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Deep-water sedimentation in the Alpine Foreland Basin of SE : New perspectives on the Gr~s d' and related systems- an introduction

PHILIPPE JOSEPH 1 & SIMON A. LOMAS 2

I lFP School/Geology-Geochemistry Division, Institut Franfais du P~trole, 228-232, avenue Bonaparte, 92852 Rueil Malmaison Cedex, France (e-mail. [email protected]) 2Baker Atlas GeoScience, Stoneywood Park North, Aberdeen AB21 7EA, UK (e-mail: simon.lomas@bakeratlas, com)

The Gr~s d'Annot and geologists, a long-term in the Gr6s d'Annot occurred in the late 1990s love affair! with the development of detailed studies of the architecture of the turbidite sandstone bodies, For over 150 years, the fascinating outcrops of in order to improve the characterization of the Gr+s d'Annot Formation of SE France analogous deep-water subsurface hydrocarbon have attracted the interest of many geologists, reservoirs. During that period and up to the from different countries and from academic as present day, many international teams have well as industrial spheres. As Stanley relates in worked intensively on the Gr6s d'Annot with this volume, the initial interest was stratigraphic complementary approaches, and the purpose of (identification of contemporaneous formations the 2001 'Confined Turbidite Systems' research corresponding to continental to marine settings) conference, jointly organized in by the and structural: the recognition of large displace- IFP and the University of Aberdeen, was to pro- ments of Alpine nappes led to new concepts of mote exchanges between these teams, to establish mountain formation. Concerning the sedimen- the state-of-the-art and to identify new avenues tology of deep marine deposits, major advances for future research. were made in the late 1950s and early 1960s From these studies, and following the classifi- with the progressive emergence of the turbidite cation of Reading & Richards (1994) based on concept and its recognition in the field (Faure- grain size and nature of the feeder system, the Muret et al. 1956; Kuenen et al. 1957; Bouma GrOs d'Annot is now considered as a benchmark 1962; Lanteaume et al. 1967), and the develop- example of a sand-rich delta-fed turbidite system. ment of the first submarine canyon/fan valley Its depositional character was strongly influ- model (Stanley 1961). From that time onwards enced by a predominance of large magnitude the Gr6s d'Annot outcrops were used as a train- flows carrying relatively coarse-grained sand, ing area in the field, with the organization of interacting with significant basin-floor numerous meetings and field courses (for induced by alpine tectonics. Its characteristics example Beaudoin et al. 1975; Stanley 1975). are very different from those of canyon-fed sys- Renewal of this research activity was stimulated tems, as in the classic sand-rich 'suprafan' in the 1980s by the upsurge of intensive explora- model (e.g. the present Avon and Calabar sub- tion on continental margins and the emergence marine fans offshore Nigeria), or mud-rich of seismic stratigraphy; the Gr6s d'Annot were channel-levee systems (e.g. Amazon and ZaYre studied in order to help seismic interpretation deep-sea fans). A recent analogue could be the and, at the same time, complementary flume Eastern Corsica fan system recently described experiments of submarine avalanches were by Gervais et al. (in press). The GrOs d'Annot developed for better understanding of turbidity has frequently been used as an analogue for current processes (Laval et al. 1988). The critical sand-rich turbidite hydrocarbon fields where field studies in the 1980s led to the first com- topographic control has played a key role in prehensive palaeogeographic scheme for the defining the reservoir bodies, like in the North Gr6s d'Annot basin sensu lato, based on palaeo- Sea (e.g. Gannet fields and Gryphon field; current directions, onlap orientation and correla- Newman et al. 1993) or on the Brazilian margin tion of key marker levels (Ravenne et al. 1987), (Campos basin; Moraes et al. 2000). which is still largely used at present. In parallel The global study area is located in the French studies, the influence of folding on basin floor departments of Alpes Maritimes, Alpes de Haute topography was recognized (Apps 1985, 1987; and Hautes Alpes. From a structural Elliott et al. 1985). A second renewal of interest point of view it belongs to the Southern Subalpine

From: JOSEPH, P. & LOMAS, S. A. (eds) 2004. Deep-Water Sedimentation in the Alpine Basin of SE France: New perspectives on the Grks d'Annot and related systems. Geological Society, London, Special Publications, 221, 1-16. 0305-8719/03/$15.00 © The Geological Society of London. Downloaded from http://sp.lyellcollection.org/ by guest on September 29, 2021

2 P. JOSEPH & S. A. LOMAS

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Fig. 1. Structural map of SE France (redrawn from the BRGM 1:1 000000 geological map 1996) and location of outcrops of Gr6s d'Annot and related systems studied in this volume (1 Amy et al., 2 Apps et al., 3 Bourgeois et al., 4 Bouroullec et al., 5 Broucke et al., 6 Callec, 7 Du Fornel et al., 8 Euzen et al., 9 Evans et al., 10 Ford & Lickorish, 11 Garcia et al., 12 Guillocheau et al., 13 Lansigu & Bouroullec, 14 Lee et al., 15 McCaffrey & Kneller, 16 Moraes et al., 17 Puigdeffibregas et al., 18 Smith & Joseph, 19 Stanbrook & Clark, 20 Tomasso & Sinclair).

Chains, part of the Alpine Foreland Basin. the geodynamical paper of Ford & Lickorish, Figure 1 displays the structural and stratigraphic deal with the whole system. framework of the Gr6s d'Annot, with the location The remnants of the Upper Eocene-Lower Oli- of the different research areas: a code number has gocene Gr6s d'Annot and related systems (Fig. l) been given to each paper of this volume, and is are located on the para-autochthonous Digne attributed to each research area in the legend of Thrust verging southward in the Arc, this figure. The two introductory historical and overlain by the allochtonous Embrunais- papers of Stanley and Bouma & Ravenne, and Ubaye Nappes (Autapie and Parpaillon) located Downloaded from http://sp.lyellcollection.org/ by guest on September 29, 2021

NEW PERSPECTIVES ON THE GRI~S D'ANNOT 3 around . The whole system is (Gulf of Lion), and therefore the shut-off of sedi- delimited by two crystalline and Palaeozoic mas- ment supply from the Corsica-Sardinia massif sifs: Pelvoux to the north and Maures-Esterel to (S6ranne 1999). the south. Two regional structural cross-sections In agreement with the subsidence modelling have already been published (Graham in Elliott of Vially (1994), Apps et al. consider that the et al. 1985, fig. 2.1, and Ford et al. 1999, fig. 2): deformation of the Gr6s d'Annot basin was they differ in the degree of involvement of base- dominated by the SW-directed Alpine thrusting, ment in the alpine thrusts, but both are still local thin-skinned extension (Gialorgues) and largely speculative at depth as no seismic profiles strike-slip faulting (Rouaine) being minor com- or boreholes are available for the area. ponents in an overall compressive setting. They This volume is organized in different sub- consider with Ford & Lickorish that the Meso- themes to reflect the varying approaches of the zoic and Palaeozoic basement (Barrot, Argen- researchers. Here we present an overview of tera) must be involved in this thrusting, even if those themes and try to emphasize where consen- there are a number of structural repetitions of sus has been reached, the new perspectives the Mesozoic cover. In contradiction to previous recently proposed, and key potential areas for interpretations that consider a late exhumation future research. (Late Miocene) of the Argentera area, Apps et aL propose an early uplift of the Barrot Massif, emergent and eroded to its Permian Geodynamic and structural evolution core by the Mid Eocene (Lutetian), and provid- ing an input of clastic material to the basin. Using a global reconstruction of the peri-alpine In this framework, Evans et al. examine the foreland basin from Eocene to Pliocene times, relationship between the westernmost Barr~me Ford & Liekorish highlight the complex trajec- Basin and the other Gr6s d'Annot sub-basins. tory of the Alpine orogenic prism and the varia- The shallow-marine turbidite formation of Gr+s bility of shortening rates through time. During de Ville is time-equivalent to (or slightly younger early collision between Italy (Apulia) and than) the last Gr6s d'Annot deposits (Mid Rupe- Europe in Eocene times, an increasingly arcuate, lian). Evans et ai. show that the Gr6s de Ville is peripheral flexural basin migrated rapidly NW not a feather-edge to the Gr6s d'Annot, but across the European plate. The Early Oligocene accumulated in a narrow thrust-sheet-top basin, was characterized by a decoupling of the oro- separated from the Gr6s d'Annot system by a genic prism from its south-western border synsedimentary anticline. These two distinct (Southern Subalpine Chains) by means of several sub-basins were fed by different sediment trans- transpressive strike-slip faults: for these authors port paths, linked only to the Maures-Esterel the evolution of the Gr6s d'Annot basin is subse- massif (and not to Corsica-Sardinia) in the case quently governed mainly by the gravitational of the Barr~me Basin. The Gr6s de Ville sliding of the internal Embrunais-Ubaye correspond therefore to the last stage of filling Nappes over the external foreland basin. of Gr+s d'Annot related sub-basins during Oligo- For Apps et al., the complex palaeotopogra- cene times, before the complete emergence of the phy of the Gr6s d'Annot basin was controlled foreland deposits. by the interaction of three different orogenic events: (1) the Pyreneo-Provengal east-west oriented fold and thrust belt, linked to the New perspectives on structural evolution Iberia-Europe collision (Late Cretaceous to Palaeocene); (2) the NW-SE oriented alpine The structural complexity of the Gr6s d'Annot folds and thrusts due to the Apulia-Europe colli- basin results from the interference of different sion to the East (Mid Eocene); and (3) to the orogenic events, acting on a Palaeozoic and South the subduction of the Tethyan oceanic Mesozoic basement characterized by significant crust (related to Apulia) below the SE margin heterogeneity in terms of thickness and rheology. of the Iberia plate (Maastrichtian to Eocene). During Eocene-Oligocene times, the deforma- This 'East Iberian' orogeny induced the uplift tion velocity field appears to have been highly of the Corsica-Sardinia massif and the rejuvena- variable, with a blocking of Alpine thrusting to tion of the Maures-Esterel structures, which the south and NW by the Maures-Esterel and provided sediment to the Gr6s d'Annot basin Pelvoux crystalline massifs, already emergent at during the Late Eocene. During Early Oligocene that time (Fig. 1). A better understanding of (Rupelian) times, the SE rollback of the subduc- the structural evolution would require full tion hinge induced the beginning of the NE-SW three-dimensional modelling (analogue and/or oriented rifting of the Liguro-Provengal basin numerical) of the foreland basin evolution, Downloaded from http://sp.lyellcollection.org/ by guest on September 29, 2021

4 P. JOSEPH & S. A. LOMAS Lithostratigraphy

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normal fault # IIFU~I Fig. 2. Schematic lithostratigraphy of the Grds d'Annot basin-fill (modified from Ravenne et al. 1987 and Apps et al., this volume). using three-dimensional tools of forward defor- levels are identified in the Mesozoic series: mation and taking into account the effects of Triassic evaporites, Middle and Upper Juras- sedimentation on the deformation field. sic black shales and mid-Cretaceous black shales. The unconformity is locally marked by the presence of non-marine 'Infra-Nummu- Chronostratigraphy and palaeogeography litic' conglomerates ('Poudingues d'Argens'), preserved in local depressions at the border The Gr~s d'Annot Formation corresponds to a of palaeohighs (see Apps et aL). The Calcaires heterogeneous pile of sand-rich gravity flow Nummulitiques Formation comprises bioclas- deposits, up to 1200m thick in a given vertical tic limestones and resedimented polygenic section, that range from Mid Eocene (Bartonian) breccias, which are interpreted respectively as to Lower Oligocene (Rupelian). This formation shallow marine and slope deposits developed belongs to the classic 'Trilogie Priabonienne' at the beginning of the Tertiary transgression. (Boussac 1912) but in fact its age is not limited (2) The overlying 'Marnes Bleues' comprise to Priabonian and it is better to refer to it as hemipelagic marlstones deposited on a the 'Nummulitic Trilogy'. (More generally, slope or distal ramp setting (Ravenne et al. Sinclair 1997 termed this type of foreland 1987). The transition to the Gr~s d'Annot basin-fill succession the 'Underfilled Trinity'.) at the top of the Marnes Bleues is named This trilogy consists of three lithostratigraphic 'Marnes Brunes Inf6rieures' because of the units (Fig. 2: see Joseph et al. 2000 for more progressive increase in thin brownish turbi- details): dites (see Stanbrook & Clark). (3) The Gr~s d'Annot sensu lato are gravity flow (1) The 'Calcaires Nummulitiques' rest uncon- deposits (siliciclastic turbidites and debris formably on the Mesozoic series which were flow deposits) that lap on to the Marnes severely deformed during the Pyreneo-Proven- Bleues palaeoslope with an angle of up to 9al compression phase. Several d~collement 20 °. Three key horizons 20 m thick are used Downloaded from http://sp.lyellcollection.org/ by guest on September 29, 2021

NEW PERSPECTIVES ON THE GRI~S D'ANNOT 5

for correlation in the northeastern Sangui- ni6re area (Jean 1985; Jean et al. 1985; Elliott o9 cO et al. 1985 and Fig. 2): two mud-rich debris Ill uJ t- .,.~_ r'O- ) ...~_,.Or" ,(~ '~"- °,£o_ flow deposits (which include blocks of sand- r~ (.9 o~ stone, shale and limestone up to 10 m thick) Ill ,_ ~% 0 O3 and an extensive shale-rich unit located oO r-2~ towards the top of the series. The very top 23.8. of the series is marked again by brownish 23.8', 23.9 Ma Ma marls ('Marries Brunes Sup~rieures'). Ma To the NE, the Nummulitic Trilogy is capped by the 'Schistes-fi-Blocs' Formation, which is a n, z NP25 thick heterolithic olistostrome emplaced on the uJ P22 n I..- sea floor at the front of the advancing Autapie n Nappe (Kerckhove 1969). Emplacement of the "1- (.3 Schistes-fi-Blocs was associated with deep ero- Ill 27.1' sion of the upper levels of the Gr6s d'Annot. Z . 27.5- The chronostratigraphic data presented in this Ill volume are based on the 'P zonation' defined by 28.5 P21 NP24 Berggren et al. (1995) for planktonic foraminifera O and the 'NP zonation' defined by Martini (1971) O 29.4 for calcareous nannofossils (Fig. 3). _l Z : : P20 ..... 29,9, Du Fornel et aL present the results of systema- O., !30.3 ...... ": " .._1 tic sampling of the top of the Marnes Bleues and W U3 13- :::::Pi9 : : ::NP23:

fine-grained levels inside the Gr6s d'Annot, in • ... 1 ...... : ::: : conjunction with an estimate of the palaeobathy- O rY : .. J metry from benthic foraminiferal associations : : ...... 3ZO. (generally in a range 200-500 m). This work pro- 323 vides a new and well-constrained framework for P18 NP223218 the correlation of the different Gr6s d'Annot NP21 remnants: a better picture of the topography of 33.7 ,,'P 17~33,8 ...... the different sub-basins may be drawn (Fig. 4), Z thanks to palaeocurrent data (giving mean trans- n," u.I port directions), onlap surface orientations 13.. (enabling the reconstruction of palaeoslopes) ILl n and palaeobathymetry estimates. This figure Z D clearly shows the diachronous onset of filling of Ill the successive sub-basins (displayed by shading O identical to that used in Fig. 3): O ILl uJ • The Eastern Italian sub-basin (Bevera and _J D Mortola, 10km NE of Menton) was actively £3 filling during Bartonian times (PI4 foraminif- eral zone). • The Contes-Pei'ra Cava system was probably separated from the previous one by the Fig. 3. Chronostratigraphic chart used in this Sospel-Oliveta palaeohigh (finer-grained volume. facies and west-directed palaeocurrents, and proximity of Triassic outcrops: see Amy because of the lack of intermediate outcrops et al.): deposition here began at Early Priabo- and the lack of biostratigraphic data from nian (P15 sup zone). the Lauzanier area. • The Mont Tournairet area, of the same Early The Sanguini6re sub-basin became active Priabonian age (P15 sup-NP 19 zone), may during the Late Priabonian (P16-NP19/20 correspond either to the westward extension zone). It was probably fed by a.['an delta (less of the Peira Cava basin, or to a distinct sub- developed than the St Antonin one) that has basin. The possible extension of this system been recently identified in the Quatre Cantons to the Lauzanier area to the north of the area (Joseph & Ravenne 2001). This narrow Argentera Massif is based only on the palaeo- sub-basin was confined between the Argentera current directions and is highly speculative and Barrot- submarine palaeohighs Downloaded from http://sp.lyellcollection.org/ by guest on September 29, 2021

6 P. JOSEPH & S. A. LOMAS

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Onset of filling of the main Digne thrust fault Gres d'Annot sub-basins Onlap direction '~ Emergent domain with continental sedimentation Bartonian (Beginning Oligocene) -.~ Palaeocurrent Lower Priabonian ~" Fluvialsystem , Main sources Upper Priabonian ~ Massif subiect to active erosion [~ Lower Rupelian Fan deltas (conglomerates) Upper Eocene-Lower Oligocene [--] Palaeohighs or lobe distal fringes par-autochthonous formations Middle Rupelian / / (fine-grained turbidites)

Fig. 4. Palaeogeographical evolution of the main Gr6s d'Annot sub-basins with age of onset of filling. Onlap and palaeocurrent directions are derived from Bouma & Coleman (1985): Contes, Menton, Peira Cava; Ford et al. (1999): Champsaur, Devoluy; Ravenne et al. (1987): Annot, Barrame, Grand Coyer, Sanguini6re, Trois Evach6s.

(clear onlaps can be recognized on both east- widened westwards to the Allos area during ern and western borders of the sub-basin). It the Early Rupelian. passed downstream to the Trois Ev6ch~s sub- • During the Late Priabonian (P16-NP19/20 basin (Lomas et al. 2000) and progressively zone), the Annot sub-basin was a fully confined Downloaded from http://sp.lyellcollection.org/ by guest on September 29, 2021

NEW PERSPECTIVES ON THE GRI~S D'ANNOT 7

(ponded) basin (Apps 1985) that is considered The complex palaeogeography of the Gr6s to have been fed by the St Antonin fan delta d'Annot basin and the beginning of clastic (Sinclair 2000). During the Early Rupelian sedimentation in each sub-basin are now better (P18-NP21 zone: Dn Fornel et aL; Puigdeffibre- constrained thanks to recent research on palaeo- gas et aL), it began to spill over to the Trois topography and biostratigraphy, but the exact Ev6ch6s basin (Chalufy) through the Grand timing of the filling of each sub-basin remains a Coyer trough. In the Grand Coyer area some matter of debate due to the limited chronostrati- disagreement remains on the geometry of the graphic resolution for the Lower Oligocene Gr6s d'Annot deposits: Stanbrook & Clark (Rupelian). Some areas remain poorly controlled reconstruct a very complex palaeotopography (Lauzanier, Quatre Cantons, Mont Tournairet, and consider, unlike Pickering & Hilton Contes, some parts in Trois Ev6chds). Systematic (1998), Sinclair (2000) and Dn Fornel et al. dating and correlation, using new techniques (this volume) but in agreement with Elliott such as chemostratigraphy, might be used to et al. (1985) and Clark & Gardiner (2000), lift the remaining uncertainty concerning the that there is a general palaeoslope dipping relationship between adjacent sub-basins. northeastwards, and not a narrow trough. For Apps et aL, the emergent Barrot palaeohigh directly provided coarse-grained sediments to Sequence stratigraphy the Grand Coyer area at that time. Using a novel sequence stratigraphic approach The end of filling of these sub-basins is poorly focused on the Annot sub-basin, Callec inter- constrained because of the lack of dating and prets the Gr~s d'Annot as the regressive part of the later erosion associated with emplacement a second-order transgressive-regressive cycle of the Schistes-/t-Blocs: during Rupelian times (sensu Mitchum & Van Wagoner 1991: duration the Gr6s d'Annot probably corresponded to a around 10 Ma) including the whole Nummulitic wide connected system blanketing most of the Trilogy (Calcaires Nummulitiques, Marnes study area (Pickering & Hilton 1998). Bleues and Gr~s d'Annot). He relates the constituent third-order depositional sequences (estimated mean duration 1-3 Ma) to global sea New perspectives on palaeogeography level variations, which are highly modulated by the tectonic deformation of the foreland. In The palaeotopography of the Gr6s d'Annot agreement with Evans et al. for the Gr~s de system therefore appears to have been controlled Ville in Barr~me, he proposes that the uplift by active tectonics from Mid Eocene (Bartonian) induced forced regressions of the sandy deposi- to Early Oligocene (Rupelian) times, with two tional systems, with an increase of the sediment main phases linked to the foreland development: flux, a reinforcement of the erosive third-order (1) large-scale flexure (on a wavelength of hun- sequence boundaries and a morphological dreds of kilometres) induced by the loading of confinement, with tilting and migration of the the internal nappes: this early phase activated depocentres (Callec 2001). eastward-dipping normal synsedimentary faults Using the new chronostratigraphic data in front of the advancing prism (Puidefiibregas previously described, Du Fornel et aL provide a et al.; Tomasso & Sinclair); (2) medium-scale detailed correlation between different Gr~s (wavelength of tens of kilometres) folding of d'Annot remnants (Fig. 6). This correlation is the autochthonous sedimentary cover above the based on the recognition of fourth-order deposi- Triassic evaporite d6collement level: this phase tional sequences (sensu Mitchum & Van Wagoner induced narrow synclinal troughs acting as dis- 1991, i.e. sequences of around 200-400 ka dura- connected sub-basins (Fig. 5). The progressive tion), made up of groups of genetic units (fifth- emergence of thrusts rooting in the basement order sequences: likely mean duration around and affecting the whole sedimentary series 20 ka, Guillocheau et aL). This analysis constrains induced the development from East to West of the correlation of major surfaces (erosive thrust-top-sheet (piggy-back) basins (Sangui- sequence boundaries, shaly maximum flooding nitre, Annot, Barr~me) and ended in Mio- surfaces). In this sequence stratigraphic frame- Pliocene times with the emplacement of the work, a detailed evolutionary scheme is proposed westernmost Digne Nappe. In this framework, for the St Antonin-Annot-Grand Coyer- the Early Oligocene appears to have been a Chalufy sub-basin (Fig. 4), evolving from period of reduced tectonic activity, with a general ponding during the Priabonian to spilling, then blanketing of the previous sub-basins by the blanketing during the Early Rupelian. This youngest deposits of the Gr6s d'Annot. evolution is essentially in agreement with the Downloaded from http://sp.lyellcollection.org/ by guest on September 29, 2021

8 P. JOSEPH & S. A. LOMAS

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NEW PERSPECTIVES ON THE GRI~S D'ANNOT 9

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..~ Downloaded from http://sp.lyellcollection.org/ by guest on September 29, 2021 l0 P. JOSEPH & S. A. LOMAS previous (but less detailed) palaeogeographic 20ka eustatic cycles (speculatively comparable reconstructions of Pickering & Hilton (1998) with variations in orbital precession). Each genetic and Sinclair (2000). Du Fornel et aL show a unit is characterized by a progradational phase downcurrent transition from the feeder fan with clinoforms, followed by an aggradational delta to transit channels then sheet-like lobes. phase of spreading. In contradiction to previous Euzen et al. validate the proposed evolution of interpretations of the Gr6s d'Annot as shallow the sub-basin using three-dimensional strati- marine deposits in that area (Sinclair 1993), the graphic modelling of gravity flow processes of authors consider that the facies organization fits erosion, transport and deposition. The main well with a model of a flood-dominated fluvio- controlling parameters of the stratigraphic archi- turbiditic ramp (sensu Mutti et al. 2000). Because tecture are the initial topography of the basin, of the direct connection between the shelf and the tectonic activity that induced third-order the slope, the sequential organization of the turbi- cycles of uplift-denudation of the feeder massifs dite deposits on the slope can be related to the (Corsica-Sardinia and Maures-Esterel massifs), activity of the feeding fan delta on the narrow and the variations of sedimentary supply (of cli- shelf (perhaps with an important contribution matic and/or eustatic origin), which controlled from hyperpycnal flows induced by fluvial the fourth-order sequences. floods, cf. Mulder & Syvitski 1995). In agreement with this modelling, Puigdeffibre- Broueke et aL demonstrate the influence of a gas et ai. relate the sudden influx of very coarse kilometre-scale synsedimentary flexure on the sand and gravels in Annot (Gastres Unit= geometry of these genetic units. The downstream discontinuity at the base of Unit C of Du increase of available space is accommodated by Fornel et aL; see Fig. 6) to a significant tectonic small normal faults induced by gravitational rejuvenation of the hinterland. sliding: this increase induces a downstream thickening of genetic units and the pinching-out of some of them upstream, but their internal New perspectives on sequence stratigraphy organization (facies preservation and cycle geo- metry) does not seem to be strongly affected. This first correlation of depositional sequences must now be extended to the other sub-basins. Three-dimensional stratigraphic modelling seems New perspectives on the depositional to be a powerful tool for ensuring the internal model consistency of the reconstruction, for evaluating scenarios where geological data are scarce, and There is now a broad consensus on the general also for visualizing the complex interaction depositional model for the Gr~s d'Annot. Fol- between sediment supply, sea level variations lowing the first reinterpretation of the St Antonin and tectonics in filling of the sub-basins. Some dis- conglomerates as a fan delta (Stanley 1980), the agreement still remains on the main controlling Gr~s d'Annot system is no longer considered as parameter of the sequence stratigraphic organiza- a classic canyon-fed submarine fan, but as a tion (global eustatic variations versus tectonic sand-rich turbidite submarine ramp fed by activity): a quantification of the range of variation multiple-source fan deltas at the border of the of these parameters would lead to a better estima- Corsica-Sardinia massif (cf. Pickering & Hilton tion of the relative importance of deformation 1998; Joseph et al. 2000; Sinclair 2000). 'Fill rate versus eustatic variations for the different and spill' concepts, in conjunction with the new areas and sedimentation periods of the basin. correlations linking the sub-basin fills (Du Such an enhanced data base would allow better Fornel et al.), have provided key insights into prediction of the nature and the architecture of the mode of basin infilling. However, these new gravity deposits developed in a 'fill-and-spill' set- results seem to argue against an essentially two- ting (initially ponded systems). dimensional sequential infilling and downslope overspilling of successive mini-basins (cf. the 'fill and spill' model for the northern Gulf of High resolution sequence stratigraphy and Mexico slope: Winker 1996; Prather et al. depositional model 1998). For the Gr~s d'Annot, interconnections between the sub-basins may have been more In the Sanguini6re sub-basin (see location in three-dimensional (Fig. 5), and hence sediment Figs 1 & 4), Guillocheau et aL recognize 10 m dispersal was likely to have involved more thick high resolution genetic units (fifth-order three-dimensional pathways, which evolved parasequences, sensu Mitchum & Van Wagoner over time as the basin floor relief changed with 1991), which are interpreted as the results of infilling and ongoing tectonics. 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NEW PERSPECTIVES ON THE GRl~S D'ANNOT 11

Within this general framework, detailed work (1) successive extensional activity during Mid remains to be done on the nature of the processes Eocene (Bartonian) times induced the (short-lived gravity surges versus sustained progressive development of a half-graben hyperpycnal flows), the link with the shallow filled by the Calcaires Nummulitiques and marine areas (fan or braided deltas) and the the lower part of Marnes Bleues (draping effect of the confinement on the resulting facies. the St Benoit palaeocliff that limited the Ultimately, these results should provide valuable half graben westwards); predictive keys in comparable confined systems (2) during the Late Eocene (Priabonian), the in the subsurface such as the Gulf of Mexico, fault was characterized by a transpressive offshore Brazil or the Tertiary of the Central sinistral strike-slip motion that induced a North Sea. monoclinal fold parallel to the fault: the residual palaeotopography in turn induced ponding of the first Gr6s d'Annot deposits Synsedimentary tectonics (Lower Braux Unit) and flow stripping of the diluted upper part of the turbiditic flow In the Sanguini&e sub-basin, Lansigu & above the palaeoslope; Bouroullee identify evidence of tectonic activity (3) during Oligocene (Early Rupelian) times, the during the deposition of the Gr6s d'Annot. fault activity ceased and coarse-grained tur- They show that a network of synsedimentary biditic flows spilled over the remaining normal faults (forming a succession of tilted palaeotopography. This change in the blocks) was strongly influenced by rheological regime of fault activity might be related to discontinuities of sedimentary origin, and the modification of the migration direction especially by the mud-rich layers limiting the of the internal thrusting units, firstly north- genetic units (equivalent to maximum flooding wards during the Lutetian-Bartonian, then surfaces): these layers acted as the nodes of westwards during the Priabonian-Rupelian antithetic and synthetic secondary faults, and (Ford & Lickorish). the rheological contrasts between mud-rich and sand-rich layers induced a staircase geometry of In the Grand Coyer remnant, Stanbrook & Clark the fault surface, with a vertical succession of discuss the relationship of the Marnes Brunes segments with different angles and curvatures. Inf~rieures to the overlying Gr~s d'Annot The deepest mud-rich layers of the series accom- deposits: they argue that this shaly transitional modate the downdip displacement of the tilted facies corresponds to a distal and lateral equiva- fault blocks by layer-parallel movement (listric lent of the coarser Gr~s d'Annot, because of their faults). local interstratification, the similarity of palaeo- Bouroullec et aL quantify the timing of fault current directions and the contemporaneity of activity, which seems to have been discontinuous the fine-grained deposits on the slope and the but frequent (periodicity between 35 and 70 ka). coarse-grained sediments in the basin. They They demonstrate its effect on the geometry of bring to light evidence of synsedimentary defor- genetic units: increase of the overall thickness mation during the deposition of the Marnes in the hanging wall, with a decrease of sand- Brunes Inf6rieures, with dip changes, slump stone:mudstone ratio ('net-to-gross') because development and a slight angular unconformity of a better preservation of fine-grained facies between Marnes Brunes Inf6rieures and Gr6s (heterolithics), and downdip pinching-out of d'Annot. thicker sandstone bodies where the fault growth is significant. These observations reveal a strong coupling between high-resolution sedimentary New perspectives on synsedimentary sequences (genetic units) and the development of tectonics a synsedimentary fault network. Most of these faults are sealed upwards by the Schistes-fi- Previously, the Gr6s d'Annot has classically Blocs Formation. been considered as having accumulated during In the Annot sub-basin near Braux, Tomasso a period of tectonic quiescence. These recent & Sinclair examine the synsedimentary activity studies have led to the recognition of minor of the St Benoit fault (also-called the Gros but frequent tectonic activity (synsedimentary Vallon fault, Pairis (1971), and Le Savelet fault, faults with throw of a few tens of metres, and Puidef~bregas et aL), which is a north-south kilometre-scale flexures). This tectonic activity satellite of the NE-SW Rouaine fault (location strongly interacted with the turbidite sedimen- on Fig. 1). This fault displays three phases of tation and influenced the geometry and activity: facies organization of small-scale sedimentary Downloaded from http://sp.lyellcollection.org/ by guest on September 29, 2021

12 P. JOSEPH & S. A. LOMAS sequences (genetic units a few metres thick). it also seems necessary to take into account the Good examples of both dip and strike evolution spatial non-unO~ormity of the flow concentration are now available along two-dimensional trans- to make a reasonable prediction of the lateral ects, but the real three-dimensional impact of evolution of the sediment thickness. the tectonic activity is still poorly understood In the same sub-basin, Lee et al. discuss the and needs more detailed studies, coupling out- origin of decametre-thick sandstone units that crop observations with modelling of the inter- were deposited close to the base of slope. These action of small-scale brittle deformation and sandstone bodies may have resulted either from sedimentation processes. An effort must also be remobilization by low-efficiency flows of sedi- made to integrate these small-scale observations ments previously deposited higher on the slope, into a comprehensive regional model of deforma- or to the progressive filling of 'spoon-shaped' tion of the entire foreland basin. erosional megascours (a few hundred of metres wide) that were created at the break in slope by the hydraulic jump of gravity flows going down Interaction between turbidity flows and the slope. Attention is drawn to the fact that in basin-floor topography two-dimensional sections these local deposits may be confused with the fill of long-lived Sea floor topography has strong impact on the channels of very different three-dimensional behaviour of turbidity flows, in terms of spatial geometry. variation (termed flow non-uniformity) and temporal evolution (termed flow unsteadiness; Kneller 1995). Changing topography induces Geochemical variability specific trends in facies organization and bed sequences (e.g. Kneller & McCaffrey 1999). By comparing the geochemical compositions of In this volume, using examples near Annot, Gr6s d'Annot deposits sampled in different MeCaffrey & Kneller identify three scales of areas and different stratigraphic levels (with the spatial non-uniformity of turbidity currents: exception of the Gr6s de Ville of the Barr6me Basin), Gareia et ai. show that the chemistry of (1) basinal scale non-uniformity is linked to the clastic components is nearly uniform and changes in slope gradients and is revealed consistent with a southern granite-dominated by the very presence of thick sedimentary provenance (Corsica-Sardinia massif). The deposits; authors examine the effects of transport and (2) flow scale non-uniformity is related to depositional mechanisms on chemical variations specific geometries, in particular the confine- at the bed scale: archetypal turbidites are found ment of turbidity flows in elongated mega- to display a geochemical trend related to vertical scours or channels; decrease of grain size (K-feldspar-quartz-zircon- (3) sub-flow scale non-uniformity results from type heavy minerals) and an upward increase in variability in the sea-floor topography, clay content, which are both related to the grad- which locally modifies the behaviour of the ing by a waning flow in non-channelized systems. flow and induces specific heterogeneity in On the other hand, the sorting of zircon-type the resulting deposits. heavy minerals in lateral deposits of channelized systems may be explained by traction-dominated In poorly-exposed or subsurface systems, these overbank deposition from sustained steady different scales must be identified before inferring flows, spilling over the channel margins. These geometries and facies changes, because small- observations are integrated into a differentiation scale effects may overprint large-scale effects con- model related to hydrodynamic processes, which trolling the overall architecture of the turbidite may explain the specific geochemical signature of system. different facies found at a single location. Using the same approach and comparing tank experiments with outcrop observations in the Pe~ra Cava remnant, Amy et ai. attempt to quan- New perspectives on topographic controls tify the impact of a lateral basin floor slope on the velocity field of the incoming flows and the A better understanding of the interaction resulting deposits. The results suggest that lateral between topography and gravity flows is now confinement reduces the spreading of the flow, achieved, but as has been the case for structural and induces thicker deposits along the slope modelling over the past decade, systematic compared with the basin if the flow velocity is (but time-consuming) experiments of different low, and bypass if the flow velocity is high. But configurations, together with three-dimensional Downloaded from http://sp.lyellcollection.org/ by guest on September 29, 2021

NEW PERSPECTIVES ON THE GRI~S D'ANNOT 13 numerical modelling of sedimentary processes, configurations and vertical connectivities of the will be necessary to better quantify the results reservoir bodies. in terms of depositional geometry and facies organization. This may improve the prediction of reservoir facies in analogous subsurface cases Seismic modelling where the depositional palaeotopography may be inferred (with some uncertainty) from seismic By using as a test case a three-dimensional facies picks and analysis of seismic attributes such as model reconstructed from an outcrop of the amplitudes. Geochemical analysis, generally Sanguini~re sub-basin, Bourgeois et aL compare used for provenance and correlation studies, two methods of seismic modelling: three-dimen- might also be used as a complementary tool to sional full wave modelling gives more realistic better understand the segregation processes. results than multi-one-dimensional convolution, because the method takes into account the lateral heterogeneity in the vicinity of each reflecting Onlap architecture point, and therefore more information on the distribution of petro-acoustic heterogeneity in Remarkable exposures of large-scale onlap rela- the sedimentary pile (reservoir analogue). The tionships are a hallmark of the Gr~s d'Annot synthetic three-dimensional seismic model is outcrops. Puigdeffibregas et al. reconstruct the used to analyse the seismic signature of different complex palaeotopography of the onlap surface sedimentary architectures, and to test seismic in both the Annot and Chalufy areas, which interpretation of comparable subsurface reser- belonged during Oligocene times to a common voirs. The main shaly permeability barriers outer basin margin (St Antonin-Annot-Grand (sedimentary maximum flooding surfaces) are Coyer-Chalufy sub-basin; see Fig. 4). The detected, and the limits of the main sand-bodies authors discuss the origin of soft-sediment defor- ('reservoir zones') are identified on amplitude mation ('slumps') and muddy 'debrites' that are time slices, but advanced seismic processing associated with the onlap surface: the sudden (migration, impedance inversion, attribute arrival of coarse-grained high-density turbidity analysis) seems necessary to derive confident currents onto the basin-flank slope would quantitative information on the small-scale create sub-horizontal injection and de-lamina- architectural heterogeneity. tion of previous deposits by overpressure, and their entrainment as overturned beds ('slumps'). In agreement with Kneller & McCaffrey (1999), this phenomenon may explain the common Subsurface analogues occurrence close to the palaeoslope of chaotic 'debrites' intercalated within single turbidite Outcrop analogues are increasingly frequently sandstone beds ('tri-partite' beds). used to help in the modelling of subsurface Using the same Chalufy exposures, Smith & deep-water oil and gas fields, where limited Joseph test a simple geometric model reprodu- information on sedimentology and small-scale cing the onlap pattern of the Gr~s d'Annot on architecture is available because of the limits of the Marnes Bleues palaeoslope. Two end- well coverage and seismic resolution. Using an members are predicted depending on the ratio example of a Brazilian Cretaceous oil field, of coeval slope to basinal aggradation rate, Moraes et ai. discuss the selection criteria for which is related to the volume of the turbidity relevant use of such outcrop analogues. At the flows and their sand/shale ratios: 'pure' abrupt reservoir scale, the first-order control parameters onlap occurs when sand-rich flows deposited seem to be the palaeotopography and the geo- sandstone beds with no or limited slope drapes metrical characteristics of the confining conduits (no slope aggradation); feathered' aggradational (rather than the tectonic context at a larger scale: onlap occurs when mud-rich flows deposited for example, active versus passive margins); the sandstone beds that interfingered with muddy second-order control parameters are the grain slope drapes (contemporaneous slope aggrada- size and the sand/mud ratio of the sediment tion). The cyclicity of alternating sand-rich and input, which influence the nature of the gravity sand-poor packets results in a stepped climbing flows, and thus the depositional geometries and trajectory of the diachronous onlap surface. In their patterns of heterogeneity. subsurface cases, the two end-members may or Subsurface modelling may benefit from the may not be resolved depending on the frequency quantitative parameters derived from the outcrop content of available seismic data: the two end- studies (such as channel dimensions, extent of member cases lead to very different geometrical shale breaks, facies continuity quantified by Downloaded from http://sp.lyellcollection.org/ by guest on September 29, 2021

14 P. JOSEPH & S. A. LOMAS correlation lengths), but the use of these statistics framework. A consistent depositional model of a must be based on the recognition of the similarity fan-delta-fed turbidite submarine ramp, differing of the sedimentary processes acting in the outcrop from the classic radial fan model, is now proposed, and subsurface cases. even if further research is needed to clarify many of the details, and to ascertain the significance of poorly-studied areas. In addition, this volume New perspectives on applications as highlights some exciting new avenues for research subsurface analogues (three-dimensional process modelling; three- dimensional coupled structural and stratigraphic An integrated approach is developing for the modelling; seismic modelling; chemostratigraphy; study of deep-water outcrops that serve as ana- geochemistry; sedimentological data quantifica- logues for subsurface fields (see examples in the tion) that may help to better understand the GCSSEPM 2000 conference volume, Weimer large- and small-scale architecture of sand-rich et al. 2000). Thanks to rapid progress in the deep-water confined systems, and provide some development of geomodelling software tools, predictive keys for better modelling of analogous three-dimensional models can be constructed, subsurface systems. displaying sedimentary body architecture and facies distribution in three dimensions. These The authors would like to thank E. Albouy, A. Mascle models may be used as test cases for seismic and J. Turner for their very helpful comments and suggestions on the manuscript. or fluid flow modelling, to identify the seismic and dynamic signature of specific sedimentary architectures and to test their sensitivity ranges. References Parallel development of three-dimensional tools for the numerical simulation of sedimentary Avvs, G. M. 1985. The Grbs d'Annot foreland processes provides a better understanding of basin, Haute Provence: the control of turbidite the relationships between gravity flow processes deposition by structurally induced basin floor and the resulting facies. A logical next step topography. 6th European Regional Meeting of would involve a comparison between high-reso- Sedimentology IA S Lleida, 18-21. lution seismic surveys on recent deep-marine Avvs, G. M. 1987. Evolution of the Grks d'Annot Basin, systems (providing detailed images of horizontal South West . Ph.D. thesis, University of organization) and comparable outcrop studies Liverpool, UK. BEAUDOIN, B., CAMPREDON, R., COTILLON,P. & GIGOT, (giving details of internal organization and verti- P. 1975. Alpes mbridionales frangaises-reconstitu- cal evolution). tion du bassin de s~dimentation. IX ~ Congrbs International de S~dimentologie. BERGGREN, W. A., KENT D. V., SWISHER, C. C. & Concluding remarks AVBV,¥, M. P. 1995. A Revised Cenozoic Geochro- nology and Chronostratigraphy. SEPM Special The Gr6s d'Annot basin is the birthplace of Publications, Tulsa, 54, 129-212. major developments in the study of deep- BOUMA, A. H. 1962. Sedimentology of some flysch marine sedimentation (recognition of turbidites deposits: a graphic approach to facies interpreta- by Kuenen; Bouma sequence for low-density tion. Elsevier Publ. 6. turbidites; Stanley's model of canyon and fan BOUMA, A. H. & COLEMAY,J. M. 1985. Peira Cava Tur- bidite System, France. In: BOUMAA. H., NORMARK valley) and a classic area for field work and W. R. & BARNESN. E. (eds) Submarine Fans and courses on gravity flow deposits. Related Turbidite Systems. Springer, New York, The scale and outstanding quality of the expo- 217-222. sures makes this region an excellent natural BotJssAc, J. 1912. Etudes stratigraphiques sur le laboratory in which to study the interaction Nummulitique alpin, M~m. Carte G~ol. France. between foreland basin evolution and deep- BRGM. 1996. Carte g6ologique de la France au marine sedimentation, on both regional and local 1:1 000000, Bureau de Recherches G6ologiques scales. Recent research presented in this volume et Mini6res, Service G6ologique National, provides novel ideas on the correlation between Orl+ans. sub-basins, their relative timing of filling, the CALLEC, Y. 2001. La d~formation syns~dimentaire des bassins palOogknes de l'Arc de Castellane ( Annot, nature of gravity flow processes and their impact Barrdme, St Antonin). Thkse de l'Ecole des Mines on facies distributions, the relative frequency of de Paris. tectonic activity, and the interaction between CLARK, J. D. & GARDINER, A. R. 2000. Outcrop ana- topography, tectonic deformation, eustatic sea- logues for deep-water channel and levee genetic level changes and variations of sediment supply, units from the Gr+s d'Annot turbidite system, SE in a better-constrained chronostratigraphic France. In: WEIMER,P., SLAXX, R. M. et al. (eds). Downloaded from http://sp.lyellcollection.org/ by guest on September 29, 2021

NEW PERSPECTIVES ON THE GRI~S D'ANNOT 15

Deep- Water Reservoirs of the WorM. Proceedings KNELLER, B. C. & MCCAFFREY, W. D. 1999. Deposi- of the GCSSEPM Foundation 20th Annual tional effects of flow nonuniformity and stratifica- Research Conference, 3-6 December 2000, tion within turbidity currents approaching a Houston, Texas. SEPM CD-ROM Special Publi- bounding slope: deflection, reflection, and facies cation, 28, 175-190. variation. Journal of Sedimentary Research, 69, ELLIOTT, T., APPS, G., DAVIES, H., EVANS, M., 980-991. GHmAUDO, G. & GRAHAM, R. H. 1985. A struc- KUENEN, P. H., FAURE-MURET, A., LANTEAUME,M. & tural and sedimentological traverse through the FALLOT, P. 1957. Observations sur les Flyschs Tertiary foreland basin of the external Alps of des Alpes Maritimes frangaises et italiennes. south-east France. In: ALLEN, P. A. , HOMEWOOD, Bulletin de la Socidtd G~ologique de France, P. & WILLIAM, G. (eds) International Symposium 6(VII), 4--26. on .foreland Basins, Excursion Guidebook, LANTEAUME, M., BEAUDOIN,B. • CAMPREDON, R. 1967. Fribourg, International Association of Sedimen- Figures s+dimentaires du Flysch 'Gr& d'Annot' tologists, 39-73. du synclinal de Peira Cava. CNRS ed., Paris FAURE-MURET, A., KUENEN, PH., LANTEAUME, M. & 99 p. FALLOT, P. 1956. Sur les flyschs des Alpes- LAVAL, A., CREMER, M., BEGHIN, P. & RAVENNE, C. Maritimes Frangaises et Italiennes. Comptes 1988. Density surges: two-dimensional experi- Rendus de l'Acaddmie des Sciences, Paris, 243, ments. Sedimentology, 35, 73-84. 1697-1701. LOMAS, S. A., CRONIN, B. T. et al. 2000. Characteriza- FORD, M., LICKORISH, W. H. & KUZNIR, N. 1999. tion of lateral heterogeneities in an exceptionally Tertiary foreland sedimentation in the southern exposed turbidite sand body, Gr6s d'Annot Subalpine chains, SE France: a geodynamic analy- (Eocene-Oligocene), SE France. In: WEIMER, P., sis. Basin Research, 11, 315-336. SLATT, R.M. et al. (eds). Deep-Water Reservoirs GERVAIS, A., SAVOYE, B., PIPER, D. J. W., MULDER, T., of the World: Proceedings of the GCSSEPM Foun- CREMER, M. & PICHEVIN, L. 2004. Present mor- dation 20th Annual Research Conference, 3-6 phology and depositional architecture of a sandy December 2000, Houston, Texas. SEPM Special confined submarine system: the Golo turbidite Publication, 28, 502-514. system, Eastern Margin of Corsica. In: LOMAS, MARTINI, E. 1971. Standard Tertiary and Quaternary S. A. & JOSEPH, P. (eds) Confined Turbidite calcareous nannoplankton zonation. Proc. 2nd Systems. Geological Society, London, Special Planktonic Conference (Roma, 1970), Technos- Publications, 222, in press. cienza ed., 2, 739-785. JEAN, S. 1985. Les Grbs d'Annot au NW du massif de MITCHUM JR., R. M. & VAN WAGONER, J. C. 1991. l'Argentera Mercantour. 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16 P. JOSEPH & S. A. LOMAS

PICKERING, K. T. & HILTON, V. C. 1998. Turbidite SINCLAIR, H. D. 2000. Delta-fed turbidites infilling topo- systems of Southeast France. Vallis Press, London. graphically complex basins: a new depositional PRATHER, B. E., BOOTH, J. R., STEFFENS,G. S. & CRAIG, model for the Annot Sandstones, SE France. P. A. 1998. Classification, lithologic calibration, Journal of Sedimentary Research, 70(3), 504-519. and stratigraphic succession of seismic facies of STANLEY, D. J. 1961. Etudes s~dimentologiques des Grbs intraslope basins, deep-water Gulf of Mexico. d'Annot et leurs Oquivalents lat~raux. Th6se d'~tat, AAPG Bulletin, 82, 701 728. Universit6 de Grenoble. RAVENNE, C., VIALLY, R., RICHLY,P. ~¢ TRI~MOLII~RES,P. STANLEY, D. J. 1975. Submarine canyon and slope sedi- 1987. S6dimentation et tectonique dans le bassin mentation (Gr6s d'Annot) in the French Maritime matin Eocene supbrieur-Oligoc~ne des Alpes du Alps, Proceedings of the IX International Congress Sud. Revue de I'IFP, 42(5), 529 553. on Sedimentology, Nice. READING, H. G. & RICHARDS, M. 1994. Turbidite STANLEY, D. J. 1980. The St-Antonin conglomerate systems in deep-water basin margins classified by in the : A model for coarse sedi- grain size and feeder system. AAPG Bulletin, 78, mentation on a submarine slope. Smithsonian 792-822. Contributions to the Marine Sciences, 5. SERANNE, M. 1999. The Gulf of Lion continental VIALLY, R. 1994. The Southern French Alps Paleogene margin (NW Mediterranean) revisited by IBS: Basin: Subsidence modelling and geodynamic An overview. In: DURAND, B., JOLIVET, L., implication. In: MASCLE A. (ed.) Hydrocarbon HORVATH, F. & SI~RANNE,M. (eds) The Mediterra- and Petroleum Geology of France. EAPG nean Basins. Tertiary Extension within the Alpine Memoir, 4, 281-293. Orogen. Geological Society, London, Special WEtMER, P., SLATT, R. M. et al. (eds). 2000. Deep-Water Publication, 156, 15 36. Reservoirs of the World. GCSSEPM Foundation SINCLAIR, H. O. 1993. High resolution stratigraphy 20th Annual Research Conference, 3-6 December and facies differentiation of the shallow marine 2000, Houston, Texas. SEPM CD-ROM Special Annot Sandstones of SE France. Sedimentology, Publication, 28. 40, 955-978. WINKER, C. D. 1996. High-resolution seismic stratigra- SINCLAIR, H. D. 1997. Tectonostratigraphic model phy of a late Pleistocene submarine fan ponded by for underfilled peripheral foreland basins: an salt-withdrawal mini-basins on the Gulf of Mexico Alpine perspective. Geological Society of America continental slope. Offshore Technology Conference Bulletin, 109, 324-346. Proceedings, 619-628.