Holocene evolution of a wetland in the Lower Seine Valley, Marais Vernier, France
Identifieur interne : 001656 ( Istex/Corpus ); précédent : 001655; suivant : 001657Holocene evolution of a wetland in the Lower Seine Valley, Marais Vernier, France
Auteurs : Millena Frouin ; Alain Durand ; David Sebag ; Marie-Françoise Huault ; Sylvie Ogier ; Eric P. Verrecchia ; Benoit LaignelSource :
- The Holocene [ 0959-6836 ] ; 2009-08.
Abstract
Estuaries like that of the Seine River in NW Europe developed in incised fluvial valleys after the last glacial maximum. Since the 1940s, several authors have studied the largest wetland of the Seine estuary, the Marais Vernier, to understand depositional environments during Holocene infilling. We reinterpret previous research based on new and published data (for example fill thickness and material source) to (1) describe facies and depositional environments; (2) reconstruct palaeoenvironmental evolution; (3) show the influence of local and global forcing on depositional environments. Before 7000—6000 cal. BC, terrestrial material was deposited because of catchment erosion related to changes in climate. Just before 7000—6000 cal. BC, estuarine material began to be deposited in low-lying areas in response to sea-level rise, while terrestrial material still settled at higher elevations. After this, but before 5850—5710 cal. BC, estuarine material areas began to accumulate at both high and low elevations. This marked a general flooding of the Marais Vernier, synchronous with that at the Seine estuary mouth. Soon after, peat accumulated over a wide area as a response to a local change in accommodation and a worldwide drop in sea level. A tidal channel developed to the west of the Marais Vernier, providing minerogenic material. After 1130—900 cal. BC, human influence becomes increasingly clear in the record. This record of regional change during the Holocene can serve as a reference for further studies in the area.
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DOI: 10.1177/0959683609105295
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<record><TEI wicri:istexFullTextTei="biblStruct"><teiHeader><fileDesc><titleStmt><title xml:lang="en">Holocene evolution of a wetland in the Lower Seine Valley, Marais Vernier, France</title><author wicri:is="90%"><name sortKey="Frouin, Millena" sort="Frouin, Millena" uniqKey="Frouin M" first="Millena" last="Frouin">Millena Frouin</name><affiliation><mods:affiliation>Department of Geography, Royal Holloway, University of London, Egham Hill, Egham TW20 0EX, UK,</mods:affiliation></affiliation><affiliation><mods:affiliation>E-mail: millena.frouin@rhul.ac.uk</mods:affiliation></affiliation></author><author wicri:is="90%"><name sortKey="Durand, Alain" sort="Durand, Alain" uniqKey="Durand A" first="Alain" last="Durand">Alain Durand</name><affiliation><mods:affiliation>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</mods:affiliation></affiliation></author><author wicri:is="90%"><name sortKey="Sebag, David" sort="Sebag, David" uniqKey="Sebag D" first="David" last="Sebag">David Sebag</name><affiliation><mods:affiliation>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</mods:affiliation></affiliation></author><author wicri:is="90%"><name sortKey="Huault, Marie Francoise" sort="Huault, Marie Francoise" uniqKey="Huault M" first="Marie-Françoise" last="Huault">Marie-Françoise Huault</name><affiliation><mods:affiliation>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</mods:affiliation></affiliation></author><author wicri:is="90%"><name sortKey="Ogier, Sylvie" sort="Ogier, Sylvie" uniqKey="Ogier S" first="Sylvie" last="Ogier">Sylvie Ogier</name><affiliation><mods:affiliation>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</mods:affiliation></affiliation></author><author wicri:is="90%"><name sortKey="Verrecchia, Eric P" sort="Verrecchia, Eric P" uniqKey="Verrecchia E" first="Eric P." last="Verrecchia">Eric P. Verrecchia</name><affiliation><mods:affiliation>Institut de Géologie, Rue Emile-Argand, 11, 2007 Neuchâtel, Switzerland</mods:affiliation></affiliation></author><author wicri:is="90%"><name sortKey="Laignel, Benoit" sort="Laignel, Benoit" uniqKey="Laignel B" first="Benoit" last="Laignel">Benoit Laignel</name><affiliation><mods:affiliation>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</mods:affiliation></affiliation></author></titleStmt><publicationStmt><idno type="wicri:source">ISTEX</idno><idno type="RBID">ISTEX:684E705A0AA21EAA0E713B4A69728A9C1614D80E</idno><date when="2009" year="2009">2009</date><idno type="doi">10.1177/0959683609105295</idno><idno type="url">https://api.istex.fr/document/684E705A0AA21EAA0E713B4A69728A9C1614D80E/fulltext/pdf</idno><idno type="wicri:Area/Istex/Corpus">001656</idno><idno type="wicri:explorRef" wicri:stream="Istex" wicri:step="Corpus" wicri:corpus="ISTEX">001656</idno></publicationStmt><sourceDesc><biblStruct><analytic><title level="a" type="main" xml:lang="en">Holocene evolution of a wetland in the Lower Seine Valley, Marais Vernier, France</title><author wicri:is="90%"><name sortKey="Frouin, Millena" sort="Frouin, Millena" uniqKey="Frouin M" first="Millena" last="Frouin">Millena Frouin</name><affiliation><mods:affiliation>Department of Geography, Royal Holloway, University of London, Egham Hill, Egham TW20 0EX, UK,</mods:affiliation></affiliation><affiliation><mods:affiliation>E-mail: millena.frouin@rhul.ac.uk</mods:affiliation></affiliation></author><author wicri:is="90%"><name sortKey="Durand, Alain" sort="Durand, Alain" uniqKey="Durand A" first="Alain" last="Durand">Alain Durand</name><affiliation><mods:affiliation>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</mods:affiliation></affiliation></author><author wicri:is="90%"><name sortKey="Sebag, David" sort="Sebag, David" uniqKey="Sebag D" first="David" last="Sebag">David Sebag</name><affiliation><mods:affiliation>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</mods:affiliation></affiliation></author><author wicri:is="90%"><name sortKey="Huault, Marie Francoise" sort="Huault, Marie Francoise" uniqKey="Huault M" first="Marie-Françoise" last="Huault">Marie-Françoise Huault</name><affiliation><mods:affiliation>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</mods:affiliation></affiliation></author><author wicri:is="90%"><name sortKey="Ogier, Sylvie" sort="Ogier, Sylvie" uniqKey="Ogier S" first="Sylvie" last="Ogier">Sylvie Ogier</name><affiliation><mods:affiliation>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</mods:affiliation></affiliation></author><author wicri:is="90%"><name sortKey="Verrecchia, Eric P" sort="Verrecchia, Eric P" uniqKey="Verrecchia E" first="Eric P." last="Verrecchia">Eric P. Verrecchia</name><affiliation><mods:affiliation>Institut de Géologie, Rue Emile-Argand, 11, 2007 Neuchâtel, Switzerland</mods:affiliation></affiliation></author><author wicri:is="90%"><name sortKey="Laignel, Benoit" sort="Laignel, Benoit" uniqKey="Laignel B" first="Benoit" last="Laignel">Benoit Laignel</name><affiliation><mods:affiliation>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</mods:affiliation></affiliation></author></analytic><monogr></monogr><series><title level="j">The Holocene</title><idno type="ISSN">0959-6836</idno><idno type="eISSN">1477-0911</idno><imprint><publisher>SAGE Publications</publisher><pubPlace>Sage UK: London, England</pubPlace><date type="published" when="2009-08">2009-08</date><biblScope unit="volume">19</biblScope><biblScope unit="issue">5</biblScope><biblScope unit="page" from="717">717</biblScope><biblScope unit="page" to="727">727</biblScope></imprint><idno type="ISSN">0959-6836</idno></series><idno type="istex">684E705A0AA21EAA0E713B4A69728A9C1614D80E</idno><idno type="DOI">10.1177/0959683609105295</idno><idno type="ArticleID">10.1177_0959683609105295</idno></biblStruct></sourceDesc><seriesStmt><idno type="ISSN">0959-6836</idno></seriesStmt></fileDesc><profileDesc><textClass></textClass><langUsage><language ident="en">en</language></langUsage></profileDesc></teiHeader><front><div type="abstract" xml:lang="en">Estuaries like that of the Seine River in NW Europe developed in incised fluvial valleys after the last glacial maximum. Since the 1940s, several authors have studied the largest wetland of the Seine estuary, the Marais Vernier, to understand depositional environments during Holocene infilling. We reinterpret previous research based on new and published data (for example fill thickness and material source) to (1) describe facies and depositional environments; (2) reconstruct palaeoenvironmental evolution; (3) show the influence of local and global forcing on depositional environments. Before 7000—6000 cal. BC, terrestrial material was deposited because of catchment erosion related to changes in climate. Just before 7000—6000 cal. BC, estuarine material began to be deposited in low-lying areas in response to sea-level rise, while terrestrial material still settled at higher elevations. After this, but before 5850—5710 cal. BC, estuarine material areas began to accumulate at both high and low elevations. This marked a general flooding of the Marais Vernier, synchronous with that at the Seine estuary mouth. Soon after, peat accumulated over a wide area as a response to a local change in accommodation and a worldwide drop in sea level. A tidal channel developed to the west of the Marais Vernier, providing minerogenic material. After 1130—900 cal. BC, human influence becomes increasingly clear in the record. This record of regional change during the Holocene can serve as a reference for further studies in the area.</div></front></TEI><istex><corpusName>sage</corpusName><author><json:item><name>Millena Frouin</name><affiliations><json:string>Department of Geography, Royal Holloway, University of London, Egham Hill, Egham TW20 0EX, UK,</json:string><json:string>E-mail: millena.frouin@rhul.ac.uk</json:string></affiliations></json:item><json:item><name>Alain Durand</name><affiliations><json:string>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</json:string></affiliations></json:item><json:item><name>David Sebag</name><affiliations><json:string>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</json:string></affiliations></json:item><json:item><name>Marie-Françoise Huault</name><affiliations><json:string>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</json:string></affiliations></json:item><json:item><name>Sylvie Ogier</name><affiliations><json:string>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</json:string></affiliations></json:item><json:item><name>Eric P. Verrecchia</name><affiliations><json:string>Institut de Géologie, Rue Emile-Argand, 11, 2007 Neuchâtel, Switzerland</json:string></affiliations></json:item><json:item><name>Benoit Laignel</name><affiliations><json:string>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</json:string></affiliations></json:item></author><subject><json:item><lang><json:string>eng</json:string></lang><value>Wetland evolution</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>depositional environments</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>inherited topography</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>climate</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>sea-level rise</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>Holocene</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>Lower Seine Valley</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>France.</value></json:item></subject><articleId><json:string>10.1177_0959683609105295</json:string></articleId><language><json:string>eng</json:string></language><originalGenre><json:string>research-article</json:string></originalGenre><abstract>Estuaries like that of the Seine River in NW Europe developed in incised fluvial valleys after the last glacial maximum. Since the 1940s, several authors have studied the largest wetland of the Seine estuary, the Marais Vernier, to understand depositional environments during Holocene infilling. We reinterpret previous research based on new and published data (for example fill thickness and material source) to (1) describe facies and depositional environments; (2) reconstruct palaeoenvironmental evolution; (3) show the influence of local and global forcing on depositional environments. Before 7000—6000 cal. BC, terrestrial material was deposited because of catchment erosion related to changes in climate. Just before 7000—6000 cal. BC, estuarine material began to be deposited in low-lying areas in response to sea-level rise, while terrestrial material still settled at higher elevations. After this, but before 5850—5710 cal. BC, estuarine material areas began to accumulate at both high and low elevations. This marked a general flooding of the Marais Vernier, synchronous with that at the Seine estuary mouth. Soon after, peat accumulated over a wide area as a response to a local change in accommodation and a worldwide drop in sea level. A tidal channel developed to the west of the Marais Vernier, providing minerogenic material. After 1130—900 cal. BC, human influence becomes increasingly clear in the record. This record of regional change during the Holocene can serve as a reference for further studies in the area.</abstract><qualityIndicators><score>9.296</score><pdfVersion>1.6</pdfVersion><pdfPageSize>595.276 x 841.89 pts (A4)</pdfPageSize><refBibsNative>true</refBibsNative><abstractCharCount>1535</abstractCharCount><pdfWordCount>5652</pdfWordCount><pdfCharCount>37096</pdfCharCount><pdfPageCount>11</pdfPageCount><abstractWordCount>233</abstractWordCount></qualityIndicators><title>Holocene evolution of a wetland in the Lower Seine Valley, Marais Vernier, France</title><refBibs><json:item><host><pages><last>92</last><first>181</first></pages><author></author><title>Fonction des outillages lithiques dans le Bassin Parisien au néolithique</title></host></json:item><json:item><author><json:item><name>J.R.L. 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UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</affiliation></author><author xml:id="author-3"><persName><forename type="first">David</forename><surname>Sebag</surname></persName><affiliation>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</affiliation></author><author xml:id="author-4"><persName><forename type="first">Marie-Françoise</forename><surname>Huault</surname></persName><affiliation>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</affiliation></author><author xml:id="author-5"><persName><forename type="first">Sylvie</forename><surname>Ogier</surname></persName><affiliation>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</affiliation></author><author xml:id="author-6"><persName><forename type="first">Eric P.</forename><surname>Verrecchia</surname></persName><affiliation>Institut de Géologie, Rue Emile-Argand, 11, 2007 Neuchâtel, Switzerland</affiliation></author><author xml:id="author-7"><persName><forename type="first">Benoit</forename><surname>Laignel</surname></persName><affiliation>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</affiliation></author></analytic><monogr><title level="j">The Holocene</title><idno type="pISSN">0959-6836</idno><idno type="eISSN">1477-0911</idno><imprint><publisher>SAGE Publications</publisher><pubPlace>Sage UK: London, England</pubPlace><date type="published" when="2009-08"></date><biblScope unit="volume">19</biblScope><biblScope unit="issue">5</biblScope><biblScope unit="page" from="717">717</biblScope><biblScope unit="page" to="727">727</biblScope></imprint></monogr><idno type="istex">684E705A0AA21EAA0E713B4A69728A9C1614D80E</idno><idno type="DOI">10.1177/0959683609105295</idno><idno type="ArticleID">10.1177_0959683609105295</idno></biblStruct></sourceDesc></fileDesc><profileDesc><creation><date>2009</date></creation><langUsage><language ident="en">en</language></langUsage><abstract xml:lang="en"><p>Estuaries like that of the Seine River in NW Europe developed in incised fluvial valleys after the last glacial maximum. Since the 1940s, several authors have studied the largest wetland of the Seine estuary, the Marais Vernier, to understand depositional environments during Holocene infilling. We reinterpret previous research based on new and published data (for example fill thickness and material source) to (1) describe facies and depositional environments; (2) reconstruct palaeoenvironmental evolution; (3) show the influence of local and global forcing on depositional environments. Before 7000—6000 cal. BC, terrestrial material was deposited because of catchment erosion related to changes in climate. Just before 7000—6000 cal. BC, estuarine material began to be deposited in low-lying areas in response to sea-level rise, while terrestrial material still settled at higher elevations. After this, but before 5850—5710 cal. BC, estuarine material areas began to accumulate at both high and low elevations. This marked a general flooding of the Marais Vernier, synchronous with that at the Seine estuary mouth. Soon after, peat accumulated over a wide area as a response to a local change in accommodation and a worldwide drop in sea level. A tidal channel developed to the west of the Marais Vernier, providing minerogenic material. After 1130—900 cal. BC, human influence becomes increasingly clear in the record. This record of regional change during the Holocene can serve as a reference for further studies in the area.</p></abstract><textClass><keywords scheme="keyword"><list><head>keywords</head><item><term>Wetland evolution</term></item><item><term>depositional environments</term></item><item><term>inherited topography</term></item><item><term>climate</term></item><item><term>sea-level rise</term></item><item><term>Holocene</term></item><item><term>Lower Seine Valley</term></item><item><term>France.</term></item></list></keywords></textClass></profileDesc><revisionDesc><change when="2009-08">Published</change></revisionDesc></teiHeader></istex:fulltextTEI><json:item><extension>txt</extension><original>false</original><mimetype>text/plain</mimetype><uri>https://api.istex.fr/document/684E705A0AA21EAA0E713B4A69728A9C1614D80E/fulltext/txt</uri></json:item></fulltext><metadata><istex:metadataXml wicri:clean="corpus sage not found" wicri:toSee="no header"><istex:xmlDeclaration>version="1.0" encoding="UTF-8"</istex:xmlDeclaration><istex:docType PUBLIC="-//NLM//DTD Journal Publishing DTD v2.3 20070202//EN" URI="journalpublishing.dtd" name="istex:docType"></istex:docType><istex:document><article article-type="research-article" dtd-version="2.3" xml:lang="EN"><front><journal-meta><journal-id journal-id-type="hwp">sphol</journal-id><journal-id journal-id-type="publisher-id">HOL</journal-id><journal-title>The Holocene</journal-title><issn pub-type="ppub">0959-6836</issn><publisher><publisher-name>SAGE Publications</publisher-name><publisher-loc>Sage UK: London, England</publisher-loc></publisher></journal-meta><article-meta><article-id pub-id-type="doi">10.1177/0959683609105295</article-id><article-id pub-id-type="publisher-id">10.1177_0959683609105295</article-id><article-categories><subj-group subj-group-type="heading"><subject>Articles</subject></subj-group></article-categories><title-group><article-title>Holocene evolution of a wetland in the Lower Seine Valley, Marais Vernier, France</article-title></title-group><contrib-group><contrib contrib-type="author" xlink:type="simple"><name name-style="western"><surname>Frouin</surname><given-names>Millena</given-names></name><aff>Department of Geography, Royal Holloway, University of London, Egham Hill, Egham TW20 0EX, UK, <email xlink:type="simple">millena.frouin@rhul.ac.uk</email></aff></contrib></contrib-group><contrib-group><contrib contrib-type="author" xlink:type="simple"><name name-style="western"><surname>Durand</surname><given-names>Alain</given-names></name><aff>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</aff></contrib></contrib-group><contrib-group><contrib contrib-type="author" xlink:type="simple"><name name-style="western"><surname>Sebag</surname><given-names>David</given-names></name><aff>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</aff></contrib></contrib-group><contrib-group><contrib contrib-type="author" xlink:type="simple"><name name-style="western"><surname>Huault</surname><given-names>Marie-Françoise</given-names></name><aff>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</aff></contrib></contrib-group><contrib-group><contrib contrib-type="author" xlink:type="simple"><name name-style="western"><surname>Ogier</surname><given-names>Sylvie</given-names></name><aff>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</aff></contrib></contrib-group><contrib-group><contrib contrib-type="author" xlink:type="simple"><name name-style="western"><surname>Verrecchia</surname><given-names>Eric P.</given-names></name><aff>Institut de Géologie, Rue Emile-Argand, 11, 2007 Neuchâtel, Switzerland</aff></contrib></contrib-group><contrib-group><contrib contrib-type="author" xlink:type="simple"><name name-style="western"><surname>Laignel</surname><given-names>Benoit</given-names></name><aff>Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France</aff></contrib></contrib-group><pub-date pub-type="ppub"><month>08</month><year>2009</year></pub-date><volume>19</volume><issue>5</issue><fpage>717</fpage><lpage>727</lpage><abstract><p>Estuaries like that of the Seine River in NW Europe developed in incised fluvial valleys after the last glacial maximum. Since the 1940s, several authors have studied the largest wetland of the Seine estuary, the Marais Vernier, to understand depositional environments during Holocene infilling. We reinterpret previous research based on new and published data (for example fill thickness and material source) to (1) describe facies and depositional environments; (2) reconstruct palaeoenvironmental evolution; (3) show the influence of local and global forcing on depositional environments. Before 7000—6000 cal. BC, terrestrial material was deposited because of catchment erosion related to changes in climate. Just before 7000—6000 cal. BC, estuarine material began to be deposited in low-lying areas in response to sea-level rise, while terrestrial material still settled at higher elevations. After this, but before 5850—5710 cal. BC, estuarine material areas began to accumulate at both high and low elevations. This marked a general flooding of the Marais Vernier, synchronous with that at the Seine estuary mouth. Soon after, peat accumulated over a wide area as a response to a local change in accommodation and a worldwide drop in sea level. A tidal channel developed to the west of the Marais Vernier, providing minerogenic material. After 1130—900 cal. BC, human influence becomes increasingly clear in the record. This record of regional change during the Holocene can serve as a reference for further studies in the area.</p></abstract><kwd-group><kwd>Wetland evolution</kwd><kwd>depositional environments</kwd><kwd>inherited topography</kwd><kwd>climate</kwd><kwd>sea-level rise</kwd><kwd>Holocene</kwd><kwd>Lower Seine Valley</kwd><kwd>France.</kwd></kwd-group><custom-meta-wrap><custom-meta xlink:type="simple"><meta-name>sagemeta-type</meta-name><meta-value>Journal Article</meta-value></custom-meta><custom-meta xlink:type="simple"><meta-name>search-text</meta-name><meta-value>717 Holocene evolution of a wetland in the Lower Seine Valley, Marais Vernier, France SAGE Publications, Inc.200910.1177/0959683609105295 MillenaFrouin Department of Geography, Royal Holloway, University of London, Egham Hill, Egham TW20 0EX, UK, millena.frouin@rhul.ac.uk AlainDurand Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France DavidSebag Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France Marie-FrançoiseHuault Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France SylvieOgier Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France Eric P.Verrecchia Institut de Géologie, Rue Emile-Argand, 11, 2007 Neuchâtel, Switzerland BenoitLaignel Université de Rouen, Laboratoire 'Morphodynamique Continentale et Côtière' - UMR CNRS/INSU 6143, 76821 Mont-Saint-Aignan, France Received 19 August 2008; revised manuscript accepted 11 February 2009 † Present address: Institute of Geology and Paleontology, University of Lausanne, Anthropole, 1015, Lausanne, Switzerland. Estuaries like that of the Seine River in NW Europe developed in incised fluvial valleys after the last glacial maximum. Since the 1940s, several authors have studied the largest wetland of the Seine estuary, the Marais Vernier, to understand depositional environments during Holocene infilling. We reinterpret previous research based on new and published data (for example fill thickness and material source) to (1) describe facies and depositional environments; (2) reconstruct palaeoenvironmental evolution; (3) show the influence of local and global forcing on depositional environments. Before 7000—6000 cal. BC, terrestrial material was deposited because of catchment erosion related to changes in climate. Just before 7000—6000 cal. BC, estuarine material began to be deposited in low-lying areas in response to sea-level rise, while terrestrial material still settled at higher elevations. After this, but before 5850—5710 cal. BC, estuarine material areas began to accumulate at both high and low elevations. This marked a general flooding of the Marais Vernier, synchronous with that at the Seine estuary mouth. Soon after, peat accumulated over a wide area as a response to a local change in accommodation and a worldwide drop in sea level. A tidal channel developed to the west of the Marais Vernier, providing minerogenic material. After 1130—900 cal. BC, human influence becomes increasingly clear in the record. This record of regional change during the Holocene can serve as a reference for further studies in the area. Wetland evolution depositional environments inherited topography climate sea-level rise Holocene Lower Seine Valley France. Introduction Estuaries formed in incised fluvial valleys in NW Europe as a response to postglacial climate warming and sea-level rise (Allen, 2000; Blum and Tornqvist, 2000; Barber et al., 2003; Streif, 2004). During the Holocene, inherited topography, postglacial cli- mate warming, sea-level rise and human action all contributed to estuary change; human action has altered natural equilibria on both a local and a regional scale. The present study focuses on the largest wetland of the Seine River estuary (Marais Vernier), also named Lower Seine Valley (Figure 1). The low-lying area (+2 to +3 m Niveau Général de la France (NGF, French General levelling survey)) consists of a marsh made up of alluvium to the north and a large peaty marsh to the south. Since the 1940s, several authors have attempted to reconstruct the palaeoenvironmental evolution by studying only the Holocene infilling of the peaty marsh (Dubois and Dubois, 1943; Elhai, 1959; Huault and Lefebvre, 1983a; Huault, 1985). In this paper we reinterpret previous research, based on new and already published data (Frouin et al., 2006, 2007a, b) to identify the factors controlling the depositional environments. The data set used contains previous palaeoecological data, new sedimentary evidence and radiocarbon dates, to describe the fill, material sources, facies and related palaeoenvironments. Geographical and geological context The Marais Vernier (European Datum 1950 Lat: 0°27′16″E; Long: 49°25′26″N) occupies an abandoned meander. It is surrounded to the east, south and west by abrupt concave-upward slopes, made up of Cretaceous chalk and associated bedded and nodular flints, 718 Figure 1 Location of the Lower Seine Valley in the context of NW Europe and the Marais Vernier (MV) in the context of the Lower Seine Valley. The marine, middle and fluvial estuaries are defined by their salinity content and the tidally related water level of the Seine River overlain by Pliocene–Quaternary chalk weathering products (clay- with-flints) and Quaternary loess (Figure 1; Lautridou, 1985; Laignel et al., 1999, 2002; Quesnel et al., 2003). Studies of the geomorphology of the Seine River meanders assign the cutoff of the Marais Vernier meander to the last Pleniglacial period (Huault and Lefebvre, 1983a; Lefebvre, 1988, 1998). During the seventeenth century, the Hollandais dyke was built, in order to dry the peaty marsh and enlarge the agricultural area (Penna, 2003). This has isolated the peaty marsh to the south from the tidal marsh made of alluvium to the north. The current climate is oceanic, with a mean annual temperature of 10.5°C and a mean annual rainfall of 800 mm. The vegetation of the peaty marsh varies: Typha (bulrush) and Phragmites (reeds) where there is standing water; Juncus (rushes), Carex (sedges) and some Gramineae (grasses) in the meadows; Quercus pedunculata (oak) and Fagus sylvatica (beech) on the slopes (Huault and Lefebvre, 1983a). Material and methods Maps and lithology Two main drilling surveys were carried out in the peaty marsh of the Marais Vernier. The Direction des Mines (1949) drilled 400 holes (Figure 2a) to calculate peat content for use as fuel. Their survey allowed us: (1) to map the extent and thickness of the covering allochthonous, mainly minerogenic material and the underlying peat (Figure 2b and c), and (2) to characterize the underlying minerogenic material (Figure 2e). New drilling surveys were carried out in order to describe the entire Holocene sequence between the late 1970s and the present decade (Huault and Lefebvre, 1983a; Frouin et al., 2007a). Frouin et al. (2007a) used the data to describe the layout of the pre-Holocene topography (Figure 2d) and characterize the Holocene deposits. Characterization of deposits We characterized deposits first visually and then by considering their carbonate content, element chemistry, grain-size and mineral- ogy. We used: (1) a Bernard Calcimeter to identify carbonate con- tents (Milliman, 1974); (2) an x-ray diffractometer to identify clay mineral composition (Brindley and Brown, 1980; Holtzapffel, 1985); (3) a laser granulometer to identify sediment texture based on a clay-silt-sand diagram (GRADISTAT; Blott and Pye, 2001); (4) a CHNS elementary analyser to identify carbon and nitrogen content of the peat material. 719 Figure 2 Mapping of the Holocene fill and palaeotopography. (a) Location of cores and drill-holes carried out since the 1940s. (b) The thickness of covering minerogenic material. (c) The thickness of upper peat. (d) The pre-Holocene topography layout (Huault, 1980; Huault and Lefebvre, 1983a; Frouin et al., 2007a). S1 is the highest and oldest fluvial incision. S2 is a mid-level and younger fluvial incision. S3 is the lowest and youngest fluvial incision. (e) The composition and elevation of underlying minerogenic material Palaeoecology Diatom studies were used to describe the salinity of the SMV2 core (Huault, 1985) and the covering minerogenic material next to the Hollandais dyke (Elhai, 1963). Pollen analysis was used to recon- struct local palaeoenvironments recorded in two cores, SMV1 and SMV2 (Huault, 1980; Huault and Lefebvre, 1983a), based on a review of the pollen assemblages present (Sebag, 2002). Radiocarbon dating A total of 31 radiocarbon dates were calibrated using Oxcal v3.5 (Bronk Ramsey, 2000) and expressed as years cal. BC/AD (cal. BC/AD; 2σ; Table 1). Results and interpretation Description of the infilling Thickness and lithology The thickness of the peaty marsh Holocene fill ranges from 1 to 20 m (Figures 3 and 4; Frouin et al., 2007a). The thinnest deposits (< 1 m) are located in the centre of the peaty marsh to the north (T5 and T9). The thickest deposits (14 m to 20 m; T2, T3, T4, T14, T13, SMV2 and SMV3) are located to the northwest, on the east- ern part of the marsh (NW–SE profile) and to the south on the western part (N–S profile). The infilling thickness ranges from 2 m to 12m for the other drill-holes (T6, T7, T8, T10, T11 and T12). 720 Table 1 Radiocarbon ages of organic matter of the Marais Vernier obtained during the last 30 years Frouin et al. (2007a) link the variation in the Holocene fill thick- nesses to the shape of the pre-Holocene topography. There are at least three erosion levels (S1, S2 and S3) that have different shapes and elevations (Frouin et al., 2007a). The bottom of the Holocene sequence consists locally of sand, where the infill is thickest (SMV2, T4, T14, SMV3 and T13), and more widely of finer deposits with occasional intercalated peat layers. They are covered by a thick peat (7 m at its thickest) that contains intercalated minerogenic material to the west. This upper peat is overlain by fine minerogenic material south of the Hollandais dyke (T15, T16 and T21). Dating and infilling model The succession of radiocarbon ages within a given drill-hole agrees with the stratigraphy of the deposits (Figures 3 and 4; Table 1). It appears that we have not sampled reworked peat during drilling. The intercalated peat layers found above S3 are younger than the basal peat layer found above S2 at the same elevation on the N–S profile (Figure 3), and this may result from the com- paction of material in the area delineated by S3. The pre-Holocene topography thus results in different patterns of deposition, which are highlighted in a depth versus age graph (Frouin et al., 2007a). Before 5850–5710 cal. BC, deposition mainly took place in the area delineated by S3. We calculate a ver- tical accretion rate of 5.5 mm/yr. After 5850–5710 cal. BC, deposi- tion occurred on the wider area delineated by S2. We then note slower vertical accretion rates ranging from 2.5 mm/yr (above S3) to 3 mm/yr (above S2). The deposition rate above S3 was different to that above S2. Subsequently, the expanding area of peat accumulation reached S1; showing that the area delineated by S1 was an island during most of the Holocene period. Source of the material Mineralogical signature/minerogenic material Frouin et al. (2007b) identified three main sources of sediments, based on an examination of the clay mineral content of core SMV2 and a comparison with their likely sources (Figure 5A), gleaned from published regional syntheses (terrestrial formations: Lebret, 1984; Lautridou, 1985; Laignel et al., 1999, 2002; and estuarine to marine sediments: Lesourd, 2000; Garnaud, 2003). We find a pre-Weichselian loess source at the bottom of the core (mainly smectite and no chlorite), an estuarine source in the mid- dle (mainly illite) and a Weichselian loess source at the top (mainly smectite and chlorite). We use the same markers to study a new data set related to drill- holes T2, T3, T4, T5, T6, T7, T9, T11 and T14. New and published data suggest that (1) deposits have a pre-Weichselian loess source at the bottom of the Holocene fill; (2) almost all deposits have an estuarine source above this. Deposits at the top of SMV2 and T7 have a Weichselian loess source. Based on clay content, the sand body at the base of T4 has an estuarine origin. Therefore, we relate its shape to an estuarine channel, rather than adopt the previously published interpretation in terms of a debris-flow deposit (Frouin et al., 2007a). Geochemical signature/organic material We measure carbon, nitrogen and carbonate content on core C1. We use the C/N ratio values as a marker for the origin of the organic matter (Meyers, 1994; Tyson, 1995). The measurements show a terrestrial plant origin for the upper peat layers (C/N > 12 and no carbonate) and a non-terrestrial origin for the lower peat layer (C/N < 12 and carbonate-rich). The latter might be the result of an altered organic material or another source of carbon, such as dissolved organic carbon (Lamb et al., 2006). Textures and structures Textures of minerogenic deposits We compare the textures of the Marais Vernier samples with those of present-day depositional environments of the Lower Seine Valley: the beach environment located to the southwest of Honfleur, the subtidal flat near Le Havre and the tidal mudflats of Le Havre, Le Trait and Oissel (Figure 1; Deloffre, 2005; Dubrulle, 2007). All data were plotted on a clay-silt-sand diagram. Beach samples have a mainly sandy texture; subtidal flats have a silty texture and tidal mudflats have a silty-sand to sandy-silt texture (Figure 5B). Our samples have a silty-sand to sandy-silt texture, confirming that they were deposited in an environment similar to present-day mudflats. Laminated sequences Frouin et al. (2006) studied possible evidence for rhythmic deposition in a laminated section of SMV2, sub-Boreal in age. The varying lam- ina thickness shows two main periodicities (16 and 32 laminae per cycle). They are similar to tidal cycles, confirming the tidal character of material of estuarine origin. Although further work is needed to define which tidal cycles are effectively recorded in the area (either semi-diur- nal or fortnightly cycles), laminated sequences only represent a short period of deposition among periods of peat accumulation (fewer than 22 years for the 3.2 m thick laminated deposit of SMV2 studied). Palaeoecology Salinity of water Two different studies have described diatom content, one focused on the minerogenic material overlying the upper peat to the south of the Hollandais dyke (Elhai, 1963), and the other dealt with the 721 Figure 3 Description of two profiles resulting from surveys made between the late 1970s and early 2000s (Huault, 1980; Huault and Lefebvre, 1983a; Frouin et al., 2007a). The NW–SE profile (top right) was carried out in the area having a thick peat. The N–S profile (bottom) was carried out in the area where tidal channels disturbed the peat layer. Ages are expressed in yr 14C BP; corresponding calibrated ages can be found in Table 1 SMV2 core material (Huault, 1985). The minerogenic material to the south of the Hollandais dyke contained mainly freshwater species, such as Fragilaria brevistata. No diatoms have been found below the oldest peat layers of SMV2. Freshwater species, such as Fragilaria brevistata, were identified in the estuarine material found above the oldest peat lay- ers. Marine to brackish species, such as Melosira sulcata, Cocconeis scutellum and Dyploneis didyma, were identified in the later layers, in varying amounts. Vegetation and landscape Huault and Lefebvre (1983a) described the first pollen below the peat dated to 7000–6000 cal. BC. Herbaceous taxa are dominant and characterize a wet meadow (Figure 5C). Then, arboreal taxa become dominant and characterize a bordering forest. After 900 cal. BC (start of sub-Atlantic period), the bordering forest remained on the eastern part of the marsh, while a wet meadow, with plants characteristic of disturbance, developed on the western part. Facies and depositional environments The following paragraph is a summary of all information avail- able on the peaty marsh. First, we distinguish organic facies from minerogenic facies. Then, we distinguish two main facies within the minerogenic facies, based on the material source (ter- restrial or estuarine). We finally identify three organic facies and eight minerogenic facies; four having an estuarine source and four having a terrestrial source, considering all available infor- mation (Table 2). Based on the presence of visible plant fragments and material composition, we have identified three organic facies (O1 to O3). Facies O1 has no identifiable plant fragments, a fine laminated structure, a C/N ratio less than 12 and is carbonate-rich. We asso- ciate these features with a flooded carbonate-rich and organic- rich environment, interpreted as an open-water environment (cf. Teichumüller, 1982). Facies O2 has reed fragments, little carbon- ate and a C/N ratio greater than 12. These features characterize a reed-swamp environment. Facies O3 has wood fragments, little 722 Figure 4 Description of the other drill-holes and cores carried out in the area (top; Huault, 1980; Huault and Lefebvre, 1983a; Frouin et al., 2007a) and reconstruction of the infilling geometry (bottom). Ages are expressed in yr 14C BP; corresponding calibrated ages can be found in Table 1 carbonate and a C/N ratio greater than 12. These features charac- terize a marsh environment. Based on the structure and texture of the deposits, we have identified four facies that have an estuarine source. Facies T1 has a clayey-silt texture, many plant fragments and calcareous precipitates (travertines; Frouin et al., 2007b). We associate these features with a flooded carbonate-rich and vegetated envi- ronment, interpreted as an open-water environment. Facies T2 has a clayey-silt texture, homogeneous structure, some pre- served gastropod shells and freshwater diatoms. These features are similar to Miall's fcf facies (homogeneous mud with fresh- water molluscs) (Miall, 1992). It is therefore interpreted as a 723 Figure 5 Characterization of the deposits based on new and published data (Frouin et al., 2006, 2007b). (A) Material source is described based on an examination of the clay mineral content of Marais Vernier samples and a comparison with their likely sources. (B) Depositional environment is described based on an examination of textures of the Marais Vernier samples compared with those of present-day depositional environments in the Lower Seine Valley (Deloffre, 2005; Dubrulle, 2007). (C) Vegetation cover is described based on a review of previously published pollen assem- blages (Sebag, 2002). The following keys VI, VIIa, VIIb and VIII represent Boreal, Atlantic, sub-Boreal and sub-Atlantic, respectively freshwater pond protected from marine incursion. Facies T3 has a sandy-silt, laminated texture, plant imprints and fragments, and brackish diatoms tolerating periods of emersion. These features are interpreted as an intertidal environment. Facies T4 has a sandy-silt texture, laminated structure, which includes organic laminae coming from the eroded surrounding peat layer 724 Table 2 Facies description based on sedimentary and palaeobiological data, and associated depositional environments Ø, no available information. (Frouin et al., 2006), and brackish to marine diatoms. The geometry of T4 suggests that tidal channels have formed and disturbed the peat forming to the west. Based on the structure and texture of the deposits, we have identified three facies that have a terrestrial source, and associated a fourth facies with that group. Facies C1 has a sandy-gravel tex- ture and is only observed at the bottom of the Holocene fill. Regionally, this facies is related to periods of greater fluvial energy of the Seine River, resulting in bedload transport (Lefebvre et al., 1974, 1994; Lautridou et al., 1999; Antoine et al., 2007). Facies C2 has a sandy-clayey-silt texture, with irregular contacts marked by gravels and bedload structures. These features are sim- ilar to Miall's Gms facies (Miall, 1977, 1992) marking debris-flow deposits. Bedload structures suggest periods of sedimentation. These features are related to an abandoned channel infill. Facies C3 has a sandy-silt texture, laminated structure, many plant debris and brackish diatoms. Bioturbation becomes more and more important nearer to the surface, indicating a landward shift in the depositional environment. These features are related to a salt marsh environment. Facies C4 has a clayey-silt texture and fresh- water diatoms. It covers the upper peat, south of the Hollandais dyke. Though we do not have data on the clay content, it is inter- preted as a floodplain environment. Discussion Palaeoenvironmental evolution At the onset of the Holocene period, the abandoned meander of the Marais Vernier presents three levels of erosion, with different ele- vations and shapes (Figure 6). These surfaces are covered by a layer of gravel (facies C1) that forms the basement of the Holocene fill. There is no palaeoecological evidence in the Marais Vernier for the early Holocene. However, the landscape is regionally domi- nated by pine trees, with some hazel, oak and birch also present (Huault, 1972). 725 Figure 6 Summary of the facies succession observed in three different contexts. Core SMV2 shows the facies succession in the deepest part of the fill. Drill-hole T16 shows the facies succession near the Hollandais dyke. Drill-hole T11 shows the facies succession above surface S2 Before 7000–6000 cal. BC (SMV2, T17 and T3), we have the following facies succession: C2, T1 and undifferentiated O. The deposition of material derived from terrestrial sources is related to periods of erosion, suggested by the presence of colluvium fans in the landscape (Lefebvre, 1998). As a result, buried pre- Weichselian loess was eroded; debris-flows occurred, alternating with periods of deposition. Then, in the low-lying area delineated by S3 (facies T1), there was a change in the source of material from terrestrial to estuarine. Soon after this change in the material origin, we have the first palaeoecological evidence. A reed-swamp developed, followed by a marsh contemporary with the presence of oak, hazel and elm in the surrounding woodland (Huault and Lefebvre, 1983a; Huault, 1985). This change was accompanied by peat formation in low-lying areas (undifferentiated facies O, 7000 – 6000 cal. BC). Meantime, terrestrial material continued to accu- mulate in the area delineated by S2. After 7000–6000 cal. BC, a mixed oak woodland characterized the landscape of the area surrounding the Marais Vernier (Huault and Lefebvre, 1983a; Huault, 1985), corresponding to other regional records (Huault, 1972). Just before 5850–5710 cal. BC (T11), estuarine material began to be deposited above the area delineated by S2 (undifferentiated facies T). Between 5520 and 3700 cal. BC (T8, T4, T11, T13, T14, T17), peat started to accumulate in the area (facies O2 and O3), and this marked the onset of a long-lasting period of paludification that is still active today. To the west, where an open-water environment (O1) has been recorded, peat formation was interrupted by devel- oping tidal channels (facies T4 and then facies C3). The terrestrial source of the upper part of the channel points to erosion of surfi- cial Weichselian loess. From 900 cal. BC (start of sub-Atlantic period), in the western part of the marsh only, some pollen characteristic of disturbance by human activities is found (Huault and Lefebvre, 1983a). Finally, minerogenic material locally settles above the peat layer, because of flood episodes (C4). Until 5850–5710 cal. BC (T11), we note a retrogradational shifting of the shoreline. After 5850–5710 cal. BC (T11), we note an aggrading sequence. The sedimentary evolution of the area suggests a high water-table, which led to the accumulation of organic matter, and some estuar- ine flooding, leading to estuarine, minerogenic sedimentation. External forcing and local controls on the Holocene evolution of the peat marsh Our work enables us to relate the palaeoenvironmental evolution of the marsh to different forcing processes and controls, such as the role of climate and the related vegetation cover, sea-level rise, pre-Holocene topography, sedimentary budget, water-table level and, to a lesser extent, human action. Deposition of terrestrial material is associated with erosion of the surrounding plateau. Before 7000–6000 cal. BC, there is little evidence of human occupation in the Lower Seine Valley (Billard et al., 2001; Sebag, 2002). Studies show the presence of hunter- gatherer people, who had little impact on the wooded landscape. Climate changes appear as the main forcing factor, explaining the formation of colluvial fans and erosion of the pre-Weichselian loess (Frouin et al., 2007b). After 7000–6000 cal. BC, people set- tled and, as indicated by Allard et al. (2001) and Sebag (2002), when people settle, they start clearing the landscape to increase their agricultural space. Their modification of the landscape increased the impact of climate changes, so that erosion took place everywhere on the plateau, supplying the marsh with surficial Weichselian loess (Frouin et al., 2007b). There is little evidence of direct human occupation of the peat marsh. Penna (2003) shows that the mist rising from the marsh has been the source of several myths in the area. For that reason, peo- ple long believed the area to be unsuitable for occupation. The area therefore remained free of human intervention until the build- ing of the Hollandais dyke during the seventeenth century, to drain the marsh and provide more space for agriculture. Apart from these periods of terrestrial supply, the influence of cli- mate changes or climate–anthropogenic related changes is difficult to identify, as other causes become dominant. Accommodation and water-table level changes then become the most important factors. 726 Accommodation changes depend on pre-Holocene topography, sea level, sedimentary budget and, to a lesser extent, compaction (pres- ence of compressible peaty material; Allen, 1999). Pre-Holocene topography and sea-level rise have also influ- enced the sedimentary evolution of the marsh. Before 5850–5710 cal. BC, estuarine material accumulated only in low-lying areas, while terrestrial material was deposited elsewhere (Frouin et al., 2007b). Around 5850–5710 cal. BC, estuarine material began to accumulate everywhere in the peat marsh, indicating a sea level higher than the altitude of surface S2 (Frouin et al., 2007a). Regionally, the period is contemporary with the flooding of the Seine estuary mouth (Delsinne, 2005). After 5850–5710 cal. BC, estuarine material rapidly filled the new accommodation, leading to peat formation because of a high water-table noted regionally (Huault and Lefebvre, 1983b; Sebag, 2002). These changes were accompanied by a global decline in the sea-level rise (eg, Pirazzoli, 1991; Mörner, 1995), following which spit barriers formed in open-coastal environments and peat accumulated behind (Denys and Baeteman, 1995; Allen, 2000; Baeteman and Declercq, 2002; Waller and Long, 2003). Therefore creation of accommodation has resulted in minerogenic sedimen- tation, while filling up of accommodation and a local high water- table level have resulted in organic accumulation. To explain tidal channel conditions to the west, Huault and Lefebvre (1983a) have suggested the presence of a natural pro- tecting barrier running across the entire area, with a break to the west. However, there is no evidence yet to support the presence of such a barrier, and the presence of tidal channels might simply result from a local disequilibrium (local increase of sediment sup- ply) or a slight elevation difference between the two parts of the marsh; the western part of the marsh having a lower elevation than the eastern one. Conclusions The Marais Vernier has one of the thickest Holocene deposits in the Lower Seine Valley (from the Boreal period to present day). Based on 1980s studies, the palaeoenvironmental evolution of the peat marsh was believed to be the result of positive pulses of sea- level rise coupled with periods of sea-level stability. However, our evidence indicates that the sedimentary evolution is also influ- enced by: (1) periods of minerogenic deposition in response to creation of accommodation; (2) periods of non-deposition, where non-peat-forming plants progressively invaded an infilled area; (3) periods of organic accumulation (peat formation). Our study shows that the evolution of the Marais Vernier can be summarized into five phases: (1) Before 7000–6000 cal. BC, only terrestrial material settled in the abandoned fluvial channel through colluvium fans. Vegetation cover, climate changes and pre-Holocene topography are the main controls. (2) Just before 7000–6000 cal. BC, estuarine material was deposited in low-elevated areas, while terrestrial material contin- ued to accumulate elsewhere. As well as the previously mentioned controls, sea level and sediment availability also affected the area. Estuarine environments developed, marking a retrograding sequence. (3) Around 5850–5710 cal. BC, estuarine material was being deposited everywhere. Sea level and the sediment budget became the main controls. The period matches a maximum flooding event. (4) From 5520 to 3700 cal. BC, peat started to accumulate, giv- ing the present peaty marsh. The extensive accommodation space filled up rapidly following a global decrease in the rate of sea- level rise. The thick peat is the result of a regional high water-table level. Local estuarine sediments are also recorded (between 4230 and 1700 cal. BC), showing the influence of the tide in the area. (5) From 1130 to 900 cal. BC, peat continued to accumulate. Climate changes were the dominant forcing but a late human influence is also recorded in the area. The Marais Vernier has a long Holocene palaeoenvironmental record that has been only recently affected by human action. It can therefore be used as a reference site for further studies of the entire Lower Seine Valley and allow better characterization of the impact of human activities on the landscape and depositional environments. Acknowledgments We would like to thank all colleagues and students that helped us in the field to collect all samples. We also would like to thank Dominique Lefebvre and Cecile Baeteman for their useful com- ments on an earlier version of the paper. We appreciated the comments and suggestions provided by John Rees, as external reviewer and Frank Oldfield. We would like to thank Barbara Silva and Anne Hickley for their help with the English. This paper is a contribution to the INQUA Commission on Coastal and Marine Processes; and to IGCP Project 495 `Quaternary Land–Ocean Interactions: Driving Mechanisms and Coastal Responses'. 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Since the 1940s, several authors have studied the largest wetland of the Seine estuary, the Marais Vernier, to understand depositional environments during Holocene infilling. We reinterpret previous research based on new and published data (for example fill thickness and material source) to (1) describe facies and depositional environments; (2) reconstruct palaeoenvironmental evolution; (3) show the influence of local and global forcing on depositional environments. Before 7000—6000 cal. BC, terrestrial material was deposited because of catchment erosion related to changes in climate. Just before 7000—6000 cal. BC, estuarine material began to be deposited in low-lying areas in response to sea-level rise, while terrestrial material still settled at higher elevations. After this, but before 5850—5710 cal. BC, estuarine material areas began to accumulate at both high and low elevations. This marked a general flooding of the Marais Vernier, synchronous with that at the Seine estuary mouth. Soon after, peat accumulated over a wide area as a response to a local change in accommodation and a worldwide drop in sea level. A tidal channel developed to the west of the Marais Vernier, providing minerogenic material. After 1130—900 cal. BC, human influence becomes increasingly clear in the record. This record of regional change during the Holocene can serve as a reference for further studies in the area.</abstract><subject><genre>keywords</genre><topic>Wetland evolution</topic><topic>depositional environments</topic><topic>inherited topography</topic><topic>climate</topic><topic>sea-level rise</topic><topic>Holocene</topic><topic>Lower Seine Valley</topic><topic>France.</topic></subject><relatedItem type="host"><titleInfo><title>The Holocene</title></titleInfo><genre type="journal">journal</genre><identifier type="ISSN">0959-6836</identifier><identifier type="eISSN">1477-0911</identifier><identifier type="PublisherID">HOL</identifier><identifier type="PublisherID-hwp">sphol</identifier><part><date>2009</date><detail type="volume"><caption>vol.</caption><number>19</number></detail><detail type="issue"><caption>no.</caption><number>5</number></detail><extent unit="pages"><start>717</start><end>727</end></extent></part></relatedItem><identifier type="istex">684E705A0AA21EAA0E713B4A69728A9C1614D80E</identifier><identifier type="DOI">10.1177/0959683609105295</identifier><identifier type="ArticleID">10.1177_0959683609105295</identifier><recordInfo><recordContentSource>SAGE</recordContentSource></recordInfo></mods></metadata><serie></serie></istex></record>Pour manipuler ce document sous Unix (Dilib)
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