The Grès d'Annot Formation comprises sandstones, siltstones, shales and occasionally, not extensively persistent, conglomerates (Appendix 2: Log Correlation). Sandstone domination is recognised in all the Grès d'Annot exposures. The sandstones form more than 70% of the successions in the northern areas (Appendix 2: Log Correlation or figure 6.1a) and up to 95% (Elliott et al., 1985) in the southern outcrop regions Annot, Contes and Menton (Figure 6.1b).

The siliciclastic sediments of the Grès d'Annot Formation have predominantly been interpreted as the deposits of sediment gravity flows (eg. Fauret-Muret, 1955; Kuenen et al., 1957; Bouma and Coleman, 1985; Ghibaudo; 1985). Three facies associations are applied for separating the turbidites in the succession (Apps et al., 1987): GdAI (Picture 6.2.1), thinly bedded sandstones with siltstones and shales; GdAII (Picture 6.2.2), sequences of medium bedded (30cm-2m), rarely sub-amalgamated, sandstones separated by thin siltstones and shales, occasionally with conglomerates; GdAIII (Picture 6.2.3a), comprises from few meters up to 100m thick sandstone beds which are sub-amalgamated to amalgamated, often separated by conglomerates and rarely by heterolithics (Apps et al., 1987).

Today, the entire spectrum of sediment flows driven by gravity, including turbidity currents as one type, has been labeled as sediment gravity flows (Middleton and Hampton, 1973). In a gravity fluid flow, the sediment is moved by gravity, and the sediment motion moves the interstitial fluid. Mechanisms such as suspension (by turbulence), saltation (by hydraulic lift forces and drag) and traction (by dragging and rolling of particles at the bottom) may all operate in some types of sediment gravity flows, as they do in some types of fluid gravity flows.

Gravity flow outlines a series of end members in the continuum of sediment gravity flow processes that take place from the time sediment movement initiates until it ceases at depositional site downstream in a system (Figure 6.1.1a). In all the processes, sediment particles move down-slope parallel to the bed in response to gravity as long as there is sediment support in the flow to keep particles from settling out. The four members are defined on the basis of the grain support mechanisms as follows: turbidity current, in which the sediment is supported mainly by the upward component of fluid turbulence (Figure 6.1.1b); fluidised sediment flow, in which the sediment is supported by the upward flow of fluid escaping from between the grains as the grains are settled out by gravity (Figure 6.1.1b); grain flow, in which the sediment is supported by direct grain to grain collisions or close approaches (Figure 6.1.1b); debris flow, in which the larger grains are supported by a mixture of interstitial fluid and fine sediment (Figure 6.1.1b), that has a finite yield strength (Middleton and Hampton, 1973 and 1976).

Deposits of turbidity currents (Figure 6.1.1c and 6.1.1d), called turbidites, are widely recognised and occur in lakes, seas, and oceans but are most important along the margins of deep marine basins. However, the terminology of a turbidite is frequently used of non sourced turbidity currents, because some sediment gravity flow types evolve from another, and since deposition may occur at any time during the current or flow. Thus, they are difficult to distinguish and an individual bed may represent deposition by a combination of sediment gravity flow processes (Middleton and Hampton, 1976). Other mechanisms, such as traction, may operate during the last stages of deposition and produce or modify textures and structures in the sediment bed that is finally deposited from the current or flow (SEPM Short Course No 14). If the four dividable gravity flow types are deposited singularly, they however, are simple to identify in the field (Figure 6.1.1c and 6.1.1d) (Siemers and Tillman, 1981).

The observed characteristics of the facies in the northern part of the basin, Lac du Lauzanier area, and those of the southern areas, Annot and Peira Cava are most often confirming earlier descriptions. Therefore, the earlier applied GdAI- II- and III facies association from other studies (Stanley et al., 1961) were also adopted in this work. Though to remark, this work is concentrating on the Lauzanier area. The areas of Annot and Peira Cava and other localities from diverse literature, are added to enable this study more complete descriptions and interpretations.

The characteristics of textures and sediment structures of each facies association are described in the chapters below. Typical features for individual facies associations are described and explained separately. However, when the same features are existing in two- or more facies associations, they are arranged prior to the lower facies association GdA-number but also mentioned in the higher GdA-numbers.

This facies association forms approximately 30% of the Grès d'Annot Formation in the Lac du Lauzanier area and much less in the southern outcrops (Picture 6.2.1). It comprises centimetre - decimetre scale sandstones which alternate with siltstones and shales. The GdAI is interbedded with the other two facies associations and is not seen in any outcrop as the lateral equivalent of the thicker bedded facies. Mostly, the finer grained beds are observed as undisturbed, not truncated or channelised. Throughout the succession, thicker sandstone bodies are separated by GdAI, sometimes tens of metres thick (Appendix 2: Log Correlation or appendix 3, Panoramic Pictures: 3.1, 3.2, 3.3 and 3.4). In the area of Lac du Lauzanier a GdAI facies association unit is 28m thick (appendix 2: Log Correlation or appendix 3.1: Panoramic Picture), similar thickness has been located in other northern localities too (Jean et al., 1985). This unit contributes as an excellent correlation marker of size in the northern region. The sandstones are laterally continuous over the traceable lengths of the observed outcrops in the Grès d'Annot basin and do not change in thickness, except where adjacent to the base Grès d'Annot angular unconformity or if the sandstones are poorly sorted. In the Lac du Lauzanier succession the sandstone beds are constant in thickness for several kilometres. These beds only show individual beds and they are neither amalgamated nor sub-amalgamated. The sandstone beds do not exceed a thickness of 50cm. If they do, they are divided into other facies associations. A sandstone bed, with the additional overlying finer grained sediments, are defined as a individual deposit derived from a single pulse of sediment gravity flow. This deposit is called a cycle which may comprise all Bouma divisions (Figure 6.1.1d) or only some of the divisions.

All grades of sandstones are observed in the GdAI facies association, but very fine- to medium grained sand is dominant. They are predominantly Bouma base (ta division) absent turbidites (Figure 6.1.1d). Typical divisions of the Bouma sequences in the Grès d'Annot cycles are: tb - td; tb, td; tb, tc; tc - td. More rare cycles are found with various sequences, starting with ta. Coarser sand are rarely present in these cycles, and if they are, the Bouma division is determined as a Bouma base present (ta - division), which mostly are not continuous. The tb division contains fine- to medium grained sandstone. tc is rather rarely present that comprises fine- to very fine-grained sandstone, frequently easy to observe because of its sediment structures like, ripples and wavy- or convoluted laminae. The plane laminated td division is generally existent in all non amalgamation-influenced cycles. They mostly contain silt-, or coarser grained sediments. They are difficult to observe in the field, though in contrast the tet division of Bouma is often observed. The differences compared with the underlying td division are very close, however, distinguishable through the tet divisions massiveness and its grain sizes are below the silt grain size. The tep division was never observed in the Grès d'Annot succession neither are there any indicators regarding their existence, nor are they mentioned in earlier literature.

All upper contacts of the sandstone beds are usually marked by a sharp grain size break with either graded siltstones or graded shales, frequently with preserved ripple current form (Appendix 2: Log Correlation). Almost all cycles are graded, though with exceptions of inverse grading at the base. Sometimes, the siltstone- or shale beds are displaying undulated- and seldom contorted bedding. Small scale slumps (Picture 6.2.1.1b) and slide marks are rarely but present in the GdAI. Common are however flute- and load casts, groove casts (Picture 6.2.1.1c) and scour surface (Picture 6.2.3.1b). The lower divisions are often accompanied with rip up clasts and fragments of heterolithics, which generally gather at base of the sandstone properties. Mica and organic fragments are concentrated in the finer grained sediment at the top of the bed and they define the laminae.

If applying the Lowe's (1982) summary figure (Figure 6.2.1.1a), which display sediment gravity flow type indicators, the deposited GdAI facies association must be classified as derived from low density turbidity currents. This conclusion is provided due to the sedimentary textures and structures of the cycles observed in the Grès d'Annot outcrops, like: Bouma base (ta) absence; if sandstone is present at base, grain sizes below medium grained sandstone are dominating; the cycles are well graded, whereby plane bedding and lamination are common, the lack of amalgamation and very well preserved, and mostly undisturbed, sequences of the Bouma divisions which are even emphasising the tet divisions. Further application of the Siemers- and Tillman's (1981) idealised sequences of sedimentary textures and structures (Figure 6.1.1c), which also includes base structures, implies that the gravity flow type of the GdAI facies association also must be concluded as a turbidity current. Based on the same features as mentioned (details, chapter 6.2.1 and figure 6.2.1.1a: application of Lowe's (1982) summary upon the GdAI facies association) and the additional sediment structures at base such as flute marks and tool marks. The upper contacts of the sandstone beds, marked with a sharp grain size break with either graded siltstones or graded shales and the preserved ripple current forms are either indicating a bypass of finer sediments or subsequent erosion.

The appearance of small-scale slumps (Picture 6.2.1.1b) and slide marks, mostly occurring in the fine grained sandstones of all facies associations, and the presence of micro-faults, which show close spacing, suggest that they were formed syn-sedimental. Most likely, these features formed, because the surface of the basin was irregular and initiated slight sedment failure down slope. However, no certain evidence was found regarding the down slope dipping direction, because the direction of the slumps and the slide marks are internally divagating strongly. The micro faulting is clearly visible in the well-defined laminae, particularly in the sandstones but also in finer grained beds.

Flute casts occur in swarms at the underside of beds, preferably at the uncommon ta-, and at the common tb division. Sometimes, flutes are associated with grooves, whereas the grooves rather tend to appear in the GdAII- and GdAIII facies association. The flute marks range from 5 - 30cm and are sub-conical structures with a rounded or bulbous up-current nose, the other end flaring out and merging with the bedding plane. They become their forms because current scour is burying holes in the unconsolidated surface which then are filled with coarser grained sediment.

The groove casts are raised, rectilinear, rounded to sharp-crested features (Picture 6.2.1.1c). Like the flutes, they seldom appear single but in sets. The observed grooves were mostly parallel, sometimes as two sets intersecting at an acute angle on the same surface. Normally, their relief is only a few millimetres, occasionally some centimetres. Mostly, they do not display their beginning or end. If they do, the beginning is abrupt and perpendicular to the surface, while the end is merging very smoothly with the surface. Their origin is the result of tools swept away by current, which engrave the surface of a relatively firm mud bottom (Pettijohn, Potter and Siever, 1987). Since both flutes and grooves are the product of current they are excellent paleo-current direction indicators.

Another current produced sedimentary structure is the rare featured parting lineation. However, it was only found at unconsolidated rock surfaces, except at one occasion, in the field. Therefore, this sediment structure could not serve as a paleo-current direction indicator. The reason for this is, they are dominantly present on fine-grained sandstone bed surfaces, which are not accessible in outcrops. They display sands that separate along bedding planes forming very regular flags, which are related to grain alignment (Bates & Jackson, 1984).

The ripple current marks are sited regularly throughout the Grès d'Annot Formation in the tc division (Picture 6.2.1.1d) . They form when sand is transported up the stoss side and avalanches down the lee side, causing the ripple to migrate downstream without any change in the level of sedimentation. However when sand is added to the system, the rate of accumulation of the lee side increases and each ripple climbs the backslope of the one in front of it to form climbing ripples. These are not as frequent as the simple marks, but are still often preserved. The sited low angles of the climbing ripples and the fact that the normal ripples are dominant, indicates a high flow regime. Since the sediment is swept to the lee side, not letting the ripples climb and mostly they were hindered. According to Pettijohn, Potter and Siever (1987), there might be a link between deformed ripples and convolute bedding, when the latter is perhaps an extreme end-product of ripple deformation.

Convoluted lamination is a common sediment structure in the upper divisions of the Bouma sequence of GdAI- and GdAII facies association, though preferably in the silty dominant td division. However, these folds or convolutions affect the laminations within a bed but not the bed itself (Pettijohn, Potter and Siever, 1987). Numerous authors suggest this appearance to have formed because of vertical transfer of material, which indicates some kind of internal readjustment of sediment in a quick or near-quick condition (Potter and Pettijohn, 1977).

Since the GdAI facies association is showing constant lateral continuity of units as well as of individual beds, it is only disrupted by one single truncated and channelised exception. It surely was not deposited on channel levees or between major distributary channels or canyons. Definitely, this part of the period during the Grès d'Annot deposition, reflects the lowest rates of sediment influx into the basin. This fact is confirmed by Mutti and Nordmark et al. (1987), which describe that the finer grained sediments are deposited much slower than the coarser grained sediments. Still the siliciclastic supply was relatively high, imaginable as a result of the low amount of shales and few detritus of the partly eroded underlying calcareous formations which were dissolved and flushed away. Additionally, the average sediment fill of the basin was very rapid (Chapter 4.2. and Figure 4.2b).

The characteristics of the GdAII facies association are recognisable, in contrast to the GdAI, through the increased sandstone thickness and the decreased spacing between the interbedding of the sandstones compared to the siltstones and shales (Appendix 2: Log Correlation and picture 6.2.2). Normally, the facies is separated through siltstone or shale, or both, but sometimes they are missing as a result of amalgamation. This erosion must be considered as partly amalgamated, or as a sub-amalgamation, since only the finer grained sediments are truncated. More intensive amalgamation was not observed in this facies. Cycles, which are influenced by amalgamation, never exceeds a thickness more than 1.5m. A bed influenced by sub-amalgamation easily exceed thicknesses of 1.5m, which in this case are multi-cycle deposits derived from more than a single pulse of sediment gravity flow. Several multi-cycle deposits can also form units, which are up to 5m thick within the GdAII facies association. Additionally, it features more preserved sedimentary structures, especially in the ta- and tb division, which are thicker and more common compared to the GdAI facies association. However, the first centimetres of the ta division is often crude and therefore devoid of structures. This crudeness of the layers is decreasing upwards and delineating the grain size of the layers more clearly, sometimes even defining small graded units, which thin upwards.
These divisions are comprised by medium- to very coarse-grained sandstones (Figure 6.1.1d). These structures record the sediment gravity flows, for example: grading; parallel- and cross-lamination; convoluted- and low angle cross-bedding and dish structures. Well preserved are also soil marks like, groove casts; load casts; flute marks; slide marks and flame structures.
A complete Bouma sequence, except the absent tep division, is occasionally preserved in the Lac du Lauzanier succession. More commonly featured divisions of the Bouma sequence in the GdAII facies association are: ta - td; ta, tc - td; ta, td; tb - td; tb, tc; tc - td. The lower divisions are often accompanied with rip up clasts and fragments of heterolithics that generally gather at base of the sandstone properties. Mica and organic fragments are concentrated in the finer grained sediment at the top of the bed and define the laminae.
Individual beds are observed as laterally extensive and predominantly of uniform thickness across the Lac du Lauzanier area (kilometres). Exceptions to this fact are only seen when adjacent to the basin floor or once sandstone beds are immature, poorly sorted and heterogeneous. Ghibaudo (1985, pers. comm.) and Jean (1985) have logged many sections through the outcrop areas of Col de la Cayolle, Trois Eveches and Grand Coyer. They demonstrate that these bodies and individual beds are lenticular over distances of kilometres. However, the precise geometries cannot be defined because correlation between outcrops is still speculative. Abrupt lateral terminations are rare, seen only at the basin margins and the edges of the few observed. For the most part, it can be assumed that the facies laterally grades into thicker or thinner bedded facies associations, anyway, this is found at some localities.

If applying the Lowe's (1982) summary figure (Figure 6.2.1.1a), which display sediment gravity flow type indicators, the deposited GdAII facies association (Picture 6.2.2) must be classified as derived from rather moderate-, accompanied with high, density sandy turbidity currents. This interpretation is based on coarser grain size than in the low density turbidity currents, the lack of clay matrix, the dominance of massive sandstone, the common presence of normal- and occasional inverse grading and the undulated bedding that probably is caused by the dish structures. Further application of the Siemers- and Tillman's (1981) idealised sequences of sedimentary textures and structures (Figure 6.1.1c), which also includes base structures, show that the gravity flow type of the GdAII facies association must be concluded as a mixture between turbidity current and fluidised flow. Based on the same features as mentioned (details, chapter 6.2.2 and figure 6.2.1.1a: application of Lowe's (1982) summary upon the GdAII facies association) and the additional sediment structures observed at base such as, groove casts, load- and flute marks, flame structures and tool marks.

Cross bedding is a rare feature in the GdAII facies association. If they are present in the Lauzanier area, they are mostly found in the tb division and in upper parts of the ta division, as single set 10 - 25cm set height. Here they are however not found in the lower super-cycle of the succession. In the upper super-cycle, they are dipping with a maximum of 25°, normally comprised by medium grained sandstone. At Peira Cava, 20cm set height cross bedding is preserved beneath a sediment drape of shale and thin sandstones. The sandstones forming the cross bedding are well sorted and medium grained, dipping eastwards with a maximum of 30° and are asymptotic towards the base of their beginning. Former authors are deviating strongly regarding the interpretation of the cross bedding appearance in the Grès d'Annot Formation. Bouma and Coleman (1985) interpret this bedding as lateral accretion surfaces forming point bars within small-scale channels. Contrary, Allen (1970) assigns forsets of mega-ripples, preserving the morphology of the bedform displaying both the stoss and lee surfaces. According to Lowe (1982) and Apps (1987) both theories are disproved. Allen's theory is deniable because the foresets mega-ripples features storm waves or tidal current bedforms, which are not present. Bouma- and Coleman's (1985) hypothesis is dismissed since two foresets mega-ripples are present in the Peira Cava area. Lowe (1982) and Apps (1987) implies, therefore, that the gravity flows were responsible for all the cross bedding observed, supported through divergent paleo-flows which suggests opposite secondary currents to develop while the primary turbidity current encountered the slope. These entire hypothesis are either supported- or disproved of more recent research, such as Ravenne (1987), Sinclair (1993 and 1994), Midtun (pers. comm.).

According to Stanley (1975) and Nagahama et al. (1975) dish structures are most common in the sandstones of turbidites (Picture 6.2.2.1a). They also propose that the escaping water from rapidly deposited sands must be the origin of their existence (Tucker, 1985). Hereby, either the moderate- or high density sandy current are accompanied by finer grained sediments which are not separated before deposition. Under ideal circumstances, like deposition of a water rich fluidised flow, the captured water is forced to percolate upwards, driven by gravity of the density differences between sediment and water, in coherence with the overburden. During this syn-sedimentary phase, the finer grained sediments are able to be displaced and transported by initial laterally percolating water and assemble relatively impermeable laminations in water drainage pathways. This fine-grained lamination breaches when the escaping water has a sufficient strong vertical component to percolate upwards, enabling the dish structures to form their characteristic shape (Picture 6.2.2.1b).

Load casts are frequently observed sediment structure at base of beds in all the studied areas. They are bulbous, mammillary or papilliform downward protrusions filled with sand, produced by convective-like pattern of motion, which result in a vertical transfer of material. Such material is initiated by an unstable density stratification, such as occurs where a bed of sand is deposited on a less dense, water-saturated finer silt or clay (Pettijohn, Potter and Siever, 1987). The load casts may also become sack-like, then they are called pouches, if these become detached and sink downward, they are called load balls. All these structures are found in the area of Peira Cava.

The presence of sub-amalgamated beds become valid if the sandstones of the GdAII facies association are thicker than approximately 1.5m, which is often seen in the field (Appendix 2: Log Correlation). Thus the thicker sandstone beds do not comprise a constant individual upward fining but several upward fining beds, obvious through the abrupt grain size breaks at varying intervals. Therefore, this characteristic is called sub-amalgamation and not amalgamation. The sub-amalgamation took place because a sediment gravity flow eroded the upper divisions of the Bouma sequences of an already deposited and unconsolidated gravity flow. In most cases, resultants of only the ta and tb remained deposited, providing thicker sandstone beds to generate, which therefore are multi-cycle depositions.

Near the base of an individual cycle, or widely spread in a multi-cycle, there is a frequent presence of rip up clasts in all the studied areas but especially in the area of Lac du Lauzanier. Their length varies from millimetre - centimetre scale, whereas the relief is up to 50% less than the length but mostly smaller. They are rectangular, sometimes rounded at the ends. Generally they comprise heterolithics, occasionally a content of fine-grained sand and calcareous rip up clasts are found. These rip up clasts indicate erosion, whereas the lack of their roundness implies a rather short transportation distance and therefore is interpreted as derived from a local origin. Their existing is explained through an encountering gravity flow, which erodes its substrate that must have been relatively well consolidated. These ripped off clasts, predominantly from thin-bedded GdAI facies association, are then transported shortly by the gravity current and deposited as one of the first fragments of the current. Sometimes these rip up clasts are observed as being layered higher as in other cycles, which in this case must reflect a relatively stronger current as the lower layered rip up clasts. Another explanation for the existing rip up clasts may be the upward escaping water which percolate the layers of the siltstones and shales (details, chapter 6.2.1.1.), these may generate a disruption of these layers, causing their rip off without being influenced by an eroding gravity flow.

Locally, in upper parts of a cycle, concentrations of plant debris are very high. According to Apps (1987) Individual fragments may be 10s of centimetre long, with well preserved biological structures. They are have a bright surface sheen and are very brittle and fragile. Their excellent preservation indicates that the plant remains were transported and deposited rapidly, without being repeatedly reworked in well-oxygenated waters. Further the organic matter implies that the Grès d'Annot Formation were neither affected by deformation nor igneous activity or mineralisation, since the maximum temperatures almost certainly reflect the burial history of the formation (Elliott, 1985).

This facies association includes single sand beds greater than approximately three metres thick and composite units, either produced by sub-amalgamation or less common by amalgamation (Picture 6.2.3a and the appendix 3, Panoramic Pictures: 3.1, 3.2, 3.3 and 3.4). Characteristic is their lack of siltstone and shale, but presence of conglomerates. (Appendix 2: Log Correlation). Just above the lower super-cycle in the area of Lac du Lauzanier a composite unit of 38m thick sandstone body is displayed, without being interbedded by heterolithics (Appendix 2: Log Correlation, Log 2). However, outcrops in southern regions even exceed thicknesses of 38m of a single sandstone body and the successions are predominantly formed by this facies association, which is not the case in northern regions (details, chapter 6.3.). Normally, these sandstone bodies extend laterally unchanged for several hundreds of metres and they are most often discontinuous, but also continuously, over distances of several kilometres (Appendix 3.3 and, especially, 3.4: Panoramic Pictures and appendix 2: Log Correlation). According to Apps et al. (1987) sandstone bodies in southern regions are also exceeding thickness of 50m. These composite units shall also be continuously for several kilometres.

The sediment structures most often record post-depositional processes like dewatering and, more rarely, the original sediment transport processes. The base of the bed is flat or undulated, on a decimetre scale. Grooves and load casts are uncommon features at the underside of beds. The sediments beneath are often undisturbed, but may be disrupted by flame structures, small scale sandstone dykes and decimetre folds. The base of the lower parts of the GdAIII facies association multi-cycles contains mostly a chaotic layer, overlain by massive sandstone which often are accompanied with dish structures. Sometimes, these may together vary from thicknesses of 3 - 5m, without exhibiting any significant grading. These bedding are no longer sub-amalgamated, but amalgamated, since no more grading or the breaks of the multi-cycles are recognisable. Neither are the breaks between the chaotic- and massive layer identifiable. If no chaotic layer is present, a coarsening upward is preserved in single cycles, or accordant, more grading intervals in multi-cycles. Inverse grading is rare, but observed more often as in other facies associations. Hereby, the base is mostly medium grained with much pebbles, overlain by coarse- to very coarse-grained sandstones and conglomerates.

The sandstones contain few pebbles and rip up clasts with variable bedding types (Appendix 2: Log Correlation). In a chaotic- and massive layer the rip up clasts might become up to 70cm long (Picture 6.2.3b). Other, similar heterolithic bodies can measure many metres, which then are determined as slides (Picture 6.2.3b). The derived rip up clasts indicate if the layer is chaotic or not, whereby no alignment implies a chaotic layer. In contrast, imbricated rip up clast is present either in sandstone with massive or graded bedding. Similar indicators are often imbricated pebbles, whereas the pebble c-axis reflects the direction of the paleo-current. Parallel bedding does not appear at lower sections of the multi-cycles but only in the upper sections of individual- or multi-cycles (Appendix 2: Log Correlation). Here are also low angle cross stratification observed even further below the parallel bedding limit.

The interbedded conglomerates are seldom observed as an individual bed or at the base of a unit. Their upper- and lower breaks are mostly sharp, whereas the underlying- or overlying beds compose various grain sizes, ranging from medium to very coarse grained sand. Peculiarly, these beds do not necessarily comprise a high amount of pebbles, and their size may also become as slightly bigger as 0.2cm (Appendix 2: Log Correlation). The conglomerates are also truncating the substrative sandstone beds, generating small-scale channel-like features (Picture 6.2.3c). The opposite is also true, as overlying sandstones are truncating about 2m of a conglomerate bed (Appendix 2: Log Correlation, Log 2 and picture 6.2.3.1a), generating a small-scale channel-like appearance. The base adjacent channel fill is characterised by a thin bed of matrix supported, low pebble content, conglomerate. This is overlain by a well sorted, coarse grained, sandstone. On one occasion, an interbedded siltstone and shale unit overlies a conglomerate (Appendix 2: Log Correlation, Log 5). Often the conglomerates show a grading, whereby the base of the conglomerate beds commonly are pebble supported. Thus upwards, it becomes more matrix supported. The base may contain pebbles up to 8cm in the Lac du Lauzanier area. In southern regions, much larger pebbles are observed, such as a granite boulder of an approximately diameter of 1.4m in the area of St. Antonin (Picture 6.2.3d). Boulders of this size are very rare and strictly limited to the southern region, where even a clast diameter is reported to be up to 8m (Elliott et al., 1985).

The upper break of a conglomerate bed, generally, is suddenly transitioned by finer grained sediments. Thus, other rare conglomerate beds are continuously graded without abrupt breaks (Appendix 2: Log Correlation, Log 5). Internally, conglomerate beds may show dividable beds in a conglomerate unit (Appendix 2: Log Correlation, Log 2), implied by the sudden changes of pebble sizes. The bed thickness ranges from a few centimetres and exceeds 5m. These thick conglomerate beds are composite units. The thinner beds rather trend to interbed between amalgamated sandstones and as base fill of small scale- and the only observed large-scale channel in the Lac du Lauzanier area. They are never pebble supported and even trend to contain low amounts of pebbles, sometimes transiting to pebble-rich sandstone. The thicker conglomerate beds seldom carry rip up clasts in their pebble supported bed parts, whereas in contradiction, up to 50cm long rip up clasts are often featured in the matrix supported conglomerates. All the conglomerate beds have in common that they comprise well to very well rounded pebbles, which are moderately- to poorly, sorted. The content of pebbles differs strongly, apparently controlled by their size of pebbles, which approximately reaches up to 50%. The residual content is made up of poorly sorted sand and matrix. The pebbles never show alignment, except sometimes in the beds with low pebble content. Such exceptions are found in thinner- or at top of thicker conglomerate beds, but especially at the base of a channel fill. In the Lac du Lauzanier area, all the conglomerate beds are discontinuously. Pinch out occur often, sometimes even both bed ends are seen, implying an extension below 100m but maybe more on occasions since they are not always traceable in outcrops.

Former authors have described the GdAIII facies association, which is emphasising conglomerate beds and composite beds of sandstones exceeding thicknesses of 50m, with very diverse interpretations. Mostly the authors concentrate their work on the southern region, whereas the northern region is studied more recently. Some of these authors are: Stanley (1982); Cremer (1983); Jean (1985); Elliott (1985); Ravenne (1985 and 1987); Apps (1987); Sinclair (1993 and 1994); Midtun (not finished PhD thesis). Stanley (1982) interpreted examples at Contes and Peira Cava as welded slumps and turbidites. He implies that turbidity currents generated from submarine slides which evolved first into slumps and then into turbidity currents. Cremer (1983) interpreted them as deposits of high-density turbidity currents, using as a basis the model of Lowe (1982) (Figure 6.2.1.1a). The other authors predominantly approve of the interpretation of high density turbidity currents, except a hypothesis of Sinclair, who is implying a much shallower facies of a delta-near deposition.

If applying the Lowe's (1982) summary figure (Figure 6.2.1.1a), which displays sediment gravity flow type indicators, the deposited GdAIII facies associations (Picture 6.2.3a) must be classified as derived from high density currents. The sandstones scoured tops and imbricated clasts near the bases indicate that the base of the flow was turbulent. The conglomerates imply probably deposition from poorly disorganised bed load high-density turbidity currents. Further application of the Siemers- and Tillman's (1981) idealised sequences of sedimentary textures and structures (Figure 6.1.1c), which also includes base structures, show that the gravity flow type of the GdAIII facies association must be concluded as being deposited by fluidised flow and even by grain flow, considering the present conglomerates. Predominantly, this is based on the emphasised scours at base of beds, which suggest traction current to erode substrate. Additionally the base is normally poor graded, if at all. Relatively frequent inverse grading is present, compared to the other facies associations. The grains are often imbricated in massive sandstone beds. As in the GdAII facies association a repeating of sediment features are observed like: dish structures at higher parts, load casts of the underside of beds, flame structures and convolute bedding adjacent bed top.

The scours become more frequently in the upper super-cycle (Picture 6.2.3.1a), where the presence of the sand-rich GdAIII facies association is dominant. They are never seen in the GdAI facies association but appear rather sporadically in the GdAII facies association. At some levels in the upper part of the Grès d'Annot succession in the area of Lac du Lauzanier, they are represented as numerous representatives on an individual bed, mostly sandstone, surface (Picture 6.2.3.1b). Each representative on an individual bed surface is strictly aligned, without exceptions. Sometimes, they do not seem to occur in such numerous examples in other levels (Picture 6.2.3.1a).
In both cases, their shape is rather uniform. Formed as small-scale channel-like features. On the bed surfaces in the field, the outset is abrupt, mostly very steep, and sometimes even perpendicular. Their trough are observed as of minor extension but may exceed 5m. Though, the trough are believed to extend much more, since their appearance in outcrops does not show their whole structure. Especially their abrupt outset, which rather seems to be an erosional- than a traction caused outset. At the end, they merge smoothly with the bed surface. In sections, the relief of small scale channel-like through may reach up to 4m. Their fill is characterised by imbricated fragments, such as pebbles and more rare rip up clasts. Further, compared to the neighbouring rock, they distinguish through their well sorting and different grain sizes with low content of pebbles. Obviously, these small-scale channel-like features must be interpreted as traction process resultants of turbulent currents (Picture 6.2.3.1b).
This interpretation may be extended further, and explain the up to 38m of composite sandstone units. As mentioned, they are common in the upper super-cycle in the area of Lac du Lauzanier. Their existence and extension observed in outcrops implicates that high density turbidity currents must have had significant turbulence forces to erode small scale channel-like features over substantial extensions (Picture 6.2.3.1b). If such strong currents are encountering the bottom surface of the basin at regular intervals, heterolithics may certainly not settle long enough to deposit and consolidate, or if they may deposit at all. Even if the currents are not strong enough to generate small-scale channel-like features, they certainly still are capable of eroding and hindering the layering of finer grained sediments. Therefore, composite sandstone units record periods of deposition with either: close interval encountering high density turbidity currents, which prevent heterolithics to settle, or strong enough turbulence to erode finer grained sediments, or possibly a mixture of both influences. These currents must also be interpreted as the origin for sub-amalgamation and amalgamation. In cases were heterolithics are observed between the GdAIII facies association, they were able to deposit and consolidate over a sufficient period of time, avoiding terminable encountering currents. Thus, these appearing heterolithics, neighbouring composite units, often seem to be discontinuous or occurring with variable thicknesses in the outcrops (Appendix 2: Log Correlation). This implies that the turbulent currents are locally eroding the heterolithics. Nevertheless, considering the overall appearance of the Grès d'Annot composite units, individual pulse of a current eroding finer grained sediments must be interpreted as, not local, but extensive.

When interpreting the conglomerate beds, it is important to keep their significant contrasts of characteristics in mind. These beds may comprise pebbles up to 8cm, which are pebble supported and occupy approximately 50% of the total rock content. Gradually, their fining increase to the transition zone between conglomerate and pebble-rich sandstone. Within this range, many types of conglomerates are represented in the Lauzanier outcrops. The finer conglomerate beds are well sorted, often pebble alignment occurs and the base is predominantly scoured. Obviously characteristics are similar to the sandstones in the GdAIII facies association and therefore also must be interpreted as deposits of traction currents, derived from high-density turbidity currents (Figure 6.1.1a, figure 6.1.1c and figure 6.2.1.1a). The coarse conglomerate beds, however, show poorly- to moderately sorting and normally absence of parallel- or cross bedding and diverting erosive or non-erosive base. Thus, no evidences provide distinct interpretation of gravity flow type advancing the deposition of coarse conglomerate beds in the Lac du Lauzanier succession. Since the diverse characteristics are present, two flow regimes must have controlled the sediment distribution. Definitely high-density currents contributed to the partly erosive bases and light grading. Concerning the relatively coarse conglomerate beds, emphasising non-erosive bases and more poorly sorted conglomerates and total absence of sediment structures, implicate a more cohesive type of gravity flow. If the characteristics of southern regions sited conglomerate beds in outcrops are included, the hypothesis of the cohesive gravity flow existence is further supported. Here, a high percentage of conglomerates show very poor sorting with rare examples of boulders (Picture 6.2.3d) and no grading or sediment structures. These deposit features certainly demonstrate that they derived from a strong cohesive gravity flow. Authors imply, based on the respective characteristics, that these flows were debris flows (Cremer et al., 1983). At some sites, the break of the conglomerate bed top is abrupt and overlain by much finer grained sediments without significant proportions of even small pebbles (Appendix 2: Log Correlation, Log1, Log 2 and Log 5). Another example even emphasises a thin conglomerate bed overlain by thin interbedding of heterolithics (Appendix 2: Log Correlation, Log 4). These features may suggest either an erosion of substrata or a bypass of sediments. Nevertheless, since no erosional structures were observed a sediment bypass indicates to be the nearest explanation.

Especially in the upper super-cycle, near its base, metre scale slides seldom appear between composite sandstone units of the GdAIII facies association (Picture 6.2.3b). These bodies are determined as GdAI facies association heterolithics, which have been displaced from their former depositional locality. Because of remnants significant size, the sliding apparently started when bodies already obtained a sufficient consolidation and could not to be dissolved or substantially damaged while moving. Slides observed in the field do, in fact, not show any damaging at all, implicating displacements of rather short distances. The timing of this strong sliding phase is certainly connected with the sudden change of facies association of the lower- and upper super-cycles. The base of the upper super-cycles is eroding its substratum heavily (Appendix 2: Log Correlation). During this most considerable erosion period of the Lauzanier succession, severe erosion may have caused local small-scale slope failures and initiated bodies in substratum to tear off and slide. It is certain that tectonic activity is not the cause of slope failure at any stage during the sliding phase, considering the upper super-cycle being devoid of synsedimentary structures. Obvious characteristics of such slide bodies show slide marks at their underside. The marks are parallel aligned striations which form while slides are descending (Picture 6.2.3.1c).

On rare occasions flame structures are observed at bases of sandstones. These sandstones are strictly associated with an underlying interbedding of a heterolithic bed. The flame structures are consisting of flame-shaped plumes of mud, whereas the mud plumes colour darker than surrounding sandstones and therefore are easily recognisable in the field. Their scale reaches amplitudes of approximately 10cm. Their existence originate from substrate mud, which is squeezed upward, mostly, into sandstone, beds. These post-depositional structures indicate differential settling and compaction (Bates & Jackson, 1983).

Another, sometimes, present post-depositional feature of the GdAIII facies association is sandstone dykes. Their formes are sharp edged, straight-walled and the latter is contorted, whereas their width reach few centimetres and their length is observed as exceeding 50cm. They generate when water-rich sediment is deposited and pressure may turn the sand quick. These sands are capable of injection into fissures and produce dykes.

The ratio of facies associations varies across the Grès d'Annot basin, with higher proportions of GdAI and II associations in the northern outcrop areas (80%) and large, massive sandstone bodies in the south (Apps, 1987). Thus, the southern part of the region contains much higher sandstones/heterolithics ratios than the northern outcrops (Figure 6.1.1a and b).

Compared to Grès d'Annot successions in other northern areas, the quantitative content of the sandstones/heterolithics ratio of the Lauzanier succession is very low (Figure 6.3.1). The variations are not gradual and may reflect compartmentalisation of the basin (Apps, 1987). They are laterally continuous over distances of 100s of metres, and even up to several kilometres (Appendix 3: Panorama Photos).

GdAI and II facies associations (Appendix 2: Log Correlation) are dominating the lower part of the 615m thick Lac du Lauzanier succession. In the upper part, their appearance decreases dramatically. In contradiction, the GdAIII facies association dominates the upper- and is less present in the lower part of the Lauzanier succession. Therefore, the complete succession is clearly dividable into two, almost equally thick, lower- and upper super-cycle (Appendix 3: Panorama Pictures, or appendix 2: Log Correlation). Hereby, the lower 325m thick super-cycle contains about 40% of the GdAI-, 55% of the GdAII- and 5% of the GdAIII facies association. In contrast, the 290m thick upper super-cycle comprises about more than 50% of the GdAIII-, 30% of the GdAII- and approximately 10% of the GdAI facies.

When calculating the sandstone/ heterolithics ratio of the entire Lauzanier succession, sandstones are dominating with 63% while the heterolithics are represented by an amount of 37% (Figure 6.3.1).
The distribution of sandstone/ heterolithics ratio is dividable into three distinguishable parts, based on noticeable divers parts of ratio appearance in the composite log (Appendix 2: Log Correlation). The lower super-cycle of the Lauzanier succession is dividable into two parts. They differ slightly while the lowest part, with ratios ranging from 1.35 to 2.60, is somewhat coarser than the middle part, with ratios ranging from 0.91 to 1.09 (Appendix 2 Log Correlation). The upper super-cycle is in contrast very significantly distinguishable from the lower parts, since the coarse sediments are dominant with ratios varying from 5.10 to 11.68 (Appendix 2: Log Correlation). A characteristic trend is revealed when comparing the logs sandstone/heterolithics ratio with each other. The base part of the succession comprises the lowest ratios in log 4, the most western one. When comparing the middle part between log 4 with the more- log 3 and most eastern located log 5, a reversible ratio is observed as log 3 contains the lowest ratio (Appendix 2: Log Correlation). In the upper super-cycle, the most eastern located log 5 is displaying the lowest ratio. Obviously, this data emphasises a trend, whereas the lower ratio move eastwards and the coarser sediments increase their deposition westwards. Apparently these distinguishable ratios depending on their locality, provides an interpretation of an eastward moving depo-center in the local basin area. During the deposition period of the middle part of the lower super-cycle, the depo-center was nearest the log located in the middle (Appendix 2: Log Correlation).

Channels are present throughout the Lauzanier succession, principally in the upper super-cycle in the GdAIII facies association. Nearly all observed channels exhibit small scales (details, chapter 6.2.3.1. and picture 6.2.3.1a). However, there have been recognised two large-scale channels, one in the Lauzanier- and one in the Peira Cava area. Other large-scale channel-like shapes have been reported from other sites. The channel interpretation is based on their structure and shape that indicate large-scale channel-like features. In Lauzanier area, it is located between the boundary of the lower- and upper super-cycle (Picture 6.4a and b or appendix 2: Log Correlation, especially Log 2). The boundary of the super-cycles is recognised as erosive and oblique. Here, the GdAIII facies association of the upper super-cycle base is variably truncating the substrative GdAI facies association of the lower super-cycle top. On one occasion the characteristics of a large-scale channel-like structure is discerned. This boundary is asymmetrically, convex-shaped and scoured by more than 15m (Picture 6.4a and b). Chaotic layers (details, chapter 6.2.3) comprise the neighbouring rock of the channel-like fill in GdAIII facies association. The lower part of the channel-like feature is neighbouring the heterolithics of the GdAI facies association. In contrast to random rock, the erosive channel fill are amalgamated, well sorted and dominated by coarse to very coarse sandstones with few rip up clasts and low amount of pebbles. Grading is not recognisable, however thin beds of conglomerates with relatively low amount of pebbles are interbedded with massive sandstones. The abundant aligned clasts, both in the conglomerates and sandstones, predominately show a northwestern - southeastern directed imbrication of the clast c-axis. Since the trough-parallel axis of the channel is pointing to southeast - northwest and the cut of the outcrop is roughly north - south directed and dipping with 33°, a very false image of the channel is being exposed. If rotating the channel back in its original position, considering the dips of the channel-sides and the inclined cut, a symmetrical structure is the outcome. Then the true width of the channel is approximately 84m.
Another large-scale channel is preserved in the area of Peira Cava, located 64km southeast of the area of Lac du Lauzanier (Picture 6.4c). Even this channel is located in the upper part of the Grès d'Annot succession and comprises similar channel fill as that of the Lauzanier channel. It is also truncating GdAI facies association, leaving an oblique boundary. The channel is estimated as 110m wide and its relief is approximately 25m, which is somewhat larger than the Lauzanier channel. Unfortunately, the outcrop is limited in vertical and lateral extension, not revealing enough to obtain an overview of the channel positioning in the succession. Thus, an effort in correlating the Peira Cava- and the Lauzanier channel would be speculative.
According to Sinclair et al. (1994) another large-scale channel-like feature is sited in a Grès d'Annot outcrop in the southern Trois Eveches area, between Sommet de Denjuan and Le Grand Croix (Figure 3.2: locality map). This large-scale channel-like feature is even more significant in size as the other channels mentioned above. It is 1km wide and truncating up to 50m of the underlying heterolithics (Hilton, 1995). By comparing the description of this channel characteristics (Sinclair, 1994) with the other two channels, but especially with the Lauzanier channel, they may almost seem identical. Besides, the similar characteristics, they are also located at the same position in their respective successions. Exactly between the erosive boundary between the lower- and upper super-cycle. Furthermore, both channels are directed equally, to the northwest. These two areas siting the channels are about 30km apart from each other (Figure 3.1), whereby the Southern Trois Eveches is located southwest of the Lac du Lauzanier area. Thus, these two channels cannot be one and the same channel, since they are parallel directed. Apparently though, their active period indicates analogous timing. Therefore, a hypothesis suggests a strong relationship of both channels such as; both are belonging to an analogous timed distributary channel system of regional scale.
If comparing the main types of channel fill model (Picture 6.4d) from Mutti and Nordmark (1987) with characteristics of the featured channels in the Grès d'Annot Formation, they demonstrate mixed channel-fill deposits. This type of channel is transitional between an erosional- and depositional channel type (Mutti and Nordmark, 1987).

Locally, in the area of Lac du Lauzanier, individual thin beds are correlational at a kilometre scale (Appendix 2: Log Correlation). This condition is complied by Logs 1, 2, 3 and 4. However, correlating distinct thin beds in Log 5 with the other logs could only be done roughly. Thus, no lateral geochemical analysing was possible, or too risky. Thicker beds or composite units could be associated with all logs. Generally, the correlation of heterolithic beds is simpler than coarser grained sediments, because of their hydraulic abilities to be transported and expand over enormous distances in submarine environment. In the lower super-cycle they predominantly provide excellent correlation between different logs. Though, in the upper super-cycle, this definitely is not the case, as the coarser-grained sediments frequently erode their substrate heterolithic beds.

Regionally, the Grès d'Annot formation is difficult to correlate but still roughly possible. Unfortunately, other logs of diverse authors appear very different. Probably, since each individual author has a personal practice of interpreting geological data and generating composite logs. Additionally the southern region comprise much more sand-rich and coarser-grained composite units than the northern region. Nevertheless, the composite log of Annot (Hilton, 1995) and of Lauzanier area (Appendix 2: Log Correlation) were compared (Figure 6.5), whereas the Annot is situated 48km south-southwest of the Lauzanier area. Obviously, the applied lower- and upper super-cycle of the Lauzanier area emphasises similar succession characteristics as that of the Annot composite log. At many sites in the logs, correlation between composite units might even be feasible, such as those occurring in the lower part of the upper-cycle. The lower super-cycles also appear as very alike, considering their high percentage of finer-grained sediments. Still totally, the Annot log show a higher sandstone / heterolithic ratio than the Lauzanier log, which is a typical contrast between the northern and southern regions. Most confident to correlate seems to be the erosive boundary between the two super-cycles, which are not recovered at about 330m in the successions, but is present in both areas (recovered in appendix 2: Log Correlation).

Numerous indicators of the paleo-current trend during deposition of the Grès d'Annot are preserved in outcrops throughout the basin. Predominantly, they are featured in various sedimentary structures but also in rock-textures. The recognising of paleo-current trend is fundamental for approaching provenance studies of the Grès d'Annot sediments. Abundant research has been performed in discerning- and assembling data, providing an overview map of the overall trending paleo-current across the basin (Figure 3.2. Locality map). Hereby, disagreements are absent among authors, all implying an overall roughly northward trending paleo-current. In the most southern areas paleo-current head strictly northwards. North of Contes, the preservations reflect diverting current trends, to the northeast and northwest. The continuing of the northwestern current trend in the northern region is nearly uniform and persistent. In Lauzanier-, Annot- and Peira Cava area, observed evidences of paleo-current direction endure almost through all of the successions, without varying much.

When sufficient time and suitable current-controlled hydraulic conditions are present, the clasts may imbricate while depositing. This is reflected by the physical ability of current, which positions clasts c-axis (longest width) parallel to their acting force. Thus, they probably form the most common preserved feature for recognising paleo-current trends in more coarse-grained sediments. These aligned clasts are mostly pebbles of different sizes. Rarely, rip up clasts on bed top surfaces may serve as indicators. However, paleo-current characteristics in large- or small-scale sedimentary structures are simpler to identify. Such large-scale feature is a current parallel channel trough. More insecure indicators of current directions are the positioning of slides and their marks on the underside of beds. More variable sedimentary structures resolving current trends are of small scales. Occurring very frequent in finer-grained sediments are asymmetric ripple-, or climbing ripple marks. Both reflecting current direction, whereby dipping end-point of stoss side indicate incoming current. As they commonly site in sections, only rough current direction may be interpreted but not distinct. The same terms are valid for seldom appearances of cross bedding, whereas the direction of a foreset reflect where the current heads. In contrast, distinct sedimentary structures are flutes and grooves, which are located at bed base undersides. Both indicating current trend where their end merge with bed underside surface, which points to former flow direction. Interpreting paleo-current on a regional scale, the grain size distribution indicates a northwards directed current, as southern- is more coarse-grained than northern region.

In the Lauzanier area the Grès d'Annot Formation is remarkable for its monotony and lack of syn-sedimentary structures, an evidence for tectonic quiescence during the deposition of the succession. Other authors confirm this lack across the basin (Elliott et al., 1985). There are no observed or reported olisthostromes or intraformational megabreccias. There are few slumped horizons adjacent the base of the succession, rare syn-sedimentary faults, or solid blocks of intra- or extra formational sediment. Those seen structures may even be related to failure of sediment from a former basin slope. Other features interpreted to be the product of tectonic activity contemporaneous with deposition of the succession, are either small-scale phenomena, or they are broad low amplitude features induced by minor movement.

In the Lauzanier area few prevalently vertical faults of minor offsets are sited throughout the outcrops. These faults are aligned more or less parallel, trending roughly east - west, forming an fault system (Appendix 3.1 and 3.4: Panorama Pictures). Remarkably, these faults are not present at any place in the upper super-cycle of the succession. Offsets in the lower super-cycles are highest at as adjacent their base as possible, which is at its maximum by 2m (Picture 6.7a). Principally, when a faulting line is studied upwards, offsets decrease gradually and starves totally before reaching the boundary of the lower- and upper super-cycle. Mostly these structures even ceases 10s- and up to 100m beneath this break. However, the most continuous fault line is traceable until it pinches out somewhere in the thickest heterolithic bed of the entire area (Appendix 2: Log Correlation, Log 4) just below the erosive super-cycles boundary (Picture 6.7a). All these east - west trending faults appear as ductile breaking. Their vertical boundaries comprise more insignificant transition zones, not indicating brittle breaking. Thus, faulting is determined as of syn-sedimentary origin. Whether their induced movement during an unconsolidated state, is a product of tectonic activity or initiated through pre-existing basin slope failure, is not interpretable.
Other syn-sedimentary phenomena in the Lauzanier succession are only preserved as small-scale slumps and slides, not revealing much of their origin. An exception is, however, syn-sedimentary features located in Italy just some kilometres beyond the French-Italian border. Here numerous small-scale slumps are sited adjacent to the lower super-cycle base, whereas its base erodes and onlaps the substrate. Calcaires Nummulitique (Picture 6.7b). Upwards in the succession, their appearance diminishes, and vanish approximately 30m above the onlap. These slumps reflect a downslope movement during a period between deposition and consolidation of the sediments.

No onlapping was recorded at the base of the Grès d'Annot Formation in Lauzanier area. However, diverse authors have reported onlaps at numerous sites across the basin (Apps et al., 1987) and described other syn-sedimentary features. Nevertheless, an agreement among various authors is based on syn-sedimentary data that implicates the Grès d'Annot succession deposited during tectonic quiescence (Apps et al., 1987).

In the Lauzanier area, organic fragments occur infrequently in the Grès d'Annot Formation. They may appear in millimetre scale beds, or even sporadically in sandstones. In this thin organic associated beds, they may form high percentages of the bed content. According to Apps (1987) some thick beds in the Trois Eveches area, comprise 80% of plant remains, whereby plant tissue preservations of 10s of centimetres have been found (Apps, 1987). Their original environment, however, is shallower marine. Apparently, these plant remnants must have been transported rapidly after they died, since plants quickly degenerate their tissue in oxygenic environment. Thus, their deposition process in deep marine environment is interpreted as organic debris. Other fossil preservations are found on a micro-scale, such as: Nummulitids, Discocyclines and corroded pelagic Foraminifera (Apps et al., 1987), or nannoplankton like: Chiasmolithus, Coccolithus, Ericsonia and Dicoaster (Muller, in the thesis of Jean, 1985). Their assembled appearance is concluding diverse interpretations of the depositional environment. Thus, the presence of fossils that indicate shallow marine environment rather are assigned as reworked from older Formations.
An exception of autochtonous fossils is the common appearance of trace fossils, or synonymously, ichnofossils, throughout the Grès d'Annot successions across the basin. No fossil of the animal itself was found, but only preservations of their activities. They form track, trail, borrow, or tube structures when for example an invertebrate is creeping, feeding, hiding or resting in soft sediment (Bates & Jackson, 1983). Ichnofossils may occur in all types of sediments in the Grès d'Annot Formation, except conglomerate beds. Though, their presence is dominantly associated in heterolithic- and fine-grained sandstone beds. Their shapes, no matter in which grain-size beds they occur, are predominantly bent tunnel-forms. In the lower super-cycle these pipe diameters are normally below 1cm (Picture 6.8a). In the upper super-cycle, pipes may exceed 3cm (Picture 6.8b). According to Sinclair (1994) all of these ichnofossils are caused by Ophiomorpha, which generate chondrites (first described by Sternberg, 1833). Condrites form genus, in the widest possible sense; plant-like dendritic patterns of small cylindrical ramifying tunnel system. This branching is observed in the field, which may trend in all directions, either vertical-, inclined-, but predominantly lateral. Since these chondrites are numerous and only featured as borrowing trails, they rather indicate characteristics of a deep marine environment (Seilacher, 1964).