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50°
Dvina
Neman
Dnieper
BlackSea
Dniester
Danube
Vistula
Odre
BalticSea
Tisz
a
20° 30° 40°
Researchareas
Rivers
State borders
Sea
Mar
os
Mountainranges
= = Subsidingareas
==
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===
==
==
=
==
==
=
Legend
===
=
50°
Dvina
Neman
Dnieper
BlackSea
Dniester
Vistula
Odre
BalticSea
Tisz
a
20° 30° 40°
Mar
os
==
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==
=
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=
=
===
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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=
==
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=
=
===
Forest teppes
= =
Gulf
Delta
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m a.s.l.
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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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MIDDLE LATVIAN LOWLAND
EAST LATVIAN LOWLAND
III
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.s.l.
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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
25
20
15
10
kaca
lBP
45
40
35
30
25
20
15
10
Polis
hC
arp
athia
ns
S-S
andom
ierz
Basi
n
N-S
andom
ierz
Basi
n
Cen
tral
Pol
and
N-P
ola
nd
Gla
ciate
d
Vis
tula
Delta
Nem
unas
W-D
vina
Upp
erD
niep
er
Mid
dle
Dni
epe
rB
asin
Tis
zaV
alle
y
Ma
ros
Fan
Som
eºu
lMic
Valle
y
Tel
eorm
an
Dan
ube
Del
ta
SM
LM
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NIG
LAC
IAL
UP
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RP
LEN
IGLA
CIA
LH
OL
OC
EN
ELA
TE
GLA
CIA
L LM LMM
LM
SM
MM
LM
+ 0m
= - 100
+ - 40
= - 120
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
lta
Sulin
aId
elta
Sul
ina
IIdelta
Co
sna
delta
Ma
tita
lag
una
rd
epo
sits
Ra
zelm
dep
osi
ts
Sf.
Gh
eor
ghe
IId
elta
Chili
ade
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Lagunar deposits
Marine deposits
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