Open Access
BSGF - Earth Sci. Bull.
Volume 194, 2023
Article Number 13
Number of page(s) 26
Published online 26 October 2023

© J. Michel et al., Published by EDP Sciences 2023

Licence Creative CommonsThis is an Open Access article distributed under the terms of the Creative Commons Attribution License (, which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.

1 Introduction

“In the general field of stratigraphy and sedimentology, a facies model could be defined as a general summary of a particular depositional system involving many studies in both ancient rocks and recent sediments” (Walker, 1967, 1992) that is set up to compare, frame and interpret sedimentary systems. Facies models are used as a priori knowledge and conceptual tools to correlate outcrops and wells with the ultimate goal of predicting the complete sedimentary system. Facies models and correlations are based on stacking patterns, which are founded on the Walther’s law and sequence stratigraphy. In this context, it becomes logical to use depositional profiles as a chronostratigraphic means of spatial correlation of facies successions. Geologists working on inter-well stratigraphic correlations are constantly dealing with these questions (e.g. van Buchem et al., 2002; Borgomano et al., 2008; Pomar et al., 2015). Carbonate facies models are, by definition, conceptual and rarely based upon laterally continuous observations of ancient sedimentary records. Facies model definition from the coastline to the basin is based on palaeoenvironmental interpretations of incomplete dataset that are not physically correlated. Only a few examples of seismic-scale continuous outcrops provide in-depth understanding of facies spatial organization, belts, transitions and stratigraphic architecture over large distances exceeding the tens-of-kilometers (e.g. Cretaceous: Istria in Croatia, Maiella in Italy, Vercors in France and Maestrat in Spain: Tišljar et al., 1998; Stössel, 1999; Richet, 2011; Richet et al., 2011; Gili et al., 2016). Such exceptional outcrops could be used as a direct analogue of comparable size subsurface systems, but detailed, continuous facies observations over such distances are not frequent practice. Apart from these few exceptional case studies, outcrops are non-continuous and/or of a limited extent in comparison to tens-of-kilometer-wide Cretaceous platform systems (e.g. Everts et al., 1995; Bover-Arnal et al., 2009; Léonide et al., 2012). As a result, data integration of these punctual, spatially limited outcrops into larger-scale analogues must be undertaken with care. Every facies model results from interpretations, interpolations and extrapolations based on a priori knowledge and hypotheses that require genuine scientific validation loops (e.g. Borgomano et al., 2020). These facts imply that, in a strict sense, a data-based definition of a facies model is not directly feasible.

In the case of Early Cretaceous carbonate platforms, determination and correlation of synchronous strata relies on interpretations from oil field observations (e.g. Yose et al., 2006), relative and absolute dating (e.g. Clavel et al., 2014; Godet et al., 2016; Frau et al., 2018; Frau et al., 2020; Brigaud et al., 2020; Frau et al., 2021), and/or stacking patterns (e.g. Godet et al., 2010; Ferry and Grosheny, 2019). All these elements are integrated within a conceptual sedimentological, palaeoecological and diagenetic model, which is supported by fundamental and deterministic sedimentological and paleontological concepts (Wilson, 1975; Tucker and Wright, 1990; Schlager, 2005). Facies models are therefore based on a large array of data and techniques that all imply uncertainties and a large interpretative part starting with facies definition (cf. Lokier et al., 2016). Consequently, different facies models can be defined depending on interpreters from a given set of data. In turn, different facies models can lead to contrasting sequence stratigraphic interpretations and stratigraphic correlations (e.g. Borgomano et al., 2008; Lallier et al., 2016; Edwards et al., 2018).

There is hardly any doubt that workflows of facies model definition must explicitly show supporting background data, concepts, hypotheses and uncertainties in order to be shared, used and be able to evolve. While these tasks might appear relatively straightforward in theory, providing explicit geological background information and uncertainties remain challenging. The present study aims at analyzing the evolution of a facies model, documenting supporting data and concepts, and exploring a methodological workflow to establish a well-supported facies model. The well-studied Urgonian carbonate platform of SE France and Switzerland are used to tackle these objectives. This analytical method could have implications for sedimentological and stratigraphic studies of Middle East Cretaceous carbonates, as the Urgonian platform is retained as a valid analog (Borgomano et al., 2008, 2013; Massonnat et al., 2017).

For more than a century, and still ongoing today, numerous works have collected facies and palaeontological data leading to diverse conceptual models of the peri-Vocontian Urgonian platform (from d’Orbigny, 1850, to Frau et al., 2021). This great deal of effort has led to improving the overall knowledge and understanding of Lower Cretaceous carbonate systems. From an exhaustive literature review, we synthetise and classify the available data that support the interpretation of the published facies models (cf. Sect. 4). The data integration aims at unifying the diverse published facies tables and theoretical depositional profiles; and ultimately at defining a harmonised facies model, which can be used by everyone independently from research focus and approach. The facies model definition follows the approach of “infrastructure of carbonate platform” defined by Handford and Loucks (1993), which has the advantage of relating data and concepts to the controlling parameters of carbonate sedimentation at specific spatial scales. The synthetic facies table and model thus show a consistent continuum across all space and time scales, and propose quantifications that allow straightforward evaluation, criticism, validation and improvements (cf. Sect. 5). The facies model design will enable a direct comparison with other peri-Tethyan carbonate platforms and stratigraphic correlations. The model also provides data input for numerical models to challenge stratigraphic correlation hypotheses (both process- and geostatic-based modelling).

2 Geological and geographical settings

During the Barremian–Aptian period, carbonate platforms record a large development with an estimated extension of 4.63 or 10–22 · 106 km2 along the Tethyan margins (Philip, 2003; Pohl et al., 2020, respectively). Most carbonate platforms are characterised by the presence of rudists and benthic foraminifera associated with tropical palaeoenvironments (Douvillé, 1900; Rat, 1983; Gili and Götz, 2018). Rudists are considered to thrive in the neritic domain, under a tropical palaeoclimate and within shallow waters (Gili et al., 1995). The relatively symmetrical palaeolatitudinal distribution of biota between 35° N and 35° S is controlled by palaeoclimatic and palaeoceanographic parameters (Kiessling et al., 2003; Steuber et al., 2005; Pohl et al., 2019). In the Lower Cretaceous, rudist assemblages of the Tethyan domain exhibit contrasting palaeobiogeographies with two main provinces, namely (1) the northern Tethyan margin (European Province) and (2) the southern Tethyan margin (Arab-African Province: Masse, 1992; Masse and Fenerci-Masse, 2008; Skelton and Gili, 2012). Each province hosts specific genera and species that differ in time and space (Hughes, 1997; Skelton, 2003; Skelton and Gili, 2012; Masse and Fenerci-Masse, 2008, 2015; Masse et al., 2020, 2022). Rudist families, however, are the same along both margins and include Caprinidae, Requieniidae, Monopleuridae and Radiolitidae. In addition to paleontological attributes, both provinces exhibit carbonate facies analogies in terms of sedimentology and rock fabrics (Borgomano et al., 2013).

In the present study, we focus on the Urgonian type platform of SE France and Switzerland. The term Urgonian herein refers to the depositional facies terminology defined by Masse (1966, 1976; also cf. Rat, 1983; Clavel et al., 2014) with “Urgonian sensu stricto” designating the rudist facies that are embedded vertically and laterally within the “Urgonian sensu lato” corresponding to the bioclastic limestones. The studied chronostratigraphic interval corresponds to the Barremian and Lower Aptian, according to the recent age reappraisal of Frau et al. (2018, 2021). The facies model results from the bibliographic synthesis of outcrop data stemming from the present-day Jura Chain and Helvetic Mountains to the North, the Mont d’Ardèche to the West, the Monts de Vaucluse and Calanques to the South, and the Verdon and the Alps to the East (Fig. 1). This area hosts the key localities of the Urgonian Jura–Subalpine platform to the North, the Bas-Vivarais platform to the west and the Provence platform to the South. Together, these platforms define the peri-Vocontian domain. Sediments deposited in the Vocontian Basin sensu stricto are not considered here. The basinal facies, which are disconnected from the platform, correspond to “pre-Vocontian” settings (sensu Frau et al., 2018; Tendil et al., 2018).

thumbnail Fig. 1

Upper Barremian (M. Sarasini ammonite zone sensu Frau et al., 2018) palaeogeography reconstruction of SE France (modified from Tendil et al., 2018).

3 Methods and semantics

In general, a facies model is built by geologists to organize and extrapolate sedimentary data in space and time (Wilson, 1975; Walker, 1992). The model helps the interpretation of limited and incomplete sedimentary records and estimates the controlling parameters of sedimentation, allowing for depositional environment analyses and prediction. Based on the works of Walker (1992) and Argenio et al. (1997), a facies is herein defined as a volume of rock distinguished upon physical characteristics such as color, texture, components and sedimentary structures. A facies is a product of a specific depositional environment and may have an early diagenetic overprint, which is not the object of the present study. However, the palaeoenvironmental interpretation of facies is not necessarily unequivocal. In order to establish its depositional framework, a facies is generally framed into a facies association (sensu Walker, 1992; Argenio et al., 1997). A facies association corresponds to a genetically-related group of facies deposited together within a bedding interval or a depositional sequence (Collinson, 1969; Reading, 1996).

Here, the construction of the conceptual facies model is based on an exhaustive compilation of bibliographic data about Lower Cretaceous, Barremian–Aptian outcrops from SE France and Switzerland. This compilation first extracts supporting data of facies models only from studies that published a facies model representation and then labels each of them according to geographic area, age, model classification and scientific school. The bibliographic database allows synthesising the evolution of scientific approaches used by different academic teams (e.g. Grenoble, Lausanne, Lyon, Marseille and Neuchâtel) and resulting facies models of the Urgonian platform from Jura, Vercors and Provence (Figs. 2 and 4).

To build a constrained and consistent conceptual facies model, we propose a formal reproducible workflow that is based on the following four steps: (1) an exhaustive bibliographic review to extract the published data (e.g. sedimentary, chronostratigraphic and palaeoecological data) and concepts (e.g. facies belt organization, morphology of platform and carbonate factory) that support the facies model; (2) the standardisation of the various depositional facies data in a systematic and consistent way; (3) the definition of facies associations and controlling parameters for each facies association (palaeobathymetry and hydraulic energy); (4) the creation of a facies association table and a conceptual facies model. Iteration between the different steps should guarantee a great consistency between data and model. The table and model of depositional facies are based on the approach described by Handford and Loucks (1993) that realizes an infrastructure of carbonate platform elements from overall geometry or grain association of deposits to unitary facies. This approach aims at bridging the different scales of study of the carbonate system into a consistent and reproducible way. Supporting data of the facies model are thoroughly reported for each spatial scale and include outcrop locations within the interpreted palaeogeographic map, facies transition observations, temporal and spatial resolution of interpreted synchronous strata and concepts.

thumbnail Fig. 2

Synthesis of the main works on the Urgonian in SE France and evolution of facies models. The color key for the depositional facies corresponds to that of the Figure 3.

thumbnail Fig. 3

Conceptual facies model of the Urgonian platform (modified from Masse and Fenerci-Masse, 2011; Tendil, 2018). The blue curve qualitatively describes hydrodynamic trends of facies deposition.

4 Literature review of the peri-Vocontian Urgonian facies models

The historical evolution of Urgonian facies models is intrinsically linked to major outcrop surveys in different regions (i.e. Jura, Vercors and Provence) executed by different academic teams (Grenoble, Lausanne, Marseille and Neuchâtel: Fig. 2; see Rat, 1983; Clavel et al., 2014). These works match the evolution of concepts that influenced the construction of the different facies models (Fig. 4).

4.1 Chronology of published depositional profiles and facies models

The peri-Vocontian Urgonian limestones went through several phases in the definition of sedimentary profiles (cf. Masse, 1992; Fig. 4): (a) pioneer works dealt with palaeogeographic occurrences of rudist and orbitolinid fossils before considering any geological model (Figs. 2 and 4); (b) these biota occurrences were then related to bio-sedimentary assemblages using actualism and following the definition of Pérès and Picard (1964, and references therein; Fig. 4); (c) in continuation, these bio-sedimentary associations were considered within a broader palaeoenvironmental context (e.g. palaeobiogeographic approach); (d) at this step only, sedimentary facies were described and associated to depositional palaeoenvironments in a spatial representation (Arnaud-Vanneau and Arnaud, 1976; Arnaud-Vanneau, 1979, Figs. 2a2c).

4.1.1 Facies model of Arnaud-Vanneau and Arnaud (1976)

The original Urgonian facies models were based on the Vercors platform. The interpreted sedimentary and palaeotopographic profiles were produced directly from the palaeontological and sedimentological correlations of putative contemporaneous depositional facies maps (Tab. 1).

  • a Lower Barremian facies model describes an isolated platform high that is surrounded by two asymmetric slopes on both sides of the sedimentary profile (“shoal” or “haut-fond” model; Fig. 2a and Tab. 1). Ooid shoals with a mixture of bioclastic facies represent the shallowest facies association on the platform top. Coarser-grained facies including few coral facies occur on the interpreted windward side of the isolated platform high (i.e. Vocontian Basin, oceanic side), while finer and muddier facies are located on the interpreted leeward side (i.e. Jura, continental side). Bioclastic and very fine-grained bioclastic facies are shown on both interpreted steep and gentle slopes that reach basinal clay-rich deposits;

  • an Upper Barremian facies model defines an attached platform (“platform” model; Fig. 2b and Tab. 1). Contemporaneous depositional facies include from the shallower to the deeper uncommon supratidal charophyte-rich marls, rudist and oncoidal facies, lagoonal muddy and sandy facies, coral facies at the margin, bioclastic facies on the slope and deeper micritic facies;

  • Orbitolinid-rich platform (Lower Orbitolina beds, Ai1 sequence) and depressions (Upper Orbitolina beds; top Ai2 sequence) represent specific, non-contemporaneous depositional environments that relate with periods of terrigenous influx. Neither the orbitolinid facies nor the marly and orbitolinid-rich platform are shown in the facies models.

Table 1

Comparison of bibliographic data supporting published Urgonian facies models. If not specifically mentioned, cited figures refer to the reference paper. See text and Section 5.5 for related comments and localities, respectively.

4.1.2 Facies model of Arnaud-Vanneau (1979)

The integration of the two above mentioned palaeogeographic map-based models and the terrigenous-related “Upper Orbitolina bed” leads to the definition of a new conceptual facies model for the Urgonian limestones (Fig. 2c and Tab. 1). The conceptual facies model is based on the definition of specific paleoenvironments along the platform profile and is supported by biotic and foraminiferal association analyses. The model does not correspond to any contemporaneous sedimentary profile as it merges models defined for different time intervals (Lower Barremian, Upper Barremian and Lower Aptian; cf. above).

Orbitolinid marly facies are recorded over large areas of the platform and within channels (cf. Arnaud-Vanneau, 1979, 1980) during specific terrigenous-influenced periods (Lower Orbitolina Bed within the Ai1 sequence and Upper Orbitolina Bed at the top of Ai2 sequence, respectively). The new conceptual model only integrates the channelised facies of the Upper Orbitolinia Bed.

4.1.3 Facies model of Arnaud-Vanneau et al. (1982)

A new Urgonian facies model of a large spatial and temporal extent is defined integrating observations of different sedimentological schools from the Valanginian to Lower Aptian from different peri-Vocontian platforms in SE France (Fig. 2d and Tab. 1). The proposed conceptual facies model is based upon regional palaeogeographic maps. Little detail is provided about the facies model in the publication. The proposed facies model is very similar to the previously published models and shows the organization of the main theoretical facies belts of an attached platform.

The model includes orbitolinid facies within channels cutting through the main facies belts, while most orbitolinid facies are found during specific terrigenous-influenced periods (“Lower and Upper Orbitolina Beds”; cf. above). Corals and ooids are shown as contemporaneous sediments that are deposited next to each other both along dip and along strike. Such a spatial organization was not characteristically observed in the Vercors facies maps of Arnaud-Vanneau and Arnaud (1976; cf. above).

4.1.4 Facies model of Arnaud-Vanneau et al. (1987)

This conceptual facies model is defined for the Lower Cretaceous of SE France and strictly corresponds to the model published previously by Arnaud-Vanneau (1979; cf. above; Fig. 2e and Tab. 1). No data is provided about the facies model in the publication, but details about typical characteristics of Urgonian limestones. A novel approach is introduced using sequence stratigraphic concepts; the lateral facies succession along dip is related to vertical log succession, which allows for direct interpretation in terms of sea-level changes. Such a facies model definition “allows interpreting temporal (vertical) succession of interpreted palaeoenvironments (microfacies) using the Walther’s law in order to recognize main discontinuities in a sequence stratigraphic framework” (Wermeille, 1996).

In terms of facies distribution, corals and ooids are not laterally contemporaneous as in the 1982 model but along dip (cf. Sect. 4.1.3). Coral facies association corresponds to the infralittoral palaeoenvironment (i.e. euphotic to mesophotic). While the ooid facies association belongs to the same shelf margin zone as the coral facies association, the ooid facies association, by contrast to Arnaud-Vanneau (1979), is placed together with the bioclastic facies association into the circalittoral zone (i.e. oligophotic to aphotic; cf. Stein et al., 2012; Bastide, 2014). Orbitolinid facies are not mentioned in the sedimentary profile, which follows observed depositional facies maps (cf. Arnaud-Vanneau and Arnaud, 1976), but not the conceptual facies model of Arnaud-Vanneau (1979; cf. above).

4.1.5 Facies model of Bodin (2006) and Bodin et al. (2006)

The definition of the facies models is based on palaeoecological concepts (Tab. 1). Two different, exclusive facies models were defined for the Lower Cretaceous interval of the Helvetic realm based on the recognition of different platform-scale grain associations or carbonate factories, which are controlled by specific oceanographic parameters (e.g. Föllmi et al., 1994; James, 1997; Schlager, 2003; Fig. 2f). Model occurrence is related with the trophic conditions of the waters at a given period (e.g. Föllmi and Godet, 2013). A photozoan, distally-steepened ramp is promoted by oligotrophic conditions, while a heterozoan, homoclinal ramp developed during mesotrophic periods. The photozoan facies model refers to the model published by Arnaud-Vanneau (1980) and Arnaud-Vanneau et al. (1982; cf. above); a supplementary algal mat facies occur at the side of the emersive facies. The new Urgonian heterozoan facies model is only composed of heterotrophic biota (e.g. crinoids, bryozoans and sponges) plus oolitic deposits. The palaeotopographic profile of these models is conceptual and results from interpretation of facies belt organization and open versus restricted oceanic biota.

4.1.6 Facies model of Godet et al. (2010)

The facies model is related with palaeotopographic characteristics, which are nevertheless speculative (Tab. 1). The rimmed-shelf model, which implies reefal slopes both seawards and shorewards, is not supported by any observation, as it is purely conceptual by referring to the classification of Pomar (2001) and based on coral-reef-barrier actualism (cf. Arnaud-Vanneau and Arnaud, 2005; Godet et al., 2016). In earlier publications of the Urgonian facies model, such rim interpretation is never mentioned in the text, only small coral patch reefs and ooid shoals are referred to as constituents of the platform margin, and the term “lagoon” is used in a general sense for inner platform facies of carbonate platforms (e.g. Arnaud-Vanneau et al., 1987). It is noteworthy that the topographic rim has no impact on the proximal-distal and associated sea-level-based sequence stratigraphic interpretation, and that this rimmed-shelf model will be abandoned in later studies from the same academic teams (e.g. Bonvallet, 2015; Bonvallet et al., 2019).

In terms of sequence stratigraphy, microfacies types of the conceptual facies model are used to define the main transgressive and regressive trends. A “facies of transgression” is hence described to characterise the main transgressive phases (also cf. Blanc Aletru, 1995). This “facies of transgression” is not included into the general facies model, but in the sedimentary profile used as a basis of sequence stratigraphic analyses. Thus, such depositional facies and facies model definitions do not refer to specific palaeoecological interpretation at a given time but include processes through time and is directly tied to sequence stratigraphic interpretation.

4.1.7 Facies model of Masse and Fenerci-Masse (2011)

The facies model is defined using palaeogeographic Cretaceous maps of depositional facies, palaeontological studies mostly from Provence (Masse, 1976, 1993; Masse and Philip, 1981), and integrating the Vercors model by Arnaud-Vanneau (1980; cf. above; Fig. 2g and Tab. 1). Facies belt transitions are not directly observed. Beyond palaeogeographic arguments (Masse and Philip, 1981; Masse, 1993), palaeontological and sedimentary facies compositions are interpreted in terms of both hydrodynamics and light-related zoning along a proximal-distal transect (i.e. infralittoral vs. circalittoral; cf. Pérès and Picard, 1964; Masse and Philip, 1981). For instance, occurrence of abundant miliolids and medium grain size (i.e. muddy sand) relates the rudist facies association with the inner platform, in which small requieniid rudist facies are interpreted as more proximal than large requieniid and caprinid rudist facies. No palaeobathymetry is assigned to specific depositional facies. Instead, a shallow platform top (including an inner and outer domain; < 30 m water depth) and a deep circalittoral (i.e. subtidal oligo- to aphotic) palaeoenvironment are defined. The “platform model” (i.e. non-rimmed, flat-topped platform) implies a significant palaeotopographic and/or environmental change at the platform break that is not directly observed on the field. Orbitolinid facies are here considered as either deep-water facies (not always occurring over the platform profile; Provence) or a specific, transient, ramp model (Vercors).

This facies model was applied on continuous outcrops (Richet et al., 2011; Léonide et al., 2012; Frau et al., 2021) and its chronostratigraphic framework was recently modified and refined (Frau et al., 2017, 2018; Tendil et al., 2018).

4.1.8 Facies model of Quesne, Bénard, Ferry and Grosheny

A different model was defined showing two non-contemporaneous facies models based on sea-level contexts (Quesne, 1998; Quesne and Bénard, 2006; Ferry and Grosheny, 2019). A rudist and marly facies model occur during periods of high sea level, while a bioclastic facies model is deposited during times of low sea level. This model is not further investigated here because no facies model definition and representation are provided beyond stratigraphic trends. To be noted that this non-contemporaneous model is in contradiction with the harmonised facies model of the present study.

4.2 Summary and classification of published facies models

4.2.1 General notes about published facies models

Palaeogeographic mapping of synchronous stratigraphic units was the foundations of the facies models of Urgonian platforms from SE France and Switzerland (cf. Arnaud-Vanneau and Arnaud, 1976; Masse and Philip, 1981; Arnaud-Vanneau et al., 1982). The continuous lateral facies transition exhibited by models is not observed, but instead are the results of interpolations of distant stratigraphic log sections along pluri-kilometer-scale transects and showing temporal resolutions of ca. 0.5–1 Ma. These deterministic approaches strongly rely on sedimentological concepts and hypothetical principles, which are generally inspired from modern carbonate environments such as the Bahamas archetype (e.g. Ginsburg, 1956; Tucker and Wright, 1990). Additional applied basics include fundamental palaeontological and sedimentological interpretation of rudists and foraminifera, grain-size and hydrodynamic relationships (e.g. Wilson, 1975; Immenhauser, 2009). In this context, the ecological classification of bathymetric intervals of Pérès and Picard (1964), which comes from the modern, warm-temperate Mediterranean Sea is a seminal contribution (also cf. Betzler et al., 1997). Later facies models directly used the above-cited, earlier palaeogeographic map-based models to interpret local depositional facies data in terms of either palaeobathymetric and/or proximal-distal trends. Consequently, the Urgonian facies models represent conceptual interpretations of stratal successions and correlations. In several cases, most key data supporting facies models come from earlier studies of the same authors that are not shown herein (Tab. 1).

Main differences between facies models are justified by the different conceptual approaches followed by authors (Fig. 4). The evolution of concepts about carbonate systems over the last century has influenced the definition of facies models. Improvement in depositional palaeoenvironment characterisation has forced diverse interpretative hypotheses about the palaeotopographic profile, the microfacies distribution along the palaeobathymetric profile and stacking pattern, the palaeoenvironmental influence on the carbonate factory and palaeontological successions.

The resulting facies belts of the models are overall closely similar to one another, not only showing a common origin but the consistency of sedimentary facies data across the entire peri-Vocontian region. Later studies, which observed lateral continuity of facies belt transitions over several kilometers, confirmed the general trends of Urgonian facies models (Bièvre and Quesne, 2004; Richet, 2011; Richet et al., 2011; Léonide et al., 2012; Frau et al., 2021). Two major differences between facies models, however, include the interpretative palaeoenvironmental setting of the orbitolinid facies and the interpretative palaeotopographic profile of ramp vs. flat-topped platform. The former point deals with different marly orbitolinid sediments, which are considered as either (i) proximal channelised structures in the Vercors (Arnaud-Vanneau, 1979; Arnaud-Vanneau et al., 1982), (ii) distal deposits in Provence (cf. Masse and Fenerci-Masse, 2011, Sect. 5.1.5; Tendil et al., 2018), or (iii) a distinct, terrigenous-influenced facies model such as the Lower Orbitolina beds in the Vercors and Helvetic Alps (Arnaud-Vanneau and Arnaud, 1976; Föllmi et al., 2006). The latter point of discrepancy about the palaeotopographic profile is critical for the interpretation of sea-level variations because the hypothesis of a flat-topped platform creates a dichotomy between proximal-distal vs. palaeobathymetric interpretation of facies associations (cf. Masse and Fenerci-Masse, 2011, Sect. 4). Platform-top facies showing the same or overlapping palaeobathymetric ranges do not allow for depositional facies change interpretation in terms of water-depth variation, and thus for the Walther’s law application.

4.2.2 Classification of conceptual approaches

The construction of the above-cited Urgonian facies models can be classified into three main approaches that are (1) topographic reconstruction, (2) microfacies succession and (3) depositional environment. Such a classification is deterministic and simplistic as these classes are neither independent nor exclusive. These approaches appear, however, to represent scientific evolution in facies model definition beyond the Urgonian realm (e.g. Middle East region). Facies zonation model following a standard topographic profile

This approach has been used in the Barremian–Aptian formations from the Middle East (e.g. Alsharhan, 1993; Hughes, 1997; Cantrell et al., 2014) and the Jura (Godet, 2006; Godet et al., 2010; see Sect. 4.1.6). It follows the work of Wilson (1975, Chapter XI) and is based on the analogy with modern reef-building corals at the origin of morphological reliefs on the seafloor (e.g. Arnaud-Vanneau and Arnaud, 2005). Following this “standard” platform profile, the rudists are considered as reef builders forming a barrier separating an internal (inner platform, lagoon, “shelf lagoon”) from an external domain (outer shelf). These shelf models imply a lagoonal depression with water depths in the order of 10 m (e.g. Alsharhan 1995; Godet et al., 2010). However, rudists were not shown to build up such morphological anomalies as it is the case for coral reefs (e.g. Gili et al., 1995; Quesne and Bénard, 2006). Outcrop and subsurface studies show instead that rudist limestones are deposited as extensive, tabular topographies without adjoining slope (Gili et al., 1995, 2016; Skelton and Gili, 2012; Skelton et al., 2019). Consequently, the relatively deep palaeobathymetric estimates of the sedimentary profile appear not to be supported by facies and palaeontological data. Model based on the definition of a standard microfacies lateral succession

This model, which was established from the end of the 80s by the Grenoble University and is based on the Vercors outcrops (e.g. Arnaud-Vanneau et al., 1987; Adatte et al., 2005; see Sect. 4.1.4), coincides with the onset of sequence stratigraphic concepts (Sarg, 1988; Jacquin et al., 1991; Handford and Loucks, 1993; Fig. 4). It has been mainly used for Urgonian limestones of the Jura–Subalpine domain (e.g. Adatte et al., 2005; Godet et al., 2010). In these models, interpretation of facies distribution is based upon the Modern Mediterranean ramp model of Pérès and Picard (1964). The facies and microfacies zonations are defined on a theoretical sedimentary profile by specific, exclusive palaeobathymetric ranges with a single polarity organizational trend from the coast to the basin. These models allow interpreting vertical successions of microfacies using the Walther’s law to define sedimentary discontinuities and stacking patterns within a sequence stratigraphic framework (e.g. Catuneanu et al., 2011; Pomar et al., 2015). Several studies have shown, however, some limitations of this approach on carbonate sedimentary systems; the distribution of depositional facies is a function of biocenosis and palaeoenvironment, and shows lateral changes within the same palaeobathymetric ranges (cf. Rankey, 2002; Wright and Burgess, 2005; Purkis et al., 2015, 2019; Pomar, 2020; Bover-Arnal et al., 2022). Facies zonation model based on palaeontological and palaeoecological interpretations

The facies distribution is based on palaeontological and palaeoenvironmental interpretations. These interpretations infer relative, non-exclusive palaeobathymetric ranges and positions along ecological successions from proximal/shallow to distal/deep waters of specific biota associations (cf. Masse, 1976, 1991). No quantification is provided. Palaeontological data offer a chronostratigraphic framework so that ecological successions can be related to contemporaneous sedimentary profile. This model distinguishes an infralittoral (euphotic/mesophotic) and circalittoral (oligophotic/aphotic) zone (cf. Pérès and Picard, 1964; Betzler et al., 1997). By contrast with the Modern warm-temperate Mediterranean model defined by Pérès and Picard (1964), the infralittoral zone contains the whole tropical platform top (e.g. Masse and Philip, 1981; Masse, 1991; Masse and Fenerci-Masse, 2011). Drowning discontinuities (sensu Schlager, 1981; Masse and Fenerci-Masse, 2011), which mark drastic carbonate production changes, define sequence boundaries and thus sedimentary sequences. The model ignores published sea-level curves. Chronostratigraphic resolution is then limited to correlation based on carbonate platform demise, biostratigraphy and isotopic chronostratigraphy.

The first, “topography-based approach” implies the use of a conceptual model of ramp vs. shelf that is not supported by available data. Moreover, sedimentary profile morphologies are still debated in many cases (e.g. Rosen and Taylor, 1990; McCall et al., 1994; Pomar et al., 2017). The second, “microfacies-based model” uses exclusive palaeobathymetric ranges that are not well constrained, and might lead to some interpretation pitfalls that are related with the concepts of facies mosaic and carbonate sequence stratigraphy (e.g. Purkis et al., 2015; Borgomano et al., 2020, respectively). In the present study, the third, “palaeontology-based approach” is followed because it represents the most descriptive method using well-defined, consistent palaeoecological and sedimentological concepts. In addition, this latter approach allows for evolution because lateral and vertical facies distributional scheme does not show a forced, unique facies succession.

5 Harmonised Urgonian carbonate facies model

5.1 General framework

In the following, published data of Urgonian facies models are harmonised into a synthetic conceptual facies model (Fig. 3). Data supporting each definition step of the facies model are documented from the broadest to the finest spatial scale following the infrastructure framework of Handford and Loucks (1993) to explicitly describe the interpreted controlling parameters of the sedimentary model (Tabs. 2 and 3). Only carbonates are analysed; siliciclastics such as turbiditic sandstones (e.g. Vocontian Basin; Parize et al., 2007) are not included.

The facies model is defined by a palaeoecological facies belt succession constrained at a given time as far as geological record and dating allow. This choice is driven by the fact that at any given time, only contemporaneous palaeoenvironmental conditions control the biota and grain distribution, not the evolution of palaeoenvironmental conditions through time. Thus, neither climate change nor sea-level context is considered in theory. In practice however, the temporal integration of “contemporaneous sedimentary records” potentially biases observed palaeoecological lateral successions (e.g. occurrence of emersive facies within a subtidal facies belt resulting from accommodation infill up to sea level).

thumbnail Fig. 4

Composite chronology of key scientific concepts applied to the Urgonian platform characterization (B). (A) The sedimentological concepts are associated with their main bibliographic references (inspired from Kenter et al., 2009).

Table 2

Infrastructure sensu Handford and Loucks (1993) of the Urgonian Platform and facies table.

Table 2


Table 3

Supporting concepts and related Urgonian data and methods used to define the proposed facies model.

5.2 Carbonate factory

Urgonian biotic association is consistently set into the broader context of tropical carbonates (Tab. 3). The determination of grain association is interpretative (cf. Kindler and Wilson, 2010) and a debate about the photozoan character of rudists remains (e.g. Gili et al., 1995; Skelton and Gili, 2012; Skelton, 2018; Pohl et al., 2019). At a platform scale however, rudist platforms are consistently placed into the photozoan grain association (sensu James, 1997) and the tropical carbonate factory (T-factory sensu Schlager, 2005; Michel et al., 2019). These platforms are thus interpreted to have developed in an oligotrophic, tropical palaeoceanographic context as witnessed by the coral patch belt that occupies the external parts of the platform (cf. Föllmi et al., 2006; Pohl et al., 2019; Michel et al., 2019). Accumulations of heterozoan grain associations, which are characterised by either (i) crinoids, bryozoans, brachiopods and siliceous sponges, or (ii) orbitolinids and detrital grains, are also described (Arnaud-Vanneau and Arnaud, 1976; Arnaud-Vanneau et al., 1982; Föllmi et al., 1994, 2006; Bodin, 2006; Michel et al., 2019). The differentiation of these grain associations led to the recognition of three exclusive Urgonian carbonate factories at the platform scale, namely the “photozoan rudist platform”, “heterozoan bryozoan-crinoid ramp” and “marly orbitolinid ramp”, which are diachronic and succeeded from one another through time as a result of palaeoceanographic changes (palaeotemperatures, nutrient concentrations and terrigenous influences; cf. Bodin, 2006; Föllmi et al., 2006; Masse and Fenerci-Masse, 2011).

5.3 Morphology of sedimentary profile

The main uncertainty of facies models lies in the palaeotopographic profile (cf. Pomar, 2001). Geological data poorly allow for the reconstruction of original angle of repose. Consequently, major discussions about the palaeobathymetry of carbonate platform margins are still ongoing (i.e. surface waves vs. fair-weather and storm wave bases vs. internal waves; Immenhauser, 2009; Peters and Loss, 2012; Pomar et al., 2012; Purkis et al., 2015; including the Urgonian platform; Masse and Fenerci-Masse, 2011; Fig. 5). The concept of T-factory for rudist platforms would imply a flat-topped stratigraphic architecture and thus a flat-topped sedimentary profile as a general predictive rule (cf. Schlager, 2005).

On the field, continuous outcrop beddings and palaeogeographic reconstructions based on section correlations show that the tens-of-kilometer-wide, flat inner rudist platform is likely to be separated from the slope environment by a coral or ooid facies belt, the width of which can reach a few kilometers (cf. Tab. 3; e.g. Masse and Philip, 1981; Arnaud-Vanneau et al., 1982; Richet et al., 2011; Tendil et al., 2018). This latter interpreted platform margin shows high-energy, grainstone sediments along the coral and large-sized rudist facies (e.g. caprinid; Masse, 1976; Fenerci-Masse et al., 2005; Masse and Fenerci-Masse, 2008; Bastide, 2014; Fig. 5). This belt can locally form slight reliefs but does not create a real barrier associated with a depression, as per the definition of a lagoon (Gili et al., 1995; Quesne and Bénard, 2006; Skelton and Gili, 2012). The slope consists of calcarenite to calcisiltite facies passing to marly basinal facies. This lateral facies succession supports increasing palaeodepths and sloping geometries of a few degrees maximum from the platform margin to the basin (Tab. 3; e.g. Everts et al., 1995; Léonide et al., 2012; Richet, 2011).

This general sedimentary profile defines a tropical, unrimmed flat-topped platform (sensu Handford and Loucks, 1993; Pomar, 2001) with shallow-water platform-top and margin facies developed within the infralittoral, euphotic zone (Figs. 5 and 6). This flat-topped interpretation is supported by stratigraphic observations of rudist infilling of accommodation space and persistent shallowing-upward sequences reaching sea level (cf. Gili et al., 1995; Masse and Montaggioni, 2001; e.g. Gorges de La Nesque: Léonide et al., 2012). Such a levelling pattern is consistent with shallow-water, inner-platform rudist palaeoecology and massive rudist carbonate production (Steuber, 2000; Gili and Götz, 2018; Pohl et al., 2020).

Both heterozoan and orbitolinid carbonate systems are consistently referred to as ramps (e.g. Föllmi et al., 1994, 2006). Even though no palaeotopographic profiles were directly observed, lateral successions of grainy facies are considered to represent diagnostic features (e.g. James, 1997; Ahr, 1998).

thumbnail Fig. 5

Interpretative relative distribution of facies associations according to hydrodynamics as a function of (A) depositional setting and (B) bathymetry, and (C) interpretative quantitative palaeobathymetric ranges of facies associations in the literature from the Urgonian and contemporaneous Middle East settings.

thumbnail Fig. 6

Characteristic distribution of biota production on theoretical platform profile for Barremian–Aptian (Masse, 1976; Masse and Fenerci-Masse, 2008; Léonide et al., 2012).

5.4 General sedimentary profile zonation

The lateral succession of facies on tropical-type platforms was described in a standard facies model defined by Wilson (1975). This model has become a widely accepted framework for the representation of carbonate facies models (e.g. Tucker and Wright, 1990; Flügel, 2004; Schlager, 2005). In this model, the facies associations are represented as successive belts along dip. This model shows limitations such as a sharp transition between facies belts and the lack of asymmetry of the platform (e.g. leeward to windward; Schlager, 2005). In the present study, the facies are defined according to Wilson (1975)’s model and placed on a three-dimensional depositional model to image the possible lateral facies changes along strike (e.g. coral and ooid facies association; Fig. 3).

Four genetically related zones are distinguished from proximal to distal, namely the inner platform, outer platform, slope and basin; the inner platform being subdivided into supratidal, intertidal and euphotic subtidal zones (Fig. 3 and Tab. 2; cf. Sect. 5.5 for details). Facies textures and biota of each zone are related to common interpretation in terms of light penetration, hydrodynamics and water depth (Figs. 5 and 6 and Tab. 3; cf. Pérès and Picard, 1964; Immenhauser, 2009; Purkis et al., 2019; e.g. Masse et al., 2003). Large interpretative overlaps exist regarding facies distribution in terms of palaeobathymetry. These overlaps imply significant uncertainties as to their interpretation in terms of vertical stacking patterns and sea-level evolution versus facies mosaic due to contemporaneous hydrodynamic processes (cf. Wilkinson and Drummond, 2004; Wright and Burgess, 2005; Purkis et al., 2015). In turn, these uncertainties limit interpretation of exclusive trends in sedimentary sequences.

5.5 Depositional environment and facies association

Additional details about facies, facies associations and supporting data of facies association definition can be found in Tables 2 and 4.

Table 4

Supporting outcrop data used to define the main facies associations and related facies model. See text, Table 2 and Figure 7 for related comments, facies association details and localities, respectively.

5.5.1 Inner platform

Facies textures and biota within an inner-platform palaeogeographic setting indicate an overall restricted, sheltered environment that is located within the supralittoral to infralittoral zones (i.e. supratidal, intertidal and euphotic subtidal). Supratidal environment

The supratidal environment is rarely preserved in Urgonian records as a result of initial thin deposits and preferential erosion of these most proximal portions of the inner platform (Fig. 7 and Tab. 4). The most proximal, emersive facies show well-known sedimentary and palaeontological signals of continental, beach and restricted palaeoenvironments (Upper Barremian, G. sartousiana ammonite zone, southern Provence; cf. Masse et al., 2003; Tabs. 2 and 4). In addition, in relatively distal palaeogeographic zones of the platform in southern Vercors and northern Provence, hundreds-of-meters-scale sedimentary records of subaerial exposure are interpreted from hardground surfaces overprinted by meteoric diagenesis and from shoal tops that show keystone vug-bearing facies within rudist-dominated successions (Fouke et al., 1996; Richet, 2011; Léonide et al., 2012).

Interestingly, these latter emersive and beach facies surround rudist facies at the top of aggrading, shallowing-upward sequences. In a strict sense, these features highlight the ability of rudist facies to fill up accommodation space, locally allowing islands to form, rather than a strict palaeoecological lateral succession (cf. Gili et al., 1995; Masse et al., 2003). The latter interpretation would imply a facies belt shift over time in the sense of the Walther’s law. In terms of facies model, this sedimentary pattern implies that (i) palaeobathymetric range of rudist facies nearly reaches the sea surface (Masse et al., 2003), and (ii) rare records support a strict, consistent lateral transition between beach and rudist facies belts.

thumbnail Fig. 7

Data support of facies model definition showing occurrence of the main facies per outcrop location and a palaeogeographic interpretation (background shadings; cf. Tab. 4 for data details). Intertidal and most proximal subtidal (peritidal) environments

The extent of the peritidal areas remains difficult to estimate due to the limited preservation of proximal settings (Fig. 7 and Tab. 4). Characteristic facies and grains include stromatolites, charophytes, gastropods, miliolids, and peloids (Arnaud-Vanneau and Arnaud, 1976; Masse et al., 2003; Tendil et al., 2018; Fig. 6 and Tabs. 2 and 4).

This proximal subtidal part of the inner, flat-topped platform is characterised by a protected palaeoenvironment, the peloidal-foraminiferal facies association and miliolid, mollusc, microbial, algal and non-skeletal facies (e.g. Tendil et al., 2018; Tab. 2). Only few, small, scattered records occur locally throughout the peri-Vocontian region. This apparent scatter of peloidal and miliolid facies as well as intertidal and emersive facies within rudist facies association records of the peri-Vocontian platform does not allow for the direct observation of the facies belts and belt transitions. In practice, a continuous gradual trend exists in facies description between the peloidal-foraminiferal and rudist facies association end members that is not well imaged using log correlations (Tendil, 2018; Fig. 7). At a regional scale, palaeogeographic maps show that the proximal inner-platform facies belt would have been located in areas where no Urgonian record can be observed at surface due to a complex structural setting (proximal Jura-Subalpine and Bas-Vivarais Platform in the surroundings of the Massif Central palaeohigh; Masse and Philip, 1981; Arnaud-Vanneau et al., 1982; Tendil et al., 2018; Barbarand et al., 2020; Fig. 7). Thus, such a peloidal-foraminiferal facies end member is locally recorded in the Vercors, the Subalpine Chains and in North and South Provence (e.g. Masse et al., 2003; Frau et al., 2018; Tendil et al., 2018; Tab. 4). Euphotic subtidal environment of the inner platform

The euphotic subtidal environment of the inner platform is dominated by rudist-bearing to rudist-rich facies with reference biostratigraphic materials being found at Cassis and Orgon (Urgonian limestone sensu stricto as defined by Masse, 1976). Such rudist facies cover most of the peri-Vocontian platforms of the Upper Barremian (Frau et al., 2018). They are roughly estimated to represent 50–60% of Vercors facies on palaeogeographic maps (cf. Arnaud-Vanneau, 1980) and 40% of Provence platform sediments both on palaeogeographic maps and in log sections (cf. Tendil et al., 2018; Tab. 4).

Rudist facies display a wide range of textures from wackestone to grainstone and floatstone and are made up of a diverse rudist fauna (Masse, 1992; Masse et al., 2003, 2020; Fenerci-Masse et al., 2005; Tab. 2). A well-defined palaeontological trend exists; while the proximal setting is dominated by small-sized rudists (e.g. requieniids), the distal part of the inner platform and the platform margin are characterised by the occurrence of large-sized rudists (e.g. caprinids; Masse et al., 1998; Masse and Fenerci-Masse, 2008).

5.5.2 Outer platform

The outer platform corresponds to the platform margin, high-energy and open-marine infralittoral zone (euphotic to mesophotic subtidal; Masse, 1976; Arnaud-Vanneau, 1980; Everts et al., 1995; Masse and Fenerci-Masse, 2011; Figs. 46 and Tab. 3), and is also referred to as the “shelf-break”. This depositional environment located at the platform-to-slope transition is dominated by bioclastic, echinoderm-rich facies, with local contribution of coral reefs and ooid-dominated deposits (Tab. 2). The bioclastic facies represents a large part of the Urgonian limestones sensu lato (as defined by Masse, 1976), and are found from the margin to the proximal slope. By contrast, both coral and oolitic sedimentary bodies show a limited, hundreds-of-meters to kilometers-scale lateral extent, and predominantly form at the platform margin (Tab. 4). Locally, the transition between the inner and outer platform environments is marked by the deposition of coarse-grained, coral and rudist fragment rudstones. These rudstone deposits possibly originate from short-lasting, storm-related events creating channel-like systems, as suggested by Léonide et al. (2012; Provence platform). Coral facies

Coral and coral-rudist gravel facies associations are recorded as patches in the surroundings of the high-energy platform margin (Masse and Philip, 1981; Masse and Fenerci-Masse, 2008; Léonide et al., 2012; Gili and Götz, 2018); they are found at the transition between the rudist and bioclastic facies association (e.g. Richet et al., 2011; Léonide et al., 2012). Coral facies records are not rare but limited in spatial distribution overall; they are roughly estimated to represent 4% of Provence records (cf. Tendil, 2018; Tab. 4). Ooid facies

As coral facies, ooid facies occur in limited, localised zones that are interpreted as outer platform setting (Richet et al., 2011; Léonide et al., 2012; Tab. 4). Ooidal facies association includes both ooidal and oobioclastic packstone and grainstone facies (Tab. 2). Typical ooidal and coral deposits appear to exclude one another at any given time period (Arnaud-Vanneau and Arnaud, 1976; Richet et al., 2011). Such a direct contact, however, is interpreted in Provence in the Gorges de La Nesque area, where a fault separates both facies association (Léonide et al., 2012). The ooid facies association passes laterally into bioclastic facies (Arnaud-Vanneau and Arnaud, 1976; Richet et al., 2011; Léonide et al., 2012; Tendil et al., 2018). Bioclastic facies

The bioclastic facies association appears as the volumetrically dominant Urgonian sediments in SE France (Masse and Fenerci-Masse, 2011; Richet et al., 2011; Tendil et al., 2018). According to palaeogeographic maps, the bioclastic facies characterise the platform margin, namely the transition between the platform top and the slope environment (Arnaud-Vanneau and Arnaud, 1976; Arnaud-Vanneau et al., 1982; Tendil et al., 2018). These calcarenite facies consist of undetermined grains and fragments of rudists, crinoids, echinoderms, bryozoans, brachiopods and orbitolinids. Sand wave and wave ripple sedimentary structures are common. This facies association is interpreted as reworked sediments of the outer platform and proximal slope (e.g. Masse, 1993; Léonide et al., 2012). More specifically, these bioclastic facies are interpreted as genetically-related to the rudist facies association and includes an increasing proportion of in situ echinoderm and bryozoan grains towards more distal and aphotic settings (e.g. Léonide et al., 2012). In Provence, the bioclastic facies association forms a facies belt varying from 5 up to 20 km in width (Léonide et al., 2012; Tendil et al., 2018; Tab. 4).

5.5.3 Slope

The slope corresponds to the circalittoral (oligophotic to aphotic subtidal) zone that is characterised by lower light and hydrodynamic levels compared to the outer platform. Other terms that are used in literature include “external slope” and “outer shelf”. The slope is composed of very fine bioclastic facies made up of fragments of sponges, echinoderms, bryozoans and a significant part of transported sediments (e.g. mass flow; South Vercors and North Provence; Arnaud-Vanneau and Arnaud, 1976; Tendil et al., 2018; Tabs. 2 and 4). Orbitolinid facies were reported from this depositional environment in Provence (Gorges de La Nesque; Léonide et al., 2012; Tendil et al., 2018).

5.5.4 Basin

In many cases, the so-called basin strictly corresponds to the termination of the continental shelf (i.e. pre-Vocontian settings sensu Frau et al., 2018) and is mostly characterised by fine-grained calcisiltite facies (Tabs. 2 and 4). The Vocontian Basin sensu stricto is located further seaward and delineated by major faulting systems (e.g. Ventoux–Lure axis in northern Provence). These basinal environments correspond to the bathyal zone and are characterised by fine-grained transported, hemipelagic and pelagic marl mudstone facies (cf. Tendil et al., 2018).

6 Discussion

A facies model of ancient sedimentary system is rarely built upon absolute and continuous real data, but rather on limited, recorded parameters generally extrapolated with deterministic interpretations (Fig. 7). In terms of data, spatial and temporal resolutions strongly limit the realism and accuracy of the model. Urgonian facies model data show an outcrop spacing varying from 3 to 55 km, and a temporal resolution between ca. 1 and 3 Ma based on biostratigraphic interpretation, increasing to 0.5 Ma based on lithostratigraphic and sequence stratigraphic interpretation (Tab. 1). In terms of interpretation, the use of concepts plays a leading role in defining a facies succession and thus a facies model (Tab. 3). Actualism views have a strong influence on the interpretation of facies distribution and their controlling parameters, and even more in a context of incomplete and uncertain data records (Ginsburg, 1956; Pérès and Picard, 1964).

Studying historical evolution can help understanding such a facies model definition of a specific zone (Figs. 2 and 3). For instance, a modern-type platform profile including a reef barrier built up to sea level is now well accepted not to be used as a direct analogue for ancient systems (e.g. Rosen and Taylor, 1990; McCall et al., 1994; Gili et al., 1995; Pomar, 2020). The birth and early developments of sequence stratigraphy had a strong imprint in the way a facies model and palaeobathymetric profile were defined (e.g. Arnaud-Vanneau et al., 1987; Wilkinson et al., 1996; Purkis et al., 2015).

The starting point of facies model definition is the depositional facies classification (Tab. 2). This basic point should not be considered as straightforward, because such a basic sedimentological observation does not provide absolute datasets but includes geological interpretation (cf. Lokier et al., 2016). Palaeontological and palaeoecological analyses represent further basics of facies model definition, even though high taxonomic level determination can be of limited value (Fig. 6). Urgonian facies definition benefits from the comparison of palaeontological and sedimentological studies for more than a hundred years that provide a great robustness in interpretation (Fig. 2).

A key constraint of facies model definition is the location of depositional facies on palaeogeographic maps. Such maps were utilised to show a convincing consistency of platform-scale, general Urgonian facies model (Masse and Philip, 1981; Arnaud-Vanneau et al., 1982; Tendil et al., 2018; Fig. 7 and Tab. 4). At this large scale, however, smaller-scale lithofacies heterogeneity is generally difficult to capture. Lithofacies heterogeneity is more easily recognized studying stacking patterns on log sections from which facies variability is directly observed (e.g. Borgomano et al., 2002; Godet et al., 2010). In a log section context in turn, the spatial interpretation of temporal stacking patterns in terms of either Walther’s law or facies mosaic is not straightforward (e.g. Purkis et al., 2015, 2019). A higher spatial resolution is required to be able to determine a better constrained facies model.

Continuous outcrop studies provide invaluable, high-resolution data about facies succession and transition. Lateral palaeontological and sedimentological transitions are directly observed on the kilometer-to-ten-of-kilometer-long outcrops and tens-to-hundreds-of-meters log section correlations of Gorges de La Nesque in Provence, Gresse-en-Vercors and the Cirque d’Archiane in Vercors (Léonide et al., 2012; Richet et al., 2011; Everts et al., 1995, respectively); these outcrops being in the surroundings of the palaeo-platform margin (Fig. 7). In a more proximal setting of the Barremian platform, down to 100-m-distant log sections were correlated in the Cassis area in Provence (Fenerci-Masse et al., 2005). As an example, the Gresse-en-Vercors outcrop directly shows lateral facies transitions from rudist to coral-rudist, coral-bioclastic and bioclastic facies along a continuously-walked-on-the-field time line (Richet, 2011; Richet et al., 2011). This lateral facies succession is consistent with platform-scale log correlations and palaeogeographic maps (Fig. 7). Such a consistency between rock observations at outcrop and platform scales and conceptual model strongly constrains the overall facies belt scheme (Figs. 4 and 7 and Tabs. 3 and 4).

Beyond the general, consistent facies distribution of these continuous outcrops, localized observations of limited amount of keystone-vug facies, coral–rudist rudstone facies, oolitic facies and orbitolinid–green algae grainstone facies highlight less constrained spatial and/or temporal sedimentological patterns such as transport or accommodation infilling events (Fig. 7 and Tab. 4). These patterns are considered as spatially random processes affecting a limited volume of sediments that show only minor imprints into the process-based facies model (Fig. 3). The possibility of the distinction between such minor vs. more general facies patterns remains questionable using a limited dataset.

Because the records of the Lower and Upper Orbitolinid Beds in the Vercors and the I. giraudi and M. sarasini Palorbitolina-rich beds in Provence tend to exclude other platform-top sediments (Arnaud-Vanneau and Arnaud, 1976; Tendil et al., 2018, respectively), a specific facies model for orbitolinid-rich deposition is considered. A distinct facies model is justified by specific palaeoenvironmental conditions; terrigenous influences are repeatedly observed and invoked in association with Cretaceous orbitolinid-rich sedimentation (general discussion and Spanish Albacete-Prebetic case study – Vilas et al., 1995; Vercors, France – Arnaud-Vanneau and Arnaud, 1976; Helvetic Alps, Switzerland – Stein et al., 2012; Lusitanian Basin, Portugal – Burla et al., 2008; Kharaib and Shuaiba formations including the Hawar member of the Arabian Platform, Saudi Arabia, UAE and Oman – Borgomano et al., 2002; Davies et al., 2002; van Buchem et al., 2002; global pattern – Michel et al., 2019).

No specific palaeobathymetry is assigned to these orbitolinid-rich facies associations (Fig. 6). If orbitolinid grains can be found in diverse facies and certain orbitolinid facies can be found in specific palaeoenvironments (e.g. Masse, 1991; Léonide et al., 2012), orbitolinid-rich deposits are considered as opportunist and thus interpreted to occur in palaeoenvironments in which other biota do not occur (e.g. terrigenous-influenced settings; e.g. Föllmi et al., 2006; Michel et al., 2019).

7 Implications

7.1 From non-continuous data correlation to conceptual continuous facies model

A facies model definition results from the integration of chronostratigraphic, palaeontological and sedimentological data and their interpretations into a consistent conceptual framework of correlations (Tabs. 14). The key principles of definition include (i) building consistent conceptual models based on lateral palaeoecological succession concepts, palaeogeographic maps, direct lateral facies transition observations and consistent stacking trends, (ii) showing existing models and their local and general differences, and (iii) providing locations of records (e.g. Tendil, 2018), an estimate of recorded volumes, a detailed chronostratigraphic framework, and the basic hypotheses and uncertainties associated with the model (e.g. absence of record of most proximal Urgonian records; Fig. 7).

In many cases, the location of recorded facies and their relative quantities within the palaeogeographic context are neither shown nor mentioned due to limited temporal and spatial resolutions and preservation, which effects can hardly be distinguished and constrained. These data, however, are key for further studies opening to re-evaluation and re-interpretation of previous works in the light of advancing science. Questions about (i) the importance of the poorly preserved, most proximal deposits of a sedimentary system and (ii) the ramp vs. shelf interpretation in the absence or poor preservation of platform margin records are first concerned by such data (e.g. Lower Cretaceous Urgonian limestones – Masse and Fenerci-Masse, 2011; Oligocene Lessini Shelf – Pomar et al., 2017 vs. Bosellini et al., 2020; Miocene Yadana Platform – Paumard et al., 2017 vs. Teillet et al., 2020).

The Urgonian facies model provides a robust, platform-scale belt scheme and large-scale facies patterns (kilometers-to-tens-of-kilometer-scale; Figs. 47). In this context however, finer, hundreds-of-meters-scale facies heterogeneity cannot be captured precisely. Specific geobody distribution and continuous outcrop studies are required to study these finer-scale heterogeneities (e.g. Borgomano et al., 2002; Fenerci-Masse et al., 2005; Richet et al., 2011; Léonide et al., 2012). Numerical modelling can be used to tackle these questions (e.g. Budd et al., 2016; Massonnat et al., 2017; Lanteaume et al., 2018; Madjid et al., 2018; Tomassetti et al., 2018).

7.2 Modelling perspective

The facies model forms the basis to predict empty spaces of stratigraphic correlations and reservoir models. Facies of the facies model are used as elementary bricks, the consistent distribution (i.e. facies belts) of which allows analyzing rock property distribution and scale change in static modelling. The facies model defined in this study and associated physical parameters (hydrodynamics, distance to the coast and spatial organization; Figs. 4, 5 and 7) can be used as a constraint and input (external drift) for facies modelling. The graphic model representation and facies extent provide rules to determining proportional cubes for this type of platform (e.g. Tendil, 2018).

In general, models with standard facies belts are statically constructed. The static assumption is important to consider during the construction of stratigraphic models because carbonate systems largely evolve through time. These temporal variations generate transient and unstable behaviors. Nevertheless, the morphology of the Urgonian sediments makes it possible to analyse facies stability (cf. Schlager, 2005) during a favorable period because the production area is of a large extent (e.g. rudist facies association). A facies model aims at characterizing such a facies stability pattern. In addition, transient events on the Urgonian platform such as orbitolinid mass occurrences appear to be the effect of palaeoclimate changes (Arnaud-Vanneau and Arnaud, 1976; Föllmi, 2012), which in turn could be triggered by volcanic events (Tendil et al., 2018). Prediction of such a facies change depends on the understanding of palaeoenvironmental controlling mechanisms.

The method of the facies model construction promotes the use of process-based modelling. This model provides elements to define sedimentary supply, bathymetric and hydrodynamic profiles. The use of these parameter values on synchronous sedimentary layers will allow refining and challenging facies transitions. The chronostratigraphical assumption of the synchronous interpretation, which stands as the “article of faith” of facies model definition, needs constant cross-testing with new available data and concepts, as well as proof of concept by numerical modelling. Process-based modelling can provide ranges of uncertainties on qualitative and quantitative facies distribution. For example, a point to explore would be the quantitative relationship between the production of the inner-platform rudists and the outer-platform bioclastic facies. Process-based models could allow balancing and quantifying the needed production and transport of sedimentary facies to fill in a defined accommodation space.

8 Conclusions

Based on a literature review and a contextualization of interpreted data and models, this study provides a unified facies model for the Urgonian carbonate platforms of SE France. The facies model is described within an infrastructure framework sensu Handford and Loucks (1993) ranging from the overall carbonate system to the unitary depositional facies. The model analysis makes it possible to discuss and argue each element of the carbonate platform at a regional scale. We therefore propose a three-dimensional sedimentary model with facies belts along dip and lateral facies variability. Sedimentary facies are related with physical characteristics and processes such as palaeobathymetry and hydrodynamics that make the model readily suitable for static and forward modelling.

The proposed facies model is defined as a contemporaneous sedimentological and palaeoecological system and placed into a consistent palaeoecological framework. Data supporting the model including location and volume estimates are explicitly mentioned, as well as fundamental assumptions and uncertainties related to the model definition. These elements are considered as prerequisite prior to the building up of a robust facies model and its subsequent comparison to others.

Specific remarks on facies model definition can be put forward:

  • the actualistic palaeotopographic model of lagoonal depression-marginal reef relief-steep slope of carbonate platform is broadly used even though no observation supports such an interpretation, which has long been cautioned (e.g. Rosen and Taylor, 1990; Gili et al., 1995; Pomar, 2020).

  • building a facies model results from a complex integration of conceptual models along with spatial and temporal data interpretations. Model definition is based on key geological hypotheses that are generally not referred to in studies, while these assumptions could evolve with scientific advances.

Author contributions

G.M., J.B., M.R., J-P.R., C.D. and P.L. conceived the research project and provided a continuous input throughout the study. C.L., A.T., F.B., C.F., J.M. and M.B. realized the bibliographic compilation and data processing. C.L. and J.M. led the writing of the manuscript. All authors have defined the proposed facies model.


Thank you to all the reviewers who contributed to the great improvement of the manuscript. This study was funded by Total Exploration and Production in the ALBION project ( This paper strongly benefited from discussions with Jean-Pierre Masse, François Fournier (Aix-Marseille Université), Pierre Masse, Jérémy Robinet and Emmanuel Dujoncquoy (TOTAL S.E., Pau).


  • Adatte T, Arnaud-Vanneau A, Arnaud H, Bodin S, Carrio-Schaffhauser E, Föllmi KB, et al. 2005. The Hauterivian-lower Aptian sequence stratigraphy from Jura platform to vocontian basin: a multidisciplinary approach. Field-trip of the 7th International Symposium on the Cretaceous (September 1–4, 2005); Série “Colloques et Excursions” n°7, Université Joseph Fournier, Grenoble 1-Université de Neuchâtel, UNINE, 181 pp. [Google Scholar]
  • Ahr WM. 1998. Carbonate ramps, 1973–1996: a historical review. Geological Society, London, Special Publications 149: 7–14. [CrossRef] [Google Scholar]
  • Alsharhan AS. 1995. Facies variation, diagenesis, and exploration potential of the Cretaceous rudist-bearing carbonates of the Arabian Gulf. American Association of Petroleum Geologists Bulletin 79: 531–550. [Google Scholar]
  • Alsharhan AS. 1993. Bu Hasa Field – United Arab Emirates, Rub al Khali Basin, Abu Dhabi. Treatise of Petroleum Geology, Atlas of Oil and Gas Fields: Structural Traps VIII: 99–127. [Google Scholar]
  • Argenio BD, Ferreri V, Amodio S, Pelosi N. 1997. Hierarchy of high-frequency orbital cycles in Cretaceous carbonate platform strata. Sedimentary Geology 113: 169–193. [CrossRef] [Google Scholar]
  • Arnaud-Vanneau A. 1979. Répartition de la microfaune dans les différents paléomilieux urgoniens. Geobios 3: 255–275. [CrossRef] [Google Scholar]
  • Arnaud-Vanneau A. 1980. Micropaléontologie, paléoécologie, et sédimentologie d’une plate-forme carbonatée de la marge passive de la Téthys : l’Urgonien du Vercors septentrional et de la Chartreuse (Alpes occidentales). PhD Thesis, Université Scientifique et Médicale de Grenoble, Géologie Alpine, Mémoire n°11, 1128 pp. [Google Scholar]
  • Arnaud-Vanneau A, Arnaud H. 1976. L’évolution paléogéographique du Vercors au Barrémien et à ĺAptien inférieur (Chaînes subalpines septentrionales, France). Geologie Alpine 52: 5–30. [Google Scholar]
  • Arnaud-Vanneau A, Arnaud H. 2005. Carbonate facies and microfacies of the Lower Cretaceous carbonate platforms. In: Adatte T, Arnaud-Vanneau A, Arnaud H, Bodin S, Carrio-Schaffhauser E, Föllmi KB, Godet A, Chaker Raddadi M, Vermeulen J, (Eds.), The Hauterivian-lower Aptian sequence stratigraphy from Jura platform to vocontian basin: a multidisciplinary approach. Field-trip of the 7th International symposium on the Cretaceous (September 1-4, 2005) ; Série spéciale “Colloques et Excursions” n°7, Université de Grenoble – Université de Neuchâtel pp. 97–126. Available at: [Google Scholar]
  • Arnaud-Vanneau A, Arnaud H, Cotillon P, Ferry S, Masse JP. 1982. Caractères et Evolution des Plates-formes Carbonatées Périvocontiennes au Crétacé Inférieur ( France Sud-Est). Cretaceous Research 3: 3–18. [CrossRef] [Google Scholar]
  • Arnaud-Vanneau A, Arnaud H, Adatte T, Argot M, Rumley G, Thieuloy JP. 1987. The Lower Cretaceous from the Jura Platform to the Vocontian Basin (Swiss Jura, France). In: 3rd Int. Cretaceous Symp, Field Guide Excursion D (August 26–September 9, 1987), Tübingen, Université de Grenoble–Université de Neuchâtel, 128 pp. [Google Scholar]
  • Barbarand J, Préhaud P, Baudin F, Missenard Y, Matray JM, François T, et al. 2020. Where are the limits of Mesozoic intracontinental sedimentary basins of southern France? Marine and Petroleum Geology 121: 104589. [Google Scholar]
  • Bastide F. 2014. Synthèse de l’évolution de la plateforme urgonienne (Barrémien tardif à Aptien précoce) du Sud-Est de la France : Faciès, micropaléontologie, géochimie, géométries, paléotectonique et géomodélisation. PhD Thesis, Université de Grenoble, 298 pp. [Google Scholar]
  • Betzler C, Brachert TC, Nebelsick J. 1997. The warm temperate carbonate province – A review of facies, zonations, and delimitations. Courier Forschungs-Institut Senckenberg 201: 83–99. [Google Scholar]
  • Bièvre G, Quesne D. 2004. Synsedimentary collapse on a carbonate platform margin (lower Barremian, southern Vercors, SE France). Geodiversitas 26: 169–184. [Google Scholar]
  • Blanc Aletru MC. 1995. Importance des discontinuités dans l’enregistrement sédimentaire de l’urgonien jurassien : micropaléontologie, sédimentologie, minéralogie et stratigraphie séquentielle. PhD Thesis, Université de Neuchâtel, Géologie Alpine, Mémoire n°24, 299 pp. [Google Scholar]
  • Bodin S. 2006. Palaeoceanographic and palaeoclimatic changes during the Late Hauterivian–Barremian and their impact on the northern Tethyan margin: A combined sedimentological and geochemical approach. PhD Thesis, Université de Neuchâtel, 272 pp. [Google Scholar]
  • Bodin S, Godet A, Vermeulen J, Linder P, Föllmi KB. 2006. Biostratigraphy, sedimentology and sequence stratigraphy of the latest Hauterivian–Early Barremian drowning episode of the Northern Tethyan margin (Altmann Member, Helvetic nappes, Switzerland). Eclogae Geologicae Helvetiae 99: 157–174. [CrossRef] [Google Scholar]
  • Bonvallet L. 2015. Evolution of the Helvetic shelf ( Switzerland) during the Barremian-early Aptian: paleoenvironmental, paleogeographic and paleoceanographic controlling factors. PhD Thesis, Université de Neuchâtel, 217 pp. [Google Scholar]
  • Bonvallet L, Arnaud-Vanneau A, Arnaud H, Adatte T, Spangenberg JE, Stein M, et al. 2019. Evolution of the Urgonian shallow-water carbonate platform on the Helvetic shelf during the late Early Cretaceous. Sedimentary Geology 387: 18–56. [CrossRef] [Google Scholar]
  • Borgomano J, Masse JP, Al Maskiry S. 2002. The lower Aptian Shuaiba carbonate outcrops in Jebel Akhdar, northern Oman: Impact on static modeling for Shuaiba petrol eum reservoirs. AAPG Bulletin 86: 1513–1529. [Google Scholar]
  • Borgomano JRF, Fournier F, Viseur S, Rijkels L. 2008. Stratigraphic well correlations for 3-D static modeling of carbonate reservoirs. AAPG Bulletin 92: 789–824. [CrossRef] [Google Scholar]
  • Borgomano J, Masse JP, Fenerci-Masse M, Fournier F. 2013. Petrophysics of Lower Cretaceous platform carbonate outcrops in provence (SE France): Implications for carbonate reservoir characterisation. Journal of Petroleum Geology 36: 5–41. [CrossRef] [Google Scholar]
  • Borgomano J, Lanteaume C, Philippe L, Fournier F, Montaggioni L, Masse JP. 2020. Quantitative carbonate sequence stratigraphy: Insights from stratigraphic forward models. AAPG Bulletin 1–28. [Google Scholar]
  • Bosellini FR, Vescogni A, Kiessling W, Zoboli A, Di Giuseppe D, Papazzoni CA. 2020. Revisiting reef models in the oligocene of northern Italy (venetian southern alps). Bollettino della Societa Paleontologica Italiana 59: 337–348. [Google Scholar]
  • Bover-Arnal T, Salas R, Moreno-Bedmar JA, Bitzer K. 2009. Sequence stratigraphy and architecture of a late Early-Middle Aptian carbonate platform succession from the western Maestrat Basin (Iberian Chain, Spain). Sedimentary Geology 219: 280–301. [CrossRef] [Google Scholar]
  • Bover-Arnal T, Salas R, Guimerà J, Moreno-Bedmar JA. 2022. Eustasy in the Aptian world: A vision from the eastern margin of the Iberian Plate. Global and Planetary Change 214: 103849. [CrossRef] [Google Scholar]
  • Brigaud B, Bonifacie M, Pagel M, Blaise T, Calmels D, Haurine F, Landrein P. 2020. Past hot fluid flows in limestones detected by Δ47-(U-Pb) and not recorded by other geothermometers. Geology 48: 851–856. [CrossRef] [Google Scholar]
  • Budd DA, Hajek EA, Purkis SJ. 2016. Introduction to autogenic dynamics and self-organization in sedimentary systems. SEPM Special Publications 106: 1–4. [Google Scholar]
  • Burla S, Heimhofer U, Hochuli PA, Weissert H, Skelton P. 2008. Changes in sedimentary patterns of coastal and deep-sea successions from the North Atlantic (Portugal) linked to Early Cretaceous environmental change. Palaeogeography, Palaeoclimatology, Palaeoecology 257: 38–57. [CrossRef] [Google Scholar]
  • Cantrell DL, Nicholson PG, Hughes GW, Miller MA, Buhllar AG, Abdelbagi ST, et al. 2014. Tethyan petroleum systems of Saudi Arabia. AAPG Memoir 106: 613–639. [Google Scholar]
  • Catuneanu O, Galloway WE, Kendall CGSC, Miall AD, Posamentier HW, Strasser A, et al. 2011. Sequence Stratigraphy: Methodology and Nomenclature. Newsletters on Stratigraphy 44: 173–245. [CrossRef] [Google Scholar]
  • Clavel B, Charollais J-J, Busnardo R, Granier B, Conrad M, Desjacques P, et al. 2014. La plate-forme carbonatée urgonienne (Hauterivien supérieur–Aptien inférieur) dans le Sud-Est de la France et en Suisse : synthèse. Archives des Sciences 67: 1–97. [Google Scholar]
  • Collinson JD. 1969. The sedimentology of the Grindslow shales and the Kinderscout grit; a deltaic complex in the Namurian of northern England. Journal of Sedimentary Research 39: 194–221. [Google Scholar]
  • Davies RB, Casey DM, Horbury AD, Sharland PR, Simmons MD. 2002. Early to mid-Cretaceous mixed carbonate-clastic shelfal systems: Examples, issues and models from the Arabian Plate. GeoArabia 7: 541–598. [Google Scholar]
  • Douvillé H. 1900. Sur la distribution géographique des Rudistes, des Orbitolines et des Orbitoides. Bulletin de la Société géologique de France 28: 222–235. [Google Scholar]
  • Edwards J, Lallier F, Caumon G, Carpentier C. 2018. Uncertainty management in stratigraphic well correlation and stratigraphic architectures: A training-based method. Computers and Geosciences 111: 1–17. [CrossRef] [Google Scholar]
  • Everts AJW, Stafleu JAN, Schlager W, Fouke BW, Zwart EW. 1995. Stratal patterns, sediment composition, and sequence stratigraphy at the margin of the Vercors carbonate platform (Lower Cretaceous, SE France). Journal of Sedimentary Research B65: 119–131. [Google Scholar]
  • Fenerci-Masse M, Masse JP, Chazottes V. 2005. Quantitative analysis of rudist assemblages: a key for palaeocommunity reconstructions. The late Barremian record from SE France. Palaeogeography, Palaeoclimatology, Palaeoecology 206: 133–147. [Google Scholar]
  • Ferry S, Grosheny D. 2019. Growth faults affecting depositional geometry, facies and sequence stratigraphy record on a carbonate platform edge (South Vercors Urgonian platform, SE France). Bulletin de la Société Géologique de France 190: 2–9. [CrossRef] [EDP Sciences] [Google Scholar]
  • Flügel E. 2004. Microfacies of carbonate rocks Analysis, Interpretation and Application. Berlin, Springer, 976 p. [Google Scholar]
  • Föllmi KB. 2012. Early Cretaceous life, climate and anoxia. Cretaceous Research 35: 230–257. [Google Scholar]
  • Föllmi KB, Godet A. 2013. Palaeoceanography of Lower Cretaceous Alpine platform carbonates. Sedimentology 60: 131–151. [CrossRef] [Google Scholar]
  • Föllmi KB, Gertsch B, Renevey JP, De Kaenel E, Stille P. 2008. Stratigraphy and sedimentology of phosphate-rich sediments in Malta and south-eastern Sicily (latest Oligocene to early Late Miocene). Sedimentology 55: 1029–1051. [Google Scholar]
  • Föllmi KB, Godet A, Bodin S, Linder P. 2006. Interactions between environmental change and shallow water carbonate buildup along the northern Tethyan margin and their impact on the Early Cretaceous carbon isotope record. Paleoceanography 21: 1–16. [Google Scholar]
  • Follmi KB, Weissert H, Bisping M, Funk H. 1994. Phosphogenesis, carbon-isotope stratigraphy, and carbonate-platform evolution along the Lower Cretaceous northern Tethyan margin. Geological Society of America Bulletin 106: 729–746.<0729:PCISAC>2.3.CO;2. [Google Scholar]
  • Fouke BW, Everts A-JW, Zwart EW, Schlager W, Smalley PC, Weissert H. 1996. Subaerial exposure unconformities on the Vercors carbonate platform (SE France ) and their sequence stratigraphic significance. Geological Society, London, Special Publications 104: 295–319. [CrossRef] [Google Scholar]
  • Frau C, Pictet A, Spangenberg JE, Masse J-P, Tendil AJB, Lanteaume C. 2017. New insights on the age of the post-Urgonian marly cover of the Apt region (Vaucluse, SE France) and its implications on the demise of the North Provence carbonate platform. Sedimentary Geology 359: 44–61. [CrossRef] [Google Scholar]
  • Frau C, Tendil AJ-B, Lanteaume C, Masse J-P, Pictet A, Bulot LG, et al. 2018. Late Barremian-early Aptian ammonite bioevents from the Urgonian-type series of Provence, southeast France: Regional stratigraphic correlations and implications for dating the peri-Vocontian carbonate platforms. Cretaceous Research 90: 222–253. [CrossRef] [Google Scholar]
  • Frau C, Tendil AJB, Pohl A, Lanteaume C. 2020. Revising the timing and causes of the Urgonian rudistid-platform demise in the Mediterranean Tethys. Global and Planetary Change 187: 103124. [CrossRef] [Google Scholar]
  • Frau C, Tendil AJ-B, Masse J-P, Richet R, Borgomano JR, Lanteaume C, et al. 2021. Revised biostratigraphy and regional correlations of the Urgonian southern Vercors carbonate platform, southeast France. Cretaceous Research 104773. [CrossRef] [Google Scholar]
  • Gili E, Götz S. 2018. Paleoecology of rudists. The University of Kansas, Treatise Online 103, Part N, Revised, Volume 2, Chapter 26B, 29 pp. [Google Scholar]
  • Gili E, Masse JP, Skelton PW. 1995. Rudists as gregarious sediment-dwellers, not reef-builders, on Cretaceous carbonate platforms. Palaeogeography, Palaeoclimatology, Palaeoecology 118: 245–267. [CrossRef] [Google Scholar]
  • Gili E, Skelton PW, Bover-Arnal T, Salas R, Obrador A, Fenerci-Masse M. 2016. Depositional biofacies model for post-OAE1a Aptian carbonate platforms of the western Maestrat Basin (Iberian Chain, Spain). Palaeogeography, Palaeoclimatology, Palaeoecology 453: 101–114. [CrossRef] [Google Scholar]
  • Ginsburg RN. 1956. Environmental relationships of grain size and constituent particles in some South Florida carbonate sediments. AAPG Bulletin 40: 2384–2427. [Google Scholar]
  • Godet A. 2006. The evolution of the Urgonian platform in the western Swiss Jura realm and its interactions with palaeoclimatic and palaeoceanographic change along the Northern Tethyan Margin (Hauterivian-earliest Aptian). PhD Thesis, Université de Neuchâtel, 405 pp. Available from [Google Scholar]
  • Godet A, Föllmi KB, Bodin S, de Kaenel E, Matera V, Adatte T. 2010. Stratigraphic, sedimentological and palaeoenvironmental constraints on the rise of the Urgonian platform in the western Swiss Jura. Sedimentology 57: 1088–1125. [CrossRef] [Google Scholar]
  • Godet A, Durlet C, Spangenberg JE, Föllmi KB. 2016. Estimating the impact of early diagenesis on isotope records in shallow-marine carbonates: A case study from the Urgonian Platform in western Swiss Jura. Palaeogeography, Palaeoclimatology, Palaeoecology 454: 125–138. [CrossRef] [Google Scholar]
  • Handford R, Loucks RG. 1993. Carbonate depositional sequences and systems tracts - Responses of carbonate platforms to relative sea-level changes. In: Loucks RG, Sarg JF (Eds.), Carbonate Sequence Stratigraphy Recent Developments and Applications. AAPG Memoir 57: 3–41. [Google Scholar]
  • Hughes GW. 1997. The Great Pearl Bank Barrier of the Arabian Gulf as a possible Shu’aiba analogue. GeoArabia 2: 279–304. [CrossRef] [Google Scholar]
  • Immenhauser A. 2009. Estimating palaeo-water depth from the physical rock record. Earth-Science Reviews 96: 107–139. [CrossRef] [Google Scholar]
  • Jacquin T, Arnaud-Vanneau A, Arnaud H, Ravenne C, Vail PR. 1991. Systems tracts and depositional sequences in a carbonate setting: a study of continuous outcrops from platform to basin at the scale of seismic lines. Marine and Petroleum Geology 8: 122–139. [Google Scholar]
  • James NP. 1997. The cool-water carbonate depositional realm, in: James NP, Clarke JAD (Eds.), Cool-Water Carbonates. SEPM Special Publication 56, pp. 1-20. [Google Scholar]
  • Kenter J, Harris PM, Playton T. 2009. Getting Started in Carbonate Sequence Stratigraphy: A Compendium of Influential Papers. AAPG/Datapages 107–132. [Google Scholar]
  • Kiessling W, Flügel E, Golonka J. 2003. Patterns of Phanerozoic carbonate platform sedimentation, Lethaia 36: 195–226. [CrossRef] [Google Scholar]
  • Kindler P, Wilson MEJ. 2010. Carbonate grain associations: their use and environmental significance, a brief review. Carbonate systems during the Oligocene-Miocene climate transition. Chichester (West Sussex): International Association of Sedimentologists Special Publications Wiley-Blackwell, pp. 35–48. [Google Scholar]
  • Lallier F, Caumon G, Borgomano J, Viseur S, Royer JJ, Antoine C. 2016. Uncertainty assessment in the stratigraphic well correlation of a carbonate ramp: Method and application to the Beausset Basin, SE France. Comptes Rendus – Geoscience 348: 499–509. [CrossRef] [Google Scholar]
  • Lanteaume C, Fournier F, Pellerin M, Borgomano J. 2018. Testing geologic assumptions and scenarios in carbonate exploration: Insights from integrated stratigraphic, diagenetic, and seismic forward modeling. Leading Edge 37: 672–680. [CrossRef] [Google Scholar]
  • Léonide P, Borgomano J, Masse JP, Doublet S. 2012. Relation between stratigraphic architecture and multi-scale heterogeneities in carbonate platforms: The Barremian-lower Aptian of the Monts de Vaucluse, SE France. Sedimentary Geology 265: 87–109. [CrossRef] [Google Scholar]
  • Lokier SW, Al Junaibi M, Pufahl P. 2016. The petrographic description of carbonate facies: are we all speaking the same language? Sedimentology 63: 1843–1885. [CrossRef] [Google Scholar]
  • Madjid MYA, Vandeginste V, Hampson G, Jordan CJ, Booth AD. 2018. Drones in carbonate geology: Opportunities and challenges, and application in diagenetic dolomite geobody mapping. Marine and Petroleum Geology 91: 723–734. [Google Scholar]
  • Masse J-P. 1966. Etude lithologique et paléocéanographique de la série marine d’Orgon (Bouche-du-Rhône). Rec. Trav. Stat. Mar. Endoume 40: 267–297. [Google Scholar]
  • Masse J-P. 1976. Les calcaires urgoniens de Provence, Valanginien-Aptien inférieur. Stratigraphie, paléontologie, les paléoenvironments et leur évolution. PhD Thesis, Université de Marseille, 445 pp. [Google Scholar]
  • Masse J-P. 1991. The Lower Cretaceous Mesogean benthic ecosystems: palaeoecologic aspects and palaeobiogeographic implications. Palaeogeography, Palaeoclimatology, Palaeoecology 91: 331–345. [Google Scholar]
  • Masse JP. 1992. The Lower Cretaceous Mesogean benthic ecosystems: palaeoecologic aspects and palaeobiogeographic implications. Palaeogeography, Palaeoclimatology, Palaeoecology 91: 331–345. [Google Scholar]
  • Masse J-P. 1993. Valanginian-Early Aptian Carbonate Platforms from Provence, Southeastern France. AAPG Memoir 53: 363–374. [Google Scholar]
  • Masse J-P, Philip J. 1981. Cretaceous coral-rudist buildups of France. SEPM Special Publication 30: 399–426. [Google Scholar]
  • Masse J-P, Montaggioni LF. 2001. Growth history of shallow-water carbonates: Control of accommodation on ecological and depositional processes. International Journal of Earth Sciences 90: 452–469. [CrossRef] [Google Scholar]
  • Masse J-P, Fenerci-Masse M. 2008. Time contrasting palaeobiogeographies among Hauterivian-Lower Aptian rudist bivalves from the Mediterranean Tethys, their climatic control and palaeoecological implications. Palaeogeography, Palaeoclimatology, Palaeoecology 269: 54–65. [CrossRef] [Google Scholar]
  • Masse J-P, Fenerci-Masse M. 2011. Drowning discontinuities and stratigraphic correlation in platform carbonates. The late Barremian-early Aptian record of southeast France. Cretaceous Research 32: 659–684. [Google Scholar]
  • Masse J-P, Fenerci-Masse M. 2015. Evolution of the rudist bivalve (Radiolitidae,Hippuritida) from the Mediterranean region. Palaeontology 58: 71–100. [CrossRef] [Google Scholar]
  • Masse J-P, Borgomano J, Al Maskiry S. 1998. A platform-to-basin transition for lower Aptian carbonates (Shuaiba Formation) of the northeastern Jebel Akhdar (Sultanate of Oman). Sedimentary Geology 119: 297–309. [Google Scholar]
  • Masse JP, Villeneuve M, Leonforte E, Nizou J. 2009. Block tilting of the North Provence early Cretaceous carbonate margin: Stratigraphic, sedimentologic and tectonic data. Bulletin de la Societe Geologique de France 180: 105–115. [Google Scholar]
  • Masse J-P, Fenerci-Masse M, Pernarcic E. 2003. Palaeobathymetric reconstruction of peritidal carbonates Late Barremian, Urgonian, sequences of Provence (SE France). Palaeogeography, Palaeoclimatology, Palaeoecology 200: 65–81. [CrossRef] [Google Scholar]
  • Masse J-P, Frau C, Tendil AJ-B, Fenerci-Masse M. 2020. Evidence for three successive upper Barremian-lower Aptian rudist faunas in the Urgonian-type deposits of southeastern France and their stratigraphic value. Cretaceous Research 115: 104561. [CrossRef] [Google Scholar]
  • Masse J-P, Frau C, Aubert F, Gesbert D. 2022. Non-rudist infralittoral bivalves from the Urgonian-type carbonate platforms of southeast France and the neighbouring regions: biodiversity, palaeoecological significance and relationships with rudists. Cretaceous Research 105294. [CrossRef] [Google Scholar]
  • Massonnat GJ, Rolando J, Danquigny C. 2017. The ALBION Project: An Observatory in the Heart of a Carbonate Reservoir ALBION dynamic outcrop analogue: a disruptive methodology. Abu Dhabi International Petroleum Exhibition & Conference, November 13-16, UAE, 9 pp. [Google Scholar]
  • McCall J, Rosen B, Darrell J. 1994. Carbonate deposition in accretionary prism settings: Early miocene coral limestones and corals of the Makran mountain range in Southern Iran. Facies 31: 141–177. [Google Scholar]
  • Michel J, Laugié M, Pohl A, Lanteaume C, Masse JP, Donnadieu Y, et al. 2019. Marine carbonate factories: a global model of carbonate platform distribution. International Journal of Earth Sciences 108: 1773–1792. [CrossRef] [Google Scholar]
  • Parize O, Beaudoin B, Champanhet J-M, Friès G, Imbert P, Labourdette R, et al. 2007. A Methodological Approach to Clastic Injectites: From Field Analysis to Seismic Modeling—Examples of the Vocontian Aptian and Albian Injectites (Southeast France). AAPG Memoir 87: 783–807. [Google Scholar]
  • Paumard V, Zuckmeyer E, Boichard R, Jorry SJ, Bourget J, Borgomano J, et al. 2017. Evolution of Late Oligocene – Early Miocene attached and isolated carbonate platforms in a volcanic ridge context (Maldives type), Yadana field, offshore Myanmar. Marine and Petroleum Geology 81: 361–387. [CrossRef] [Google Scholar]
  • Pérès JM, Picard J. 1964. Nouveau manuel de bionomie benthique de la Mer Méditerranée. Recueil de la Station Marine d’Endoume 31: 137 pp. Available from [Google Scholar]
  • Peters SE, Loss DP. 2012. Storm and fair-weather wave base: A relevant distinction? Geology 40: 511–514. [Google Scholar]
  • Philip J. 2003. Peri-Tethyan neritic carbonate areas: Distribution through time and driving factors. Palaeogeography, Palaeoclimatology, Palaeoecology 196, 19–37. [CrossRef] [Google Scholar]
  • Pohl A, Laugié M, Borgomano J, Michel J, Lanteaume C, Scotese CR, et al. 2019. Quantifying the paleogeographic driver of Cretaceous carbonate platform development using paleoecological niche modeling. Palaeogeography, Palaeoclimatology, Palaeoecology 514: 222–232. [CrossRef] [Google Scholar]
  • Pohl A, Donnadieu Y, Godderis Y, Lanteaume C, Hairabian A, Frau C, et al. 2020. Carbonate platform production during the Cretaceous. GSA Bulletin 132: 2606–2610. [CrossRef] [Google Scholar]
  • Pomar L. 2001. Types of carbonate platforms: A genetic approach. Basin Research 13: 313–334. [CrossRef] [Google Scholar]
  • Pomar L. 2020. Chapter 12 – Carbonate Systems, in: Roberts D, Bally AW (Eds.), Regional Geology and Tectonics (Second Edition), Volume 1: Principles of Geologic Analysis, pp. 235–311. [Google Scholar]
  • Pomar L, Morsilli M, Hallock P, Bádenas B. 2012. Internal waves, an under-explored source of turbulence events in the sedimentary record. Earth-Science Reviews 111: 56–81. [CrossRef] [Google Scholar]
  • Pomar L, Aurell M, Bádenas B, Morsilli M, Al-Awwad SF. 2015. Depositional Model for a Prograding Oolitic Wedge, Upper Jurassic, Iberian basin. Marine and Petroleum Geology 67: 556–582. [CrossRef] [Google Scholar]
  • Pomar L, Baceta JI, Hallock P, Mateu-Vicens G, Basso D. 2017. Reef building and carbonate production modes in the west-central Tethys during the Cenozoic. Marine and Petroleum Geology 83: 261–304. [CrossRef] [Google Scholar]
  • Purkis S, Casini G, Hunt D, Colpaert A. 2015. Morphometric patterns in Modern carbonate platforms can be applied to the ancient rock record: Similarities between Modern Alacranes Reef and Upper Palaeozoic platforms of the Barents Sea. Sedimentary Geology 321: 49–69. 10.1016/j.sedgeo.2015.03.001. [Google Scholar]
  • Purkis SJ, Harris PM, Cavalcante G. 2019. Controls of depositional facies patterns on a modern carbonate platform: Insight from hydrodynamic modeling. The Depositional Record 5: 421–437. [CrossRef] [Google Scholar]
  • Quesne D. 1998. Propositions pour une nouvelle interprétation sequentielle du Vercors. Bulletin de la Société Géologique de France 169: 537–546. [Google Scholar]
  • Quesne D, Bénard D. 2006. Interprétations nouvelles sur les relations entre calcarénites et calcaires à rudistes du Barrémien inférieur dans le Vercors méridional (sud-est de la France). Geodiversitas 28: 421–432. [Google Scholar]
  • Rankey EC. 2002. Spatial Patterns of Sediment Accumulation on a Holocene Carbonate Tidal Flat, Northwest Andros Island, Bahamas. Journal of Sedimentary Research 72: 591–601. [CrossRef] [Google Scholar]
  • Rat P. 1983. L’Urgonien évolution des idées et des usages. Travaux du Comité français d’Histoire de la Géologie 93–106. [Google Scholar]
  • Rat P, Pascal A. 1979. De l’étage aux systèmes bio-sédimentairesurgoniens. Geobios 12: 385–399. 10.1016/S0016-6995(79)80076-5. [Google Scholar]
  • Reading HG. 1996. Sedimentary environments: Processes, facies and stratigraphy. 3rd edition, Wiley-Blackwell, Oxford, 704 pp. [Google Scholar]
  • Richet R. 2011. High-resolution 3D stratigraphic modelling of the Gresse-en-Vercors Lower Cretaceous carbonate platform (SE France): from digital outcrop modeling to carbonate sedimentary system characterization. PhD Thesis, Université Aix-Marseille, 175 pp. [Google Scholar]
  • Richet R, Borgomano J, Adams EW, Masse JP, Viseur S. 2011. Numerical outcrop geology applied to stratigraphical modeling of ancient carbonate platforms: The Lower Cretaceous Vercors carbonate platform (SE France). SEPM Special Publication Vol. 10, Outcrops revitalized: Tools, techniques and applications, 195–209. [Google Scholar]
  • Rosen BR, Taylor PD. 1990. Reefs and carbonate builds-ups, in: Palaeobiology: A Synthesis. p. 341. [Google Scholar]
  • Sarg JF. 1988. Carbonate sequence stratigraphy. In: Wilgus CK, Hastings BS, Kendall CGsC, Posamentier HW, Ross CA, Van Wagoner JC, eds. Sea Level Changes - an Integrated Approach. SEPM Special Publication 42, pp. 155–181. [Google Scholar]
  • Schlager W. 1981. The paradox of drowned reefs and carbonate platforms. GSA Bulletin 92: 197–211.<197:TPODRA>2.0.CO;2. [CrossRef] [Google Scholar]
  • Schlager W. 2003. Benthic carbonate factories of the Phanerozoic. International Journal of Earth Sciences 92: 445–464. [CrossRef] [Google Scholar]
  • Schlager W. 2005. Carbonate sedimentology and sequence stratigraphy. SEPM Concepts in Sedimentology and Paleontology No. 8, Tulsa, Oklahoma, 200 pp. [Google Scholar]
  • Skelton PW. 2003. The Cretaceous world. Cambridge University Press, New York, 360 pp. [Google Scholar]
  • Skelton. 2018. Part N, Volume 1, Chapter 26A: Introduction to the Hippuritida (rudists): Shell structure, anatomy, and evolution. Treatise Online 104: 1–37. [Google Scholar]
  • Skelton PW, Gili E. 2012. Rudists and carbonate platforms in the Aptian: A case study on biotic interactions with ocean chemistry and climate. Sedimentology 59: 81–117. [CrossRef] [Google Scholar]
  • Skelton PW, Castro JM, Ruiz-Ortiz PA. 2019. Aptian carbonate platform development in the Southern Iberian Palaeomargin (Prebetic of Alicante, SE Spain). BSGF – Earth Sciences Bulletin 190(3): 1–19. [CrossRef] [EDP Sciences] [Google Scholar]
  • Stein M, Arnaud-Vanneau A, Adatte T, Fleitmann D, Spangenberg JE, Föllmi KB. 2012. Palaeoenvironmental and palaeoecological change on the northern Tethyan carbonate platform during the Late Barremian to earliest Aptian. Sedimentology 59: 939–963. [CrossRef] [Google Scholar]
  • Steuber T. 2000. Skeletal growth rates of Upper Cretaceous rudist bivalves: implications for carbonate production and organism-environment feedbacks, in: Insalaco E, Skelton PW, Palmer TJ (Eds.), Carbonate Platform Systems: Components and Interactions. Geol. Soc, London, Spec. Publ 178: 21–32. [Google Scholar]
  • Steuber T, Rauch M, Masse J-P, Graaf J, Malkoc M. 2005. Low-latitude seasonality of Cretaceous temperatures in warm and cold episodes. Nature 437: 1341–1344. [CrossRef] [Google Scholar]
  • Stössel IP. 1999. Rudists and Carbonate Platform Evolution: the Late Cretaceous Maiella Carbonate Platform Margin, Abruzzi, Italy. Memorie de Scienze Geologiche 51(2): 333–413. Padova. [Google Scholar]
  • Teillet T, Fournier F, Montaggioni LF, BouDagher-Fadel M, Borgomano J, Braga JC, Villeneuve Q, Hong F. 2020. Development patterns of an isolated oligo-mesophotic carbonate buildup, early Miocene, Yadana field, offshore Myanmar. Marine and Petroleum Geology 111: 440–460. [CrossRef] [Google Scholar]
  • Tendil A. 2018. Contrôles tectoniques, climatiques et paléogéographiques sur l’architecture stratigraphique de la plateforme carbonatée urgonienne provençale (France) : approches sédimentologiques, géochimiques et numériques intégrées. [Google Scholar]
  • Tendil AJ-B, Frau C, Léonide P, Fournier F, Borgomano JR, Lanteaume C, Masse J-P, Massonnat G, Rolando J-P. 2018. Platform-to-basin anatomy of a Barremian-Aptian Tethyan carbonate system: New insights into the regional to global factors controlling the stratigraphic architecture of the Urgonian Provence platform (southeast France). Cretaceous Research 91: 382–411. [CrossRef] [Google Scholar]
  • Tišljar J, Vlahovic I, Velic I, Maticec D, Robson J. 1998. Carbonate Facies Evolution from the Late Albian to Middle Cenomanian in Southern Istria (Croatia): Influence of Synsedimentary Tectonics and Extensive Organic Carbonate Production. Facies 38: 137–157. [CrossRef] [Google Scholar]
  • Tomassetti L, Petracchini L, Brandano M, Trippetta F, Tomassi A. 2018. Modeling lateral facies heterogeneity of an upper Oligocene carbonate ramp (Salento, southern Italy). Marine and Petroleum Geology 96: 254–270. [CrossRef] [Google Scholar]
  • Tucker ME, Wright VP. 1990. Carbonate sedimentology. Blackwell Science Ltd, 482 pp. [CrossRef] [Google Scholar]
  • van Buchem FSP, Pittet B, Hillgärtner H, Français I, Grötsch J, Mansouri A, Billing IM, Droste HHJ, Oterdoom WH. 2002. High-resolution sequence stratigraphic architecture of Barremian/Aptian carbonate systems in northern Oman and the United Arab Emirates (Kharaib and Shuaiba Formations). GeoArabia 7: 461–500. [CrossRef] [Google Scholar]
  • Vilas L, Masse JP, Arias C. 1995. Orbitolina episodes in carbonate platform evolution: the early Aptian model from SE Spain. Palaeogeography, Palaeoclimatology, Palaeoecology 119: 35–45. [Google Scholar]
  • Walker RG. 1967. Turbidite sedimentary structures and their relationship to proximal and distal depositional environments. Journal of Sedimentary Research 37: 25–43. [CrossRef] [Google Scholar]
  • Walker RG. 1992. Facies, facies models and modern stratigraphic concepts, in: Walker RG, James NP (Eds.), Facies models: response to sea-level change. Geological Association of Canada, St. John’s, Newfoundland, Canada pp. 1–14. [Google Scholar]
  • Wermeille S. 1996. Étude sédimentologique micropaleontologique et minéralogique des calcaires Urgoniens de la région SubAlpine (Savoie, France). Unpubl. Dipl. Université de Neuchâtel, 130 pp. [Google Scholar]
  • Wilkinson BH, Diedrich NW, Drummond CN. 1996. Facies successions in peritidal carbonate sequences. Journal of Sedimentary Research 66: 1065–1078. [Google Scholar]
  • Wilkinson BH, Drummond CN. 2004. Facies mosaics across the Persian Gulf and around Antigua—Stochastic and deterministic products of shallow-water sediment accumulation. Journal of Sedimentary Research 74: 513–526. [CrossRef] [Google Scholar]
  • Wilson JL. 1975. Carbonate Facies in Geologic History. Springer-Verlag, Berlin Heidelberg New York, 471 pp. [CrossRef] [Google Scholar]
  • Wright VP, Burgess PM. 2005. The carbonate factory continuum, facies mosaics and microfacies: An appraisal of some of the key concepts underpinning carbonate sedimentology. Facies 51: 17–23. [CrossRef] [Google Scholar]
  • Yose LA, Ruf AS, Strohmenger CJ, Al-Hosani I, Al-Maskary S, Bloch G, et al. 2006. Three-dimensional characterization of a Heterogeneous Carbonate Reservoir, Lower Cretaceous, Abu Dhabi (United Arab Emirates), in: Harris PM, Weber LJ (Eds.), Giant hydrocarbon reservoirs of the world: from rocks to reservoir characterization and modeling. AAPG Memoir Vol. 88 and SEPM Special Publication, pp. 173-212. [Google Scholar]

Cite this article as: Michel J, Lanteaume C, Massonnat G, Borgomano J, Tendil AJ-B, Bastide F, Frau C, Léonide P, Rebelle M, Barbier M, Danquigny C, Rolando J-P. 2023. Questioning carbonate facies model definition with reference to the Lower Cretaceous Urgonian platform (SE France Basin), BSGF - Earth Sciences Bulletin 194: 13.

All Tables

Table 1

Comparison of bibliographic data supporting published Urgonian facies models. If not specifically mentioned, cited figures refer to the reference paper. See text and Section 5.5 for related comments and localities, respectively.

Table 2

Infrastructure sensu Handford and Loucks (1993) of the Urgonian Platform and facies table.

Table 2


Table 3

Supporting concepts and related Urgonian data and methods used to define the proposed facies model.

Table 4

Supporting outcrop data used to define the main facies associations and related facies model. See text, Table 2 and Figure 7 for related comments, facies association details and localities, respectively.

All Figures

thumbnail Fig. 1

Upper Barremian (M. Sarasini ammonite zone sensu Frau et al., 2018) palaeogeography reconstruction of SE France (modified from Tendil et al., 2018).

In the text
thumbnail Fig. 2

Synthesis of the main works on the Urgonian in SE France and evolution of facies models. The color key for the depositional facies corresponds to that of the Figure 3.

In the text
thumbnail Fig. 3

Conceptual facies model of the Urgonian platform (modified from Masse and Fenerci-Masse, 2011; Tendil, 2018). The blue curve qualitatively describes hydrodynamic trends of facies deposition.

In the text
thumbnail Fig. 4

Composite chronology of key scientific concepts applied to the Urgonian platform characterization (B). (A) The sedimentological concepts are associated with their main bibliographic references (inspired from Kenter et al., 2009).

In the text
thumbnail Fig. 5

Interpretative relative distribution of facies associations according to hydrodynamics as a function of (A) depositional setting and (B) bathymetry, and (C) interpretative quantitative palaeobathymetric ranges of facies associations in the literature from the Urgonian and contemporaneous Middle East settings.

In the text
thumbnail Fig. 6

Characteristic distribution of biota production on theoretical platform profile for Barremian–Aptian (Masse, 1976; Masse and Fenerci-Masse, 2008; Léonide et al., 2012).

In the text
thumbnail Fig. 7

Data support of facies model definition showing occurrence of the main facies per outcrop location and a palaeogeographic interpretation (background shadings; cf. Tab. 4 for data details).

In the text

Current usage metrics show cumulative count of Article Views (full-text article views including HTML views, PDF and ePub downloads, according to the available data) and Abstracts Views on Vision4Press platform.

Data correspond to usage on the plateform after 2015. The current usage metrics is available 48-96 hours after online publication and is updated daily on week days.

Initial download of the metrics may take a while.