TY - JOUR A1 - Pedoja, K. A1 - Jara Muñoz, Julius A1 - De Gelder, G. A1 - Robertson, J. A1 - Meschis, M. A1 - Fernandez-Blanco, D. A1 - Nexer, M. A1 - Poprawski, Y. A1 - Dugue, O. A1 - Delcaillau, B. A1 - Bessin, P. A1 - Benabdelouahed, M. A1 - Authemayou, C. A1 - Husson, L. A1 - Regard, V. A1 - Menier, D. A1 - Pinel, B. T1 - Neogene-Quaternary slow coastal uplift of Western Europe through the perspective of sequences of strandlines from the Cotentin Peninsula (Normandy, France) JF - Geomorphology : an international journal on pure and applied geomorphology N2 - The Cotentin Peninsula (Normandy, France) displays sequences of marine terraces and rasas, the latter being wide Late Cenozoic coastal erosion surfaces, that are typical of Western European coasts in Portugal, Spain, France and southern England. Remote sensing imagery and field mapping enabled reappraisal of the Cotentin coastal sequences. From bottom to top, the N Cotentin sequence includes four previously recognized Pleistocene marine terraces (T1 to T4) at elevations <40 m as well as four higher and older rasas (R1 to R4) reaching 200 +/- 5 m in elevation. Low-standing marine terraces are not observed in the central part of the Peninsula and a limited number of terraces are described to the south. The high-standing rasas are widespread all over the peninsula. Such strandline distributions reveal major changes during the Late Cenozoic. Progressive uplift of an irregular sea-floor led to subaerial exposure of bathymetric highs that were carved into rocky platforms, rasas and marine terraces. Eventually, five main islands coalesced and connected to the mainland to the south to form the Cotentin Peninsula. On the basis of previous dating of the last interglacial maximum terrace (i.e. Marine Isotopic Stage, MIS 5e), sequential morphostratigraphy and modelling, we have reappraised uplift rates and derived: (i) mean Upper Pleistocene (i.e. since MIS 5e similar to 122 +/- 6 ka, i.e. kilo annum) apparent uplift rates of 0.04 +/- 0.01 mm/yr, (ii) mean Middle Pleistocene eustasy-corrected uplift rates of 0.09 +/- 0.03 mm/yr, and (iii) low mean Pleistocene uplift rates of 0.01 mm/yr. Extrapolations of these slow rates combined with geological evidence implies that the formation of the sequences from the Cotentin Peninsula occurred between 3 Ma (Pliocene) and 15 Ma (Miocene), which cannot be narrowed down further without additional research. Along the coasts of Western Europe, sequences of marine terraces and rasas are widespread (169 preserve the MIS Se benchmark). In Spain, Portugal, S England and other parts of western France, the sequences morphostratigraphy is very similar to that of Cotentin. The onset of such Western European sequences occurred during the Miocene (e.g. Spain) or Pliocene (e.g. Portugal). We interpret this Neogene-Quaternary coastal uplift as a symptom of the increasing lithospheric compression that accompanies Cenozoic orogenies. (C) 2017 Elsevier B.V. All rights reserved. KW - Marine terrace KW - Rasa KW - Cotentin and Western Europe KW - Neogene and Quaternary coastal uplift Y1 - 2017 U6 - https://doi.org/10.1016/j.geomorph.2017.11.021 SN - 0169-555X SN - 1872-695X VL - 303 SP - 338 EP - 356 PB - Elsevier CY - Amsterdam ER - TY - JOUR A1 - Pedoja, Kevin A1 - Husson, Laurent A1 - Johnson, Markes E. A1 - Melnick, Daniel A1 - Witt, Cesar A1 - Pochat, Stephane A1 - Nexer, Maelle A1 - Delcaillau, Bernard A1 - Pinegina, Tatiana A1 - Poprawski, Yohann A1 - Authemayou, Christine A1 - Elliot, Mary A1 - Regard, Vincent A1 - Garestier, Franck T1 - Coastal staircase sequences reflecting sea-level oscillations and tectonic uplift during the Quaternary and Neogene JF - Earth science reviews : the international geological journal bridging the gap between research articles and textbooks N2 - Many coasts feature sequences of Quaternary and Neogene shorelines that are shaped by a combination of sea-level oscillations and tectonics. We compiled a global synthesis of sea-level changes for the following highstands: MIS 1, MIS 3, MIS 5e and MIS 11. Also, we date the apparent onset of sequences of paleoshorelines either from published data or tentatively extrapolating an age for the uppermost, purported oldest shoreline in each sequence. Including the most documented MIS 5e benchmark, we identify 926 sequences out of which 185 also feature Holocene shorelines. Six areas are identified where elevations of the MIS 3 shorelines are known, and 31 feature elevation data for MIS 11 shorelines. Genetic relationships to regional geodynamics are further explored based on the elevations of the MIS 5e benchmark. Mean apparent uplift rates range from 0.01 0.01 mm/yr (hotspots) to 1.47 0.08 mm/yr (continental collision). Passive margins appear as ubiquitously uplifting, while tectonic segmentation is more important on active margins. From the literature and our extrapolations, we infer ages for the onset of formation for -180 coastal sequences. Sea level fingerprinting on coastal sequences started at least during mid Miocene and locally as early as Eocene. Whether due to the changes in the bulk volume of seawater or to the temporal variations in the shape of ocean basins, estimates of eustasy fail to explain the magnitude of the apparent sea level drop. Thus, vertical ground motion is invoked, and we interpret the longlasting development of those paleoshore sequences as the imprint of glacial cycles on globally uplifted margins in response to continental compression. The geomorphological expression of the sequences matches the amplitude and frequency of glacial cyclicity. From middle Pleistocene to present-day, moderately fast (100,000 yrs) oscillating sea levels favor the development of well identified strandlines that are distinct from one another. Pliocene and Lower Pleistocene strandlines associated with faster cyclicity (40,000 yrs) are more compact and easily merge into rasas, whereas older Cenozoic low-frequency eustatic changes generally led to widespread flat-lying coastal plains. KW - Cenozoic KW - Coastal sequence of shorelines KW - Strandlines KW - Rasa KW - Geodynamic Y1 - 2014 U6 - https://doi.org/10.1016/j.earscirev.2014.01.007 SN - 0012-8252 SN - 1872-6828 VL - 132 SP - 13 EP - 38 PB - Elsevier CY - Amsterdam ER -