50°

Dvina

Neman

Dnieper

BlackSea

Dniester

Danube

Vistula

Odre

BalticSea

Tisz

a

20° 30° 40°

Researchareas

Rivers

State borders

Sea

Mar

os

Mountainranges

= = Subsidingareas

==

======

===

==

==

=

==

==

=

Legend

===

=

50°

Dvina

Neman

Dnieper

BlackSea

Dniester

Vistula

Odre

BalticSea

Tisz

a

20° 30° 40°

Mar

os

==

======

===

==

==

=

==

==

=

=

===

Danube

LGM

Permafrost limit

Present Rivers

State borders

Present Sea

Mountain ranges

Subsiding areas

Legend

Dunes

Ice marginstreamways

Maximum extentof the Ice Sheet

Mountain glaciers

Tundra

Steppe

Park tundra

Deciduous foreststeppe

Transfer of glacialmeltwaters

50°

Dvina

Neman

Dnieper

BlackSea

Dniester

Vistula

Odre

BalticSea

Tisz

a

20° 30° 40°

Mar

os

=

Danube

GS-1 / Holocene

Present Rivers

State borders

Present Sea

Mountain ranges

+ + Uplifting areas

Legend

Boreal forest

Tundra

Steppe

Forest tundra

Deciduous forest

++

+ ++

+ +

+ +

+ +++ +

+++ +

+

+ + ++

+++

Sea limitduring GS-1

Subsiding areas

==

======

===

==

==

=

==

==

=

=

===

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Factors controlling the evolution of fluvial systems in C-E Europeduring the last cold stage (60-8 ka BP)

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60 50 40 30 20 10 0 ka BP43.6 24.1 11.5 ka cal BP34.5

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EAST LATVIAN UPLAND

Leszek Starkel , Danuta J. Michczyńska Piotr Gębica Timea Kiss , Andrei Panin , Ioana Persoiu1 2 4 5 6, ,3

1Institute of Geography and Spatial Organization, Polish Academy of Sciences, Cracow, Św. Jana 22, 31-018 Krakow, Poland,

Silesian University of Technology, Institute of Physics CSE, GADAM Centre of Excellence, Krzywoustego 2, 44-100 Gliwice, Poland,University of Information Technology and Management in Rzeszów, Department of Geography, Sucharskiego 2, 35-225 Rzeszów, Poland,

Department of Physical Geography and Geoinformatics, University of Szeged, Egyetem u. 2-6, H-6722, Szeged, Hungary,Lomonosov Moscow State University, Geography Faculty, Lengory 1, Moscow, 119991, Russia

Ştefan cel Mare University, Department of Geography, Universităţii 13, 720229, Suceava, Romania,

2 –

,

3

4

5

6

starkel@zg.pan.krakow.pldanuta.michczynska@polsl.pl

piotrgebica@wp.plkisstimi@gmail.com

a.v.panin@yandex.ruioanapersoiu@gmail.com

The evolution of fluvial systems in Central-Eastern Europe reflects in general a sequence of climatic changes registered on Greenlandin ice cores and the isotopic O curve. But in C-E Europe region we observe several deviations connected with different factors.

The C-14 and TL/OSL data helped to recognize the role of the second order climatic fluctuations in the mountains and theirforelands, change in longitudinal valley profiles and superposition of other factors – like tectonic component uplift or subsidence,blocking by Scandinavian ice sheet (or crossing of interfluves), marine regression or transgression as well as connected withdiachronous expansion of forest vegetation and change in temperature and humidity in north-south and east-west transects.

The long Interpleniglacial (58-28 ka cal BP) is represented in the mountains and plateaus by thick slope deposits interfingering withalluvia rich in organic remains (peat layers). Large alluvial fans are extending at the outlet from the mountains. In these fans, 2-3 cutsand fills were registered at several localities. They are especially well recognized in the Sandomierz Basin (S Poland).Rapid cool ingand the increase of continentality caused expansion of permafrost and a distinct change to incission, which preceded the maximumadvance of Scandinavian ice sheet and caused the covering of the interpleniglacial alluvial plains by thick younger loess. ThatInterpleniglacial period, with frequent climatic fluctuations, was the time of deposition of deluvial and colluvial silts and sands up to 20 mthick, and in smaller valleys dissecting loess plateaus. Only in the subsiding Pannonian Basin we observe permanent trend toaggradation.

During maximum extend of the ice sheet, ice-dammed lakes and ice-marginal valleys were formed. Also glaciofluvial fills wereformed during the transfluence into the Black Sea (area). Braided rivers at the mountain forelands formed incised lower alluvial fans.Strong eolian activity caused the formation of dune fields, especially extensive in the western elevated part of the Pannonian Basin(Transdanubia) build of sands probably blown out from glaciofluvial fan of Danube at its outlet from theAlps. Wind activity was very highin some intramountain depression (like Jasło-Sanok Doły) where deflation eroded shallow depressions and coarser Carpathian loesshas filled some valley floors.

During the ice-sheet recession, there has been gradual downcutting, supported by glacioisostatic uplift. The erosion was goingdown several tens meters below the present-day Baltic Sea level, and it was stopped by the Littorina transgression in the mid-Holocene. From about 18 ka cal BP, a gradual expansion of boreal trees from the East and the reduction of the sediment load started.

Only the greatest rivers, as the Danube and Tisza in the subsiding depressions far from supplying mountain areas preservedmeandering channels during the whole time. In most river valleys gradual change from braided channel to meandering ones wastypical. There were two warmer phases when followed formation of great

�18

palaeomeanders: 19-17 ka cal BP (Sagvar – Lascauxinterstadial) and 14.7 – 11.7 er Dryas. The large palaeomeanders of the older phase are developedover boreal forests-steppes of northern Ukraine and southern Russia, along tributaries of Tisza, and very rare in other regions. Afternext cool phase (equivalent of Pomeranian glacial advance) followed second warmer phase of Late Glacial, when great meandersdeveloped, which are better expressed north of the Carpathians where advance of forest stabilized the outflow. That system wasabandoned during Younger Dryas and changed to stable discharges reflected in small scale palaeomeanders.

Much greater diversity has been registered after Upper Pleniglacial on the extensive alluvial fan of Maros River surrounded bypermanently subsiding areas. Here frequent channel avulsions reflected the changes in hydrological regime of the headwater area.

During the early Holocene, under dense forest, which climbed up to 1500-2000 m a.s.l., relatively low discharge and sediment loadwas characteristic of rivers, especially in the Pannonian Basin, still occupied partly by steppe vegetation.

The climate has changed about 9.5 ka cal BP when followed the phase of frequent floods and expansion of deciduous trees,reflected in minerogenic layers in peatbogs and avulsions of river channels even with local tendency to braiding.

ka cal BP (Bølling –Allerød – Young

Global and regional factors influencing the evolution of the fluvial systems in C-E Europe.

CEE fluvialsystem

Sea level fluctuations(Baltic and Black Seas)

Scandinavian icesheet

Location(distance from theAtlantic Ocean )

Vertical crustalmovements

risingmountains

subsidingbasins

Permafrost

Vegetation coverIncrease of

continentality

glacioisostaticmovments

CLIMATE

Area of interest

DNIEPER. Transfer of meltwaters to Dniepervalley (after Sidorchuk et al. 2011). Legend: 1 -deposits of proglacial lakes; 2 - sandy glacio-fluvialdeposits; 3- melt-water blow-out channels; 4 -present-day direction of flow.

Changes in the vertical zonality of the vegetation cover during the last44 ka cal BP (simplified).

Palaeogeographic maps during LGM and GS-1/ Holocenetransition (simplified).

VISTULA. Longitudinal profile and schematic transversalprofiles of the Vistula River valley (after Starkel 2007,changed): 1 longitudinal channel profile, 2 fluvialterraces, 3- glaciofluvial terraces, 4 Vistulian terrace withdunes, 5 Vistulian terrace with loess cover, 6 channelfacies, 7 overbank facies, 8 organic deposits, 9marine deposits, 10 bedrock. Used abbreviation: VVistulian, LV Late Vistulian, H Holocene, res waterreservoir. Name of the Vistula catchments are in italics.

– ––

– –– – –

– –– – –

VISTULA. Fluctuations ofthe channel level during thelast cold stage along VistulaRiver (after Starkel et al.2007, changed). Greyrectangles show the mainphases of cl imatical lycontrolled erosion in mostregions of the formerperiglacial zone in southernand middle Poland. A. TheLower Vistula valley intheToruń Basin B. TheVistula valley in the WarsawBasin, C. Middle course ofthe Prosna valley, D. TheMroga valley on the ŁódźPlateau, E. Belnianka valley(after Ludwikowska-Kędzia2000) and Bierawka valley,F. The Vistula gap throughuplands, G. Middle course ofthe Wieprz valley on LublinPlateau, H. General schemeof channel fluctuations in theSandomierz Basin, I. UpperVistula in the OświęcimBasin, J. Lower course ofthe Carpathian valleys.

REFERENCES:Starkel et al., 2014. CLIMATIC FLUCTUATIONS REFLECTED IN THE EVOLUTION OF FLUVIAL SYSTEMS OF CENTRAL-EASTERN EUROPE (60 - 8 kacal BP). , submitted; and references cited herein.

Presented studies were partly obtained in the framework of an interdisciplinary research project from the Polish National Science Centre N N306034040 Contribution ofAndrei Panin was supported by the Russian Foundation for Basic Research, Project No.12-05-01148. Ioana Perşoiu contribution wassupported by two grants of the Romanian Ministry of Education, CNCS – UEFISCDI, project number PN-II-RU-PD-2012-3 – 0547 and project number PN-II-ID-PCE-2011-3-0057.

Quaternary International

.

MAROS. Paleochannel generations and their channelpattern on the Maros alluvial fan. 1 paleochannel, 2meandering, 3 anastomosing, 4 braided pattern, 5OSL age (ka) of the point- or mid-channel bars (afterSümeghy et al., 2013, changed).

– –– – –

70° 60° 50° 40° N�

ice sheet

tundra and arctic desert

park tundra

forest tundra

boreal forest

deciduous forest

forest steppe

steppe

boundary of permafrost

2500 m

0 m

Present time

2500 m

0 m

Late Glacial

2500 m

0 m

LGM

2500 m

0 m

34 - 44 ka cal BP

Legend

Data from different river valleys:

TISZA. Channel generations in the Middle Tisza and Sajó-Hernádalluvial fan region (after Gábris et al., 2012, changed). 1 LGMbraided paleochannel, 2 paleochannel from the last interstadial ofthe Upper Pleniglacial, 3 braided Oldest Dryas paleochannel, 4B lling/Aller d paleochannel, 5 Preboreal meanders, 6 Subborealmeanders, 7 unidentified age, 8 settlements.

––– –

ø ø – –– –

Black Sea level changes and stratigraphic sketch of the Danube deltadeposits (after Ghenea and Mihailescu 1991, changed).

NEMUNAS. The stream profile of the Nemunas River (after Dvareckas 1995). 1-8exposures. Names of the Nemunas catchments are in Italics.

–

WESTERN DVINA. Terraces of Western Dvina (after Eberhards 1972).

SEIM. The large meandering channel of thepalaeo-Seim River near Kudintsevo village(Borisova et al., 2006 changed).;

-44 -40 -36

45

40

35

30

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20

15

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kaca

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40

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25

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fluvial aggradationbraided rivermeandering riverlarge / small meandersglaciofluvial depositsorganic depositscolluvia - solifluction

M

LM / SM

+=LM

GS-1GI-1b

GI-1d

GS-2

GS-3

GS-4

GS-5

GS-6

GS-7

GS-8

GS-9

GS-10

GS-11

GS-12

8.2 ka event

9.3 ka event

BR

Legend

erosional phasetransition (erosional)ice margin streamtransfluent meltwaterssea transgresionsea regresioneolian activity

LM

LM

LM

SM

SMSM

LM

SM

LM

SM

SM

BR

BR

LM

BR

16000

14000

12000

10000

8000

6000

4000

2000

0

calB

P

-100 -50 0 50

Oldest Dryas

BollingOlder Dryas

Allerod

Younger Dryas

HO

LO

CE

NE

STRATIGRAPHYSea level changes (m)

DANUBE DELTA

Initi

als

pit

Sf.

Gh

eor

ghe

Ide

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Sulin

aId

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Sul

ina

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Lagunar deposits

Marine deposits