12th Meeting of the International Nannoplankton Association (Lyon, September 7-10, 2008)

Guidebook for the post-congress fieldtrip in the Vocontian Basin, SE France (September 11-13, 2008)

Emanuela MATTIOLI (special editor), Silvia GARDIN, Fabienne GIRAUD, Davide OLIVERO, Bernard PITTET & Stéphane REBOULET

ISBN 978-2-916733-02-9 Dépôt légal à parution Manuscrit en ligne depuis le 7 Septembre 2008 Manuscript online since September 7, 2008

Carnets de Géologie / Notebooks on Geology - Book 2008/01 (CG2008_BOOK_01)

Guidebook for the post-congress fieldtrip in the Vocontian Basin, SE France (September 11-13, 2008)

Emanuela MATTIOLI (special editor) 1,2, Silvia GARDIN 3, Fabienne GIRAUD 1, Davide OLIVERO 1, Bernard PITTET 1 & Stéphane REBOULET 1

1 UMR 5125 PEPS (CNRS), Université Lyon 1, Campus de la DOUA, Bâtiment Géode, 69622 Villeurbanne Cedex (France) 2 [email protected] 3 UMR 5143 (CNRS), Université Pierre et Marie Curie, Paris 6, 75013 Paris (France) Manuscript online since September 7, 2008

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Carnets de Géologie / Notebooks on Geology - Book 2008/01 (CG2008_BOOK_01)

Chapter 1. The Aalenian-Bajocian northward, with many hiatuses (JAUTÉE, 1984). (Middle Jurassic) of the Digne Basinal facies, represented by marl-limestone alternations, are recorded in the southernmost area areas but in the sector south of the Verdon Davide OLIVERO with the contribution of River a shallow-water platform developed, Emanuela MATTIOLI documented by the occurrence of bioclastic limestones with corals. This development is Geographical and geological context evidence of a progressive extension to the Provence platform southward. The Digne area is located in southeastern France (Fig. 1.1), in the department of "Alpes In the Middle Jurassic, the central part of the de Haute-Provence". French authors classically basin (Laragne area, North of Sisteron; Fig. name this region the "Dauphinois Basin", for 1.2) was subject to strong subsidence, as the major portion of the Jurassic period, and evinced by dark-colored marls formed under the "Vocontian Trough" (or Basin) for the Late dysoxic conditions ("Terres Noires" Formation). Jurassic - Late Cretaceous interval. For the Conversely, along the southernmost edge of the Jurassic succession discussed here the name basin, shallower facies and a dominantly carbo- "French Subalpine Basin" is preferred. In nate sedimentation are documented (ELMI, Jurassic and Cretaceous times the French Sub- 1984). A marked regression occurred during the alpine Basin was a gulf located along the Late Jurassic (ATROPS, 1984), when calcareous northwestern margin of the Tethys (Fig. 1.2). sediments indicative of a shelf environment The gulf was bounded to the West by the were deposited over the entire basin (Tithonian Paleozoic "Massif Central" and to the East by cliffs). the Alpine chain. To the South, was a land mass represented now by the Corsica-Sardinia and Maures-Esterel massifs. From Berriasian through Aptian times, in a general regime of extensional tectonics, the depth of the basin increased progressively. Some authors (LEMOINE, 1984, 1985) Limestone-marl alternations were deposited on consider the French Subalpine Basin as an the Tithonian older strata (ATROPS, 1984). A analog of the present European margin of the maximum depth was probably attained during Atlantic Ocean, for it was formed by a series of the Aptian-Albian interval. At the end of the tilted blocks that deepened eastward toward the Albian, the basin began to be infilled; general open Tethyan Ocean. FERRY (1990) suggests emergence took place during the Santonian. that the evolution of the area was in relation This uplift is contemporaneous with the first with an aborted rift basin. In this view, the phase of Alpine tectonics: the "Pyrénéo- French Subalpine Basin may be considered as a Provençale" phase. This phase involved the sort of pull-apart basin. In Middle Jurassic formation of structures with a general W-to-E times, the French Subalpine Basin was a trend. transitional area between the epicontinental sea of the Paris Basin and the deeper water Piedmont domain, where an oceanic ridge was The Aalenian – Bajocian active until the Early Cretaceous. The basin The Aalenian-Bajocian interval in the Digne probably attained its maximum depth (~500 - area is represented by a thick series of marl- 800 m) in the Early Cretaceous (Hauterivian- limestone alternations. Limestones are both Barremian; FERRY, personal communication). packstones (with recrystallised Bositra, rare benthic foraminifers and siliceous sponge Geological history spicules) and wackestones with radiolarians, rare Bositra, lagenid foraminifers and sponge The French Subalpine Basin began its spicules (PAVIA, 1983). Marls are locally very development during the Middle to Late Triassic, shaly and finely laminated. This stratigraphic with the formation of a Germanic-type salt succession is the equivalent of the "Calcaires à basin along the fractured Alpine margin of the Cancellophycus" Formation, which in the Digne Tethys in which evaporites predominate (FERRY, area is dated Middle Aalenian - end of Bajocian 1990). During Jurassic times the shallow sea or basal Bathonian. These limestones are deepened after a general marine transgression overlain by the dark-grey to black marls of the (HALLAM, 2001). In the Early Jurassic, a "Terres Noires" Formation. The thickness of the threshold (the Verdon sill) separated a shelf "Terres Noires" Fm. ranges widely in the French area (the Provence Platform) to the north from Subalpine Basin: it may reach 700 metres in a deeper facies (dolomitic limestones) to the the section near Les Dourbes (Figs. 1.1b and c). south. On this threshold is a sedimentary The age of the Terres Noires Formation is Late succession consisting of mixed carbonate-silico- Bathonian to Middle Oxfordian, with a hiatus at clastic sediments that is reduced in thickness its base.

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S Figure 1.1. (a) Location of the stops to be made during the fieldtrip in SE France. (b) Location of the sections to be visited during day 1 near the towns of Digne and Barrême. (c) Topographic map showing the location of the Feston section near Les Dourbes (SE of Digne; day 1, stop 4). common, represented mainly by Chondrites and Cephalopods (ammonoids, belemnoids and Zoophycos (Cancellophycus of French authors). nautiloids) are locally abundant both in the Locally Zoophycos can be very abundant "Calcaires à Cancellophycus" and in the "Terres (OLIVERO, 2003). These marl and limestone Noires" formations, their presence thus allowing alternations were deposited on the continental detailed biostratigraphical studies (STURANI, slope, at depths ranging between 300 and 500 1967; PAVIA, 1973, 1983). Ichnofossils are also metres (OLIVERO, 2003).

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Day 1 – Stop 4. Les Dourbes section have been carried out (PAVIA, 1973, 1983; PAVIA & STURANI, 1968), and a sequence In the Digne area, an uninterrupted and stratigraphy has been developed (FERRY, 1990, beautifully exposed section covering the entire 1991; FERRY & MANGOLD, 1995). The base of Middle Jurassic exists in the "Ravine du Feston", the section studied by PAVIA (1973) is at the near Les Dourbes, 5 km east-southeast of floor of the valley, and can be followed up to Digne (Fig. 1.1b). The section is exposed on the the ridge from an elevation of 874 metres to norteast side of the valley (Fig. 1.1c). Here, the the Serre d'Enchas, a few tens of metres south Bajocian succession is 250 metres thick (Figs. of the village of Condamine (Fig. 1.1c). 1.3 and 1.4). Several biostratigraphical studies

S Figure 1.2. The French Subalpine Basin or Vocontian Basin was bounded by the crystalline basement of the Massif Central to the West, by the Provençal Platform to the South and it was open to the East towards the Tethys Ocean. The basin-platform boundaries for Jurassic and Cretaceous times are also shown.

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S Figure 1.3. Picture (taken from the road D19) showing the different formations encountered in the Feston – Les Dourbes section, in particular the transition from the Calcaires à Cancellophycus to the Terres Noires formations is clearly visible. Ammo- noid zones are also indicated. W Figure 1.4. Stratigraphical log of the Feston – Les Dourbes section (modified after FERRY & MANGOLD, 1995). Biostratigraphical limits are sited in accordance with PAVIA (1973, 1983). The relationships of nannofossil biohorizons to ammonoid biozones are those of ERBA (1990), who has studied three sections in the Digne area. Note that large Watznaueria contracta and small W. manivitiae sensu MATTIOLI & ERBA (1999) correspond respectively to Watznaueria sp. 4 and Watznaueria sp. 5 of ERBA (1990).

The lower part of the section is made up of an alternation of limestones and shaly marls dated as the Humphresianum ammo- nite Zone. After a clear break in the topographic profile (Fig. 1.3), the marl-limestone alternations become richer in clays, especially in the upper part of the section. This interval corresponds to the Niortense (42 m) and Garantiana ammonite zones, and to the Tetragona Subzone (43 m), where a slump of 8 metres is clearly visible (Fig. 1.4). The upper part of the section (Par- kinsoni ammonite Zone) is char- acterized by thin calcareous beds in alternation with thick marls. In time terms this interval corres- ponds roughly to the base of the "Terres Noires" Formation. A hiatus followed by a flooding surface (Ferry, 1990) separates the Bajocian from the Bathonian stage. The basal Bathonian is represented by the Zigzag ammonite Zone (Convergens Subzone) in a "Terres Noires" facies.

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S Figure 1.5. Five of the six morphotypes of Watznaueria britannica described by GIRAUD et alii (2006) were found in the Feston – Les Dourbes section. Note that preservation in the samples ranges from moderately good to poor.

of the six morphotypes described by GIRAUD et Nannofossil biostratigraphy alii (2006). In the forms of Early Bajocian age, Three sections of the Digne area were five of the six morphotypes described by GIRAUD et alii (2006) were recognized: mor- studied by ERBA (1990): the Beaumont section (close to the Les Dourbes section), Chaudon photypes A, B, D, E and F (Fig. 1.5). The (near Barrême), and La Blache (near Castel- morphotypes A and B are recorded from the lane, some 10 km south of Barrême; Fig. 1.1b). base of the Bajocian. Morphotypes D, E and F The several bio-horizons, precisely correlated are in samples of Late Bajocian age. They appear after the last occurrence (LO) of by ERBA (1990) with the ammonite zones, are shown in Figure 1.4. The most striking pattern Carinolithus superbus. In the light of recent of events in Figure 1.4 is the great number of study on cryptic or pseudo-cryptic species first occurrences (FO) in the vicinity of the (GEISEN et alii, 2002), it cannot be completely Aalenian/Bajocian boundary. The new occur- excluded that the morphotypes shown by rences are mainly species of the genus GIRAUD et alii represent discrete biological Watznaueria, which experienced a major species. diversification at that time. In fact, only three species of Watznaueria are known from the The increase in speciation between the Late Toarcian, namely W. fossacincta, W. colacicchii, Aalenian and the Early Bajocian represents the and W. contracta. Conversely, in the interval second major pulse of diversification in Jurassic between the end of the Aalenian and the Early coccolithophores, following the first speciation Bajocian, several new species of Watznaueria at the Pliensbachian/Toarcian boundary. make their appearance, in a number of mor- Furthermore, the Aalenian/Bajocian diversi- photypes. fication is coincident with the emergence of the genus Watznaueria that soon becomes The FOs shown in Figure 1.4 may dominant in the assemblages of coccoliths underrepresent their true number. In fact, only during the remainder of the Jurassic and the the FO of W. britannica and of the large entire Cretaceous. This major event in coccolith history is probably a result of an important morphotype of W. britannica are noted by ERBA (1990), repectively in the Discites and Sauzei change in paleoceanographic conditions in Mid ammonite zones. Recently, in the Oxfordian of Jurassic times. The pattern of oceanic circu- lation was altered and the surface occupied by SW Germany, GIRAUD et alii (2006) differ- rentiated six morphotypes of W. britannica that epicontinental seas was reduced at that time, differ in size significantly. Using biometrics, the probably in relation to the establishment of authors interpret these morphotypes to be the effective connections between the western result of intra-specific variability, in particular in Tethys and the central Atlantic. It is however the size of the coccoliths. However, differences difficult to differentiate any one cause that also exist in the structure of the bridge in the triggered coccolithophore evolution. A combi- nation of various environmental modifications central area of the coccoliths of the several 2 morphotypes. Unfortunately, this structure is (such as changes in pCO , nutrient availability, too small to be analysed biometrically. A few of ocean chemistry, climate, and sea level the samples from the Les Dourbes section have fluctuations) may together have been respon- been studied, in order to check the occurrence sible for evolutionary innovations (ERBA, 2006).

6 Carnets de Géologie / Notebooks on Geology - Book 2008/01 (CG2008_BOOK_01) Chapter 2. The Global Boundary The alternation of marl and limestone has Stratotype Sections and Points been interpreted as the result of cycles in the production of calcareous nannoplankton caused (GSSP) of the Hauterivian: La by climatic fluctuations in the MILANKOVITCH Charce section (Drôme, France, frequency band (COTILLON et alii, 1980; Vocontian Basin) GIRAUD, 1995). Alternatively, REBOULET et alii (2003) have proposed for the Vocontian Basin a Stéphane REBOULET model of cyclic export of carbonate mud from Introduction shallow platform environments towards the basin. Occasionally, synsedimentary slumping The La Charce section is located in the and turbidites (rust-coloured calcarenites) French department of Drôme (Fig. 1.1a). The occurred in the basin. These calcarenites are biostratigraphy of the section has been well- particularly well-exposed in portions of the studied. In the last four decades a considerable Campylotoxus and Verrucosum zones of the La number of works on palaeontology and Charce section (REBOULET, 1996, and references biostratigraphy have been published: on therein). ammonoids (THIEULOY, 1977a; REBOULET et alii, 1992; BULOT et alii, 1993, 1996; BULOT, 1995; Recent research (FESNEAU C., DECONINCK J.- REBOULET, 1996; REBOULET & ATROPS, 1997, F., PELLENARD P., GARCIA J.-P. & REBOULET S., 1999, and references therein), on belemnites in progress) on some outcrops in the Vocontian (JANSSEN & CLÉMENT, 2002), on trace fossils Basin (La Charce and Vergol sections in the (GAILLARD, 1984; GAILLARD & JAUTÉE, 1987; Drôme, Montclus in the Hautes-Alpes) has OLIVERO, 1996), on foraminifers (MOULLADE, revealed the occurrence of centimetre-thick 1966; MAGNIEZ-JANNIN, 1992; MAGNIEZ-JANNIN goethite-rich horizons. These horizons (reddish & DOMMERGUES, 1994), and on calcareous in colour), already mentioned by BEAUDOIN et nannofossils (THIERSTEIN, 1973; GARDIN, this alii (2003), resemble Oxfordian and Aptian volume). Sedimentological, geochemical and bentonites described in other sections of the palaeomagnetic data are also available Vocontian Basin (DAUPHIN, 2002; PELLENARD & (COTILLON et alii, 1980; FERRY et alii, 1989; DECONINCK, 2003). FERRY, 1991; HENNIG et alii, 1999; SCHOOT- BRUGGE et alii, 2003; GRÉSELLE, 2007, and Biostratigraphy of ammonoids references therein). Here, we present the lithological evolution of the La Charce section, The La Charce section is well dated because along with a synthesis of the biostratigraphic of the important number of ammonoids, which work on ammonoids. comprise almost all of the macrofauna (REBOULET et alii, 1992; ATROPS & REBOULET, Day 1 – Stop 1. Lithology of the La Charce 1995; REBOULET, 1996; REBOULET & ATROPS, section 1999, and references therein). But other nektonic macrofossils are present: belemnites A detailed lithology of the Valanginian- are common and there are a few nautiloids. Hauterivian portion of the La Charce section is Bivalves and gastropods are rare. presented in REBOULET (1996) and REBOULET & ATROPS (1999). So here we discuss only the More than 15,000 ammonoids were collected stratigraphy of the sequence encompassing the in a hundred metre section (REBOULET, 1996). boundary between the stages (Fig. 2.1). There The assemblage consists of six families. Most the lithology is characterized by marl-limestone turnovers took place during the evolution of the alternations. The section is intensively Neocomitidae and Olcostephanidae. The ammo- bioturbated, with both limestones and marls noid spectra are often dominated by: Haplo- affected (GAILLARD, 1984). Zoophycos feeding ceratidae, Bochianitidae, Phylloceratidae, and burrows are common in the limestones (OLI- Lytoceratidae; their abundance indicates a VERO, 1996). Carbonate-rich marl-limestone deep-water palaeoenvironment (REBOULET, alternations predominate the lowest Valanginian 1996). beds (Pertransiens ammonite Zone), then gradually become richer in argillaceous content An ammonoid turnover occurred at the in the uppermost part of the Lower Valanginian boundary of the Valanginian and Hauterivian, (Campylotoxus ammonite Zone). The Verru- and has been interpreted as the response of cosum ammonite Zone of the Upper Valanginian nektonic organisms to eustatic and climatic (Fig. 2.2a) is also the site of an increase in changes (REBOULET et alii, 1992; REBOULET & argillaceous content. The relative abundance of ATROPS, 1995; REBOULET, 1996). The biozo- carbonate in the marl-limestone succession nation reflects the evolution of the ammonoid increases gradually upward toward the fauna (REBOULET & ATROPS, 1999). The zonal Valanginian/Hauterivian boundary. The marls scheme of these authors has been adopted by and limestones of Early Hauterivian age show a the Lower Cretaceous Ammonite Working Group marked contrast: white limestones quite (= KILIAN Group) of the IUGS Subcommission regularly alternate with dark marls (Fig. 2.2b). on Cretaceous Stratigraphy and is included in Their thicknesses are comparable.

7 Carnets de Géologie / Notebooks on Geology - Book 2008/01 (CG2008_BOOK_01) the Cretaceous Standard Zonation (HOEDE- REBOULET & HOEDEMAEKER (reporters) et alii, MAEKER & REBOULET (reporters) et alii, 2003; 2006).

S Figure 2.1. Ranges of the ammonoids in and zonation of the La Charce section based on data from REBOULET et alii (1992), BULOT et alii (1993, 1996), BULOT (1995), REBOULET (1996), REBOULET & ATROPS (1997, 1999). This figure is the fruit of a collaboration with Luc BULOT. (a) Stages; (b) ammonoid zones; (c) bed numbers according to L. BULOT; (d) bed numbers according to S. REBOULET. The main nannofossil events recorded in the La Charce section are also shown (data from Silvia GARDIN, unpublished).

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A B

C

S Figure 2.2. La Charce section. (A) Picture showing Upper Valanginian marl-limestone alternations (Verrucosum ammonoid Zone). (B) Marl-limestone alternations at the base of the Hauterivian Stage. (C) Panorama of the La Charce section.

well-documented), during the Brussels meeting The Hauterivian stage and the Global in 1995 (MUTTERLOSE et alii, 1996), the Boundary Stratotype Sections and Points Hauterivian Working Group agreed to recom- mend the La Charce section as the global RENEVIER (1874) defined the Hauterivian stage in the Hauterive area (Neuchâtel, boundary stratotype for the base of the Northwest Switzerland). For a long time this Hauterivian. The IUGS-ICS Subcommission on locality has been considered to be unsa- Cretaceous Stratigraphy recommended the La Charce section for the Hauterivian GSSP during tisfactory as the stratotype due to the nd condensation of some parts of the section, its the 32 International Geological Congress at poor exposure and the scarcity of ammonoids. Florence in 2004 (RAWSON, 2004; OGG et alii, For most of the 20th century and thereafter 2004). The members of the Hauterivian Wor- king Group are currently preparing a formal KILIAN and other French authors have investigated the expanded sections of the proposal in accordance with this recommenda- Vocontian Basin, where rich ammonoid faunas tion. The village of La Charce has agreed to are recorded in the marl-limestone alternations preserve the section outcropping along the of the hemi-pelagic successions. road.

As regards the Valanginian/Hauterivian The Acanthodiscus radiatus Zone (Radiatus boundary, the La Charce section is the best Zone) and the Golden Spike of the Hauterivian documented. It was proposed by THIEULOY (1977a, p. 125) as a candidate for the The base of the Hauterivian in the Tethyan boundary stratotype. The IUGS retained this realm was traditionally defined by the first proposal during the Copenhagen meeting in appearance of the index-species Acanthodiscus 1983 (BIRKELUND et alii, 1984). Because no radiatus (THIEULOY, 1977a). This choice was other supplementary section has been proposed recommended during the 1st and 2nd interna- in Spain, the Caucasus or in the Crimea (all are tional symposia on the Cretaceous Stage Boun- areas in which the Valanginian-Hauterivian is

9 Carnets de Géologie / Notebooks on Geology - Book 2008/01 (CG2008_BOOK_01) daries (Copenhagen, 1983 and Brussels, 1995; Palaeoecology and palaeogeography of BIRKELUND et alii, 1984; MUTTERLOSE et alii, Acanthodiscus 1996). Due to the scarcity of the index-species in deep-water distal environments it was also In southeastern France, Acanthodiscus is suggested that the base of the Radiatus Zone common or even relatively abundant in be made concomitant with the first appearance hemipelagic palaeoenvironments (Vivarais/Cé- of the genus Acanthodiscus (A. radiatus and vennes area, BUSNARDO in ELMI et alii, 1989, related species). This proposal was reported in 1996; REBOULET, unpublished data) and in the Geologic Time Scale of OGG et alii (2004); shallow-water, proximal environments (Proven- further discussion can be found in KLEIN (1997) ce platform, THIEULOY et alii, 1990; AUTRAN, and REBOULET & ATROPS (1999). REBOULET 1993; BULOT, 1995; REBOULET, 1996; Jura (1996, p. 263 and figure 22) also supports this platform, BUSNARDO & THIEULOY, 1989). definition of the Radiatus Zone. This author Conversely, it is reported as rare in deeper- shows that the genus Acanthodiscus is probably water, distal palaeoenvironments (Vocontian a biological species with a great variability in Basin, REBOULET, 1996; Veveyse de Châtel macroconchs (A. radiatus, A. rebouli, A. vaceki, area, Switzerland, BUSNARDO et alii, 2003). A Leopoldia leopoldina), and in microconchs (Brei- similar distribution is observed in other Tethyan strofferella peyroulensis, B. castellanensis and and Atlantic basins (Betic Chains, Spain, B. varappensis; REBOULET, 1996). Therefore, COMPANY, 1987; HOEDEMAEKER, 1995; Atlantic when Acanthodiscus is very rare or absent in High Atlas, Morocco, ETTACHFINI, 1991). deep-water palaeoenvironments, the recogni- tion of the Radiatus Zone is possible using the In the Boreal realm, Acanthodiscus occurs species of Breistrofferella that are also generally mainly in the shallow-water facies of NW abundant on platforms. In addition, the faunal Germany, the Polish seaway and Crimea assemblage of the Radiatus Zone is well (KEMPER et alii, 1981). In North Germany, characterized by other genera, like Teschenites, Acanthodiscus, which is generally rare in the Eleniceras, Olcostephanus, Spitidiscus and Endemoceras beds (KEMPER, 1973; RAWSON, Oosterella (Fig. 2.1; REBOULET, 1996). 1973), seems to be restricted to the Noricum Zone (THIEULOY, 1977b; QUENSEL, 1988) in In accordance with these recommendations deep-water environments, but it is recorded in and considerations the Golden Spike of the the upper part of the Amblygonium Zone in Hauterivian stage (= the base of the Radiatus shallow-water settings (KEMPER et alii, 1981; Zone) is placed at layer 189 of the La Charce MUTTERLOSE et alii, 1996). The presence versus type-section (Fig. 2.1), which is the first occur- absence of Acanthodiscus in the upper part of rence of Acanthodiscus rebouli (REBOULET, the Amblygonium Zone in the Boreal Realm 1996). Bed 189 corresponds to bed 250 in the may be controlled in large part by palaeo- system of numbering proposed by BULOT et alii environmental factors (bathymetry and/or a (1993). proximal versus a distal location). The same pattern was observed in southeastern France The chronologic age of the base of the (MCARTHUR et alii, 2007, and references Hauterivian is either 123 Ma (+6/-2 Ma, ODIN, therein). 1994), 136.4 Ma (+/-2 Ma, OGG et alii, 2004), 124.1 Ma (+/-0.4 Ma, FIET et alii, 2006) or Despite the fact that the presence or 133.9 Ma (+/-2 Ma, MCARTHUR et alii, 2007). It absence of Acanthodiscus is in part controlled is practically coincident with the base of by palaeoenvironmental factors, this genus has subchron M10n (FERRY et alii, 1989; MCARTHUR a wide palaeobiogeographic distribution and et alii, 2007), or with chron M11n (OGG et alii, thus is a very good index for the base of the 2004). Hauterivian in Europe (KEMPER et alii, 1981; MCARTHUR et alii, 2007), North Africa (Morocco, Conventionally, the base of the Ambly- ETTACHFINI, 1991, 2004; WIPPICH, 2001; gonium Zone of the Boreal Realm is correlated ATROPS et alii, 2002), and Chili (MOURGUES, with the base of the Radiatus Zone (THIEULOY, 2007). For further information on the palaeo- 1973; RAWSON, 1983, 1993; MUTTERLOSE et alii, geographic distribution of Acanthodiscus, see 1996; JACQUIN et alii, 1998; OGG et alii, 2004). also the synonymies of type species of 87 86 Recent Sr/ Sr data suggest that the base of Acanthodiscus, Leopoldia, and Breistrofferella in the Amblygonium Zone may correlate with the KLEIN (2005). uppermost part of the Furcillata Zone (Upper Furcillata Subzone; MCARTHUR et alii, 2007). This correlation is in agreement with similar proposals by other authors (THIEULOY, 1977b;

KEMPER et alii, 1981; RAWSON, 1983; MUTTERLOSE et alii, 1996; figure 6 in RAWSON & X Figure 3.1. Distribution chart of nannofossil taxa HOEDEMAEKER (reporters) et alii, 1999). in the La Charce section across the Valanginian/Hau- terivian boundary.

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11 Carnets de Géologie / Notebooks on Geology - Book 2008/01 (CG2008_BOOK_01) Chapter 3. The nannofossil netic etching and/or overgrowths of calcite that succession of la Charce across can affect nannofloral assemblages (Fig. 3.2). the Valanginian-Hauterivian Analysis of the complete and expanded boundary Valanginian-Hauterivian sequence at La Charce Silvia GARDIN has allowed a sequence of local events to be evaluated in relation to the established Euro- Calcareous nannofossils around the pean sequence. Nannoconus bucheri and Valanginian/Hauterivian boundary Nannoconus wassalli occur sporadically starting at the Callidiscus ammonoid Zone; their Although there are several publications occurrence is always rare and spotty. These concerning Lower Cretaceous calcareous taxa are more abundant and from the Loryi nannofossils, the biostratigraphic resolution of ammonoid Zone upward are continuously recor- nannofossils across the Valanginian/Hauterivian ded. Tubodiscus verenae and Tubodiscus jura- boundary has increased little. In the published pelagicus occur sporadically up to the end of literature few datums are proposed to delineate the Late Hauterivian (Ligatus ammonoid Zone). the Valanginian/Hauterivian boundary. SIS- Staurolithithes mitcheneri was first seen in bed SINGH (1977) suggested using the FO (first 251 of BULOT et alii (1993; Radiatus ammonoid occurrence) of Cretarhabdus loriei as a marker Zone, Castellanensis Horizon). The LO of for the Early Hauterivian, though this particular Eiffellithus windii is in bed 270, and the FO of occurrence proved to be much younger Diloma galiciense in bed 272 (Radiatus (Aptian). PERCH-NIELSEN (1979, 1985) acknow- ammonoid Zone, Buxtorfi Horizon; Fig. 2.1). ledged the difficulty of using Cretarhabdus loriei These two species are rare but their strati- due to problems in recognizing or differentiating graphical ranges are reasonably consistent. this species from other species of Cretarhabdus. ROTH (1978, 1983) and THIERSTEIN (1976) The first Litraphidites bollii was observed in proposed the LOs (last occurrences) of bed 292 (Loryi /Jeannoti ammonoid Zone) but Diadorhombus rectus and Tubodiscus verenae its occurrence is common only upward from bed to mark the top of the Valanginian; however, 296 in the Nodosoplicatum/Variegatus ammo- these species have much younger extinctions. noid Zone (Fig. 3.1). The last occurrence of Rhagodiscus dekaeneli is at the top of this zone In terms of nannofossil biozones, the ("non-nome" subzone). All these events are Valanginian/Hauterivian boundary (as defined summarized in Figure 3.1. The value as by ammonoid fauna) falls within Biozone CC4a markers in other geographical areas must be of APPLEGATE & BERGEN (1989) who modified carefully evaluated. No important originations the standard zonation of SISSINGH (1977). This or extinctions are coincident with the boundary zone is defined by the FAD (first appearance (Callidiscus / Radiatus ammonoid Zones). At La datum) of Eiffellithus striatus and the FAD of Charce, the nannofossil event that best Litraphidites bollii. Biozone CC4 also approximates the Valanginian/Hauterivian corresponds to the NC4a Zone of ROTH (1978), boundary is the LO of Eiffellithus windii. as modified by BRALOWER et alii (1995). It is noteworthy that the last common occurrence of Calcareous nannofloras at La Charce have a Tubodiscus verenae corresponds approximately predominantly low-latitude (Tethyan) affinity with the FO of Eiffellithus striatus in the Late (common Cruciellipsis cuvillieri, Speetonia Valanginian. colligata and Calcicalathina oblongata) though Nannoconids, which are known to prefer low- Nannofossil biostratigraphy of the La latitude, warm surface waters, and hemipelagic Charce section settings (THIERSTEIN, 1976; MUTTERLOSE, 1992; ERBA, 1994; KRUSE & MUTTERLOSE, 2000) are Splits from the marly intervals were very rare. Taxa more commonly associated with processed using standard preparation higher latitudes such as Sollasites spp., techniques and were examined under a light Crucibiscutum salebrosum, Corollithion silva- microscope. All these samples were productive, radion, are consistently present at La Charce with abundant calcareous nannofossil assem- although in much lower quantities than in blages (Fig. 3.1); the number of species is boreal sites. This is due to the northern Tethyan usually high (about 80 species), preservation is location of the Vocontian Basin, which acted as moderate. Identification of specimens with the a "gateway" to boreal domain of northwestern light microscope was not hampered by diage- Europe.

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S Figure 3.2. Micrographs showing some nannofossil taxa recorded in the La Charce section. Scale bar is 5 µm. 1. Eiffellithus windii, sample LCH 251; 2-3. Eiffellithus striatus, LCH 255. Same specimen rotated; 4. Cruciellipsis cuvillierii, LCH 255; 5-6. Staurolithites mitcheneri, LCH 255. Same specimen rotated; 7. Tubodiscus verenae, LCH 272; 8. Rhagodiscus asper, LCH 270; 9. Nannoconus bucheri, LCH 260; 10. Nannoconus cornuta, LCH 260; 11. Nannoconus circularis, LCH 266; 12. Tribrachiatus sp., LCH 251; 13. Diloma galiciense, LCH 278; 14. Corollithion silvaradion, LCH 272; 15. Staurolithites sp., LCH 272; 16. Calcicalathina oblongata, LCH 272.

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S Figure 4.1. Picture showing the BREISTROFFER interval in the Blieux section.

S Figure 4.2. Total abundance (specimens per view), diversity, and percentage of selected calcareous nannofossil taxa across the BREISTROFFER interval of the Blieux section (after GIRAUD et alii, 2003). The colour variations from pale-grey to dark-grey reflect change from oligotrophic to mesotrophic conditions.

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Chapter 4. The OAE 1d (Oceanic (BRÉHÉRET, 1995-1997). Anoxic Event, latest Albian) Calcareous nannofossils are well preserved Fabienne GIRAUD and are predominantly heterococcoliths, but holococcoliths are also present. The range in Day 1 – Stop 2. The BREISTROFFER interval in the number of species fluctuates from 32 to 50 the Vocontian Basin: the OAE. per sample. As pelagic carbonate production is The Aptian-Albian interval of the Vocontian limited, the carbonate fraction is derived mainly Basin is represented by the Marnes Bleues from the tests of nektonic/benthic organisms, Formation. It is about 800 metres of rather but in part may be allochthonous (export to the homogeneous dark-blue marls and shales with basin from adjacent carbonate-platforms). a grayish cast. In southeastern France the OAE There is little organic carbon in the BREI- 1d level is called the BREISTROFFER interval STROFFER interval, and it is not associated with (BRÉHÉRET, 1988). Nine laminated horizons high productivity in surface waters. Organic containing 1 to 2% wt%TOC (Total Organic matter is mainly terrigenous in origin and its Carbon) have been identified in the central part presence is due to: 1) dysoxic conditions that of the Vocontian Basin, NW of Sisteron preserved it and 2) a weak input of (BRÉHÉRET, 1988; Fig. 1.2). allochthonous carbonates. Eustatic fluctuations strongly influenced the changes in nannofossil Palaeoenvironmental conditions across the and macrofaunal abundances. In the BREI- STROFFER interval there are also distinctive BREISTROFFER interval patterns in nannofossil assemblages and macro- Near Blieux (Alpes de Haute-Provence) near faunal abundance (Figs. 4.2 and 4.3) that the southern margin of the Vocontian Basin reflect changes in trophic levels. Low diversity (GIRAUD et alii, 2003; REBOULET et alii, 2005; in nannoplankton assemblages and very Fig. 1.2) in the 38 metre succession of dark abundant macrofaunas suggest that meso- colored marls intercalated with centimetric-thick trophic conditions prevailed in the lower part of lighter grey marls (Figs. 4.1 and 4.2) there are the interval (Fig. 4.3a). In the upper part there changes upward in the abundance of calcareous is a greater diversity in nannofossil assem- nannofossils and in the composition of their blages, more abundant ammonoids and a lesser assemblages, along with varying proportions of amount of benthic macrofauna (Fig. 4.3b). This macrofossils, assemblages of ichnofossils and in divergence might be the result of climatic the degree of bioturbation. Palaeogeographi- changes associated with periods of increased cally this section is in a key position to record precipitation and runoff during the deposition to palaeoenvironmental changes involving both the lower part of the BREISTROFFER interval, and proximal areas (platform environments) and the to a period of drier conditions in the upper part pelagic realm (open marine), and is rich in of this interval. The work of GIRAUD et alii nektonic/benthic macrofauna. Because of the (2003) and REBOULET et alii (2005) shows that relatively proximal position of the Blieux the BREISTROFFER deposits did not indicate an section, the BREISTROFFER interval is devoid of eutrophication of marine surface waters that the typical laminated black-shale horizons in occurs with the expansion of an oxygen- the central part of the Vocontian Basin minimum zone.

W Figure 4.3. Sket- ches showing the pre- sence/absence of some Late Albian ammonoids, their varying abundance and their position in the water column in relation to trophic conditions during the BREI- STROFFER interval of the Blieux section (after GIRAUD et alii, 2003). (A) Lower part of the BREISTROFFER interval: mesotrophic conditions in surface waters and episodic density stratifi- cation of the water column; (B) Upper part of the BREISTROFFER interval: oligotrophic conditions in surface waters and more stable paleoenvironment.

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A high-resolution quanti- tative analysis of the several microfossil groups and of the bulk-rock stable isotope data was made on the black shalesof the main BREI- STROFFER interval in the central part of the Vocontian Basin (Col de Palluel section, IGN map French Série Bleue 1:25,000 Rosans number 3239 Ouest, Lambert III Zone coordinates 853.750; 3238.425, Fig. 1.1) by BORNEMANN et alii (2005). This work quantified the absolute abundance of calca- reous nannofossils (Fig. 4.4), using the settling method of GEISEN et alii (1999). Nannofossils are well-to- moderately preserved at Col de Palluel. Like the work of GIRAUD et alii (2003), this study suggests that the accumulation of organic matter was controlled by preservation rather than by an increase in its productivity in the photic zone. Paleo- climatic and oceanographic changes caused by moon- soonal activity were identified. In the BREISTROF- FER interval, the black shales were laid down by surface waters in a warm and humid climate under oligotrophic conditions while marlstones were deposited under relati- vely cool and arid conditions that favored increased productivity of carbonates.

X Figure 4.4. Location of the Col de Palluel section. Columns show the lithology of the succession and the absolute abundance of calcareous nanno- fossils in the Col de Palluel section (modified after BORNE- MANN et alii, 2005).

16 Carnets de Géologie / Notebooks on Geology - Book 2008/01 (CG2008_BOOK_01) Chapter 5. The GSSP (Global section exposes a continuously accessible boundary Stratotype Section and succession of nearly 250 m, from the BREISTROFFER interval in the upper part of the Point) for the base of the Marnes Bleues Formation to Lower Cenomanian Cenomanian stage (KENNEDY et marly limestones and marls, with no evidence alii, 2004) of sedimentary breaks or condensation (GALE et alii, 1996, Fig. 5.1). Ammonites, planktonic Fabienne GIRAUD foraminifera, and calcareous nannofossils are Day 1 – Stop 3. The Mont Risou section abundant throughout the succession and allow accurate biostratigraphy (Fig. 5.1). The base of The GSSP for the base of the Cenomanian is the Cenomanian stage lies 36 m below the top the Mont Risou section, Hautes-Alpes (IGN map of the Marnes Bleues Formation and is chosen French Série Bleue 1:25,000 Rosans number at the first occurrence of the planktonic 3239 Ouest, Lambert II Zone coordinates foraminifer Rotalipora globotruncanoides. 852.725; 1937.625, Figs. 1.1 and 4.4). This Preservation of calcareous nannofossils is moderate throughout the sequence and the nannofloral assemblages are highly diverse (153 taxa). Biscutum ellipticum, Rhago- discus achlyostaurion, Tranol- ithus orionatus, Watznaueria barnesiae and Watznaueria manivitiae are common to abundant. Holococcoliths are unusually common and sometimes well-preserved in particular levels (LEES in GALE et alii, 1996).

The carbon-isotope curve has a large peak made up of four distinct spikes (A to D, Fig. 5.1). Temperatures of sea-surface water deduced from the oxygen isotope data are comprised between 26 and 27°C. A slight cooling of about 1°C distinguishes the earliest Cenomanian (GALE et alii, 1996, Fig. 5.1).

S Figure 5.1. See Figure 4.4 for the location of the Global Stratotype Section and Point of Mont Risou. Integrated litho-, biostratigraphy and stable isotopic data across the Albian-Cenomanian boundary at Mt Risou (modified after KENNEDY et alii, 2004). Nannofossil data are from J.A. LEES.

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Chapter 6. The Cenozoic of the A brief summary of the functioning of Barrême syncline foreland basins

Bernard PITTET Foreland basins are intrinsically related to Today we will analyse the sedimentary continent-to-continent collision and the evolution of the Cenozoic in the Barrême formation of Alpine-type mountain chains. They region. This area is in the second of the are narrow, elongated basinal troughs located foreland basins formed to the west of the Alps at the periphery of a mountain chain during its during the collision Adria-Europe. The first formation. They receive the products of the foreland basin formed during Late Cretaceous erosion of the rising chain, and are thus filled times in conjunction with the Pyrénées- mainly by siliciclastic material. They record the Provençal tectonic phase (e.g., deposition of the major tectonic events that occur during a "Flysh à Helminthoïdes", Campanian-Maas- continent-to-continent collision. trichtian). The second foreland basin developed in Late Eocene-Early Oligocene (Nummulitic Basically, mountain chains forming during Sea) during the second Alpine tectonic phase, such a collision can be regarded as a large and the third was present during the Miocene in accretion prism of continental crust. During connection with the late Alpine tectonic phase. intensive tectonic activity in the chain, accretion is responsible for a thickening of the crust (e.g., ~50 km for the Alps, ~70 km for the Himalaya) of the lithosphere. In isostatic response to this thickening, the mountain chain subsides (Fig. 6.1a). Consequently, along the periphery of the mountain chain subsidence is also important, and creates on both sides of the chain a foreland basin in which continental or marine sedi- ments are deposited and preserved. In response to the overcharge of the mountain chain, the continental crust (and lithosphere) forms a bulge some few hundred kms away from the chain (Fig. 6.1a). This rise accounts for the fact that foreland basins are asymmetrical and narrow.

Because it can be seen as an accretional prism of conti- nental crust, the mountain chain in formation will not only thicken but also enlarge laterally, thus causing the foreland basin to migrate away from the zone of accretion at the outer limit of the mountain chain (Fig. 6.1b). Consequently, the oldest sediments deposited in a foreland basin are the closest to the chain and can, as the basin migrates, become involved in the accretion prism. The youn-

gest sediments are deposited S Figure 6.1. Diagrams showing the relationships between Alpine far from the chain, and mountain-building and the development of foreland basins (see the text for a more detailed explanation). generally are not deformed.

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S Figure 6.2. Lithostratigraphy and facies of the stratigraphic entities encountered in the Barrême syncline. The major unconformities are also shown. An interpretation of the evolution of the different environmental conditions is shown as well as the polarity of the several sedimentary systems. of different ages (Early to Late Cretaceous). The The Barrême region was very close to the first sediments attributed to the Cenozoic are developing Alpine chain. Consequently, this continental alluvial deposits that develop from area records both foreland dynamics (the south to north (Argens Conglomerates; Fig. accommodation space created by subsidence 6.2) and are present only locally, thus due to thickening of the Alps during intense suggesting that river drainage was already tectonic pulses) and Alpine dynamics (folding of controlled by pre-existing N-S folds. On these the sediments deposited in the foreland basin alluvial facies (when present), or directly on whenever accommodation space was available). folded Mesozoic rocks is the Nummulitic These two mechanisms (subsidence and fol- Limestone (Fig. 6.2), which consists of shallow- ding) underpin the Cenozoic geological history marine bioclastic sediments (nummulites, of the Barrême region. bivalves – mainly oysters) but can locally contain fluvial conglomerates deposited in the Summary of the sedimentary evolution in shallow Nummulitic Sea. As transgression the Barrême syncline continued deeper-water marls accumulated in the Nummulitic Sea, forming two sub-units, the The Barrême syncline, oriented N-S, exposes Lower and the Upper Nummulitic Marls, the Upper Eocene-Oligocene sediments separated by the Ville Sandstones that are deposited in the inner part of the Nummulitic- turbiditic lobe deposits. Sedimentary structures Molasse foreland basin, directly on previously (flute casts, prod casts, current ripples) in the folded and eroded Mesozoic "deep-water" turbidites of the Ville Sandstones indicate a sediments (Figs. 1.1 and 1.2). Consequently, south to north direction for the turbidity the marine transgression of the Nummulitic Sea currents, thus implying a southern source of the in the Late Eocene invaded complex paleoreliefs siliciclastic material (Corsica-Sardinia block).

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The Nummulitic deposits, both limestone and marls, were folded in some localities before the deposition of the Clumanc Conglomerates (Fig. 6.2). These conglomerates contain Alpine- derived gravels. They demonstrate that the centre of the Alps (oceanic crust and deep- ocean sediments, i.e. serpentinites and radiolarites) was already exposed some 32 Ma ago. Here at Clumanc the conglomerates are remarkable because they are formed by successive flows of phreato-magmatic debris that followed the river system to be deposited at the mouth of a delta on the shore of the Nummulitic Sea. The genesis of phreato- magmatic flows is demonstrated by their andesitic matrix and the presence of andesite gravels. A rapid forceful discharge of material is evinced by the presence of thick (30–80 cm) layers containing mud boulders that testify to a mass-flow origin for these deposits.

In the Clumanc area, the Nummulic Sea includes a succession of 3 phreato-magmatic episodes that alternate with "normal" num- mulitic marls to fill this part of the basin. The Barrême syncline (still in formation) then served as a river valley. This river formed a new delta in St-Lions, some 7 km south of Clumanc. The progradation of the delta from Clumanc to St-Lions attests that the river flowed from north to south at that time.

The Red Molasse that overlies the Clumanc and St-Lions conglomerates is slightly discor- dant, suggesting that tectonic movements occurred after deposition of the Clumanc/St- Lyons conglomerates ended, and before (or at the beginning of) the deposition of the Red Molasse. Alluvial fan deposits comprise this new sedimentary unit. In the Barrême syncline, the Red Molasse is dominantly argillaceous (alluvial plain red-clays) interrupted by small channels, which are infilled by conglomerates. The conglomerates are for the most part of local origin (Mesozoic carbonates from the flanks of the Barrême syncline). Southwards, in the Senez region (some 6 km farther from Barrême; Fig. 1.2), the Red Molasse is dominantly conglomeratic, and clays are much rarer. This implies that the alluvial fan developed from south to north.

Above the Red Molasse and concordant with it is the Grey Molasse. Its deposits are mainly argillaceous (whitish to light-greenish alluvial plain sediments), with a few sandstone levels and common palustrine-lacustrine limestones. S Figure 6.3. Topographic map of the Barrême The evolution from the Red to the Grey Molasse syncline [Some rights reserved]. is thought to reflect a flattening of the relief in the back-land due to increased subsidence. The change in colour from one formation to the other probably has a climatic origin.

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Outcrops visited fine-grained bioclasts, with abundant oyster fragments and locally with nummulites. The Day 2 - Stop 1. Les Sauzeries Basses Lower Nummulitic Marls deposited above the section limestones have a thickness of 80m to about 100m. The Ville Sandstones are a succession of This section, along the road from Les fine-grained turbiditic lobes. The turbidites Sauzeries Basses to La Poste (1 km to the typically have plane-parallel laminations with south-east; Fig. 6.3), exposes a continuous few occurrences of current ripples. An erosional sedimentary succession, approximately 150- contact at the base of the turbidites is common. 200 m thick that occupies the interval between Looking south from the road, three units of the the Nummulitic Limestone and the Clumanc Clumanc Conglomerates can be seen, as Conglomerates. The Nummulitic Limestone in intercalations into the Upper Nummulitic Marls. this area was deposited in unconformity on the To the southeast, below the Clumanc castle Blue Marls (Fig. 6.4a), which are earliest Albian (Stop 2), these 3 units are amalgamated. A in age to the north and latest Late Aptian to the geometry of the deltaic system of the Clumanc south. Two plurimetric limestone beds Conglomerates can be reconstructed by separated by nummulitic marls represent the geological mapping. Nummulitic Limestone here. The limestones are

S Figure 6.4. (A) Picture showing the unconformity between the Albian Blue Marls and the deposits of the Nummulitic Sea at Les Sauzeries Basses. The Ville sandstones are visible at the top of the hill. (B) Picture illustrating the complex geometrical relationships between the Clumanc Conglomerates and the Nummulitic Limestone and Marls at the Clumanc Castle. Day 2 – Stop 2. Clumanc castle Day 2 – Stop 3. The Red Molasse along the road D19 at mid-distance from St-Lions A perpective of the hill on which the and St-Jacques Clumanc castle was constructed will be exami- ned at this stop (Fig. 6.4b). The three A short stop here is devoted to the alluvial amalgamated units of the Clumanc Conglo- fan facies of the Red Molasse. An outcrop along merates constitute the hilltop. They rest uncon- road D19 epitomizes the typical characteristics formably on the previously folded synclinal of alluvial fans: 1) ephemeral conglomeratic Nummulic Limestone and Marls. Finally, both channels filled by local material; 2) sheet flood the Nummulitic Limestone and Marls and the deposits that coarsen upward, thickening- Clumanc Conglomerates were again folded to upward silt-to-sand sediments; and 3) flooding form an anticline. This sequence of events is a clays deposited at considerable distances from good illustration of the tectonic activity in the the channels during the partial or entire Alps as it was recorded in the Barrême syncline, flooding of the fan. In this outcrop the for the sequence described is repeated predominance of clays indicates that this area generally: 1) subsidence creates a depressed was in a distal position on the alluvial fan. space to accommodate marine or continental sediments; 2) these sediments are folded; 3) a new phase of accommodation is created by subsidence, and more sediments are deposited; 4) folding, etc. … Note that both folding and the creation of accommodation can occur at the same time.

21 Carnets de Géologie / Notebooks on Geology - Book 2008/01 (CG2008_BOOK_01) Acknowledgments 2003).- Société Géologique de France, Paris, p. 8-9. The authors wish to warmly thank Bruno BIRKELUND T., HANCOCK J.M., HART M.B., AWSON EMANE OBASZYNSKI GRANIER for his precious help in editing this R P.F., R J., R F., guidebook and for his useful advices. Special SCHMID F. & SURLYK F. (1984).- Cretaceous thanks are due Nestor SANDER for language stage boundaries – proposals.- Bulletin of corrections and improved readability of the the Geological Society of Denmark, Copen- text. hagen, vol. 33, p. 3-20. BORNEMANN A., PROSS J., REICHELT K., HERRLE Bibliographic references J.O., HEMLEBEN C. & MUTTERLOSE J. (2005).- Reconstruction of short-term palaeocea- APPLEGATE J.L. & BERGEN J.A. (1989).- 20. nographic changes during the formation of Cretaceous calcareous nannofossil biostrati- the Late Albian 'Niveau BREISTROFFER' black graphy of sediments recovered from the Ga- shales (Oceanic Anoxic Event 1d, SE licia margin, ODP Leg 103.- In: BOILLOT G., France).- Journal of the Geological Society, WINTERER E.L. & MEYER A.W. (eds.), Galicia London, vol. 162, p. 101-114. Margin, Sites 637-641.- Proceedings of the BRALOWER T.J., LECKIE R.M., SLITER W.V. & Ocean Drilling Project, Scientific Results, THIERSTIEN H.R. (1995).- An integrated College Station, vol. 103, p. 293-348. Cretaceous microfossil biostratigraphy. In: ARNAUD H. & LEMOINE M. (1993).- Structure BERGGREN W.A., KENT D.V., AUBRY M.-P. & and Mesozoic-Cenozoic evolution of the HARDENBOL J. (eds.), Geochronology, time South-East France Basin (SFB).- Géologie scales, and global stratigraphic correlation.- Alpine, Grenoble, (série spéciale "Colloques Society of Economic Paleontologists and et Excursions"), n° 3, p. 53-58. Mineralogists (SEPM) Special Publication, ATROPS F. (1984).- 2.7. Chaînes subalpines Tulsa, n° 54, p. 65-79. (Jurassique supérieur : Malm). In: DEBRAND- BREHERET J.G. (1988).- Épisodes de sédi- PASSARD D.S. (ed.), Synthèse géologique du mentation riche en matière organique dans Sud-Est de la France.- Mémoire du Bureau les Marnes Bleues d'âge aptien et albien de des Recherches Géologiques et Minières, la partie pélagique du bassin vocontien.- Orléans, n° 125, vol. 1 (Stratigraphie et Bulletin de la Société Géologique de France, paléogéographie), p. 255-257. Paris, (Série 8), t. IV, n° 2, p. 349-356. ATROPS F., AOUTEM M., LHAMYANI B. & MASROUR BRÉHÉRET J.G. (1995).- L'Aptien et l'Albien de la M. (2002).- Biostratigraphie par ammonites, Fosse vocontienne (des bordures au bassin). au passage Valanginien-Hauterivien, dans le Évolution de la sédimentation et ensei- Haut Atlas occidental (région d'Agadir, gnements sur les événements anoxiques.- Maroc). In: GAILLARD C. & HANTZPERGUE P. Thèse Doctorat de l'Université François (eds.), Strati 2002 : 3ème congrès français Rabelais, Tours, 564 p.; Publication de la de stratigraphie, Lyon (8-10 juillet 2002).- Société Géologique du Nord, Lille, t. 25 Documents des Laboratoires de Géologie de (1997), 614 p. Lyon, p. 22. BULOT L.G. (1995).- Les formations à ammo- ATROPS F. & REBOULET S. (1995).- Le nites du Crétacé inférieur dans le Sud-Est de Valanginien-Hauterivien basal du bassin la France (Berriasien à Hauterivien): biostra- vocontien et de la bordure provençale: tigraphie, paléontologie et cycles sédimen- zonation et corrélations.- Comptes Rendus taires.- Unpublished Ph.D. thesis, Muséum de l'Académie des Sciences, Paris, t. 320, National d'Histoire Naturelle, Paris, 398 p. (série II), n° 10, p. 985-992. BULOT L.G., THIEULOY J.-P., ARNAUD H. & AUTRAN G. (1993).- L'évolution de la marge DELANOY G. (1996).- The Lower Cretaceous Nord-Est provençale (Arc de Castellane) du of the South Vocontian Basin and margins.- Valanginien moyen à l'Hauterivien à travers Géologie Alpine, Grenoble, (Mémoire H.S.), l'analyse biostratigraphique des séries de la t. 20, p. 383-399. région de Peyroules: séries condensées, BULOT L.G., THIEULOY J.-P., BLANC É. & KLEIN J. discontinuités et indices d'une tectogenèse (1993).- Le cadre stratigraphique du distensive. Paléobiologie.- Annales du Valanginien supérieur et de l'Hauterivien du Muséum d'Histoire Naturelle de Nice, t. X, Sud-Est de la France: définition des biochro- 240 p. nozones et caractérisation de nouveaux BEAUDOIN B., AGASSANT J., ANDRÉ M., ATROPS biohorizons.- Géologie Alpine, Grenoble, t. F., BAHAMIAN O., BULOT L., DELATTRE M., 68, p. 13-56. DAUPHIN L., ECKERT S., FRIÈS G., GUYARD F., BUSNARDO R., CHAROLLAIS J., WEIDMANN M. & JACQUEMIN O., LALANDE M., MARCOMBES D., CLAVEL B. (2003).- Le Crétacé inférieur de la MAZINGUE V., PARIZE O., PASQUIER C., Veveyse de Châtel (Ultrahelvétique des PINAULT M., REBOULET S., ROSENZWEIG F., Préalpes externes; canton de Fribourg, ROUGER G., SANDAMIANI A., SPINDLER P., Suisse).- Revue de Paléobiologie, Genève, SZYMKOWSKI B. & VERET G. (2003).- Les vol. 22, n° 1, p. 1-174. bentonites du Crétacé inférieur du SE de la BUSNARDO R. & THIEULOY J.-P. (1989).- Les France. In: Bassins crétacés de France et ammonites de l'Hauterivien jurassien: d'Europe occidentale, Paris (6-7 Novembre révision des faunes de la région du

22 Carnets de Géologie / Notebooks on Geology - Book 2008/01 (CG2008_BOOK_01)

stratotype historique de l'étage hauterivien.- Vocontian Trough.- Publication de l'Asso- Mémoire de la Société neuchâteloise de ciation des Sédimentologistes français, vol. Sciences naturelles, vol. 11, p. 101-147. 12, p. 121-140. COMPANY M. (1987).- Los ammonites del Valan- FERRY S. (1991).- Une alternative au modèle de ginense del sector oriental de las Cordilleras stratigraphie séquentielle d'Exxon : la modu- Béticas (SE de España).- Tesis Doctoral de la lation tectono-climatique des cycles orbi- Universidad de Granada, 294 p. taux.- Géologie Alpine, Grenoble, (Mémoire COTILLON P., FERRY S., GAILLARD C., JAUTEE E., H.S.), t. 18, p. 47-99. LATREILLE G. & RIO M. (1980).- Fluctuation FERRY S. & MANGOLD C. (1995).- Faciès de des paramètres du milieu marin dans le dépôt et stratigraphie séquentielle des domaine vocontien (France Sud-Est) au calcaires bajociens du Jura méridional.- Crétacé inférieur: mise en évidence par Documents des Laboratoires de Géologie de l'étude des formations marno-calcaires alter- Lyon, n° 133, 96 p. nantes.- Bulletin de la Société Géologique de FERRY S., POCACHARD J., RUBINO J.L. & GAUTIER France, Paris, (Série 7), t. XXII, n° 5, p. F. (1989).- Inversions magnétiques et cycles 735-744. sédimentaires: un premier résultat dans le DAUPHIN L. (2002).- Litho-, bio- et chrono- Crétacé de la fosse vocontienne (Sud-Est de stratigraphie comparées dans le Bassin la France).- Comptes Rendus de l'Académie Vocontien, à l'Aptien.- Unpublished Ph.D. des Sciences, Paris, t. 308, (série II), n° 2, thesis, Université des Sciences et Techniques p. 773-780. Lille 1, Lille, 516 p. FIET N., QUIDELLEUR X., Parize O., BULOT L.G. & ELMI S. (1984).- 2.8 Causses -Bordure vivaro- GILLOT P.Y. (2006).- Lower Cretaceous stage cévénole s.l. (Jurassique moyen : Dogger). durations combining radiometric data and In: DEBRAND-PASSARD D.S. (ed.), Synthèse orbital chronology: Towards a more stable géologique du Sud-Est de la France.- relative time scale?- Earth and Planetary Mémoire du Bureau des Recherches Science Letters, Amsterdam, vol. 246, n° 3- Géologiques et Minières, Orléans, n° 125, 4, p. 407-417. vol. 1 (Stratigraphie et paléogéographie), p. GAILLARD C. (1984).- Bioturbation des 205-211. sédiments pélagiques du Crétacé inférieur ELMI S., BROUDER P., BERGER G., GRAS H., dans le bassin vocontien (Chaînes subalpines BUSNARDO R., BEDARD P.& VAUTRELLE C. méridionales, France).- Geobios, (Mémoire (1989).- Notice explicative, Carte Géolo- spécial), n° 8, p. 205-214. gique de France 1/50000, feuille Bessèges GAILLARD C. & JAUTÉE E. (1987).- The use of (888).- BRGM, Orléans, 115 p. burrows to detect compaction and sliding in ELMI S., BUSNARDO R., CLAVEL B., CAMUS G., fine-grained sediments: an example from KIEFFER G., BERARD P.& MICHAËLY B. the Cretaceous of SE France.- Sedimen- (1996).- Notice explicative, Carte Géolo- tology, Oxford, vol. 34, n° 4, p. 585-593. gique France 1/50000, feuille Aubenas GALE A.S., KENNEDY W.J., BURNETT J.A, CARON (865).- BRGM, Orléans, 170 p. M. & KIDD B.E. (1996).- The Late Albian to ERBA E. (1990).- Calcareous nannofossil Early Cenomanian succession at Mont Risou biostratigraphy of some Bajocian sections near Rosans (Drôme, SE France): an from the Digne area (SE France).- Memorie integrated study (ammonites, inoceramids, Descrittive della Carta Geologica d'Italia, planktonic foraminifera, nannofossils, Roma, vol. XL, p. 237-255. oxygen and carbon isotopes).- Cretaceous ERBA E. (1994).- Nannofossils and super- Research, London, vol. 17, n° 5, p. 515-606. plumes: the Early Aptian "nannoconid GEISEN M., BILLARD C., BROERSE A.T.C., CROS crisis".- Paleoceanography, Washington, vol. L., PROBERT I. & YOUNG J.R. (2002).- Life- 9, n° 3, p. 483-501. cycle associations involving pairs of holo- ERBA E. (2006).- The first 150 million years coccolithophorid species: intraspecific history of calcareous nannoplankton: Bio- variation or cryptic speciation?- European sphere-geosphere interactions.- Palaeogeo- Journal of Phycology, London, vol. 37, n° 4, graphy, Palaeoclimatology, Palaeoecology, p. 531-550. Amsterdam, vol. 232, n° 2-4, p. 237-250. GEISEN M., BOLLMANN J., HERRLE J.O., MUT- ETTACHFINI M. (1991).- Le Valanginien de l'Atlas TERLOSE J. & YOUNG J.R. (1999).- Calibration atlantique (Maroc) : stratigraphie et ammo- of the random settling technique for nitofaune.- Unpublished Ph.D. thesis, calculation of absolute abundances of Université Cadi Ayyad, Faculté des Sciences, calcareous nannoplankton.- Micropaleon- Marrakech, 153 p. tology, New York, vol. 45, n° 4, p. 437-442. ETTACHFINI M. (2004).- Les ammonites néoco- GIRAUD F. (1995).- Recherche des périodicités miennes dans l'Atlas atlantique (Maroc). astronomiques et des fluctuations du niveau Biostratigraphie, paléontologie, paléobiogéo- marin à partir de l'étude du signal carbonaté graphie et paléoécologie.- Strata, Toulouse, des séries pélagiques alternantes. Applica- vol. 43, (série 2 : mémoires), 223 p. tion au crétacé inférieur du Sud Est de la FERRY S. (1990).- Post-field comments. Meso- France (bassin vocontien), de l'Atlantique zoic eustacy record on western Tethyan central (Site 534 DSDP) et du golfe du Mexi- margins. Post-meeting field-trip in the que (Site 535 DSDP).- Documents des Labo-

23 Carnets de Géologie / Notebooks on Geology - Book 2008/01 (CG2008_BOOK_01)

ratoires de Géologie de Lyon, n° 134, 279 p. p. 509-522. GIRAUD F., OLIVERO D., BAUDIN F., REBOULET JAUTÉE E. (1984).- Écailles de l'Arc de S., PITTET B. & PROUX O. (2003).- Minor Castellane (Jurassique inférieur : Lias). In: changes in surface water fertility across the DEBRAND-PASSARD D.S. (ed.), Synthèse oceanic anoxic event 1d (latest Albian, SE géologique du Sud-Est de la France.- France) evidenced by calcareous nanno- Mémoire du Bureau des Recherches Géolo- fossils.- International Journal of Earth Scien- giques et Minières, Orléans, n° 125, vol. 1 ces (Geologische Rundschau), Stuttgart, vol. (Stratigraphie et paléogéographie), p. 157- 92, n° 2, p. 267-284. 158. GIRAUD F., PITTET B., MATTIOLI E., & AUDOIN V. KEMPER E. (1973).- The Valanginian and (2006).- Paleoenvironmental controls on the Hauterivian stages in northwest Germany.- morphology and abundance of the coccolith In: CASEY R. & RAWSON P.F. (eds.), The Watznaueria britannica (Late Jurassic, Boreal Lower Cretaceous.- Geological southern Germany).- Marine Micropaleon- Journal, Liverpool, special issue, n° 5, p. tology, Amsterdam, vol. 60, n° 3, p. 205- 327-344. 225. KEMPER E., RAWSON P.F. & THIEULOY J.-P. GRÉSELLE B. (2007).- Impact des variations (1981).- Ammonites of Tethyan ancestry in paléoclimatiques sur la sédimentation the early Lower Cretaceous of north-west carbonatée au Valanginien.- Unpublished Europe.- Palaeontology, vol. 24, p. 251-311. Ph.D. thesis, Université de Lyon, 154 p. KENNEDY W.J., GALE A.S., LEES J.A. & CARON M. HALLAM A. (2001).- A review of the broad (2004).- The Global Boundary Stratotype pattern of Jurassic sea-level changes and Section and Point (GSSP) for the base of the their possible causes in the light of current Cenomanian Stage, Mont Risou, Hautes- knowledge.- Palaeogeography, Palaeocli- Alpes, France.- Episodes, Beijing, vol. 27, n° matology, Palaeoecology, Amsterdam, vol. 1, p. 21-32. 167, n° 1-2, p. 23–37. KLEIN J. (1997).- Ammonite stratigraphy for the HENNIG S., WEISSERT H. & BULOT L. (1999).- C- Valanginian and Lower Hauterivian of the isotope stratigraphy, a calibration tool Mediterranean region.- Tethyan and Boreal between ammonite and magnetostrati- Cretaceous Correlation - Newsletter, n° 9, p. graphy: the Valanginian-Hauterivian transi- 6-15. tion.- Geologica Carpathica, Bratislava, vol. KLEIN J. (2005).- Lower Cretaceous Ammonites 50, n° 1, p. 91-96. I, Perisphinctaceae 1: Himalayitidae, Olco- HOEDEMAEKER P.J. (1995).- Ammonite distri- stephanidae, Holcodiscidae, Neocomitidae, bution around the Hauterivian-Barremian Oosterellidae. In: RIEGRAF W. (ed.), Fossi- boundary along the Río Argos (Caravaca, SE lium Catalogus I: Animalia.- Backhuys Spain).- Géologie Alpine, Grenoble, Publishers (Leiden), part 139, 484 p. (Mémoire H.S.), t. 20, p. 219-277. KRUSE S. & MUTTERLOSE J. (2000).- Coccoliths HOEDEMAEKER P.J. & REBOULET S. (reporters), under stress? Lower Cretaceous calcareous AGUIRRE-URRETA M.B., ALSEN P., AOUTEM M., nannofossil assemblages of nearshore and ATROPS F., BARRAGAN R., COMPANY M., pelagic settings (NW Africa).- Journal of GONZALEZ ARREOLA C., KLEIN J., LUKENEDER Nannoplankton Research, London, vol. 22, A., PLOCH I., RAISOSSADAT N., RAWSON P.F., n° 2, p. 171. ROPOLO P., VASICEK Z., VERMEULEN J. & LEMOINE M. (1984).- Mesozoic evolution of the WIPPICH M.G.E. (2003).- Report on the 1st western Alps.- Annales Geophysicae, vol. 2, International Workshop of the IUGS Lower n° 2, p. 171-172. Cretaceous Ammonite Working Group, the LEMOINE M. (1985).- Structuration jurassique 'KILIAN Group' (Lyon, 11 July 2002).- des Alpes occidentales et palinspastiques de Cretaceous Research, London, vol. 24, n° 1, la Téthys ligure.- Bulletin de la Société p. 89-94 ; erratum, vol. 24, n° 6, p. 805. Géologique de France, Paris, (Série 8), t. I, JACQUIN T., RUSCIADELLI G., AMEDRO F., n° 1, p. 126-137. GRACIANSKY P.C. de & MAGNIEZ-JANNIN F. MCARTHUR J.M., JANSSEN N.M.M., REBOULET S., (1998).- The north atlantic cycle: an LENG M.J., THIRLWALL M.F. & SCHOOTBRUGGE overview of 2nd-order transgres- B. van de (2007).- Palaeotemperatures, sive/regressive facies cycles in the lower polar ice-volume, and isotope stratigraphy Cretaceous of western Europe.- In: (Mg/Ca, δ18O, δ13C, 87Sr/86Sr): The Early GRACIANSKY P.C. de, HARDENBOL J., JACQUIN Cretaceous (Berriasian, Valanginian, T. & VAIL P.R. (eds.), Mesozoic and Cenozoic Hauterivian).- Palaeogeography, Palaeocli- sequence stratigraphy of European basins.- matology, Palaeoecology, Amsterdam, vol. Society of Economic Paleontologists and 248, n° 3-4, p. 391-430. Mineralogists (SEPM) Special Publication, MAGNIEZ-JANNIN F. (1992).- Enregistrement de Tulsa, n° 60, p. 397-409. l'eustatisme par les foraminifères dans les JANSSEN N.M.M. & CLÉMENT A. (2002).- séquences de dépôt du Crétacé inférieur du Extinction and renewal patterns among bassin vocontien (Sud-Est de la France).- Tethyan belemnites in the Verrucosum Palaeogeography, Palaeoclimatology, Palaeo- Subzone (Valanginian) of southeast France.- ecology, Amsterdam, vol. 91, n° 3-4, p. Cretaceous Research, London, vol. 23, n° 4, 247-262.

24 Carnets de Géologie / Notebooks on Geology - Book 2008/01 (CG2008_BOOK_01)

MAGNIEZ-JANNIN F. & DOMMERGUES J.L. (1994).- PAVIA G. & STURANI C. (1968).- Étude Foraminifères vs. ammonites en fosse biostratigraphique du Bajocien des Chaines vocontienne vers la limite Valanginien- Subalpine aux environs de Digne (Basses Hauterivien.- Comptes Rendus de l'Académie Alpes).- Bollettino della Società Geologica des Sciences, Paris, t. 319, ( série II), n° 2, Italiana, Roma, vol. LXXXVII, p. 305-316. p. 957-962. PELLENARD P., DECONINCK J.-F., HUFF W.D., MATTIOLI E. & ERBA E. (1999).- Synthesis of THIERRY J., MARCHAND D., FORTWENGLER D. calcareous nannofossil events in Tethyan & TROUILLER A. (2003).- Characterization Lower and Middle Jurassic successions.- and correlation of Upper Jurassic (Oxfordian) Rivista Italiana di Paleontologia e bentonite deposits in the Paris Basin and the Stratigrafia, Milano, vol. 105, n° 3, p. 343- Subalpine Basin, France.- Sedimentology, 376. vol. 50, n° 6, p. 1035-1060. MOULLADE M. (1966).- Étude stratigraphique et PERCH-NIELSEN K. (1979).- Calcareous nanno- micropaléontologique du Crétacé inférieur de fossils from the Cretaceous between the la fosse vocontienne.- Documents des North Sea and the Mediterranean.- Aspekte Laboratoires de Géologie de Lyon, n° 15, der Kreide Europas, Stuttgart, IUGS Serie A, 369 p. n° 6, p. 223-272. MOURGUES A. (2007).- La transgression du PERCH-NIELSEN K. (1985).- Mesozoic calcareous Crétacé inférieur au Nord du Chili. nannofossils.- In: BOLLI H.M., SAUNDERS J.B Biostratigraphie, Paléontologie (Ammonites), & PERCH-NIELSEN K. (eds.), Plankton Strati- Statigraphie séquentielle et tectonique graphy.- Cambridge University Press, p. synsédimentaire.- Unpublished Ph.D. thesis, 329-426. Université Paul Sabatier, Toulouse, 293 p. QUENSEL P. (1988).- Die Ammoniten im MUTTERLOSE J. (1992).- Biostratigraphy and Valangin-Hauterive Grenzbereich vom palaeobiogeography of early Cretaceous Mittlelandkanal bei Pollhagen.- Berliner calcareous nannofossils.- Cretaceous geowissenschaftliche Abhandlungen, Reihe Research, London, vol. 13, n° 2, p. 167-189. A, Band 94, p. 15-71. MUTTERLOSE J. (reporter), AUTRAN G., RAWSON P.F. (1973).- Lower Cretaceous (Rya- BARABOSCHKIN E.J., CECCA F., ERBA E., zanian-Barremian) marine connections and GARDIN S., HERNGREEN W., HOEDEMAEKER P., cephalopod migrations between the Tethyan KAKABADZE M., KLEIN J., LEEREVELD H., and Boreal Realms. In: CASEY R. & RAWSON RAWSON P.F., ROPOLO P., VAŠÍČEK Z. & and P.F. (eds.), The Boreal Lower Cretaceous.- SALIS K. von (1996).- The Hauterivian Geological Journal, Liverpool, Special Issue, Stage.- Bulletin de l'Institut Royal des vol. 5, p. 131-144. Sciences Naturelles de Belgique, Sciences de RAWSON P.F. (1983).- The Valanginian to Aptian la Terre, n° 66 suppl., p. 19-24. stages – current definitions and outstanding ODIN G.S. (1994).- Geological time scale problems.- Zitteliana, München, Heft 10, p. (1994).- Comptes Rendus de l'Académie des 493-500. Sciences, Paris, t. 318, (série II), n° 1, p. RAWSON P.F. (1993).- The influence of sea level 59-71. changes on the migration and evolution of OGG J.G., AGTERBERG F.P.& GRADSTEIN F.M. early Cretaceous (pre-Aptian) ammonites. (2004).- The Cretaceous Period. In: In: HOUSE M.R. (ed.), The ammonoidea: GRADSTEIN F., OGG J., SMITH A. (eds.), A Environment, Ecology, and Evolutionary geological time scale.- Cambridge University change.- Systematics Association Special Press, Cambridge, p. 344-383. Volume, n° 47, p. 227-242. OLIVERO D. (1996).- Zoophycos distribution and RAWSON P.F. (2004).- Report of the IUGS-ICS sequence stratigraphy. Examples from the Subcommission on Cretaceous Stratigraphy.- Jurassic and Cretaceous deposits in south- Stratigraphy Newsletter, n° 6, 12 p. eastern France.- Palaeogeography, Palaeo- RAWSON P.F & HOEDEMAEKER P.J. (reporters), climatology, Palaeoecology, Amsterdam, vol. AGUIRRE-URRETA M.B, AVRAM E., ETTACHFINI 123, n° 1-4, p. 273-287. M., KELLY S.R.A., KLEIN J., KOTETISHVILI E., OLIVERO D. (2003).- Early Jurassic to Late OWEN H.G., ROPOLO P., THOMSON M.R.A., Cretaceous evolution of Zoophycos in the WIPPICH M. & VASICEK Z. (1999).- Report on French Subalpine Basin (southeastern the 4th International Workshop of the Lower France).- Palaeogeography, Palaeocli- Cretaceous Cephalopod team (IGPC-Project matology, Palaeoecology, Amsterdam, vol. 362).- Scripta Geologica, Leiden, Special 192, n° 1-4, p. 59-78. Issue 3, p. 3–13. PAVIA G. (1973).- Ammoniti del Baiociano REBOULET S. (1996).- L'évolution des ammo- superiore di Digne (Francia SE, dip. Basses- nites du Valanginien-Hauterivien inférieur du Alpes).- Bollettino della Società Paleon- bassin vocontien et de la plate-forme tologica Italiana, Modena, vol. 10, n° 2, p. provençale (Sud-Est de la France): relations 75-142. avec la stratigraphie séquentielle et PAVIA G. (1983).- Ammoniti e biostratigrafia del implications biostratigraphiques.- Documents Baiociano inferiore di Digne.- Bollettino del des Laboratoires de Géologie de Lyon, n° Museo Regionale di Scienze Naturali di 137, 371 p. Torino, Monografie, II, 257 p.

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REBOULET S. & ATROPS F. (1995).- Rôle du Western North Atlantic (Site 534): climat sur les migrations et la composition biostratigraphy, preservation, and some des peuplements d'ammonites du Valangi- observations on biogeography and nien supérieur du bassin vocontien (S-E de paleoceanography.- Initial Reports of Deep la France).- Geobios, vol. 28, Supplement 1, Sea Drilling Project, College Station, vol. 76, p. 357-365. p. 587-621. REBOULET S. & ATROPS F. (1997).- Quantitative SCHOOTBRUGGE B. van de, KUHN O., ADATTE T., variations of the valanginian ammonite STEINMANN P.& FÖLLMI K. (2003).- fauna of the Vocontian Basin (south-eastern Decoupling of P- and Corg-burial following France) between limestone-marls and within Early Cretaceous (Valanginian-Hauterivian) parasequences.- Palaeogeography, Palaeocli- platform drowing along the NW Tethyan matology, Palaeoecology, Amsterdam, vol. margin.- Palaeogeography, Palaeoclima- 135, n° 1-4, p. 145-155. tology, Palaeoecology, Amsterdam, vol. 199, REBOULET S. & ATROPS F. (1999).- Comments n° 3-4, p. 315-331. and proposals about the Valanginian-Lower SISSINGH W. (1977).- Biostratigraphy of Hauterivian ammonite zonation of south- Cretaceous calcareous nannoplankton.- eastern France.- Eclogae Geologicae Geologie en Mijnbouw, Amsterdam, vol. 56, Helvetiae, Basel, vol. 92, n° 2, p. 183-197. n° 1, p. 37-65. REBOULET S., ATROPS F., FERRY S. & SCHAAF A. STURANI C. (1967).- Ammonites and (1992).- Renouvellement des ammonites en stratigraphy of the Bathonian in the Digne- fosse vocontienne à la limite Valanginien- Barrême area (south-eastern France, dept. Hauterivien.- Geobios, n° 25, fasc. 4, p. Basses-Alpes).- Bollettino della Società 469-476. Paleontologica Italiana, Modena, vol. 5, n° 1, REBOULET S., GIRAUD F. & PROUX O. (2005).- p. 3-57. Ammonoid abundance variations related to THIERSTEIN H.R. (1973).- Lower Cretaceous changes in trophic conditions across the calcareous nannoplankton biostratigraphy.- Oceanic Anoxic Event 1d (Latest Albian, SE Abhandlungen der Geologischen France).- Palaios, Tulsa, vol. 20, n° 2, p. Bundesanstalt, Wien, Band 29, 52 p. 121-141. THIERSTEIN H.R. (1976).- Mesozoic calcareous REBOULET S. & HOEDEMAEKER P.J. (reporters), nannoplankton biostratigraphy of marine AGUIRRE URRETA M.B., ALSEN P., ATROPS F., sediments.- Marine Micropaleontology, BARABOSKIN E.Y., COMPANY M., DELANOY G., Amsterdam, vol. 1, p. 325-362. DUTOUR Y., KLEIN J. LATIL J.L., LUKENEDER THIEULOY J.-P. (1973).- The occurrence and A., MITTA V., MOURGUES F.A., PLOCH I., distribution of boreal ammonites from the RAISSOSSADAT N., ROPOLO P., SANDOVAL J., Neocomian of southeast France (Tethyan TAVERA J.M., VASICEK Z., VERMEULEN J., Province). In: CASEY R. & RAWSON P.F. ARNAUD H., GRANIER B. & PREMOLI-SILVA I. (eds.), The Boreal Lower Cretaceous.- (2006).- Report on the second international Geological Journal, Liverpool, Special Issue, meeting of the IUGS Lower Cretaceous vol. 5, p. 289-302. Ammonite Working Group, the "KILIAN THIEULOY J.-P. (1977a).- La zone à Callidiscus Group" (Neuchâtel, Switzerland, 8 du Valanginien supérieur vocontien (Sud-Est September 2005).- Cretaceous Research, de la France). Lithostratigraphie, London, vol. 27, n° 5, p. 712-715. ammonitofaune, limite Valanginien-Haute- REBOULET S., MATTIOLI E., PITTET B., BAUDIN F., rivien, corrélations.- Géologie Alpine, OLIVERO D. & PROUX O. (2003).- Ammonoid Grenoble, t. 53, p. 83-143. and nannoplankton abundance in Valangi- THIEULOY J.-P. (1977b).- Les ammonites nian (early Cretaceous) limestone-marl boréales des formations néocomiennes du successions from the southeast France Sud-Est français (province submédi- Basin: carbonate dilution or productivity?- terranéenne).- Geobios, n° 10, fasc. 3, p. Palaeogeography, Palaeoclimatology, Palaeo- 395-461. ecology, Amsterdam, vol. 201, n° 1-2, p. THIEULOY J.-P., FUHR M. & BULOT L.G. (1990).- 113-139. Biostratigraphie du Crétacé inférieur de l'Arc RENEVIER E. (1874).- Tableau des terrains de Castellane (S.E. de la France). 1 : Faunes sédimentaires.- Bulletin de la Société d'ammonites du Valanginien supérieur et Vaudoise des Sciences Naturelles, Lausanne, âge de l'horizon de "La Grande Lumachelle".- n° 13, p. 218-52. Geologie Méditerranéenne, Marseille, vol. ROTH P.H. (1978).- Calcareous nannoplankton XVII, n° 1, p. 55-99. biostratigraphy and oceanography of the WIPPICH M.G.E. (2001).- Die tiefe Unter-Kreide Northwestern Atlantic Ocean.- Initial Reports (Berrias bis Unter-Hauterive) im südwest- of the Deep Sea Drillling Project, College marokkanischen Becken: Ammonitenfauna, Station, vol. 44, p. 731-760. Bio-und Sequenzstratigraphie.- Thesis Uni- ROTH P.H. (1983).- Jurassic and Lower versität Bochum, 142 p. Cretaceous Calcareous nannofossils in the

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