmel fills, 6 . overbank loams, 7 _organic sedimcnts, 8 -locss. 1"1&. 4. Longitudinal profile of the Vistula valley (Starkel, 1990). 9 - aeolian sands, 10 - fossil soil horizons, 1 _ mean river level profile, 2 - terrace levels, 3 - oulwash plains from lasl ice sheet advance, 4 - plcniglaeial terrace with late glacial dunes, S • interp1cniglaeialleTTa<:c covered by locss.

10 II L. Starl

_ LaI'IlIt", Ol "~.r _ _ OUKI_otllow _ .~, ( ... f I ,) "'"--!.L. ""b------•C-.______------( A B 1\" "-"- f---- -j l (-)...... - ~~__ s.. E' -- ...... f------7-., ,1," ...... _ ...... _ T , f------/- Am'sl \ 7' b -) : I:) --- --. --- -- \ '" • f-- 7' ---7 l'Ab '? /' 10 I tJ;N---JI~;R;-:-Ai!(lJ----:-=--=--:;;-...,..,Tr;r;4,...,..., n,r;"'l'7,",I"" cl.. lake f------.<---;T',- rf0l~az1ht~~~~U.(;~~:":~~' ;i,,~,,":,:·r~:,~.~~: I~t',..n ~. --..L ______- J 1; l,lT ,-- a I-- _/L..,...__ ~~'I'I 1'1 fi4i II I'~ f I fffi IIII IT f l:::Ii1-r8~:~,(j1T 111 : II ,",'1'1" ~ ~J,l! r~j,y.W.M*,~iT \1~ II J I J J I 1 I r 1 IEI I 1 r 11 IIIJI1IIIIII J I I J 1 I I 11 1 1 J.Lt ~t\'\ " . II,II J r J I J 1 , Pt IIIIIII ! IIIII J I J t IrIIIII1III r:--=- Fig. 6. Two ways of "expanding" river valleys in the 7,.onc orlasl deglacialion (afler 20 ka DP). ...~ IIII J I J t IIIII J JIIII)I t IJII I 1 r I t t I 1 1 I ! III J ).:; ,. ~ I 1 r I I ! II I('~ IIIIIIIIIII t I1III1IIIII j I::=~ w' A - Expanding downstream (e.g. Vislula. Odcr); a - growing length in time (later transgression), b . expansion of fioodplain ' .. \1 II I1 III IJ' '~J I I.,L!.J IIIIII 11 I 1 I II 1~.lJfu~<:".' lea Iha.1 controlled from upstream, 20 jl\ilrJI 1(')1 1' '111(. "b'-:--)l1111 11»""""---= B - Tributary valleys expanding "upstream". conlrollcd by low base level: c, . backward growth of river in zone ofolder phases, ',' Iyl IIUJI\,;;llx~"",11111111''':':'>:-' \..",~,~~ pha.~e. '..11 J 11I1I (1"'11 t J II1 J J 1111 J 111";·:....:..:'.' ~~~~~~~~\\,,\'" ell " backward growlh in zone of Pomcl3nian d, • fonnatiun of uniform floodplain in zone of older phases, dll - formation '. '.~ IIIIIIIII I I I I t J JII t I III ! J J IIII t-r-: '\U)~~\l1 of tloodplain in the 7.one ofthe Pomeranian phase. :- >, IIIIII I IIII1IIrIrII I I t J I J I I J 1 I r 1 :::::::~:~.~ULlLLUJ.llllUJllJ}})< After a slight aggradation during the Younger Drya.... distinct The large transit ,'alley of the Vistula river :::::::::: :A:b::::::::::::::::::.:::::::::.':::':::::::::::::::::::::'::. episodes of higher nuvial activity about 8.5. 5.5 - 4.5 and Following the ice retreat. the water ofall ri"ers draining 3.5 - 3.0 ka BP were recorded (Turkowska. 1988: the southern periglacial zone as well as that accumulated in Kaminski, 1993). Ihe ice dammed lakes (Warsaw Basin) fonned the gaps across the marginal zones and, step by step extended Iheir eourses Ice marginaJ streamways - underfit streams towards the Baltic depression (Fig. 2). In several transverse In northern Poland a system of ice marginal streamways reaehes systems ofterraces are found. up to 10-12 in number, fo"ig. S. E~olUlion ~f tbe. ViSlula valley In longitudinal profile during last 30 ka (after Slarkel. 1990. modified). (prndolinas) de,-e1ped, following the three main phases ofthe whieh reflect this pronounced incision (Galon, 1934), Several I • erosIon by bra,ded nver (Eb). 2 . aggnodauon by braided nver (Ab), 3 " CIl)5ion by mcandcnng nvcr . large mcandel1 (Em(I)). 4 _erosion ice retreat (Galon, 1967. 1968). After detailed studies in Wcst authors have made effons 10 correlate these steps along the wllh iOmc a~tlon by anastomosing or 51111ight river (E>Aa). 5 • accumulation eIther by mundenng river" small meanders (Am(s» or by Poland se"eral new phases were recognised (Kozaniki. 1988). Lower VlStuJaand tributaries (Galon. 1967), but only !hedating an an;Lnomosl~g onc (A>E.). 6. dclllle deposil$ (Ad). 7· ice dammed lake. 8" sea. 9· iee shCCl (modified after KOUBki 1995). 10" fonnel The existence ofonly one streamway in the east is a common and correlation of the 3-4 lowest ones has proved possible oulf1ow dlrecllOns (westward along pradohna.s and south....ard over out....uh plains). 11 "retreal orpcrmafrOSI. 12 " lum of deposition during nood phase. 13 - ehannel avulSion. feature; in the west. their "avulsions" developed due to fast (Rosz.k6wna, 1968; Drozdowskl & Ikrglund. 1976; Tomczak. retreat fium the marginal zones ofLesmo(20 ka BP), Poznan 1987). As concluded by Wisniewski (1982. 1987; also see The South-Polish Uplands river pattern may be distinguished, The first are easily (18.5 ka), Chodziez (17,2 ka). Pomcrnnian (15.2 ka) and Slarkcl. 1990), the correlation of higher terrnce levels based Most ofthe upland nvers drain directly eitherto the Vistula recognised in the Warsaw Basin, where the staircase of terraces Gardno(l3.2 ka) ( Kozarski. 1988), Some p.-rrtsofthese wide on altitude is useless because these levels are nll associated orlhe Oder, llteirwidlh diftcrs. according to their glacial hisrry was earlier associated with thc retreat phases of the last floors were gradunlly dissected (as in the case of Toruit ­ with transfonnations ofdlfTerent reaches during deglaciahon and tectonic tendencies. and Iheir pregl:lcial floors may be Seandinavian ice sheet (R6iycki, 1967). then with lateglacial Ebcrswalde pradolina; K07.arski. 1962) and sOJnetilnes bccUlllC (Fig. 4). buried to several decametres below the present river(Gilewska. climatic oscillations (Baranieda & KOllecka-Betley. 1987) active up to the Balling (like the Warta south of Poznan ­ In the lowest course, incision probnbly continued unlil 1972; Maruszczak. 1972). In areas built from chalk and with and later the pre-Epc (>14.5 ka BP) erosion downstn:am of Kozarski et al.. 19R8). Thennokarst probably played a the beginning ofthe Holocene, when the low water level of a thick loess mantle, complex fluvio-deluvial-colluvial bodies Warsaw was documented by ovcrbank deposits underlying considerable role in their lateral development. This was the Yoldia Sea stnrted to rise from - 80 metres. Fluvial deposits dat<..'d either 10 inlerpleniglacial (Harasimiuk. 1991) or to the the dunes on lhe rust overflood terrace which have been dated assumed by Jahn (1975) and later supponed by Kozarski ofearly Holocene age are recorded below the Vistula delta kalaglaciai phaseoflhe upp<..'I"plenigiacial (Jersak.. 1976: Jersak at 145 ka BP (Manikowska, 1985), (1995) and his team (Antczak. 1986) afier discovery of ice (Mojsh. 1990). The construction ofthe Vistula delta started et aJ.. 1992; Superson, 1996) are very conunon. In the valleys In the Prosna valley, ROlnicki (1987) recognised the wedge casts and frost cracks connected with expansion of from 7 ka BP jointly with the Litorina transgression. The with thick reservoirs ofglacifluviai sands their reworking under dissection ofthe higher terrace (with radiocarbon dates between pennafrost over the deglacialed areas south of the limits of Holocene evolution ofthe Lower Visrula valley is controlled pcnnalToSl condilions was very active and extensive sandy 28 and 26 ka BP) which preceded an erosional phase which the Pomeranian phase. Later. these floors were overgrown by more and more by the hydrological regime of the upper and fills are observed in their lower reaches (kn.ak & Sendobry. coincided with the maximum ofthe glacial advance and then peat. The peat accumulation started in the AllerOd and totally middle pan of the basin, This means that the phases of 1991; Buraczyilski. 1994). The late VlStulianorearly H010cene aggradation about 18.5 ka BP. During the laiC Vistulian up to fossilised the floorofthe Biebrza pradolina nearthe iDlerfluve Subboreal and Suballanic aggradation and channel organic deposilS ID the valley floors indicate earlier intensive the Younger Dryas. the Prosna created large palaeomeanders. between the VlStula and the Niemcn Basin (:lurek. 1975), This abandonment are synchronous with those identified in the erosion (Snieszko & Dwucet. 1995). This was followed by which indicate a 5-fold increase in bankful discharge (Rolnickl pan represents a classical undcrfit stream. The shon-lived Subcarpathian Basins (Florek et al.. 1987: Tomczak, 1987; Holocene aggradation. which accelerated after forest & Mtynarczyk. 1989). During the I-Iolocene lateral migration. narrow pradolinas drained at present by the Zglowil\czka and Starkcl. 1990). clearances (Snieszko, 1985). several generations ofsmaller meanders were created. Bachorza streams at the Vistula - Warta interfluve have asimilar Detailed studies of the divergence of the Middle Wana A slightly different picture is obscn'ed in the limestone In the smaller valleys ofthe l6di. region. the role ofthe character(AndrLCjewski. 1995; Wisniewski, 1982). valley (to the west ofthe pradolina, nonh ofthe Powan gap) areas Where, after the lale Vistulian. erosion followed a1 many Vistulian valley formation depends on the nature of New dating.-; from the Baltic Sea floor (cC. Mojski. 1995) have shown that the transformalion from braiding to localities. The deposition ofcalcareous tufa was interrupted transfonnation ofme previous river pattern fonned after the and the Gardno pha.'iC (Rotnicki & Borowka. 1994) indicate meandering followed in the early BOiling stage. and the next during phases with frequent flood episodes (Rutkowski. 1991; retreat ofthe Warta ice sheet. Many closed depressions were that the age of thc marginal zones must be increased and change towards small meanders and a narrowing of the P~uretal., 1988; Alexandrowicz. 1988). incorporated into the unifonn valley system (Klatkowa. 1989). K07.arski (1995), in his last paper. accepts the age of the floodplain coincided with lotal reforestation at the beginning DClailed studies ofpcriglacial scdiment have shown that, after Chodziei phase as being about 17.7 ka. older then 16 kn for ofthe Holocene (Kozarski er al.. 1988; Kozarski. 1991), But The Lowland periglacial zone (extraglacial) the post-interpleniglacial aggr-J.dation, a phase ofstrong aeolinn the Pomcranian phase nnd about 14.5 ka BP for the Gardno even here in a lowland valley, the formation of abandoned This zone, 100-250km wide, was glaciated in its nonhcm activity followed with the fomlation ofa gravel pavement and, phase. The most northern pradolinaofBollingor AllerOd nge meanders coincided with wet phases before 8, 4 and pan during the penultimate Warta advance, In this zone, large later, during the late Vistulian, deposition tumed to erosion is submerged under the Baltic Sca (Mojski, 1990). ca 2.5 ka BP, It'ansit valleys (Vistula, Bug, Oder, Warta, Prosna) and smaller again (Manikowska, 1985, 1995; Twkowska, 1988, 1995).

12 13 L. Starkef The evolution offluvial systems in the Upper Vistutian. ..

The tributaries of V"tstula river in northern Poland periods ofboth increased erosion. a straightening ofchannel the Laleglacial and Holocene. Fa/ia Quaternaria 53: G~bica. P., 1995: Evolution ofthe VlStula valley and alluvial In their evolution. tribulary valleys show a close as well as of aggradalion (Starkel, 1983, 1995d). The 191 pp. fans ofthe Raba and Uszwica rivers between UScie Solne association with the main valley. Therefore. the incision during transitional phase of reorientarion of the fluvial system Andrzcjewski. L., 1994: Ewolucja systcmu fluwialnego doliny and Szczurowa m the Vistulian and Holocene. the deglaciation fluctuated between 20 and 50 metres (Galon. combined with revegetation is reflected in erosion combined dolnej Wisty w p6inym vistulianie i holocenie na Geographical Studies, Special Issue 8: 31·50. 1953: Niewiarowski. 1968). A detailed study of several with a transfonnation ofthe braided panem 10 a meandering podstawie wybranych dolin i jej doptyw6w. Rozpruwy Gilewska, S., 1972: Wyiyny SI'lsko-Malopolskie. In: M. Iributaries by Andrzejewski (1994) has shown various one with a transitional phase of large meanders (Szumanskl, Uniwer:rytetu Mikolaja Kopemika. Torun: 1·112. Klimaszewski (Ed.) Geomorfologia Polski. t. I. mechanisms ofevolution which relate 10 the previous origin 1983: Ko~ki et al., 1988: Starkel, 1990; Vanderberghe et al., Antczak. B.. 1986: Channel pattern conversion and cessation PWN: 232·339. of valley segmenlS (sandur plain, ice marginal streamways, 1994· Fig. 5). of the Warta river bifurcation in the Warsaw-Berlin Harasimiuk, M.. 1991: Vistulian glacial cycle of the fluvial subglacial strcamways), which laterwere incorporated in one As concluded by Falkowski (1975) the best conditions pradolina and the southern Poznan gap section during the processes development in the valley ofthe Middle Wieprz system. In scveral valleys with a low gradient, even the late for studying the chain ofchanges are those in the middle valley Late Vistulian. Seria geografia. Uniwersytet Adama River (SE Poland). Annales Uniwersyte/u M. Curie· Vistulian transitional phase, with ilS large palaeomeanders. segment which has reached a stage of maturity with free Mickiewicza, Poznan. 35: I-Ill. Sklodoll'skiej sec. B. 46 (5). Lublin: 81·l()9. registered. meandering. In young fluvial systems these changes are not Baraniecka. M.D. & Konecka·Betley. K.. 1987: Fluvial Jahn. A.. 1957: Przyczynki do znajomoSci tems karpackich. In me evolution of these vallcys. lheir fir.>1 phases of synchronous in the whole longitudinal profile. But, to some sediments of the Vistulian and Holocene in the Warsaw Czasopismo Geografic=ne 28 (I): 171·185. tmnsfonnation jusl after the deglaciation are very important extent, the reaction to climalic change in a unifonn landscape Basin. In: L Stadel fEd) Evolution orthe Vistula river Jahn. A., 1975: Problems ofthe Periglacial Zone. PWN. Under a cold pcriglacial climate in the southern part of the may be synchronous in the valleys of various orders. This is valley during the last 15000 years, voL U., Geographical Warszawa: 186 pp. Pomeranian marginal mne. winter freezing was combined with probably trueofthe Lublin Plateau. where episodes oferosion Studie5. Spec. Issue 4. Warsaw: 151·189. Jent7SCh. A., 1901: Er/atenmgell :urgeologischen Karte Blau the formation oficings which were recorded on the outwash and aggradation during the last cold stage were simultaneous Brykczyilski, M., 1986: 0 g10wnych kierunkach rozwoju sieci Grauden:. Berlin. plain in the shape oforienled depressions (Kozarski. 1975). (Superson,I996). rzecmej Niw Polskiego w czwartorz~ie. Pneglqd Jersak. J., 1973: Litologia i strarygrafia lessu Wyiyn The melLing of dead·ice blocks conlinued unlil the AllerOd Polish territory provides a good opportunity for studying Geograficzny 48 (3): 411-440. Pofudniowej Polski. Acta Geographica Lodziensia 32. period when most of Ihe lakes were fonned. especially in the impact ofice sheet advances and retreats on the foonation Buraczyitski. J.. 1994: Zmiennosc procesOw eolicznych na L6di: 139 pp. subglacial channels (cf. Kozar.>ki, 1995). Many of the small and evolution of fluvial systems (Rotnicki, 1987; Starkel, Roztoczu i w Kotlinie Sandomicrskiej podczas pieak. J.. 1976: Zwi'\zek akumulacji lessu z rozwojem lakes are still not fully incorporated imo the fluvial system. I995d). But the reliefconfiguration and type ofsubstrate create Wisty. Annales UniIVersytetll M. Cllrie-Sklodowskiej. procesow rzecznych w dolinach przcdpola Karpat i na The larger ones, those located in subglacial depressions and condtions different from those described from Canada (Teller. sec. B.49. 4: 51-79. wyiynach poludniowej Polski. Acta GeograplJica draining to the pradolinas. show a tendency to overgrowth by 1995) or Finland (Koutaniemi. 1991; Mansikkaniemi. 1991). Drozdowski. E. & Berglund. 8.E.• 1976: Development and Lodziensia 37: 25·52. peat (Niewiarowski. 1994). In the whole Poland, two types ofevolution ofthe river valleys chronology of the lower Vistula Rivcr valley. Nonh Jersak, J. & Sendobry, K.. 1991: VlStu/ian deposits in the mlley are present: the expanding downstream and the expanding Poland. Borea:." 5: 95·107. of/he Bierall'ka in Kotlamia. Ill: 1 Jersak (Ed.) Le.fS I The river valleys in the coastal zone upstream (Fig. 6). Also the underfit streams overtheprndolinas Falkowski. E., 1975: Variability of channel processes of osaJy dolinne. Uniwersytet SI'lSki, Katowice: 93-118. In this belt, which isoplo lOOIcrn wide. and which drains and sandurplains are very typical in this area. lowland rivers in Poland and changes ofthe valley floors Jeryk,J., Sendobry. K... & Snieszko, Z., 1992: Postwarciailska 10 the Baltic Sea. all valley patterns are superimposed on the The Vistula and Oder are examples of the expanding during the Holccne. BiuteO'1l Geo/ogiczny Uniwers)'letu ewolucja wyZyn lessowych w Polsce. Prace Nauleowf' meltout dcpositional reliefcreated during the deglaciation of downstream valleys. Their length and gradient increased with II'ruszow.fhego 19, Warszawa: 45-78. Uniwers)'/em Slqskiego 1227. Katowice: 195 pp. the Pomeranian and Gardno phases belWeen 16 and 14 BP. progressive deglaciation. But also with time the floodplain Florek, W, 1988: The Slupia valley in the vicinity ofSlupsk Kalicki. T.. 1991: The evolution of the Vistula river valley Most of the valleys are composed of fragments of different fanned unifonnly in all upstream sections. It developed like a towards the close of the Vistulian and in the Holoccne. between Cracow and Niepolomice in Late Vistulian and genesis including various meltout depressions, e.g. the Radunia carpet being unrolled downstream. Such a floodplain is under Geographia Polonica 53: 67·84. Holocene times. Geogmphical Stu.dies. Spec. Issue 6, valley nearGdailsk (Koutaniemi and Rachocki. 1981). A very the control offlood waves originating in mountain headwaters Florek. W. 1991: Pas/glacjalll)' 1"0:11'0} do/in nek.flYKlkowej WafS7,.3Wa: J 1·37. low base level during the late Vistulian and early Holocene and ofsediment waves from the deforested foothills and locss CIf.ici po/lwcnego sklollll Pall/ana. Wyi:sza Szkola Kalicki. T.. Starkel. L.. Sal". 1, Soja. R. & Zernickaya. v.P.. created Ihe conditions for erosional advances upstream but plateau. Pedagogiczna. Slupsk: 142 pp. 1996: Subborcal paleochannel system in the Vistula valley various types of lithology and influence of transfluent lakes The converse direction ofevolution may be observed in Florek, E.. Florek. W. & Myciclska·Dowgiallo. E.. 1987: near Zabierz6w Bochenski (Sandomierz Basin). fanned barriers to the small river.>. Studies ofseveral ofthcse the tributary valleys draining the ice·free areas. The Morphogenesis ofthe Vistula valley between Kwa Polska GeographicalSllIdies. Special1ssue 9. Wroclaw: 129-158. rivers by Florek (1988. 1991) has shown that. in their lower "backward" evolution. connected with the lowered base level. and Plock in the Late Glacial and Holocene.ln: L. Starkel Kaminski. M. Unpublished: Poinog/acjallla ; holocenska courses. these river reached the stage of floodplain maturity is realised by the expansion of the river catchment, incision (Ed.) Evolution ofthe Vislula river valley during the last tralLifonnacja doliny Mos=c=enicy jako re::ultOl :mian and the fIrst meandering patterns are recorded from ca 8 ka and. of sections in between. by aggradation. The rate of 15000 years. \'01.11, GeographicalStudies. Spec. Issue 4, srodowiska namralnego oraz dzialalnosci alowleka. BP. The impact of the Baltic transgression. earlier estimated adaptation depends on riVeT discharge and the duration of Warsaw: 189-205. Ph.D. thesis. Dep!. ofGeography.lOd.: Universily, 1993. as a very imponant factor (Rosa. 1964). appeared to be incorporation into the new system. 1l1erefore. the matun::: river Friedberg, W. 1903: Alias Geologiczn)' Galicjl. objaitlienia Keilhack, K.. 1904: Die grosse baltische Endmorane un

14 15 L. Starkef The evolution offluvial systems in the Upper Vistulian...

Klimaszewski. M., 1971: The effect ofsolifluction processes Liszkowski. J., 1982: Geneza pola wsp6kzesnych piooowych I)oi:aryski. W & Kalicki, T., 1995: Evolution ofthe gap section Starkel, L., 1983: The reflection of hydrologic changesin the on the development of mountain slopes in the Beskidy I\IchOw skorupy ziem.s.kiej na obsune Polski. Razprawy of the Vistula valley in the lale glacial and Holocene. fluvial environment ofthc tempernle zone during !he last (Flysch Carpathian). Folia Quoreman'a 38: 1-32. Uniwers)'tetu WClI'n"awsbego 174: 1·179. Geographical Studies, Special Issue 8: 11-137. 15000 years. /11: K. J. Gregory, J. Wiley (Eds.) Klimek, K., 1992: The age oftransformation ofsubcaJpathian Lanczo!, M., 1995: Warunki paleogeograficme akumulacji fWska-Jasiewiczowa, M., 1983: lsopolen maps for Poland: Background to Palaeohydrology: 213-234. river channel pattern during Late Vistulian, Papers and oraz stratygraficzne znJZnicowanie utwor6w lessowyeh 0-11000 yean> BP. Ne'M' Phytologist 94: 133-175. Starke1. L, 1985: The reflection of the Holocc:ne climatic Abstracts of Papers. Symposium on Global Conrinental we wschodniej ~i Pog6rza Karpackiego. Wydzial Ralska-Ja..iewiczowa. M. & Starkel, L., 1975: The basic variations in the slope and fluvial deposits and forms in Paleohydrology, Krnkow and Mogilany: 3 p. Biologii i Nauk 0 Ziemi UMCS. Lublin. Rozprawy problems of palat.'Ogcogmphy of the Holocenc in the the European mountains. Ecologia Medirerranea 11: KJimek, K. & StaTkel, L, 1974: History and actual tendency habilitacyjne 50: 126 pp. Polish Carpathians. Biuleryn Geologiczny Unill'ersytetu 91-97. of noodplain development al the border of the Polish Lomnicki.A. M., 1903: Atlar GeologicznyGalicji, objainienia WrocIawskiego 19. Warszwa: 2744. StarkeL L (Ed.) 1990: Evolution of the Vistula river "alley Carpathians, Nachrichren Akademie der Goltingen. Ill: do z. 15. Akademia Umiej,,-tnoSci, Krnk6w, 68 pp. Rosa, B., 1964: 0 ulworach aluwialnych i biogenicznych during the last 15000 years vol. rn. Synthesis, Prace Rep. ofComm. on present-day processes. IGU: 185-1 %. Mamakowa, K., 1962: RoSlinnoU kotliny Sandomierskiej w wyScielajllcych dna dolin rak nadbattyckich, ich zwi:tZki Geograficzne IGiPZ PAN. Special Issue 5, Koutaniemi. L., 1991: Glacio-isostatically adjusted p6...:rtym glacjale i holocenie. Acta Palaeobotanica 3 (2): ztransgresjll morz.'1 i znaczenie dla badaJl. nad neotekloniq Warsaw. 220 pp. palaeohydrology. the rivers lvalojoki and Oulankajoki, I-57. obszaru. Zeszyty Nmlkoll'e Uniwersytew Mikolaja Starke\, L. 1994: Reflection oflhe glacial-interglacial cycle Northern Finland. In: L. Starkel. K. J Gregory, J B. Mamakowa, K. & SrodOll, A., 1977: 0 plcniglacjalnej norze Kopernika. Geograjia 10, Tonlll: 125 pp. in the evolution ofthe Vistula river basin, Poland. Terra Thomes & J Wiley (Etu.) Temperare Paleohydmlogy: z Nowej Huty i osadach czwartorz~du doliny Wisly pod Roszko, L., 1968: Z historii rozwoju doliny dolnej Wisly. Folia Nova 6: 1-9. 65-78. Krakowem. Roczllik Pol.l'kiego Towarzystll'a Quaternaria 29: 97-108. Starkel, L., 1995a: New data on the Late Vistulian and Koulaniemi. L. & Rachocki. A .• 1981: Palaeohydrology and Geologiczl1ego 47: 4. Rotnicki, K., 1987: Main phases oferosion and accumulation Holocene evolution of the Wisloka valley ncar Dl;bica. landscape development in the middle course of Ihe Mamakowa. K. & Starkel. L.. 1974: New data aboul theprofile in the middle and lower Prosna valley in the last glacial· Geographical Smdies. Special Issue 8: 73-90. Radunia basin. North Poland. Fennia 1959.2.335-342. of Young Quaternary deposits at Brzeinica in Wisloka interglacial cycle. Geographia Polollica 53. Warszawa: Starkel. L, 1995b: Evolution of the Carpathian valleys and Kozarski, S.. 1962: Rccesja oSlatniego I~dolodu z pOInocnej valley, Sandomierz Basin. Studio Geomorphologica 53-65. the Forccarpathian Basins in Ihe Vistulian and Holocene. cz~i Wysoczyzny Gnie-~ienskiej a ksztaltowanie sic:: C(IIpatho-Balca"ica 8: 47-59. Rotnicki. K.• 1991: RelrodiClion of palaeodischarges of Stl/dia GeomOlphologica Carpatho--Balcanica 29: 5-40. Pradoliny NOleci - Warty. Poznanskie Towarzyslwo Manikowska, 8., 1985: 0 glebach kopalnyeh. stratygrnfii i meandering and sinous alluvial rivers and its Starkel. L., 1995c: Odbicie ekstremalnych wezbrnn okresu Przyjaciol Nauk. Prace Komisji Geograficzno­ litologii wydm Polski srodkowej. Acta Geographica palaeohydroclimatie implications. In: L. Starkd. KJ. historyczncgo w osadach rl.ecznych i stokowych w GeoIogic:.nej (2, 3): 1-154. Loddensia 52. LOdi: 1-137. Gregory, J.B. Thomes & J Wiley (Eds.) Tempe/'Ute dorzcczu gomej \Visly. Acta Uni\'ersitaris N. Copernici, K07.atSki, S., 1975: Oriented kenle holes in outwash plains. Manikowska. B. (Ed). 1995: The Pleislocene - Holocene Palaeohydrology: 431-471. Geograjia 27: 13-20. Quantionn Geographicae 2: 99-112. transition (20-8 ka BP) in the area of Poland. Biuletyn Rotnicki, K. & Bor6wka. R.K.. 1994: Slraligraphy. Starkel. L. 1995d: Palaeohydrology ofthe Temperate zone. Kozarski, S., 1980: An outline of Vislulian stratigrnphy and Peryglacjalny 34. palaeogeography and rl.1ting ofthe North Polish Stage in In_' KJ. Gregory, L Starkel. V.R. Baker & J Wiley (Eds.) chronology of the Great Polish Lowland. Quaternary Mansikkaniemi. H.. 1991: Development of river valleys the Gardno-leba Coastal Plan. In: K. Rotnicki (Ed.) Global Continental Palaeohydrology: 233-257. $ll/dies in Poland 2: 21-35. originated by emergence, S-Finland. Case study of the Changes olthe Polish Coastal Zone. Adam Mickiewicz Starkd, L & G~bica. P., 1995: Evolution of river valleys in Kozarski, S., 1983: River channel chang.:s in the middle reach river Kyronjoki. In: L Starkd. K.J Gregory,J. B. ~ University, Poznan: 84-88. Southern Poland during the Pleistocene-Holocene ofthe Warta valley. Great Poland Lowland. Quaternary & J \Viley (Edr.) Temperate Palaeohydrology; 79-104. Rotnicki. K. & Mlynarczyk. Z., 1989: Late Vistulian and transition. Billlel)'" Peryglacjalny 34: 177-190. Smdies in Poland 4: 159-169. Maruszczak. H., 1972: \Vyi:yny Lubtlsko-Wolyilskie. III M. Holocene channel fonus and deposits of the Middle Starkel, L, G,,-bica, P., Niedzialkowska, E. & Podg6rska­ Kozarski, S., 1988: Time and dynamicsofthe last Scandinavian Klimaszewski (Ed.) Geomorlologia Polski. t. I. rWN: Prosna rivcr and their palcohydrological interpretation. Tkacz. A., 1991: Evolution ofboth the Vistula floodplain ice-sheet retreat from northwestern Poland. Geographitl 340-384. Uniwersyt~t Aroma Mickicwicza. Seria Geographica 43: and laleglacial • early Holocene palaeochannel systems Polonica 55: 91-1Ol. Manlszczak, H.. 1987: Loesses in Poland, their strntigraphy 1-76. in Ihe Grobla Forest (Sandomierz Basin). I,,: L. Slarkel Kozarski, S.. 1991: WaI1a - a case study of a lowland river. and paleogeographical interpretation. AIIIUlle~' Rotnicki. K. & Starkel, L., 1991: Ewolucja den dolin. (Ed.) Evolution ofthe Vistula river during the last 15000 In: L. Starkel. K. J. Gregory, J. B. Thorne... & J_ Wiley UniwersylefU M. Cllrie-SklodolVskie 41 (2) sec. B, Lublin In: L. Starkel (Ed.) Geograjia Po/ski, sl'odoll'isko years, part IV. Geographical StlIdies. Spec. Issue 6: 87-99. (Eds.) Temperate PalaeolJ)'(Jrology: 189-215. 1986: 15-54. pr::yrodnicze, PWN. Warszawa: 151-159. Starkel, L.. Kalicki, T., Knwicc. M., Soja, R., G,,-bica, P. & K07..arski. S., 1995: The periglacial impact on the deglaciated Mojski, J E. 1990: The \fistula delta. in: Evolution of the Rozycki. S.Z., 1967: Plejstocen Polski srodkowej na tie Czyi:owska E., 1996: Hydrolohtical changes ofvalley noor area of noI1hem Poland afler 20 kyr BP. Biulety" Vistula river valley during the lasl 15000 years. przeszloSci w g6rnYll1 trzcciorzl.-dzie. nle Pleistocelle Iy· in the upper ViSlula Basin during LaIc Vistulian and Peryglacjalny 34: 73-102. Geographical Stl/dies Ill, Special Issue. 5: 126-14I. Middle Polalld. PWN. Warszawa: 251 pp. Holoccne. Geographical SlIIdies, Special Issue 9: 7·128. K07.atSki. $., Gonern, P. & Antczak. 8., 1988: Valley floor Mojski. J L 1995: An outline ofthe evolution ofthe Southern Rutkowski, J., 1987: ViSlula river valley in the Cmcow Gate Superson, J.. 1996: Funkcjonowanie systcmu Ouwialnego developmenl and paleohydrological changes: The Late Baltic area al the end ofthe last glaciation and beginning during the Holocene, Ill: Evolulion of the Vistula river wyzynnej cZ~Sci dorzecza Wicprza w zlodowaceniu Vistulian and Holocene history of the Warta River ofthe Holocene. Billleryn Per)'glacjalny 34: 167-176. valley during the lObi 15000 years vol. 11. Geographical \\rtsly. Wydzial Biologii i Nauk 0 Ziemi UMCS, Lublin, (Poland). In: G. Lang& Ch. Schliichter(Edr.)Loke. Mire Niedzialkowska, E., Gilot. E., Pazdur. M. & Szczcpanek, K. Studies, Speciallssue 4. Warsaw: 31-50. Rozpra"y habilitacyjlle 53: 1-280. and Ri\Y!:r Environment. Balkcrna: 185-203. 1985: 1be evolution of the Upper Vistula valley in ~ Rutkowski. J.• 1991: Holocen doliny dolnej Raclawki. SzumaJi.ski, A., 1983: Paleochannels oflarge meanders in the K.r;wiec, M., 1992: Skale dendrochronologiczne pci..~ego region ofDrogomySl in the upper Vislulian and Holocene. GeoIogio 17, 1-2. Wydawnictwo AGH: 173-190. river valleys ofthe Polish Lowland. Quaternary Studies holoeenu poIudniowej i cenualnej Polski. Kwartalnik Folia Quaternaria 56: 101-132. Starkel, L, 1960: Rozwoj rze.."y PoLskich Karpal fliszowych in Poland 4: 207·216. AGH, Geologia 18.3: 37·119. Niewiarowski. W.• 1968: Morfologia i rozwoj prndoliny i w holocenie. Prace Geograficzne InstytlllU Geograjii Snieszko, Z., 1985: Paleogeografia holoccnu w dolinie Knwiec. M., 1996: Dendrochronology of"black oaks" from doliny Drw~y. Smdia Societatis Scientiarum Tonmensis PAN. 22: 1·239. Sancygni6wki. Acta Geographica Lodziensia 51: I-lOO. river valleys in Southern Poland. Ill: Hydrological changes 6(6).scc.C: 118 pp. Starkel, L.. 1968: Remarques sur retagernent des processes Snieszko, Z. & Dwucet. K., 1995: Theevolution ofloess covers ofVistula valley floor in the upper Vistulian and Holocene. Niewiarowski, w., 1994: Palaeohydrological changes during morphogenetiques dans Carpates au cours de la demiers in Poland between 20 and 8 ka BP. BiuletYIl Pelyglacjalny Geographical Stl/die.f, Spec. Issue 9. 61-78. the Vistulian and Holocene in Southern pan of Znin glaciation. Billlet)'1l Peryglacja/ny 17: 205-220. 34: 191-208. Laskowska-WysoczaiLska, w., 1971: Stralygrafia i subglacial channel, the Biskupin region. Qllaternary Starkel, L. 1977: Last Glacial and Holocene fluvial chronology Teller, J. T., 1995: The impact of large sheets on continental paleogoomorfologia ezwaI1or7.~du Niziny Sandomierskiej Studies in Poland 12: 59-72. in the Carpalhian valleys. Stlldia Geomorphologica palaeohydrology. Ill: K.J. Gregory, L. Starkel. i Prl.cdg6rza Karpat regionu rzeszowskiego. Studia Pazdur, A., Pazdur. M.F., Starkel, L & Szulc, J, 1988: Stable CarpatllO-Blllcaflica I I: 33·51. V.R. Baker & J. Wiley (Eds.) Global COllli1J(mtal Geolugiw Polollica 34, 1-109. isotopes ofthe Holoccnc calcareous tufla in S-Poland as Starkel, L., 1979: Typology of river valleys in the temperate Palaeohydrology: 109-129. Lencewicz, S., 1927: Glaciation et morphologic du bassin de paleoclimatic indicators. QllalCrllary Research 30, 2: zone during the last 15000 years. Acta U"iver.~ilati.\· la Vistula moyenne. Prace Pmi.ftwowego Instytulll 177-189. Oll/uen~isA, 82, Geologia 3: 9-18. Geo/ogicznego 2: 2.

16 17 L Starkel

Tomczak. A.. 1987: 1be evolution ofthe Vistula valley in the 15000 years. in: Geographical Studies, IGiPZ PAN. Landform Analysis, Vol. 1: 19-31 (1997) Torun Basin in the Lale Glacial and Holocene. Special Issue I, Warsaw: 93-107. In: Evolution of the Vistula river during the last Wisniewski. E., 1987: The evolution ofthe Vistula river valley 15000 years, voJ. 11. Geographical Studies, Special between Warsaw and Plock Basins during the last 15000 Issue 4: 207-231. years, In: Evolution ofthe Vistula river valley during the Turkowska, K., 1988: Rozw6j dolin rzecznych na Wyiynie last 15000 years, vo!. 11. Geographical Stlfdies, Special L6dzkiej w czwartOIz~dzie, Acta Geographica /..odzien.ria Issue 4, Warsaw: 171-187. 57.132 pp. W6jcik, A .• 1987: Lateglacial lacustrine sediments from Sources of material supply and nature of fluvial transport in Turkowska. K., 1995: Recognilion ofvalley evolution during Roztoki and Tamowiec near JasJo. Acta Palaeobotanica the Pleistocene-Holocene lnlnsition in non-glacialed 27 (I): 27-41. post-glacial agricultural-forested catchment regions of the Polish Lowland. Biulet)'n Peryglacjalny Zarc;.czny, 5.. 1894: Objasnienia do arkusza Krak6w 34: 209-227. Pars~ta i Chrzan6w. Atla.f GeologiC2ny Galicji3. Krak6w: 1-290. (the upper river, Poland) Vanderberghe,J., Kasse, c., Bohncke, 5, & Kozarski. 5., 1994: Zuchiewicz. W" 1987: Evolution ofthe eastern Beskid Niski Climate - related river activity al Ihe Weichselian. Mts. and morphotectonics of the Polish Carpathians, Andrzej Kostrzewski, Matgorzata Mazurek, Zbigniew Zwoliriski Holocene transition: a comparative study of the Warta Zeszyty Naukowe AGH, Kwurralnik Geologia l3 (3-4): and Mans rivers. Terra Nom 6: 476-485. 1-167, Adam Mickiewicz Unil'ersity, QuaterllOlY Re.~earch Jnstirute. Wisniewski. E., 1982: Theevolution ofthe Vistula river valley Zurek, S., 1975: Geneza zabagnienia Pradoliny Biebrzy. ?race Ill. Fredry /0, 61·70J POZIIOri, Poland between Wloctawek and Ciechocinek during the last GeografiClnelG PAN 110: 1-107.

Abstrllct: Understanding the c1wacter and temporal nriability of fluvial uansport is of fundamenlallmportante for !he quahtau\'c 3.IId quantlIJ11\'C description of contemporary flu\ul systems, In the present SlUdy cenalll fUMes of fluvial LA traltSpot1 are regarded as markers which indIcate the WilY the denudation system of a catchment operates. On the basIS of mapping carrit'd out along thc upper PaBl;tll channel. only a small pan ofthe nlehmcnt ....-as found 10 take part in the supply _.­ of suspended material 10 the rh'er channel. The occurrence and Intensity ofprocesses active in the supply ofsediment for 'M' transJlOn in the Parsc;ta channel depends largely on lithology, channel morpholob'Y, conditions ofwalcr flow, hydrogcological conditions, and vegClation. These f3cto1"5 are modified by the activity of man and animals. Variations in the transport of solutes along the upper Pal"5~ta result from differences in lithological sources. which, in turn, arc associated with other environmcnllll fllCtors which determine the rate ofwater circulation. The figures for ionic and suspended flows obtained in this research confirm lhe regulanlY With .....hich dlssoh"ed matmal is overwhelmingly predominant in the fluvial tr:lnspon ofPomeramall rivers. The changing meteorological conditions in the catchment. and also the SUSOfIal development of its plant CO\'Cf. are re(ll;(:ted in !he W3Y the m'er flow IS sustained and. In the flu\'u,1 regime, is expressed as the amount ofmatenalleaV\ng the catchment SYStrnJ. The thl'C'C' penods ofdenudallOOal activil)' whicb ba\"e bttn distinguished on the basis of dlffermces in their flU\'lal tmlsport regimes. reflttl the susooal efficiency of denudation proctsSes in the catchment. The seasonal variallons 10 the fluvialtranspot1 In tbe uppcr Parsc:ta proVIde an insight mto the dC\'elopment ofthe present-day relief ortbe young-glacial area of West Pomerania.

Key ",'(lrds: fluvial transport, source of material, solute load, sediment load. post.glacial catchmenl

Introduction basis for the conception of geoecosyslem operation. as formulated in Kostrzewski (1986. 1993). The following, In the contemporary denudation syslem of West already established regularity is the basic assumption of this Pomerania, fluvial transport plays a fundamental role by invcstigation: the kind and amount ofmaterial flowing through carrying away material from erosion and denudation in the the measuring point reflect current geomorphological processes catchments. A detailed analysis offluvial transport provides a taking place in the river channel and catchment (Grcgory & good indicator ofreliefevolution. including soillcaching and Walling, 1973: Schumm, 1977; Richards. 1982; Froehlich. erosion. The character of the fluvial transport is also a good 1982; Knighton. 1984; Zwoliftski, 1989). indicator ofchange in the landscape structure of a region. In The basic objective ofthe research conducted in theupper the present study, the subject ofthe investigalion was the upper Pars",ta catchment is the underst'andingofthe operation ofthe Pars~ calchmenl. which is regarded as represenlative ofthe geo--ecosystcm ofa lowland river in the conditions ofclimatic post-glacial zone of West Pomerania and the Polish Plain.. change and various foons ofhuman impact. The aims ofthe Systematic investigations ofmodem morphogenetic processes presenl investigations include: in the upper r~ta catchment have been carried out since I)an evalualion ofthecontrols. pattern and intensity offluvial 1981. Since I November 1985. daily measurements have been transport, which are reflectionsofthe denudation processc.:s taken in the profile which closes Ihe upper Pars<;.ta catchment occuning in the upper P~calchmentsystem, i.e. mainly (at Storkowo); this catchment is regarded as an independent soil erosion and leaching. denudation system. 2) an analysis ofvariations in the physico-chemical properties Thc programme ofresearch in the upper Pars<;:1.a catdunent ofsolutcs and solids in the upper Parsl{la channel as factors is based on methodological assumptions derived from controlling the variability of fluvial transpon and Cholley's concept ofa denudation system (Trican., 1960) and determining its role in the conlemporary denudation systtm BertallanfTy's (1984) systems theol)'. They have provided the ofthe catchment;

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