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Morphological evolution of the middle and lower seine valley (Normandy, France) during the quaternary: morphometric analysis of the paleo­meanders.

Évolution morphologique de la moyenne et de la basse vallée de la Seine (Normandie, France), au cours du quaternaire : analyse morphométrique des paléo-méandres.
Kim Genuite, Dominique Todisco, Carole Nehme, Daniel Ballesteros et Damase Mouralis
p. 203-220

Résumés

La Seine draine un espace de plus de 80 000 km2 couvrant l’essentiel du nord de la France et constitue l’un des cours d’eau majeurs du nord de l’Europe. Cependant, peu d’études se sont attachées à caractériser son évolution géomorphologique au cours du Quaternaire. Dans la région Normandie, la moyenne et la basse vallée de la Seine sont caractérisées par une dynamique en méandres semi-inscrits au sein desquels se développent des terrasses alluviales étagées pour la basse vallée, et semi-étagées pour la moyenne vallée, sur environ 100 m d’altitude relative par rapport au talweg rocheux. Ces morphologies et leurs dépôts associés reflètent les évolutions du cours d’eau sur une période d’au moins 1 Ma.Ce travail a pour objectif de reconstituer les paléo-trajectoires de la moyenne et de la basse vallée de la Seine au moyen d’analyses morphométriques et des outils de cartographie 3D et SIG des témoins morphologiques tels que les paléo-méandres. L’étude des morphologies au moyen des modèles numériques de terrain permet de préciser la stratigraphie quaternaire et l’étagement des terrasses alluviales sur l’ensemble des secteurs étudiés. Une nouvelle cartographie géomorphologique des dépôts fluviatiles est ainsi proposée et permet une meilleure compréhension de l’incision progressive du cours d’eau, de même que l’évolution de sa dynamique sur plus de 100 m d’étagement. Cinq générations d’abandon de méandre ont ainsi pu être déterminés. L’association de la cartographie géomorphologique avec l’étude des indices morphométriques permet de mettre en regard la dynamique fluviatile avec la surrection tectonique des plateaux de craie normands, l’évolution du bassin versant et les forçages glacio-eustatiques.

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This work was supported by the Paris Mega Region program and MESRI (ministère de l’Enseignement Supérieur et de la Recherche).

1 -Introduction

1The Seine River drains most of northern France. Despite its importance, few studies focused on the Seine catchment and its landscape evolution, to the benefit of smaller rivers such as the Somme, which remains a reference for the Quaternary because of the world famous archaeological sites it contains such as Saint Acheul (D’Acy, 1887; Tuffreau, 1979; Antoine & Limondin-Lozouët, 2004), or Moulin Quignon sites (Lartet, 1860; The Seine River drains most of northern France. Hurel et al., 2016), and the well described and well Despite its importance, few studies focused on the Seine dated stratigraphy of the fluvial deposits (Antoine et catchment and its landscape evolution, to the benefit al., 2000, 2007, 2019, 2020). The lower Seine valley of smaller rivers such as the Somme, which remains a is nevertheless a crucial territory for understanding the reference for the Quaternary because of the world famous Quaternary evolution of the Paris Basin occupied by past archaeological sites it contains such as Saint Acheul societies, including reference archaeological and paleo­environmental sites. Within the Seine fluvial and aeolian archives, Middle Paleolithic industry or macrofauna remains were found in the lower Seine valley, for example at Saint-Pierre-Lès-Elbeuf (Lautridou et al., 1974, 1984; Cliquet et al., 2009), Tourville-la-Rivière (Descombes, 1983; Cordy et al., 2003; Faivre et al., 2014; Jamet, 2014; Bahain et al., 2019), and La Celle tufa (Limondin-Lozouët et al., 2006, 2010; Voinchet et al., 2015), suggesting human frequentation of the Seine valley since at least 400 ka. Previous works focused on the stratigraphy of alluvial sequences (Lautridou et al., 1984; Lécolle, 1984, 1989; Jamet, 2014) and led to an accurate characterization of the Seine lower fluvial and estuarine deposits from Marine Isotope Stage (MIS) 11/12 to 1 (Chauhan et al., 2017). Nowadays, the Seine course continues underwater in the Channel (fig. 1). This terminal part of the Seine course was mainly subaerial during the Last Glacial Cycle (Antoine et al., 2003; Lericolais et al., 2003; Benabdellouahed et al., 2013). The lower Seine course is today under the tidal influence. Holocene fine-grained estuarine deposits fill the valley up to the Grande Garenne meander, near Les Andelys (fig. 1), and cover the river course developed during the Upper Pleistocene glaciations, which is buried under estuarine deposits (Porcher, 1977, 1981). The present-day Seine course is underfit into the valley, such as other rivers in Europe (Blum et al., 2013), with gravels associated to the valley course formed during the last glacial stage as it was observed along the entire lower and middle sections (Lefebvre, 1988). The lower Seine valley presents ingrown meanders (semi-entrenched) incised into the Normandy Plateau mainly made of Cretaceous chalk (Lefebvre, 1988). That specific geological configuration allowed the preservation of some paleo-morphologies such as cutoff meanders, which are related to previous incision stages. For the lower fluvial terraces, the Seine evolution is represented in a well-preserved stepped structure in the lower valley. For the middle valley, a unique system of 16 alluvial units lying on weakly marked bedrock steps (Antoine et al., 2007) is visible near Guernes-Moisson meanders and Mantes-La-Jolie (Lécolle, 1989). However, very few studies focused on the Seine upper terraces (between 60 and environ 100 m above the current river talweg) due to the scarcity of the fluvial records and their difficulty to be adequately dated. The middle and lower Seine semi-entrenchment, paleo­hydrology and trajectory evolution have been influenced by both endogenic factors (uplifting) and exogenic dynamics (glacio-eustasy; bio-rhexistasy). However, the decoupling of those signals in the river entrenchment remains complex. The first incision stages are considered to be older than 1 Ma (Lautridou, 1983; Westaway, 2004; Nehme et al., 2020) and may correspond to a former paleo-catchment that included a part of the present-day Loire watershed. More ancient deposits representing such paleo-catchment were also described as Pliocene (e.g. Lozère Fm; Tourenq & Pomerol, 1995; Westaway, 2004; Dugué et al., 2009). Such configuration implies major changes in the watershed paleogeography along with sediment transport and discharge reductions. Previous works did not reconstruct the oldest paleo-trajectories of the Seine (Musset, 1928; Lefebvre, 1988), because of the poor conservation of field evidence. Indeed, the upper paleo-meander shapes do not fit at all with the current Seine trajectory even if entrenched in the Normandy plateau. These meander loop morphologies and associated deposits can provide new insights on the river transformations over the Quaternary (Lefebvre, 1988). Although an increasing amount of literature focuses on the Quaternary evolution of fluvial systems, most of the studies on meander evolution deal with free meander morphology (Willis & Tang, 2010; Ielpi & Ghinassi, 2014; Debnath et al., 2017) and few on semi-entrenched meanders (Cox et al., 2014). Working on Quaternary timescale means dealing with scarce and weathered morphologies in the landscape (Blum et al., 2013). Consequently, morphometric analysis of semi­entrenched meanders remains unstudied when working on long temporal scale as the entire Quaternary (Cox et al., 2014). The present study focuses on the middle and lower Seine in line with recent numerical developments on topographic surveys. The recent RGE alti 1 m high­resolution Digital Elevation Models (DEM) acquired by the Institut National de l’Information Géographique et Forestière and the Groupement d’Intérêt Public (GIP) Seine-Aval over the Seine lower valley in 2008 and 2010­2012 respectively, as well as the RGE Alti 5 m (IGN) on the middle Seine valley, improved the identification of fluvial paleo-morphologies preserved in the landscape. Such data was acquired through the combination of airborn LiDAR survey (Light Detection And Ranging) and photogrammetry. 1 m and 5 m resolution were combined in the same model to analyse both the middle and lower valley altogether, with a better resolution (1 m) for the lower valley. Our research aims to constrain the morphological evolution of the lower and middle Seine valley based on 1) new numerical analysis of the perched landforms such as paleo-meanders and 2) a review of the fluvial deposits in the investigated area. The analysis of the paleo-meanders at different relative heights combined with numerical models brings new insights as morphometric indices and paleo-discharge estimations for constraining the generations of fluvial terraces over long distances (about 300 km) and long periods of time (the Quaternary). These new numerical elements are discussed regarding the relative impact of endogenous and exogenous forcings in the river entrenchment and led to define five main generations of meander cutoffs.

Fig. 1: The middle and lower Seine River.

Fig. 1: The middle and lower Seine River.

Bathymetry of the Channel reveals the morphologies of the paleo-Seine and paleo-Somme rivers that were subaerial during the Quaternary glacial stages.

2 -Site and landscape settings

2.1 -Organization of the fluvial deposits

2Climatic variations and local bedrock specificities played an important role in the morphological evolution of the Seine River (Lefebvre, 1988). Climatic alternations between glacial and interglacial stages generated fluvial deposits still depicted in the current landscape. These deposits are organized differently between the middle and lower course of the river. Between Mantes-La-Jolie and Les Andelys (fig. 1), the Seine middle course develops along the Seine fault (Lécolle, 1984). It is characterized by a linear trajectory (few meanders) separating the large Paris meanders from those of the lower course. In this middle course, the previous studies of the Seine terraces suggested the development of more than 16 successive incision-filling phases that resulted in fluvial terraces stepped between + 60 m and the present-day talweg (Tourenq et al., 1991; Lautridou et al., 1999; Antoine et al., 1998, 2000).

3Further downstream, between Les Andelys and Le Havre (fig. 1), the lower Seine describes eleven large meanders about 10 km wide (Lefebvre, 1988). Unlike the Seine middle course, the alluvial terraces here seem to be organized in a stepped system including 7 to 13 generations of deposits depending on the authors (Lautridou et al., 1984; Antoine et al., 2000, 2007; Jamet, 2014; Nehme et al., 2020). Despite some effort to correlate fluvial generations between the middle and lower course (Lefebvre et al., 1994), the stratigraphic correlation remains complex and unclear (Lautridou et al., 1984). The ages obtained from the Saint-Pierre­Lès-Elbeuf and Tourville-La-Rivière sandy deposits suggest the formation of alluvial terraces following the major glacial/interglacial climatic cycles (Balescu et al., 1997; Voinchet et al., 2015; Bahain et al., 2019). These deposition phases would occur mostly during the transition from a glacial to an interglacial stage (Bridgland et al., 2009).

4The lower Seine course is presently influenced by estuarine dynamics up to Poses meander (fig. 2a), and associated with post Last Glacial Maximum and Holocene deposits visible on the borehole profiles along the lower Seine talweg (e.g., in Marais-Vernier paleo­meander) (Lefebvre, 1988; Frouin et al., 2007; 2009). Those coarse fluvial deposits representing the former subaerial river course are then buried below the estuarine sediment as they follow the bedrock slope (Porcher, 1977; Porcher, 1981; Alduc et al., 1979; Lautridou et al., 1984; Antoine et al., 2007).

Fig. 2: Location of the lower Seine paleo-meanders.

Fig. 2: Location of the lower Seine paleo-meanders.

Abandoned morphologies are entrenched in the Cretaceous chalk between 0 and + 106 m RH. Fluvial deposits are after the geological map performed by the Bureau de Recherches Géologiques et Minières (BRGM) (Quesnel et al., 2008; Van Lint et al., 2003), and modified following fieldwork prospections (this study). The Marais-Vernier underground geomorphological data is after Frouin et al., 2007.

2.2 -The lower and middle Seine valley paleo-meanders

5In the middle and lower Seine valley, paleo-meander morphologies are preserved between 0 and + 100 m of relative height (RH) above the maximum incision of the current bedrock talweg (Lefebvre, 1988). These meanders are considered as ingrown type (Thornbury, 1954; Rich, 1914), i.e with a pronounced asymmetry of cross-section, which usually develop under slow incision rates. Most of them were described or mapped by Lefebvre (1988), Lécolle (1984) and Dewolf et al. (1976). These paleo-morphologies from the river end (Le Havre) to Mantes-La-Jolie are described herein (fig. 2). The Le Havre section (estuarine mouth) is a large paleo-valley filled with estuarine deposits (~ 4 to 11 km wide section from Le Havre to Tancarville). Lefebvre (1988) interpreted this part as a consequence of the fluvial incision in the easily-eroded Lower Cretaceous chalk and Jurassic limestone, and the influence of marine inputs. The meander scars are still visible at Honfleur and Tancarville, but its stalk and morphological paleo-trajectory is masked under marine sediments (Porcher, 1977, 1981). Two meander remains are visible at Foulbec-Conteville and Saint-Samson-de-Laroque sites, respectively at 63 m RH and 85 m RH (fig. 2A). One meander morphology also present on the opposite bank (right side) is slightly incised in the chalk bedrock at Radicatel (85 m RH). One particular abandoned meander is the Marais Vernier that turned into a peat and wetland (Frouin et al., 2007, 2009) (fig. 2A). This meander also comprises fluvial gravels at + 3 m RH dated back to the last glacial period (Huault, 1980; Huault & Lefebvre, 1983). At 5 km North of Notre-Dame de Gravenchon, a paleo-meander shape is recognized with bedrock slopes at 80 m RH (fig. 2B). However, the meander does not comprise clearly deposit associated with an active stage. Facing Notre-Dame de Gravenchon, a small paleo-meander remain entrenched into the bedrock presents flat areas around 80 m RH. Further upstream, the Brotonne paleo-meander (40 m RH) is the largest among the Seine River paleo-meanders, with a radius reaching 3 km (fig. 2B). At 5 km North of Duclair, a large paleo-meander is identifiable on the plateau, at 106 m RH. Another meander of similar shape is located 10 km north of Caumont/La Bouille at 97 m RH (fig. 2C). Unlike the first one, the latter is associated with fluvial deposits, according to the geological map carried out by the Bureau de Recherches Géologiques et Minières (BRGM) (Quesnel et al., 2008; Van Lint et al., 2003). At 2 km East of Saint Martin de Boscherville, two paleo-meanders are identified at + 100 m RH. The Tourville-La-Rivière / Saint-Pierre-Lès-Elbeuf fluvial, estuarine and lacustrine deposits (fig. 2E) located at the fringe of the lower Seine course displays abandoned meanders between + 88 m and + 83 m RH (Balescu et al., 1997), further upstream, other paleo-meanders are located close to Les Andelys such as the abandoned meander of Daubeuf at + 64 m RH. At 10 km west of Mantes-La-Jolie, the Guernes and Moisson meanders (fig. 2F) seem to have been relatively stable during the incision process. Nevertheless, other two marked paleo­meanders can be observed at + 50 m and + 60 m RH south to the Guernes meander.

3 -Methods

3.1 -Reconstructing bedrock elevation

6The altitude of the morphological observations above sea level (a.s.l) was transformed to relative height values above the bedrock (m RH) in order to refine previous estimations made by Antoine et al (2007) and Jamet (2014), fig. 3. Due to the thickness of the estuarine deposits of the lower Seine River, classic raster algorithms such as Vertical Distance to Channel Network (Olaya & Conrad, 2009) cannot be used for automatic characterization of the fluvial deposit’s organization. The mentioned transformation was then performed semi-manually based on bedrock data between Duclair and Mantes-La-Jolie (Lautridou et al., 1984), and between Le Havre and Marais-Vernier from Lefebvre (1988) and references therein. Eleven boreholes from the Banque du Sous-Sol (BSS) database of the BRGM were also added to our database to better constrain the bedrock geometry. Local variations were discarded due to the irregular bedrock surface caused by karstification (e.g. Chedeville, 2015), that generated overdeepenings and lateral variations. Alternatively, in areas such as Caumont and Les Andelys, a mean slope calculated on bedrock points (uncertainty of ± 3 m) was considered to represent the talweg morphology. The selected points were digitized using 3DReshaper modelling software (fig. 3A) and replaced with the 1 m-resolution DEM (IGN RGE Alti 1 m) covering the lower Seine course. Points were then projected on each corresponding alluvial bank regarding the general path of the Seine river (fig. 3A) and were meshed following a Delaunay 2D linear interpolation (Delaunay, 1934; Maur, 2002; Gomes et al., 2009; Verhoeven, 2017) (fig. 3B). The reconstructed bedrock slope became here the main component for the topography normalization conducted with SAGA GIS (Conrad et al., 2015) using a DEM difference calculation (between the present topography DEM and the Bedrock DEM, fig. 3C). This step was a prerequisite to remove the bedrock slope and the estuarine impact on the alluvial deposit determination, leading to a new geomorphological map of the fluvial deposits, and a cross-section of the Seine valley (fig. 3D). Terrain Profile plugin (Jurgiel et al., 2020) was used with Matplotlib library. To complete the cross section, the geological map of Van Lint et al., (2003) and Quesnel et al., (2008) representing the fluvial deposits were used and refined with DEM observations and fieldwork (fig. 3E). Both incision and relative altitude values were corrected from the loess coverage (Chedeville, 2015). The produced DEM raster data was then extracted according to fluvial deposit’s polygons extension in order to obtain layers with specific morphological data for each fluvial terrace (fig. 3F). The layers representing fluvial deposit’s extensions were then plotted along a NW-SE trending topographical cross-section defined in figure 2. All data, maps and extracted layers were plotted on the figure 4 cross-section using QGIS 3.10.12.

Fig. 3: Morphometric analysis steps performed on the Seine River middle and lower course for reconstructing and characterizing their paleotrajectories over the Quaternary.

Fig. 3: Morphometric analysis steps performed on the Seine River middle and lower course for reconstructing and characterizing their paleotrajectories over the Quaternary.

(A, B & C) Creation of a bedrock-normalized digital elevation model (DEM). (D) Projection of the fluvial deposits on the cross-section defined in figures 2 & 4. (E) Geomorphological mapping performed to define the limits of the fluvial deposit’s extent, by drawing polygons on GIS-based software.(F) DEM cut according to the corresponding polygons of the geomorphological map. (G) Paleo-meanders indices and paleo-trajectories. Those were traced according to fluvial deposits extent and paleo-meanders scarps.

Fig. 4: Reconstructed fluvial terraces system of the middle and lower Seine course.

Fig. 4: Reconstructed fluvial terraces system of the middle and lower Seine course.

Cross-section is based on methodological procedure and former works described in section 3. Vertical scale is exaggerated x 850 and the location of the cross-section is shown in figure 2. The red line represents the maximum fluvial level of the Holocene period.

3.2 -Paleo-meander morphometric indices calculation

7Few paleo-meander morphologies and sparce fluvial deposits are preserved in the landscape for studying the entire Quaternary evolution of the Seine River. According to Williams (1986), in modern rivers, meander radius and channel width are strongly correlated with discharge. Such parameters were selected for the analysis, as they also apply for large rivers with entrenched paleo­meanders (Cox et al., 2014). Virtual circles were plotted inside the paleo-meander morphologies visible on the DEM in order to define the size of meanders by their radius (fig 3H). Each circle was fitted on the morphological evidence representing a part of a paleo­meander and a relative height (RH) value (above bedrock) was attributed to each. Fitted circles were used as a basis for the reconstruction of the river paleo- trajectories. Those circles were measured and considered as landmarkers of morphological changes of the Seine trajectories, especially using measurement of the radius both in the paleo-meanders and on the reconstructed trajectories (fig. 3G), before comparing the mean values for each fluvial stage. Paleo-meander numbers per level were analyzed through a Kernel Density Estimation (KDE) (Abramson, 1982; Botev et al., 2010) performed under IsoplotR (Vermeesch, 2018) with the following parameters: Kernel bandwidth: 2, and adaptive KDE. Paleo-trajectories along the Seine were reconstructed, from the first incision stage visible at the Normandy plateau (+ 106 m RH) to the current bedrock level. The first reconstruction steps follow previous interpretations for the fluvial terrace levels (Lefebvre, 1988), and were extended to the upper terraces. Meander paleo­trajectories were digitized manually using B-Spline curves between two paleo-meander morphologies in QGIS 3.10.12 (fig. 3G). When no paleo-meander was reported, we followed the external limits of the corresponding fluvial deposit maximum extension, perched and preserved meander point bars are visible in the middle and lower Seine River courses (Lefebvre, 1988, fig. 2). The reconstruction was performed starting from the lower to the upper stages. When no alluvial deposit was locally visible for one specific terrace stage, the digitizing step was conducted following the trajectory of the most recent meander. The incision depth was calculated for each paleo-meander by comparing their cutoff altitude with the one from the plateau, or with the previous generation of paleo-meander. A mean sinuosity index (Schumm, 1963) for each reconstructed Seine paleo-trajectory was estimated. Using RiverMetrics plugin (Clerici & Perego, 2016), we compared sinuosity variations between reconstructed trajectories. In order to encompass all the meander morphological evolutions and size variations, a fixed 10 km linear wavelength value was used for the analysis, with a sampling value of 1 km. This reference value expresses most of the morphological evolutions of the Seine River and represents the mean sinuosity for the Seine middle and lower course during the last glacial period (Lefebvre, 1988). All calculated sinuosity values are represented from Mantes-La-Jolie (plotting origin) to Le Havre, which allow to compare the Seine paleo-courses in terms of sinuosity and length variation.

8Finally, the length of the reconstructed paleo­trajectories was also taken into account between Mantes­La-Jolie and Le Havre. The Mantes-La-Jolie site was also taken as a reference start point because its position is located close to the entrance of the middle Seine course.

3.3 -Paleo-discharge estimation

9Considering the scarcity of the morphometric data collected on oldest levels, paleo-discharge modelling is suggested here using the width values equation from Dury (1976).

10where Q is the calculated paleo-discharge (m3·s-1) and W the river bankfull width (in m). Paleo-discharge calculation can also be performed using the paleo­meander radius (Alford & Holmes, 1985), and the equations of Manning or Brownlie (1983). However, the enlarging evolution of the Seine meanders due to the river incision and inherited weathering processes (e.g. affecting slopes) limited the paleo-discharge estimations with those methods, explaining the use of equation 1. Despite the poor preservation of the oldest fluvial deposits (+ 85 and + 100 m RH), discharge estimations can be carried out as coherent results for long periods of time (Cox et al., 2014).

4 -Results

4.1 -New correlations of the fluvial terrace system between the Seine river lower and middle courses.

11Figure 4 shows the reconstructed fluvial terrace and paleo-meanders system with respect to the bedrock altitude for the Seine River middle and lower course. This cross-section is the base for establishing the evolution of the Seine over the Quaternary with correlations based on the maximum levels of the fluvial deposits. The bedrock height is also indicated when available as it corresponds to the incision stages on the Seine River. While the distinction between the top of the fluvial sequence and the bedrock can be considered negligible for the highest levels (e.g., < 5 m thick for the + 100 m level), it becomes significant for the lowest levels as they are better preserved in the landscape. Thirteen paleo­courses were recognized parallel to the current bedrock slope, and up to the first incision stages on the Normandy plateaus, at + 106 m RH. Four major abandonment levels can be identified at around + 100 m (level 13), + 85 m (level 12), + 60 m (level 10) and + 40 m RH (level 8) due to the high relative abundance of cutoff markers. The cross-section clearly reveals the estuarine influence and the impact of the post-glacial marine transgression, as previously discussed in Lefebvre (1988). Deposits associated with the maximum flooding event during the Holocene are horizontal up to Saint-Pierre-Lès-Elbeuf site. The correlation between the organization of the fluvial deposits and the bedrock mean slope is clear for all fluvial levels with paleo-meanders. Fluvial deposits seem to be regularly spaced (around 10 - 15 m between each), which makes correlations possible over long distances such as the entire course of the middle and lower Seine River (fig. 4). One should remain careful regarding correlations between the middle and lower Seine valley that would require deeper work on the transition area, as discussed in Lautridou (1983) and Antoine et al (2007). Previous work of Lécolle (1989) allowed to characterize the bedrock incision steps, yielding 16 incision steps separated by 1-2 m between each other. However, the top of the fluvial deposits is trunked by erosion, making altitudinal correlations only at the state of hypothesis. Nevertheless, ESR datings delivered at St-Pierre-Lès-Elbeuf fluvial deposit (level 7) delivered comparable ages with deposits of similar relative height at La Celle (Antoine et al., 2007; Cliquet et al., 2009; Limondin-Lozouët et al., 2010; Jamet, 2014; Voinchet et al., 2015), making altitudinal correlations conceivable. A slight slope increase of the bedrock is visible between Rouen and Saint-Pierre-Lès-Elbeuf. This morphological distinction is however not clearly distinguishable in the fluvial deposit organization. The higher level (+ 100 m/level 13) can be correlated between Duclair and Saint Martin de Boscherville with visible paleo-meanders and corresponding fluvial sequences. An erosion surface corresponding to this level is also visible downstream the Guernes meander, at the confluence with the Epte river. For the + 85 m deposit (level 12), most of the morphological remnants corresponding to that level are visible in the lower Seine course and regularly crops out between Saint­Samson-de-Laroque and Tourville-La-Rivière, making its attribution relatively easy. It is not the case for the +70 m fluvial deposit (level 11) which does not appear to be correlated with any nearby paleo-meanders. The + 60 m deposit (level 10) is found both in middle and lower Seine course, the deposit thickness is around +15 m, and thicker than most of the other observed deposits (between 5 and 10 m). Two major paleo-meanders are associated to that level, upstream and downstream of the Seine lower course (Foulbec and Daubeuf). The Saint-Pierre-Lès-Elbeuf sequence seems to be correlated with the Brotonne paleo-meander last perennial stage with a bedrock reaching + 32/35 m RH and a fluvial sequence reaching 40 m RH (level 8). In figure 4, such a deposit may be correlated with the upper part of the Mantes-La-Jolie 16 fluvial sequences between +0 and + 45 m RH, accordingly with Lécolle (1984). The Oissel sequence (+ 30 m RH, level 6) is well visible at the beginning of the lower course. Two superimposed fluvial sequences (+ 18 and + 22 m RH/levels 4 and 5) are observed at the base of the Tourville-La-Rivière fluvial / tidal sequence (Jamet, 2014). The lower levels (between + 0 and + 10 m RH/levels 1-3) remain difficult to be distinguished from each other as they seem to be superimposed and covered by estuarine deposits.

4.2 -Paleo-meander morphometry

12Figure 5 depicts the radius size and channel width of the paleo-courses generations identified in section 4.1 to evaluate the morphometric evolution of the Seine lower and middle courses over the Quaternary. The mean radius of the + 100 m stage reaches 2223 ± 590 m for a width of 1030 ± 60 m (tab. 1). The second cutoff stage (+ 85 m HR) comprises six paleo-meanders with a mean radius of 2018 ± 478 m and a width of 957 ± 74 m. The third cutoff stage (+ 60 m RH) encompasses four paleo-meanders with a mean radius size of 2300 ± 334 m and a width of 648 ± 48 m. The + 50 m RH level comprises two paleo­meanders of 2044 ± 490 m radius size but the absence of clear riverine morphologies prevents width estimations. At + 40 m RH, two paleo-meanders were cutoff with a mean radius value of 2779 ± 486 m for a width of 699 ± 17 m (tab. 1). At + 20 m RH, one paleo-meander displays a radius of 2518 m. Finally, near the current bedrock talweg, the Marais-Vernier paleo-meander reaches a radius value of 3376 m and a width of 708 ± 16 m. In conclusions, the length, width, and sinuosity values seem to covariate on the entire sequence, except for the younger level for which the sinuosity index increases unlike the width and length trend (fig. 6). Width and radius only covariate in the highest levels (between + 70 and + 106 m RH) and seem to be disconnected since +60 m to the current level. The observed decrease in radius size disappears and yields larger values below paleo­course of + 60 m RH, with an increase of the standard deviations.

4.3 -Paleo-discharge estimations

13The calculation of paleo-discharges, using equation 1, suggests values ~ 1000 m3.s-1 for the first generation of paleo-courses (85 – 100 m RH), and ~ 500 m3·s-1 for other (younger) generations, equivalent to a decrease of about 30-50 % (tab. 1). Discharge estimations for the lowest levels are very close to the current Seine discharge (width = 246 ± 35 m and average discharge = 513 m3·s-1). Such results seem to be underestimated due to the underfitted paleo-meanders as well as the anthropic flood regulation of the river (Lesueur et al., 2003) which leads to important discharge underestimation by the equation of Dury (1976). When compared to the current Seine discharge, the river width seems to be 50 to 75 % lower for a similar discharge value. Calculated values should then be considered only as minimum estimation for the glacial stages when the lower Seine probably yielded higher discharge values than during interglacial periods.

5 -Discussion

5.1 -Morphological evolution

14The numerous cutoff markers still visible in the lower Seine course provide insights on the river evolution during the Quaternary. Both reconstructed paleo-trajectories and morphometrical indices along the whole incision depth (figs. 6 & 7) are used to discuss the landscape, from the onset of the incision to the Holocene transgression.

5.1.1 - First and second generation of meander cutoffs (+ 100 m and + 85 m RH; levels 13 and 12)

15Paleo-meanders are more numerous and better preserved at specific levels: the 85 -100 m RH levels for instance are especially well developped in the current topography. Their high number makes the reconstitution relatively easy. The + 100 m paleo-meanders downstream Rouen (Duclair, Caumont and Saint Martin de Boscherville) are the most difficult to reconstruct because they are relatively close to each other, or only appear as a highly weathered sub-horizontal paleo-surface close to Mantes-La-Jolie (fig. 4). Such meander cutoff stage is clearly visible (fig. 7A). The wavelength spectra of the 100 m and 85 m RH levels are relatively close to each other compared to the late and more entrenched stages and yield similar and very important sinuosity values (1.86). Those levels also comprise the most important number of paleomeander markers (n = 11, fig. 6). This is notably the case for the + 85 m level (n = 7). Such process is remarquable as the first stage of meanders (+ 100 m) is already incised between 15 and 40 m depth in the chalk plateau, reducing thus the displacement compared to general free-like meanders (Lefebvre, 1988; Leopold & Wolman, 1960; Leopold & Langbein, 1966). The morphological configuration of the first incision stage (+ 100 m RH) nevertheless represents an inherited feature testifying to the hydrological conditions from previous periods. The meander cutoff phase is more pronounced for the following phase: the + 85 m level is incised 60 m deep into the plateau, with most of the Seine paleo-meander markers (fig. 6). However, we noticed that the winding/sinuosity values do not change between both stages, as for their estimated paleo-discharges (between 900 and 1000 m3.s-1; tab. 1) which led us to consider them as representing similar hydrological conditions.

5.1.2 - Third and fourth generation of meander cutoffs (+ 60 m to + 40 m RH; levels 10 to 8)

16Reconstructing the trajectories of the + 40 and + 60 m RH levels was easily carried out based on existing maps in addition to well-preserved alluvial deposits (Lautridou et al., 1984; Jamet, 2014). However, less paleo-meander markers are visible under the + 85 m and + 100 m RH level. The trajectories between the 85 m level and the younger ones are relatively different, suggesting a change in the Seine paleo-hydrological conditions (fig. 6A). The channel width is reduced from ~ 1000 m to ~ 650 m. Nevertheless, morphological changes still occur, even if less important than the +85 m and +100 m RH levels, leading thus to meander abandonment and reorganization in both levels. The general river distance between Mantes­La-Jolie and Le Havre is also significantly reduced (figs. 6B & 7), following the decrease of the sinuosity index (1.7-1.6, fig. 6). The paleo-meander radius shows a relative stability with a slight tendency to increase. Whilst both generations are marked by a lowering of the sinuosity, it is more important for the + 40 m RH stage, which also displays more meander cutoffs. The + 40 m stage constitutes thus the second main peak of cutoffs in the Seine incision process (fig. 6).

5.1.3 -Fifth generation of paleo-courses (+ 40 m to 0 m RH; levels 6 to 1)

17Between + 40 m RH and the current talweg, the river incision continues and is mainly marked by the general enlarging process (increase of the radius values, fig. 6). These younger levels are locally better preserved in the landscape and are the most studied for their paleo­environmental implications (Cordy et al., 2003) and archaeological remains (Limondin-Lozouët et al., 2006, 2010 ; Bahain et al., 2019). ESR dating on these levels, specifically on the Elbeuf stage, provide an age ranging between 350 and 600 ka (Voinchet et al., 2015). Fewer paleo-meanders are visible though (n = 3). On a general viewpoint, the 0 – 40 m RH meander tendency is to prograde forward toward the Channel (to the West, see fig. 6). The forwarding translation movement is particularly visible between 40 and 0 m RH because of the scarcity of meander cutoffs (fig. 7B). No channel width change is noticed here, but the Marais Vernier buried gravel map (Frouin et al., 2007) is the only reference, which makes it difficult to interpretate potential changes in level displacement between 10 and 30 m RH.

5.2 -Potential forcing factors

5.2.1 -Quaternary uplifting

18The morphometrical analysis conducted on the paleo­meanders of the Seine middle and lower course reveal co-variations and indices that can be used to characterize the transformations affecting the Seine catchment, including incision process. The main indice is the number of paleo-meanders and their relative positioning above the current talweg. Such transformation implied a significant fluvial reorganization under forcing factors at a large scale. Meandering processes affecting the Seine middle and lower course were described as the consequence of a superimposition process. This is especially the case for the highest / oldest ones as they are the direct imprint of the previous paleo-hydrological conditions, when the Seine final course had free-like meanders in a large floodplain (Huault, 1987; Wazi et al., 1987; Lefebvre, 1988).

19The progressive incision process follows the uplifting, which most often leads to the reorganisation of the fluvial dynamics and general morphology over long timescales (Vandenberghe, 1995; Keller & Pinter, 1996; Blum et al., 2013). In the case of the Seine middle and lower course, their semi-incised morphologies (asymmetrical river banks) is typical of rivers adjusting to slow uplift rates, as it is supposed to be the case for the Seine and the Cotentin area (Pedoja et al., 2018). Such an uplifting mechanism was ascribed to changes in tectonic constraints during the Pliocene-Quaternary period (NE-SW compression), which were initiated at the end of the Miocene period and caused by the alpine convergence (Guillocheau et al., 2000; Briais, 2015).

20The onset of the valley incision is constrained by the presence of late Pliocene marine and fluvio-marine sands (St-Eustache and Lozère Fms) as well as Gelasian La Londe Fm made of lagoonal clay on the Normandy plateau (Van Vliet-Lanoë et al., 2002; Dugué et al., 2009; Dugué et al., 2012). Those sandy and clayish deposits are reported between + 112 m and + 130 m RH, which implies the development of a large erosion surface entrenched into soft hills for those stages, and free meandering dynamics. The onset of the Seine incision inside its bedrock starts at + 106 m RH, which represents the highest incision markers. Few data exist for the highest levels. Nehme et al. (2020) compared terrace levels with cave deposits using paleomagnetic analysis in karst caves and showed that uplifting rates was probably slow between + 130 and + 100 m RH. The main onset of the incision occurs after the +100 m level and possibly reached values between 20 to 30 mm.ka-1 that lasted until the + 60 m RH level. Whilst the lack of chronological data makes further interpretations rather difficult, such acceleration may be directly correlated with the numerous meander cutoffs visible between + 100 and + 85 m RH (levels 13-12). Acceleration in the uplift process may indeed lead to meander cutoffs (Maher & Harvey, 2008). It is recognized that greatest rates of lateral erosion coincide with peaks of maximum net incision (Cordier et al., 2017; Bridgland & Westaway, 2008; Bridgland, 2000), hence the relative quantity of meander cutoffs. Such an acceleration

21is discussed in Nehme et al. (2020) between + 100 m (levels 13-12) and + 60 m RH (level 10) and could be related to an increase of the uplifting rate (Guillocheau et al., 2000; Robin et al., 2003) . This could be linked with the incision process that slowly channelled the river course into the bedrock, making cutoff processes more difficult.

22The concentration of abandoned meander markers around + 40 m RH resulted from unclear reasons since a potential acceleration of the river entrenchment has not been documented (Nehme et al., 2020). Nevertheless, Lefebvre et al (1988) described meander changes being influenced by sub-catchment captures at these altitudes such as the Risle and the Eure rivers (fig. 2). River captures bring more directional power to water flows and can generate important meander migrations. Such case is visible for the Elbeuf meander (S-E to N-W migration with the Andelle capture), and for the Daubeuf meander (N-S migration with the Eure capture; fig. 7). Such captures may be influenced by fluvial seepage and uplifting process that leads to a re-organization of the Seine watershed. Between + 60 and + 0 m RH, the incision process decreased with rates comprised between 5 and 8 mm.ka-1 corresponding to the Chibanian (i.e. Middle Pleistocene) and upper Pleistocene (Voinchet et al., 2015; Nehme et al., 2020). However, one might be cautious in interpreting incision rates, rather than considering it as a broad estimation, due to the scarcity of absolute ages on fluvial deposits. Nevertheless, the low number of paleo-meanders between + 40 m and

23+ 0 m RH corresponds well with a decreasing uplift rate, that may have induced a stability of the meander evolution. Morphological implication of such change in the regional dynamism induces a meander widening, generating important lateral erosion (increasing meander radius values).

24The paleo-meander location is also significant regarding headward erosion as for the highest levels, most of the paleo-meander markers are located at in the lower course, whilst the most recent cutoffs seem to be located mainly in the middle course (fig. 4).

5.2.2 -Loire-Seine separation and catchment changes

25Other factors could explain the oldest parts of the Seine paleo-trajectories evolution since meander cutoff loops can be related to paleogeographic changes such as captures or separations of large rivers (Blum et al., 2013). The meander radius reduction observed for the + 85 m RH level could be related to the consequences of a Loire-Seine separation event, which implies important decrease of the Seine catchment extension and discharge (Tourenq & Pomerol, 1995; Antoine et al., 1998 ; Debrand-Passard et al., 1998; Larue, 2005; Étienne & Larue, 2011; Larue & Étienne, 2014). Such fluvial diversion would be also related to a regional uplift, which consequences may also impact the Seine trajectories, and so, mix the signal implied in the meander morphologies. However, the reduction of the estimated paleo-discharge is important and yields more than 50 % reduction compared to the upper levels (around 500 m3.s-1). Whilst more independent elements need to be taken into account, the remaining questions around the Loire-Seine separation chronology, processes and consequences lead to consider the observed width and paleo-discharge reduction on the river profiles in future research.

5.2.3 -Climate-driven meander cutoffs and marine impact

26Considering the paleomagnetic inversion attributed to Matuyama-Brunes reversal (781 ka) found in cave sediments at + 60 m RH in the lower Seine course (Nehme et al., 2020), some of the Seine morphological changes might be correlated with climate driven processes coevally to the Calabrian-Chibanian transition from 41 ka to 100 ka cycles (Clark et al., 2006; Bridgland & Westaway, 2008). Such process could explain the meander abandonment peaks visible between + 60 and + 40 m RH. The morphological evolution of the Seine River lower part (+ 40 m to + 0 m RH) represents the end of the Quaternary, from the Chibanian to the Holocene. Whilst these periods are not marked by important cutoff stages, the general enlargement of the meanders and the forward movements (fig. 7B) could be the consequence of an increase in material transport caused by enhanced cold conditions (more pronounced glacial periods after the transition from 41 ka to 100 ka stages). Those stages are very well preserved in the Paleo-Channel sediments, which could be related to a direct impact on the fluvial contribution to the Atlantic Ocean (Toucanne et al., 2009). The global increase of the Seine watercourse length on the studied part (between Mantes-La-Jolie and Le Havre) is also a possible consequence of the lateral entrenchment process of the meanders.

27The marine influence on the lower Seine River is also a consequence of the paleoclimate evolution during the Quaternary, as enhanced glaciations lead to more pronounced incision during the interglacial-glacial transitions (Bridgland, 2000), and enlarged paleo-valleys during interglacial periods (Lefebvre, 1988). The Seine middle course has shown regular deposition processes for at least the last 400-600 ka (Lécolle, 1984), and was described as free from marine influence, hence a different preservation of the fluvial deposits organization (Antoine et al., 2000). In the lower course, the river is directly impacted by estuarine processes, and displays the majority of the paleo-meander markers (fig. 4). Cutoffs may have developed under the influence of marine invasion as the avulsion process generates important changes in river watercourses (Mocochain et al., 2009), hence potential rapid morphological changes. Such process is difficult to identify on meander cutoffs morphologies, however it seems more conceivable that it impacted the downstream and lower-level paleo­meanders such as the Marais-Verniers and the Brotonne one as they are in the area of influence of the marine transgression and in the more enlarged part of the current valley. Such mechanics is less relevant for the middle Seine valley and the upper levels as meanders are less numerous (structurally driven river course), and farther away from the marine influence, hence other mechanisms may be at play in the cutoff processes (meander lateral progradation in high discharge and sedimentation periods). For the upper levels (+100/85/60 m RH; levels 13 to 10), meander cutoffs may be related to vertical incision mechanisms as they may follow a potential increase in the valley incision rate (Nehme et al., 2020), but more chronological data is needed to ascertain such a hypothesis. The absence of any estuarine sedimentary input for the highest terraces might be related to warmer conditions, whilst the presence of tidal inputs observed at the Elbeuf stratigraphic sequence (Jamet, 2014) would coincide with enhanced glacial / interglacial conditions (100 ka cycles) and valley enlargement. Such tidal inputs may remain to be discovered but their absence could also be related to the narrowing of the Channel near Rouen which may not favour the preservation of such deposits.

28The co-evolution of the morphometric factors is clearly visible, and significant regarding either uplifting increase, catchment size diminution or climate transitions (figs. 5 & 6). As such endogenic and exogenic factors are certainly intertwined.

296 -CONCLUSIONS

30The new geomorphological investigations enhance numerous entrenched paleo-meanders visible along the Seine middle and lower course reflecting the adaptation of the river to successive catchment-scale impacts. The morphometric analysis provides useful indicators for investigating the river evolution through the Quaternary. The morphometric study of meander abandonments at specific relative heights reveals at least five main evolutionary stages from the first incision mark at + 100 m RH to the current Seine riverbed.

31A first stage between 106-100 m RH is marked by numerous large paleo-meanders, which can be considered as inherited from the previous free-meander like functioning of the Seine estuarine paleo-erosion surface.

32A second stage at 90-85 m RH implies an important change of the river trajectory, following the continuing of the uplifting.

33A third stage at 70-60 m RH with less paleo-meander cutoffs that seem to correspond to a transition phase.

34A fourth stage at 50-40 m RH with larger paleo-meander cutoffs that also seem to correspond to a transition phase. Finally, a fifth and last stage between 40 and 0 m RH corresponding to a slow and relatively stable and mature evolution of the paleo-meanders that progressively enlarge by eroding the chalk river banks.

35Whilst several endogenous and exogenous forcing factors are suggested here without distinction between them, the morphological analysis enhanced the discharge reduction that occurred after the 85 m meander generation. Geochemical and mineral analysis as well as absolute dating measurements are required to provide a more accurate age-model for the middle and upper levels evolution.

36Finally, the study enhanced the particular aspect of the Seine middle and lower courses regarding its preserved fluvial morphologies and the possibility of using ingrown meanders as indicators of regional changes related to Quaternary endogenous and exogenous events.

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Titre Fig. 1: The middle and lower Seine River.
Légende Bathymetry of the Channel reveals the morphologies of the paleo-Seine and paleo-Somme rivers that were subaerial during the Quaternary glacial stages.
URL http://journals.openedition.org/quaternaire/docannexe/image/15902/img-1.jpg
Fichier image/jpeg, 76k
Titre Fig. 2: Location of the lower Seine paleo-meanders.
Légende Abandoned morphologies are entrenched in the Cretaceous chalk between 0 and + 106 m RH. Fluvial deposits are after the geological map performed by the Bureau de Recherches Géologiques et Minières (BRGM) (Quesnel et al., 2008; Van Lint et al., 2003), and modified following fieldwork prospections (this study). The Marais-Vernier underground geomorphological data is after Frouin et al., 2007.
URL http://journals.openedition.org/quaternaire/docannexe/image/15902/img-2.jpg
Fichier image/jpeg, 139k
Titre Fig. 3: Morphometric analysis steps performed on the Seine River middle and lower course for reconstructing and characterizing their paleotrajectories over the Quaternary.
Légende (A, B & C) Creation of a bedrock-normalized digital elevation model (DEM). (D) Projection of the fluvial deposits on the cross-section defined in figures 2 & 4. (E) Geomorphological mapping performed to define the limits of the fluvial deposit’s extent, by drawing polygons on GIS-based software.(F) DEM cut according to the corresponding polygons of the geomorphological map. (G) Paleo-meanders indices and paleo-trajectories. Those were traced according to fluvial deposits extent and paleo-meanders scarps.
URL http://journals.openedition.org/quaternaire/docannexe/image/15902/img-3.jpg
Fichier image/jpeg, 74k
Titre Fig. 4: Reconstructed fluvial terraces system of the middle and lower Seine course.
Légende Cross-section is based on methodological procedure and former works described in section 3. Vertical scale is exaggerated x 850 and the location of the cross-section is shown in figure 2. The red line represents the maximum fluvial level of the Holocene period.
URL http://journals.openedition.org/quaternaire/docannexe/image/15902/img-4.jpg
Fichier image/jpeg, 101k
URL http://journals.openedition.org/quaternaire/docannexe/image/15902/img-5.jpg
Fichier image/jpeg, 4,2k
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Kim Genuite, Dominique Todisco, Carole Nehme, Daniel Ballesteros et Damase Mouralis, « Morphological evolution of the middle and lower seine valley (Normandy, France) during the quaternary: morphometric analysis of the paleo­meanders.  »Quaternaire, vol. 32/3 | 2021, 203-220.

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Kim Genuite, Dominique Todisco, Carole Nehme, Daniel Ballesteros et Damase Mouralis, « Morphological evolution of the middle and lower seine valley (Normandy, France) during the quaternary: morphometric analysis of the paleo­meanders.  »Quaternaire [En ligne], vol. 32/3 | 2021, mis en ligne le 01 septembre 2023, consulté le 14 février 2025. URL : http://journals.openedition.org/quaternaire/15902 ; DOI : https://doi.org/10.4000/quaternaire.15902

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Auteurs

Kim Genuite

UMR IDEES 6266, CNRS / Université Rouen Normandie, 17 rue Lavoisier, FR-76130, MONT-SAINT-AIGNAN. Email: kim.genuite@univ­rouen.fr

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Dominique Todisco

UMR IDEES 6266, CNRS / Université Rouen Normandie, 17 rue Lavoisier, FR-76130, MONT-SAINT-AIGNAN. Email: dominique.todisco@univ-rouen.fr

Carole Nehme

UMR IDEES 6266, CNRS / Université Rouen Normandie, 17 rue Lavoisier, FR-76130, MONT-SAINT-AIGNAN. Email: carole.nehme@univ-rouen.fr

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Daniel Ballesteros

Departamento de Geodinámica / Universidad de Granada, Campus de Fuentenueva, s/n ES-18071, GRANADA. Email: dballesteros@ugr.es

Damase Mouralis

UMR IDEES 6266, CNRS / Université Rouen Normandie, 17 rue Lavoisier, FR-76130, MONT-SAINT-AIGNAN. Email: damase.mouralis@univ-rouen.fr

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