And Wave-Dominated Successions: an Example from the Late Tortonian – Early Messinian Terravecchia Formation (NW Sicily)

Cent. Eur. J. Geosci. • 3(3) • 2011 • 235-259 DOI: 10.2478/s13533-011-0025-3

Central European Journal of Geosciences

Partitioning between “wedge-top” river- and wave-dominated successions: an example from the late Tortonian – early Messinian Terravecchia Formation (NW Sicily)

Research Article

Calogero Gugliotta1∗

1 Dipartimento di Scienze della Terra e del Mare, Università degli Studi di Palermo, Palermo, 90123, Italy

Received 28 April 2011; accepted 1 August 2011

Abstract: Detailed field sedimentological and facies analyses have been performed in the Terravecchia Formation cropping out in NW Sicily, in order to differentiate and describe, for the first time, wave- and river-dominated shallow-marine (deltaic) siliciclastic successions. The latter were deposited filling syntectonic basins, developed between the late Tortonian and early Messinian time, within the wedge-top depozone of the Sicilian Foreland Basin System. It has been observed that river-dominated successions, recording the deposition of small fan-deltas are characterized by fining- to coarsening upward, transgressive-regressive sequences which were mostly deposited filling relatively narrow and often oversupplied basins. These basins were probably located in a proximal sector of the wedge-top depozone, closer to emergent sectors of the chain and probably sheltered from the main marine areas. Wave- dominated successions, on the other hand, are characterized by upward fining, mostly transgressive sequences which were deposited filling wider basins open to major marine regions and located in a more distal position of the wedge-top depozone. The documented partitioning between river- and wave-dominated successions, as a function of the position of the sedimentary basin within the wedge-top depozone, is coherent with data from analyses of the deformational patterns of the Terravecchia Formation in this study area. Furthermore, the data here presented could be considered as a preliminary database for future characterization and analysis of siliciclastic reservoirs from Sicilian outcrop analogues. Keywords: river-dominated deltas • wave-dominated deltas • late Miocene • Terravecchia Formation • wedge-top depozone • Foreland Basin System • Sicily © Versita Sp. z o.o.

1. Introduction ated and described [1–3], in central-northern and north- western Sicily, as characterizing part of the Terravecchia Formation (TRV in the text). The TRV is a composite lithostratigraphic unit [4–8] recently revised [9] and de- Wave- and river-dominated shallow-marine siliciclastic scribed as made up of upper Tortonian – lower Messinian successions (delta systems) have been recently differenti- [10] conglomerates, sandstones, marls and clays. These rocks were considered [1–3] the sedimentary fill of different

∗E-mail: [email protected] syntectonic basins located in the inner sectors (wedge-top

235 Partitioning between “wedge-top” river- and wave-dominated successions: an example from the late Tortonian – early Messinian Terravecchia Formation (NW Sicily)

Figure 1. a) Structural map of Sicily (modiﬁed from [32]). The dashed square indicates the study area. Key: VB: Vita Basin; CMB: Camporeale Basin; CB: Ciminna Basin; SB: Scillato Basin; CALB: Caltanissetta Basin; b) Tectonic sketch of the central Mediterranean (mod. after [33]). The dashed square indicates the location of the study area.

depozone sensu [11]) of the Late Miocene Sicilian Fore- waves driven by winds rework and redistribute the sedi- land Basin System (SFBS). ments especially under storm conditions. Mouth bar deposits, in contrast to deposits observed for river-dominated Based upon the main regimes at the delta-front, deltas deltas, often appear as elongate bodies parallel to the are classified [12, 13] into three main categories: river- coastline [17]. A correct distinction between these two , wave- and tidal-dominated, respectively. Among these, kinds of deltas in ancient successions represents a valu- river- and wave-dominated successions are the most im- able tool, not only for understanding the main depositional portant for this paper. River-dominated deltas and wave- processes which drive the sedimentation in a sedimentary dominated deltas show several differences including their basin (or part of it) but also for palaeogeographic and shape, dispersal pattern of sediments and sedimentary palaeotectonic reconstructions. evolution, due to the different processes which dominate the deposition at the frontal part of these systems. The Ancient river- and wave-dominated deltas have been de- river-dominated deltas commonly develop under microtidal scribed by many authors [14, 18–25] among many others regimes, prograding across very gently sloping shelves. In from different settings in several parts of the world. Of this setting wave energy is mostly dissipated before the particular interest for the aims of this paper are the re- waves reach the coast. For these reasons river-dominated searches of Mutti and co-workers [26, 27] and references deltas tend to be highly lobate to elongate, furthermore, therein. These authors subdivided shallow marine and they contain abundant channels which extend basinward shelfal foreland basin successions into three main types forming the characteristic “bird’s foot” pattern [14, 15]. of depositional systems, based on their facies associations In contrast, wave-influenced deltas (or shoreface systems and relative water depth. The systems are: (i) flood- [16]) are lobate to straight, sand-dominated systems with a dominated deltaic systems, (ii) mixed depositional sys- low proportion of distributary channels. At the delta front, tems and (iii) basinal turbidite systems. The first of these

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Figure 2. Schematic composite logs (not to scale) representative of the two end-members “inner wedge-top sequence” (a) and “outer wedge- top sequences” (b) cropping out in the study area (mod. from [2, 3]). The logs are not representative of all outcrops but they have been inferred from comparisons among several studied stratigraphic sections; c) Scheme resuming the late Tortonian to Early Pliocene lithostratigraphic units outcropping in the study area (mod. from [9]). See Tab. 1 for symbols and acronyms. systems develop filling wedge-top type basins with sed- 2. Geological setting iments correlable across a broad region extending from the delta front to the base-of-slope (see also [28, 29] for Sicily is a sector of the Apenninic-Maghrebian chain details). For such reasons the successions studied in this whose development is related to the subduction of con- paper have been regarded as good examples of ancient tinental and oceanic crust beneath a complex ”European flood-dominated deltaic systems. crust” (Calabrian Arc, [30]) (Fig. 1b). The accretionary This paper aims to present, for the first time, both a de- processes related to continental collision were respon- tailed sedimentological description and a comparison in sible for the deformation and tectonic transport of some term of facies arrangement, between the wave-dominated main palaeogeographic domains located, since the Per- and river-dominated delta successions characterizing the mian time, along the African continental margin (Imerese, TRV. The study area comprises an E-W trending belt, lo- Sicano, Panormide and Trapanese domains) and the east- cated in the northern and north-western Sicily (Fig. 1a), ward prolongation of this margin toward the “oceanic” along which the TRV crops out widely. The partition- Tethys (Sicilide domain) [31–35]. A number of qualita- ing between river- and wave-dominated successions pre- tive descriptions point out that the subduction A system sented here has been explained (through a preliminary in Sicily and offshore appears as an E- and SE-vergent model) within the framework of the complex tectono- chain, locally up to 18 km thick [31–33, 36–41]. The tec- depositional and palaeogeographic arrangement of the tonic wedge is superimposed on the Iblean-Pelagian fore- Late Miocene Sicilian wedge-top depozone. This paper land (Fig. 1a, b). A recent foredeep developed in the also provides some potential field outcrop analogues for central sector of the collisional system. future reservoir characterization and analysis. Regional geological sections, based on integrated field

237 Partitioning between “wedge-top” river- and wave-dominated successions: an example from the late Tortonian – early Messinian Terravecchia Formation (NW Sicily)

and geophysical data, imaged the architecture of the fold lana Sicula Formation, SIC, see [1–3, 9, 38] for details) and thrust belt in NW Sicily [9, 33, 38, 42, 43] as made or directly cuts the syntectonic sediments (Sicilidi and/or up of four main structural elements, bounded in turn by Numidian Flysch units). The abovementioned angular un- regional decollements. The aforementioned tectonic as- conformity can be related to the first episode of subaerial semblage is the result of two Miocene-Pleistocene com- exposure and erosion of some uplifted sectors of the SFTB pressional tectonic events [32, 33, 39, 43, 44]. In the [1, 3], thus marking the time since the Sicilian orogen be- growing fold and thrust belt, the simultaneous develop- come the main source of sediments for the inner sectors ment of thrusts, backthrusts, and lateral displacement and of the foreland basin (continental wedge phase [50] or the occurrence of clockwise nappe rotations [44–46] during molasse stage [51, 52]. This unconformity has been rec- Late Miocene - Early to Middle Pleistocene, create mor- ognized not only in the stratigraphy of Sicily, but even phostructural depressions filled by syntectonic deposits in the northern and southern Apennines [53, 54] indicat- during a continuous forward migration. In this regional ing a Mediterranean-scale event. The discordance asso- context, the TRV which crops out in the study area has ciated with this unconformity decreases southward and is been interpreted as the sedimentary record of the in- replaced by a paraconcordance (in the central and south- ner portion (wedge-top depozone sensu [11]) of the Late ern Sicily), a feature which is also documented on land Miocene (Tortonian-Messinian) (SFBS, [1, 3]). TRV was [8]. unconformably deposited above already deformed units In central-eastern and central-southern Sicily (eg. Cal- characterizing two “end member”units, named [2, 3] in- tanissetta Basin, see [48, 49, 55, 56] the TRV fills broad ner (IWS) and outer (OWS) wedge-top sequence, respec- depressions and is mainly characterized by fine-grained tively (Fig. 2a, b). These sequences crop out widely in rocks (marls and clays), belonging to a complex wedge- the study area filling morphostructural depressions whose top-to-foredeep depozone transition. present day position results from both syn- and post- depositional Mio-Pliocene tectonics and the contemporaneous syn-kinematic differential rotations of the thrust sheets. 3. Methods

2.1. The Terravecchia Formation: general Methods used include a geological survey performed at a scale of 1:10.000 as well a detailed study of several features and previous works measured stratigraphic sections (see Tab. 1 for symbols and acronyms). Facies and stratigraphic analyses were Between the late Tortonian time and Pliocene time the combined with study of large scale outcrops in order to evolution of the inner sectors of the SFBS was punctu- identify major stratigraphic surfaces and lateral and ver- ated by alternating episodes of marine and subaerial de- tical facies variations. Following the Miall’s [57–59] facies position. These events are identified by a stratigraphic classification of alluvial deposits, the facies associations succession made up of different lithostratigraphic units recognized in the field were codified and interpreted in (some of them informal) cropping out within the study area terms of depositional processes and settings based both (Fig. 2c). The older of these units is the Terravecchia on their granulometry and sedimentary structures (Tab. 1). Formation. In the study area, as well as, in many other An alternative interpretation of facies associations has regions of Sicily the TRV is commonly represented by a been performed by using the “facies tracts” approach of coarsening- to fining upward or fining- to coarsening up- Mutti and co-workers [26–28] and [29]. These authors ward sedimentary succession made up of: (i) sandstones suggested that ancient flood-dominated depositional sys- and conglomerates (alluvial or paralic), (ii) sandstones, tems and associated flood-generated delta front sandstone (iii) marls and clays (transitional to shallow-marine) [1, 7– lobes in tectonically active basins can be mostly related to 10, 38, 47]). Following the informal subdivision of the two main end-members which are: fan delta systems and Tortonian ([9, 39] and references therein, Fig. 2c), these river-delta systems, respectively. Flood-generated delta rocks would cover a time span of about 3.15 Ma, between front sandstone lobes typically consist of thick and lat- the late Tortonian (not older than 10,4Ma) and the early erally extensive successions characterized by a cyclic al- Messinian (or pre-evaporitic, not younger than 6.42Ma). ternation between sheet-like sandstone bodies and mud- The TRV outcrops above a well developed, previously doc- dier facies quite similar to those described in this pa- umented erosional unconformity ([7–10, 38, 48, 49] among per. Samples for biostratigraphic analysis (both plank- others) which cuts an already deformed late Serravallian tonic and benthonic foraminifers and calcareous nanno- to early Tortonian thrust-top marine succession (Castel- plankton) were collected throughout the study basin. Each

238 Calogero Gugliotta

Figure 3. Schematic geological map (a) and stratigraphic log (b) of the Scillato Basin (mod. from [1]). See text and Tab. 1 for symbols and acronyms.

sample has been analysed in order to evaluate both the whole of the TRV succession unconformably rests above relative age and the palaeoenvironmental conditions. the Castellana Sicula Fm. or directly covers the already emplaced Sicilidi units (Fig. 3a, b). No typical Messinian rocks (such as reefal limestones and evaporites) or Early 4. Sedimentology and facies analy- Pliocene limestones (Trubi Fm.) are present at the top of sis the TRV in the SB. In this setting an approximately 900m-thick deltaic unit characterizes the middle and upper portion of a 4.1. River-dominated delta system: sedimen- transgressive-regressive succession (Fig. 4a, b, c). At the tological characterization basin scale, the deltaic rock body rests above an unconformity (Fig. 3a; 4a, b, c). The latter appears, in the Siliciclastic successions related to river-dominated delta field, as a complex and locally erosional surface inter- systems pertaining to the TRV widely crop out in the study preted [62] as an intraformational angular unconformity region characterizing part of the sedimentary succession (sensu [63]). This surface asymmetrically cuts an upward- of the Ciminna and Scillato basins (Fig. 1a). These basins fining entrenched stream valley fill system succession (and have been considered [1, 10, 38] as erosional remnants of the associated older unconformity) which characterizes the Late Miocene to Pliocene sedimentary basins filled by lowermost portion of the TRV, or directly cuts the de- thousand metres-thick siliciclastic, evaporitic and carbon- formed substrate (Sicilidi units) (Fig. 4a, b, c). Through atic successions. Particularly, the Scillato Basin (SB in the unconformity the sudden disappearance of the alluvial the text) has been interpreted [1, 47, 60–62] as the rem- deposits (not treated in this paper) is accompanied by a nant of a late Tortonian depocenter. There, continen- slightly angular discordance (the time gap is not evaluable tal to marginal marine terrigenous clastics (about 1250 due to poor chronostratigraphic resolution) and also by a metres-thick) forming part of the TRV, are present, provid- strong variation in the mean palaeoflow direction (from ing good quality and laterally continuous outcrops. The SE-directed in the underlying alluvial deposits to NW-

239 Partitioning between “wedge-top” river- and wave-dominated successions: an example from the late Tortonian – early Messinian Terravecchia Formation (NW Sicily)

Figure 4. a, b, c) - Schematic logs (not to scale) showing the facies arrangement of the river-dominated succession in the Scillato Basin; d) stratigraphic log (not to scale) of a river-dominated delta front sequence as recognized in the SB; e) siltstones with interbedded sheet- like sandstones and conglomerates of facies association A1; f) cross-laminated sandstones with layers of conglomerates of facies association A2; g) large-scale ripple marks on top of a sandstone strata; h) interbedded sandstones and conglomerates of facies association A3 (mod. from [1]). Numbers refer to location of stratigraphic log in the map of ﬁg. 3a; see Tab. 1 for symbols and acronyms.

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Figure 5. Panoramic views of the Scillato Basin showing the basin-scale arrangement of the main facies associations.

and WNW-directed in the overlying deltaic deposits, see tically arranged forming several (up to 7), decametric to [62]). At the top, the river-dominated succession is uncon- hectometric in scale, shallowing and coarsening upwards formably covered by delta-top / braided stream conglom- delta front sequences (Figs 4a, b, c; 5a, b, c, d). A single erates and sandstones. sequence shows three main lithofacies, named from the lowermost A ,A and A , respectively (Fig. 4d). These Three main facies association, respectively: (i) sandy - 1 2 3 lithofacies have been related to the distal, intermediate gravelly river-dominated delta front “A”; brackish prodelta and proximal delta front environments respectively (ac- clayey siltstones “B” and prograding delta slopes and cording with Colella’s scheme [64] as modiﬁed by [65]). distal delta front “C” were recognized within the river- dominated delta succession and described below. -A1 distal delta front: represented by centimetre thick, sheet-like clayey to sandy siltstones. Lens-shaped sand- 4.1.1. Facies association “A”, sandy - gravelly river- stone bodies showing normal gradation, horizontal or low- dominated delta front: angle cross lamination (lithofacies Sh, Sl) and rare layers of normally graded granule to pebble conglomerates - Description are variably interbedded within the ﬁne-grained deposits (Fig. 4e); This facies association (up to 350m thick) is made up of interbedded siltstones, sandstones and conglomerates ver- - A2 intermediate delta front: medium- to coarse-grained

241 Partitioning between “wedge-top” river- and wave-dominated successions: an example from the late Tortonian – early Messinian Terravecchia Formation (NW Sicily)

yellowish sandstones with horizontal to trough- and pla- ripple marks and the bird’s foot tracks, locally observable

nar cross lamination (lithofacies Sh, St, Sp) interbed- at the top of facies A3 support this interpretation. The ded with sandy siltstones (Fig. 4f). The sets of cross- conglomerates often observed in the facies A3 have been laminated sandstones are often marked at the base by interpreted as depositional remnants of small channels de- a layer of imbricated and poorly sorted clasts (pebbles veloped in response to the delta lobe progradation. to granules). Interbedded sharp-based, lens- to planar- This facies association could be also interpreted as shaped bodies (up to 1 meter thick) of massive conglom- recording the deposition of ﬂood-generated delta front erates (Gms to Gm lithofacies) are also locally present; sandstones lobes, probably developed as part of a small -A3 proximal delta front: very coarse sand- fan-delta system [27, 28]. A critical observation against stones and pebbly sandstones showing trough-cross- and this interpretation could be represented by the apparent

planar-cross lamination (lithofacies St, Sp) arranged in absence (in the finer facies associations A1 and A2) of centimetre-thick sets; the sandstones are regularly in- sedimentary structures developed under oscillatory mo- terbedded with sharp-based pebble conglomerate beds. tion (such as HCS) abundantly documented in similar de- The frequency of these beds increases upsection. The posits of other basins [29]. The backstepping delta front conglomerates have a clast-supported texture (lithofacies sequences outlined in the middle portion of the SB suc- Gm), the clasts are middle- to poorly-sorted, well rounded cession have been interpreted [66] as imaging the ret- and often imbricated, normal gradation is diffuse. Often, rogradational stage of the delta front system. These se- the conglomerates and sandstones are closely interbed- quences merge laterally and pass upward into a thick body ded to form meter-scale fining upward cycles with an ero- of prodelta siltitic clays and siltstones (facies association sional base (Fig. 4h) that characterize the top of facies A3. B, see next section) (Fig. 5a, b). Meanwhile, the amal- 30cm up to 50cm wavelength ripple marks, showing sinu- gamated sequences which characterize the upper SB suc- ous to bifurcated-straight crests in plan view, have been cession are related to a progradational stage [66] of the also observed at the top of some sequences associated delta front system (Fig. 4c, 5e) in turn cut at the top by with bird’s foot tracks [47](Fig. 4g). Wave- and storm- fluvial braided conglomerates and sandstones. derived structures (such as HCS-SCS or tempestites) and tidal-induced structures (such as herringbone cross lami- 4.1.2. Facies association “B”, brackish prodelta clayey nation) are not clearly observable. siltstones In the middle portion of the SB succession (Figs 4a, b) - Description the described facies are superposed upon each other to form delta front sequences with a “backstepping” stacking Up to 400-450m thick of centimetre-thick, light blue - pattern [66]. While, as locally observable in the upper part greyish to brownish siltstones and silty clays (mud-rich of the SB (eastern and north-eastern SB margins Fig. 4c), subfacies of [27]) crop out widely in the SB depocenter (as these facies are vertically arranged to form amalgamated well as in the Ciminna Basin). These muddy lithofacies delta front sequences with an aggradational to slightly are interbedded with greyish to yellowish, centimetre- progradational stacking pattern [66]. thick, sheet like or lens-shaped sandstones (sand-rich subfacies of [27]) showing horizontal lamination and nor- - Interpretation mal gradation (Fig. 6a, b, c). Isolated vertical trace fossils As a whole, the facies association A has been related to are also locally observed. a sandy -gravelly river-dominated delta front environment Microscopic analyses [1, 68] revealed a poorly pre- [12] developing in the submerged distal part of small fan- served late Tortonian microfossil assemblage character- delta lobes under a microtidal regime. ized by an often oligotypic association of benthic and

The facies A1 records the deposition in the more distal planktonic foraminifera (Ammonia spp., Elphidium spp., portion of the delta front; there, clays and silts were de- Valvulineria spp., Valvulineria complanata; Cribroelphid- posited during the low-energy stage of river activity. Lay- ium dehishens., Cassidulina carinata, Bulimina echinata, ers of normal grading conglomerates and laminated sand- Bolivina dentellata Globigerina Bulloides, Turborotalita stones could be related to gravity-driven deposition along multiloba, Neogloboquadrina humerosa, Neogloboquad- the delta front (see delta front turbidites,[67]). The pro- rina acostaensis dx,), rare calcareous nannofossils (Retic- gressive increase of grain size and the presence of struc- ulofenestra spp) and brackish ostrachods [69]. Miner- tures such as cross lamination observed in the lithofacies alogical and geochemical analyses performed by [70–72]

A2 and A3 indicate that these lithofacies were deposited also revealed the presence of kaolinite, illite, smectite and in a progressively shallower setting, related to the inter- chlorite with a conspicuous content of pyrite, low CaCO3 mediate and proximal delta front, respectively. Both the percentage (from 3% to 9%) and a 9.7 to 8 Ph value. The

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Figure 6. Main features of the facies association B from outcrop pictures (a-b-c). Panoramic view showing the transition between the facies association B and the Messinian evaporites in the Ciminna Basin.

frequency and thickness of sandstones interbeds increases problem which could be treated in further research. upsection. - Interpretation Mass-flow conglomerates, related to prograding delta slope deposits (facies association C in the next section), The facies association B has been interpreted as the sed- interfinger with prodelta mudstones in the upper por- imentary record of a quiet shallow-water (40 up to 100 tion of the SB succession (i.e. at Cozzo Gracello area, meters of bathymetry) environment such as a prodelta Fig. 4a, 5b, e). In the neighbouring Ciminna Basin de- (delta front wedge) affected by strong fresh water influx posits equivalent to facies association B (age-dated to and by intermittent periods of restricted circulation. The the latest Tortonian-earliest Messinian, [10, 38, 73] pass large presence of oligotypic and brackish-water microfos- upward into a thin horizon (about 100m-thick) of marine sil associations, together with the widespread presence blue-greyish marls with oligotypic planktonic microfauna of organic matter and pyrite sustain this interpretation. (Turborotalita multiloba,). These latter are, in turn, uncon- Interbedded layers of laminated sandstones could be in- formably overlaid by Messinian evaporites (Fig. 6d) ([38] terpreted as flood-generated hyperpycnal flows induced for details). The meaning of the absence of Messinian by major flooding events at the distal delta front. evaporites and limestones in the SB does not represent an aim of the present paper and still represents an open

243 Partitioning between “wedge-top” river- and wave-dominated successions: an example from the late Tortonian – early Messinian Terravecchia Formation (NW Sicily)

Figure 7. Main features of the facies association C from outcrop and panoramic pictures.

4.1.3. Facies association “C”, prograding delta slopes cello (Figs 5b, e and 7a, b, c). Mass-ﬂow-related and distal delta front: structures such as large clay chips, normal gradation and load casts are common in the conglomerate beds. - Description Furthermore, cross-stratiﬁed sandstones and layers of This facies association is made up of ∼100m of yel- poorly-reworked, matrix-supported breccias, containing lowish silty-claystones interbedded with tabular- to also bivalve shells (such as Omphaloclathrum miocenicum, slightly lens-shaped conglomerate bodies (each up to Glycimeris glycimeris, Arca syracusaensis, Ostrea gingen- 5m-thick) and sandstones outcropping at Cozzo Gra- sis, Hinnites brussonii, Ringicardium hians, [69]) have

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Figure 8. Schematic geological map (a) and stratigraphic log (b) of the Camporeale Basin; c) schematic geological cross section showing the main features of the Camporeale Ridge (mod. from [3, 75]). See text and Tab. 1 for symbols and acronyms.

been observed associated with the conglomerates and in- ditions have been related (Venetian foreland basin, see terfingered with the prodelta siltstones (Fig. 7c, d, e, f). [74]) to a tectonic-controlled setting. In the study area, The preliminary compositional analyses of conglomerate the facies association C appear slightly discordant with clasts highlights an “intrabasinal - intraformational” sup- the underlying facies association B suggesting that both ply [62]. the steeping of the delta slopes and the cannibalization of the basin margins could be related to syn-sedimentary - Intrepretation tectonics. This facies association has been interpreted [1, 2, 66] as deposited in a prograding “steepened” delta slope to distal delta front setting with slump-scars. The progradation of the delta slope/front by mean of activation of 4.2. Wave-dominated shoreface system: gravity-flow processes has probably been induced by the sedimentological characterization rapid introduction of coarse-grained deposits directly in the prodelta areas. The sudden increase of coarse clas- Shallow-marine siliciclastic deposits forming the TRV and tics supply could also reveal a rejuvenation of streams related to wave-dominated delta (shoreface) systems occur induced by an inferred relative sea level fall at the basin in the Camporeale Basin (CMB). The latter is a wide mor- margin [62, 66]. The occurrence in the conglomerates of re- phostructural depression located in north-western Sicily worked TRV clasts could record the local cannibalization (Fig. 1a) and interpreted as the remnant of a Late of the basin margins during a period of major regression Miocene wedge-top basin developed in the outer wedge- (relative sea level fall) of the shoreline. This hypothe- top depozone [1, 3]. In the CMB the TRV is part of a late sis could explain the over-supplying and the instability of Serravallian to early Messinian composite stratigraphic the distal delta front and delta slope areas and the con- succession (up to 900 meters-thick) and unconformably sequent deposition of mass-flow deposits. Similar con- rests between (Fig. 8a, b) the Castellana Sicula Fm.

245 Partitioning between “wedge-top” river- and wave-dominated successions: an example from the late Tortonian – early Messinian Terravecchia Formation (NW Sicily)

Figure 9. a) Schematic log (not to scale) showing the facies arrangement of the wave-dominated succession in the Camporeale Basin, number refers to location in ﬁg. 3a, b) stratigraphic log (not to scale) of a wave-dominated shoreface sequence as recognized in the CMB; c) panoramic views of the facies association D arrangement along the northern slope of the Camporeale Ridge. (mod. from [1, 3]). See text and Tab. 1 for symbols and acronyms.

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Figure 10. Schematic log (not to scale) and cross-sections showing the facies arrangement of the facies association D in the Camporeale Basin (mod. from [1]). Numbers refer to the location on the map of ﬁg. 7a. See Tab. 1 for symbols and cronyms.

(SIC, at the base) and the Baucina Formation (BAU, at unconformably covers the previously deformed substrate the top). (Figs 8a, c and 9a). Within the TRV, the wave-dominated deltaic rock body is characterized by well-exposed and laterally-continuous Two main facies associations characterize the deltaic suc- outcrops along both northern and southern sides of the cession, these are: (i) sandy wave- and storm-dominated Camporeale Ridge (Fig. 8c ). At the basin scale, the delta front “D” and offshore-transition to offshore clays deltaic rock body rests above unconfined braidplain con- “E”. The main characters of these facies associations are glomerates and sandstones (not treated in this paper) or reported below.

247 Partitioning between “wedge-top” river- and wave-dominated successions: an example from the late Tortonian – early Messinian Terravecchia Formation (NW Sicily)

Figure 11. Main features of the facies association D from outcrop pictures; a - b) wave rippled sandstones with erosional base interbedded with clayey layers (facies association D1); c) cross-laminated sandstones of facies association D2; d) sandstones with HCS interbedded with highly cemented and highly burrowed layers (facies association A2); e) scour-based storm bed showing pebbly and coarse- grained sandstones passing upward into medium-grained sandstones with HCS and horizontal planar lamination; g) trough-cross laminated sandstones in the facies association D3; h) trough-cross laminated sandstones interbedded with pebble-conglomerates in facies association A3; Iron oxides-encrusted wave ripple marks on top of a sandstone bed, section (i) and plan view (l).

central CMB reaching more than 600m in thickness along the Camporeale Ridge. The latter is an E-W-trending, 4.2.1. Facies association “D”, sandy wave- and storm- about 25Km long, morphostructure which has been in- dominated shoreface system terpreted [1, 3, 75] as an incomplete N-verging anticline bounded, both N- and S-ward, by high-angle, dextral - Description transpressive faults (Fig. 8a, c). This peculiar structural These are the predominant deposits within the TRV in the

248 Calogero Gugliotta

setting provides well-exposed and laterally-continuous Thalassinoides types [77]. outcrops studied in detail by means of measured strati- -D , cross-bedded sandstones and conglomerates - Upper graphic sections (Fig. 10). Along the Camporeale Ridge 3 shoreface: yellowish medium-to-very coarse sandstones the facies association D crops out, arranged in several and pebbly sandstones interﬁngered with sharp-based (up to six), decametre-scale, coarsening and shallowing layers of clast- to matrix-supported pebble and granule upward “shoreface” sequences (50 to 100 m-thick) in turn conglomerates. Sandstones show high-angle trough-cross bounded by surfaces of marine ingression (Figs 9a, b, c). bedding and horizontal-planar lamination (Fig. 11f, g, Each sequence is composed of three main lithofacies, from h). Cross lamination is arranged in sets, 20 to 40 cen- the lowermost D ,D and D , respectively. 1 2 3 timetres thick. Bioturbation is characterized by isolated

-D1 storm-fairweather sequences - lower shoreface: or grouped vertical or U-shaped burrows related to the Skolithos, Ophiomorpha and Diplocraterion types [77]. This facies association is characterized by interbedded fine- and medium-grained lithotypes arranged to form The above described facies association D characterizes up to 1m sequences representative for single storm- the middle portion of the Terravecchia Formation and fairweather event [76]. In particular the following has been evolves with a thinning upward (retrogradational) trend observed: interfingering toward the top with the offshore clays of facies association E. - greenish, glauconite-rich siltstones and clayey siltstones (post-storm faiweather deposition) with scarce and poorly - Interpretation preserved microassemblage characterized by the presence The whole facies association D is here interpreted as the of Neogloboquadrina acostaensis dx, Ammonia becarii sp. sedimentary record of a delta front migration induced by and Globigerinoides quadrilobatus. Often, a brackish- a continuous supply of clastics along the coastline (see water fauna composed of ostracods Cyprideis sp. and ben- [18–22, 24, 25, 78] among others). The observed sedi- thonic foraminifera Ammonia beccari tepida occurs [1, 10]. mentary characteristics are coherent with the depositional The clayey lithotype interbeds with isolated yellowish processes that occur in wave-dominated shoreface delta hummocky cross-stratified or horizontal planar-laminated systems [79, 80]. In this setting, sediments supplied by sandstones (main storm deposition) (Fig. 11a, b, e). streams were distributed along the coastline to form sev- The sandstones, fine- to medium-grained are arranged in eral and laterally continuous sandy bars. Following [81] sharp-based strata, showing well developed normal gra- the mean wave ripple orientation (ESE-WNW) is consid- dation, clay chips, sole marks and load cast structures. ered parallel to the palaeocoastline. Iron oxide-encrusted wave ripples and megaripple marks (waning storm deposition) have been frequently observed The facies D1 appear to be typical deposits of a storm- at the top of the sandstone strata, just above the clayey dominated lower shoreface setting characterized by mod- layer (Fig. 11a, b). Crests of wave ripples are straight, bi- erate energy and subjected episodically to storm events furcate or slightly sinuous. In cross section ripples appear as indicated by the storm-fairweather sequences [18, 79, symmetric or slightly asymmetric, with relatively sharp 80, 82]. During the main storm deposition stage, normally crests, locally double; the amplitude (A) ranges from 1cm graded, sandy beds with HCS and planar lamination were to 10cm and the wavelength (l) is from about 4cm to 30cm; deposited covered by the clayey layers deposited during the average crests orientation ranges from E-W to ESE- the post-storm/faiweather deposition stage. The transi- WNW (Fig. 11i, l). Bioturbation is poorly developed. tion between these two stages is characterized by development of widespread wave ripples (waning storm de-

-D2 amalgamated hummocky cross-stratified sandstones position stage). Double-crest ripple marks and slightly - middle to upper shoreface: Medium- to coarse-grained asymmetric ripples are related to wave-induced oscilla- sandstones arranged in well defined, planar-shaped, up to tory motion, locally combined with superimposed unidi- 1m-thick strata. Strata show a well developed normal gra- rectional flow [83, 84]. The occurrence of brackish wa- dation and are stacked along sharp sub-horizontal erosive ter fauna in some fine-grained layers could reveal that amalgamation surfaces. Medium-scale swaley (SCS) and the sedimentary environment was periodically affected by hummocky (HCS) cross stratification is observable in the a fresh-water influx from closer river mouths. This hy- sandstones associated with layers with horizontal-planar pothesis supports both the poorly developed bioturbation lamination (Fig. 11c, d, e). Close to the transition to the and the poorly diversified microfossil assemblage. The facies A1 the sandstones appear characterized by trough- upward transition into amalgamated hummocky and swa- cross bedding. Traces fossils, often concentrated along ley cross-stratified sandstones (amalgamated storm beds) well cemented horizons (Fig. 11d), are dominantly re- (Facies D2) associated toward the top with trough cross- lated to the Skolithos, Diplocraterion, Ophiomorpha and bedded sandstones, suggests that deposition occurred in a

249 Partitioning between “wedge-top” river- and wave-dominated successions: an example from the late Tortonian – early Messinian Terravecchia Formation (NW Sicily)

middle to upper storm-dominated shoreface environment. sedimentary environment with an up to 100mts palaeo- The trace fossils assemblage recognized at the top of the bathymetry. cemented layers (Skolithos ichnofacies) indicates a high energy condition and therefore is compatible with this interpretation [24, 77, 78]. The dominant high-angle, trough 5. River-dominated vs wave- cross-stratification of facies D3 suggests a shallow and high energy environment located above the fairweather dominated successions, a brief com- wave base in an upper shoreface setting. There, storms parison. and long shore currents (long shore drift) were able to form and migrate three-dimensional dunes or sand-waves, A brief comparison performed between river- and wave- particularly during the main storm events. The verti- dominated successions allows the author to point out some cal trace fossils are related to the Skolithos ichnofacies interesting considerations about the palaeotectonic and that in association with the above-mentioned sedimentary palaeogeographic setting of the basins in which these two structures, reveal a typical upper shoreface environment successions were deposited. [77, 78]. The detailed analysis of microfossil associations performed during the present research and in large part known from many previous authors allowed the author to 4.2.2. Facies association “E”, clayey offshore- consider that the river-dominated and the wave-dominated transition to offshore successions are essentially coeval and relatable to a - Description time span including the latest Tortonian and earliest Messinian. This facies association is characterized by up to 200m- In particular, the deposits pertaining to the facies asso- thick of sandy to siltitic-clays and marls with planc- ciations A and B in the Scillato Basin (delta front and tonic foraminifers (Turborotalita multiloba) and calcare- prodelta) were considered to be late to latest Tortonian ous nannofossils. Planar-laminated, coarse-grained sand- in age [1, 60, 69]. The equivalent deposits outcropping in stone and lenses of matrix-supported granule to pebble- the Ciminna Basin have been considered [9, 10, 38] to be conglomerates are locally present variably interbedded to latest Tortonian to earliest Messinian in age. The marls the siltstones. Biostratigraphic analyses in the siltitic- with Turborotalita multiloba outcropping in the Ciminna clays revealed planktonic foraminifer associations relat- Basin, just below the Messinian evaporites, have been able to the Globigerinoides obliquus extremus, Globoro- age-dated to the earliest Messinian (about 6,42Ma; FCO talia suterae and Globorotalia conomiozea biozones. Cal- of Turborotalita multiloba see [9, 10, 85] with references careous annnofossils are relatable to the Minilytha con- therein). The whole of wave-dominated deposits studied vallis, Coccolithus pelagicus, Amaurolithus primus and in the Camporeale Basin have been considered to be lat- Reticulofenestra rotaria biozones (see also [9, 10] for more est Tortonian – earliest Messinian in age [1, 9]. Owing details). to the lack of adequate chronological control of the stud- This latter facies association characterizes the upper por- ied successions it is difficult to present a more accurate tion of the Terravecchia Formation and widely outcrops in scenario. the lowered area located N-ward and S-ward of the Cam- Some insights about the different tectonic control recorded poreale Ridge (Fig. 8a). Southward from the study area by the river- and wave-dominated successions were this facies association characterizes almost the whole of pointed out in the following paragraph, comparing the data the Terravecchia Formation. relative to the main deformation pattern which character- - Interpretation ize these two kind of successions [1–3]. This facies association is interpreted as consisting of offshore-transition and offshore deposits. Interbedded 5.1. River-dominated successions lenses of conglomerates and sandstones are interpreted as gravity flow deposits or as storm density current due River-dominated successions typically characterize the to powerful storm events (storm-induced gravity flows). middle and upper part of mostly coarse-grained, conti- A similar facies association has been described in other nental to transitional “inner wedge-top sequences, IWS” basins (such as in the Ciminna Basin by [8] and [10]). (Fig. 2a, 12) described in the Terravecchia Formation Based on the microfossil assemblage, previous Authors [2, 3]. The IWS was developed filling quite narrow and of- [73] related the marls with Turborotalita multiloba to a ten oversupplied morphostructural depressions, enclosed

250 Calogero Gugliotta

Figure 12. Schematic tectono-depositional sketch inferred for the Late Miocene (Tortonian-Messinian) Sicilian Foreland Basin System showing both the subdivision of the wedge-top depozone into an “inner” and “outer” sector (mod. from [1, 3]) and the partitioning between river- and wave-dominated successions.

among structural highs, located in the innermost sectors of strated by the presence of regional unconformities which the wedge-top depozone. These basins probably evolved bounding the Terravecchia Formation, the tectonics has as “sea inlets” closer to the subaerially exposed areas of played a principal role in the sedimentary evolution of the chain and probably sheltered from the main “open” these slightly structurally external basins (outer wedge- marine areas. As it as been documented in both the Scil- top depozone, [3]. Nevertheless, the deposition of wave- lato [62, 66] and in the Ciminna basins [1, 2, 10, 86], the dominated successions seems not to have been influenced main controlling factor of sedimentation in such sectors by a strong “local-scale” syn-sedimentary deformation of the foreland basin system was represented by synsed- (lack of evident intraformational unconformities). It is imentary and mainly transpressional tectonics. This lat- reasonable to hypothesize that during the late Tortonian ter was active during at least the latest Tortonian time as – early Messinian the deep-seated deformation strongly demonstrated by the widely observed intraformational an- recorded by the river-dominated successions which were gular unconformities (sensu [63]). In such basins, localised developed in the inner wedge-top depozone was already structural highs were raised up along S-ward-directed and active in this portion of the SFBS but still confined to mainly N- and NW-ward-directed high angle transpres- the deeper structural layers. This hypothesis could ex- sive faults modifying the original shape of the basins, pro- plain why the wave-dominated successions recorded only ducing new source areas for clastic materials, controlling a long wavelength deformation accompanied with develop- the basin scale drainage pattern and promoted the local ment of “basin-scale” unconformities. In this setting, the development of an upward regressive evolution of the suc- shallower structural layers and thus the Terravecchia For- cessions [1, 62]. mation strata were probably reached and deformed since the earliest Messinian time, just before the deposition of the reefal limestones [3]. 5.2. Wave-dominated successions 5.3. Brief comparison with similar deposi- Like the above described succession, the wave-dominated tional settings shoreface successions have been observed in the middle and upper part of the Terravecchia Formation . In A brief comparison between the delta successions de- particular, this kind of succession characterizes part of a scribed in this paper and other ancient and modern mainly upward-fining succession named “outer wedge-top analogues can be made, in the frame of a more com- sequence, OWS” ([3], Fig. 2b, 12). It has been inferred plete palaeogeographic reconstruction. Basing on the ob- from litho- and chronostratigraphic data [1, 3, 9, 10, 47] served dominant process of sediment dispersal at delta that the OWS is coeval with the IWS but, the OWS was front [12] and on the prevailing grain size [67] the river- developed filling wide morphostructural depressions (such dominated succession here described as characterizing as the Camporeale Basin) open to the main marine ar- the inner wedge-top depozone could be compared with eas. The coarse clastics were sourced to the coastline by the modern Alta-type delta, based also on the small the streams and here distributed in the shoreface forming scale of this depositional system. According to the previ- small delta systems controlled by waves and storms. In ous description, this type of modern river-dominated and the front of these deltas, large scale sandy bars developed mainly coarse-grained (gravelly sand) delta develops in parallel to an about ESE-WNW-oriented palaeoshoreline mainly shallow-water settings and under micro-tidal con- [1, 3]. The clastic shoreline was, in turn, flanked bas- ditions. The drainage areas are commonly small and the inward by an open marine depositional zone (offshore) topography shows high gradients. On the other hand, dominated by a fine-grained deposition. As also demon- the wave-dominated succession deposited in the outer

251 Partitioning between “wedge-top” river- and wave-dominated successions: an example from the late Tortonian – early Messinian Terravecchia Formation (NW Sicily)

wedge-top depozone could be compared with the mod- lease sediment that is flushed into the delta system. Each ern Skeidararsandur- or Punta Gorda-type delta. Both flood results in a sheet of sandstone that dips, thins and these type of delta are wave-dominated and medium to fines in a seaward direction. Where mouth-bar sandbod- coarse-grained (sandy to gravelly) and are characterized ies are present (not observed in the study successions), by small drainage area. seaward-dipping mud-draped clinoform surfaces can occur (e.g. [93]) representing the former positions of the Moreover, most of the facies characteristics observed in depositional surface that existed between flood-induced the described successions are similar to those charac- influxes of sand. These mud-draped surfaces are poten- terizing some modern short and very steep ephemeral tial significant barriers to both horizontal and vertical fluid gravel-bed streams with torrential regime known as “Fi- flow within mouth-bar reservoirs [94]. In wave-dominated, umara”. These streams are widespread along the tectoni- shallow-marine depositional systems, the majority of sed- cally steepened Sicily and Calabria Tyrrhenian coastlines iment is brought to the shoreline by fluvial systems and where they develop draining close, high relief source areas then transported along the shoreline by longshore drift [87, 88]. The sedimentary processes are mainly dominated until it is deposited [15, 90]. Sediment introduced to by sudden and often catastrophic floods, alternating with the marine part of the system is transported along the periods of inactivity. In their frontal part, the Fiumaras shoreface by longshore transport processes, whilst fair- are associated with the development of wide unconfined weather waves steadily move the sediment obliquely land- gravelly braidplains, flanked seaward by small arcuate- to ward and deposit a series of trough cross-bedded sand- straight-shaped deltas. The palaeogeographic scenario stones in the upper shoreface (like facies association D ). inferred here is also consistent with those described by 3 These deposits are generally mineralogically and textu- [89] regarding sedimentation along active margins. In rally mature, have a very low clay content and generally these settings sediment flux to the sea is enhanced by make excellent reservoirs. Periodic storms erode the upper high-elevation source areas close to the shoreline. Both shoreface and deposit sheets of hummocky cross-stratified the lack of extensive alluvial and coastal plains and the sandstones across the lower shoreface and (ii) offshore- periodic flooding of small-sized streams characterized by transition zone. The hummocky cross-stratified beds are short and high-gradient transfer zone described by these generally finer grained than those of the upper shoreface, authors are features also commonly observed in the Ter- and the lower shoreface interval may contain thin, dis- ravecchia Formation. continuous mudstone horizons. Consequently, the reservoir properties are poorer than the upper shoreface. The lower shoreface interval is still sand dominated and will 5.4. Insights for future characterization of sili- typically contribute to hydrocarbon production. Seaward of the offshore-transition zone and below the storm wave ciclastic reservoirs from Sicilian outcrop ana- base (offshore), deposition of hemipelagic and pelagic silt logues and clay occurs. The offshore deposits are treated as non- reservoir. Consequently, in a typical succession which Sedimentology and stratigraphy of siliciclastic shallow- passes up from offshore mudstones through interbedded, marine successions forming reservoirs in many of the hummocky cross-stratified sandstone and mudstone into world’s major hydrocarbon provinces have been well doc- the sandstones of the shoreface (similar to those described umented by many authors (e.g. [14, 90] among many oth- in this paper, see section 5.2) there is an upward increase ers). Reservoir quality and architecture are usually very in reservoir properties. variable parameters due to the high degree of heterogeneity of sedimentary and tectonic conditions. River- The discovery of the Lippone gas field (360 million Sm3 and wave dominated siliciclastic successions, like those gas) in the late Tortonian siliciclastics similar to the Ter- described in this paper, develop following quite different ravecchia Formation, described in this paper, has rep- sedimentary processes which produce a variable deposi- resented an important result in western Sicily. In this tional architecture thus influencing the internal hetero- sector, in fact, due to the lack of a source rock simi- geneity. Within river-dominated delta systems, the sedi- lar to the naftogenetic Noto and Streppenosa formations ment brought in by the fluvial system is not redistributed known from Eastern Sicily, oil exploration has not pro- by either wave or tide processes so, river-dominated deltas duced valuable results (for details see also [42, 95]. For are often highly lobate [91, 92]. At the front of the delta, these reasons a future detailed characterization (concern- the finest sediment is carried furthest into the basin in ing sedimentological features, tectonic setting and degree a buoyant plume and the coarsest material is deposited of internal heterogeneity) of river- and more important of nearest to the river mouth. Periodic floods in the river re- wave-dominated successions pertaining to the Terravec-

252 Calogero Gugliotta

chia Formation in this sector of the Sicilian chain could tial deep-seated tectonics recorded into the stratigraphic be considered of interest for future researches. succession by development of long-wavelength unconformities. The palaeogeographic scenario here inferred on the base 6. Concluding remarks of sedimentary facies recognized in the studied successions is also in agreement with those described by other authors (e.g. [89]) in active margins setting. A detailed differentiation between river-dominated and wave-dominated successions has been presented, for the The inferred partitioning between river- and wave- first time, from the late Tortonian – early Messinian Ter- dominated successions as a function of the more proximal ravecchia Formation by using sedimentologic and facies or distal position occupied by the different sedimentary analyses. The study has been performed in different sec- basins across the wedge-top depozone opens some inter- tors of NW Sicily. In these sectors the Terravecchia For- esting points for future discussions about the arrangement mation crops out widely with several well exposed and of the Terravecchia Formation in Sicily. A more com- laterally continuous stratigraphic sections. The detailed plete and regionally-extended tectono-depositional sce- characterization of the different facies and facies asso- nario concerning this formation can be built step by step ciations which characterize the two types of successions in the frame of a “long-term” and yet active research. In allowed the author to infer some interesting aspects of this view, the present work aims to present a fragment of the palaeogeographic and palaeotectonic reconstruction a more complicated scenario, giving some important infor- of the Late Miocene Sicilian wedge-top depozone. mation. Unfortunately, the lack of adequate chronological control of the studied deposits prevents any univocal con- In the inferred model (Fig. 12), the wedge-top depozone clusion and leaves open questions for future research. was characterized by an articulate physiography in which a proximal inner (mountainward) and a distal outer por- The data here presented aim also to provide a prelimi- tion (basinward) can be differentiated. In response to the nary field database which could be usable for characteri- position across the wedge-top depozone the siliciclastic zation and analysis of siliciclastic reservoirs from Sicilian “deltaic” successions developed recording a sedimento- outcrops. In this framework, more detailed future stud- logical partitioning between river- and wave-dominated ies concerning the sedimentological parameterization of which was driven by the different sedimentary and struc- Late Miocene Sicilian shallow-marine successions crop- tural conditions dominating the single basin. ping out in an area wider than those here presented could be made. As it has been observed and documented in this paper the river-dominated siliciclastic successions mainly characterize the Terravecchia Formation deposited in the inner wedge-top depozone. There, relatively small and Acknowledgements coarse-grained deltas were probably deposited filling narrow basins. These basins were enclosed among structural This work forms part of the Ph.D thesis of C. Gugliotta. highs and deeply influenced by active syn-sedimentary Professors Raimondo Catalano and Francesco Massari are tectonics. The predominance of coarse-grained facies as- thanked for their help in the earlier phases of this re- sociations, the presence of thicker shallow-water and of- search. Special thanks are also due to Prof. Rodolfo ten brackish-water deposits, as well as, the general fa- Sprovieri and Prof. Enrico Di Stefano for the analysis of cies architecture of the study river-dominated successions microfossil assemblages. The author is grateful to the As- suggests that the basins which were located in the inner sociate Editor Ondrej Babek and to anonymous reviewers wedge-top depozone could not be wholly connected to the who provided valuable comments and suggestions. major sea areas; they could have developed as “proximal sea inlets” closer to an emerging chain with high relief. These “proximal” depositional areas were flanked basinward by wider basins probably connected to major marine References areas which were developed in the slightly structurally external outer wedge-top depozone. In these basins coarse [1] Gugliotta C., L’evoluzione tortoniano-messiniana to medium and medium to fine grained wave-dominated dell’avanfossa s.l. siciliana; interazione tra sedimen- deltaic successions were predominantly deposited, ar- tazione e tettonica. PhD Thesis, Dottorato di Ricerca ranged with an overall transgressive trend. Deposition XXI Ciclo. Dipartimento di Geologia e Geodesia, Uni- in these external basins was primarily controlled by ini- versità degli Studi di Palermo, 2010

253 Partitioning between “wedge-top” river- and wave-dominated successions: an example from the late Tortonian – early Messinian Terravecchia Formation (NW Sicily)

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257 Partitioning between “wedge-top” river- and wave-dominated successions: an example from the late Tortonian – early Messinian Terravecchia Formation (NW Sicily)

Geol., 1999, 154, 383–398 the world. AAPG Special Volumes, 1986, 40, 567–584 [95] Sestini G., Flores G., Future petroleum provinces of

258 Calogero Gugliotta

Table 1. a) Symbols and acronyms used in the text and ﬁgures; b) Miall’s codiﬁcation of alluvial facies and architectural elements (mod. from [57–59])

259