Mapping the rise and demise of Urgonian platforms (Late Hauterivian - Early Aptian) in southeastern France and the Swiss Jura

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Cretaceous Research xxx (2012) 1e18

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Mapping the rise and demise of Urgonian platforms (Late Hauterivian - EarlyAptian) in southeastern France and the Swiss Jura

Bernard Clavel a, Marc André Conrad b, Robert Busnardo c, Jean Charollais d, Bruno Granier e,f,*a24 Chemin des Champs d’Amot, F-74140 Messery, Franceb 71 Chemin de Planta, CH-12223 Cologny, SwitzerlandcChemin Meruzin, F-69370 St Didier au Mont d’Or, FrancedDépartement de Géologie et de Paléontologie, Sciences de la Terre et de l’Environnement, 13 Rue des Maraîchers, CH-1211 Genève 4, SwitzerlandeUniversité de Brest, UMR 6538 Domaines Océaniques, 29238 Brest, FrancefCNRS, UMR 6538 Domaines Océaniques, 29238 Brest, France

a r t i c l e i n f o

Article history:Received 26 July 2011Accepted in revised form 9 February 2012Available online xxx

Keywords:UrgonianLate HauterivianBarremianBedoulianAptianSE FranceSwiss JuraOrbitolinidsVocontian basinPaleogeographySequence stratigraphy

* Corresponding author. Département des Sciences ddes Sciences et Techniques, Université de Bretagne OcGorgeu - CS 93837, F-29238 Brest Cedex 3, France. Tel.

E-mail addresses: [email protected] (B. Clavel)(B. Granier).

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a b s t r a c t

Lower Cretaceous carbonate deposits historically called “Urgonian limestones” are widely exposedaround the margins of the Vocontian basin in southeastern France and in the adjacent Swiss Jura. Thispaper presents the history of their rise, growth and sudden demise. Eleven maps were constructed fordeposits ranging in age from the Late Hauterivian pro parte to the Early Aptian (Bedoulian) pro parte.Based on sequential interpretations, they illustrate the present geographical distribution of the innerplatform facies (Urgonian limestones stricto sensu, with rudists), the outer platform facies (essentiallybioclastic deposits) and the basinal facies (slope, hemipelagic, pelagic deposits). These maps depict onlythe final terms of each successive sequence (the late highstand intervals). Chronostratigraphy is con-strained by ammonites found mainly in basinal deposits, by echinoids, by rudists and to a lesser extent bydinoflagellates and calcareous nannoplancton. Inner platform, outer platform and slope (talus) depositsare dated by rich assemblages of orbitolinids and dasycladalean algae. Currently 39 species of orbitolinidshave been recognized and their ranges collated with those of the ammonites in the area.

In the Jura and in Provence the oldest Urgonian deposits are dated early Late Hauterivian, thusshowing the synchroneity of the onset of platform carbonates development on both the southern andnorthern margins of the basin. Thereafter, growth of the platforms led a clearly regressive shallowing-upward trend, resulting from a stepwise progradation toward the center of the Vocontian area, coor-dinated with cyclical exposures in the inner platform areas. The maximum reduction of the platformdeposits occurred early in Late Barremian times, coeval with a noticeable turnover in the orbitolinidsassemblages.

Thereafter, carbonate platform deposition shifted toward the margins of the Vocontian basin. In EarlyAptian time, a well-dated discontinuity of regional extent marks the sudden, almost synchronousdisappearance of the Urgonian deposits.

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1. Introduction

Sequence stratigraphic interpretation (according to EXXONmodel, Van Wagoner et al., 1988; Catuneanu et al. 2011) ofa number of sections and a new biostratigraphic calibration (basedamong other considerations on a refined orbitolinid scale) made

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feasible the recognition of successive sequences in the develop-ment of the Urgonian platforms of southeastern France and theadjacent Swiss Jura. Their build-up and rapid disappearance tookplace in an interval of time ranging from Late Hauterivian to EarlyAptian. Here we present transects that illustrate the resultsobtained to date supplemented thereafter by eleven paleogeo-graphic maps that portray the successive periods of highstanddeposits. They include the Ha5 sequence of the Lower Hauterivianthrough the Bd 3e4 of upper Lower Aptian. A special emphasis ismade on the termination of Urgonian facies deposition, witha number of correlated sections in the Jura, Subalpine, Vivarais,Provence and Vocontian provinces supporting the idea of a rapid,

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nearly contemporaneous demise of shallow-water carbonateseverywhere in the studied area. So it is now possible to reconstructthe development of the Urgonian platforms, dating it to an intervalinvolving the Late Hauterivian, the Barremian and the Early Aptian.Available paleontological criteria are briefly discussed, followed byan examination of the rise and sudden demise of the platformcarbonates, and differences in their development on either side ofthe Vocontian basin.

2. Dating the Urgonian limestones

Paleontological studies involving primarily orbitolinids anddasycladalean algae are progressing. However recent advances ofthis work in southeastern France and the adjacent Swiss Jura(Fig. 1) have made feasible the development of a reasonably

Fig. 1. General location map. A: Jura and Subalpine cha

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precise stratigraphic framework, making it possible to datedepositional sequences and their discontinuities as observed inthe field.

Biostratigraphic analysis of the Urgonian limestones reliesprimarily on the presence in the interior of the platforms, on theirmargins, and in adjacent talus deposits, of numerous orbitolinidsand dasycladalean algae (Clavel et al., 1987, 2007). A recent work,published by Clavel et al. (2009), deals with the distribution oforbitolinids in southeastern France and adjacent portions of theSwiss Jura, in strata dated Late Hauterivian (sequences Ha3 to Ha7pars), Barremian (sequences Ha7 pars to Ba5 pars) and Early Aptian(sequences Ba5 pars to Bd4 pars). Here (Fig. 2), this distribution issupplemented by frequencies, based on data from a number ofsections. Among them 23 include levels containing orbitolinidsassociated with, framed, or capped by beds containing

ins; B: Vivarais; C: Provence. See Fig. 3 for details.

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Fig. 2. Stratigraphic distribution of the orbitolinids and their calibration with the ammonites in southeastern France and the Swiss Jura. Strata are dated Late Hauterivian, Barremianand Early Aptian. A pronounced turnover in species occurs in lower Upper Barremian strata, coeval with a maximum reduction of the Urgonian platform deposits. Data in Clavelet al. (2009) are revised as follows: distributions of Eopalorbitolina charollaisi and Valserina turbinata are corrected. In accordance with observations by J.-P. Masse (Marseille, oralcomm.) and new studies on the Barremian stratotype (Vermeulen, 2005), the TST of the sequence Ba4 begins at the base of the ammonite Sartousiana Zone.

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stratigraphically significant ammonites (Clavel et al., 1986;Charollais et al., 2003, 2009).

Currently, 27 species of orbitolinids are listed in the UpperHauterivian pro parte (sequences Ha3 to Ha7 pars) of the Jura of theSwiss Canton Vaud and of the Vercors massif in France, Urgoniandeposits containing orbitolinids are directly dated Late Hauterivianby assemblages of dinoflagellates and calcareous nannofossils(Clavel et al., 2007). Currently, 36 species of orbitolinids are listed inan interval of time involving the whole of the Early Barremian andthe base of the Late Barremian (sequences Ha7 pars to Ba4 pars). Apivotal turnover of orbitolinids occurred during the lowstand ofBa4 sequence, which included the maximum regression of the seaon the Urgonian platforms. Nearly half of the species of orbitolinidspresent at that moment disappeared. A similar loss took placeamong the dasycladalean algae.

Present higher in the same interval are other fossils that serveto define the Barremian-Aptian boundary: echinoids (Heterastercouloni, H. oblongus), rudists, dasycladalean algae and char-ophytes (Martin-Closas et al., 2009). However, their presenceprovides sufficiently precise biostratigraphic criteria only fora half-stage.

3. Distribution of the facies around the Vocontian basin

Three transects, dated and interpreted in a sequence stratig-raphy point of view, have been used to illustrate the rise, thestepwise growth and sudden demise of the Urgonian platforms on

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either margin of the Vocontian basin (Figs. 3e6). The transects arelocated respectively on the northern, western and southernmargins of the basin. Those shown in Figs. 4 and 5, i.e. on thenorthern and western margins illustrate the development of theplatforms in a relatively stable tectonic setting. On the other hand,the transect shown in Fig. 6, i.e. on the southern margin, is locatedin a structurally complex area.

3.1. Northern margin of the Vocontian area: Jura and northernSubalpine chains

A first transect perpendicular to the structural trends of the Jurain a tract between the French Jura and the Subalpine Chains (Bornesmassif) has already been published by Charollais et al. (2001, 2003).The new transect (Fig. 4) trending NNE-SSW runs for about 300 kmbeginning in the Neuchâtel Jura and continues across the northernsubalpine chains, the Chartreuse and Vercors massifs. It improvesan earlier version by Clavel et al. (1995, fig. 7), for it benefits fromsubstantial data acquired later (Clavel et al., 2007, 2010; Martin-Closas et al., 2009).

This transect illustrates the regional, pulsed, rapid progradationof the outer and inner platform deposits toward the south-southwest. Progradation was also directed toward the southeast(Charollais et al., 2003). This pattern changes to aggradation afterBa1 sequence: surface areas of the successive platforms may thenbe relatively small during sequences Ba2 to Bd1. Sequence Bd2marks a new change in trend to retrogradation. The demise of theplatform took place during the next sequence, i.e. Bd3, that is

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Fig. 3. Location maps of the transect areas. 3A: Jura - Subalpine chains; 3B: Vivarais (1: Montagne de la Serre; 2: Les Darboussières; 3: Gorges de l’Ardèche; 4: Forêt de Bois Sauvage;5: Mas de Gras/Chirolong; 6: Saint Montan; 7: Viviers). 3C: Provence (1: Marseille area; 2: La Fare; 3: Alpilles; 4: SW Monts de Vaucluse; 5: Gorges de la Nesque; 6: Ventoux;7: Rissas). Red arrows ¼ the illustrated transects.

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Fig. 4. Schematic lithostratigraphical transect across the Urgonian limestones in the Jura and Subalpine chains sited on the northern, relatively stable margin of the Vocontian basin.1: charophytes from La Lance (Blanc-Alétru, 1995; Clavel unpublished); 2.: charophytes from Bellegarde e Montanges (Martin-Closas et al., 2009); 3: charophytes from Chartreuse,Pas du Frou and Berland sections (Mojon and Médus, 1990; Arnaud et al., 1998; Mojon, 2002; Clavel et al., 2002, 2007; Martin-Closas et al., 2009) and from Vercors, Font Renard andGorges du Nant sections (Clavel et al., 2007; Martin-Closas et al., 2009); 4: charophytes from the Chartreuse, Pas du Frou and Berland sections (Mojon and Médus, 1990; Arnaudet al., 1998; Mojon, 2002; Clavel et al., 2002, 2007; Martin-Closas et al., 2009); 5: charophytes from the Chartreuse, Pas du Frou sections (Clavel et al., 2002; Martin-Closas et al.,2009); 6: ammonites (Ancyloceras matheroni, Pseudohaploceras matheroni) from the Vercors, le Faz and Rochefort-Samson sections (Paquier, 1900; Jacob, 1907; Girod and Weiss,1965; Arnaud et al., 1998); 7: ammonite (Ancyloceras gr. matheroni) from the Chartreuse, Cirque de Roche Blanche section (Gidon, 1952; Arnaud et al., 1998); 8: ammonite(Deshayesites gr. saxbyi) from the Geneva Jura, Bellegarde e Montanges section (“Valserine valley”, Clavel et al., 2007).

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Fig. 5. Schematic lithostratigraphical transect across the Urgonian limestones in the Vivarais. 1: ammonites (Holcodiscus diversecostatus, Astieridiscus menglonensis) from the Gorgesde l’Ardèche - Serre de Tourre (coll. Busnardo, Clavel et al., nearing completion); 2: ammonites (Toxoceras moutonianum, Holcodiscus perezi) from Mas de Gras (Schroeder et al.,2000; Clavel et al., 2007); 3: ammonite (Toxoceras gr. moutonianum) from the Forêt de Bois Sauvage e Chastelas de Baravon section (Renaud, 1978); 4: ammonites (Puezalpellacf. uhligi, Silesites cf. cirtense) from the Gorges de l’Ardèche - Serre de Tourre section. (Clavel et al., nearing completion); 5: ammonite (Pseudocrioceras sp.) from the Gorges del’Ardèche - Pont d’Arc section (coll. Busnardo, Clavel et al., nearing completion). For symbols, see Fig. 4.

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Fig. 6. Schematic lithostratigraphical transect across the Urgonian limestones of Provence. For symbols, see Fig. 4.

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Fig. 7. Latest Barremian and earliest Aptian evolution of the northern Urgonian platform in a proximal setting (innermost platform). The section illustrates the succession of theUrgonian strata near Bellegarde-Montanges, west of Geneva in the French Jura (Ain Department). Five sequences (Ba2 to Bd1) are missing below a conspicuous disconformity, whilefarther south the deposits that represent these sequences are present. Log: Martin-Closas et al., 2009; biostratigraphy: Clavel et al., 2007; sequence stratigraphy: this work. Forsymbols, see Fig. 13.

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during the Early AptianWeissi ammonite Zone. In Chartreuse, thereis no record of sequences younger than Bd2 due to post-depositional (Late Cretaceous) erosion. In southern Vercors too,erosionmay even cut deeply into Barremian strata.We found relictsof Upper Barremian and Lower Aptian platform carbonates depositsfarther south in the Vocontian basin where they are found withinhuge debris flows and megaslumps involving mostly slope facies(see sub-section 3.4).

The paleogeographic setting at Bellegarde-Montanges(southern Jura, southwest of Geneva) is illustrated in Fig. 7. Therudistid limestone forming the lower third of the section is dated byorbitolinids and dasycladalean algae as lowermost Barremian (Ba1sequence). A large, conformable discontinuity terminates this unit.The hiatus involved covers the stratigraphic range of five sequences(Ba2 to Bd1, i.e. Barremian pro parte and Lower Aptian pro parte).These missing sequences are present south, because there thehiatus is progressively shorter. At Bellegarde, the sequences Bd2and Bd3 are dated Early Aptian by ammonites and orbitolinids.Fresh or brackish water deposits containing charophytes occur atthe base of the series (Martin-Closas et al., 2009). As shown by thesmall maps in Fig. 8, highstand deposits of the sequences Ba4 andBa5 follow a southward progradational trend. In contrast, above thediscontinuity the trend is clearly retrogradational, starting withBd1 sequence.

Fig. 8. Depositional environments and the final discontinuity between Urgonian facies anddemise of the Urgonian platform in the western Vocontian area. Correlated with the BedouliaEvent (OAE1a) noted. 1) Cassis-La Bédoule: log and biostratigraphy: Moullade et al., 1998aVallon-Pont-d’Arc (Mézelet), and others sections: logs and biostratigraphy: Busnardo in Elm

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Fig. 9 depicts the depositional environments underneath thefinal discontinuity of the Lower Aptian (Bedoulian) Urgonian stratain the northern Vocontian domain. The succession has beencorrelated with the Bedoulian stratotype at Cassis-La Bédoule, eastof Marseille (Moullade et al., 1998a,1998b). The Selli Oceanic anoxicEvent (OAE1a) matches the HST of the Bd3 sequence.

3.2. Western margin of the Vocontian basin: Vivarais - Ardèchetransect

Located on the western margin of the Vocontian basin thistransect (Fig. 5) trending WSW-ENE with a length of about 35 km,subtends the area between theMontagne de la Serre and the Rhônevalley and cuts across the Cevennes fault. It occupies only thecentral part of the platform. In this region a general, eastwardlyprogradation in the direction of the Vocontian basin occurred.

Eastward progradation takes place in strata dated Early Barre-mian and Late Barremian pro parte. Higher up, aggradation occurswhere the transect crosses the center of the platform. Platformconditions ceased to exist in strata referred to the middle LowerAptian (Weissi Zone).

Six sections (Fig. 8) present the depositional environments andfinal discontinuity of the Lower Aptian (Bedoulian) Urgonian stratain Vivarais (western margin of the Vocontian domain). Correlations

upper Lower Aptian (upper Bedoulian) strata in Vivarais (Ardèche): dating the overalln stratotype at Cassis-La Bédoule, east of Marseille. Location of the Selli Oceanic Anoxic, 1998b; sequence stratigraphy: this work; 2) Bourg-Saint-Andéol (Font de Beaume),i et al. (1996); Busnardo, unpublished; sequence stratigraphy: this work.

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Fig. 9. Depositional environments and the final discontinuity between Urgonian facies and upper Lower Aptian (upper Bedoulian) strata in the Jura and Vercors dating the overalldemise of the Urgonian platform in the northern Vocontian area, and correlated with the Bedoulian stratotype at Cassis-La Bédoule, east of Marseille. The location of the SelliOceanic anoxic Event (OAE1a), above the flooding event, is highlighted. 1) Cassis-La Bédoule: log and biostratigraphy: Moullade et al., 1998a, 1998b; sequence stratigraphy: thiswork; 2) L’Achard: log and depositional environments: Arnaud-Vanneau, 1980, modified; biostratigraphy: Arnaud-Vanneau, 1980; Busnardo, unpublished; sequence stratigraphy:this work; 3) Les Rimets: log: Clavel, unpublished; biostratigraphy: Arnaud-Vanneau, 1980; Busnardo, unpublished; sequence stratigraphy: this work; 4) Bellegarde e Montanges:log: Clavel et al., 2007; Delamette in Clavel et al. (2007); biostratigraphy: Delamette in Clavel et al. (2007); sequence stratigraphy: this work; 5) La Presta: log : Clavel et al., 2007;biostratigraphy: Renz and Jung, 1978; sequence stratigraphy: this work.

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Fig. 10. Latest Barremian and earliest Aptian evolution of the southern Urgonianplatform in a distal setting (outermost platform). The section illustrates the succession of the Urgonianstrata at Gorges de laNesque, northeast of Avignon (Provence). Log:Masse,1976,modified; ammonites:Masse,1976; Busnardo, unpublished; bio- and sequence stratigraphy: thiswork.For symbols, see Fig. 13.

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are made with the Bedoulian stratotype at Cassis-La Bédoule, eastof Marseille.

3.3. Southern margin of the Vocontian basin: Provence transect

As shown by the transect in theMarseille area (Fig. 5), the oldestinner platform deposits are dated early Late Hauterivian. So theonset of Urgonian limestone deposition was synchronous in thesouthern and northern margins of the basin. However, in southernProvence these Upper Hauterivian platform deposits are uncon-formably overlain by Upper Barremian hemipelagic sediments ofthe South-Provence furrow (Masse, 1976). Higher in the successionof this area, platform progradation began in the basal Barremian,moving northward in the direction of the Vocontian basin.However, here too the demise of shallow-water carbonatesoccurred during Early Aptian times (Masse, 1976; Masse andFenerci-Masse, 2011), above Bd2 sequence.

The transect is located on the southern margin of the Vocon-tian basin. Note the conspicuous progradational trend, ending in

Fig. 11. Depositional environments and the final discontinuity between Urgonian facies andthe Gard (southern margin of the Vocontian domain): dating the overall demise of the Urgoat Cassis-La Bédoule, east of Marseille. Location of the Selli Oceanic Anoxic Event (OAE1asequence stratigraphy: this work; 2) Plateau d’Albion: logs and depositional environmenLe Rissas: logs, depositional environments and biostratigraphy: Monier, 1986; sequence stMasse, 1976 modified; biostratigraphy: Leenhardt, 1883; Masse, 1976; sequence stratigraphy:biostratigraphy and sequence stratigraphy: this work; 5) Gargas - Le Chêne: logs and depositMoullade et al., 2009; sequence stratigraphy: this work; 6) Serviers: logs and depositional en1990; Conte, 1999, 2001; Masse and Fenerci-Masse, 2011; sequence stratigraphy: this work

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the middle Early Aptian. Post-depositional erosion may havecaused ablation and downslope transportation of Lower Aptiandeposits.

The Gorges de la Nesque section northeast of Avignon wasfirst surveyed by Masse (1976). Here, the Upper Barremiansequences appear to be complete and inner platform depositswith rudists are found high enough to include the Lower AptianBd1 sequence. As shown in the small maps of Fig. 10, the rise ofthe platforms clearly follows a northward progradational trend.Like that of the northern margin of the basin, a change in trendto retrogradation occurs at the base of Bd2 sequence. Thetransgression is marked by a change in facies to outer platformdeposits.

Fig. 11 shows the depositional environments and the termi-nating discontinuity of the Lower Aptian (Bedoulian) Urgonianstrata in the Monts de Vaucluse (Provence) and the Gard (southernmargin of the Vocontian domain). Again, correlations are madewith the Bedoulian stratotype at Cassis-La Bédoule, east ofMarseille.

upper Lower Aptian (upper Bedoulian) strata in the Monts de Vaucluse (Provence) andnian platform in the southern Vocontian area. Correlated with the Bedoulian stratotype) noted. 1) Cassis-La Bédoule: log and biostratigraphy: Moullade et al., 1998a, 1998b;ts: Masse, 1976; biostratigraphy: Kilian, 1888; sequence stratigraphy: this work; 3)ratigraphy: this work; 4) Gorges de la Nesque: logs and depositional environments :this work. Rustrel-Lagarde: logs and depositional environments: Masse, 1976 modified;ional environments: Moullade, 1963; biostratigraphy: Leenhardt, 1883; Moullade, 1963;vironments: Clavel, unpublished; biostratigraphy: Dumas, 1876; Pellat, 1903; Thieuloy,.

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Fig. 12. Schematic lithostratigraphical transect across the northwestern margin of the Vocontian basin illustrating the geographical distribution of Urgonian, slope and basinaldeposits dated Early Barremian pro parte to Early Aptian pro parte, according to Ferry (1988). A: paleogeographic map; B: location map; C: lithostratigraphical transect according toFerry (1988), revised; D: lithology and significant fauna according to Ferry (1976); bio- and sequence stratigraphy according to the present authors.

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3.4. Fourth transect: the northwestern margin of the Vocontianbasin

The relationship of the edge of the Urgonian platform to thenorthwestern margin of the Vocontian basin has been discussed inseveral publications (Ferry, 1976, 1979, 1988; Ferry and Flandrin,1979). We refigure their principal conclusions (Fig. 12).

During Late Barremian and Early Aptian times the northwesternmargin of the Vocontian basin sank to form a saddle (the Rhoda-nian corridor) separating the Vercors and Vivarais Urgonian plat-forms. The related fan is represented, farther in the deep VocontianTrough, by bioclastic debris flows, megabreccias, along with largelenses of slump ranging up to 10 sq km in area from the ablatedmargins of the platforms. The largest lenses have been mapped bythe aforementioned authors. Here (Fig. 12) these phenomena areillustrated by a revision of Ferry’s original profile (1988) and his LaChaudière section (1976) whereby the debris flows correspond tolowstand deposits. Correlations are also made with the stratotypicsections.

4. Paleogeographical maps

The 11 maps of Figs. 13 and 14 illustrate the progradation andretrogradation of the platforms in the several domains (Jura,Subalpine, Vivarais, Provence, and Vocontian), surrounding theVocontian basin. They are built to show highstand deposits, sorepresent only the upper part of the sequences named. In theLate Hauterivian pro parte, inner platform deposits, commonlywith rudists (historically the Urgonian limestones sensu stricto),

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are first developed only in the Jura and southern Provence,Marseille area. They then expand, progressively and concentri-cally, toward the depositional center of the basin. In lowermostBarremian strata (Ba1 sequence), highstand deposits appear inthe Vivarais and the northern subalpine chains. Progradationcontinued southward in Vercors (south of Grenoble), eastward inthe Vivarais and northward in Provence. By Early Aptian times(sequences Bd1 and Bd2), Urgonian deposits are present in all ofthe northern Subalpine chains, the Vivarais and southernProvence.

The main steps of this evolution are as follows, noting thatbecause the succession of outcrop sections is diachronous, none ofthem can span the whole of the time represented by these Urgo-nian deposits:

1. onset of the carbonate platforms, with bioclastic marginal andrudistid inner platform deposits. These appear as early as thebase of the Late Hauterivian in the central Jura and Provence(references for 1, 2, 3, 4: Clavel et al., 1986, 1987, 1995, 2002,2007, 2010; Charollais et al., 2003, 2008, 2009; Conrad et al.,2011; Schroeder et al., 2000; Martin-Closas et al., 2009);

2. stepwise progradation expands in all directions toward theVocontian basin;

3. cyclical exposures occur in the innermost platform areas,paired with long hiatuses in the more distal areas (Jura);

4. a maximum reduction of the platform deposits occurs early inLate Barremian time;

5. Upper Barremian and Lower Aptian platform debris are trans-ported into the basin (Ferry, 1976, 1979, 1988; this work).

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Fig. 13. Geographical distribution of the Urgonian, slope and basinal deposits from Upper Hauterivian pro parte (Ha5 sequence) to Lower Barremian pro parte (Ba2 sequence). Onlyhighstand deposits are shown.

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6. platform demise dated Early Aptian is sudden and almostsynchronous in all localities (this work), a conclusion that doesnot concern the whole of the Provence platform becauseearlier, near the transition from the Barremian to the Aptian,two segments, a Northern and a Southern domains, get indi-vidualized by the collapse of the median segment of thisplatform, that is by the genesis of the South Provence basin(Masse and Fenerci-Masse, 2011).

5. Dating the end of the Urgonian platforms as illustrated bysections of the upper portion of the Urgonian limestones inthe southern Jura and in southeastern France

From a stratigraphic standpoint these sections are properlydated, directly by ammonites or indirectly by coeval assemblages oforbitolinids, dasycladalean algae and charophytes. Because theranges of the microfossils have been calibrated in basinal or tran-sitional (talus) settings on the ammonite zones they allow us toidentify the sequences in the platform environments too. Fig. 15depicts the known distribution of the most significant Bedoulian

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ammonites in the stratotypic section of Cassis-la Bédoule, alongwith the corresponding biozonation and a tentative scheme of theirsequential distribution.

The paleontological data and correlations shown in Figs. 8, 9and 11 are based mainly on literature. They are constructed todelineate the demise of the Urgonian platforms on the northern(Fig. 9), western (Fig. 8) and southwestern (Fig. 11) margins of theVocontian basin. Each of the 15 outcrop sections shown in Figs. 8, 9and 11 is correlated with the Lower Aptian basinal deposits atCassis-La Bédoule, east of Marseille. At this location a conspicuousdiscontinuity caused by emergence occurs just above Bd2sequence. Based on paleontological evidence (ammonites andorbitolinids below and above the discontinuity), the Urgonianplatforms lost their identities almost synchronously everywhere inthe area surrounding the Vocontian basin, during the lowstand ofour Bd3 sequence, in the upper part of the Weissi ammonite Zone.Below the discontinuity, the distribution of three types of sedi-mentation (lagoon, shoal -eventually preserved in channels- andouter ramp) shows that the facies of the inner platform areprogressively younger toward the margins of the basin, thus

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Fig. 14. Geographical distribution of the Urgonian, slope and basinal deposits dated Early Barremian pro parte (Ba3 sequence) and Early Aptian pro parte (sequence Bd3/4). Onlyhighstand deposits are shown. Note the inception of a northward transgressive, onlapping trend in sequence Ba4. Arrows shown in sequences Ba4 and Bd3/4 indicate downslopetransportations of platform deposits. For symbols, see Fig. 13.

B. Clavel et al. / Cretaceous Research xxx (2012) 1e18 15

illustrating the retrogressive-transgressive character of Urgoniandeposits during Early Aptian times.

6. Discussion

The phenomenon responsible for the termination of the Urgo-nian platforms is often referred to as a typical example of“drowning” events. However this name does not offer a key to anunderstanding of how andwhy Urgonian sedimentation came to anend. The “drowning” concept was first introduced to explainstratigraphic events during which production of carbonate sedi-ments stopped abruptly: it was assumed to be caused by a rapid riseof the relative sea-level “submerging” the platform to a level belowthe euphotic zone (Schlager, 1981). In our opinion, the sameconcept is better expressed by the term “give-up” (Neumann andMacIntyre, 1985). Schlager (1989) suggested that drowning eventscould also be effected by a decrease in the clarity of the water (dueto an increase of its turbidity) or even by a sea-water cooling. His

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concept originally applied to isolated platforms (like the Bahamas).When platform growth take place on the margin of a continent(Florida for example), a rapid transgression leads to a landwardshift of the shoreline and to the back stepping of the carbonatefacies, but not to their demise. For example, for the Wilmingtonplatform illustrated by Schlager (1989), it is correct to say that thereis no record of Lower Valanginian carbonate sediments in the distalpart of the continental shelf, however shallow-water carbonatesare present in the proximal area: there facies belts are merelybackstepped at the distances prescribed by the amplitude of therelated transgression.

In the Urgonian platforms, the flooding events of the sequencesBd3 and Bd4 led to deposition of hemipelagic facies immediatelyabove the fossilized Urgonian platforms. Carbonate sedimentationprobably backsteppedonpreviously emergent tracts. Hypothetically,we suggest that the rise in relative sea-level made possibleconnectionswith cooler northern seawayswhich caused a change insedimentation from tropical carbonates to cooler-water carbonates.

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Fig. 15. Stratotypic Bedoulian section at Cassis e La Bédoule. Log and biostratigraphy: Moullade et al., 1998a, 1998b; Ropolo et al., 1998, 2008a, 2008b; additional biostratigraphicdata from Bogdanova and Tovbina (1994); sequence stratigraphy: this work. Location of the Selli Oceanic Anoxic Event (OAE1a) noted.

B. Clavel et al. / Cretaceous Research xxx (2012) 1e1816

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B. Clavel et al. / Cretaceous Research xxx (2012) 1e18 17

7. Conclusions

Advances in paleontological studies, particularly those con-cerning the taxonomy and distribution of the orbitolinids, permita calibrated interregional correlation of the strata in an Urgonianfacies that then delimited the Vocontian basin and its adjuncts. Thebulk of Urgonian limestones range in age from the time representedby the youngest beds of the Upper Hauterivian substage, the wholeof the Lower Barremian and the lower Upper Barremian. Withinthis interval the depositional setting is clearly progradational onboth margins of the Vocontian basin, confirming a model explicitlydescribed and named more than a decade ago (Clavel et al., 1995,2007). This interpretation is clearly the opposite of that putforward by H. Arnaud (in Adatte et al., 2005) and Godet et al. (2010)as discussed in detail in Conrad et al. (2011).

In the long term the “maximum regression” (that is, themaximum reduction of the platform deposits) observed in the earlyLate Barremian (during the lowstand of the Ba4 sequence) is coevalwith a pivotal turnover in the distribution of the orbitolinids, and asyet not properly documented with that of the dasycladalean algae.From that point in time, the carbonate factory moved toward themargins of the basin and succeeding platforms are generallynarrow fringes with an aggradational rather than a progradationalpattern. In Early Aptian time, that is in the Weissi ammonite Zone,a pronounced discontinuity marks the final, almost synchronousdisappearance of the carbonate platforms.

Acknowledgments

The core of this paper was presented during STRATI2010(4ème Congrès Français de Stratigraphie, UPMC, Paris, August30eSeptember 2, 2010) in the form of a set of conferencesand posters: http://www.univ-brest.fr/geosciences/conference/ocs/index.php/CFS/STRATI2010/schedConf/presentations

We thank the guest editors, Michel Moullade and Peter Skelton,as well as Serge Ferry and an anonymous reviewer, whosecomments and suggestions have helped improving the originalmanuscript.

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