Millena Frouin
CRC-LRMH USr 3224 sorbonne université, Pôle Grottes Ornées, Department Member
- Geography, Geology, Sedimentology, GeoArcheology, Archaeology, Architecture, and 13 moreMedieval History, Medieval Studies, Effects of Geography and Geology on Human Settlements, Geomatics, Landscape Archaeology, Geoarchaeology, Environmental Archaeology, Palaeoenvironment, Paleoenvironment, Fluvial Sedimentology, Quaternary Sedimentology and Geomorphology, Lithic Raw Material Sourcing, and Archaeological Scienceedit
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Inca platforms forming part of an architectural complex commonly defined by the term usnu are in ethnohistorical sources described as being associated with ritual events involving performances of speech, music and dance. This paper... more
Inca platforms forming part of an architectural complex commonly defined by the term usnu are in ethnohistorical sources described as being associated with ritual events involving performances of speech, music and dance. This paper reviews the performance role, its relevance and function and discusses their effectiveness with respect to the use of sound, based on experimental use of the human voice, the drum and a shell trumpet at a number of these sites. It is demonstrated that sound was a factor of some importance in the planning of the site of Usccunta and indeed that a particular instrument, the shell trumpet or pututu may have been considered in the layout of the largest communal space here.
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Post-glacial climate changes and sea-level fluctuations have strongly influenced N-W European environments and sedimen- tation. To these natural events, increasing anthropogenic pressure has to be added. Forest clearance and... more
Post-glacial climate changes and sea-level fluctuations have
strongly influenced N-W European environments and sedimen-
tation. To these natural events, increasing anthropogenic
pressure has to be added. Forest clearance and agricultural
development are the main factors responsible for the erosional
processes in Northwest Europe. This article analyses Holocene
sequences of the Lower Seine Valley (LSV) (Paris Basin) to
understand better the origin of detrital and terrigenous input
and how much humans have contributed to it. Three main
sectors of the LSV are analysed: estuarine, fluvial and tributar-
ies. Since Neolithic times, there are seven erosional phases that
can be identified and essentially linked to human pressure.
strongly influenced N-W European environments and sedimen-
tation. To these natural events, increasing anthropogenic
pressure has to be added. Forest clearance and agricultural
development are the main factors responsible for the erosional
processes in Northwest Europe. This article analyses Holocene
sequences of the Lower Seine Valley (LSV) (Paris Basin) to
understand better the origin of detrital and terrigenous input
and how much humans have contributed to it. Three main
sectors of the LSV are analysed: estuarine, fluvial and tributar-
ies. Since Neolithic times, there are seven erosional phases that
can be identified and essentially linked to human pressure.
The response of coastal systems to allogenic forcing factors is of interest to diverse research communities, including those interested in global change, sequence stratigraphy and modelling. Quaternary systems are of particular interest... more
The response of coastal systems to allogenic forcing factors is of interest to diverse research communities, including those interested in global change, sequence stratigraphy and modelling. Quaternary systems are of particular interest because they provide analogues for ancient rock records. To understand the processes responsible for the sedimentary evolution of estuarine systems, it is necessary to study as many fluvial systems as possible. The objective of this review of the sedimentary evolution of a coastal marsh is to describe the influence of glacial paleotopography on the record of climatic and sea-level changes. The Marais Vernier, located at the interface between the marine and fluvial parts of the estuary, is a part of the Lower Seine Valley wetland network, which formed after the Last Glacial Maximum. Previous studies have described the Holocene filling, which is composed of peat and detrital material deposited following climatic and sea-level changes. To understand the sedimentary evolution, a paleotopographical (based on drillings and electromagnetic surveys) and a chronological framework (based on radiocarbon dates) for the southern peat marsh were defined. The peat marsh paleotopography has three erosional surfaces. The S1 surface is the oldest and also the highest, topographically; the S2 surface is younger, wider, and incised below the S1 surface; the S3 surface, the youngest of the three, is narrow and deeply incised. Radiometric ages were considered on the basis of their geographical position in relation to the S3 surface.
Prior to 7.5 ka cal BP, sediments accumulated only above the narrow area described by the S3 surface, at a rate of 5.5 mm yr−1. After 7.5 ka cal BP, shortly after the flooding of the Seine estuary, sediments accumulated as peat deposits over the entire peat marsh at a rate of 3 mm yr−1 in response to the sea-level rise. The paleotopography delimits the area of deposition during the Holocene, and thus plays a critical role in determining the vertical accretion rate expressed as a thickness: prior to 7.5 ka cal BP, the vertical accretion rate (5.5 mm yr−1) was less than that observed for the Seine estuary (6.8 mm yr−1). However, rate of sea-level rise and sediment supply, which also affects sediment accumulation rates, vary in northwestern Europe during the Holocene. Therefore, although the Marais Vernier is a good illustration of paleotopographic influence, the effects of autocompaction, sea level and sediment supply complicate efforts to quantify the degree to which it controls sediment accumulation.
Prior to 7.5 ka cal BP, sediments accumulated only above the narrow area described by the S3 surface, at a rate of 5.5 mm yr−1. After 7.5 ka cal BP, shortly after the flooding of the Seine estuary, sediments accumulated as peat deposits over the entire peat marsh at a rate of 3 mm yr−1 in response to the sea-level rise. The paleotopography delimits the area of deposition during the Holocene, and thus plays a critical role in determining the vertical accretion rate expressed as a thickness: prior to 7.5 ka cal BP, the vertical accretion rate (5.5 mm yr−1) was less than that observed for the Seine estuary (6.8 mm yr−1). However, rate of sea-level rise and sediment supply, which also affects sediment accumulation rates, vary in northwestern Europe during the Holocene. Therefore, although the Marais Vernier is a good illustration of paleotopographic influence, the effects of autocompaction, sea level and sediment supply complicate efforts to quantify the degree to which it controls sediment accumulation.
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A 20 m thick core drilled in the Vernier Marsh allowed us the study of the Holocene infilling downstream the lower Seine valley. This core presents an alternation of peats and detrital deposits. These detrital deposits were... more
A 20 m thick core drilled in the Vernier Marsh allowed us the study of the Holocene infilling downstream the lower Seine valley. This core presents an alternation of peats and detrital deposits. These detrital deposits were sedimentologically characterized (e. g.
grain-size, clay mineral, carbonate . . .) what allowed us to define three different units: (i) the core bottom presents a great proportion of sand, carbonate and smectite and no chlorite; (ii)
the median part of the core presents chlorite and a great proportion of illite and silt; (iii) the core top presents chlorite and a great proportion of smectite and sand. These three units were
the result of different sedimentary dynamics (i. e. material source and particle transport dynamic). The clay mineral contents used as indicators of the material source were compared to these of regional formations (i. e. loess, clay-with-flints, chalk and suspended particle matter) what enabled us to distinguish: (i) a continental supply resulting from the erosion of the watershed (i. e. loess) in the core bottom dated from the Boreal and in the core top dated from the Upper Subboreal; (ii) an estuarine supply in the median part dated from the Upper Boreal to the Lower Subboreal. The grain-size distribution principally indicated a particle transport by suspension in the entire core to which a transport by traction that occurred in coarse detrital deposits was added.
grain-size, clay mineral, carbonate . . .) what allowed us to define three different units: (i) the core bottom presents a great proportion of sand, carbonate and smectite and no chlorite; (ii)
the median part of the core presents chlorite and a great proportion of illite and silt; (iii) the core top presents chlorite and a great proportion of smectite and sand. These three units were
the result of different sedimentary dynamics (i. e. material source and particle transport dynamic). The clay mineral contents used as indicators of the material source were compared to these of regional formations (i. e. loess, clay-with-flints, chalk and suspended particle matter) what enabled us to distinguish: (i) a continental supply resulting from the erosion of the watershed (i. e. loess) in the core bottom dated from the Boreal and in the core top dated from the Upper Subboreal; (ii) an estuarine supply in the median part dated from the Upper Boreal to the Lower Subboreal. The grain-size distribution principally indicated a particle transport by suspension in the entire core to which a transport by traction that occurred in coarse detrital deposits was added.
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... more
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.
This record of regional change during the Holocene can serve as a reference for further studies in the area.
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Quaternary climato-eustatic oscillations and tectonic movements result in base-level changes that modify the shape of fluvial systems. At the onset of the Holocene, NW European fluvial systems were deeply incised and comprised several... more
Quaternary climato-eustatic oscillations and tectonic movements result in base-level changes that modify the shape of fluvial systems. At the onset of the Holocene, NW European fluvial systems were deeply incised and comprised several terraces. Some terraces now lie beneath the estuary that formed in response to the Holocene sea-level rise.
The macrotidal estuary of the Seine River is one example of that NW European fluvial valley evolution. Although the system has been extensively studied over the last 40 years, no study has drawn together all the research on its Holocene evolution. We gathered available data on five sites distributed across the system, in order to discuss that evolution and the related forcing factors. We have identified four main phases. (1) Prior to 6000 BC, there was a retrogradational shifting of the shoreline, where pre-Holocene topography and the sea level were the main forcing factors. Only depositional environments of low-elevated areas were affected by the influence of the sea-level rise, while the others were affected by climatic changes. (2) Around 6000-5000 BC, there was a maximum flooding event, where all depositional sites were affected by the influence of the sea-level rise. (3) Between 5000 and 1100 BC, there was an aggrading sequence, where tide and local hydrological conditions were the main forcing factors. The deposition record indicates that there were open tidal environments toward the sea, while landward peat accumulated, and was sometimes disturbed by tidal channel formation. (4) From 1100 BC, there was a progradational shifting of the shoreline, where human activity was the main forcing factor. Seaward environments at this time still indicate open-tidal conditions, while landward ones show a return to clastic deposits related to floodplain deposition. All the 14C data accumulated in the area should allow us to present a regional sea-level curve in the near future.
The macrotidal estuary of the Seine River is one example of that NW European fluvial valley evolution. Although the system has been extensively studied over the last 40 years, no study has drawn together all the research on its Holocene evolution. We gathered available data on five sites distributed across the system, in order to discuss that evolution and the related forcing factors. We have identified four main phases. (1) Prior to 6000 BC, there was a retrogradational shifting of the shoreline, where pre-Holocene topography and the sea level were the main forcing factors. Only depositional environments of low-elevated areas were affected by the influence of the sea-level rise, while the others were affected by climatic changes. (2) Around 6000-5000 BC, there was a maximum flooding event, where all depositional sites were affected by the influence of the sea-level rise. (3) Between 5000 and 1100 BC, there was an aggrading sequence, where tide and local hydrological conditions were the main forcing factors. The deposition record indicates that there were open tidal environments toward the sea, while landward peat accumulated, and was sometimes disturbed by tidal channel formation. (4) From 1100 BC, there was a progradational shifting of the shoreline, where human activity was the main forcing factor. Seaward environments at this time still indicate open-tidal conditions, while landward ones show a return to clastic deposits related to floodplain deposition. All the 14C data accumulated in the area should allow us to present a regional sea-level curve in the near future.
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Trois fenêtres furent ouvertes lors de la fouille couvrant une surface totale de 13 215 m². La fenêtre 1, concentrait la majeure partie des structures archéologiques (quelques unes attribuables au Néolithique récent d’après l’étude... more
Trois fenêtres furent ouvertes lors de la fouille couvrant une surface totale de 13 215 m². La fenêtre 1, concentrait la majeure partie des structures archéologiques (quelques unes attribuables au Néolithique récent d’après l’étude céramique et le reste associé au premier âge du Fer) ainsi que deux zones de concentration en silex (une attribuée au Paléolithique supérieur et l’autre au Néolithique moyen, récent ou final). Les fenêtres 2 et 3, d’une surface cumulée de 6 057 m², comprenaient la majeure partie du mobilier isolé collecté lors de la fouille (chaque pièce fut relevé dans les trois dimensions de l’espace) et quelques rares structures archéologiques associées au premier âge du Fer (puits, fosse et fossé). Des relevés géomorphologiques et des prélèvements furent également effectués dans ces fenêtres afin de documenter l’évolution paysagère dans ce secteur de la vallée de la Marne. La collecte exhaustive du mobilier archéologique dans les horizons identifiés comme riches n’a pas permis de mettre en évidence une micro-stratigraphie/organisation des vestiges (âge vs. profondeur). Ceci est sans doute en grande partie lié au nombre limité d’artefacts isolés finalement attribuables chronologiquement. Les études entreprises montrent une fréquentation des lieux dès le Paléolithique supérieur. Cette période, marquée par un réseau fluviatile en tresse d’où émergent des « îlots » sableux entre les chenaux, est représentée par une zone de concentration en silex, occupant une surface d’environ 15 m², dont l’agencement des pièces témoigne d’une spatialisation de l’activité (débitage et rejet d’une part et découpe de matière et travail de la peau d’autre part). Si aucun indice d’une occupation des lieux au Mésolithique ne fut identifié, il est à noter la persistance dans le paysage et dans le temps de l’« îlot » sableux, sur lequel la zone de concentration en silex du Paléolithique supérieur fut identifiée et en arrière duquel s’installent dès le début de l’Holocène un marécage bien drainé. Au moins au Néolithique, le réseau fluviatile en tresse laisse sa place à un réseau à méandres à sédimentation fine, dont une boucle fut recouvrée dans les diagnostics voisins. L’emprise est fréquentée dès le Néolithique moyen II et ce jusqu’au Néolithique final pour des activités de débitage. La collecte exhaustive du mobilier permet d’illustrer l’organisation spatiale des espaces de débitage (vaste étendue dans la fenêtre 2 et plus restreinte dans la fenêtre 1 – notamment une zone de concentration lithique d’une étendue d’environ 12 m²), en dehors des zones d’habitat ou d’extraction généralement documentées. Si au Paléolithique supérieur la matière première est essentiellement locale et plutôt du silex secondaire, elle se diversifie au Néolithique avec du matériel local et divers (silex secondaire comme tertiaire) et du matériel lointain (silex pressignien). L’âge du Bronze est très timidement représenté par du mobilier isolé (métal et céramique). Le premier âge du Fer est lui bien représenté sur l’emprise aussi bien en termes de mobilier isolé que de structures associées. Il semble former un ensemble homogène auquel nous avons associé les structures pour lesquelles l’absence de mobilier ne permit pas une attribution chronologique certaine. Cet ensemble comprend des structures d’extraction de matière, des puits pour l’accès à l’eau et une vaste aire de stockage au nord de l’emprise – fenêtre 1 – constituée quasi-exclusivement de greniers sur poteaux rattachés au Hallstatt moyen/final. Le secteur semble ensuite déserté, bien que ponctuellement fréquenté, au 2nd âge du Fer et à l’époque gallo-romaine. Aucun vestige médiéval n’a été recouvré sur l’emprise.
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Des enregistrements sédimentaires de l’évolution du climat postérieure au dernier maximum glaciaire ont été étudiés en trois régions du Niger : la vallée de l’Azawagh et le massif de Termit localisés sur la limite actuelle Sahara-Sahel... more
Des enregistrements sédimentaires de l’évolution du climat postérieure au dernier maximum glaciaire ont été étudiés en trois régions du Niger : la vallée de l’Azawagh et le massif de Termit localisés sur la limite actuelle Sahara-Sahel (environ 100mm.an-1), la partie méridionale du Manga à la limite sud actuelle du Sahel (environ 400mm.an-1). A l’Holocène inférieur, dans un contexte climatique humide (« Sahara Vert »), on observe néanmoins l’existence d’une dynamique sédimentaire éolienne considérée comme liée à l’aridité. L’enregistrement de cette dynamique sédimentaire éolienne est variable selon la latitude (gradient climatique) mais aussi selon les caractéristiques propres à chaque géosystème (topographie, morphologie, lithologie, hydrogéologie). La présence constante de poussières éoliennes, même pendant le maximum humide, implique la permanence de zones où le couvert végétal était, au moins saisonnièrement, insuffisant pour assurer la protection du substratum. Dans l’Azawagh, ...
La plaine champenoise crayeuse présente actuellement une végétation de milieu ouvert, très marquée par les activités anthropiques et notamment la culture céréalière. La quasi-absence de végétation climacique dans cette zone géographique... more
La plaine champenoise crayeuse présente actuellement une végétation de milieu ouvert, très marquée par les activités anthropiques et notamment la culture céréalière. La quasi-absence de végétation climacique dans cette zone géographique entraîne des débats controversés, notamment sur un possible indigénat du pin (Bouderias et Timbal 1980 ; Couderc 1985). Les analyses anthracologiques menées sur des chantiers étudiés par l’Inrap (Institut national de recherches archéologiques préventives) entre 2011 et 2014, dans le département de la Marne (51) permettent d’enrichir le débat. Les résultats obtenus sur sept sites archéologiques, datés du Néolithique au deuxième âge du Fer (La Tène C2), ont révélé une présence importante des charbons du Pinus sp./ Pinus cf. sylvestris. Le pin occupait donc une place relativement importante dans les espaces boisés en association avec le chêne à feuillage caduque (Quercus sp., type caducifolius). Cette persistance du pin dans la composition des massifs f...
... David Sebag 1 , Benoît Laignel 1 , Christian Di-Giovanni 2 , Alain Durand 1 , Millena Frouin 1. (2003). Except ancient tectonic structures, the main morphological elements of the western Paris Basin are essentially associated to the... more
... David Sebag 1 , Benoît Laignel 1 , Christian Di-Giovanni 2 , Alain Durand 1 , Millena Frouin 1. (2003). Except ancient tectonic structures, the main morphological elements of the western Paris Basin are essentially associated to the Quaternary periglacial climates. ...