FN Archimer Export Format
PT J
TI Wave train model for knickpoint migration
BT 
AF LOGET, Nicolas
   VAN DEN DRIESSCHE, Jean
AS 1:1,2;2:3;
FF 1:PDG-DOP-DCB-GM-LES;2:;
C1 IFREMER, French Res Inst Exploitat Sea, DRO GM, F-29280 Plouzane, France.
   Coll France, Chaire Geodynam, F-13545 Aix En Provence, France.
   Univ Rennes 1, UMR 6118, F-35042 Rennes, France.
C2 IFREMER, FRANCE
   COLL FRANCE, FRANCE
   UNIV RENNES, FRANCE
SI BREST
SE PDG-DOP-DCB-GM-LES
IN WOS Ifremer jusqu'en 2018
   copubli-france
   copubli-univ-france
IF 2.119
TC 85
UR https://archimer.ifremer.fr/doc/00000/11075/8056.pdf
LA English
DT Article
DE ;Knickpoint;Migration rate;Wave train;Messinian Salinity Crisis;Base level drop
AB Rivers respond to a drop in their base level by incising the topography. The upstream propagation of an incision, as usually depicted by a knickpoint migration, is thought to depend on several parameters such as the drainage area, lithology, and the amplitude of the base level drop. We first investigate the case of the Messinian Salinity Crisis that was characterized by the extreme base level fall (1500 m) of the Mediterranean Sea at the end of the Miocene. The response of drainage areas of three orders of magnitude (10(3) to 10(6) km(2)) highlights the dominant role of the drainage area (with a square root relationship) in controlling the knickpoint migration after a base level fall. A compilation of mean rates of knickpoint propagation for time durations ranging from 10(2) to 10(7) years displays a similar relationship indicating that successive wave trains of knickpoint can migrate in a river: first, wave trains linked to the release of the alluvial cover and then, wave trains related to the bedrock incision, which correspond to the real time response of rivers. Wave trains with very low retreat rates (long lived knickpoints >1 My) rather correspond to the response time of regional landscape. (C) 2008 Elsevier B.V. All rights reserved.
PY 2009
PD MAY
SO Geomorphology
SN 0169-555X
PU Elsevier Science Bv
VL 106
IS 3-4
UT 000265343700021
BP 376
EP 382
DI 10.1016/j.geomorph.2008.10.017
ID 11075
ER

EF