Simon Andrieu
email: simon.andrieu@u-psud.fr

Benjamin Brigaud

Jocelyn Barbarand

Eric Lasseur

Thomas Saucède

Disentangling the control of tectonics, eustasy, trophic conditions and climate on shallow-marine carbonate production during the Aalenian-Oxfordian interval: from the western France platform to the western Tethyan domain

Keywords: Carbonate platform, Facies, Sequence stratigraphy, Tectonics, Jurassic

The objective of this work is to improve our understanding of the processes controlling changes in the architecture and facies of intracontinental carbonate platforms. We examined the facies and sequence stratigraphy of Aalenian to Oxfordian limestones of western France.

Seventy-seven outcrop sections were studied and thirty-one sedimentary facies identified in five depositional environments ranging from lower offshore to backshore. Platform evolution was reconstructed along a 500 km cross-section. Twenty-two depositional sequences were identified on the entire western France platform and correlated with European third-order sequences at the biozone level, demonstrating that eustasy was the major factor controlling the cyclic trend of accommodation. The tectonic subsidence rate was computed from accommodation measurements from the Aalenian to the Oxfordian in key localities.Tectonism controlled the sedimentation rate and platform architecture at a longer time scale. Tectonic subsidence triggered the demise of carbonate production at the Bathonian/Callovian boundary while the uplift made possible the recovery of carbonate platform from Caen to Le Mans during the mid Oxfordian. Topography of the Paleozoic basement mainly controlled lateral variations of paleodepth within the western France platform until the mid Bathonian. A synthesis of carbonate production in the western Tethyan domain at that time was conducted. Stages of high carbonate production during the Bajocian/Bathonian and the middle to late Oxfordian are synchronous with low δ 13 C, high eccentricity intervals, and rather dry climate promoting (1) evaporation and carbonate sursaturation, and (2) oligotrophic conditions. Periods of low carbonate production during the Aalenian and from the middle Callovian to early Oxfordian correlate with high δ 13 C and low eccentricity intervals, characterized by wet climate and less oligotrophic conditions. Such conditions tend to diminish growth potential of carbonate platforms. This work highlights the importance of climate control on carbonate growth and demise at large scale in western Tethyan epicontinental seas.

42

Introduction

In recent decades, numerous studies have been conducted on Jurassic carbonate platforms of the Western Tethys to characterize their architectures, facies, and discontinuities. They highlighted the importance of interactions among the multiple processes that control the evolution of carbonate depositional systems, that is: (1) eustasy, (2) tectonism in that it modifies accommodation, and (3) environmental conditions including seawater temperature, depth, salinity, chemistry, trophic conditions and productivity, with this last aspect determining the nature of carbonate producers and production rates [START_REF] Pomar | Types of carbonate platforms: a genetic approach[END_REF][START_REF] Brigaud | Facies and climate/environmental changes recorded on a carbonate ramp: A sedimentological and geochemical approach on Middle Jurassic carbonates[END_REF][START_REF] Carpentier | Sequential and climatic framework of the growth and demise of a carbonate platform: implications for the peritidal cycles (Late Jurassic, North-eastern France)[END_REF]. Deciphering the precise influence of each factor on depositional sequences, on carbonate platform architecture, growth, and demise, and on facies distribution and composition is still a challenge [START_REF] Mutti | Carbonate systems along nutrient and temperature gradients: some sedimentological and geochemical constraints[END_REF][START_REF] Léonide | Interaction of tectonics, eustasy, climate and carbonate production on the sedimentary evolution of an early/middle Jurassic extensional basin (Southern Provence Sub-basin, SE France)[END_REF][START_REF] Merino-Tomé | Sequence development in an isolated carbonate platform (Lower Jurassic, Djebel Bou Dahar, high Atlas, Morocco): influence of tectonics, eustacy and carbonate production[END_REF], especially because accommodation and carbonate production are interdependent factors [START_REF] Pomar | Types of carbonate platforms: a genetic approach[END_REF]. For instance, intracratonic basins were considered stable until recent studies showed that tectonics influenced sedimentation [START_REF] Guillocheau | Meso-Cenozoic geodynamic evolution of the Paris Basin: 3D stratigraphic constraints[END_REF][START_REF] Carcel | Tectonic and eustatic control on a mixed silicoclasticcarbonate platform during the Late Oxfordian-Kimmeridgian (La Rochelle platform, western France)[END_REF][START_REF] Brigaud | Growth and demise of the Jurassic carbonate platform in the intracratonic Paris Basin (France): Interplay of climate change, eustasy and tectonics[END_REF][START_REF] Wright | A new section through the Corallian Group (Oxfordian, Upper Jurassic) rocks of Calne, Wiltshire, southern England[END_REF].

Nevertheless, determining the specific control of tectonics on carbonate platform development is complex, especially because vertical movements are of low amplitude and detected over long wavelengths. Moreover, the control of the inherited basement structure over the architecture of carbonate platform is rarely discussed [START_REF] Allenbach | The ups and downs of "Tectonic Quiescence" -recognizing differential subsidence in the epicontinental sea of the Oxfordian in the Swiss Jura Mountains[END_REF].

Western Tethyan carbonate platforms underwent several stages of growth and demise during the Jurassic, which are particulary well-marked in the Paris Basin [START_REF] Brigaud | Growth and demise of the Jurassic carbonate platform in the intracratonic Paris Basin (France): Interplay of climate change, eustasy and tectonics[END_REF].

However, no large-scale synthesis of such changes in sedimentation patterns and facies has been conducted, while it could provide new insights on the main factors controlling the type of carbonate producers and production rate.

From the Aalenian to the Oxfordian (about 17 My, [START_REF] Gradstein | The geologic time scale 2012[END_REF], a vast carbonate platform developed in western France. Several stratigraphic studies based on the distribution of ammonite and brachiopod species provide a precise and reliable biostratigraphic framework within which to study the evolution of this platform at the biozone level. However, such studies remain limited to specific geographic areas or stages (Caen to Alençon: [START_REF] Dugué | Géodynamique d'une bordure de massifs anciens. La bordure occidentale du Bassin angloparisien au Callovo-Oxfordien[END_REF][START_REF] Rioult | Outcrop sequence stratigraphy of the Anglo-Paris Basin Middle to Upper Jurassic (Normandy, Maine, Dorset)[END_REF][START_REF] Préat | Iron bacterial and fungal mats, Bajocian stratotype (Mid-Jurassic, northern Normandy, France)[END_REF][START_REF] Dugué | Le massif armoricain dans l'évolution mésozoïque et cénozoïque du Nord-Ouest de l'Europe. Contrôles tectonique, eustatique et climatique d'un bassin intracratonique[END_REF]Poitiers region: Mourier, 1983;[START_REF] Lorenz | Le Dogger du Berry, contribution à la connaissance des plate-formes carbonatées européennes du Jurassique[END_REF][START_REF] Gonnin | Les facteurs de contrôle de la sédimentation au début du Jurassique moyen sur le seuil du Poitou et ses abords[END_REF][START_REF] Gonnin | Stratigraphie séquentielle des séries du Bajocien inférieur au Bathonien moyen du seuil du Poitou et de son versant aquitain (France)[END_REF][START_REF] Gonnin | La stratigraphie séquentielle, outil régional complémentaire de la biostratigraphie : application à la reconstitution de la dynamique sédimentaire des séries bathoniennes de surface du seuil du Poitou (France)[END_REF][START_REF] Lenoir | Faciès, géométries et déformations du Sud-Ouest du bassin de Paris : un domaine faiblement subsident, transition avec le bassin d'Aquitaine[END_REF]; Saint-Maixent l'École to Montbron [START_REF] Foucher | Géodynamique sédimentaire et évolution paléogéographique de la plate-forme nord-est aquitaine au Jurassique moyen (Charente, Dordogne), tome II : Planches[END_REF][START_REF] Faugeras | Evolution de la plate-forme carbonatée est-aquitaine du Jurassique Moyen en Périgord. Stratigraphie, sédimentologie, paléogéographie[END_REF][START_REF] Branger | La marge nord-aquitaine et le seuil du Poitou au Bajocien : Stratigraphie séquentielle, évolution biosédimentaire et paléogéographie[END_REF]. The western France platform has tremendous potential for improving our understanding of Jurassic intracratonic carbonate systems because (1) it offers a continuous record of 17 My that can be studied through numerous outcrops and boreholes with a good time control based on biostratigraphy, (2) it rests upon a highly structured Hercynian basement, and (3) it has never been studied as a whole.

The first objective of this work is to reconstruct changes in facies and architecture of the western France platform and to determine the respective influences of eustasy, tectonics, environmental conditions, and the topography of the Paleozoic basement on platform evolution. The second objective is to compare our results at broad scale with other platforms in western Tethyan epicontinental sea. Facies were described and classified so as to define depositional environments. A 500 km-long north-south cross-section from Deauville to Montbron is examined within a sequence stratigraphy framework to model the evolution of the platform from the Aalenian to the Oxfordian. Four accommodation curves are established to quantify the amplitude of vertical movements and precisely identify tectonic control over the evolution of this intracontinental carbonate platform. A synthesis of sedimentation patterns in western Tethyan domain during the Middle Jurassic and the Oxfordian is conducted and a large-scale model for western Tethyan carbonate platforms evolution is provided.

Geological setting

The Paris and Aquitaine Basins are two intracontinental sedimentary basins filled with Triassic to Quaternary deposits. They developed respectively over a Cadomian and Variscan basement (Paris Basin, [START_REF] Guillocheau | Meso-Cenozoic geodynamic evolution of the Paris Basin: 3D stratigraphic constraints[END_REF] and a Variscan basement (Aquitaine Basin, [START_REF] Biteau | The Aquitaine Basin[END_REF]. The study area stretches from Deauville, in the northwestern Paris Basin, to Angouleme, in the northern Aquitaine Basin, along an approximately 500-km transect (Fig. 1). From Aalenian to Oxfordian times, western France was positioned at subtropical latitudes (20-30°N) and was covered by a shallow epicontinental sea. Sediments are predominantly composed of shallow marine carbonates deposited over a vast platform open to the Atlantic, Tethys, and Artic oceans (Fig. 2A-B; [START_REF] Enay | Synthèse paléogéographique du Jurassique français[END_REF][START_REF] Thierry | Late Sinemurian, Middle Toarcian, Middle Callovian, Early Kimmeridgian, Early Tithonian[END_REF].

Several studies of ammonite and brachiopod fauna have been conducted for Middle and Late Jurassic outcrops in areas around Caen [START_REF] Rioult | Outcrop sequence stratigraphy of the Anglo-Paris Basin Middle to Upper Jurassic (Normandy, Maine, Dorset)[END_REF], Argentan [START_REF] Kuntz | Notice explicative de la carte géologique d'Argentan (1/50000)[END_REF][START_REF] Ménillet | Notice explicative de la carte géologique de Sées (1/50000)[END_REF][START_REF] Moguedet | Notice explicative de la carte géologique de Mortagne-au -Perche (1/50000)[END_REF], Poitiers [START_REF] Gabilly | Guide géologique régional[END_REF][START_REF] Mourier | Le versant parisien du Seuil du Poitou de l'Hettangien au Bathonien. Stratigraphie, Sédimentologie, Caractères paléontologiques[END_REF]Cariou and Joubert, 1989a;[START_REF] Lorenz | Le Dogger du Berry, contribution à la connaissance des plate-formes carbonatées européennes du Jurassique[END_REF], and between Saint-Maixent l'École and Montbron [START_REF] Cariou | Notice explicative de la carte géologique de Ruffec (1/50000)[END_REF][START_REF] Foucher | Géodynamique sédimentaire et évolution paléogéographique de la plate-forme nord-est aquitaine au Jurassique moyen (Charente, Dordogne), tome II : Planches[END_REF][START_REF] Faugeras | Evolution de la plate-forme carbonatée est-aquitaine du Jurassique Moyen en Périgord. Stratigraphie, sédimentologie, paléogéographie[END_REF][START_REF] Branger | La marge nord-aquitaine et le seuil du Poitou au Bajocien : Stratigraphie séquentielle, évolution biosédimentaire et paléogéographie[END_REF][START_REF] Cariou | Notice explicative de la carte géologique de Saint-Maixent-l'École (1/50000)[END_REF]. They have made it possible to define a precise and reliable biostratigraphical framework at the ammonite biozone level (Fig. 3). The stratigraphic framework is briefly described for the five areas of our study, displaying numerous outcrops and various facies: Caen, Argentan/Alençon, Poitiers Saint-Maixent-l'École, and Montbron. Readers should refer to [START_REF] Mégnien | Synthèse géologique du Bassin de Paris[END_REF] for a detailed description of lithostratigraphic units of the study area.

The Caen area was more or less isolated from the Paris Basin during the Trias and at the onset of the Jurassic, and remained separated from Argentan by emersive basement reliefs until the end of the Bathonian [START_REF] Enay | Synthèse paléogéographique du Jurassique français[END_REF][START_REF] Dugué | Le massif armoricain dans l'évolution mésozoïque et cénozoïque du Nord-Ouest de l'Europe. Contrôles tectonique, eustatique et climatique d'un bassin intracratonique[END_REF]. Around Caen, the Bajocian to Oxfordian succession includes two major episodes of carbonate platform growth, (1) from the late Bajocian (parkinsoni Zone) to the late Bathonian (discus Zone) and (2) from the mid (densiplicatum Zone) to late Oxfordian (glosense Zone; Fig. 3, [START_REF] Rioult | Outcrop sequence stratigraphy of the Anglo-Paris Basin Middle to Upper Jurassic (Normandy, Maine, Dorset)[END_REF]. From the late Bajocian to the late Bathonian, bioclastic facies rich in echinoderms (Calcaires de Caen, Calcaires de Creully, Calcaires de Ranville Formations), bryozoans (Calcaires de Lagrune Formation), and sponge bioconstructions (Caillasses de Basse-Ecarde Formation) dominated.

The middle to upper Oxfordian deposits display ooid-and coral-dominated facies (Calcaires d'Auberville, Calcaires oolithiques de Trouville, Coral Rag Formations;Fig. 3;[START_REF] Rioult | Outcrop sequence stratigraphy of the Anglo-Paris Basin Middle to Upper Jurassic (Normandy, Maine, Dorset)[END_REF]. The Aalenian to late Bajocian (garantiana Zone) was, like the Toarcian, a period of low carbonate production, with highly condensed ferruginous levels (Oolithe ferrugineuse aalénienne, Couche verte, Conglomérat de Bayeux, Oolithe de Bayeux Formations, [START_REF] Rioult | Outcrop sequence stratigraphy of the Anglo-Paris Basin Middle to Upper Jurassic (Normandy, Maine, Dorset)[END_REF]. A carbonate platform demise occurred from the very late Bathonian (discus Zone) to late early Oxfordian (cordatum Zone), a period characterized by clayey deposits (Argiles de Lion, Marnes d'Escoville, Marnes d'Argences, Marnes à Belemnopsis latesulcata, Marnes et calcaires sableux de Crevecoeur, Marnes de Dives, Marnes de Villers, Oolithe ferrugineuse de Villers and Argiles à Lopha gregarea Formations; Fig. 3).

The area from Argentan to Alençon formed a small basin, separated from Caen by emersive basement reliefs [START_REF] Dugué | Le massif armoricain dans l'évolution mésozoïque et cénozoïque du Nord-Ouest de l'Europe. Contrôles tectonique, eustatique et climatique d'un bassin intracratonique[END_REF]. Detrital deposits formed during the Aalenian (Sables et graviers de Tessé Formation), displaying brachiopods and ammonites (Graphoceras sp., Graphoceras cornu) from the murchisonae and concavum Zones (Fig. 3; [START_REF] Juignet | Notice de la carte géologique de Fresnay-sur-Sarthe (1/50000)[END_REF].

During the Bajocian to late Bathonian (discus Zone), a bioclastic to oolitic carbonate platform grew (Oolithe à pentacrines, Oolithe de Vilaines-la-Carelle, Calcaires d'Ecouché, Calcaires de Sarceaux and Calcaires d'Argentan Formations;Fig. 3;[START_REF] Juignet | Notice de la carte géologique de Fresnay-sur-Sarthe (1/50000)[END_REF][START_REF] Kuntz | Notice explicative de la carte géologique d'Argentan (1/50000)[END_REF]. The very late Bathonian (discus Zone), Callovian, and early Oxfordian deposits are characterized by clays to sands (Marnes de Montcel, Marnes du Chevain, Oolithe de Suré, Marnes et calcaires sableux, Oolithe ferrugineuse de Chemilli, Marnes de Montarlo, Sables de Saint-Fulgent, Marnes à Pernes, Sables de Mortagne Formations; Fig. 3 ; [START_REF] Ménillet | Notice explicative de la carte géologique de Sées (1/50000)[END_REF]. The mid to late Oxfordian limestone displays ooid and coral rich facies (Calcaires coralliens de Mortagne, Calcaires à Astrates; Fig. 3; [START_REF] Moguedet | Notice explicative de la carte géologique de Mortagne-au -Perche (1/50000)[END_REF].

Around Poitiers, the marl/limestone alternations (Calcaires argileux d'Airvault Formation) of the early Aalenian pass upwards into bioclastic to oolitic limestones (Calcaires finement dolomitiques à silex, Calcaires roux bioclastiques à oncolithes, Calcaires dolomitiques à bioclastiques de Poitiers, Calcaires graveleux de Poitiers, and Pierre des Lourdines Formations; Fig. 3 ; [START_REF] Mourier | Notice explicative de la carte géologique de Poitiers (1/50000)[END_REF]Cariou and Joubert, 1989a). There is a sedimentary gap between the late Callovian and the late early Oxfordian (athleta, lamberta and mariae Zones; Cariou and Joubert, 1989a). Middle and upper Oxfordian deposits are composed of crinoid limestones (Pierre grise de Bonnillet, Calcaires crinoïdiques Formations) and clayey sedimentary sets (Banc de Pierre sublithographique, Calcaires argileux et glauconieux de Mirebeau Formations; Fig. 3 ; Cariou and Joubert, 1989a).

The Saint-Maixent-l'École area was located on a relatively low-energy platform at the margin of the Golfe Charentais basin during the Mid Jurassic [START_REF] Enay | Synthèse paléogéographique du Jurassique français[END_REF]. The Saint-Maixent-l'École area is dominated by marl/limestone alternations overlying the Aalenian (Marnes bleues Formation) and from the early Callovian to the late Oxfordian (macrocephalus to bimmamatum zones; Calcaires argileux de Pamproux, Marnes de Velluire, Pierre chauffante, Marnes gris-bleues à ammonites pyriteuses, Marnes grises à spongiares, Marnes Schisteuses and Calcaires blancs de Fors Formations; [START_REF] Cariou | Notice explicative de la carte géologique de Saint-Maixent-l'École (1/50000)[END_REF]. The Bajocian and Bathonian limestones are characterized by bioclast-rich facies (Calcaires ponctués de Saint-Maixent, Calcaires à silex Formations; [START_REF] Cariou | Notice explicative de la carte géologique de Saint-Maixent-l'École (1/50000)[END_REF].

In the Montbron area, in the western part of the high-energy Central Platform (Figs 2A and 3), dolomite (Dolomies de Montbron Formation) and shallow carbonate facies (Calcaires de Combe Brune, Calcaires de Saint-Sauveur, Calcaires de Vilhonneur, Calcaires crayeux à stromatolithes de Montbron, Calcaires oolithiques et coralliens de Garat Formations; [START_REF] Foucher | Géodynamique sédimentaire et évolution paléogéographique de la plate-forme nord-est aquitaine au Jurassique moyen (Charente, Dordogne), tome II : Planches[END_REF][START_REF] Pochat | Notice explicative de la carte géologique de Montbron (1/50000)[END_REF] were deposited from the Bajocian to Oxfordian. The biostratigraphy of brachiopod faunas [START_REF] Foucher | Géodynamique sédimentaire et évolution paléogéographique de la plate-forme nord-est aquitaine au Jurassique moyen (Charente, Dordogne), tome II : Planches[END_REF]) reveals a sedimentary gap during the early Callovian. The Aalenian deposits are characterized by clay and marl facies (Argiles et marnes grises Formation).

Material and methods

Sedimentology

This study is based on the detailed examination of 77 outcrop sections lying between the cities of Deauville and Montbron. Observations were completed with data from previous works carried out on 13 outcrop sections [START_REF] Foucher | Géodynamique sédimentaire et évolution paléogéographique de la plate-forme nord-est aquitaine au Jurassique moyen (Charente, Dordogne), tome II : Planches[END_REF][START_REF] Dugué | Géodynamique d'une bordure de massifs anciens. La bordure occidentale du Bassin angloparisien au Callovo-Oxfordien[END_REF][START_REF] Louail | Notice explicative de la carte géologique de La Flèche (1/50000)[END_REF][START_REF] Maire | Le Jurassique supérieur charentais : plate-forme carbonatée et faciès de bassin, stratigraphie, sédimentologie, paléogéographie, tome II -planches[END_REF][START_REF] Rioult | Outcrop sequence stratigraphy of the Anglo-Paris Basin Middle to Upper Jurassic (Normandy, Maine, Dorset)[END_REF] and 37 boreholes [START_REF] Guyader | Carte géologique du Havre (1/50000[END_REF][START_REF] Bourgueil | Carte géologique de Chauvigny (1/50000)[END_REF][START_REF] Roger | Carte géologique de Nontron (1/50000), forage de la Tour-Blanche[END_REF][START_REF] Rioult | Carte géologique de Caen (1/50000)[END_REF][START_REF] Ménillet | Notice explicative de la carte géologique de Livarot (1/50000)[END_REF] and from borehole data of the French Geological Survey avaible online http://infoterre.brgm.fr/, Fig. 1). Outcrop sections were logged in detail: lithology, texture [START_REF] Dunham | Classification of carbonate rocks according to depositional texture[END_REF][START_REF] Embry | A late Devonian reef tract on northeastern Banks Island, Northwest Territories[END_REF][START_REF] Insalaco | The descriptive nomenclature and classification of growth fabrics in fossil scleractinian reefs[END_REF], allochem content, and sedimentary structures were reported. A total of 268 thin sections were examined to determine the microfacies using a polarizing microscope. The proportion of facies components (bioclasts and non-bioclastic elements), texture, granulometry, grain sorting, and early cement types were characterized in each thin section.

We followed the definition (1997) of James for photozoan and heterozoan grain associations.

Photozoan grain association is rich in hermatypic corals, chlorophytes, benthic foraminifera and non-bioclastic components as ooids, peloids and aggregates. Heterozoan facies association displays abundant rhodophytes, molluscs, echinoderms and bryozoans.

Transitional facies designates grain associations in which neither heterozoan or photozoan producers are prevailing.

Sequence stratigraphy

Following Embry's definition (2009), outcrop sections and boreholes were interpreted in terms of sequence stratigraphy to establish a stratigraphic cross-section. In this sequence stratigraphy model, units are bounded either by a subaerial unconformity (SU) when the surface was exposed, or by a maximum regressive surface (MRS) when the surface was not exposed. Maximum regressive surfaces, also called transgressive surfaces [START_REF] Van Wagoner | An overview of the fundamentals of sequence stratigraphy and key definitions[END_REF] or flooding surfaces [START_REF] Homewood | Corrélations haute résolution et stratigraphie génétique: une démarche intégrée[END_REF], coincide with shifts in stacking patterns between shallowing-upward and deepening-upward trends, and correspond to the shallowest depositional environment recorded within a sequence [START_REF] Embry | Practical Sequence Stratigraphy[END_REF]. Maximum flooding surfaces (MFSs) mark a shift between deepening-upward and shallowing-upward trends, and correspond to the deepest facies encountered within a sequence. Subaerial unconformities or maximum regressive surfaces form sequence boundaries (SBs).

Depositional sequences are composed of transgressive and regressive systems tracts (TSTs and RSTs). The transgressive systems tract is characterized by retrograding architectures, with more distal facies upward and the regressive systems tract is characterized by prograding architectures, with more proximal facies upward.

Decompacted depth, accommodation, subsidence, and tectonic subsidence calculation

Decompacted depth, also called total subsidence, corresponds to the thickness of sediments after decompaction [START_REF] Steckler | Subsidence of the Atlantic-type continental margin off New-York[END_REF][START_REF] Allen | Basin Analysis[END_REF]. [START_REF] Goldhammer | Compaction and decompaction algorithms for sedimentary carbonates[END_REF] demonstrates that, in mud-supported carbonates at least, compaction mainly occurs during shallow burial with 100 to 400 m overburden. Considering that all the formations of the Middle and Upper Jurassic were buried beneath more than 500 m of sedimentary deposits, the following compaction factors were used for the entire sedimentary series: 1.2 for grainstones, 1.5 for packstones, 2 for wackestones, 2.5 for mudstones, and 3 for marls [START_REF] Hillgärtner | Quantification of high-frequency sea-level fluctuations in shallow-water carbonates: an example from the Berriasian-Valanginian (French Jura)[END_REF].

Accommodation space can be defined as the sum of the decompacted thickness of sediments and of paleodepth variations [START_REF] Robin | Time and space-scales of the tectonic control on a flexural intracratonic basin: the Paris Basin[END_REF]. For each facies, paleodepths were estimated based on the examination of sedimentary structures and fossil fauna (especially corals, [START_REF] Lathuilière | Coral zonation of an Oxfordian reef tract in the northern French Jura[END_REF]. The classic wave zonation is used, considering depths of 10-15 m for the fair-weather wave base and more than 40 m for the storm wave base [START_REF] Walker | Facies Models, response to sea level change[END_REF][START_REF] Sahagian | Eustatic curve for the Middle Jurassic-Cretaceous based on Russian platform and Siberian stratigraphy: zonal resolution[END_REF].

Subsidence corresponds to the increase in accommodation that is not due to eustasy, and so created by basement movements. It was calculated by subtracting eustasy variations from accommodation using the eustasy curve of [START_REF] Haq | Chronology of fluctuating sea levels since the Triassic[END_REF]. The curve was placed in the European context of third-order sequences as defined by Hardenbol et al. (1998b). Although there is debate about this curve [START_REF] Miller | The Phanerozoic Record of Global Sea-Level Change[END_REF], it is the only eustasy curve precise enough to estimate eustatic variations at the time resolution used in this study, and so the only curve that can be used to reconstruct subsidence variations at the third-order sequence scale.

Current criticisms of Haq's charts claim that it overestimates the amplitude of eustatic variations. In Cretaceous and Cenozoic times, [START_REF] Rowley | Sea Level: Earth's Dominant Elevation-Implications for Duration and Magnitudes of Sea Level Variations[END_REF], based on worldwide continental flooding, have identified large overestimations of the magnitude of variations and restored elevations of eustatic level. No reassement of the kind has yet been published for the Jurassic, but this could be a major bias in estimates of subsidence amplitudes. However, as the eustasy values substracted from the measured accommodation are all from the same chart [START_REF] Haq | Chronology of fluctuating sea levels since the Triassic[END_REF], this misestimate may affect the amplitude but not the trend. We therefore focus mainly on the trend and variations between sites. Tectonic subsidence is independent of the isostatic adjustment due to sediment deposition or paleodepth variations. It was calculated using the equation of [START_REF] Steckler | Subsidence of the Atlantic-type continental margin off New-York[END_REF]: the storm wave base and the fair-weather wave base, (3) shoal/barrier environments for waveand tide-dominated facies deposited above the fair-weather wave base, (4) lagoon to intertidal environments for most mud-supported carbonate rocks deposited in calm and shallow environments, and (5) backshore for facies deposited in sebkha, brackish, or continental environments, above high tides. Observations and descriptions are summarized in Table 1.

Five synthetic sedimentological logs synthesize the succesion of Aalenian to Oxfordian deposits in the Caen, Alençon, Poitiers, Saint-Maixent-l'École, and Montbron areas (Fig. 5).

Lower offshore: facies F1a to F1f

Claystones and marls with micritic limestone alternations (F1a-b-c, Fig. 6A-B), ferruginous ooid wackestones to packstones (F1d, Fig. 6C-D), ferruginous oncoid floatstones (F1e, Fig. 6C-E-F), and glauconitic to phosphatic bioclastic wackestones to floatstones (F1f, Fig. 6G) are present in the lower offshore. Fauna are composed of ammonites, belemnites, bivalves, brachiopods, benthic and planktonic foraminifers, sponge spicules, ostracods, echinoderms, dinoflagellates, serpulites, and gastropods. Bioturbation is frequent and trace fossils abundant (Chondrites, Thalassinoïdes, Walthonensis;[START_REF] Dugué | Géodynamique d'une bordure de massifs anciens. La bordure occidentale du Bassin angloparisien au Callovo-Oxfordien[END_REF]. Ferruginous oncoids of facies F1e are composed of microstromatolitic iron mats dominated by filamentous bacteriae and fungi living below the photic zone in dysaerobic waters [START_REF] Préat | Iron bacterial and fungal mats, Bajocian stratotype (Mid-Jurassic, northern Normandy, France)[END_REF]. The very fine grain size, the absence of sedimentary structures, the absence of scleractinian corals that are typical of the euphotic zone, the abundant bioturbation, and the presence of ammonites and belemnites indicate a very calm depositional environment, probably below the storm wave base [START_REF] Pomar | Types of carbonate platforms: a genetic approach[END_REF][START_REF] Lathuilière | Coral zonation of an Oxfordian reef tract in the northern French Jura[END_REF].

Upper offshore: facies F2a to F2f

Mostly bioclastic limestones, intercalated with thin marl interbeds are present in the upper offshore environments (Fig. 7A). Six facies were identified: (1) alternations of marl and echinoderm/peloid packstones to grainstones (F2a, Fig. 7A-B), (2) alterning marls and bivalve/brachiopod wackestones to packstones (F2b, Fig. 7C), (3) marl/ooid grainstone alternations (F2c), (4) sponge wackestones to floastones (F2d, Fig. 7D-E), (5) sheetstone to platestone facies with lamellar corals, and (6) sponge bioconstructions in marls (F2e-f, Fig. 7F). The dominant fauna is composed of echinoderms, bivalves, sponges, lamellar microsolenid corals, brachiopods, bryozoans, and foraminifers. It indicates normal oxygenation and salinity conditions. The dominance of lamellar microsolenid corals argues for an environment located within the photic zone. In the eastern Paris Basin, similar coral associations developed in paleodepths ranging between 20 m and 40 m during the Oxfordian [START_REF] Lathuilière | Coral zonation of an Oxfordian reef tract in the northern French Jura[END_REF]. The upper surface of the limestone beds is often bioturbated by vertical burrows filled in with the overlying clays. The accumulation of fragmented bivalve shells forming shell-graded layers (F2a-b), gutter casts (F2a-b-c, Fig. 7A), hummocky crossstratification (HCS, F2b), and upturned sponges (F2c) suggests that sedimentation was under storm influence in the upper offshore between the storm wave base and the fair-weather wave base.

Shoreface: facies F3a to F3l

Twelve facies are distinguished in shoreface environments: (1) very fine peloidal grainstones (F3a, Fig. 8A), (2) superficial ooid grainstones (F3b), (3) bivalve grainstones to rudstones (F3c, Fig. 8B), (4) bioclastic peloidal grainstones (F3d, Figs 8C and 9A), (5) quartz bioclastic sands to sandstones (F3e, Fig. 9B), (6) sponge bioconstructions in bioclastic grainstones (F3f, Fig. 9C), (7) mixstone to domestone coral bioconstructions (Isastrea, Thecosmilia, Rioult et al., 1989) in oolitic grainstones (F3g), (8) echinoderm grainstones (F3h, Figs 8D and 9D), ( 9) bryozoan grainstones to rudstones (F3i, Fig. 8E), (10) ooid grainstones to sands (F3j, Figs 8F

and 9E-F-G), (11) lithoclast-ooid grainstones to rudstones (F3k,Figs 8G and 9F),(12) lithoclast-oyster calcareous conglomerates (F3l,Figs 8H and 9H). The presence of grainstone to rudstone textures, common low-angle large-scale clinobeds (Fig. 9A), tabular to trough cross bedding in dunes (Figs. 9B andG), erosive channels (Fig. 9A), wedges in clinobedded oolitic grainstones (Fig. 9F), and herringbone cross bedding suggests a high-energy wave-or tide-influenced environment located above the fair-weather wave base. This is congruent with the mixstone to domestone texture of coral bioconstructions and with the occurrence of the coral genera Isastrea and Thecosmilia, which characterize paleodepths between 20 m and 0 m in the eastern Paris Basin during the Oxfordian [START_REF] Lathuilière | Coral zonation of an Oxfordian reef tract in the northern French Jura[END_REF].

Lagoon and intertidal environments: facies F4a to F4d

Four facies are distinguished in : (1) coral bioconstructions (mixstones to domestones) in micritic limestones (F4a), (2) bioclastic/peloid/quartz mudstones (F4b, Fig. 10A), (3) pellet/peloid grainstone/packstones (F4c, Fig. 10B), and (4) oncoid-ooid rudstones to packstones associated with grapstones and lithoclasts (F4d, Fig. 10C-D-E). In these muddominated facies, the fauna is mainly composed of bivalves, corals, gastropods, and miliolids.

Brachiopods, bryozoans, and echinoderms occur in low numbers. From Argentan to the Alençon area, these facies may be directly transgressive on the basement highs and alternate with oolitic shoal deposits (Fig. 10F). The dominance of peloid to oncoid facies and the presence of miliolids and well-preserved gastropods (especially nerineids) argue for protected lagoonal environments. However, washover deposits in facies F4b are characteristic of events of high-hydrodynamism (storms probably). Tangential cross bedding in dunes, and grainsupported to mud-supported textures in facies F4c and F4d indicate variable hydrodynamic conditions. Microbialites and microbial peloids are common in facies F4c and F4d (Fig. 10C).

Microstalactitic and meniscus cements also occur in both facies (Fig. 10D); they are characteristic of cementation occurring in a vadose diagenetic environment. The local occurrence of birdseyes (Fig. 10E) and of planar-bedding in facies F4c and F4d indicate that they can form in intertidal environments.

Supratidal to continental environments: facies F5a to F5c

Three facies can be present in supratidal to continental environments: (1) dolomitic facies (F5a, Fig. 10G), (2) lignite-rich facies (F5b), and (3) paleosoil layers (F5c). The dolomitic facies (F5a, Fig. 10G), exclusively present at Montbron, includes stromatolites (Le [START_REF] Pochat | Notice explicative de la carte géologique de Montbron (1/50000)[END_REF]. It is characteristic of supratidal environments of high salinity or evaporation rates present in sabkha environments. The lignite facies (F5b) consists of organic matter rich deposits, of very fine grain size (silt), and displays characeae gyrogonites and ostracods [START_REF] Foucher | Géodynamique sédimentaire et évolution paléogéographique de la plate-forme nord-est aquitaine au Jurassique moyen (Charente, Dordogne), tome II : Planches[END_REF] suggesting a very calm and protected brackish depositional environment. Paleosoils (F5c) are described by [START_REF] Dugué | Géodynamique d'une bordure de massifs anciens. La bordure occidentale du Bassin angloparisien au Callovo-Oxfordien[END_REF] and [START_REF] Ménillet | Notice explicative de la carte géologique de Livarot (1/50000)[END_REF] around Caen and Argentan. They are composed of silts, clays, and quartz grains of about 0.1 mm diameter. The occurrence of characeae gyrogonites and roots suggests environments of coastal plain deposits [START_REF] Dugué | Géodynamique d'une bordure de massifs anciens. La bordure occidentale du Bassin angloparisien au Callovo-Oxfordien[END_REF].

Facies architecture and depositional sequences

The spatial distribution and temporal evolution of the facies defined above is described below.

Twenty-two transgressive-regressive cycles were identified between the early Aalenian and the late Oxfordian, whose maximum flooding surfaces are underlined by clays (Figs 5 and 11). Considering a time range of about 17 My for the entire interval [START_REF] Gradstein | The geologic time scale 2012[END_REF], a rough estimate of the average duration of each cycle comes to 0.8 My, which is close to the duration range of third-order cycles as reported by several authors [START_REF] Haq | Chronology of fluctuating sea levels since the Triassic[END_REF]Hardenbol et al., 1998a;[START_REF] Schlager | Fractal nature of stratigraphic sequences[END_REF]. Moreover, it corresponds to a multiple of 0.4 My, which is the duration of Earth's eccentricity cycle, often considered as the controlling factor for third-order sequences (e.g. [START_REF] Strasser | Third-order depositional sequences reflecting Milankovitch cyclicity[END_REF]. and Parkinsonia cf parkinsoni respectively. At the top of sequence MJVII, the maximum regressive surface Bt5 is underlined by (1) a lignite layer attesting to emersion at Argentan (French Geological Survey, http://infoterre.brgm.fr/) and ( 2) a perforated hardground encrusted with oysters around Le Mans, which also marks a sedimentary gap of sequence MJVIII [START_REF] Juignet | Notice de la carte géologique de Beaumont-sur-Sarthe (1/50000)[END_REF].

From Saumur to Poitiers, a ramp gently shallowed southward from lower offshore to [START_REF] Foucher | Géodynamique sédimentaire et évolution paléogéographique de la plate-forme nord-est aquitaine au Jurassique moyen (Charente, Dordogne), tome II : Planches[END_REF].

Mid and late Bathonian: echinoderm/bryozoan ramp from Deauville to Le Mans, oolitic platform at Montbron (sequences MJIX-X-XI).

The middle to late Bathonian is composed of three third-order sequences: MJIX Calcaire et oolithe ferrugineuse à Montlivaltia Formations; [START_REF] Dassidat | Notice explicative de la carte géologique d'Alençon (1/50000)[END_REF][START_REF] Juignet | Notice de la carte géologique de Beaumont-sur-Sarthe (1/50000)[END_REF][START_REF] Ménillet | Notice explicative de la carte géologique de Vimoutiers (1/50000)[END_REF]and 1997). -Late mid Aalenian to early Bajocian (sequences MJIII to MJV). Accommodation and decompacted sediment thickness rates for the entire interval range from 0 m/My in Argentan to 15 m/My in Montbron (Fig. 13). A substantial accommodation rate is only recorded in Poitiers for sequence MJIV (70 m/My, Fig. 14). This interval is marked by a tectonic uplift, synchronous over the entire western France platform (Fig. 13).

-Late Bajocian to late Bathonian (sequences MJVI to MJXI).

Discussion

Accomodation changes on the western France carbonate platform -Global and regional trends

Platform architecture and sedimentary dynamics change with time from Deauville to Montbron over the Mid Jurassic and the Oxfordian, raising questions about the factors controlling this evolution. Sedimentary sequences, systems tracts, and platform architectures depend directly on the ratio between accommodation space (A) and sedimentation rate (S); [START_REF] Jervey | Quantitative modeling of siliciclastic rock sequences and their seismic expression[END_REF][START_REF] Schlager | Accommodation and supply -a dual control on stratigraphic sequences[END_REF][START_REF] Schlager | Carbonate Sedimentology and Sequence Stratigraphy[END_REF][START_REF] Catuneanu | Towards the standardization of sequence stratigraphy[END_REF]. The A/S ratio controls the progradational, aggradational, or retrogradational geometries of sediments. Retrograding structures and facies that are more distal upward mark the transgressive systems tract, when the A/S ratio is higher than 1. Prograding structures and upwardly more proximal facies characterize the regressive system tract, when the A/S is lower than 1. Accommodation space is generated by changes in (1) global eustasy and/or (2) subsidence, the latter being associated with (3) isostatic adjustment due to sediment deposition or paleodepth variation, and with (4) tectonics. At local scale, tectonic subsidence can be explained by syn-sedimentary active faults. Sedimentation rate relates to (1) terrigenous input or to (2) in-situ carbonate production and its redistribution, which is largely influenced by environmental conditions (e.g. trophic conditions and seawater temperature).

Overall eustasy variations in European basins have been modeled by Hardenbol et al. (1998b) and are presented in Figures 13 and15. Changes in depth, decompacted sediment thickness (observed total subsidence, [START_REF] Steckler | Subsidence of the Atlantic-type continental margin off New-York[END_REF]Alen and Alen, 2005), accommodation (total subsidence +/-depth variation), subsidence, and tectonic subsidence [START_REF] Steckler | Subsidence of the Atlantic-type continental margin off New-York[END_REF]Fig. 13) were reconstructed in four key localities to discuss the factors controlling sediment architectures (Caen, Argentan, Poitiers, and Montbron, Fig. 13). By reconstructing long-distance depositional sequences and dating basement flooding it was possible to reconstruct the ante-Aalenian topography and discuss its influence on platform architecture.

Eustasy as the major control on 3rd-order transgressive-regressive systems tracts

The overall correlation between European third-order sequences and the 22 depositional sequences along with their continuity over the entire western France platform suggests that eustasy is the main factor affecting accommodation variations at the scale of third-order sequences (Hardenbol et al., 1998a, Fig. 15). The maximum flooding surfaces identified were also found in other European basins of similar ages at the biozone scale (Hardenbol et al., 1998a). However, five third-order sequences described in other European basins were not identified in the study area: two within the Bathonian deposits (zigzag/progracilis Zones However, there are significant differences in second-order transgressive-regressive cycles between European basins and the western France platform, but also within the western France platform (Figs 11 and 15). Lateral dissimilarities in sedimentation rate and carbonate production, and the sharp local depth variations recorded over the western France platform cannot have been under global or eustatic control and must be related to local tectonics (Fig. 11).

5.1.2.Tectonics contribution on sedimentation rate, carbonate platform architecture, growth, and demise

Several episodes of facies and platform architecture change are interpreted to be connected with tectonic activity over all or part of western France. The major tectonic uplift, associated with an accommodation rate of about zero, that occurred over the entire study area from the mid Aalenian to the early Bajocian (sequences MJIII to MJV, Fig. 13) corresponds to the Mid-Cimmerian Unconformity, a subtle deformation event identified all around the Paris Basin [START_REF] Guillocheau | Meso-Cenozoic geodynamic evolution of the Paris Basin: 3D stratigraphic constraints[END_REF][START_REF] De Graciansky | Évolution des structures et de la paléogéographie au passage Lias-Dogger dans le bassin de Paris d'après les données de la subsurface[END_REF] and in Western Europe related to North Sea doming [START_REF] Underhill | Jurassic thermal doming and deflation in the North Sea: implications of the sequence stratigraphic evidence[END_REF]. Eustatic rise between sequences MJIII and MJV was not sufficient to offset the loss of accommodation due to the uplift [START_REF] Haq | Chronology of fluctuating sea levels since the Triassic[END_REF] During the late Bajocian and the Bathonian, about 150 m of accommodation space was created, despite a global sea-level fall (Figs 13 and 14;Hardenbol et al., 1998b). This indicates that the western France platform underwent a major phase of tectonic subsidence (estimated at about 100 m considering a sea-level fall of 45 m; Fig. 13; Hardenbol et al., 1998b). The accommodation generated by tectonics, coupled with the subsidence related to sediment loading, made it possible for 100 to 150 m of decompacted carbonates to accumulate (Fig. 13). Over sequences MJIX to MJXI, the Caen and Montbron shallow platforms prograded northwards, indicating that carbonate production was sufficient to fill the accommodation space generated by tectonic subsidence (Fig. 11). Significant variations in decompacted sedimentation/accommodation rate were observed within sequence MJXI between Falaise (decompacted sedimentation/accommodation rate about 36 m/My) and Argentan (about 240 m/My; [START_REF] Gradstein | The geologic time scale 2012[END_REF]Figs 11 and 14). This implies a local tectonic subsidence of about 40 m/My in the Argentan area, the remaining subsidence being controlled by sediment loading. Argentan is bordered by three faults affecting the Mesozoic series, which may have controlled this tectonic subsidence for the latest Bathonian: the Montabard-Gouffern fault to the north [START_REF] Ménillet | Notice explicative de la carte géologique de Sées (1/50000)[END_REF][START_REF] Gigot | Notice explicative de la feuille de Falaise (1/50000)[END_REF], the Pommereux-Sentilly fault to the west, and the Sées fault to the southwest [START_REF] Kuntz | Notice explicative de la carte géologique d'Argentan (1/50000)[END_REF] Fig. 1). The Montabard-Gouffern fault displays a high subvertical dip and a vertical offset of between 30 and 40 m. At its northwestern extremity, Bajocian to Bathonian limestones were brought into contact with Triassic to Ordovician deposits, indicating Bathonian to post-Bathonian activity [START_REF] Gigot | Notice explicative de la feuille de Falaise (1/50000)[END_REF].

The early Callovian is marked by a sudden carbonate demise that is commonly explained by a eustatic rise and a consequent extensive drowning event within the Paris Basin [START_REF] Jacquin | Séquence de dépôt et cycles régressif/transgressifs en domaine marin carbonaté: exemple du Dogger du Bassin de Paris[END_REF](Jacquin et al., , 1998;;Jacquin and de Graciansky, 1998;[START_REF] Brigaud | Growth and demise of the Jurassic carbonate platform in the intracratonic Paris Basin (France): Interplay of climate change, eustasy and tectonics[END_REF]. The sudden disappearance of carbonates in favor of clay sedimentation occurred from Deauville to Le Mans during deposition of the early transgressive systems tract of sequence MJXII (Figs 11,12G and 13). The progressive rise in the overall eustatic level, estimated at about 15 m, was not sufficient to explain sudden shallowing of at least 40 m (Hardenbol et al., 1998b;Figs 11 and 13). From Deauville to Le Mans, the steep deepening resulting in carbonate demise for the earliest Callovian was triggered by prominent tectonic subsidence of an amplitude between at least 35 m in Argentan and 55 m in Caen (Fig. 13). The increased accommodation was then maintained through the Callovian and into the early Oxfordian due to a eustatic rise (Hardenbol et al., 1998b). Several reactivated basement faults affecting the Mesozoic series from Falaise to Alençon may have caused this tectonic subsidence: the Cordey-Ronai, Montabard-Gouffern, Merlerault, Courtomer, and Fresnay-sur-Sarthe faults (Fig. 1). The Merlerault and Courtomer faults display a vertical offset varying between 50 m and 130 m in the Mesozoic succession [START_REF] Ménillet | Notice explicative de la carte géologique de Sées (1/50000)[END_REF][START_REF] Insalaco | The descriptive nomenclature and classification of growth fabrics in fossil scleractinian reefs[END_REF]. Northwards, the Cordey-Ronai and Montabard-Gouffern faults affect the Middle Jurassic series with a vertical offset of about 40 m [START_REF] Ménillet | Notice explicative de la carte géologique de l'Aigle (1/50000)[END_REF].

In Montbron, the accommodation rate was zero for sequences MJXII and MJXIII over a period of eustatic rise (about +20 m, Figs 13 and 14, Hardenbol et al., 1998b). This implies an uplift, the amplitude of which is estimated at about 40 m, preceding emersion, which occurred during a second-order transgression in European basins, and accounting for the absence of sequences MJXII and MJXIII at Montbron (Fig. 11; Hardenbol et al., 1998a). This local tectonics implies that the sequence boundary between the two complete second-order cycles In Argentan, the accommodation rate was zero for sequences LJII and LJIII over a period of eustatic rise (about +15 m, Figs 13 and 14, Hardenbol et al., 1998b). This implies an uplift of Cariou and Joubert, 1989b). In Montbron, the increased accommodation due to gradual and slow tectonic subsidence coupled with a global eustatic rise over sequences LJV to LJVII (Hardenbol et al., 1998b, Fig. 13) accelerated sedimentation and led to the deposition of about 180 m of decompacted carbonates (Figs 11 and 13).

Basement topography as a major control of paleodepth on the western France carbonate platform

The Jurassic platform of western France developed over a pre-structured bottom surface. This includes basement rocks that are mostly Cambrian and Ordovician quartz sandstones, displaying major paleotopographic changes that can be directly observed in the field [START_REF] Juignet | Notice de la carte géologique de Beaumont-sur-Sarthe (1/50000)[END_REF][START_REF] Ménillet | Notice explicative de la carte géologique de Vimoutiers (1/50000)[END_REF][START_REF] Cariou | Notice explicative de la carte géologique de Saint-Maixent-l'École (1/50000)[END_REF]. Post-Variscan relief of the basement has been partly lowered by the deposition of Liassic series, for example in the Montbron area that is filled by about 250 m of Triassic to Liassic deposits [START_REF] Roger | Carte géologique de Nontron (1/50000), forage de la Tour-Blanche[END_REF]. The topography of the basement was reconstructed for the time interval under study from borehole data with paleobathymetric interpretations (Fig. 12). Over the Aalenian to early Bathonian, the basement topography was the major factor determining lateral variations of paleodepth, as shallow environments were located on basement highs and deeper environments in basement depressions (Fig. 12A to E). From the late Bathonian to late Oxfordian, the basement depressions were filled by sediments and flattened, and the influence of the basement topography on bathymetries became negligible, except from Le Mans to Saumur, where lower offshore environments persisted (Fig. 12F to I).

Between Argentan and

Local tectonic subsidence and uplifts changed basement topography through time as described in part 4.1.2. However, tectonic movements were rather homogenous across western France through the Aalenian to early Bathonian and the basement topography remained approximately the same (Figs 12A to E and 13). From the late Bathonian to late Oxfordian, local tectonic movements greatly modified the basement topography (Figs 12F to I and 13).

Growth and demise of carbonate platforms in western Tethyan domain

A bibliographic synthesis of sedimentation in western Tethyan domain was conducted and coupled with our results to propose a model of sedimentary evolution and carbonate production in Western Tethys from Aalenian to Oxfordien (see Table 2 for references and Figure16 for maps).

Two periods of global carbonate platform growth were identified in Western Tethys in France, England, Spain and Italy platforms during this period: one during Bajocian/Bathonian and the subsequent during middle/late Oxfordian in France, England, Spain, and Italy platforms. In shoreface environments, marked by facies with grainstone texture and crossbedding, photozoan facies are dominant and include abundant ooids, peloids, and hermatypic corals (Fig. 17A). Heterozoan facies, characterized by the predominance of mollusk, echinoderms and bryozoans (Fig. 17A), are rather found in micritic limestones and limestone/marl alternations forming in offshore environments. However, shallow facies in northern Germany and Scotich Cleveland basin are dominated by sandstones. 2009) for the early Jurassic.

A comprehensive model for western Tethyan carbonate platform growth and demise

High an low eccentricity cycles

Martinez and [START_REF] Martinez | Orbital pacing of carbon fluxes by a ~9-My eccentricity cycle during the Mesozoic[END_REF] synthetized the evolution of δ 13 C measured in well-preserved belemnite rostra over the Jurassic in western European basins (Fig. 15). Changes in carbonate production on western Tethyan platforms during the Middle Jurassic and Oxfordian correlates with stable δ 13 C values as long-term δ 13 C maxima are synchronous with low carbonate production rates (Aalenian and from middle Callovian to early Oxfordian) and long-term δ 13 C minima correspond to periods of high carbonate production (Bajocian/Bathonian and from middle to late Oxfordian). [START_REF] Martinez | Orbital pacing of carbon fluxes by a ~9-My eccentricity cycle during the Mesozoic[END_REF] interpreted these long-term δ 13 C variations as resulting from a 9.1 My eccentricity orbital cycle.

Carbonate production during high-eccentricity intervals

The late Bajocian-Bathonian and middle-late Oxfordian intervals are characterized by clay fraction with small kaolinite amounts in the eastern Paris Basin (0-10%, [START_REF] Pellenard | Mineralogical variability of Callovo-Oxfordian clays from the Paris Basin and the Subalpine Basin[END_REF][START_REF] Brigaud | Facies and climate/environmental changes recorded on a carbonate ramp: A sedimentological and geochemical approach on Middle Jurassic carbonates[END_REF]. Due to relative low burial depth and temperatures that never exceeded 50 °C in this area (Clauer et al., 2007), mineralogical clay associations can be considered as detrital, which can be used as an environmental proxy [START_REF] Debrabant | Clay sedimentology, mineralogy and chemistry of Mesozoic sediments drilled in the Northern Paris Basin[END_REF][START_REF] Dera | Distribution of clay minerals in Early Jurassic Peritethyan seas: palaeoclimatic significance inferred from multiproxy comparisons[END_REF]. High kaolinite content may indicate either intense chemical weathering of kaolinite soils or reworking of ancient kaolinite-bearing rocks (Chamlet, 1989[START_REF] Dera | Distribution of clay minerals in Early Jurassic Peritethyan seas: palaeoclimatic significance inferred from multiproxy comparisons[END_REF], and low kaolinite amount in the Bajocian-Bathonian and middle-late Oxfordian limestones may then characterize an arid climate. This is consistent with results of [START_REF] Ma | Simulation of long eccentricity (400-kyr) cycle in ocean carbon reservoir during the Miocene Climate Optimum: Weathering and nutrient response to orbital change[END_REF] who suggested that high eccentricity intervals induced a dry climate disturbed by short episodes of intensive rainfalls and storms. Although these moosonal episodes intensified the net transfer of nutrient, organic carbon and carbonates ions to the ocean, organic carbon burial was prevented because of the prevailing dry climate and the efficient oxidizing conditions in seawater (Fig. 17B; [START_REF] Martinez | Orbital pacing of carbon fluxes by a ~9-My eccentricity cycle during the Mesozoic[END_REF]. This lead to (1) an enrichment of seawater in 12 C and a consequent decrease of δ 13 C values in the oceanic reservoir, and to (2) carbonate sursaturation in epicontinental seas due to high evaporation [START_REF] Martinez | Orbital pacing of carbon fluxes by a ~9-My eccentricity cycle during the Mesozoic[END_REF]. This model is consistent with the high carbonate production rate recorded in western Tethyan epicontinental seas during the Bajocian/Bathonian and middle/ late Oxfordian intervals. The ratio between photozoan and heterozoan associations is mainly controlled by seawater temperature, trophic conditions, and bathymetry (Fig. 17A; James, 1997, Mutti and[START_REF] Mutti | Carbonate systems along nutrient and temperature gradients: some sedimentological and geochemical constraints[END_REF]. Photozoan association development is favored by high seawater temperatures (subtropical to tropical, >18°C) and low trophic resources (oligotrophic to mesotrophic), but can also be found in temperate waters under oligotrophic conditions (Fig. 17A; [START_REF] Mutti | Carbonate systems along nutrient and temperature gradients: some sedimentological and geochemical constraints[END_REF]. Heterozoan grain association dominates in warm waters (>18°C) under eutrophic conditions or in cool waters (<18°C) whatever the trophic conditions. In western Tethyan platforms, during the Bajocian/Bathonian and middle/late Oxfordian, photozoan producers were distributed in shoreface environments, indicating prevailing olitrophic conditions, whereas heterozoan producers are mainly present in offshore environments (Figs.

tide-dominated environments, as in northwestern France during the Bathonian (Fig. 16). This could be induced by local changes in environmental conditions as an increase of trophic inputs or a decrease of seawater temperatures (e.g. [START_REF] Lécuyer | Thermal evolution of Tethyan surface waters during the Middle-Late Jurassic: Evidence from δ 18 O values of marine fish teeth[END_REF].

Carbonate production during low-eccentricity intervals

During the Jurassic, low eccentricity intervals induced wet conditions, which promoted high weathering rates, nutrient inputs, productivity levels, and organic burial in the ocean, and led to an increase of δ 13 C values [START_REF] Martinez | Orbital pacing of carbon fluxes by a ~9-My eccentricity cycle during the Mesozoic[END_REF]. This happened during the Aalenian and from the middle Callovian to early Oxfordian (Fig. 17B; [START_REF] Martinez | Orbital pacing of carbon fluxes by a ~9-My eccentricity cycle during the Mesozoic[END_REF]. The high kaolinite ratio in the Paris Basin (> 20% of the clay mineralogical association; [START_REF] Pellenard | Mineralogical variability of Callovo-Oxfordian clays from the Paris Basin and the Subalpine Basin[END_REF][START_REF] Brigaud | Facies and climate/environmental changes recorded on a carbonate ramp: A sedimentological and geochemical approach on Middle Jurassic carbonates[END_REF], and vascular plant biomarkers used as a proxy for palaeoflora [START_REF] Hautevelle | Vascular plant biomarkers as proxies for palaeoflora and palaeoclimatic changes at the Dogger/Malm transition of the Paris Basin (France)[END_REF] support enhanced weathering conditions under a humid climate during the middle Callovian to early Oxfordian. Moreover, organic-rich layers are found in Central Atlantic [START_REF] Dromart | Perturbation of the carbon cycle at the Middle/Late Jurassic transition: geological and geochemical evidence[END_REF] and in the western Tethyan domain (England, [START_REF] Kenig | Isotopic biochemistry of the Oxford Clay Formation (Jurassic), UK, London[END_REF]Saudi Arabia, Carrigan et al., 1995) during the middle Callovian. The Aalenian clay mineralogical association is also dominated by kaolinite in the southern Paris Basin (Delavenna et al., 1989) and in England [START_REF] Sellwood | Mesozoic and Tertiary argillaceous units: distribution and composition[END_REF]. The presence of anoxic conditions at the sea bottom is evidenced in southern Poland by the presence of agglutinated foraminifera, but the association with organic-rich deposists is not obvious [START_REF] Tyszka | Response of Middle Jurassic benthic foraminiferal morphogroups to dysoxic/anoxic conditions in the Pieniny Klippen Basin, Polish Carpathians[END_REF][START_REF] Tyszka | Factors controlling distribution of agglutinated foraminifera in Aalenian-Bajocian dysoxic facies (Pieniny Klippen Belt, Poland)[END_REF]. It is likely that organic carbon was either (1) locked up but disseminated in shelf mudstones and therefore, is not readily identified, (2) stored in deep marine areas or (3) stored in terrestrial settings [START_REF] Price | Carbon-isotope stratigraphy and temperature change during the Early-Middle Jurassic (Toarcian-Aalenian), Raasay, Scotland, UK[END_REF]. Clay contents and palaeoflora data, as well as evidences of prevailing anoxic conditions at the sea-floor during the Aalenian and from the middle Callovian to early Oxfordian are consistent with the hypothesis of a wet climate during low-eccentricity intervals leading to high nutrient inputs.

Such an eutrophication of sea waters is noxious for photozoan carbonate producers and tends to diminish the growth potential of carbonate platforms [START_REF] Weissert | Late Jurassic climate and its impact on carbon cycling[END_REF]Bartolini et al., 1996;[START_REF] Bartolini | 20 My hiatus in the Jurassic of Umbria-Marche Apennines (Italy): carbonate crisis due to eutrophication[END_REF][START_REF] Bartolini | 20 My hiatus in the Jurassic of Umbria-Marche Apennines (Italy): carbonate crisis due to eutrophication[END_REF][START_REF] Mutti | Carbonate systems along nutrient and temperature gradients: some sedimentological and geochemical constraints[END_REF], promoting siliciclastic sedimentation (Figs. 15,16 and 17B). On the western France platform, decompacted carbonate accumulation rate was over 60 m/My during the Bathonian and middle/late Oxfordian but fell down under 20 m/My at the Aalenian and during the middle Callovian/early Oxfordian interval. The mean biological carbonate content in marls varies from 35% to 20% in the Callovian to early Oxfordian, the lowest values being recorded in the mariae Zone [START_REF] Dugué | Géodynamique d'une bordure de massifs anciens. La bordure occidentale du Bassin angloparisien au Callovo-Oxfordien[END_REF], which correlates with the δ 13 C maxima [START_REF] Martinez | Orbital pacing of carbon fluxes by a ~9-My eccentricity cycle during the Mesozoic[END_REF]. Proximal deposits are sandstone or heterozoan to transitional grain associations, whose development is favored by eutrophic conditions (Figs. 16 and17B). Photozoan facies can develop locally, probably due to local changes in trophic conditions or seawater temperatures (e.g. London platform during the Aalenian). Low sedimentation rates (mainly between 0 and 10 m/My), the abundance of condensed ferruginous deposits and gaps during the Aalenian are the consequence of a decrease of accommodation space related to a global uplift in Western

Europe. This event corresponds to the Mid-Cimmerian unconformity (Figs. 16 and17B; [START_REF] Underhill | Jurassic thermal doming and deflation in the North Sea: implications of the sequence stratigraphic evidence[END_REF][START_REF] Guillocheau | Meso-Cenozoic geodynamic evolution of the Paris Basin: 3D stratigraphic constraints[END_REF][START_REF] De Graciansky | Évolution des structures et de la paléogéographie au passage Lias-Dogger dans le bassin de Paris d'après les données de la subsurface[END_REF].

High clayey sedimentation rates during the middle Callovian to early Oxfordian, generally between 20 and 50 m/My, was allowed by an increase in accommodation space both due to

(1) the global eustatic sea-level rise (Hardenbol et al., 1998b) and ( 2) increase of subsidence rate (Fig. 17B). In western France, the demise of the carbonate platform initiated at the Bathonian/Callovian boundary because of a sharp, local tectonic subsidence, but it persisted in deeper and shallower environments until the middle Oxfordian due to (1) the eutrophic conditions of neritic environments and to (2) the global eustatic sea level rise.

Conclusions

Thirty-one facies were characterized in Aalenian to Oxfordian formations of western France, deposited in lower offshore to backshore settings. Changes in platform geometry and facies were identified over a time interval of ~17 Ma (Aalenian to Oxfordian) and across a long distance (500 km). A high-resolution correlation scheme was realized at the ammonite biozone scale in a sequence stratigraphy framework. Twenty-two third-order depositional sequences have been defined. They are bounded by maximum regressive surfaces that are either marine (e.g. perforated hardgrounds encrusted with bivalves) or emersive (microstalactitic, meniscus, and dogtooth cements, lignite, paleosoils). Depositional sequences of the western France platform correlate at the ammonite biozone scale with the third-order sequences of European basins, indicating that eustasy is the major factor controlling thirdorder transgressive-regressive systems tracts (Hardenbol et al., 1998a) The present work shows that the development of carbonate platforms in intracontinental settings was influenced by multiple factors, each one exerting a precise control on sedimentation. In particular, we highlitghted the control of basement topography on lateral depth variations and the influence of local and regional tectonics on carbonate platform architecture, even in intracontinental basins. Finally, climate evolution in western Tethys was controlled by long-term eccentricity variations and can be related to the major stages of carbonate platform growth and demise and largely influenced the producer types (photozoan versus heterozoan). paleogeographic reconstruction (modified from [START_REF] Brigaud | Facies and climate/environmental changes recorded on a carbonate ramp: A sedimentological and geochemical approach on Middle Jurassic carbonates[END_REF]based on Enay and Mangold, 1980;[START_REF] Ziegler | Evolution of the Arctic -North Atlantic and the Western Tethys[END_REF][START_REF] Thierry | Late Sinemurian, Middle Toarcian, Middle Callovian, Early Kimmeridgian, Early Tithonian[END_REF][START_REF] Hendry | Geochemical trends and palaeohydrological significance of shallow burial calcite and ankerite cements in Middle Jurassic strata on the East Midlands Shelf (onshore UK)[END_REF] D. Location of the study area during the Oxfordian in a paleogeographic reconstruction (modified from [START_REF] Strasser | Palaeogeography of a shallow carbonate platform: The case of the Middle to Late Oxfordian in the Swiss Jura Mountains[END_REF]based on Enay and Mangold, 1980;[START_REF] Ziegler | Evolution of the Arctic -North Atlantic and the Western Tethys[END_REF][START_REF] Thierry | Late Sinemurian, Middle Toarcian, Middle Callovian, Early Kimmeridgian, Early Tithonian[END_REF]. Biostratigraphic ammonite zonation from [START_REF] Gradstein | The geologic time scale 2012[END_REF]. Standard European sequences from Hardenbol et al. (1998a). (1996).

Figure captions

Fig. 5. Synthetic sedimentological log with geological stages, ammonite biozones, and biostratigraphic data (ammonites, brachiopods, and foraminifers), lithostratigraphic formations, carbonate textures, depositional environments, third-order sequence stratigraphy and stratigraphic locations of outcrops and samples. The parts of the logs not observed in the field have been completed using boreholes and descriptions from the literature. A. Synthetic sedimentological log of the Caen region, completed from Rioult et al. (1989[START_REF] Rioult | Outcrop sequence stratigraphy of the Anglo-Paris Basin Middle to Upper Jurassic (Normandy, Maine, Dorset)[END_REF] and [START_REF] Maurizot | Notice explicative de la carte géologique de Bayeux-Courseulles-sur-Mer (1/50000)[END_REF]. B. Synthetic sedimentological log of the Argentan to Alençon region, completed from [START_REF] Kuntz | Notice explicative de la carte géologique d'Argentan (1/50000)[END_REF] and [START_REF] Moguedet | Notice explicative de la carte géologique de Mortagne-au -Perche (1/50000)[END_REF]. C. Synthetic log of the Poitiers region completed from [START_REF] Mourier | Notice explicative de la carte géologique de Poitiers (1/50000)[END_REF] and Cariou and Joubert, (1989a). D. Synthetic log of the Saint-Maixent-l'École region, completed from [START_REF] Cariou | Notice explicative de la carte géologique de Saint-Maixent-l'École (1/50000)[END_REF]. E. Synthetic log of the Montbron region, completed from Le [START_REF] Pochat | Notice explicative de la carte géologique de Montbron (1/50000)[END_REF]. Deauville-Montbron transect. This illustration is composed of 61 outcrop sections studied in this work completed by previous descriptions of 13 outcrop sections (Foucher, 1986 -outcrops 72, 73, 88, and 90;Dugué, 1989 -outcrops 16, 17, and 40;Louail et al., 1989 -outcrop 47;Rioult et al., 1991 -outcrops 1, 4, 8, 10, 13, and 15) and 37 boreholes (Guyader et al., 1970borehole A;Bourgueil et al., 1971 -borehole AB;Roger et al., 1979 -borehole AK;Rioult and Doré, 1989 -borehole B;[START_REF] Ménillet | Notice explicative de la carte géologique de Livarot (1/50000)[END_REF] western France sequences, second-and third-order European cycles/sequences (Hardenbol et al., 1998b), δ 13 C isotopic curve [START_REF] Martinez | Orbital pacing of carbon fluxes by a ~9-My eccentricity cycle during the Mesozoic[END_REF], and semi-quantitative estimation of decompacted carbonate production, carbonate producers, and depositional profile on the western France platform.

  These cycles are arranged into lower-order cycles from an Aalenian regressive hemicycle topped by the maximum regressive surface Bj1 (Caen) or Bj3 (Montbron); a Bajocian-Bathonian cycle topped by the maximum regressive surface Bt2 (Caen) of Bt4 (Montbron; maximum flooding surface zigzag); and a Callovian-mid Oxfordian cycle until the maximum regressive surfaces Ox6 (maximum flooding surface mariae or tenuiserratum). A constant characteristic of the western France platform throughout the Aalenian to Oxfordian interval is the presence of clayey lower offshore environments from La Flèche to Mirebeau, where sedimentation only occurred during sequences MJIV, MJVII , LJVI and LJVII (Figs 11 and 12).4.2.1. Aalenian to early Bathonian: detrital to bioclastic ramp (sequences MJI to MJVIII) This interval contains eight third-order sequences from Deauville to Montbron (Figs 5 and 11): MJI (Middle Jurassic I, opalinum Zone), MJII (opalinum to murchisonae Zones), MJIII (bradforensis to concavum zones), MJIV (discites and laeviuscula Zones), MJV (propiquans and early humphriesianum Zones), MJVI (late humphriesianum and niortense Zones), MJVII (parkinsoni Zone), and MJVIII (zigzag/progracilis Zones). The Aalenian to early Bathonian is characterized by ramp geometries that are either detritic (Aalenian) or bioclastic (echinoderms, bivalves, and sponge bioherms; Bajocian/early Bathonian; Figs 11 and 12A to D). The zigzag Zone maximum flooding surface is marked by an increase in paleodepth leading to large-scale retrogradations and maximum expansion of clayey facies in the study area (Figs 5, 11, and 12D). Offshore environments dominate from Argentan to Deauville, where a ramp deepens northward. Sequence MJI consists in 1 meter of ferruginous oncoid facies (F1d, Oolithe ferrugineuse aalénienne Formation, opalinum Zone) and is capped with marly to silty limestones of sequences MJII to MJIV (facies F1c, Malière Formation, murchisonae to concavum Zones, Figs 5, 11, and 12A). Sequences MJV and MJVI are located in a condensed succession composed of glauconitic limestones (F1f, Couche verte Formation, propiquans Zone), oncoid ferruginous facies (F1e, Conglomérat de Bayeux Formation, humphriesianum zone), and ooid ferruginous facies (F1d, Oolithe ferrugineuse de Bayeux Formation, garantiana to niortense Zones, Figs 5, 11, and 12B). Sequence MJVIII is marked by a mid ramp rich in sponges that progrades northward (F2d, Calcaires à spongiaires Formation, Figs 5A, 11, and 12C). Around Caen, the maximum regressive surface between sequences MJVII and MJVIII (Bj5) is characterized by upper offshore sponge facies sharply overlain by lower offshore marl/limestone alternations of sequence MJVII (F1a-b, Marnes de Port-en-Bessin Formation, Figs 5D, 11, and 12D). Over the Aalenian to early Bathonian, the shallowest environments were located on Ordovician basement highs, between Argentan and Le Mans. For the Aalenian, facies are clastic sands with rare ammonites (Graphoceras sp. and Graphoceras cornu) characterizing the concavum Zone (facies F3e-l, Sables et graviers de Tessé Formation, Figs 5B, 11, and 12A). Sequence MJIII is bounded at the top by a maximum regressive surface marked by a perforated hardground with encrusting bivalves, also characterizing a sedimentary gap that occurs during sequences IV to VI (Bj1, Figs 5, 11, and 12B). Over sequence MJVII, basement highs are covered with oolitic sands to grainstones (F3j, Oolithe de Vilaines-la-Carelle Formation, Figs 5B, 11, and 12C) that prograde toward Saumur. These shallow oolitic facies were dated to the niortense and parkinsoni Zones based on ammonites Pseudogarantiana sp.

  shoreface environments, dominated by echinoderms and bivalve mud-supported facies (F2a-b, Calcaires dolomitiques à bioclastiques de Poitiers, Calcaires graveleux de Poitiers, and Calcaires à silex Formations; Figs 5C, 11, and 12a to D). Maximum regressive surfaces are marked by bioclastic to superficial ooid grainstones at Poitiers changing to micritic limestones toward Saumur (Aa1 to Bt1; F3b-h, F2a-b, Calcaires roux bioclastiques à oncolithes and Calcaires graveleux de Poitiers Formations; Figs 5 and 11). Sequence MJVI is condensed from Mirebeau to Saint-Maixent-l'École. Depositional environments deepen again towards Saint-Maixent-l'École and Ruffec, where upper offshore bioclastic mud-supported facies to lower offshore marls and glauconitic limestones were deposited (F2b, F1f, and F1b, Calcaires ponctués de Saint-Maixent, Banc pourri and Marnes bleues Formations, Figs 5D, 11, and 12A to D). Towards Ruffec then Montbron, the ramp became shallower during the Aalenian to early Bajocian with the deposition of upper offshore detrital to bioclastic facies (sequences MJII to MJV, Figs 11, 12A, and B). Paleodepth decreased abruptly from offshore to shoreface, marking the platform edge around Montbron over sequences MJV to MJVIII. An oolitic shoal protected lagoonal/supratidal environments where dolomite precipitated over the regressive systems tracts of sequences MJV and MJVI (Fig. 11). During sequences MJVII and MJVIII, the lagoon was filled by mud-supported facies. The maximum regressive surfaces Bj3 to Bj5 correspond to periods of maximum expansion of lagoon environments prograding to the northwest during the deposition of regressive systems tracts. The maximum regressive surface at the top of sequence MJVIII (sequence boundary Bt1) is marked by lignite, characterizing subaerial exposure (F5b; Fig. 11;

(

  subcontractus to early morrisi Zones), MJX (late morrisi to orbis Zones), and MJXI (early discus Zone). Maximum regressive surfaces (Bt2-3-4) are marked either by marine perforated surfaces encrusted with bivalves in upper offshore and shoreface environments, or by exposure surfaces with vadose cements, stromatolites, or lignite levels in shoal and lagoonal environments (Figs 5A-B-E and 11). During sequences MJIX and MJX, an echinoderm-rich shallow ramp, prograding northwards, stretched from Argentan to Deauville (F3h, Calcaires de Saint-Pierre-du-Mont and Calcaires de Ranville Formations, Figs 5A, 11 and 12E). A protected lagoon composed of peloidal mudstones to packstones (F4b-c-d, Calcaires de Valframbert Formation, Figs 11 and 12E) developed between the basement highs from Argentan to Alençon. Basement highs were overlain by shallow shoreface and lagoonal facies during the Bathonian (Figs 11 and 12A; Calcaires de Villedieu, Calcaires de Valframbert,

  In this time interval, decompacted sedimentation rates vary from 27 m/My in Poitiers to 46 m/My in Caen, and accommodation rates vary from 27 m/My in Poitiers to 34 m/My in Argentan (Fig. 13). The highest accommodation rates are recorded for sequence MJXI, with values of 83 m/My in Montbron, 130 m/My in Caen and Poitiers, and 240 m/My in Argentan. Continuous subsidence and tectonic subsidence are recorded in the Argentan, Poitiers, and Montbron areas. -Early Callovian (sequence MJXII). The Caen and Argentan areas show high rates of decompacted sedimentation (respectively 76 m/My and 65 m/My) and accommodation (104 m/My, Figs 13 and 14), whereas Poitiers and Montbron are characterized by decompacted sedimentation and accommodation rates of about zero. High positive subsidence and tectonic subsidence rates are recorded for Caen and Argentan, whereas negative tectonic subsidence rates characterized the Poitiers and Montbron areas (Fig. 13). -Late early Callovian to mid Oxfordian (sequences MJXIII to LJIV). Over this interval, high decompacted sedimentation rates (respectively 51 m/My and 58 m/My) and accommodation rates (41 m/My and 46 m/My) are recorded in Caen and Argentan. A negative accommodation rate (-17 m/My) coupled with a high negative tectonic subsidence rate mark an uplift in Caen during sequence LJIV, following a period of relative stability (Figs 13 and 14). Stage 5 is characterized by near-zero rates of decompacted sedimentation, accommodation, and subsidence (Figs 13 and 14). Subsidence and tectonic subsidence curves display negative rates in Poitiers and Montbron over the entire interval. Only sequence MJXIV displays a different pattern in Montbron, with high decompacted sedimentation (154 m/My) and accommodation rates (163 m/My). -Late mid to late Oxfordian (sequences LJV to LJVII). This last phase is characterized in Caen by high rates of decompacted sedimentation (109 m/My) and accommodation (124 m/My), which correlate with major tectonic subsidence (Figs 13 and 14). In Argentan, stage 6 exhibits low decompacted sedimentation and accommodation rates of 27 m/My and 34 m/My, and steady tectonic subsidence. The Poitiers area recorded a very high accommodation rate over sequence LJV (192 m/My), contemporaneous with significant tectonic subsidence (Figs 13 and 14). During deposition of sequences LJVI and LJVII, a stable tectonic phase is recorded in Poitiers, where the decompacted sedimentation and accommodation rates are 34 m/My (Figs 13 and 14). Around Montbron, the decompacted sedimentation rate (67 m/My) and accommodation rate (67 m/My) might have been constant over the last stage, and the area was subsiding (Figs 13 and 14).

  transition and discus subzone maximum flooding surfaces), two within the Callovian succession (koegini and lamberti Zones maximum flooding surfaces), and one within the late Oxfordian (bimmamatum Zone; Fig. 15; Hardenbol et al., 1998a). The absence of several European basin sequences from western France can be explained by (1) non deposition/preservation in proximal areas (hardgrounds and exposure surfaces), especially at the Bathonian/Callovian boundary (Figs 5 and 11), and by (2) condensation in deep claydominated environments, which is the case for Callovian and early Oxfordian sequences (koegini, lamberti and bimmamatum Zones; Fig. 11).

  . The consequences were the very low sedimentation rates (0 to 15 m/My) and overall shallowing(Figs 11 and 13). Around Montbron, lagoon environments expanded northwards during the humphriesianum Zone, marking the regressive maxima of a second-order cycle, and oolitic wedges formed in Poitiers over sequences MJIV and MJV,(Figs 11 and 15). In Caen, uplift was active until the end of sequence MJVII (negative accommodation rate of -17 m/My, Fig.14) and may have induced the shallowing trend marked by upper offshore sponge facies prograding northwards.

  in western France corresponds to Bt4 in Montbron whereas it corresponds to Bt2 in Caen and Argentan (Figs 11 and 15). In Poitiers and Montbron, the uplift phase remained constant until the end of sequence LJIV (Middle Oxfordian, Fig. 13). The postulated lack of deposition of sequences MJXV to LJIV in Montbron was certainly due to emersion due to uplift. Over sequences LJII to LJIV, uplift in the Poitiers area controlled sedimentation despite global eustatic rise, leading to the non-deposition of sequences LJII and LJIII and to the shallowingupward trend marked by the deposition of cross-bedded bioclastic grainstones during sequence MJXIV (Figs 11 and 13). From Poitiers to Montbron, the maximum flooding surface of the Callovian-Oxfordian cycle cannot be positioned in the mariae Zone as for the Caen and Argentan areas or for European second-order cycles, but is located in the tenuiserratum Zone (Figs 11 and 15).

  about 30 m, leading to the progradation of shoreface sands topped by an exposure surface (Roussier de Gacé and Sables ferrugineuxde Vairais Formations, Ox1, Figs 11 and 13). In Caen, drastic shallowing from lower offshore to shoreface between sequences LJII and LJIV during a period of eustatic rise (about +10 m,Hardenbol et al., 1998b) implies a major uplift, of about 40 m (Fig.13). This early/mid Oxfordian uplift made possible the growth of a shallow carbonate platform prograding northwards during sequence LJIV. This carbonate platform persisted until the end of the Oxfordian from Caen to Le Mans. However, the sharp carbonate demise resulting in the deposition of lower offshore clays and in retrograding environments southwards cannot have been the consequence of the eustatic rise alone (about 12 m,Hardenbol et al., 1998b) and must also have been due to intense tectonic subsidence occurring in Deauville over sequencesLJV and LVI (Figs 11 and 13). Deauville is separated from Caen by the Viller-Reux fault which diplays a vertical offset of about 55 m and brought Jurassic and Cretaceous series into contact (Fig.1,[START_REF] Pareyn | Notice explicative de la carte géologique de Lisieux (1/50000)[END_REF]. This fault may have been reactivated during the Late Jurassic, causing the major tectonic subsidence recorded in Deauville. The deepening from shoreface to lower offshore around Poitiers during sequence LJV, in a context of relative eustatic stability (+3 mHardenbol et al., 1998b), and leading to carbonate demise, was the consequence of sudden and intense tectonic subsidence. This event may have been due to the late Oxfordian reactivation of the Lusignan fault: a 100 km-long basement structure oriented NW-SE and affecting Jurassic series to the north of Poitiers

(

  Alençon, sequences MJI to MJVIII are not found overlying the basement, indicating an emerged area from the early Aalenian to the mid Bathonian (Figs 11 and 12A to D). These areas were flooded over sequences MJI to MJIX, during which shallow environments were essentially located on basement highs: from Argentan to Alençon and in Poitiers (Fig. 12A to D). From sequence MJI to MJIX, deep platform environments (lower offshore) were located in basement depressions in Caen and from Le Mans to Saumur (Fig. 12A to D).

  . Topography of the Paleozoic basement controlled lateral depth variations until the mid Bathonian, resulting in the development of (1) shoreface environments from Argentan to Le Mans and in Poitiers and to (2) lower offshore environments in Caen and from La Flèche to Mirebeau. Evolution of tectonic subsidence was reconstructed in four key areas of western France: Caen, Argentan, Poitiers, and Montbron. A major uplift was identified to have occurred over the middle/late Aalenian and the early Bajocian. It corresponds to the Mid-Cimmerian Unconformity. Throughout the Middle Jurassic and Oxfordian, tectonics controlled sedimentation rate and platform architecture; it also triggered two major phases of carbonate growth and demise. Uplifts favoured low sedimentation rates (i.e. late Aalenian to early Bajocian), the occurrence of exposure surfaces and prograding systems, as observed around Montbron during the early to mid Callovian. Tectonic subsidence promoted high sedimentation rates, for example during the Bathonian over the entire western France platform (decompacted sedimentation rate about 70m/my) or during the mid/late Oxfordian around Montbron (decompacted sedimentation rate about 70m/my). The major carbonate production demise at the Bathonian/Callovian boundary was triggered by sharp tectonic subsidence of about 35 m to 55 m, causing an increase in paleodepths. In contrast, the development of the prograding mid-Oxfordian carbonate platform in north-western France was made possible by the tectonic uplift that generated shallow-water and favourable conditions for carbonate growth. A synthesis of sedimentation on western Tethyan platforms was conducted. Two periods of high carbonate production during the Bajocian/Bathonian and middle/late Oxfordian, with prevailing photozoan producers in shallow-marine environments, are synchronous with high eccentricity intervals marked by low δ 13 C values (Martinez and Dera, 2015). Carbonate production was promoted by dry climates disturbed by short episodes of intensive rainfalls and storms leading to (1) high evaporation and carbonate sursaturation and (2) low trophic conditions. Both periods of low carbonate production during the Aalenian and from the middle Callovian to early Oxfordian are synchronous with low eccentricity intervals and high δ 13 C values. This was marked by a wet climate and the eutrophication of epicontinental seas that tend to diminish growth potential of western Tethyan carbonate platforms. The uplift of the Aalenian (corresponding to the Mid-Cimmerian unconformity) lead to the formation of sedimentation hiatus and condensed levels, whereas the global eustatic sea-level rise of the Callovian-early Oxfordian generated an important accommodation space and favored high sedimentation rates.

Fig. 1 .

 1 Fig. 1. Location of the study outcrops, boreholes, and faults with presumed Mid to Late Jurassic activity on a simplified geological map of western France.

Fig. 2 .

 2 Fig. 2. A. Global palaeogeographical map of the Callovian simplified from R. Blakey's maps (http://cpgeosystems.com) B. Location of the study area on a palaeogeographical map of the Western Tethys during the Callovian. C. Location of the study area during the Bathonian in a

Fig. 3 .

 3 Fig. 3. Schematic lithostratigraphic illustration of the north-south transect of the study area.

Fig. 4 .

 4 Fig. 4. Location of the Middle Jurassic to Oxfordian facies with allochem distribution on a downdip profile from the lower offshore to backshore in the western Paris to northern Aquitaine basins. The range of variation of the fair-weather wave base and storm-wave base depths are estimated from Walker and James (1992), Lathuilière et al. (2005), and Sahagian

Fig. 6 .

 6 Fig. 6. A. Clay/marl to marl/micritic limestone alternations -F1a-b-c -Port-en-Bessin (6) -Marnes Port-en-Bessin Formation, sequence MJVIII. B. Mudstone -F1c -Pierre Levée quarry (54) -Banc de Pierre sublithographique Formation, sequence LJVI. C. Historic Bajocian stratotype with ferruginous oncoids (On.), bivalves (Bi.), belemnites (Be.), stromatolites (Str.) and sponges (Sp.) -Sainte-Honorine-des-Pertes (5) -Malière Formation (F1c), Couche verte Formation (F1f), Conglomérat de Bayeux Formation (F1e), Oolithe ferrugineuse de Bayeux Formation (F1d), Calcaire à spongiaires Formation (F2d), sequences MJIV to MJVI. D. Ferruginous oolite (Oo.) wackestone with bivalves (Bi.) -F1d -Sainte-Honorine-des-Pertes (5) -Oolithe ferrugineuse de Bayeux Formation, sequence MJVI. E. Microbialites -F1e -Feuguerolles quarry (18) -Conglomérat de Bayeux Formation, sequence MJV. F. Ferruginous oncoid (On.) floatstone with belemnites (Be.) and bivalves (Bi.) -F1e -Feuguerolles quarry (18) -Oolithe ferrugineuse aalénienne Formation, sequence MJI. G. Glauconite (Gl.) wackestone with quartz (Qz), ferruginous ooids (Oo.), echinoderms (Ech.) and bivalves (Bi.) -F1f -Sainte-Honorine-des-Pertes (5) -Couche verte Formation, sequence MJIV.

Fig. 7 .

 7 Fig. 7. A. Marl/echinoderm limestone alternation with gutter clasts -F2a -Tracy-sur-Mer (7) -Calcaire de Saint-Pierre-du-Mont Formation, sequence MJVIII. B. Echinoderm (Ech.) packstone with peloids (Pe.) -F2a -Cintheaux quarry (20) -Calcaire de Caen Formation, sequence MJVIII. C. Bivalve (Bi.) packstone -F2b -Moulin à Vent quarry (65) -Calcaires argileux de Pamproux Formation, sequence MJXIII. D. Wackestone with sponge spicules (Spi.) -F2d -Limalonges quarry (71) -Calcaires à spongiaires et silex Formation, sequence MJX. E. Sponge (Sp.) limestone -F2d -Sainte-Honorine-des-Pertes (5) -Calcaire à spongiaires Formation, sequence MJVI. F. Coral (boundstone) in marls -F2e -Belle-Eau quarry (32) -Caillasse de Belle-Eau Formation, sequence MJXI.

Fig. 11 .

 11 Fig. 11. Correlation diagram of the Middle Jurassic and the Oxfordian in western France on a

Fig. 12 .

 12 Fig. 12. Facies distribution on carbonate architecture morphology of western France in nine successive steps from Aalenian to Oxfordian in a third-order sequence stratigraphy framework. Potentially active faults, Paleozoic basement and Lias deposits are represented to illustrate the multiple influences on carbonate platform/ramp morphology. A. Ramp geometry marked by the dominance of silty to sandy facies -sequences MJII and MJIII, Aalenian. B. Ramp geometry with condensed ferruginous facies in Caen and bioclastic upper offshore facies from Poitiers to Montbron -sequence MJV, Bajocian. C. Predominance of a storm dominated ramp with sponges, although oolitic facies develop in shallow environments (Montbron, Le Mans)sequence MJVII, Bajocian. D. Bioclastic ramp rich in echinoderms -sequence MJVIII, Bathonian. E. Shallow ramp with echinoderm facies from Deauville to Le Mans, oolitic platform in Poitiers and Montbron -sequence MJX, Bathonian. F. Shallow ramp with bryozoan facies and sponge bioherms from Deauville to Le Mans, upper offshore bioclastic ramp in Poitiers, oolitic shallow platform in Montbron-sequence MJX, Bathonian. G. Lower offshore clayey ramp from Deauville to Mirebeau, bioclastic upper offshore in Poiters; lagoon protected by an oolitic shoal in Montbron -sequence MJXIV, Callovian. H. Shallow protected platforms in Argentan and Montbron, separated by clayey deposits in lower offshore environments -sequence LJV -Oxfordian. I. Emerged platform with soil horizon in Argentan separated from a shallow platform in Montbron by clayey deposits in lower offshore environments -sequence LJVI -Oxfordian.

Fig. 13 .

 13 Fig. 13. Synthetic chronostratigraphic diagram showing western France sequences, eustasism curve (Hardenbol et al., 1998b), bathymetry, decompacted sediment thickness, accommodation, subsidence, and tectonic subsidence curves in Caen/Deauville, Argentan, Poitiers, and Montbron.

Fig. 14 .Fig. 15 .

 1415 Fig. 14. Accommodation rate for each western France sequence in Caen/Deauville, Argentan, Poitiers, and Montbron for the Aalenian to Oxfordian interval.

Fig. 16 .

 16 Fig. 16. Evolution of sedimentation and dominant carbonate producers during the MiddleJurassic and the Oxfordian in western Tethyan platforms represented in its regional palaeogeographical context. Data are compiled from our results (western France) and literature (France, Germany, Spain, England, Scotland, Poland, Italy, Switzerland, Morocco; see table2for references).

Fig. 17 .

 17 Fig. 17. A. Qualitative proportions of allochems in heterozoan and photozoan grain associations (modified from James, 1997), and schematic representation of the distribution of Photozoan-Heterozoan carbonates with respect to common temperature/nutrient gradient (modified from Mutti and Hallock, 2003). The width of the bars indicates estimated abundance of each association from 0-100%. B. Scheme of palaeoenvironmental, sedimentation and carbonate production changes linked to δ 13 C isotopic signal (maxima and minima of eccentricity), local and global tectonism, and eustasy.

  Photozoan

  Photozoan

  Calcaires Crayeux à Stromatolithes de Montbron Formation; Figs5E, 11, 12G). Brachiopod-based biostratigraphy indicates a gap for sequences MJII and MJXIII[START_REF] Foucher | Géodynamique sédimentaire et évolution paléogéographique de la plate-forme nord-est aquitaine au Jurassique moyen (Charente, Dordogne), tome II : Planches[END_REF], and sequences MJXV to LJI might be missing as well.The mid to late Oxfordian interval is composed of five third-order sequences: LJIII (Early plicatilis Zone), LJIV (Late plicatilis Zone), LJV (tenuiserratum Zone), LJVI (glosense to early serratum Zones), and LJVII (late serratum to rosenkranzi Zones). Ooid/coral shallow platform geometries predominate, with very steep slopes (Figs11 and 12H-I). They change abruptly to lower offshore clays around Deauville (Argiles de Villers Formation, Fig.11). These are overlain by the lagoon, mud-supported facies of sequence LJVII (F5c;

	Another ramp profile deepened southwards from Poitiers (shoreface to upper offshore) to
	Saint-Maixent-l'École (upper to lower offshore; Figs 11, 12E, and F). Around Montbron,
	shallow lagoon environments rich in peloids and oncoids (F3b-c-d, Calcaires de Saint-Calcaires à Astrates Formation; Figs, 5B, 11, 12I; Dugué, 1989; Ménillet, 1999).
	Sauveur and Calcaires de Vilhonneur Formations, Figs 5E, 11, and 12E-F) were edged by 4.2.3. Middle to late Oxfordian: Coral/ooid platforms development (sequences LJIII-IV-V-During sequence LJV, facies changed suddenly from marls (Marnes à spongiaires Formation)
	VI-VII)
	ooid/lithoclast wedges progading to the northwest over the mid to late Bathonian (F3j-k, to fine peloid/echinoderm grainstones between Mirebeau and Poitiers (F3a-h; Pierre grise de
	Calcaires de Combe Brune Formation). Bonnillet and Calcaires crinoïdiques Formations), and a ramp deepened from Poitiers to
	4.2.2. Callovian and early Oxfordian: clayey ramp (sequences MJXII-XIII-XIV-V and LJI-II) Ruffec, where lower offshore facies dominated. Over sequences LJVI and LJVII, lower
	The Callovian to early Oxfordian contains six third-order sequences: MJXII (herveyi and offshore clayey environments predominate from Saumur to Ruffec (F1c; Banc de pierre
	Sequence LJIII occurs only in the northern part of the study area, where it is composed of
	clayey offshore facies. Over sequence LJIV and LJV, a shallow platform stretches from Caen
	to Le Mans, where a 100 km-long lagoon developed (F4d and F4a; Calcaires coralliens de
	Mortagne and Calcaires coralliens de la Ferté-Bernard Formations; Figs 5A-B, 11, and
	12H). An oolitic to coral barrier delimited the northern and southern lagoon (F3a-j, Figs 11

The brachiopod fauna in the Calcaires de Valframbert Formation is composed of Burmirhynchia turgida, Rhynchonelloidella elegantula, and Epithyris oxonica that indicate a mid Bathonian age (Subcontractus to Morrisi Zones; sequence MJIX;

[START_REF] Rioult | Discontinuités de sédimentation et unités lithostratigraphiques dans le Jurassique de Normandie[END_REF][START_REF] Rioult | Outcrop sequence stratigraphy of the Anglo-Paris Basin Middle to Upper Jurassic (Normandy, Maine, Dorset)[END_REF]

. The Calcaire et oolithe ferrugineuse à Montlivaltia Formation displays cephalopods (Paroecotraustes waageni, Grossouvria bathonica, Homoeplanulites sp., Cosmoceras contrarium, Opis lorierei, and O. similis) and brachiopods (Rioultina triangularis and Avonothyris sp.) indicating the early late Bathonian, hodsoni Zone (sequence MJX;

[START_REF] Juignet | Notice de la carte géologique de Beaumont-sur-Sarthe (1/50000)[END_REF][START_REF] Gall | Notice explicative de la carte géologique de Sillé-le-Guillaume (1/50000)[END_REF]

. The fauna can be used to date the flooding of the basement highs to the mid and late Bathonian, subcontractus to hodsoni Zones (sequence MJIX and MJX). During sequence XI (Discus Zone), a flat and shallow bryozoan to bivalve-rich ramp stretched from Deauville to Le Mans (F3i-c; Figs

11 and 12F

). Oolitic limestones prograde from Le Mans to La Flèche (Fig.

11

). For sequences MJIX and MJXI, a ramp shallowing southward developed between Poitiers and Saumur. Facies alternate between echinoderm to sponge wacke/packstones (sequences MJIX and MJXI; F2a-d; Calcaires à silex and Calcaires graveleux de Poitiers Formation) and prograding superficial ooid grainstones (sequence MJX and regressive systems tract of sequence MJXI; F3b; Calcaires graveleux de Poitiers Formation; Figs 5C-D, 11, and 12E).

early koegini Zones), MJXIII (late koegini and calloviense Zones), MJXIV (jason and coronatum Zones), MJXV (athleta and lamberti Zones), LJI (mariae and early cordatum Zones), and LJII (Late cordatum Zone). Transgressive systems tracts are characterized by increasingly clayey sedimentation upward, with a gradual disappearance of carbonate beds. The upper reaches of regressive systems tracts are commonly marked by prograding sandy to carbonate deposits until maximum regressive surfaces, corresponding to marine surfaces (Cal1 to Cal4, Ox1), which can display encrusting bivalves and phosphate coatings (Cal4, Foucher 1986), or exposure surfaces, with early meniscus cements (Ox 1; Sables ferrugineux de Varais Formation; Figs 5 and 11). From Deauville to Le Mans, the study area is dominated by a flat clayey ramp (F1a-b-c; Figs 5A-B-C-D; 11 and 12G). From Mirebeau to Poitiers, a ramp progressively shallowed to upper offshore environments dominated by echinoderm to bivalve wackestones/packstones during Callovian sequences MJXII to MJXIV (F2a-b, Pierre des Lourdines and Calcaires argileux de Pamproux Formations, Figs 5C, 11, and 12G). Sequences MJXV and LJI are missing (gap of the athleta to mariae Zones) and sequence LJII is condensed in a less than 1 m-thick carbonate level in Poitiers. A ramp gradually deepened from Poitiers to Ruffec, and the paleodepth then abruptly shallowed at Montbron, with the development of a shallow platform lagoon protected by an oolitic shoal over sequence MJXIV (F3j and F4b; Transgressive systems tracts are characterized by major retrogradations from Deauville to Argentan, from La Flèche to Le Mans, and from Saint-Maixent l'École to Montbron. The maximum flooding surfaces are marked by the deposition of marl to mud-supported upper offshore facies over the entire study area. Regressive systems tracts are marked by major progradations of lagoonal to shoreface environments from Argentan to Deauville, from Le Mans to Saumur, and from Montbron to Saint-Maixent-l'École (e.g. Calcaire oolithique de Lisieux Formation, Fig. 11). Maximum regressive surfaces correspond to periods of maximum expansion of lagoonal and shoreface facies, and may be either marine (Ox4, Ox5 and Ox6) or emersive, with the occurrence of meniscus cements (Ox4, Argentan to Alençon) or soils (Ox6, Caen to Le Mans, Fig. 11 and 12I). and 12H). During the regressive systems tract of sequence LJVI, cross-bedded sands prograded from Caen towards Deauville (F3e, Sables de Glos Formation, Fig. 11). sublithographique, Calcaires argileux et glauconieux de Mirebeau, Marnes grises à spongiaires Formations; Figs 5C, 11, and 12H-I). During the mid/late Oxfordian, the Montbron area saw the emplacement of an ooid/peloidal barrier with coral bioconstructions ahead of a calm lagoon where coral/peloidal mudstones accumulated (F3a-d-j, F4b, Calcaires oolithiques et coralliens de Garat Formation, Figs 5E, 11, and 12H-I).

4.3. Decompacted sedimentation, accommodation, subsidence, and tectonic subsidence -Early to early mid Aalenian (sequences MJI and MJII). This interval is characterized by stable accommodation and near-zero decompacted sediment thickness rates (Figs 13 and 14). Notable decompacted accumulation (13 m/My) and subsidence rates (5 m/My) are only present in the Poitiers area.

  Two general period of low carbonate production occurred during the Aalenian and middle Callovian to early Oxfordian intervals. The middle Callovian to early Oxfordian period is marked by thick clayey accumulations in offshore environments. On the contrary, condensed levels, often ferruginous, prevailed during the Aalenian, while thick marly deposits locally formed in Switzerland, Germany and southern Poland. Shallow environments are marked by crossbedded siliciclastic sands (Scotland, northern Germany, and northwestern France) or heterozan to transitional carbonate grain associations (southern France), except in England (London platform) where oolitic grainstones were deposited during the Aalenian. In low latitude areas (Apennines and Apulia platforms in Italy, Morocco) no neat carbonate production demises are recorded during the Aalenian and Callovian to early Oxfordian intervals, which could be the consequence of more favorable environmental conditions for carbonate growth induced by a drier climate, as suggested byDera et al. (

Table 1 .

 1 Calcaires de Saint-Martial Formation, sequence MJIX. F. Unconformity of Bathonian limestone on Brioverian flyschs -F4b, F4c and F3j -Boitron quarry (39) -Calcaires de Valframbert Formation, sequence MJIX. G. Dolomite formed in a presumably supratidal protected environment, as evidenced by the presence of stromatolites (Le Pochat et al., 1986) -F5a -La Rochebertier (82) -Dolomies de Montbron Formation, sequence MJV. H. Position on the downdip profile, lithofacies, non-bioclastic and bioclastic components, sedimentary and biogenic structures, granulometry, sorting, and paleoenvironmental interpretations of the Middle Jurassic and Oxfordian rocks of western France.

	Caillasses de Basse-Ecarde Formation, sequence MJXI. D. Trough cross-bedding
	stratifications with alternating fine and coarse levels in echinoderm grainstone -F3h -
	Creully quarry (12) -Calcaires de Creully Formation, sequence MJVIII. E-F. Wedge of
	clinobedded oolitic grainstone foresets -F3j and F3k -Combe Brune quarry (84) -Calcaires
	de Combe Brune Formation, sequences MJIX to MJXI. G. Trough cross-bedded oolitic
	grainstone -F3j -Cosses Noires quarry (85) -Calcaires Vilhonneur Formation, sequence
	MJX. H. Lithoclast-oyster rich conglomerate, probably storm deposit -F3l -Fay quarry (41)
	-Sables et graviers de Tessé Formation, sequence MJIII.
	Fig 10. A. Bivalve (Bi.) mudstone -F4b -Garat Quarry (86) -Calcaires coralliens et
	oolithiques de Garat Formation, sequence MJXII. B. Peloidal (Pe.) and oolitic (Oo.)
	packstone to grainstone with quartz (Qz) -F4c -Boitron quarry (39) -Calcaires de
	Valframbert Formation, sequence MJIX. C. Lithoclast (Li.) and oncoid (On.) rudstone with
	miliolids (Mi.), ooids (Oo.), echinoderms (Ech.), and microbial peloids (Pe.) -F4d -
	Vilhonneur quarry (83) -Calcaires de Vilhonneur Formation, sequence MJIX. D. Lithoclast
	(Li.) grainstone with meniscus cements (M. Ce.) -F4d -Combre Brune quarry (84) -
	Calcaires de Combe Brune Formation, sequence MJXI. E. Birdseye in a lithoclast (Li.)
	grainstone with ooids (Oo.), peloids (Pe.), and foraminifers (Fo.) -F4d -Chez Trappe quarry

Acknowledgements

This work is the result of collaborative project no PO4990 between Paris-Sud University and the BRGM. This project was funded by the BRGM and by a doctoral PhD from the French Ministry of Research and Higher Education. We are grateful to Philippe Blanc (Lithologie Bourgogne) for the high-quality thin-sections and to Christophe Durlet and Philippe Courville for the stratigraphy of Aalenian deposits of Orne.

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