Integrating facies and structural analyses with subsidence history in a Jurassic–Cretaceous intraplatform basin: Outcome for paleogeography of the Panormide Southern Tethyan margin (NW Sicily, Italy)

SEDGEO-05023; No of Pages 15 Sedimentary Geology xxx (2016) xxx–xxx

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Integrating facies and structural analyses with subsidence history in a Jurassic–Cretaceous intraplatform basin: Outcome for paleogeography of the Panormide Southern Tethyan margin (NW Sicily, Italy) Luca Basilone ⁎, Attilio Sulli, Maurizio Gasparo Morticelli Department of Earth and Marine Sciences, University of Palermo, Via Archirafi 22, 90123 Palermo, Italy

a r t i c l e

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Article history: Received 14 January 2016 Received in revised form 16 March 2016 Accepted 17 March 2016 Available online xxxx Editor: Dr. B. Jones Keywords: Intraplatform basin Basin analysis Tectonics vs. sedimentation Restoration Jurassic–Cretaceous paleogeography Southern Tethyan margin

a b s t r a c t We illustrate the tectono-sedimentary evolution of a Jurassic–Cretaceous intraplatform basin in a fold and thrust belt present setting (Cala Rossa basin). Detailed stratigraphy and facies analysis of Upper Triassic–Eocene successions outcropping in the Palermo Mts (NW Sicily), integrated with structural analysis, restoration and basin analysis, led to recognize and describe into the intraplatform basin the proximal and distal depositional areas respect to the bordered carbonate platform sectors. Carbonate platform was characterized by a rimmed reef growing with progradational trends towards the basin, as suggested by the several reworked shallow-water materials interlayered into the deep-water succession. More, the occurrence of thick resedimented breccia levels into the deep-water succession suggests the time and the characters of synsedimentary tectonics occurred during the Late Jurassic. The study sections, involved in the building processes of the Sicilian fold and thrust belt, were restored in order to obtain the original width of the Cala Rossa basin, useful to reconstruct the original geometries and opening mechanisms of the basin. Basin analysis allowed reconstructing the subsidence history of three sectors with different paleobathymetry, evidencing the role exerted by tectonics in the evolution of the narrow Cala Rossa basin. In our interpretation, a transtensional dextral Lower Jurassic fault system, WNW–ESE (present-day) oriented, has activated a wedge shaped pull-apart basin. In the frame of the geodynamic evolution of the Southern Tethyan rifted continental margin, the Cala Rossa basin could have been affected by Jurassic transtensional faults related to the lateral westward motion of Africa relative to Europe. © 2016 Elsevier B.V. All rights reserved.

1. Introduction Intraplatform basins are documented worldwide as peculiar synsedimentary tectonic features forming in rifted margins. Several examples, coming from the Mesozoic shallow-water carbonates of the Tethyan realm, have been described in the Alps (Bosellini, 1984; Jadoul et al., 1992), in the Transdanubian Range, Hungary (Haas and Tardy-Filácz, 2004), in the Apennines (Casero et al., 1991; Ciarapica, 2007; Carannante et al., 2009), in the Adria and Apulia (Stampfli, 2005; Vlahović et al., 2005; Čadjenović et al., 2008), and in the Sicilian region (Catalano and D'Argenio, 1978; Casero and Roure, 1994; Catalano et al., 2000; Basilone et al., 2010). Most of these studies relate the formation of intraplatform basins to strike-slip tectonics or transcurrent regime occurring in the rifted continental margins, during the opening of the Neotethys. Some of these intraplatform restricted troughs, with poorly oxygenated bottom waters, have originated large source rocks (e.g., the

⁎ Corresponding author. E-mail address: [email protected] (L. Basilone).

Streppenosa basin in the Iblean foreland, Frixa et al., 2000; Granath and Casero, 2004, the Vienna Basin in Austria, Fuchs and Hamilton, 2006). Among the different types of basins formed in strike-slip zones (see Allen and Allen, 2005), the “pull-apart basin” (sensu Ingersoll and Busby, 1995) is a class formed in local transtensional settings. Examples of modern pull-apart basins are those coming mainly from the Dead Sea and S. Andreas fault systems, developed in transcurrent/ transform margins and connected to continental rifting and/or spreading areas (Christie-Blick and Biddle, 1985; Garfunkel and Ben-Avraham, 2001; Hurwitz et al., 2002; Smit et al., 2008). Reconstruction of strike-slip basins from ancient geological systems, as those incorporated in the strongly deformed fold and thrust belts, are not simple to deciphering and few examples have been reported (McClay and Bonora, 2001, Gonzalez et al., 2012). In these cases, the most applied methodologies deal with three-dimensional stratigraphic and facies analyses aimed to adequate restoration of the platformbasin paleogeography (e.g., Doglioni, 1988; Escalona and Mann, 2003; Rouby et al., 1996; Haas et al., 2010). Detailed facies and structural analyses were used to highlight the main lateral facies changes among the study sections and to evaluate

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Please cite this article as: Basilone, L., et al., Integrating facies and structural analyses with subsidence history in a Jurassic–Cretaceous intraplatform basin: Outcome for pal..., Sedimentary Geology (2016), http://dx.doi.org/10.1016/j.sedgeo.2016.03.017

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the kinematics of the paleotectonic structures to reconstruct the evolution and geometry of the basin. Furthermore, the combination of traditional geology methods with basin analysis (i.e., subsidence history) is a useful tool for the reconstruction of ancient tectono-sedimentary structures, involved in a fold and thrust belt deformation, and for the understanding of the geological processes concurring in their formation (e.g., Pitman and Andrews, 1985; Hu et al., 2001; Bridges and Castle, 2003; Kwon et al., 2011). The study area, located in the north-western sector of the Sicilian Fold and Thrust Belt (FTB, Palermo Mts., Fig. 1), records a complex geological history lasting from the Late Triassic. The aim of this paper is to describe the Upper Triassic–Eocene tectono-sedimentary evolution of the outcropping successions pertaining to the Panormide carbonate platform, a domain developed along the Southern Tethyan margin. Using several integrated methodologies, comprising field geology, facies and basin analyses, stratigraphic correlation, structural analysis, and restoration, we were able to inset the reconstructed basin model in a reliable strike-slip tectonic setting and to relate it to the kinematics of the Mesozoic Southern Tethyan margin. 2. Geological setting and stratigraphic framework Sicily, located in the central Mediterranean, links the African Maghrebides with the Apennines across the Calabrian accretionary wedge (inset in Fig. 1). The Sicilian FTB, considered a segment of the Alpine collisional belt, is a complex stack of S- and SE-verging imbricates,

locally more than 15 km-thick. It is formed by Meso–Cenozoic deepwater carbonate and siliciclastic units, overriding a more than 10 kmthick carbonate platform thrust wedge, which is detached from the crystalline basement (Catalano et al., 2013a and references therein). Upper Miocene to middle Pleistocene clastics and evaporites fill thrust-top basins, sealing unconformably the shortened tectonic units (Gasparo Morticelli et al., 2015). The study area is located in the Palermo Mts (Fig. 1), the northernmost sector of the outcropping Sicilian FTB (inset in Fig. 1), which results from the piling-up of deep-water and carbonate platform tectonic units (Imerese and Panormide, Catalano et al., 2013b and references therein). The Panormide tectonic units consist of geological bodies, 900–1200 m thick and 4–8 km2 wide, stacked along thrusts, with ramp and flat geometry, with the interposition of Oligo-Miocene Numidian flysch deposits, postdating the tectonic emplacement (Abate et al., 1978). During this deformation a strong clockwise rotation (90° to 130°) occurred (Channell et al., 1990; Oldow et al., 1990). In the north-westernmost sector of the Palermo Mts (Figs. 1, 2a), the tectonic relationships among the Capo Rama-M. Palmeto, Cala Rossa-Piano Tavole, and M. Longa Panormide tectonic units, are highlighted. These are progressively superimposed along NW–SE trending thrusts (Fig. 2). The investigated successions, now incorporated into the Sicilian FTB, originated from the deformation of the Mesozoic-Cenozoic sedimentary cover of the Sicilian sector of the African continental margin (Catalano and D'Argenio, 1978). The Upper Triassic–Eocene Panormide succession is characterized by Bahamian-type platform facies, with periodic

Fig. 1. Structural map of the northern Palermo Mts, showing the relationships between shallow- and deep-water Mesozoic (Imerese and Panormide) carbonate units (modif. from Catalano et al., 2013b). The three minor tectonic units described in the text are differentiated; inside the tectonic map of Central Mediterranean (after Catalano et al., 2013a).

Please cite this article as: Basilone, L., et al., Integrating facies and structural analyses with subsidence history in a Jurassic–Cretaceous intraplatform basin: Outcome for pal..., Sedimentary Geology (2016), http://dx.doi.org/10.1016/j.sedgeo.2016.03.017

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Fig. 2. Geological map of the study area (a), geological cross-section (b) and panoramic view (c) showing the structural relationships among the Capo Rama-M. Palmeto, Cala Rossa-P. Tavole and M. Longa tectonic units; in (c) black lines show the bedding, white lines and symbols represent main thrusts and fold axis of ramp anticlines.

Please cite this article as: Basilone, L., et al., Integrating facies and structural analyses with subsidence history in a Jurassic–Cretaceous intraplatform basin: Outcome for pal..., Sedimentary Geology (2016), http://dx.doi.org/10.1016/j.sedgeo.2016.03.017

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subaerial exposure and continental deposition (Di Stefano et al., 2002; Basilone and Di Maggio, 2016), and pelagic sedimentation episodes (e.g., Ammonitico Rosso). Several formations, recently revised and amended (Basilone, 2012), compose the lithostratigraphic columns reconstructed for the study area. 3. Methodologies Field geology, stratigraphy, physical-stratigraphy, and facies analysis are the main methodologies used to recognize the geometries and relationships among the different outcropping lithofacies, and to define their sedimentological and environmental setting. Several thin-sections have been analysed using a petrographic microscope. The microfacies of the deep-water successions were agecalibrated using the available biostratigraphic studies (Catalano et al., 1973). Subsidence history was a useful tool for unravelling and reconstructing the evolution of the sedimentary basin (Watts and Ryan, 1976; Van Hinte, 1978; McKenzie, 1978). The backstripping method (Steckler and Watts, 1978) permitted to calculate the tectonic subsidence curve and to isolate it from other components of subsidence, mainly represented by the sediment load and sediment compaction, and from the effects of the sea-level fluctuations. Backstripping is generally performed on 1D borehole stratigraphy (e.g., North-western Atlantic margin, Sleep, 1971; Steckler and Watts, 1978; North Sea, Sclater and Christie, 1980; Allen and Allen, 2005), but under favourable conditions, reliable backstripping curves have been obtained from outcrops (e.g., Bond and Kominz, 1984; Berra and Carminati, 2010). The method assumes that, during progressive burial in a subsiding basin, sediment compaction is depth-dependent (Schmoker and Halley, 1982). In the decompaction procedure, we used the exponential porosity–depth relation ϕ ¼ ϕ0 exp−cy where ϕ is the porosity at depth y, ϕ0 is the porosity of sediments at the surface and c is an empirically-derived, lithologically-dependent coefficient. Decompaction parameters available in literature (Table A in supplementary materials, Sclater and Christie, 1980; Schmoker and Halley, 1982; Goldhammer, 1997) are usually referred to single lithologies. For multiple-lithology formations, we assumed mean decompaction parameters calculated by arithmetically averaging (weighted average) of the parameters of the single lithologies constituting the formation (Hözel et al., 2008; Tables B1, B2, and B3 in supplementary materials). Mesostructural analysis of fault planes and fold axes was used to reconstruct the kinematics of the main paleotectonic events and the orientation of the paleostructures. The structural data have been synthetized using statistical methods (stereograph projection obtained with Daisy 2.0 software, Salvini, 2001). The values of tectonic structures have been plotted by restoring the original attitude of the strata (horizontal bedding), avoiding the subsequent (Neogene) deformation. In the strongly deformed Jurassic–Eocene succession, outcropping in the natural section of the Cala Rossa cliff, we reconstructed the detailed geometry of the folds. On the latter, we applied unfold-structural modelling analysis (tool of Move 2013.1 software) using the “length linemethod” with the aim to restore the unfolded succession and to evaluate the original width of the basin. 4. Results 4.1. Stratigraphy and facies analysis The collected stratigraphic data have been synthetized in the stratigraphic columns of Fig. 3a. The Palmeto composite section has been

reconstructed from the M. Palmeto anticline and the Capo Rama coastal plain (Fig. 2a). The Longa section has been reconstructed from the northern sector of the faulted E-vergent anticline in the homonymous relief (Fig. 2a). The Cala Rossa section has been investigated and sampled along the coastal sector of the Terrasini village, from the Cala Rossa bay, where the oldest deposits outcrop, to the Magaggiari beach, where the Eocene carbonate deposits are followed by the Upper Oligocene clays of the Numidian flysch (Fig. 2a, c). The Tavole sections have been reconstructed from the flanks of the Piano Tavole anticline (Fig. 2a), where several metres of Upper Tithonian-Valanginian carbonate breccias, interlayered with pelagic deposits, outcrop. In the study area, the Jurassic–Cretaceous Panormide succession displays substantial lateral facies variations (Fig. 3b). The following description, related to different sections, took in account the thickness and facies variations of the coeval deposits (Table 1). 4.1.1. Norian–Sinemurian rock interval In the whole area, the Norian–Sinemurian carbonate platform deposits represent the common base of three differentiated Jurassic– Cretaceous successions (Fig. 3). These peritidal limestone (Table 1), 500–800 m-thick in the outcropping area, regionally reach more than 1000 m in thickness. The upper boundary of the unit is an erosional surface onlapped by younger pelagic limestone, whose age reveal different long hiatus along the three main sections. A dense and pervasive network of neptunian dykes, filled by red to gray crinoidal and ammonite bearing-pelagic limestone, characterizes the topmost beds (Figs. 4a, 5a). 4.1.2. Pliensbachian–Lower Tithonian rock interval This interval, mostly represented by pelagic deposits (Table 1), is characterized by strong lateral facies changes. Along the Palmeto and Longa sections, it is represented by Pliensbachian crinoidal lmst, cm-thick laminated iron-manganese oxide crusts (hardgrounds) and condensed thin-bedded ammonitebearing limestone (Bositra lmst), and Kimmeridgian-Lower Tithonian packstone–grainstone with pelagic crinoids, benthic foraminifers, and Apthycus sp., alternated with radiolarians and calpionellids-bearing mudstone and bedded chert (Saccocoma lmst). The Tavole sections display carbonate platform-derived breccias in massive beds and, upward, reddish and grayish thin-bedded ammonite-bearing mudstone–wackestone with intercalations of thick and massive fine-grained breccias. The latter consist of carbonate platform-derived elements and few red pelagic limestone angular fragments. The Middle Jurassic thin-bedded pelagites onlap, directly, the fractured Norian–Sinemurian peritidal lmst, revealing a long hiatus. The Cala Rossa section is a more or less continuous succession consisting of nodular siliceous mudstone, radiolarites and bedded cherts, alternated with fine-grained calciturbidites; thin-bedded Kimmeridgian-Lower Tithonian graded and laminated fine-turbiditic packstone, with abundant reworked shallow-water bioclasts, alternated to siliceous mudstone–wackestone with pelagic crinoids, radiolarians, sponge spicules and, in the uppermost beds, primitive calpionellids, follow upwards. 4.1.3. Upper Tithonian–Valanginian rock interval Along the Palmeto and Longa sections, gray boundstone, with calcified demosponges, alternated with oolitic grainstone and fore-reef breccias (Ellipsactinia reef lmst, Table 1), follow unconformably the Kimmeridgian-Lower Tithonian Saccocoma lmst. Upwards, paleokarst dissolution, fractures and neptunian dykes, filled by Aptian-Albian pelagites, affect the unit. Along the Tavole sections, thick massive resedimented channelized carbonate breccias (Fig. 4b) with dm-large reef-derived elements (Fig. 4c, d) alternated with graded and laminated oolitic packstone–

Please cite this article as: Basilone, L., et al., Integrating facies and structural analyses with subsidence history in a Jurassic–Cretaceous intraplatform basin: Outcome for pal..., Sedimentary Geology (2016), http://dx.doi.org/10.1016/j.sedgeo.2016.03.017

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Fig. 3. Detailed columnar sections of the Upper Triassic–Eocene deposits (a). The lateral facies variations among the distinguished units and lithofacies are shown in the sketch (b), where the crinoidal, Bositra and Saccocoma lmst lithofacies are not in scale.

grainstone (Fig. 4d) follow unconformably, with erosion, the older pelagites. In the Cala Rossa section, this interval is represented by fine-grained periplatform ooze (calpionellid lmst), alternated with thin-bedded calciturbidites and reef-derived calcareous breccias. 4.1.4. Late Lower Cretaceous–Eocene rocks interval Varicoloured thin-bedded mudstone–wackestone rich in planktonic foraminifers (globotruncanids and globorotalids), radiolarians, belemnites and Apthycus sp., outcrop all over the study sections (Table 1). In the Palmeto and Longa sections, these pelagites onlap the Ellipsactinia reef lmst, displaying low thicknesses. Differently, in the Tavole and Cala Rossa sections these deposits are thicker (Table 1). They onlap, with a few degrees angular relationships, the calcareous breccias in the Tavole section, filling the tectonically originated fractures and neptunian dykes (Fig. 5d). They rest, paraconformably, above the calpionellid lmst in the Cala Rossa section, where slumping structures

and thin-bedded graded and laminated fine-grained packstone (calciturbidites) occur (Fig. 3). 4.2. Backstripping and subsidence analysis The subsidence curves were obtained evaluating the effect of the tectonic subsidence and sediment load, treated as linked to the local (Airy) isostatic balance. Incorporating the various effects of paleobathymetry, eustatic change, and sediment load gives the Airy compensated tectonic subsidence (Steckler and Watts, 1978), applying the following formula: Y ¼ Sðρm −ρb =ρm −ρw Þ−ΔSL ðρw =ρm −ρw Þ þ ðWd −ΔSL Þ where Y is the depth of the basement, S is the decompacted thickness of the column obtained by the backstripping method, ρm, ρb, and ρw are mantle, mean sediment column, and water density respectively, ΔSL is

Please cite this article as: Basilone, L., et al., Integrating facies and structural analyses with subsidence history in a Jurassic–Cretaceous intraplatform basin: Outcome for pal..., Sedimentary Geology (2016), http://dx.doi.org/10.1016/j.sedgeo.2016.03.017

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Table 1 Main sedimentological and facies characteristics of the study deposits in the different reconstructed sections.

the paleosea-level relative to the present sea-level, and Wd is the paleowater-depth (Bond and Kominz, 1984). Given the uncertainties among the absolute values of the global eustatic curves obtained by different approaches (see discussion in Miller et al., 1998), accordingly to Allen and Allen (2005), a correction based on a widely accepted long-term eustatic variation (i.e., Haq et al., 1987) is, however, justified. To obtain paleobathymetry values we used sedimentological and paleoecological evidence, including micropaleontological methods (Leckie and Olson, 2003), and the published data concerning the same lithologies (Yellin-Dror et al., 1997; Zarcone and Di Stefano, 2010). The subsidence history of the backstripped sections, reconstructed from the study area, is shown in Fig. 6. Each panel displays tectonic and total subsidence curves (both decompacted and corrected for paleobathymetry and sea-level). The subsidence curves, generated from the different stratigraphic successions, show variable subsidence history, but some common features can be recognizable. The following four different evolutionary trends are displayed in each panel of Fig. 6: 1) During the Late Triassic (227 Ma)–Early Jurassic (190.8 Ma), the curves display high subsidence rates (up to 1200 m), guided both by the tectonic component and sediment load. During this time, sedimentation was able to keep pace with subsidence and about 1000 m of peritidal carbonates at 0 m water depth developed, suggesting high rates of carbonate production (ca. 30 m/My). Stretching of the continental lithosphere, producing rapid synrift subsidence, is by far the most important mechanism for prolonged and widespread subsidence (Allen and Allen, 2005). At the end of the rifting phase (Early Jurassic), an exponentially decreasing post-rift subsidence, due to thermal relaxation, is marked by the break in the subsidence curves, as predicted by the theoretical model (Fig. 6). 2) A marked differentiation between the three sections occurs since the Jurassic (190.8 to 155 Ma). A decreasing subsidence rate is recorded

by the Palmeto and Longa sections, whereas higher subsidence rates are estimated for the Tavole and Cala Rossa sections (Fig. 6). In the formers, hardground and condensed Ammonitico Rosso deposits accumulated in a paleowater depth varying from 100 to 150 m (Gill et al., 2004), suggesting that these areas maintained for the whole Jurassic a structural high setting (e.g., pelagic carbonate platforms top, Santantonio, 1994). The low rates of tectonic subsidence could be related to thermal subsidence (cooling). Differently, the coeval siliceous deposits (radiolarites of the Cala Rossa section) highlight a rapid increase in paleobathymetry, suggesting the active role exerted by tectonics. Regarding their paleobathymetry, the similar lithologies occurring in the Jurassic Tethyan sea, especially those associated with ophiolites and genetically related with the silica released by volcanic activity, have been referred to water depth below the lysocline and carbonate compensation depth (N 2500 m), largely based on present-day depth figures (Hsü and Jenkyns, 1974; Bosellini and Winterer, 1975; McBride and Folk, 1979). Other interpretations, based on the large oceanic radiolarian blooms during the Jurassic, have suggested that the accumulation of radiolarites can preferably be comparable with zones of high bioproductivity (and upraising CCD), as those related with upwelling (e.g., “Caribbean River Plume Model” in Baumgartner, 2013; see also Jenkyns and Winterer, 1982; De Wever et al., 1994). Furthermore, paleobathymetry determination based on unambiguous sedimentary features and autochthonous fossils suggests a paleowater depth around 500 m (Gill et al., 2004), which appears the most reliable paleobathymetry for our succession. About the depositional environment of the scarp breccias, considering that it was comprised between the deeper basinal areas and the pelagic carbonate platform top, where the condensed facies of the Bositra lmst accumulated, a paleowater depth around 350 m (average depth) with an uncertainty range of 240–450 m, is suggested. A 250 m of paleowater depth is

Please cite this article as: Basilone, L., et al., Integrating facies and structural analyses with subsidence history in a Jurassic–Cretaceous intraplatform basin: Outcome for pal..., Sedimentary Geology (2016), http://dx.doi.org/10.1016/j.sedgeo.2016.03.017

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indicated for the equivalent deposits of the Kimmeridgian–Lower Tithonian Saccocoma lmst outcropping in the Apennines, where Gill et al. (2004) found unambiguous autochthonous fossils (e.g., corals). 3) The Late Jurassic (147 Ma)–Early Cretaceous (138 Ma) subsidence curves highlight an overall uplifting trend (Fig. 6), interrupting the trend of the Jurassic continue-subsidence curve. Along the Palmeto and Longa curves, this effect is evidenced by the decrease of paleobathymetry due to the occurrence of shallow-water deposits (Ellipsactinia reef lmst). In the Cala Rossa curve, this uplifting trend is highlighted by the sedimentation of the calpionellid lmst referred to lower paleowater depth respect to the older siliceous lithologies (see also Yellin-Dror et al., 1997). These lower paleobathymetries can be put in relation to tectonic uplift as well as to the sea-level drops and general regressive trend recognized at that time (Jacquin and De Graciansky, 1998). 4) Relative stability is observed for the last tract of the subsidence curves, encompassing the Cretaceous (138 Ma)–Eocene (33 Ma) time interval, during which subsidence rate is relatively constant (Fig. 6). They are related to the lithosphere cooling and to the effect of sediment loading, as shown by the typical “concave-up” geometry. 4.3. Synsedimentary tectonics The measured tectonic structures consist of extensional fractures, neptunian dykes, and extensional paleofaults (Figs. 7, 8), frequently with lateral component of movement, as extrapolated by kinematic indicators

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(i.e., slickenlines, calcite fibers and stylolithic peaks). We dated the tectonic structures based on stratigraphic relationships (e.g., erosional unconformity that caps the previously deformed deposits, Fig. 4b) and different age of the deposits filling neptunian dykes recognized at different stratigraphic position (Figs. 4a, 5a, 5d). Based on different orientation and age (Fig. 8), we distinguished three deformational steps: 1) Lower Jurassic deformation. In the Norian-Sinemurian shallowwater lmst we measured: i) NW-SE oriented extensional paleofaults, SW-dipping and generally sub-vertical (225/83°, Fig. 7a); ii) NE–SW (N30°) oriented sub-vertical right transtensive fault planes with 15° of rake; iii) NW–SE (N135°) oriented sub-vertical extensional fractures; iv) NW–SE (N120–150°) and ENE–WSW (N70°) oriented neptunian dykes (Figs. 4a, 7a), filled by dolomitized breccias derived from fragmentation of the host deposits and generally orthogonal to the stratification (Fig. 5a). 2) Upper Jurassic deformation. In the Jurassic Bositra lmst we recognized: i) NW–SE (N145°) and E–W (N100°–80°) oriented subvertical neptunian dykes (Fig. 7b), filled by the same material of the host deposits; ii) NW–SE (N130°) and E–W (N95°) oriented extensional fractures and neptunian dykes; iii) NW–SE oriented enéchelon veins (Fig. 5b). 3) Cretaceous deformation. In the Upper Tithonian–Valanginian breccias, NW–SE (220/60° and 240/60°) oriented extensional paleofaults (Figs. 5c, 7b) and neptunian dykes, filled by yellowish mudstone of Cretaceous age (Fig. 5d), largely occur.

Fig. 4. Sedimentological and paleotectonic features of the lithofacies: a) condensed red Bositra lmst filling sub-vertical neptunian dykes (n) cutting the Norian-Sinemurian peritidal lmst (h); b) Upper Tithonian–Valanginian channelized conglomerates eroding the underlying faulted massive breccias; c) detail of the Upper Tithonian–Valanginian breccias, where coarsesized gray and red angular fragments, deriving from erosion of shallow-water Ellipsactinia reef lmst (e) and pelagic Bositra lmst (r) respectively, are welded by pelagites with radiolarian and calpionellids; d) Upper Tithonian–Valanginian massive breccias with large fragments of colonial corals (c) and oolitic grainstone (o). (For interpretation of the references to color in this figure legend, the reader is referred to the web version of this article.)

Please cite this article as: Basilone, L., et al., Integrating facies and structural analyses with subsidence history in a Jurassic–Cretaceous intraplatform basin: Outcome for pal..., Sedimentary Geology (2016), http://dx.doi.org/10.1016/j.sedgeo.2016.03.017

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Fig. 5. Structural features recognized in the studied sections: a) Jurassic neptunian dykes cutting the sub-vertical Norian–Sinemurian strata; b) right-lateral shear zone structures in the Jurassic ammonite-bearing lmst; c) normal fault plane cutting the Upper Tithonian–Valanginian carbonate breccias; d) neptunian dykes, cutting the Upper Tithonian–Valanginian carbonate breccias and successively filled by Cretaceous pelagites. (For interpretation of the references to color in this figure, the reader is referred to the web version of this article.)

4.4. Restoration The structural analysis of the pelagic succession exposed along the Cala Rossa cliff highlighted asymmetrical and double-verging trains of chevron NW-SE trending folds, frequently dissected along the hinge zone by reverse faults (Fig. 9). The folds are characterized by high amplitude and values of wavelength spanning 1 to 10 m (Fig. 9e). They are parallel-type with flexural slip mechanism, where the deformation occurs discretely between the bed interfaces. This deformation is associated with the Miocene compressional tectonic event, affecting and thickening the Panormide units along SW-dipping thrusts (Fig. 2). Some laterally continuous marker beds (i.e., the white limestone beds interlayered in the mostly reddish limestone, Fig. 9a) helped to measure the effective percentage of shortening, using an unfold percentage of the 100%, which means that we restored the whole deformation. Consequently, the present-day length of 2700 m, measured orthogonally to the main folds orientation (i.e. along the NE–SW direction, Fig. 2a), was restored to the original length of about 3566 m, corresponding to a shortening of 24.29%. The total length decreases SE-ward (Piano Tavole, Fig. 2a), where we measured a present-day length of about 1550 m. Here, most of the deformation is caused by high-angle reverse faults that produce horizontal displacement minor than in the Cala Rossa area, where a low-angle thrust plane occurs (Fig. 2b). As a consequence, we can presume that also the original length of the north-western sector of the basin (Cala Rossa) was major than the southeastern one (Piano Tavole).

5. Discussion On the whole, facies analysis highlighted the occurrence of different depositional areas during the Jurassic–Cretaceous. Those sectors

characterized by prevalent shallow-water sedimentation up to the Valanginian (Palmeto and Longa sections, Fig. 3) represent two structural highs, which are separated by a structural low (Tavole and Cala Rossa sections, Fig. 3a), whose sedimentary evolution was dominated by pelagic and resedimented deposits (Fig. 3b). In detail, the resedimented shallow-water carbonate materials occupied a sector of the basin proximal to the slope toe, whereas the prevalently pelagic succession represents the distal sector (Fig. 3). 5.1. Tectono-sedimentary evolution In the study area, the recognized features confirm that an overall synsedimentary tectonics was the main driving force influencing the sedimentary evolution (Fig. 10). Different trends in the subsidence curves (Fig. 6) within the same sedimentary basin are considered as a tool to hypothesize position, throw and period of activity of synsedimentary faults (Ten Veen and Kleinspehn, 2000; Wagreich and Schmid, 2002). Four main evolutionary stages have been differentiated: 5.1.1. Late Triassic–Early Jurassic stage The early evolutionary stage records high subsidence rates (stage 1 in Fig. 6a, b, c). The accommodation space, useful for the accumulation of the thick carbonate platform succession, reflects the subsidence effects of the thinning of lithosphere during the stretching phase of the continental rifting, as well as the high-frequency eustatic oscillations (Haq et al., 1987). The Early Jurassic tectonic episode produced block faulting of the Norian–Sinemurian carbonate platform, causing drowning and, consequently, widespread pelagic sedimentation during the whole Jurassic. 5.1.2. Jurassic stage The Jurassic evolutionary trend reflects the slow thermal subsidence following the rifting event, as recorded by the Palmeto and Longa subsidence curves (stage 2 in Fig. 6a). On the contrary, the high subsidence

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Fig. 6. Subsidence curves of the backstripped sections: a) Palmeto and Longa sections, b) Tavole sections, c) Cala Rossa section. Each panel shows both tectonic and total subsidence curves, displaying four evolutionary trends (1 to 4).

rate of the Tavole sections, and even more of the Cala Rossa section, is related to the intraplatform deformation. The abrupt facies change of the Jurassic deposits (Fig. 3b) and the patterns of the tectonic subsidence curves (stage 1 in Fig. 6b, c) suggest that the differentiated faulted

blocks of the original carbonate platform were displaced for several hundred of metres along sub-vertical walls/faults and differently among them (Fig. 10c, d, e). Tilting processes are supposed to be the cause producing the movements of the Tavole-Cala Rossa faulted blocks,

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Fig. 7. Detailed maps showing two examples of the Jurassic–Cretaceous structural sites. The legend is common for the two maps; location is reported in Fig. 2a. Base map from Google Earth©.

whose coeval deposits display different facies characteristics. Large grain-sized breccias deposited at the base of these fault scarps (Fig. 10c, d, e) pass downslope and basinward to fine-grained resedimented materials, along a gentle slope (Fig. 10c, e). A subsidence evolution similar to the Palmeto-Longa curves has been highlighted by Zarcone and Di Stefano (2010) in adjacent areas, confirming this regional trend (rifting to cooling phases) in the Sicilian sector of the continental margin. However, the Authors related the

drowning as mostly caused by productivity crises in the carbonate factory induced by paleoceanographic driving forces. In this frame, the differentiated trends of the Tavole and Cala Rossa curves could confirm the tectonic influence related to the opening of the intraplatform basin. 5.1.3. Late Jurassic–Early Cretaceous stage Complex and variable vertical motions since the Late Jurassic, including uplift (Fig. 6), suggest tectonic instability. This is consistent

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breccias appear as a distinctive feature of the sedimentation in faultcontrolled basins (e.g., Spence and Tucker, 1997; Allen and Densmore, 2000). The Late Jurassic–Early Cretaceous uplift, which interrupted the slow thermal subsidence of the structural highs during the Jurassic, is also recognized in the central Mediterranean, on the Tunisian (Jongsma et al., 1985) and Hyblean (Yellin-Dror et al., 1997) platforms and in the Eastern Mediterranean, on the Levant transform margin (Hirsch et al., 1995; Stampfli et al., 2001). 5.1.4. Cretaceous–Eocene stage The subsidence curves of this time interval suggest slow post-rift thermal and sediment load subsidence almost in the whole area (Fig. 6). At the end of the Upper Tithonian–Valanginian shallow-water sedimentation, a further tectonic event, also causing drowning of the carbonate platform, is suggested by the dense network of neptunian dykes, filled by the uppermost Lower Cretaceous pelagites. This event is also evidenced in the coeval apron breccias of the slope sector (Tavole sections), where the several neptunian dykes associated to extensional faults, are filled by these pelagites. This tectonic event, whose faults reactivated the Jurassic fault planes separating structural highs from low, caused different block dislocation. As a consequence, in the structural low more sediment accumulated, as evidenced by the large thickness of the Cretaceous–Eocene pelagic lmst in the Cala Rossa section with respect to the Palmeto and Longa sections (Table 1). The differences in thickness of these pelagic deposits, more than 250 m in the Cala Rossa (basin) section and 150–180 m in the Tavole (slope) section, suggest the occurrence of extensional and transtensional faults in between, causing different subsidence rates (Fig. 6b, c). Differently, the minor thickness (no more than 80 m) of these pelagic sediments in the Palmeto and Longa (pelagic platform) sections confirms that during the same time interval (more than 40 Ma), these areas were maintaining a structural high setting, where few and condensed pelagic sediments accumulated (Figs. 3b, 10c, d, e). 5.2. Geometry of the strike-slip system

Fig. 8. Stereographic projection of the collected structural data. On the left extensional fractures and neptunian dykes are reported; on the right extensional and transtensional faults.

with the presence of numerous fault-controlled basins in the region (Basilone, 2009). The Late Jurassic tectonic event produced displacements among the structural highs (i.e., Capo Rama-Palmeto and M. Longa sectors) and the structural lows (Tavole and Cala Rossa sectors) in an overall regional uplifting trend (Fig. 6). The structural high sectors, which have maintained a pelagic platform depositional setting up to Late Jurassic, were tectonically uplifted at a water depth at which the carbonate factory was able to produce the thick carbonate platform with rimmed shelf margins (Ellipsactinia reef lmst). Since Late Tithonian, carbonate platform sedimentation occurred only in the structural highs, where a continue accommodation space was created, up to some hundreds of metres, mostly caused by sea-level oscillations. Contemporaneously, in the adjacent structural low resedimentation of shallow-water materials was occurring. In the proximal sector of the basin, near the fault scarp, thick reef-derived breccias accumulated. They were transported, together with fine-grained calciturbidites, in the distal basin by means of submarine debris flows and turbiditic currents (Fig. 10c). The platform-derived turbiditic limestone and scarp

The mesostructural data (Figs. 7, 8) evidenced that the tectonic structures have maintained the same directions (present-day NW–SE) in the different tectonic phases. During the Early Jurassic, prevalent transtensive faults and neptunian dykes deformed the original carbonate platform producing an incipient subsiding area that developed as an intraplatform basin (Fig. 10b). Subsequently, during the Jurassic and Cretaceous, a prevalent extensional tectonics drove the deepening of the depositional environments in the distal part of the basin (Fig. 10b). The evaluation of the original extent of the basin, as estimated by the restoration of the Cala Rossa and Tavole sections (Fig. 9), suggests that the structural low was originally a narrow and elongated basin, wider towards the present-day northern sectors (Cala Rossa deep-water basin) and narrower towards the southern sectors (Piano Tavole slope, Figs. 2a, 10c). Basins with similar shape (i.e., narrow rhombic to spindle-shaped) are described from strike-slip fault systems, where elongated depression developed between two structural highs (Christie-Blick and Biddle, 1985; Woodcock and Fischer, 1986; Cloetingh et al., 1996; Mann, 2007). The geometric relationships among the transtensive synthetic and antithetic faults, and the orientation of coeval extensional fractures (Figs. 7, 8), appear very similar to those described for the damage zone between two segments of right strike-slip fault associated to the formation of pull-apart basin (McClay and Dooley, 1995; Kim et al., 2004; Cunningham and Mann, 2007). Their margins (i.e., the principal displacement zones) were characterized by development of en-échelon oblique-extensional faults (Fig. 10b) with increasing displacement (Dooley et al., 2004; Wu et al., 2009).

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Fig. 9. Restoration of the deformed Cala Rossa section: a) panoramic view of the Cala Rossa cliff; b) line drawing of the deformed stratal pattern; c) stereographic projection of the fold hinges; d) restored Cala Rossa section; e) details of the chevron folds; f) location map, where R1–R7 are the restored transects (see Fig. 2a for legend).

Differently from the quoted examples, in the Cala Rossa basin, which was involved in the compressional deformation acted during the Sicilian Miocene orogenic phase, it is more difficult to trace the master faults, whilst we are able to recognize the extensional faults separating the pull-apart basin from the carbonate platform structural highs (Fig. 10b, c). These faults could coincide with and were reactivated by those thrusts that at present-day bound the three tectonic units occurring in the study area (Figs. 2a, 10a). If we apply the counterclockwise rotation to restore to their original position the Panormide tectonic units (Fig. 10a), rotated during the orogenic event (Channell et al., 1990; Oldow et al., 1990), we obtain NNW–SSE oriented tectonic boundary among the differentiated faulted block compartments (Fig. 10b, c), in agreement with the presumed WNW–ESE right lateral shear zone (Fig. 10b). 5.3. Basin forming mechanisms The high subsidence rates recorded in the early evolutionary stage in all the backstripped sections (stage 1 in Fig. 6a, b, c) reflect rapid tectonic subsidence related to an overall rifting process. Theoretical studies and observations suggest that many strike-slip basins experience very little thermally driven post-rift subsidence (Mann et al., 1983; Pitman and Andrews, 1985; Wagreich and Schmid, 2002). In the Cala Rossa basin, the thermal anomaly decays during the rifting stage only for the structural highs bordering the basin (Palmeto and Longa sections), indicating rapid cooling of the crust (stage 2 in Fig. 6a). Differently, the Jurassic post-rift subsidence history of the basinal sectors displays rates similar to those of the previous rifting stage

(stage 2 of Tavole section, Fig. 6b) and higher in the deepest sector of the basin (stage 2 of Cala Rossa section, Fig. 6c). As a consequence, the extensional tectonics (i.e., the Jurassic extensional tectonic events recorded only in the Tavole and Cala Rossa sections) played an important role in the development of the intraplatform basin in a continue sub-rift process (sensu Hu et al., 2001). Moreover, rapid subsidence associated with initial sediment starvation is a typical characteristic of narrow pull-apart basins, as those associated with the S. Andreas transform fault (Pitman and Andrews, 1985). 5.4. Geodynamic implications Subsequent to the initial rifting, ocean floor spreading and development of large, continent-encroaching carbonate platforms characterized the evolution of the NW Neotethys since the Triassic. The opening of the ocean led to the thinning of the continental crust in the marginal zone and gave rise to tectonic backstepping of the shelf margin and development of narrow extensional basins on the shelf (Haas and Tardy-Filácz, 2004 and references therein). The tectono-sedimentary history of the Cala Rossa intraplatform basin, located during the Mesozoic in the north-western Sicilian sector of the Southern Tethyan margin, reflects: a) Rifting event that dissected the carbonate platform also with strikeslip movements (Late Triassic–Early Jurassic evolutionary stage); b) Subsequent continue extensional driving forces that caused high subsidence rates and conditioned the evolution of the intraplatform basin (Jurassic–Eocene evolutionary stages). The subsidence curves

Fig. 10. Reconstructed model of the Cala Rossa basin: a) present-day geographic distribution of the Capo Rama-M. Palmeto, Cala Rossa-Piano Tavole, and M. Longa tectonic units. Bold lines mark the present-day main thrusts bounding the tectonic units, corresponding to the faults bordering the Cala Rossa intraplatform basin; b) structural evolution of the Cala Rossa basin in the frame of a right-lateral shear zone. The light gray lines are the inferred WNW-ESE (present-day) transcurrent master faults; c) Jurassic–Cretaceous paleogeography of the Cala Rossa basin, where the main tectono-sedimentary features are shown; d) and e) inferred schematic cross-sections (see traces in c), showing the tectono-sedimentary relationships among the block-faulted compartments; f) paleogeographic reconstruction of the Sicilian intraplatform basins framed in the Tethyan paleogeography during the Early Jurassic (after Stampfli and Borel, 2002). Cr: Cala Rossa basin, Mb: Marineo and Balatelle basins, Sp: Streppenosa basin, Pa: Panormide platform, Si: Sicanian domain, Hy: Hyblean platform, La: Lagonegro domain, Ap: Apulia. The paleogeographic location of the Apenninic platform and related intraplatform basins (V: Verbicaro; P: Picentini; F: Filettino; C: Mt. Camicia; E: Emma) is from Ciarapica (2007) and Speranza et al. (2012).

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(Fig. 6), which display similar evolutionary trends to those reconstructed from other areas in the central and eastern Mediterranean basins (Hirsch et al., 1995; Yellin-Dror et al., 1997; Stampfli et al., 2001), support this interpretation.

This model is confirmed by the several small intraplatform basins developed during the Mesozoic in strike-slip zones both along the Sicilian (e.g., Upper Triassic Streppenosa basin, Catalano and D'Argenio, 1978; Frixa et al., 2000, Lower Jurassic Marineo and Balatelle basins, Catalano et al., 2000; Basilone et al., 2010) and Adria continental margins (e.g., Norian and Cretaceous basins in the Southern Apennines and Apulia carbonate platforms, Ciarapica, 2007; Speranza et al., 2012, Fig. 10f). The Cenomanian intraplatform basins within the Apulian Platform, developed as a result of extensional/transtensional tectonics (Carannante et al., 2009), produced important oil fields (e.g., Val d'Agri and Tempa Rossa). In our interpretation the present-day main thrusts bounding the tectonic units represent the inverted structure of the original normal faults dissecting the Panormide platform, as also observed for Tempa Rossa basin in the Apulian platform and Streppenosa basin in the Pelagian platform, in the southern Apennines and Sicily Channel, respectively (Casero and Roure, 1994). Thus, Cala Rossa could be interpreted as a pull-apart basin developed along a Lower Jurassic transcurrent fault with dextral movements, originated during the opening of the western Neotethys (Fig. 10f), and probably linked to the westward motion of Africa relative to fixed Europe (Dewey et al., 1989). The uplift event recorded during the Late Jurassic–Early Cretaceous could be related to the reactivation of the master fault, suggesting an overall re-organization of the lithospheric plates encompassing the Tethyan realm (e.g., Hirsch et al., 1995; Stampfli et al., 2001). 6. Conclusions Stratigraphic, sedimentological, and structural data collected in the Upper Triassic–Eocene Panormide sections outcropping in the northwestern edge of the Palermo Mts (NW Sicily) allow several features to be distinguished to reconstruct the tectono-sedimentary evolution and subsidence history of the region. The tectonic history highlighted by the backstripped sections reveals some evolutionary stages: (1) the early stage (Late Triassic–Early Jurassic) reflects rifting and rapid tectonic subsidence, generally leading to the continental break-up and opening of the NW Neotethys ocean; (2) the Jurassic stage reflects slow thermal subsidence in the basin shoulders and higher rate in the intervening depression; (3) the Late Jurassic–Early Cretaceous regional uplift interrupts the thermal subsidence curve trend; (4) the latest stage (Cretaceous–Eocene) suggests again slow thermal post-rift subsidence, influenced also by sediment load. The different subsidence curves, reconstructed from different positions in the sedimentary basin, demonstrate as its evolution could be driven by the noticed synsedimentary faults. Fault activity results in different subsidence in each sector of the basin, as recorded by thickness and/or facies changes across faults. Based on the lateral facies relationships, restoration, and structural analysis, the described intraplatform basin can be framed in a geometry reflecting strike-slip movements, characterized by transtensional regime where a pull-apart basin could develop. The tectono-sedimentary evolution of the Cala Rossa intraplatform basin contributes to the knowledge of the Mesozoic plate tectonics in the Southern Tethyan margin. This basin originated during the opening of the NW Neotethys, along a Mesozoic dextral transcurrent fault system, and could be linked to the westward motion of Africa relative to Europe. The Late Jurassic–Early Cretaceous uplift event suggests an overall reorganization of the lithospheric plates encompassing the Tethyan realm.

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Please cite this article as: Basilone, L., et al., Integrating facies and structural analyses with subsidence history in a Jurassic–Cretaceous intraplatform basin: Outcome for pal..., Sedimentary Geology (2016), http://dx.doi.org/10.1016/j.sedgeo.2016.03.017