Earth-Science Reviews 185 (2018) 624–648 Contents lists available at ScienceDirect Earth-Science Reviews journal homepage: www.elsevier.com/locate/earscirev Provenance of Mesozoic to Cenozoic circum-Mediterranean sandstones in relation to tectonic setting Salvatore Critelli T ⁎ Dipartimento di Biologia, Ecologia e Scienze della Terra, Università della Calabria, 87036 Arcavacata di Rende (CS), Italy A R T I C LE I N FO A B S T R A C T Keywords: Circum-Mediterranean Orogens Sandstone detrital modes Provenance analysis Paleogeography Paleotectonic evolution The composition and stratigraphic relations of clastic strata in diverse sedimentary basins of the circumMediterranean region reflect a complete record of provenance relations since break-up of Pangea, neo-Tethyan taphrogenesis, and subsequent plate convergence between the two major plates of Europe and Africa, and other related microplates of Iberia, Adria, Mesomediterranean, and toward to the eastern Mediterranean, the Anatolian microplate. Since plate reorganization after the breakup of Pangea, at the end of Paleozoic-earliest Mesozoic, clastic wedges filled sedimentary basins within geodynamic settings evolving from intracontinental rifts, rifted-continental margins, protoceanic basins, arc-trench basin-systems, remnant ocean basins, foreland basin systems and intramontane and back-arc basins within the circum-Mediterranean region. The changing nature of clastic particles in these clastic wedges reflect the provenance relations from different source rocks within the spatial and temporal evolving geo-puzzle terranes, including relations between ophiolitebearing, uplifted continental crust (both shallow to deep crust terranes), volcanic and sedimentary (particularly carbonate strata) source rocks. Mixed siliciclastic and carbonate shallow- to deep-marine clastic wedges are diffuse in many filled basin systems along the Mediterranean, as such as occurrence of volcaniclastic layers interbedded with siliciclastic wedges. The variable mosaic of source terranes within the Mediterranean region, offered the possibility to investigate provenance relations with a new plane of precision and sophistication, discriminating grain particles in clastic wedges using spatial (extrabasinal versus intrabasinal) and temporal (coeval versus noncoeval) distinction of detrital signals. The spatial/temporal approach in deciphering particles in clastic rocks has been widely used to detail the basinal dispersal pathways in different geotectonic settings, wherever mixed silicate and carbonate terranes act as the major source rocks, from rifted-continental margins to collisional orogens. 1. Introduction The circum-Mediterranean belt is largely debated in terms of geodynamic evolution, timing of deformations, and plate circuit reconstructions, that is mainly related to the multiple phases of closure of branches of the Tethys Ocean basin (e.g. Guerrera et al., 1993; Perrone et al., 2006; Critelli et al., 2008; Guerrera et al., 2005; Hosseinpour et al., 2016, and bibliography therein). The circum-Mediterranean belt evolved throughout the Mesozoic and into the Cenozoic within the area bounded by Mediterranean margins of Eurasia and Africa. The region (Fig. 1) is mainly dominated by the evolution of the Tethys Ocean system, occupying the region between Eurasia and Africa, characterized by multiple phases of rifting, seafloor spreading, subduction, and ⁎ collision. Only small fragments of oceanic crust formed within the Tethys Ocean are believed to be preserved in situ (Speranza et al., 2012), while remnants of its closure can be found in the Pyrenees, Alpine, and Carpathians orogenic belts in the north, the Anatolian plate in the east, and the northwestern coast of Arabia and Atlas Mountains in the south (e.g. Hosseinpour et al., 2016, and bibliography therein). The most characteristic expressions of circum-Mediterranean tectonism are foreland basin systems that mark orogenic belts that stand parallel with them. These orogenic systems are mainly related to the multiple phases of closure of branches of the Tethys Ocean basin, defining (i) north-vergent orogenic systems, as the Alps and Betic Cordillera, related to closure of the western branch of the Tethys Ocean (Ligurian-Piedmont-Nevadofilabride oceanic realm), and (ii) southern Corresponding author. E-mail address: [email protected]. https://doi.org/10.1016/j.earscirev.2018.07.001 Received 29 March 2018; Received in revised form 5 July 2018; Accepted 5 July 2018 Available online 18 July 2018 0012-8252/ © 2018 Elsevier B.V. All rights reserved. Earth-Science Reviews 185 (2018) 624–648 S. Critelli Fig. 1. Location of tectonic features in the Western Tethys and surrounding areas showing the position of the Mesomediterranean Microplate and related other plates. Modified from Perri et al. (2017). integrated with fresh data. Table 1 lists the mean detrital modes of all available data subdivided for the key tectonic history of the circumMediterranean belt in terms of types of sedimentary basins, the subdivision of the Tethyan oceanic realms (western vs. eastern and southern realms), geographic location of circum-Mediterranean thrust belts, and for some typical provenance terranes (i.e., cratonic provenance, magmatic-arc provenance). Data base consists of 63 sandstone suites made up of about 2235 individual samples for which point counts are reported in 56 different references. The modal sandstone composition is determined by point-counting using the Gazzi-Dickinson method (Ingersoll et al., 1984; Zuffa, 1985, 1987). The framework grain types that are used for discussions of detrital modes are those of Dickinson (1970, 1985), Zuffa (1985, 1987), Critelli and Le Pera (1994), and Critelli and Ingersoll (1995) and comprise: and northeastern-vergence orogenic systems, as northern Africa orogen (Rif and Tell belts) and Apennines, related to closure of the eastern/ southern branch of the Tethys Ocean (Maghrebide Flysch Basin, Lucanian and Ionian oceanic realm) (Fig. 1). Ancient sedimentary basins preserved within the circumMediterranean belt, are thick sedimentary sequences that record the tectonic evolution of the region since breakup of Pangea, from Tethyan Rifting, to consume Tethyan oceanic plate and related accretionary orogenic system. Mesozoic to Tertiary sedimentary strata are clastic, pelagic and carbonate dominantly. Clastic strata are well preserved in all the tectonic evolution of the circum-Mediterranean belt from supercontinent breakup to continental accretionary processes. This paper discusses detrital modes of sandstones in ancient sedimentary basins that are exposed in the circum-Mediterranean belt, discussing and combining previously published data with new fresh data. The sandstone compositions are fully compatible with derivation from sources within the circum-Mediterranean orogenic belt, defining intriguing provenance relations from recycled orogenic provenance, uplifted continental block provenance, cratonic provenance, and interbedded minor contribution from active magmatic arcs. These tectonic provenance terranes defines distinctive sandstone suites or mixed petrofacies. Provenance interpretations are essential to reconstruction and testing of paleogeographic and paleotectonic models. The general significance here is that the complex tectonic history of the circumMediterranean orogen can benefit from the application of petrographic provenance analysis as a test of alternative tectonic scenarios, that can be useful for analysis of sediment dispersal systems on a global scale of other major orogens. a) Quartz grains, including monocrystalline quartz grains (Qm), and polycrystalline quartzose lithic fragments (Qp), and total quartzose grains (Qt = Qm + Qp); b) Feldspar grains (F), including both plagioclase (P) and potassium feldspar (K); c) Aphanitic lithic fragments (L), as the sum of volcanic and metavolcanic (Lv and Lvm), sedimentary (Ls) and metasedimentary (Lm; including Lsm as the sum of Ls + Lm). Ls includes here also carbonate lithic fragments (extrabasinal carbonate grains of Zuffa, 1980, 1985; Critelli et al., 1990a, 2007), because of their importance and occurrence in detrital modes of Apenninic sandstones; d) phaneritic + aphanitic rock/lithic fragments (R), recalculated by point-counting of specific assignment of aphanitic Lm, Lv and Ls lithic fragments plus quartz, feldspar, micas and dense minerals in polimineralic fragments in which these minerals individually are larger than the lower limit of the sand range (0.0625 mm), that during counting are summed as quartz (Qm) and feldspar (F) or micas or dense mineral grains (e.g., Ingersoll et al., 1984; Zuffa, 1985, 1987; Critelli and Le Pera, 1994; Critelli and Ingersoll, 1995). 2. Data presentation and petrological parameters Most circum-Mediterranean sandstones that have been used in detail are of early-middle Mesozoic (upper Triassic-earliest Jurassic) to Cenozoic age. Sandstone compositions are reported here as mean detrital modes of selected suites in the format adopted to decipher and subdivide the suites for their tectonic provenances and types of sedimentary basins. Data set includes a review of both revised of previously published data For diagrams, the proportions of quartzose grains, feldspar grains and aphanitic lithic fragments are recalculated to 100%, and summary 625 65 20 27 40 84( ± 8)-6( ± 5)-10 ( ± 9) 89 ( ± 4)-9 ( ± 4)-2 ( ± 1) 94 ( ± 7)-2 ( ± 1)-4 ( ± 2) 91 ( ± 4)-4 ( ± 1)-5 ( ± 3) 79( ± 7)-1( ± 1)-20 ( ± 7) 70( ± 7)-1( ± 1)-29 ( ± 7) 77( ± 8)-6( ± 5)-16 ( ± 9) 79 ( ± 9)-5 ( ± 5)-16 ( ± 11) ( ± 6)-0 ( ± 6)-0 ( ± 6)-4 ( ± 6)-4 ( ± 1)-1 ( ± 1)-1 ( ± 4)-4 ( ± 5)-2 ( ± 6) ( ± 6) ( ± 3) ( ± 3) 626 F. Betic Cordillera: foreland sequences Syn-orogenic foreland Betic Cordillera, Spain (Río Pliego and El Niño de Mula formations) 8 4 19 18 6 19 23 16 12 32 18 ( ± 2)-1 ( ± 1)-4 ( ± 3) ( ± 4)-3 ( ± 2)-10 ( ± 4) ( ± 3)-0 ( ± 0)-3 ( ± 3) ( ± 3)-0 ( ± 0)-3 ( ± 3) ( ± 5)-8 ( ± 4)-0 ( ± 0) ( ± 5)-5 ( ± 5)-0 ( ± 0) ( ± 5)-11 ( ± 5)-0 ( ± 0) ( ± 3)-0 ( ± 0)-3 ( ± 3) ( ± 3)-2 ( ± 2)-4 ( ± 2) ( ± 4)-0 ( ± 0)-8 ( ± 4) 44 ( ± 20)-1 ( ± 1)-55 ( ± 20) 95 87 97 97 92 95 89 97 94 92 ( ± 2)-1 ( ± 1)-5 ( ± 3) ( ± 4)-3 ( ± 2)-12 ( ± 4) ( ± 3)-0 ( ± 0)-4 ( ± 3) ( ± 3)-0 ( ± 0)-4 ( ± 3) ( ± 5)-8 ( ± 5)-0 ( ± 0) ( ± 5)-5 ( ± 5)-0 ( ± 0) ( ± 5)-11 ( ± 5)-0 ( ± 0) ( ± 3)-0 ( ± 0)-4 ( ± 3) ( ± 5)-2 ( ± 4)-6 ( ± 0) ( ± 4)-0 ( ± 0)-10 ( ± 4) 46 ( ± 20)-1 ( ± 1)-53 ( ± 20) 94 85 96 96 92 95 89 96 92 90 ( ± 1)-0 ( ± 4)-3 ( ± 1)-0 ( ± 1)-0 ( ± 5)-6 ( ± 5)-0 ( ± 5)-7 ( ± 1)-0 ( ± 4)-3 ( ± 5)-8 ( ± 6)-5 ( ± 3)-6 ( ± 5)-3 ( ± 6)-2 ( ± 6)-2 ( ± 0)-1 ( ± 3)-2 ( ± 0)-1 ( ± 0)-1 ( ± 3)-4 ( ± 0)-3 ( ± 3)-4 ( ± 0)-1 ( ± 3)-2 ( ± 1) ( ± 3) ( ± 1) ( ± 1) ( ± 3) ( ± 1) ( ± 3) ( ± 1) ( ± 3) ( ± 3)-16 ( ± 4) ( ± 3)-21 ( ± 5) ( ± 2)-16 ( ± 2) ( ± 2)-27 ( ± 5) ( ± 15)-70 ( ± 13) ( ± 2)-18 ( ± 4) (continued on next page) 99 ( ± 1)-0 ( ± 0)-1 ( ± 1) 71 74 73 70 28 80 – – – – 75 ( ± 5)-4 ( ± 3)-21 ( ± 2) 82 ( ± 8)-3 ( ± 2)-15 ( ± 7) – 94 ( ± 4)-4 ( ± 3)-2 ( ± 2) 91 ( ± 3)-1 ( ± 1)-8 ( ± 3) – – 99 99 92 94 99 95 99 99 90 97 89 99 95 – ( ± 5)- 7( ± 6) ( ± 4)-1 ( ± 1) ( ± 1)-0 ( ± 0) ( ± 1)-3 ( ± 3) ( ± 1)- 11( ± 6) ( ± 1)- 11( ± 6) ( ± 5)- 8( ± 6) ( ± 5)-5 ( ± 4) QmKP D. Craton-derived Sequences (suites from Rif and Tell represent the filling of its foreland basin system) D1 Pre-Orogenic (Espuña and As Formations), Betics, Spain D2 Asilah Sandstone (Rif, Morocco) D3 Zoumi-Sidi Mrait, Ouezzane Units (Rif, Morocco) D4 Fortuna Formation D5 Numidian Sandstone (Sicily) D6 Numidian Sandstone (southern Apennines) D7 Numidian Sandstone (southern Apennines) D8 Bifurto Formation (Apennine Platform Unit) D9 Numidian Sandstone (northern Africa: Rif, Tell) D10 Tanger Unit (Burdigalian-Serravallian) ( ± 7)-6 ( ± 4)-9 ( ± 1)-2 ( ± 4)-4 ( ± 6)-1 ( ± 6)-1 ( ± 7)-6 ( ± 6)-5 QmFLt – – – 74 ( ± 6)-9 ( ± 3)-17 ( ± 5) – – 87 90 98 93 88 88 86 90 QtFL C. Late Cretaceous-Paleogene Subduction Complexes western Tethyan Realm (Onset of rifting 270–200 Ma; Onset of Sea floor Spreading (SFS) 200–150 Ma; End of SFS 130–90 Ma) 119 53 ( ± 19)-19 ( ± 13)-28 ( ± 21) 51 ( ± 19)-19 ( ± 13)-30 ( ± 21) C1 Late Cretaceous Ligurian-Piedmont Basin (Alpine Tethys) including Ostia Sandstone, Mt Caio, Mt Cassio, Casanova Sandstone, Sillano and Pietraforte formations C2 Paleogene-earliest Miocene Remnant Ocean Basin (eastern and southern Tethys) C2a Tectonic Mélange (Eocene-Late Oligocene; Lucanian Ocean) 14 62 ( ± 4)-21 ( ± 6)-17 ( ± 7) 61 ( ± 4)-21 ( ± 6)-18 ( ± 7) C2b Saraceno Formation (Lucanian Ocean) 15 54 ( ± 11)-10 ( ± 5)-36 ( ± 10) 52 ( ± 11)-10 ( ± 5)-38 ( ± 10) C3 Maghrebian Flysch Basin (Late Oligocene-early Miocene) C3a Corleto-Perticara Formation 55 66 ( ± 4)-18 ( ± 6)-16 ( ± 7) 62 ( ± 4)-18 ( ± 6)-20 ( ± 7) C3b Albanella Fm. 15 66 ( ± 4)-16 ( ± 6)-18 ( ± 7) 62 ( ± 4)-16 ( ± 6)-22 ( ± 7) C3c Colle Cappella Formation 24 64 ( ± 4)-16 ( ± 6)-20 ( ± 7) 60 ( ± 4)-16 ( ± 6)-24 ( ± 7) C3d Tufiti di Tusa Formation (quartzolithic suite) 16 50 ( ± 18)-18 ( ± 3)-32 ( ± 16) 46 ( ± 18)-18 ( ± 3)-36 ( ± 16) C3e Tufiti di Tusa Formation (volcanolithic suite) 22 14 ( ± 6)-28 ( ± 15)-58 ( ± 13) 12 ( ± 6)-28 ( ± 15)-60 ( ± 13) C3f Corleto Formation in wells 15 62 ( ± 11)-14 ( ± 3)-24 ( ± 9) 61 ( ± 11)-14 ( ± 3)-25 ( ± 9) C3g Algeciras Formation, Spain 16 57 ( ± 9)-29 ( ± 5)-14 ( ± 9) 55 ( ± 9)-29 ( ± 5)-16 ( ± 9) C3h Viñuela Formation, Spain 8 55 ( ± 9)-5 ( ± 5)-40 ( ± 9) 52 ( ± 7)-5 ( ± 5)-43 ( ± 9) C3i Beni Ider Formation, Rif, Morocco 21 40 ( ± 8)-35 ( ± 5)-25 ( ± 9) 37 ( ± 8)-35 ( ± 5)-28 ( ± 9) C3j Sidi Abdesslam Formation, Morocco 6 52 ( ± 6)-9 ( ± 3)-39 ( ± 6) 48 ( ± 6)-9 ( ± 3)-43 ( ± 6) C4 Late Oligocene-earliest Miocene forearc basin over Mesomediterranean microplate C4a Paludi Formation 38 57 ( ± 5)-36 ( ± 6)-7 ( ± 8) 55 ( ± 5)-36 ( ± 6)-9 ( ± 8) C4b Stilo-Capo d'Orlando Formation 55 47 ( ± 7)-49 ( ± 6)-4 ( ± 9) 45 ( ± 7)-49 ( ± 6)-6 ( ± 9) C4c Frazzanò Formation 27 62 ( ± 5)-23 ( ± 4)-15 ( ± 4) 67 ( ± 5)-21 ( ± 4)-12 ( ± 4) C4d Piedimonte Formation 23 60 ( ± 5)-21 ( ± 4)-19 ( ± 4) 60 ( ± 5)-21 ( ± 4)-19 ( ± 4) C4e Ciudad Granada Fm., Spain 5 41 ( ± 7)-4 ( ± 5)-55 ( ± 8) 37 ( ± 7)-4 ( ± 5)-59 ( ± 9) C4f Fnideq Formation, Morocco 3 81 ( ± 6)-7 ( ± 4)-12 ( ± 6) 79 ( ± 6)-7 ( ± 4)-14 ( ± 6) Jurassic Longobucco Group (F. Petrone and Trionto Fm.) Lucanian Ocean Complex (Crete Nere-Frido Unit) Lower Cretaceous Maghrebian Flysch Basin Monte Soro Unit (Cretaceous, Sicily) B. Proto-Oceanic Rift Troughs (Onset of Sea floor Spreading (SFS) 180–170 Ma; End of SFS 130–120 Ma) B1 B2 B3 B4 N 12 90 57 41 Description and Location of Unit A. Early Mesozoic Terrestrial Rift Valleys (mainly continental redbeds; Onset of rifting 250–220 Ma) A1 Pseudoverrucano Tuscany, Italy A2 Calabria-Peloritani Redbeds (Longi-Taormina, Stilo and Longobucco Group) A3 Rif, Morocco (Sebtide, Ghomaride units) A4 Betic Cordillera (Malaguide and Alpujarride units) Suite Table 1 Mean framework modes of selected Circum-Mediterranean Sandstone Suites. Dataset includes southern Apennines, Calabria, Sicily, northern Africa and southern Spain. S. Critelli Earth-Science Reviews 185 (2018) 624–648 Description and Location of Unit 627 Baronia Synthem (early Pliocene) Sferracavallo Synthem (middle Pliocene) 58 ( ± 26)-1 ( ± 1)-41 ( ± 27) 65 ( ± 18)-1 ( ± 2)-34 ( ± 19) 94 ( ± 17)-4 ( ± 9)-2 ( ± 11) 79 ( ± 23)-2 ( ± 4)-19 ( ± 23) 1 ( ± 1)-4 ( ± 5)-96 ( ± 5) 0 ( ± 1)-5 ( ± 6)-95 ( ± 6) RgRsRm A3 A4 LmLvLs 50 ( ± 7)-43 ( ± 5)-7 ( ± 3) 50 ( ± 6)-39 ( ± 6)-11 ( ± 4) 50 ( ± 8)-36 ( ± 9)-14 ( ± 6) 50 ( ± 7)-38 ( ± 7)-12 ( ± 5) 1 ( ± 1)-4 ( ± 4)-96 ( ± 6) 1 ( ± 1)-4 ( ± 4)-96 ( ± 6) QpLvmLsm 140 98 84 ( ± 6)-12 ( ± 5) ( ± 6)-5 ( ± 2) ( ± 5)-19 ( ± 6) ( ± 7)-11 ( ± 7) ( ± 5)-5 ( ± 2) ( ± 7)-9 ( ± 7) ( ± 6)-5 ( ± 2) ( ± 5)-9 ( ± 6) ( ± 11)-18 ( ± 17)-30 ( ± 20) ( ± 8)-5 ( ± 4)-83 ( ± 12) ( ± 10)-21 ( ± 5)-31 ( ± 14) ( ± 5)-47 ( ± 8)-14 ( ± 4) ( ± 6)-20 ( ± 5)-38 ( ± 6) ( ± 4)-42 ( ± 5)-40 ( ± 5)-28 ( ± 7)-34 ( ± 5)-48 ( ± 5)-44 ( ± 5)-40 ( ± 5)-40 49 ( ± 6)-37 ( ± 8)-14 ( ± 6) 49 ( ± 3)-37 ( ± 4)-14 ( ± 4) 49 ( ± 5)-37 ( ± 6)-14 ( ± 5) 52 12 48 39 42 5 21 5 156 33 27 9 46 55 53 55 47 47 55 51 68 30 48 46 14 21 22 52 ( ± 4)-18 ( ± 3)-30 ( ± 5) 62 ( ± 5)-23 ( ± 4)-15 ( ± 4) 52 ( ± 5)-45 ( ± 5)-3 ( ± 1) 52 ( ± 5)-45 ( ± 5)-3 ( ± 1) 52 ( ± 5)-45 ( ± 5)-3 ( ± 1) 55( ± 5)-38( ± 5)-7( ± 3) 42 62 20 22 18 ( ± 5)-15 ( ± 5) ( ± 5)-13 ( ± 4) ( ± 5)-13 ( ± 4) ( ± 5)-9 ( ± 3) ( ± 5)-10 ( ± 3) ( ± 5)-12 ( ± 4) 64 65 65 57 61 62 ( ± 6)-21 ( ± 4)-22 ( ± 4)-22 ( ± 5)-34 ( ± 4)-29 ( ± 5)-26 QtFL 42 72 54 26 26 N A. Early Mesozoic Terrestrial Rift Valleys (mainly continental redbeds; Onset of rifting 250–220 Ma) A1 65 ( ± 17)-2 ( ± 3)-33 ( ± 17) 87 ( ± 17)-7 ( ± 10)-6 ( ± 14) A2 65 ( ± 17)-2 ( ± 3)-33 ( ± 17) 87 ( ± 17)-7 ( ± 10)-6 ( ± 14) Suite J. Backarc extensional rifting basins (Late Miocene) Tortonian-Messinian sequences of western Calabria I. Mid- Late Miocene-Pliocene Wedge-Top Basins I1 Crotone Basin I2 Rossano Basin (regionalTortonian-early Pliocene petrofacies (G1-G2) H. Pliocene foreland basin H1 H2 (regional early-middle Pliocene petrofacies (F1 + F2) G. Foreland Basin Systems: Apennines (Tortonian-Messinian) G9 Castelvetere Formation G10 Sorrento Sandstone Formation G11 Argilloso-Arenacea and Frosinone fms. G12 San Bartolomeo Formation G13 Vallone Ponticello and Villanova del Battista formations G14 Anzano Unit (Altavilla Supersynthem) G15 Tempa del Prato-Civita Sandstone (regional late Tortonian-Messinian petrofacies (E9 -to- E153) G16 Torrente Fiumarella Unit (Altavilla Supersynthem) G17 Brecce della Renga Formation (calclithite petrofacies) G18 Brecce della Renga Formation (quartzofeldspathic) G19 Laga Formation G20 Umbria-Marche Tortonian-Messinian basins G. Foreland Basin Systems: Apennines (early Miocene-early Tortonian) G1a,b,c Cilento Group: G1a Pollica Formation G1b San Mauro Formation G1c Albidona Formation G2 San Giorgio Formation G3 Serra Palazzo Formation (Lagonegro Basin) (regional Langhian-early Tortonian petrofacies (G1-to-G3) G4 Piaggine Sandstone (Serravallian-early Tortonian) G5 Gorgoglione Formation G6 Monte Sacro Formation G7 Oriolo Formation G8 Nocara Conglomerate Formation (regional early Tortonian petrofacies (G5-to-G8) Suite Table 1 (continued) ( ± 6)-21 ( ± 4)-22 ( ± 4)-22 ( ± 5)-34 ( ± 4)-29 ( ± 5)-26 ( ± 5)-18 ( ± 5)-15 ( ± 5)-15 ( ± 5)-11 ( ± 5)-14 ( ± 5)-14 ( ± 5) ( ± 4) ( ± 4) ( ± 3) ( ± 3) ( ± 4) ( ± 6)-13 ( ± 5) ( ± 6)-7 ( ± 2) ( ± 6)-26 ( ± 6) ( ± 7)-14 ( ± 7) ( ± 5)-8 ( ± 3) ( ± 7)-12 ( ± 8) ( ± 6)-7 ( ± 2) ( ± 5)-12 ( ± 6) ( ± 12)-18 ( ± 17)-33 ( ± 21) ( ± 7)-5 ( ± 4)-84 ( ± 11) ( ± 10)-21 ( ± 5)-34 ( ± 14) ( ± 5)-47 ( ± 8)-15 ( ± 4) ( ± 6)-20 ( ± 5)-46 ( ± 6) ( ± 4)-42 ( ± 5)-40 ( ± 5)-28 ( ± 7)-34 ( ± 5)-48 ( ± 5)-44 ( ± 5)-40 ( ± 5)-40 ( ± 5)-33 ( ± 4)-22 ( ± 4)-26 ( ± 3)-23 ( ± 2)-30 ( ± 4)-26 ( ± 4)-22 ( ± 4)-26 ( ± 4) ( ± 4) ( ± 6) ( ± 5) ( ± 5) ( ± 6) ( ± 4) ( ± 5) ( ± 15)-12 ( ± 8)-12 ( ± 8) ( ± 8)-12 ( ± 7)-17 ( ± 6) ( ± 2)-10 ( ± 2)-22 ( ± 2) ( ± 6)-24 ( ± 5)-34 ( ± 6) ( ± 5)-17 ( ± 4)-20 ( ± 4) ( ± 6)-15 ( ± 5)-22 ( ± 5)-12 ( ± 7)-17 ( ± 5)-22 ( ± 6)-24 ( ± 5)-22 ( ± 6)-19 ( ± 3)-7 ( ± 4)-19 ( ± 4) ( ± 4)-13 ( ± 3)-16 ( ± 3) ( ± 5)-20 ( ± 4)-27 ( ± 5) ( ± 5)-20 ( ± 4)-27 ( ± 5) ( ± 5)-20 ( ± 4)-27 ( ± 5) ( ± 5)-18 ( ± 4)-23 ( ± 5) ( ± 6)-9 ( ± 3)-21 ( ± 4) ( ± 6)-15 ( ± 4)-11 ( ± 4) ( ± 6)-15 ( ± 4)-11 ( ± 4) ( ± 5)-15 ( ± 2)-23 ( ± 4) ( ± 3)-10 ( ± 4)-24 ( ± 4) ( ± 6)-13 ( ± 3)-18 ( ± 4) 54 ( ± 6)-24 ( ± 3)-22 ( ± 4) 55 ( ± 6)-23 ( ± 5)-22 ( ± 5) 57 ( ± 9)-21 ( ± 5)-22 ( ± 7) 56 ( ± 7)-22 ( ± 5)-22 ( ± 6) 55 ( ± 7)-19 ( ± 5)-26 ( ± 7) 54 ( ± 4)-19 ( ± 3)-27 ( ± 1) 54 ( ± 5)-19 ( ± 4)-27 ( ± 4) 76 71 68 42 63 52 56 62 60 48 50 56 55 74 71 53 53 53 59 70 74 74 62 66 69 QmKP (continued on next page) Hosseinpour et al., 2016 and bibliography therein unpublished data Zuffa et al., 1980; Critelli and Ferrini, 1988; Critelli et al., 2008, 2018; Perri et al., 2011; and unpublished data Critelli et al., 2008, 2018; Zaghloul et al., 2010 Critelli et al., 2008, 2018; Perri et al., 2013 Reference 48 ( ± 7)-43 ( ± 5)-9 ( ± 3) 48 ( ± 6)-39 ( ± 6)-11 ( ± 7) 55 ( ± 7)-36 ( ± 9)-9 ( ± 6) 52 ( ± 7)-38 ( ± 7)-10 ( ± 7) 46 ( ± 5)-37 ( ± 8)-17 ( ± 8) 43 ( ± 3)-37 ( ± 4)-20 ( ± 5) 45 ( ± 5)-37 ( ± 6)-18 ( ± 6) 49 11 45 34 34 45 53 46 52 44 44 53 48 50 ( ± 4)-18 ( ± 3)-32 ( ± 4) 59 ( ± 4)-23 ( ± 4)-18 ( ± 3) 50 ( ± 5)-45 ( ± 5)-5 ( ± 1) 50 ( ± 5)-45 ( ± 5)-5 ( ± 1) 50 ( ± 5)-45 ( ± 5)-5 ( ± 1) 53( ± 5)-38( ± 5)-9( ± 3) 61 63 63 55 57 60 QmFLt S. Critelli Earth-Science Reviews 185 (2018) 624–648 Zuffa and De Rosa, 1978 Cavazza, 1989; Puglisi, 1998 Puglisi et al., 2001 Puglisi, 2008, 2014; Puglisi et al., 2001 Guerrera et al., 1997; Puglisi et al., 2001; MartinAlgarra et al., 2000 Puglisi et al., 2001 – – – – – – 4 ( ± 3)-30 ( ± 12)-66 ( ± 14) 45 ( ± 13)-28 ( ± 14)-27 ( ± 6) – – – – – – – – Late Oligocene-earliest Miocene forearc basin over Mesomediterranean microplate – – – – – – 11 ( ± 6)-2 ( ± 3)-87 ( ± 7) 72 ( ± 14)-4 ( ± 3)-24 ( ± 6) – – – C3f C3g C3h C3i C3j C4 C4a C4b C4c C4d C4e C4f 628 12 ( ± 14)-0 ( ± 0)-88 ( ± 14) – G. Foreland Basin Systems: Apennines (early Miocene-early Tortonian) G1a,b,c G1a 4 ( ± 3)-32 ( ± 13)-64 ( ± 12) F. Betic Cordillera: foreland sequences D10 57 ( ± 9)-34 ( ± 13)-9 ( ± 6) 37 ( ± 27)-0 ( ± 0)-63 ( ± 27) – D. Craton-derived Sequences (suites from Rif and Tell represent the filling of its foreland basin system) D1 – – D2 14 ( ± 3)-2 ( ± 3)-84 ( ± 6) 3 ( ± 4)-2 ( ± 2)-95 ( ± 4) D3 – – D4 – – D5 – – D6 – – D7 – – D8 – – D9 – – – 8 ( ± 3)-88 ( ± 7)-4 ( ± 3) 9 ( ± 6)-4 ( ± 3)-87 ( ± 10) 0 ( ± 0)-64 ( ± 7)-36 ( ± 7) – 0 ( ± 1)-95 ( ± 3)-4 ( ± 3) – – – – – – – – – – – – – – Valloni and Zuffa, 1984 – (continued on next page) Critelli and Le Pera, 1990a, 1994, 1995a Perri et al. (2017) Perri et al., 2017 Cazzola and Critelli, 1987 Cazzola and Critelli, 1987 Van Houten, 1980; and unpublished data Barbera et al., 2014 Carbone et al., 1987; Patacca et al., 1992; Fornelli, 1998; Fornelli et al., 2015 Critelli, 1999 Moretti et al., 1991; Thomas et al., 2010; and unpublished data Zaghloul et al., 2005 Critelli, 1993 Critelli, 1993 Hosseinpour et al., 2016 and bibliography therein (SFS) 200–150 Ma; End of SFS 4 ( ± 3)-90 ( ± 6)-6 ( ± 4) Zuffa et al., 1980; Perri et al., 2008 Critelli, 1993, and unpublished data El Talibi et al., 2014 Barbera et al., 2011 C3e 1 ( ± 1)-4 ( ± 5)-96 ( ± 5) – – – Hosseinpour et al., 2016 and bibliography therein Reference Fornelli and Piccarreta, 1997; Critelli et al., 2017 Critelli et al., 1994 Critelli, 1999; Perrotta, 2006 Critelli et al., 1990a, 1990b; Perri et al., 2012; and unpublished data Critelli and Le Pera, 1990a, 1990b; Perri et al., 2012; de Capoa et al., 2002; unpublished data Puglisi et al., 2001 Guerrera et al., 1987; Puglisi et al., 2001 Puglisi et al., 2001; Zaghloul et al., 2002 Puglisi et al., 2001 94 ( ± 17)-0 ( ± 0)-6 ( ± 11) 30 ( ± 28)-0 ( ± 0)-70 ( ± 28) – – RgRsRm – 6 ( ± 3)-6 ( ± 6)-88 ( ± 11) 6 ( ± 3)-15 ( ± 6)-79 ( ± 11) – 58 ( ± 26)-1 ( ± 1)-41 ( ± 27) 56 ( ± 20)-0 ( ± 0)-44 ( ± 20) – – B. Proto-Oceanic Rift Troughs (Onset of Sea floor Spreading (SFS) 180–170 Ma; End of SFS 130–120 Ma) B1 B2 B3 B4 LmLvLs C. Late Cretaceous-Paleogene Subduction Complexes western Tethyan Realm (Onset of rifting 270–200 Ma; Onset of Sea floor Spreading 130–90 Ma) C1 – – C2 Paleogene-earliest Miocene Remnant Ocean Basin (eastern and southern Tethys) C2a 4 ( ± 2)-58 ( ± 4)-38 ( ± 4) 37 ( ± 4)-57 ( ± 4)-6 ( ± 3) C2b 6 ( ± 3)-5 ( ± 3)-89 ( ± 4) 56 ( ± 15)-5 ( ± 4)-39 ( ± 15) C3 C3a 8 ( ± 3)-16 ( ± 5)-76 ( ± 7) 64 ( ± 11)-16 ( ± 3)-20 ( ± 6) C3b 3 ( ± 3)-10 ( ± 6)-87 ( ± 6) 84 ( ± 6)-6 ( ± 5)-10 ( ± 5) C3c 11 ( ± 6)-2 ( ± 3)-87 ( ± 7) 72 ( ± 14)-4 ( ± 3)-24 ( ± 6) C3d 8 ( ± 3)-26 ( ± 5)-66 ( ± 8) 47 ( ± 7)-29 ( ± 7)-24 ( ± 3) QpLvmLsm Suite Table 1 (continued) S. Critelli Earth-Science Reviews 185 (2018) 624–648 59 50 76 76 74 67 17 ( ± 9)-0 ( ± 0)-83 ( ± 9) 18 ( ± 4)-10 ( ± 4)-72 ( ± 6) 10 ( ± 5)-23 ( ± 9)-67 ( ± 10) 10 ( ± 4)-26 ( ± 6)-64 ( ± 6) 12 ( ± 5)-15 ( ± 5)-73 ( ± 7) 3 ( ± 4)-21 ( ± 13)-76 ( ± 13) 3 ( ± 4)-16 ( ± 5)-81 ( ± 9) 3 ( ± 4)-16 ( ± 5)-81 ( ± 9) 6 ( ± 5)-17 ( ± 8)-77 ( ± 10) G2 G3 (regional Langhian-early Tortonian petrofacies (G1-to-G3) G4 G5 G6 G7 G8 (regional early Tortonian petrofacies (G5-to-G8) 629 ( ± 12)-4 ( ± 2)-74 ( ± 12) ( ± 6)-7 ( ± 3)-66 ( ± 6) ( ± 12)-0 ( ± 0)-75 ( ± 12) ( ± 20)-1 ( ± 1)-60 ( ± 20) ( ± 24)-1 ( ± 2)-69 ( ± 24) ( ± 12)-4 ( ± 2)-74 ( ± 12) ( ± 12)-3 ( ± 3)-72 ( ± 13) 24 ( ± 14)-0 ( ± 0)-76 ( ± 14) 32 ( ± 7)-0 ( ± 0)-68 ( ± 7) 28 ( ± 9)-0 ( ± 0)-72 ( ± 9) 19 ( ± 18)-0 ( ± 0)-81 ( ± 18) 2 ( ± 2)-0 ( ± 0)-98 ( ± 2) 7 ( ± 6)-4 ( ± 2)-89 ( ± 7) 26 ( ± 6)-4 ( ± 2)-70 ( ± 12) 15 ( ± 5)-15 ( ± 2)-70 ( ± 7) 22 27 25 39 30 22 25 J. Backarc extensional rifting basins (Late Miocene) 9 ( ± 4)-4 ( ± 7)-87 ( ± 9) I. Mid- Late Miocene-Pliocene Wedge-Top Basins I1 13 ( ± 13)-1 ( ± 1)-86 ( ± 13) I2 25 ( ± 13)-1 ( ± 2)-74 ( ± 13) (regionalTortonian-early Pliocene 19 ( ± 13)-1 ( ± 2)-80 ( ± 13) petrofacies (G1-G2) H. Pliocene foreland basin H1 H2 (regional early-middle Pliocene petrofacies (F1 + F2) G10 G11 G12 G13 G14 G15 (regional late Tortonian-Messinian petrofacies (E9 -to- E153) G16 G17 G18 G19 G20 G. Foreland Basin Systems: Apennines (Tortonian-Messinian) G9 9 ( ± 4)-6 ( ± 7)-85 ( ± 9) 34 ( ± 13)-0 ( ± 0)-66 ( ± 13) 28 ( ± 9)-12 ( ± 5)-60 ( ± 8) 47 ( ± 11)-24 ( ± 8)-29 ( ± 7) 5 ( ± 4)-37 ( ± 8)-58 ( ± 8) G1c ( ± 14)-5 ( ± 14)-3 ( ± 18)-0 ( ± 21)-2 ( ± 21)-1 ( ± 14)-5 ( ± 18)-3 ( ± 5)-54 ( ± 3)-51 ( ± 0)-55 ( ± 3)-68 ( ± 3)-83 ( ± 5)-54 ( ± 3)-50 ( ± 16) ( ± 14) ( ± 18) ( ± 21) ( ± 22) ( ± 16) ( ± 19) 76 ( ± 9)-2 ( ± 1)-22 ( ± 6) 62 ( ± 17)-0 ( ± 1)-38 ( ± 17) 50 ( ± 20)-1 ( ± 1)-49 ( ± 20) 56 ( ± 18)-1 ( ± 1)-43 ( ± 19) 6 ( ± 5)-0 ( ± 0)-94 ( ± 5) 6 ( ± 4)-0 ( ± 0)-94 ( ± 4) 6 ( ± 4)-0 ( ± 0)-94 ( ± 4) 4 ( ± 9)-0 ( ± 0)-96 ( ± 9) 3 ( ± 2)-0 ( ± 0)-97 ( ± 3) 27 ( ± 9)-2 ( ± 1)-71 ( ± 9) 55 ( ± 14)-4 ( ± 4)-41 ( ± 14) 28 ( ± 6)-15 ( ± 2)-57 ( ± 12) 41 46 45 30 16 41 37 41 ( ± 14)-5 ( ± 5)-54 ( ± 16) ( ± 7)-15 ( ± 6)-26 ( ± 6) ( ± 12)-17 ( ± 6)-33 ( ± 12) ( ± 15)-22 ( ± 13)-2 ( ± 5) ( ± 15)-14 ( ± 6)-10 ( ± 9) ( ± 15)-14 ( ± 6)-12 ( ± 9) ( ± 15)-18 ( ± 7)-15 ( ± 9) 59 ( ± 11)-38 ( ± 8)-3 ( ± 5) 59 ( ± 11)-38 ( ± 8)-3 ( ± 5) 5 ( ± 4)-37 ( ± 8)-58 ( ± 8) G1b LmLvLs QpLvmLsm Suite Table 1 (continued) ( ± 4)-35 ( ± 7)-50 ( ± 8) ( ± 9)-23 ( ± 7)-34 ( ± 7) ( ± 7)-2 ( ± 2)-34 ( ± 7) ( ± 9)-4 ( ± 7)-35 ( ± 11) ( ± 9)-7 ( ± 7)-32 ( ± 11) ( ± 8)-10 ( ± 6)-34 ( ± 9) ( ± 7)-13 ( ± 8)-33 ( ± 8) ( ± 6)-28 ( ± 12)-54 ( ± 11) ( ± 8)-39 ( ± 16)-49 ( ± 17) ( ± 10)-13 ( ± 7)-33 ( ± 10) ( ± 10)-46 ( ± 9)-12 ( ± 4) ( ± 7)-13 ( ± 8)-33 ( ± 8) ( ± 10)-25 ( ± 9)-34 ( ± 11) 72 ( ± 7)-2 ( ± 2)-26 ( ± 7) 26 ( ± 11)-18 ( ± 12)-56 ( ± 13) 27 ( ± 17)-23 ( ± 15)-50 ( ± 15) 27 ( ± 13)-21 ( ± 12)-52 ( ± 13) 44 ( ± 14)-39 ( ± 13)-17 ( ± 8) 41 ( ± 8)-43 ( ± 7)-16 ( ± 7) 42 ( ± 8)-41 ( ± 9)-17 ( ± 7) 29 ( ± 34)-65 ( ± 34)-6 ( ± 3) 2 ( ± 2)-92 ( ± 7)-6 ( ± 4) 8 ( ± 2)-55 ( ± 14)-37 ( ± 13) 8 ( ± 10)-10 ( ± 5)-82 ( ± 12) – 54 18 12 54 42 54 41 54 ( ± 16)-20 ( ± 9)-26 ( ± 12) 15 43 64 61 61 56 26 ( ± 13)-38 ( ± 16)-35 ( ± 13) 42 ( ± 5)-44 ( ± 7)-14 ( ± 7) 37 ( ± 8)-18 ( ± 6)-45 ( ± 10) 54 ( ± 10)-3 ( ± 2)-43 ( ± 10) 54 ( ± 10)-3 ( ± 2)-43 ( ± 10) RgRsRm and and and and and Le Pera, 1995a, 1998 Loiacono, 1988; Critelli and Le Pera, 1994 Le Pera, 1990b, 1994 Le Pera, 1995a, 1998 Le Pera, 1995a, 1998 Critelli and Le Pera, 1995a, Caracciolo et al., 2012; unpublished data Barone et al., 2008; and unpublished data Barone et al., 2008 Matano et al., 2014 Matano et al., 2014; and unpublished data Barone et al., 2006 Critelli et al., 2007 Critelli et al., 2007 Corda and Morelli, 1996; Stalder et al., 2018 Chiocchini and Cipriani, 1992 Critelli and Le Pera, 1995a, 1995b; and unpublished data Critelli and Le Pera, 1995a, 1995b; Critelli et al., 2007 Matano et al., 2014; and unpublished data Matano et al., 2014 Barone et al., 2006 unpublished data Critelli Critelli Critelli Critelli Critelli Critelli, 1987; Critelli and Le Pera, 1994, Critelli and Le Pera, 1995a, 1995b De Rosa and Gallo, 1982; Critelli and Le Pera, 1995a, 1998 Barone et al., 2006 Critelli and Le Pera, 1995a, 1998 Reference S. Critelli Earth-Science Reviews 185 (2018) 624–648 Earth-Science Reviews 185 (2018) 624–648 S. Critelli Fig. 2. Geological sketch map of the Circum-Mediterranean orogenic belts (after Critelli et al., 2008, 2017) and location of the studied area. Maghrebian Chain includes the Rif Chain in Morocco, the Tell Chain in Algeria, and the Sicilian Maghrebian in Sicily. the Internal units of the Betic Cordillera, the Calabrian terranes (Amodio Morelli et al., 1976; Scandone, 1982; Bonardi et al., 2001), the Rif and Tell Chains, including ophiolites, crystalline basement rocks and Mesozoic to Tertiary sedimentary sequences; (2) The western Tethys oceanic realm, including obducted Mesozoic ophiolite-bearing terranes, that are extended in the western and northern portions of the circum-Mediterranean region, and include the Nevado-Filabride unit of the Betic Cordillera, the Ligurian-Piedmont units of the Alps, Corsica and northern side of Apennines, and the ophiolitic units of northern Calabria; (3) The eastern oceanic realm, including the Lucanian Oceanic terranes, having ophiolitic blocks, metasedimentary and sedimentary rocks, and the Maghrebian Flysch units of northern Africa and Sicily; (4) The external domain, including the (i) inner carbonate platform having Mesozoic to lower Miocene shallow-water carbonate strata, (ii) deep-marine pelagic basins, having Mesozoic to lower Miocene pelagic deep-sea sequences (i.e. the Lagonegro Basin in southern Apennines), (iii) Mesozoic to Quaternary carbonate outer platform (i.e. Apulia Unit) and low-land or cratonic regions (i.e. African and Iberian continental margins) (Critelli et al., 2011, 2017 and references therein) (Fig. 2). In the southern and eastern oceanic realm, the Paleogene (Eocene to early Oligocene) tectonic phase corresponds with the subduction of the oceanic lithosphere beneath the Mesomediterranean microplate and African plate. This tectonic stage is responsible for the initial flexure and the onset of consequent general erosional processes of the African and Adria continental margins. The Paleogene tectonic phase caused regional metamorphism at around 38 Ma (e.g. Steck and Hunziker, 1994) and intra-orogenic magmatism along the Periadriatic zone. The middle-late Oligocene (32–30 Ma) is characterized by intense magmatic activity, part of which is directly linked to the Algero-Provencal rift (Provence and Sardinia), part along the Insubric line and part along the periadriatic domain. In the Alps and northern Apennines, the Eocene and Oligocene siliciclastic sedimentary sequences record provenance from the (a) Iberian plate (Corsica-Sardinia-Brianconnais), (b) Adria plate (austroalpine domain), (c) European plate, (d) syneruptive magmatic activity, and from (e) both European and Adria forebulges. Final closure of the eastern and southern Tethys oceanic realm is marked by accretionary processes of the Mesomediterranean microplate (represented by the internal domains of the circum-Mediterranean orogenic belt; Fig. 2) over the deformed oceanic terranes and the African, Iberian and Adria continental margins. Since early Miocene, huge volumes of clastic sedimentary sequences, dominantly deep-marine turbidite systems, were deposited at the front of the accretionary orogenic detrital modes are then reported as Qt%-F%-L% and Qm%-F%-Lt%. Description of sandstone petrofacies includes values of QtFL% and QmFLt%. General descriptions of changing nature of detrital budget in terms of calculations of both phaneritic and aphanitic rock/lithic fragments as values of Rg (plutonic) Rs (sedimentary) Rm (metamorphic) are also included in the petrofacies definition. The available data include modal point counts for huge amounts of rock samples. Attention here is restricted to sandstone suites of key areas of the circum-Mediterranean belt, including Betic Cordillera (Spain), Rif Chain (Morocco), Sicilian belt and Apennines (Italy) where data are useful with comparable methodology to define overall compositional trends. Because of the large occurrence of Mesozoic to Tertiary carbonate systems, both from large shallow-marine carbonate platform systems and deep-marine pelagic systems, in the paleogeographic fragmentation of the continental margins, notable compositional signatures of the circum-Mediterranean sandstone suites are provenance from carbonates, both coeval and noncoeval, and extrabasinal and intrabasinal, representing key detrital signals during tectonic evolution of sedimentary basins (e.g. Zuffa, 1980, 1985, 1987; Fontana, 1991; Critelli et al., 2007). Here, coeval carbonate grains, as such as other coeval grain types (i.e. glauconite, etc.) are not included in recalculated grain parameters and in typical triangular diagrams, while extrabasinal carbonate grains (ancient carbonate lithic fragments) are included in recalculated grain parameters and related diagrams. Only exception, in recalculations and related diagrams, of including coeval grains are neovolcanic particles related to active magmatic activity in the source areas. 3. Geodynamic setting and time frame The study area contains rocks affected by numerous geodynamic events that occurred between Paleozoic orogenies and the present time. Apart the Paleozoic history of exposed terranes, the key geodynamic events within the circum-Mediterranean orogens occurred after breakup of Pangea. In this paper we focus on the Mesozoic to Cenozoic history of clastic sedimentary sequences using sandstone strata to decipher the close relations between regional provenance and paleotectonics. Circum-Mediterranean mountain belts, from the Betic Cordillera to the Northern Apennines and from the northern Africa (Rif and Tell chains) to Calabria are subdivided into the following morphotectonic domains (e.g. Perrone et al., 2006; Critelli et al., 2008, 2011, 2017; Bonardi et al., 2009) (Fig. 2): (1) The internal domain, represented by 630 Earth-Science Reviews 185 (2018) 624–648 S. Critelli Fig. 3. Chart identifying time slices for which paleotectonic maps are constructed with accompanying QFL diagram. Time scale after Harland et al. (1989). The following brief statements define the seven time slice stratigraphically related to major events (Fig. 3). terranes in diverse foreland basin systems all along the various tracts of the circum-Mediterranean belt. Fragmentation of the Mesomediterranean microplate occurred during two main rifting stages within the western Mediterranean, the late Oligocene-earliest Miocene AlgeroProvencal-Balearic rifting basin, and the mid-late Miocene and Pliocene Tyrrhenian Sea rifting basin (e.g. Malinverno and Ryan, 1986; Dewey et al., 1989; Doglioni, 1991; Doglioni et al., 1996). Sandstone detrital modes are discussed in conjunction with paleotectonic maps to indicate their relationships to key geological events. 1. Mid-Late Triassic (230 Ma); Terrestrial Rift-valley stage after breakup of Pangea and onset of the Tethyan taphrogenesis; This phase corresponds with deposition of continental redbeds suite (mainly Pseudoverrucano unit; A1-to-A4 suites in Table 1). 2. Early Cretaceous-Earliest Paleogene (110–60 Ma); Early Cretaceous (110) sea-floor spreading of the Tethyan realms, and deposition of 631 Earth-Science Reviews 185 (2018) 624–648 S. Critelli 3. 4. 5. 6. and bibliography therein for major details). The continental redbeds represent the oldest strata of successions with a similar tectono-sedimentary evolution from the Middle Triassic to compressional deformation, and they represent the onset of Mesozoic sedimentation during the rift-valley stage (Fig. 4). Middle Triassic–Lower Jurassic continental redbeds (in the internal domains of the Betic, Maghrebian, and Apenninic chains) can be considered a regional lithosome marking the Triassic-Jurassic rift-valley stage of Tethyan rifting. Sandstones are quartzose to quartzolithic and represent a provenance of continental block and recycled orogen (Fig. 4), made up mainly of Paleozoic metasedimentary rocks similar to those underlying the redbeds.The close similarity in composition, sedimentology, and diagenetic evolution of the redbeds in different sectors of the circum-Mediterranean orogens suggests deposition in a distinctive Mesozoic belt (Pseudoverrucano Subdomain; Perrone et al., 2006; Critelli et al., 2008, 2018). The redbeds were deposited on a block of Variscan continental crust. This block had a central erosional mountain area that provided terrigenous sediments to surrounding intracontinental rift basins. After having been deeply eroded during the Triassic, the mountain areas were transformed to a peneplaned area of low relief, whereas the former continental basins evolved to neritic carbonate basins after the start of the Early Jurassic. The Triassic Pseudoverrucano-Verrucano Domains were surrounded by the German-Andalusian facies, now cropping out in the Iberian and African plates, whereas eastward it opened toward Tethyan marine domains (Fig. 4). quartzose turbidite sandstones in the southern and eastern Tethyan ocenic realm (B2-to-B4 suites in Table 1), and Late Cretaceous-earliest Paleogene (60 Ma) closure of the western Tethyan realm, and deposition of quartzofeldspathic and quartzolithic turbidite sandstone suites (C1 suite in Table 1; Ostia Sandstone, Mt. Caio, Mt. Cassio, Casanova Sandstone, Sillano and Pietraforte formations; Valloni and Zuffa, 1984). Late Oligocene to earliest Miocene (30–22 Ma); Closure of the southern and eastern Tethyan oceanic realm, and onset of continental accretionary processes involved the internal domains of the Mesomediterranean crustal block; eastern Tethyan realm experienced subduction processes, onset of calcalkaline magmatic arc, and accomodation of quartzolithic and volcanolithic sandstone suites (C2a-to-C3j in Table 1) in the remnant ocean basin, and quartzofeldspathic sandstone suites (C4a-to-C4f in Table 1) in the subsiding areas of the overplate (forearc region within the Mesomediterranean microplate). Langhian to early Tortonian; 15–10 Ma); growing of the circumMediterranean orogenic belt and onset of deep-marine foreland basin systems, particularly in the Apennines belt. Flexure of the northern Africa continental margin generating huge volumes of cratonic-derived turbidite sandstones (Numidian Sandstone and other suites; D1-to-D10 in Table 1). Late Tortonian to early Pliocene (8–5 Ma), increasing eastward displacement of the Mesomediterranean microplate involving in deformation large portions of the Adria continental margin. Onset of the Tyrrhenian Sea rifting processes, and eastward displacement of the southern Apennines foreland basin system. Late Messinian-Pliocene; partially a detail of the previous time slice, increasing uplift and deep erosion of the Mesomediterranean microplate and the Alps, to the west and southwest and to the north, respectively; abrupt increasing of the rifting of the Tyrrhenian Sea. 4.2. Map 2. Neotethyan proto-oceanic rift-trough sandstone suites (Mesozoic) The continental redbeds pass upward to Middle Jurassic transitional shallow-marine and deep-marine mainly carbonate sequences, including quartzose sandstone turbidite systems (i.e. the Longobucco Group; Zuffa et al., 1980; Santantonio and Teale, 1987) that represent the following proto-oceanic stage during opening of the western Tethys Ocean (Perrone et al., 2006; Critelli et al., 2008; Fig. 5). Sedimentary cover of the Tethyan oceanic crust includes Upper Jurassic mudrocks, pelagic carbonate strata, argillaceous chert, isolated quartzose turbidite strata (Critelli, 1993), radiolarian chert, and Lower Cretaceous pelagic limestone, marl, claystone and quartzose sandstone. Quartzose turbidite sandstone are widespread in the oceanic realm (e.g. Critelli, 1993; Barbera et al., 2011 and bibliography therein) testifying lowland regions with no evident abrupt uplifted continental block signals. Quartzose detrital supply is uncertain in terms of provenance, it can be derived from African continental margin or the lowland relief of the Mesomediterranean microplate (e.g. Perrone et al., 2006; Critelli et al., 2008). Although there are still conflicting ideas about whether the westernmost branch of the Neotethys opened as a single ocean (Schmid et al., 2008; Schettino and Turco, 2011), or was divided into northern and southern branches (Stampfli et al., 2002), much evidence suggests two distinctive ocean basins having different time of closure, the northern and western Nevado-Filabride, Ligurian-Piedmont oceanic realm, and the southern and eastern Maghrebian, Lucanian, Ionian oceanic realm that remain an active oceanic branch during Paleogene. 4. Paleogeography and Paleotectonics and related key detrital modes At regional scale, the key clastic stratigraphic units that are discussed here comprise (a) the Late Triassic-Early Jurassic continental redbeds that mark the fragmentation of Pangea identifying distintive continental margins and representing the terrestrial rift-valley sequences of the Tethyan rifting, following by Jurassic shallow-to-deepmarine sequences, including sandstone turbidites interbedded with carbonates and pelagic mudrocks; (b) the Late Jurassic to Early Cretaceous sandstones of the Tethyan Ocean realm; (c) the Paleogene clastic strata of the final closure of the eastern-southern Tethyan oceanic realm, including the Paleogene subduction complex (accretionary wedge) of the Lucanian oceanic terranes, and the early Miocene clastics of the forearc region; (d) the Paleogene sandstone units of the African and Iberian continental margins; (e) the Miocene sandstone clastic wedges representing the key foreland basin systems of the Betic Cordillera, the northern Africa orogen (Rif and Tell), and the Apennines (Fig. 2). Further details and descriptions are in the discussion of the paleotectonic maps in this section. 4.1. Map 1. Terrestrial rift-valley sequences 4.2.1. Western Tethyan realm Over the ophiolitic gabbros (166 to 163 Ma; Bill et al., 2001) in diverse portions of occurrence of ophiolitic suites of Alps, Betic Cordillera, Corsica and Apennines, sedimentary sequences include siliceous shale, radiolarian chert, calcareous ooze, marl and shale, and Calpionella Limestone Formation (late Tithonian to Valanginian; Bill et al., 2001 and references therein). Occurrence of clastic strata during rifting and the sea-floor spreading of the western Tethyan realm is minor; few sandstone turbidites are interbedded with Late Jurassic-Early Cretaceous pelagic sequences and sandstones are quartz-rich; its occurrence is on the sedimentary cover of ophiolitiferous suites in Calabria (Frido First evidences of nascent rift-valley sequences are represented by widespread occurrence of Triassic to earliest Jurassic continental redbeds lying over Paleozoic metasedimentary and locally (Calabrian terranes) plutonic rocks in the Betics (Perri et al., 2013), Rif and Tell (Zaghloul et al., 2010), Calabrian terranes and Tuscany (e.g. Perrone et al., 2006; Critelli et al., 2008, 2018; Perri et al., 2008, 2011). These continental redbeds are fluvial strata of conglomerate, sandstone and mudrock mostly reddish-purple in color and formally are named “Verrucano” and “Pseudoverrucano” in the Italian stratigraphic record, and Saladilla Formation in the Betic Cordillera (e.g. Perrone et al., 2006 632 Earth-Science Reviews 185 (2018) 624–648 S. Critelli Fig. 4. Paleotectonic map 1 for the Middle Triassic time, showing the Middle Triassic–Lower Liassic continental redbeds (in the internal domains of the Betic, Maghrebian, and Apenninic chains). The redbeds can be considered a regional lithosome marking the Triassic-Jurassic rift-valley stage of Tethyan rifting, which led to the Pangaea breakup and subsequent development of a mosaic of plates and microplates. Note that conventionally, the Apulia microplate is referred to the Mesozoic paleogeography and paleotectonics, while, during Tertiary it is called Adria microplate (see Channel et al., 1979). Sandstone suites related to the Map 1 with QtFL and QpLvmLsm diagrams (main provenance fields in QtFL are those of Dickinson et al., 1983; Dickinson, 1985) of the redbeds (Pseudoverrucano lithosome) sandstone suite. Oceanic belt (Bouillin et al., 1986) through related terrains in southern Apennines, which have been interpreted as deposited in an oceanic belt (Lucanian Ocean) representing the northeastward extension of the Maghrebian Flysch Basin (Bonardi et al., 2001; de Capoa et al., 2003; Guerrera et al., 2005; Perrone et al., 2014). Sandstone suites of the southern and eastern oceanic branch are exclusively quartzose in composition (Qt90–98 F2–9 L0–3) (Table 1; Fig. 5). Proto-Oceanic rifttroughs include diverse well-preserved stratigraphic sequences all along the circum-Mediterranean orogen. The Jurassic slope to deep-marine sequence of the Longobucco Group (Fosso Petrone and Trionto Formations; Zuffa et al., 1980; Santantonio and Teale, 1987; Santantonio et al., 2016) include about 1000 m thick strata of sandstone and shale interbedded with pelagic limestones and olistostroma. Turbidite sandstones are quartzarenite and sublitharenite (Zuffa et al., 1980) lying over shallow-marine carbonate and sandstone (Bocchigliero Formation) and continental redbeds (Torrente Duno Formation). Other correlated Mesozoic continental-margin sequences are more pelagic with few sandstone strata having quartzarenite to quartzolithic compositions. The Upper Jurassic-to-Cretaceous turbidite sandstones within the ocean floor of the eastern Tethyan realm are quartzose sandstones in the Lucanian Oceanic terranes (i.e., Frido-Crete Nere formations; Qm89 ± 4 F9 ± 4 Lt2 ± 1; Critelli, 1993), in few sandstone strata of the Sicilide Complex and the Sicilian Monte Soro Unit (Qm91 ± 4 F4 ± 1 Lt5 ± 3; Barbera et al., 2011). The eastern and southern Tethyan realm includes the Maghrebian Flysch Basin of northern Africa. The most typical and widest outcropping Massylian flysch beds are constituted by the Aptian–Albian Flysch of the Chouamat Nappe, a thick succession of Aptian–Albian pelites (locally marly) and mediumto fine-grained siliciclastic turbidite sandstones upwards. The succession is 150–250 m thick and starts with bluish marls and mudstones up Unit; Bonardi et al., 1988; Critelli, 1993), and in the Palombini Shale Formation of northern Apennines. Sandstones are more abundant since Late Cretaceous, and composition change to be quartzolithic and quartzofeldspathic, during stages of closure of the western Tethyan realm (e.g. Valloni and Zuffa, 1984; Cavazza et al., 2018). 4.2.2. Eastern Tethyan realm Rifted continental-margin sequences of Longobucco Group (earlyMiddle Jurassic), Jurassic-to-Cretaceous quartzose turbidites of the Lucanian Ocean Complex (Crete Nere and Frido Units), Cretaceous-toEarly Tertiary Monte Soro Unit, and the Lower Cretaceous Maghrebian Flysch Basin, are the main well-exposed sedimentary sequences having sandstone suites of the Eastern Tethyan oceanic branch and its continental margin. In the western Mediterranean, the Maghrebian Flysch Nappes are mainly made of pelagic fine grained sediments and of carbonatoclastic and siliciclastic turbidites spanning since the Middle-Late Jurassic (Durand-Delga, 1980; Suter, 1980; Wildi, 1983; de Capoa et al., 2007, 2013; Zaghloul et al., 2007). The sedimentary successions of these Flysch Nappes were deposited in a very deep marine basin known as Maghrebian Flysch Basin. These terrains extend over more than 2000 km from the western Betic Cordillera through the Rif Chain to the eastern Sicilian Maghrebides and up southern and northern Appenines (Guerrera et al., 2005; de Capoa et al., 2013; Perrone et al., 2014). The Maghrebian Flysch Basin has been considered as a southern branch of the western Tethys, separated by means of a Mesomediterranean microplate from the Nevado–Filabride–Ligurian-Piedmont western and northern branch (Guerrera et al., 1993, 2005, 2012; Bonardi et al., 2001; Chalouan et al., 2001; Chalouan and Michard, 2004; Belayouni et al., 2012). Other authors, however, interpreted this basin as a single extension toward the west of the Piedmont–Ligurian 633 Earth-Science Reviews 185 (2018) 624–648 S. Critelli evolves to Upper Cretaceous claystones and marls with siliceous black shales and black radiolarites, sandstones, pelites and marly limestones, followed by Paleocene–Oligocene marls, breccias and nummuliticbearing limestones. The sequence is topped by Aquitanian–Burdigalian Numidian sandstone suites that marks the deformation and accretion of oceanic terranes and the onset of collisional events (Wildi, 1983; Gübeli et al., 1984; Durand-Delga and Olivier, 1988; Thomas et al., 2010). 4.3. Late cretaceous closure of western Tethys The western realm of the Tethys Ocean is known to be progressively closed during Late Cretaceous to earliest Paleogene. Numerous deepmarine turbidite formations of northern Apennines (Ostia, Sillano, Pietraforte, Casanova, Cassio and Caio formations) and Corsica testify the progressive closure of the western Tethyan oceanic realm, (e.g. Valloni and Zuffa, 1984; Cavazza et al., 2018). Sandstones are quartzolithic in the Late Cretaceous formations that pass to quartzofeldspathic and quartzo-feldspatholithic sandstones during the Late Cretaceous-Paleogene (Valloni and Zuffa, 1984; Cavazza et al., 2018). 4.4. Map 3. Late Paleogene-earliest Miocene closure of eastern and southern Tethys The eastern Tethyan oceanic area (Maghrebian and Lucanian basins) experienced deformation and accretion, involving in a remnant ocean basin (Fig. 6). A tectonic mélange (Liguride Complex of Ogniben, 1969; or Northern-Calabrian Unit; Critelli, 1993, 1999) was formed in this time frame, including olistholiths and broken formations of oceanic sequences and crystalline rocks (Critelli, 1993). The subduction of the eastern Tethyan oceanic lithosphere beneath the Mesomediterranean microplate, generates a continental-margin calcalkaline volcanic arc in Sardinia (e.g. Scandone, 1982; Assorgia et al., 1986; Malinverno and Ryan, 1986; Channell and Mareschal, 1989; Dewey et al., 1989) and the progressive closure of the Lucanian and Maghrebian oceanic realm. At its top, the tectonic mélange includes a Late Paleogene (upper Eocene to upper Oligocene) quartzolithic, quartzofeldspathic and volcanolithic sandstone strata (Fig. 6) tectonically assembled within the tectonic mélange (Northern-Calabrian Unit; Critelli, 1993; Critelli et al., 2017). In the Maghrebian basin, the Cretaceous and Paleogene pelagic sequences are capped, during the early Miocene, by a series of turbidite sandstone systems that have been subdivided in several lithostratigraphic formations. These latter successions occur from eastern to western, in the (i) southern Apennines and Sicily, and include the Corleto, Albanella, Colle Cappella, Tufiti di Tusa, Poggio Maria, Reitano, Piedimonte formations; (ii) northern Africa, and include the Beni Ider, Fnideq and Sidi Abdesslam formations, and (iii) southern Spain and Betic Cordillera, and include Algeciras, Viñuela and Ciudad Granada formations. Along the accreted Mesomediterranean microplate, the subduction of the eastern oceanic realm, generated a series of subsiding depocenters in which are accumulated hundred meters of clastic sedimentary sequences. The Stilo-Capo d'Orlando, Paludi and Frazzanò formations are the key sandstone suites that are accumulated over the Calabrian accretionary wedge in the forearc region. Fig. 5. Paleotectonic map 2 for the Early Cretaceous to earliest Paleogene time, showing the northern and western Tethyan realm, and the southern and eastern Tethyan realm, during the Late Jurassic-Early Cretaceous sea-floor spreading, and location of plate mosaic in the western Mediterranean. Northern and western Tethyan realm (Nevado-filabrie, Ligurian-Piedmont basins) was progressively closed since Late Cretaceous to earliest Paleogene (boundary of subduction plane is marked) due to convergence between Adria-Europe and Iberia-Mesomediterranean plates (after Critelli et al., 2011, modified). Sandstone suites are plotted in the map and mark two main regional suites, a quartzose sandstone suite to the south, in the southern and eastern Tethyan realm, and a quartzofeldspathic and minor quartzolithic sandstone suite in the western and northern Tethyan realm. Data set of these sandstone suites are listed in Table 1 (including references). 4.5. Lucanian Remnant ocean basin 4.5.1. Quartzofeldspathic petrofacies During Paleogene to early Miocene, the internal domain of the Calabrian terranes was partially covered by synorogenic clastic wedges, including deep-marine turbidite sandstones and conglomerates. Clastic units include the Upper Oligocene to lower Miocene Frazzanò Formation (de Capoa et al., 2000) and the Stilo-Capo d'Orlando Formation, in the southern sector of the Calabrian terranes, and the upper Oligocene to lower Miocene Paludi Formation (northern sector) (Table 1). These sandstones are quartzofeldspathic (mean of the Paludi to 60 m thick, overlain by thick bedded quartzarenite stratasets usually amalgamated (El Talibi et al., 2014). Sandstone are quartzarenite (Qm94 ± 7 F2 ± 1 Lt4 ± 2; El Talibi et al., 2014). The succession 634 Earth-Science Reviews 185 (2018) 624–648 S. Critelli Fig. 6. Paleotectonic map 3 for the late Oligocene-early Miocene time, showing closure of the eastern and southern Tethyan oceanic realm, and locations of the Mesomediterranean microplate, the Sardinia/Periadriatic magmatic arc, and major deep-sea fan. During earliest Miocene, the western portions of the Mesomediterranean microplate overthrust on the southern Iberian margin forming the Betic Cordillera and its related foreland basin system. Adapted after various sources including de Capoa et al. (2002), Critelli et al. (2011, 2017), Amendola et al. (2016), Guerrera and Martín-Martín (2014) and Perri et al. (2017). Sandstone suites related to the Map 3 with QtFL diagram include quartzolithic and volcanolithic sandstone suites filling the eastern (Lucanian) and southern (Maghrebian) Tethyan realm, and quartzofeldspathic sandstone suites in related forearc region. Critelli, 1993), Albanella, Corleto and Colle Cappella Formations (Q61 F17 L22; Sicilide Complex, Auct.; e.g. Critelli et al., 1994, 2011, 2013; Fornelli and Piccarreta, 1997; Critelli and Le Pera, 1995a, 1998; Table 1). The quartzolithic petrofacies is interbedded with mixtures of siliciclastic and carbonatoclastic strata. Metamorphiclastic quartzolithic sandstones occur also in the lower portions of the Tufiti di Tusa Formation (Q46 F18 L36), below the volcaniclastic strata (Critelli et al., 1990b) and characterize all the thickness of the Corleto, Colle Cappella and Albanella formations (Critelli et al., 1994; Fornelli and Piccarreta, 1997). They are derived from low to middle grade metasedimentary terranes, and are partly derived also from ophiolitic rocks (Fornelli and Piccarreta, 1997). Interbedded thick carbonatoclastic (calcarenitemarl) strata within the Tufiti di Tusa, Albanella and Corleto Formations, testify a provenance from the forebulge area. These sandstones reflect a provenance evolution from sedimentary-dominant (both Formation, Q55 F36 L9; Zuffa and De Rosa, 1978; mean of the StiloCapo d'Orlando Formation, Q45 F49 L6; Puglisi, 1987; Cavazza, 1989; Nigro and Puglisi, 1993; Critelli et al., 1995) and reflect their local provenance from crystalline rocks of the Calabrian terranes. The tectonic setting of these basins is complex; the sequences suturing some crystalline thrust units could represent a wedge-top deposition on advancing calabrian thrust-belt (e.g. Weltje, 1992; Patacca et al., 1993; Wallis et al., 1993) or may represent deposition in a forearc setting (e.g. Cavazza et al., 1997; Cavazza and Ingersoll, 2005). 4.5.2. Quartzolithic petrofacies The early Miocene quartzolithic petrofacies widely occurs at the final basin-fill stage of the remnant Lucanian Ocean. The quartzolithic sandstone suites occur in the siliciclastic deep-sea turbidite systems of the Saraceno Formation (Q52 F10 L38; Liguride Complex, Auct.; 635 Earth-Science Reviews 185 (2018) 624–648 S. Critelli carbonate and siliciclastic fragments) detritus to low-grade metamorphic and sedimentary mixtures. The provenance evolution testifies the initial signal of accretion and unroofing of the frontal thrust system of the northern Calabrian terranes (Sila Unit; e.g. Messina et al., 1994; Critelli and Le Pera, 1998). metamorphic sources, and minor extrabasinal carbonate grains and volcanic detritus. Source regions for the quartzolithic sandstone petrofacies are from exhumed and uplifted Paleozoic metasedimentary terranes widely exposed in the internal domains of the circum-Mediterranean belt (i.e. Malaguide, Ghomaride and Sila Unit). 4.5.3. Volcaniclastic petrofacies Syneruptive volcanolithic sandstones having a late Oligocene age (Q16 F24 L60; Critelli, 1993), having basaltic and andesitic fragments, reflect climax of activity of the Sardinia volcanic arc during its initial volcanism (late Oligocene, 32–30 Ma; Critelli, 1993). Huge volumes of volcanolithic turbidite sandstones occur in the Tufiti di Tusa Formation (up to 300 m in thickness), early Miocene in age, at the top of the Sicilide Complex. Volcanolithic strata of the Tufiti di Tusa (Q14 F28 L58) include syneruptive (e.g. Critelli and Ingersoll, 1995; Marsaglia et al., 2016) sandstones, recording climax of volcanic activity of the calcalkaline magmatic arc (Critelli et al., 1990b; Fornelli and Piccarreta, 1997; Perri et al., 2012a). The volcanic detritus includes abundant microlitic to felsitic seriate volcanic texture testifing an andesite and basaltic andesite composition of the volcanic debris (Critelli et al., 1990b; Perri et al., 2012a). The turbidites consist of reworked ash-falls that contain abundant grains characterized by vitric textures, glass shards and single neovolcanic minerals of hornblende, pyroxene and euhedral plagioclase. Mixing provenance from the active volcanic source and the crystalline sources of the Calabrian terranes are interbedded to the top of the Sicilide complex, forming distinct early Miocene siliciclastic turbidite systems having sand compositions ranging from volcanolithic (Tufiti di Tusa Formation; Critelli et al., 1990b; Perri et al., 2012a; Puglisi, 2014) to quartzolithic (Albanella, Corleto and Colle Cappella Formations) (Critelli et al., 1994; Fornelli and Piccarreta, 1997; Critelli and Le Pera, 1998; Perri et al., 2012a). Other early Miocene volcaniclastic strata are interbedded with quartzose sandstone strata and shallow-water carbonates along the carbonate platform sequences of the Adria margins (e.g. Perrone, 1987) and the deep-sea Lagonegro basin (Pieri and Rapisardi, 1973; Pescatore et al., 1988; Critelli, 1991, 1999; Patacca et al., 1992). 4.6.2. Volcanolithic sandstone petrofacies The volcanolithic sandstones (Qt14 ± 6 F28 ± 15 L58 ± 13; C3e in Table 1) are mostly confined in the Tufiti di Tusa Formation of the Sicilian Maghrebian and the southern Apennines, and the Bisciaro Formation in the northern Apennines, and detritus is dominantly derived from coeval andesitic volcanism. The source area for the volcanolithic sandstone petrofacies is suggested from the active volcanic region exposed in western Sardinia (e.g. Critelli et al., 2011, 2013, 2017). 4.7. Forearc region (Late Oligocene-earliest Miocene) The forearc region of the eastern Tethys subduction is inferred to be located over the Mesomediterranean microplate located between the active magmatic arc (Sardinia) to the west, and the subduction complex (Lucanian Ocean), to the east. 4.7.1. Quartzofeldspathic sandstone petrofacies Over the Paleozoic-Mesozoic block of the Calabrian terranes unconformably overly the siliciclastic strata of the early Miocene StiloCapo d'Orlando, Paludi and Frazzanò formations. These three clastic sequences have dominantly turbidite sandstone strata that have a general quartzofeldspathic composition (Qt55 F36 L9), reflecting close provenances from the Paleozoic plutonic and metamorphic rocks of the Calabrian terranes (i.e. Aspromonte, Stilo and Sila units; Cavazza and Ingersoll, 2005). 4.7.2. Quartzolithic sandstone petrofacies Over and at the front of the Mesomediterranean microplate, other clastic units include the Ciudad Granada Formation in the Betic Cordillera and the Fnideq Formation in the Rif Chain (e.g. Puglisi et al., 2001; Martín-Algarra et al., 2000). These sandstone units differ in composition with respect the quartzofeldspathic sandstones of the StiloCapo d'Orlando, Paludi and Frazzanò formations, and they mark a quartzolithic sandstone suite, more quartzose for the Fnideq Formation of northern Rif Chain (Qt81 ± 6 F7 ± 4 L12 ± 6), and more lithic for the Ciudad Granada Formation (Qt41 ± 7 F4 ± 5 L55 ± 8). The Fnideq sandstones have abundant low-grade metamorphic detritus closely related to a provenance from the Ghomaride and Malaguide units of the Rif and Betic chains, while the Ciudad Granada Formation includes also clasts in conglomerate strata interbedded with sandstones of high-grade metamorphic and plutonic rocks that have been inferred to derive from units that are exposed nowday in the Calabrian terranes (i.e. Aspromonte and Stilo units; see Martín-Algarra et al., 2000 for furter details). 4.6. Maghrebian Basin The Maghrebian basin includes a late Cretaceous to earliest Miocene pelagic successions of varicoloured mudstones, including marl, limestone and claystone, and since earliest Miocene (Aquitanian to Burdigalian) by several deep-marine siliciclastic turbidite systems that have been subdivided into several lithostratigraphic units. The arrival of siliciclastic turbidite systems, within the Maghrebian Basin, indicates the closure of the oceanic realm and the accretionary processes of the internal domains (Mesomediterranean microplate) overthrusting over the Adria, African and Iberian continental margins. From western to eastern these siliciclastic units include (Table 1): (i) the Viñuela and Algeciras formations in the Betic Cordillera, (ii) the Sidi Abdesslam and Beni Ider formations (Puglisi et al., 2001; Zaghloul et al., 2002; Puglisi, 2008), in the Rif Chain, (iii) the Reitano, Tufiti di Tusa, Troina sandstone, Poggio Maria, Frazzanò formations in Sicily (de Capoa et al., 2002; Puglisi, 2008, 2014), and (iv) the Corleto Perticara, Albanella, Colle Cappella and Tufiti di Tusa formations in southern Apennines (Critelli et al., 1990b; Critelli et al., 1994; Critelli and Le Pera, 1995a, 1998; Fornelli and Piccarreta, 1997). 4.8. Betic cordillera Foreland Basin system The thrust tectonics and the alpine metamorphism of the Betic terranes is in response of continental collision (Guerrera and MartínMartín, 2014) of the Mesomediterranean microplate with the South Iberian continental margin involving the Nevado-Filabride oceanic branch (subducted below the Mesomediterranean microplate) (e.g., Perrone et al., 2006; Critelli et al., 2008; Perri et al., 2013, 2017). The Malaguide and Alpujarride complexes were related to the Kabylian and Calabrian Internal units, and all of them constituted the southern part of the Mesomediterranean microplate (Martín-Martín et al., 2006) to the N of the Maghrebian Basin (e.g., Bouillin, 1986; Guerrera et al., 4.6.1. Quartzolithic sandstone petrofacies Sandstone suites of the Maghrebian sedimentary units include dominantly quartzolithic sandstone petrofacies (Qt58 ± 12 F15 ± 9 L27 ± 13; this mean and standard deviation is a regional scale from C3a to C3j excluding C3e in Table 1). Quartzolithic sandstones have dominantly metasedimentary detritus from low-to-medium grade 636 Earth-Science Reviews 185 (2018) 624–648 S. Critelli 4.9. Rif chain (Morocco) foreland basin system 2005; El Talibi et al., 2014; Perri et al., 2017 and references therein). This basin separated the Mesosediterranean microplate broke off, which caused the western Mediterranean basins to form during the Miocene (Critelli et al., 2008; Guerrera and Martín-Martín, 2014; Guerrera et al., 2015; Perri et al., 2017). The Mesomediterranean microplate had previously formed a laterally continuous orogenic belt (e.g. Bouillin, 1986; Guerrera et al., 1993). Compositional signatures of Paleocene to Burdigalian sandstones of the stratigraphic cover of the Malaguide Complex constrain the tectonic history of the orogenic accretionary processes and related Betic Cordillera foreland basin system. The Paleocene to Lower Miocene succession of the Sierra Espuña area is made up of several formations evolving from continental and shallow marine, to deep marine environments (e.g. Perri et al., 2017 and bibliography therein). The succession is divided into (i) pre-orogenic depositional sequences, including the Paleocene Mula Formation, the Cuisian-Early Lutetian Espuña and the Valdelaparra formations, the Middle Lutetian-Priabonian Malvariche and the Canovas formations, and the Early Oligocene As Formation; (ii syn-orogenic depositional sequences, including the Late Oligocene-Aquitanian deltaic to shallow-marine strata of the the Bosque Formation, and deep-marine strata of the Rio Pliego Formation, and the Burdigalian p.p. deep-marine strata of the El Niño Formation, the latter as a part of the Viñuela Group (Perri et al., 2017 and bibliography therein). The Rif Chain is the western end of the Maghrebian Chain (with together the Tell and large portions of Sicily) and, together with the Betics, forms the main Alpine orocline of the western and central Mediterranean Sea (Durand-Delga, 1980; Durand-Delga and Fontboté, 1980). The foreland basin system of the Rif Chain is mainly located within the Intra-Rif and Meso-Rif of the External domain. The external domain is represented by a Triassic-Tertiary sedimentary succession, originated from the African paleomargin. Since the Early Miocene the northern Africa continental margin experienced flexural features due to progressive tectonic load of the nappe stack of the deformed southern Tethyan realm (Maghrebian basin) and the Mesomediterranean microplate (internal domains of Ghomaride and Sebtide and Dorsale Calcaire) and the margin has been progressively involved in a foreland basin system filled by turbidite systems. 4.10. Quartzarenite petrofacies Since the Oligocene the external domain was filled by huge arrival of quartzose sediments from the African Craton, and several turbiditic successions have a quartzarenite composition. The quartzose sandstones include the Tanger Unit of the Intra-Rif (Zaghloul et al., 2005), the Numidian Sandstone (Moretti et al., 1991; Thomas et al., 2010), the Asilah (Cazzola and Critelli, 1987), Larache, Zoumi, Ouezzane sandstone formations of the Habt and Ouezzane thrust units of the Intra-Rif nappe (e.g. Wildi, 1983; Zaghloul et al., 2005 and bibliography therein). All these units are deep-marine turbidite systems, while shallow-marine to continental quartzarenite strata are not evident in Mesorif and pre-Rif, while in the Tunisia, fluvio-deltaic quartzarenite systems are present (i.e. the Fortuna Formation; Van Houten, 1980; Thomas et al., 2010). The Numidian quartzarenites as such as other quartzose strata represent the major Cenozoic drainage system on the entire northern Africa margin (e.g. Thomas et al., 2010). At regional scale and correlations, the Numidian event is well represented in Sicily (Wezel, 1970; Barbera et al., 2013), and the southern Apennines (known as Numidian Flysch and the Bifurto Formation; Carbone et al., 1987; Patacca et al., 1992; Fornelli, 1998, Fornelli et al., 2015). 4.8.1. Preorogenic Betic hybrid and quartzose sandstone petrofacies Pre-orogenic strata are hybrid arenites (e.g. Zuffa, 1980) including abundant coeval intrabasinal carbonate and extrabasinal carbonate grains. The siliciclastic signals are present in the lower layers of the Espuña Formation (NCE38CI62CE0; Qm96F0Lt4), and it continues to increases with the As Formation (NCE51CI2CE47; Qm92F0Lt8), as well as extrabasinal carbonate grains, although the composition always is quartzarenite (Perri et al., 2017). Compositional data indicate that the Tertiary succession had their multiple source areas derived from metamorphic, siliciclastic and carbonate rocks, with a minor supply of mafic rocks. The siliciclastic samples are mature (i.e. Espuña Formation, Qm96F0Lt4; As Fm: Qm92F0Lt8) and indicate a clear provenance from a craton interior area. 5. Key provenance relations of sandstones during growing (late Oligocene-Pliocene) circum-Mediterranean Orogen 4.8.2. Rio Pliego- El Niño quartzolithic sandstone petrofacies Sandstone detrital modes for the syn-orogenic cycle abruptly changed from carbonate-rich to siliciclastic rocks. The onset of increasing siliciclastic content occurs in the upper part of the Bosque Formation and the Rio Pliego Formation. Sandstones of the Rio Pliego Formation are quartzolithic (Qm56F0Lt44), in lower portions, with phyllite, slate and fine-grained schist, while sedimentary lithic fragments are minor; sandstones of the upper portions of the Rio Pliego Formation are also quartzolithic (Qm26F0Lt 74) having variable extrabasinal non-carbonate (NCE) versus carbonate CE) grains with a general dominance of siliciclastic content (NCE73 CI1CE26). Similarly, they have variable sedimentary and carbonate versus metamorphic lithic fragments (average value; Lm41Lss29Lsc30; Rg0Rs55Rm45) with a slight dominance of metamorphic grains. The Burdigalian p.p. El Niño Formation, contains fine-medium grained quartzolithic sandstones (Qm61F0Lt39) with significant extrabasinal carbonate grains (NCE64CI0CE36) (Perri et al., 2017). In terms of provenance relations, the onset of the syn-orogenic cycle (Bosque Formation) is marked by a continuous carbonate detrital supply coming from erosion of older Malaguide Mesozoic-Paleogene formations that began to uplift. The sharp increase of the siliciclastic component in the Rio Pliego and El Niño formations testifies abrupt changes of the source area involving the Paleozoic to Mesozoic metamorphic, carbonate and terrigenous rocks of the internal domains (Malaguide and Alpujarride complexes) and neighbor domains as suggested by abundance of slate, phyllite and metarenite, extrabasinal carbonate grains in sandstone strata (Perri et al., 2017). 5.1. Cratonal (African)-derived collisional sandstones During the final closure of the southern and eastern Tethyan realm and onset of accretionary processes, the northern Africa continental margin experienced intense flexural features of the continental lithospere. Since late Eocene, enormous quantities of cratonic derived sandstones widespread accumulated along the various sedimentary basins confined between the African plate and the Iberian, Mesomediterranean and Adria microplates. Tertiary quartzose clastic wedges are clearly derived from African plate, and these clastic wedges include huge volumes of dominantly deep-marine quartzarenite turbidite systems deposited along the flexed flank of the northern Africa continental margin (Table 1; Fig. 6). It includes Eocene through early Miocene turbidite systems of the Meso-Rif and External Rif Nappe domains of the Rif Chain in Morocco (Chiocchini et al., 1978; Cazzola and Critelli, 1987; Puglisi, 2008, 2014), in the Malaguide Complex of the Betic Cordillera (Mula, Espuña and As formations; Perri et al., 2017), the widespread turbidite system of the Numidian Sandstone Formation (formally Numidian Flysch; Thomas et al., 2010; Guerrera et al., 2012; Alcalá et al., 2013; Barbera et al., 2014; and bibliography therein), the Algeciras Formation of the Gibraltar Arc and the fluvio-deltaic system of the Fortuna Formation and Nubian Sandstones of the Tell Chain represent a key regional scale lithosome (Qt94 F3 L3; see Table 2) of the circumMediterranean orogen. In the southern Apennines, equivalent 637 Earth-Science Reviews 185 (2018) 624–648 S. Critelli more felsic (dacite, rhyodacite and rhyolite); these latter volcaniclastic strata are within the Apennines foreland basin system (Cilento Group, Castelvetere and Anzano formations; Critelli and Le Pera, 1994, 1995b; Critelli, 1999; Critelli et al., 2017; Barone et al., 2006; Matano et al., 2014 and in the synrift peri-Tyrrhenian backarc basins (e.g. Critelli et al., 2011, 2017). The late Miocene volcaniclastic strata seems to be not related to the previous Oligo-Miocene magmatism of Sardinia that was dissected at the end of Miocene, and other volcanic sources are inferred as the central Tyrrhenian volcanic arc (e.g. Argnani et al., 1995; Serri et al., 2001). sedimentary sequences of the Numidian quartzarenite occur during the early stage of foreland basin system evolution within the foredeep, the flexed forebulge (Bifurto Formation covering the Mesozoic to early Miocene shallow-marine carbonate platforms) and back-bulge (Lagonegro Basin) depozones (Patacca et al., 1992; Critelli and Le Pera, 1995a; Fornelli, 1998; Critelli, 1999; Critelli et al., 2013, 2017; Fornelli et al., 2015). 5.2. Recycled Orogen sandstones Sandstones derived from accretionary terranes related to collisional processes are widespread all along the various sedimentary basins of the circum-Mediterranean region during closure of remnant ocean realms and subsequent continental collision, from Betic Cordillera to the Rif-Tell and Apennines. One of the most intriguing and contrasting example of foreland basin systems having differentiated recycled orogenic provenances is the Apennines foreland basin system, where clear provenance from Alpine Chain to the north (e.g. Gandolfi et al., 1983; Valloni and Zuffa, 1984; Cibin et al., 2001; Stalder et al., 2018), and the Mesomediterranean microplate, to the west and southwest (Critelli and Le Pera, 1995a, 1998; Critelli et al., 2007, 2013, 2017; Amendola et al., 2016) are alternate and interfingered together, particularly during early-middle Miocene and Late Miocene (Fig. 6). The Betic and RifTellian foreland basin systems are filled by shallow-to-deep-marine clastic sequences reflecting provenance relations from stable flexed continental margins of African craton and Iberian continental block, and from the accreted thrusted terranes of the internal domains of Betic Cordillera in Spain and Rif-Tell Belt in Morocco and Algeria. 5.4. Map 4. Langhian-early Tortonian foreland basin systems 5.4.1. Apennines foreland basin system The Apennines foreland region preserve clastic wedges with contrasting and mixed petrofacies in which the key provenance terranes are coming from the Alps, at its northern edge, from the Sardinia-Corsica block, at its western edge, and from the eastern margin of the Mesomediterranean microplate (mainly the Calabrian terranes) at its western and southwestern and southern edge. Additional provenances of foreland sandstones are from the progressively deformed Adria continental margin, and the active volcanism in the central Mediterranean region since the late Oligocene (e.g., Critelli, 1999; Critelli et al., 2013, 2017). Since early Miocene, the Apenninic domain is the place where huge volume of turbiditic sedimentation were deposited in response of E-NE accretionary processes along the Adria plate (e.g. Ricci Lucchi, 1986; Patacca and Scandone, 1987; Boccaletti et al., 1990). The foreland basin system (i.e. wedge-top, foredeep, forebulge, back-bulge depozones) migrated in time, and siliciclastic and carbonatoclastic deposits, filling the wedge-top and the foredeep, derived from progressive unroofing of crustal blocks of Alps, Sardinia-Corsica and Mesomediterranean microplate (mainly Calabrian terranes) or from erosion of the Adria forebulge (e.g. Critelli, 1999). Final closure of the eastern Tethyan ocean (Lucanian ocean basin) and onset of continental collision in the southern Apennines are dated as early Miocene (Burdigalian). The provenance of the detrital constituents of the Miocene foreland sandstones was dominantly from the eastern continental margin of the Mesomediterranean microplate (Calabrian terranes), the active growing front of the fold-thrust belt (Fig. 7). The key sources of clastics deposited within the foreland basin system include different present-day realms that are: (a) the basement rocks of the northern Calabrian Terranes. Initial signals of provenance from the Calabrian terranes are during final closure of the Lucanian Ocean (Saraceno Formation); (b) the uplifted subduction complex (the Lucanian Oceanic terranes), during the mid-late Miocene; (c) the Mesozoic to Tertiary Apulia/Adria basinal and carbonate platform domains. Since Langhian time, elongate turbidite basins have formed on top of advancing thrust-sheet systems. The Cilento Group, Serra Palazzo, Piaggine, San Giorgio and Gorgoglione formations (Amore et al., 1988; Patacca et al., 1990, 1993; Castellano et al., 1997; Critelli et al., 2011) are the main turbiditic successions of the wedge-top and foredeep depozones in growing foreland basin system, confined between the Mesomediterranean microplate and the Adria forebulge (Fig. 8). Critelli and Le Pera (1994, 1995, 1998) and Critelli et al. (2011, 2013, 2017) discuss in detail the sandstone detrital mode evolution during initial stage of filling of the southern Apennines foreland basin system defining diverse petrofacies since early Langhian with deposition of the Cilento Group basin in the inner portions of the frontal orogen, and the Piaggine sandstone, the Gorgoglione and San Giorgio formations accomodated in wedge-top and foredeep depozones during Serravallian to early Tortonian. Three main regional sandstone suites (petrofacies) are defined to infer the regional paleotectonics of accretionary processes in the southern Apennines foreland evolution. 5.3. Magmatic Arc-derived sandstones Within the Mediterranean region magmatic activity is weadspread since Oligocene and it is mainly subdivided into orogenic and anorogenic magmatic provinces (Serri et al., 2001; Lustrino and Wilson, 2007; Caracciolo et al., 2011). Volcanolithic sandstone suites occur in the circum-Mediterranean region mainly during the late Oligocene, early Miocene, the middle-to-late Miocene and early Pliocene. Occurrence of volcaniclastic layers post early Pliocene is not the subject of this paper and therefore are not discussed here. Volcanolithic sandstones are present during subduction and final closure of the eastern and southern Tethyan oceanic realm generating a Late Oligocene-early Miocene magmatic arc (e.g. Malinverno and Ryan, 1986; Dewey et al., 1989). Remnants of magmatic arc platform are in western Sardinia (e.g. Assorgia et al., 1997) and in the subsurface of the peri-Adriatic region (e.g. Cibin et al., 2001; Di Capua et al., 2016; Di Capua and Groppelli, 2016, and bibliography therein). The magmatic activity during tha late Oligocene-early Miocene is responsible of accomodation of volcanolithic (mainly andesitic) sandstones within the tectonic mélange of the Lucanian Ocean (e.g. Critelli, 1993, 1999; Critelli et al., 2017), the Taveyanne Sandstones in the Alpine foreland basin (Di Capua and Groppelli, 2016), the Petrignacola (Qt7 F48 L45; Valloni and Zuffa, 1984) and Val d'Aveto (Di Capua et al., 2016; Mattioli et al., 2012) formations of sub-ligurian basin of northern Apennines, a northern extension of the Lucanian ocean basin. These sedimentary successions are late Oligocene in age and are interpreted to be derived from the active magmatic arc of Sardinia and Periadriatic volcanic centers (Critelli, 1993; Cibin et al., 2001; Di Capua and Groppelli, 2016; Di Capua et al., 2016). Volcanolithic (andesitic) sandstones are also present in the early Miocene (Burdigalian to Langhian), particularly in the southern Apennines and Sicily in the Tufti di Tusa, Troina-Tusa and Poggio Maria formations (e.g. Ogniben, 1964; Critelli et al., 1990b; de Capoa et al., 2002; Puglisi, 2014), and as isolated volcanolithic layers interbedded with shallow-marine carbonate platform strata (Perrone, 1987; Critelli, 1999) or pelagic sequences (e.g. Bisciaro Formation; Guerrera et al., 2015). Other occurrence of volcaniclastic strata are in the middle and late Miocene, and composition of volcanic debris is 638 Earth-Science Reviews 185 (2018) 624–648 S. Critelli Fig. 7. Paleotectonic map 4 for the Langhian to early Tortonian time, showing onset of accretion of the Mesomediterranean microplate over the Adria margin to form ancestral Apennines. Foreland basin system includes the diverse depozones (according to DeCelles and Giles, 1996) filled by the main clastic wedges of the Cilento Group, Piaggine sandstone, Numidian Sandstone, during Langhian to Serravallian, and the Gorgoglione, Monte Sacro, Nocara, Oriolo, San Giorgio and Serra Palazzo formations, during Serravallian to early Tortonian. Location of the Sardinia magmatic arc that was yet active during Langhian-Serravallian. Adapted after Patacca and Scandone (1987), Patacca et al., (1990, 1993), and Critelli et al. (2011, 2013, 2017). Sandstone suites related to the Map 4 with QtFL diagram include the quartzolithofeldspathic sandstone of the Cilento Group, quartzolithic sandstone of the Piaggine Formation (detritus mainly derived from the oceanic terranes) and following Gorgoglione, Monte Sacro, Oriolo, Serra Palazzo, San Giorgio formations. Quartzose suites are referred to the Numidian sandstones, as such as volcanolithic sandstones are interbedded within the Cilento Group. Dotted polygons are referred to the closure of the eastern/southern Tethyan realm. Shifting of detrital modes suggest onset of unroofing history of the Calabrian terranes. metamorphic detritus (Rg9 ± 6 Rs4 ± 3 Rm87 ± 10) in the lower Cilento Group (Pollica Formation) to abrupt increases of phaneritic plutonic detritus (Rg54 ± 10 Rs3 ± 2 Rm43 ± 10) in the middle and upper Cilento Group (San Mauro Formation) (e.g. Critelli and Le Pera, 1994, 1998; Critelli et al., 2017). In addition to siliciclastic turbidite beds, the Cilento Group includes numerous carbonatoclastic megabeds (ranging from few meters to 65 m thick; Colella and Zuffa, 1988; Cieszkowski et al., 1995; Critelli, 1999), olistostrome beds (ranging from tens to hundreds of meters in thickness), and coarse volcaniclastic debris flows and turbidites. Olistostroma beds are siliciclastics, and include mountain-sized blocks of crystalline rocks of the Calabrian 5.4.2. Langhian to early Tortonian quartzofeldspatholitic/ quartzofeldspathic sandstone petrofacies Corresponds with deposition of the Cilento Group (Pollica, San Mauro and Albidona formations; Langhian-early Tortonian), and the San Giorgio and Serra Palazzo (Langhian-early Tortonian). At regional scale sandstones of these formations are quartzo-feldspatholitic (Qt62 ± 5 F26 ± 5 L12 ± 4; Lm47 ± 11 Lv24 ± 8 Ls29 ± 7; Rg37 ± 8 Rs18 ± 6 Rm4 ± 10), even if in spite of general homogeneous composition, changing nature of detrital signatures are evident during stratigraphic evolution. Particularly in the Cilento Group, detrital supplies changes abruptly from abundance of low-medium 639 Earth-Science Reviews 185 (2018) 624–648 S. Critelli Fig. 8. Paleotectonic map 5 for the Late Tortonian to early Pliocene time, showing eastward shifting of the souuthern Italy orogenic belt deforming and assembling portions of the Adria margin and new location of the foreland basin system. To the west, the Sardinia magmatic arc was dissected to become a remnant arc, due to the onset of rifting of the Tyrrhenian Sea, including syn-rift clastic wedges in the peri-Tyrrhenian area. A new magmatic arc (the central Tyrrhenic magmatic arc) was inferred to be present. Adapted after Patacca and Scandone (1987), Patacca et al. (1990, 1993), Argnani et al. (1995), and Critelli et al. (2011, 2013, 2017). Sandstone suites related to the Map 5 with QtFL diagram include quartzofeldspathic sandstones of the selected foreland clastic wedges on the inner wedge-top over the Calabrian terranes (Crotone and Rossano basins), outer wedge-top depozone (San Bartolomeo, Nocara, Tempa del Prato, Civita and Sorrendstone formations) and within the late Miocene (Castelvetere, Agnone, Anzano-Altavilla) and early-middle Pliocene (Baronia and Sferracavallo synthems) foredeep depozone. Within the inner wedge-top, an Apenninic backthrust (Cariati Nappe; Muto et al., 2014) was accomodated. The QtFL diagram includes previous foreland clastic wedges, and the Late TortonianPliocene foreland, and Late Miocene synrift wedges (Perityrrhenian basins) detrital modes. The arrow, testifies the progressive unroofing history of the fold and thrust belt. limestone and radiolarian chert, mixed with metmorphic detritus in the quartzolithic sandstone testified the obduction and erosion of the accreted oceanic terranes of the oceanic suites. terranes and ophiolitiferous rocks of the Lucanian oceanic terranes. The volcaniclastic interval in the lower San Mauro Formation is interbedded with quartzofeldspatholitic sandstones, and includes abundant felsic (rhyodacite to rhyolite) calcalkaline volcanic particles (Critelli and Le Pera, 1994). The Serra Palazzo (Qt61 ± 4 F29 ± 5 L10 ± 3) and the San Giorgio (Qt57 ± 5 F34 ± 5 Lt9 ± 3; Matano et al., 2014) formations, interpreted as the foredeep basin of the Langhian to Serravallian (Tortonian?) southern Apennines foreland region (Patacca et al., 1990) have quartzofeldspathic sandstones, hybrid arenite and calcarenite, suggesting provenance from both thrust belt and forebulge. 5.4.4. Early Tortonian quartzofeldspathic sandstone petrofacies Corresponds with the Gorgoglione, Monte Sacro, Oriolo and Nocara Conglomerate formations (Selli, 1957, 1962; Critelli and Le Pera, 1994, Critelli and Le Pera, 1995a, 1995b), unconformably covering the deformed oceanic terranes and the Cilento Group, representing the wedge-top depozone sequences of the Tortonian foreland basin system of southern Apennines. Sandstones are quartzofeldspathic (Qt55 ± 5 F38 ± 5 L7 ± 3) having similar provenance to that of the upper Cilento Group, San Giorgio and Serra Palazzo sandstones. This petrofacies with together the Langhian-Tortonian quartzofeldspatholitic petrofacies record accretionary processes and initial unroofing of the crystalline terranes of the Calabrian terrane. 5.4.3. Serravallian to early Tortonian quartzolithic sandstone petrofacies A local Serravallian to early Tortonian quartzolithic petrofacies occurs in the Piaggine Sandstone Formation (Q52 F18 L30). Abundance of serpentinite, serpentine schist, metabasalt, and pelagic calpionellid 640 Earth-Science Reviews 185 (2018) 624–648 S. Critelli The Castelvetere, Agnone and the Altavilla-Anzano sandstones are deposited within the foredeep depozone and detrital modes are plutonic-rich, with up-section increases of sedimentary detritus (Critelli and Le Pera, 1995b). The Castelvetere Formation has a thick olistostrome bed in the basal portions, including mountain-block carbonate olistoliths (Cocco et al., 1974; Critelli and Le Pera, 1995b; Critelli, 1999) that record involvement of the Langhian to Tortonian passive margin (e.g., the inner platform domain) within the thrust belt (Critelli, 1999). Sedimentary detritus is carbonate dominant in the lower Castelvetere; upsection, increases of siliciclastic detritus suggests progressive erosion of older clastic wedges. Interbedded with quartzofeldspathic turbidite sandstone, the upper Castelvetere has a thick olistostrome bed (Cocco et al., 1974), composed of clastic detritus derived from the oceanic complex, and a 1 m-thick volcaniclastic layer. The siliciclastic olistostroma may be the signal of the synthrust accomodation of the deformed oceanic terranes. The syneruptive volcaniclastic layer consists of pyroclast fragments (pumice and shards) having felsic composition (dacite) (Critelli and Le Pera, 1995b). Other volcaniclastic layers are interbedded in other foredeep sandstone suites as the Anzano-Altavilla unit (Barone et al., 2006; and it is testified within the post-evaporitic Laga Formation (Corda and Morelli, 1996), and in synrift basins of the peri-Tyrrhenian region (i.e. Amantea Basin; Muto et al., 2015; Critelli et al., 2017). The volcanic centers of these ash turbidites is unknown, even if the inferred central Tyrrhenian volcanic arc (e.g. Argnani et al., 1995) may be a possible source. The Calabrian terranes represent the key source areas to supplies huge volumes of siliciclastic detritus to the foreland region and other related sedimentary basins of southern Apennines (Fig. 9). Since early Tortonian, backarc rifting has produced the Tyrrhenian Sea (Scandone, 1982). At this time, the western margin of Calabria was affected by detachment causing tectonic denudation (Fig. 9). Syn-rift basins of the western Calabria, and the inner (Barone et al., 2008; Tripodi et al., 2013; Brutto et al., 2016) to the outer foreland basin system have identical detrital modes, plotting within ideal arkose or continental block provenance field (e.g., Dickinson, 1985, 1988) (Fig. 9), in response of major changes in uplift rate in the northern Calabrian terranes (Critelli, 1999). Miocene foreland sandstone suites of the circum-Mediterranean orogenic belt suggest close interplay of lithospheric flexure, thrust accomodation, exhumation and unroofing histories during plate interactions. A key rule has played the Mesomediterranean microplate in forming the tectonic load for developing foreland basin systems in the southern Iberian margin (Betic Cordillera), the African margin (Rif and Tell) and the Adria margin (Apennines). However, differences in sandstone suites between these diverse foreland basin systems testify differences in accretionary processes, exhumation and uplift of differentiate portions of crust involved during the accretion of the Mesomediterranean microplate. Foreland sandstone suites are quite different in composition, suggesting that three main suites are typically (Fig. 10): (i) quartzolithic, for the Betic foreland basin system, involving in thrusting low level of crustal terranes as source areas; (ii) quartzarenite, for the northern Africa (Rif and Tell) foreland basin system, where great influence of the African craton deliveries huge volumes of quartzose material to the basin, and (iii) quartzolithic-to-quartzofeldspathic, for the Apennines foreland basin system, involving in thrusting deeper portions of crustal terranes and major exhumation and uplift generating unroofing sequences of detrital modes in response of increasing tectonic load of the fold-thrust belt in time and space. 5.5. Maps 5 e 6. Late Miocene-early Pliocene foreland basin systems The geodynamic evolution of the last 10 My, in the western-central Mediterranean is named the Tyrrhenian phase (15–0 Ma). The Tyrrhenian phase (or back-arc extension) was responsible for the fragmentation and dispersion of pieces of the Mesomediterranean microplate (Calabria, Sardinia, Corsica), increased the displacement of the accretionary prism over the Adria microplate, the eastward migration of the magmatic arcs, and the roll-back of the adriatic lithosphere (Malinverno and Ryan, 1986; Patacca et al., 1990, 1993; Argnani et al., 1995; Doglioni et al., 1996; Gueguen et al., 1998, 1997). The Tyrrhenian backarc basin migrated eastwards (northeastwards in the northern Apennines and southeastwards in Calabria and Sicily) at velocities of up to 5–7 cm/yr (Doglioni, 1991; Gueguen et al., 1998). Since late Tortonian an abruptly shift in sandstone composition toward arkose or continental-block derived sandstone occurs, suggesting deep erosional processes that affected the Mesomediterranean microplate, and particularly the Calabrian terranes (Fig. 8) (e.g. Critelli and Le Pera, 1998; Caracciolo et al., 2013). In spite of the huge volumes of midcrustal rock detritus, significant contributions are coming from the eroded sedimentary systems of the deformed portions of the Adria margin, both shallow-marine carbonates and deep-marine pelagic strata. The history of deep erosion of the Calabrian terranes is clearly recorded by Tortonian to Messinian clastics (Fig. 8). These foreland sedimentary sequences include (i) inner wedge-top depozones, directly over the Calabrian block, including the peri-ionian Rossano and Crotone basins (Barone et al., 2008; Zecchin et al., 2012, 2013a, 2013b; Muto et al., 2014, 2015) and allochthonous terranes (the Cariati Nappe, a backthrust of late Tortonian age, related to the middle Miocene accretionary phases that created the Foreland Basin system at the intersection of southern Apennines-Calabrian terrane; e.g. Muto et al., 2014, 2015), (ii) outer wedge-top depozones, directly over deformed oceanic terranes, previous foreland strata and the Adria margin domains, including shallow-to deep marine deltaic and turbidite sandstones of the Anzano and San Bartolomeo, Argilloso-Arenacea, Frosinone, Brecce della Renga; (iii) foredeep depozone, at the front of the late Messinianearly Pliocene orogenic wedge, including turbidite systems of the Castelvetere, Agnone, Vallone Ponticello and Villanova del Battista and Torrente Fiumarella formations, and more northward the Laga Formation (e.g. Corda and Morelli, 1996; Stalder et al., 2018, and bibliography therein) and related sequences in wedge-top basins (Chiocchini and Cipriani, 1989, 1992). A key arkosic sandstone petrofacies summarize the late Miocene-early Pliocene filling of the southern Apennines foreland basin system. 5.5.1. Late Miocene arkosic petrofacies Since late Tortonian, the Calabrian terranes have provided abundant detritus to both the foreland region and intermontane basins of the backarc region (Fig. 9); the previous forebulge of the inner platform domain, were assembled within the fold-thrust-belt, and the new forebulge of the foreland basin system might be located on the inner Apulia platform (Monte Alpi Unit; Patacca et al., 1992; Critelli et al., 2017). On the fold-thrust belt, arkosic sandstone strata unconformably overlain the deformed tectonostratigraphic terranes of the southern Apennines orogenic belt (e.g. Patacca et al., 1992; Critelli and Le Pera, 1998; Critelli et al., 2017). These arkosic strata crop out over the Calabrian block, with deposition of evaporitic and post-evaporitic strata (e.g. Barone et al., 2008; Zecchin et al., 2013a, 2013b), the previous foreland clastic wedges and pelagic units (San Bartolomeo, Sorrento, Vallone Ponticello and Villanova del Battista formations; Patacca et al., 1990, 1992, 1993; Barone et al., 2006; Matano et al., 2014; Critelli et al., 2017) and over the inner platform unit (Tempa del Prato Sandstone and Civita Sandstone), and include abundant plutonic and high-grade metamorphic detritus, as such as extrabasinal carbonate detritus. 6. Modern Mediterranean sand analogues to ancient circumMediterranean sandstones Modern geodynamic setting, regional geomorphology and sediment dispersal pathways of the Mediterranean Sea as reflected by 641 Earth-Science Reviews 185 (2018) 624–648 S. Critelli Fig. 9. Paleotectonic map 6 for the late Messinin-early Pliocene, overlapping with previous Map 5, showing the entire filling and provenance relations of the Apennine foreland basin system, with detrital supply coming from both the Alps, for the northern Adriatic foreland clastic wedges (the Laga Formation and the previous Marnoso-Arenacea Formation), and from the Mesomediterranean microplate, for the southern and central Apennine foreland clastic wedges. On he top right of figure, a detail of the tectono-stratigraphic relations of western and eastern Calabria, with evolving Perityrrhenian basin (to the west) and the Peri-ionian basin to the east. Adapted after Barone et al. (2008), Muto et al. (2014, 2015) and Critelli et al. (2011, 2017). Sandstone suites relate to the map 6 with QtFL diagram shows quite homogeneous detrital modes for both Perityrrhenian synrift basins and Peri-ionian and Apennine foreland clasti wedges. Previous discussed sandstone suites are plotted as filled circle, with indication of stratigraphic boundaries times (regional unconformities), while the arrow testifies the general trend of changing nature of composition related to the unroofing history of the fold and thrust belt. intersect the dispersal pathways and sand delivery in a “Eurotype” composite continent, mixed with “Afrotype” rifting continent (e.g. Dickinson, 1988). composition of modern sand, may offer great opportunity for better understanding ancient analogues and regional sandstone suites. The Mediterranean region, in the framework of megageomorphology 642 Earth-Science Reviews 185 (2018) 624–648 S. Critelli collisional events. Sedimentary basins of the circum-Mediterranean orogenic belt contain voluminous sandstones within (i) rifted-continental belt of the Tethyan oceanic realms, (ii) subduction-related basins during the Late Mesozoic-Paleogene closure of the western and northern Tethyan oceanic realm, and Late Paleogene-earliest Miocene closure of the southern and eastern Tethyan oceanic realm; (iii) foreland region of growing circum-Mediterranean orogenic belt of the Betic Cordillera, Rif-Tell belt and the Apennines. Sandstone detrital modes, provenance and dispersal pathway of sand of the large number of clastic wedges during the complex evolution of the circum-Mediterranean orogenic belt, have been integrated with paleotectonic and paleogeographic restorations to unraveal the major tectonic events during evolution of the Mediterranean-type orogens. Mesozoic-to-Pliocene sandstone suites are calibrated with major tectonic settings defining by using test of classification (QtFL, QmFLt, QmKP, QpLvmLsm, LmLvLs, NCeCeCi and RgRsRm) schemes (e.g. Dickinson et al., 1983; Dickinson, 1985; Ingersoll et al., 1984; Zuffa, 1985; Critelli and Le Pera, 1994) to define regional sandstone petrofacies, as follow: 1 Mesozoic Rifted continental margin sequences related to the Tethys Ocean taphrogenesis have significant quartzose sandstone suites from terrestrial rift-valley to proto-oceanic syn-rift and post-rift stages mainly related to peneplaned area of low relief all around the nascent continental plates (Africa and Europe) and microplates (Iberia and Mesomediterranean) and the diverse oceanic realms of the Tethyan Ocean. 2 Late Mesozoic-to Early Paleogene closure of the western and northern Tethyan oceanic realm accomodated quartzofeldspathic and quartzolithic sandstone suites (e.g. Valloni and Zuffa, 1984) in subducted-related basins preciding the Alpine orogen. The eastern and southern Tethyan oceanic realm continued to receive quartzose sandstone suites during the Cretaceous and early Paleogene (e.g. Critelli, 1993; Barbera et al., 2011). 3 Late Paleogene-earliest Miocene closure of the eastern and southern Tethyan oceanic realm is responsible of subduction-related sandstone suites within the tectonic mélange of the Lucanian Ocean (e.g. Bonardi et al., 1988; Critelli, 1993), the onset of a calcalkaline magmatic arc (Sardinian and Periadriatic volcanic centers; Assorgia et al., 1997; Cibin et al., 2001), accretionary tectonics of the Mesomediterranean microplate over the Iberian, Africa and Adria continental margins, and huge volumes of quartzolithic and volcanolithic sandstone suites derived from accreted Paleozoic metamorphic terranes and Mesozoic sedimentary strata (quartzolithic), and active volcanic-arc source (volcanolithic). 4 Early-middle Miocene continental accretion of the Mesomediterranean microplate over (i) the Iberian margin, generating the Betic Cordillera; (ii) the Africa margin, generating the Rif and Tell belt, and (iii) the Adria margin, generating the Apennines. All these circum-Mediterranean belts generate distinctive foreland basin systems. Accretionary processes of the deformed and obducted southern and eastern Tethyan terranes and the Mesomediterranean microplate accomodated huge volumes of mainly deep-marine turbidite sandstones in foreland basins. In the Betic Cordillera, sandstone suites are quartzolithic directly derived from the Malaguide and Alpujarride tectonostratigraphic terranes. In the Rif and Tell belt, huge flexural features of the African continental margin accomodated impressive volumes of quartzarenite turbidites to the adjacent foreland basin, while quartzolithic sandstones are very minor. In the Apennines, the fold-thrust belt was dominated by growing accretionary processes of the Calabrian continental block and other terranes of the eastern margin of the Mesomediterranean microplate, representing the main source area of huge volumes of quartzolithic and quartzofeldspathic and arkosic sandstone suites in response of the unroofing history of the Calabrian terranes. Fig. 10. QtFL diagram of sandstone suites for the circum-Mediterranean foreland basin systems. Data include (i) the northern Africa foreland basin (Rif and Tell), where the main dominantly deep-marine turbidite is quartzarenite in composition, reflecting abrupt flexure of the African continental margin delivering huge volumes of sand from the African craton; (ii) the southern Spain (Betic Cordillera) foreland basin, where sandstones strata are quartzolithic in composition, closely related to a provenance from the Malaguide and Alpujarride complexes of the internal domains of the Betic Cordillera; (iii) the Apennines foreland basin system, where sandstone suites testify changing nature of composition in time from quartzolithic to quartzofeldspathic and arkosic in response of huge uplift, erosion and unroofing of mid-crustal continental blocks of the Mesomediterranean microplate and Alps. Studies on modern sand detrital modes at the Mediterranean scale have focussed on the southern drainage and coastal environments of Spain (e.g. Critelli et al., 2003), of northern Morocco (e.g. Zaghloul et al., 2009; Reddad et al., 2016), the deep-sea fan of the Alboran Sea (Marsaglia et al., 1999; Critelli et al., 2003), the volcanic islands of central Tyrrhenian Sea (Aeolian Island; Morrone et al., 2017) the Tyrrhenian coast of Apennines (Garzanti et al., 2002), drainage, coastal and deep-marine environments of western (Tyrrhenian Sea) and eastern (Ionian Sea) Calabria (e.g. Le Pera and Critelli, 1997; Le Pera et al., 2001; Critelli and Le Pera, 2003; Perri et al., 2015, 2012b) (See Fig. 11). For Calabria, useful dataset includes also sediment and weathering profiles on phaneritic crystalline rocks at the onset of sedimentary cycle (e.g., Le Pera et al., 2001; Scarciglia et al., 2005, 2007, 2016; Borrelli et al., 2012, 2014). This data set, that it is not included in Table 1 reveal close analogies of modern sand modes with Miocene sandstone detrital modes in identical source rocks and dispersal pathways from drainages to deep-marine environments in intra-arc, backarc and foreland settings. The modern setting of the Mediterranean sand dispersal pathways testifies provenance relations with main typical sand suites of quartzolithic sand petrofacies (Betic, Rif, and Tyrrhenian back-arc side of Apennines), quartzofeldspathic sand petrofacies (Ionian piedmont, coast and deep-sea of Calabria), polycyclic quartzose sand petrofacies (eastern end of Betic at intersection with the Atlantic Coast, and northern Morocco), and volcanolithic sand petrofacies in intra-arc setting of Aeolian Islands and the Tyrrhenian coast of Italy derived from the Campania-Latium volcanic province. 7. Conclusions and general implications The geodynamic evolution of the Western Tethys is characterized by multiple phases of rifting, seafloor spreading, subduction, and 643 Earth-Science Reviews 185 (2018) 624–648 S. Critelli Fig. 11. Map with location of samples and QtFL diagram of modern sand suites (river, beach, delta, shallow-marine and deep-marine turbidite) for the circumMediterranean region. Data include (they are not included in Table 1) the: (i) river and beach quartzolithic and quartzose sand of the Mediterranean coast of Spain (data from Critelli et al., 2003); (ii) river and beach quartzolithic sand of the Mediterranean coast of northern Morocco (data from Zaghloul et al., 2009; Reddad et al., 2016); (iii) volcanolithic, quartzofeldspathic and quartzolithic river and beach sand of Tyrrhenian coast of Apennines and Calabria (data from Le Pera and Critelli, 1997; Garzanti et al., 2002; Critelli and Le Pera, 2003) and shallow-marine and deep-marine lithofeldspathic turbidite sand of the Paola Basin (Tyrrhenian Sea) (Critelli and Le Pera, 1998, 2003; Critelli, 1999); (iv) river, beach, delta, shallow-marine and deep-marine quartzofeldspathic turbidite sand of the Ionian Sea (data from Critelli and Le Pera, 1994, 2003; Le Pera et al., 2001; Perri et al., 2012, 2015); (v) river and beach quartzolithic sand of Ionian coast of Apennines (Critelli and Le Pera, 1998, 2003), and (vi) beach volcanolithic sand of the Aeolian volcanic archipelago (Lipari Island; Morrone et al., 2017). Dataset includes also Middle Miocene, Pliocene and Pleistocene sands of ODP Leg 161 Sites 976, 977, 978 Alboran Sea; Marsaglia et al., 1999). Adria continental margin, including pelagic and shallow-marine carbonate platform strata. 5 Late Miocene-early Pliocene in central Mediterranean correspond with the rifting stage of the opening of the Tyrrhenian Sea, the detachment of inner portions of the fold-thrust belt causing tectonic Important sources for the northern Apennines foreland turbidite systems are also the uplifted Alpine chain, particularly since Serravallian (Marnoso-Arenacea Formation; e.g. Gandolfi et al., 1983) to the late Miocene (Laga Formation; e.g. Stalder et al., 2018). Additional source areas are the progressive deformed terranes of the 644 Earth-Science Reviews 185 (2018) 624–648 S. Critelli denudation and increasing of uplift. The Calabrian terrains experienced huge uplift and denudational processes and sediment generation with dispersal pathway in the Apennines foreland basin system, and to the clastic wedges of the Perityrrhenian basins. Barbera, G., Barone, G., Mazzoleni, P., Puglisi, D., Khozeyem, H.M., Mashaly, O., 2013. Mineralogy and Geochemistry of the Numidian Formation (Central-Northern Sicily): intra-formation variability and provenance evaluation. Ital.J.Geosci. 132, 13–26. Barbera, G., Barone, G., Mazzoleni, P., Puglisi, D., Khozeyem, H.M., Mashaly, O., 2014. Mineralogy and Geochemistry of the Numidian Formation (Central-Northern Sicily): intra-formation variability and provenance evaluation. Ital. J. Geosci. 133, 13–26. Barone, M., Critelli, S., Le Pera, E., Di Nocera, S., Matano, F., Torre, M., 2006. 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Bonardi, G., Amore, F.O., Ciampo, G., de Capoa, P., Miconnet, P., Perrone, V., 1988. Il Complesso Liguride Auct.: stato delle conoscenze e problemi aperti sulla sua evoluzione pre-appenninica ed. i suoi rapporti con l'Arco Calabro. Mem. Soc. Geol. Ital. 41, 17–35. Boccaletti, M., Ciaranfi, N., Cosentino, D., Deiana, G., Gelati, R., Lentini, F., Massari, F., Moratti, G., Pescatore, T., Ricci Lucchi, F., Tortorici, L., 1990. Palinspastic restoration and paleogeographic reconstruction of the peri-Tyrrhenian area during the Neogene. Paleogeography Paleoclimatology Paleoecology 77, 41–50. Bonardi, G., Cavazza, W., Perrone, V., Rossi, S., 2001. Calabria-Peloritani terrane and northern Ionian Sea. In: Vai, G.B., Martini, I.P. (Eds.), Anatomy of an Orogen: the Apennines and Adjacent Mediterranean Basins. Kluwer Academic Publishers, pp. 287–306. Bonardi, G., Ciarcia, S., Di Nocera, S., Matano, F., Sgrosso, I., Torre, M., 2009. Carta delle principali unità cinematiche dell'Appennino meridionale. Nota illustrativa. 128. Bollettino della Società Geologica Italiana, pp. 47–60. Borrelli, L., Perri, F., Critelli, S., Gullà, G., 2012. Minero-petrographical features of weathering profiles in Calabria, southern Italy. Catena 92, 196–207. Borrelli, L., Perri, F., Critelli, S., Gullà, G., 2014. Characterization of granitoid and gneissic weathering profiles of the Mucone River Basin (Calabria, southern Italy). Catena 113, 325–340. Bouillin, J.P., 1986. Le bassin maghrébin: une ancienne limite entre l'Europe et l'Afrique à l'ouest des Alpes. Bulletin de la Société Géologique de France 8, 547–558. Bouillin, J.P., Durand Delga, M., Olivier, Ph., 1986. Betic-Rifain and Tyrrhenian arcs: distinctive features, genesis and development stages. In: Wezel, F. (Ed.), The Origin of Arcs. Elsevier Science Publishers, Amsterdam, pp. 281–304. Brutto, F., Muto, F., Loreto, M.F., De Paola, N., Tripodi, V., Critelli, S., Facchin, L., 2016. The Neogene-Quaternary geodynamic evolution of the Central Calabrian Arc: a case study from the western Catanzaro Trough Basin. J. Geodyn. 102, 95–114. de Capoa, P., Guerrera, F., Perrone, V., Serrano, F., Tramontana, M., 2000. The onset of the syn-orogenic sedimentation in the Flysch Basin of the Sicilian Maghrebids: state of the art and new biostratigraphic constraints. Eclogae Geol. Helv. 93, 65–79. de Capoa, P., Di Staso, A., Guerrera, F., Perrone, V., Tramontana, M., Zaghloul, M.N., 2002. The Lower Miocene volcaniclastic sedimentation in the Sicilian sector of the Maghrebian Flysch Basin: geodynamic implications. Geodin. Acta 15, 141–157. de Capoa, P., Guerrera, F., Perrone, V., Tramontana, M., 2003. The extension of the Maghrebian Flysch Basin in the Apenninic Chain: Palaeogeographic and palaeotectonic implications. 21. Travaux de l'Institut Scientifique de Rabat, pp. 77–92. de Capoa, P., Di Staso, A., Perrone, V., Zaghloul, M.N., 2007. The age of the foredeep sedimentation in the Betic-Rifian Mauretanian Units: a major constraint for the reconstruction of the tectonic evolution of the Gibraltar Arc. Comptes Rendus de l'Academie des Sciences 339, 161–170. de Capoa, P., D'Errico, M., Di Staso, A., Perrone, P., Somma, R., Zaghloul, M.N., 2013. Biostratigraphic constraints for the paleogeographic and tectonic evolution of the Alpine Central-Western Mediterranean orogenic belt (Betic, Maghrebian and Apenninic chains). Rend. Online Soc. Geol. Ital. 25, 43–63. Caracciolo, L., Critelli, S., Innocenti, F., Kolios, N., Manetti, P., 2011. Unravelling provenance from Eocene-Oligocene sandstones of the Thrace Basin, North-east Greece. Sedimentology 58, 1988–2011. Caracciolo L., Von Eynatten H., Tolosana-Delgado R., Critelli S., Manetti P., Marchev P., 2012. Petrological, geochemical, and statistical analysis of Eocene-Oligocene sandstones of the Western Thrace Basin, Greece and Bulgaria. J. Sediment. Res. 82, 482–498. Caracciolo, L., Gramigna, P., Critelli, S., Calzona, A.B., Russo, F., 2013. Petrostratigraphic analysis of a Late Miocene mixed siliciclastic-carbonate depositional system (Calabria, Southern Italy): implications for Mediterranean paleogeography. Sediment. Geol. 117–132 284–285. Carbone, S., Lentini, F., Sonnino, M., De Rosa, R., 1987. Il Flysch Numidico di Valsinni (Appennino Lucano). Boll. Soc. Geol. Ital. 106, 331–345. Castellano, M.C., Putignano, M.L., Sgrosso, I., 1997. Sedimentology and stratigraphy of the piaggine sandstones (Cilento, southern Apennines, Italy). Giorn. Geol. 59, 273–287. Cavazza, W., 1989. Detrital modes and provenance of the Stilo-Capo d'Orlando Formation (Miocene), southern Italy. Sedimentology 36, 1077–1090. Cavazza, W., Ingersoll, R.V., 2005. Detrital modes of the Ionian forearc basin fill (Oligocene-Quaternary) reflect the geodynamic evolution of the Calabria-Peloritani terrane (southern Italy). J. Sediment. Res. 75, 268–279. In conclusions, provenance interpretations, used in conjunction with other stratigraphic and structural evidence can contribute to test alternate paleogeographic and paleotectonic evolution. The circumMediterranean orogen is a key place to test provenance relations at regional scale, and can be useful for analysis of sediment dispersal systems on a global scale of other major orogens. Acknowledgments This research was funded by MIUR (Italian Ministry of Education, University and Research), MIUR-PRIN Project 2001.04.5835 “Age and characteristics of the Verrucano-type deposits from the Northern Apennines to the Betic Cordilleras: consequences for the palaeogeographic and structural evolution of the central-western Mediterranean Alpine Chains”, the 2006–2008 MIUR-PRIN Project 2006.04.8397 “The Cenozoic clastic sedimentation within the circum-Mediterranean orogenic belts: implications for palaeogeographic and palaeotectonic evolution”, the 2010-2012 MIUR-PRIN Project The Thrace sedimentary basin (Eocene-Quaternary; Turkey, Greece, Bulgaria): stratigraphicdepositional architecture and sediment dispersal pathway within postorogenic basins”, and the University of Calabria MIUR-ex60% Projects (Palaeogeographic and Palaeotectonic Evolution of the CircumMediterranean Orogenic Belts, 2001–2005; and Relationships between Tectonic Accretion, Volcanism and Clastic Sedimentation within the Circum-Mediterranean Orogenic Belts, 2006-2018; support to S. Critelli). This paper was supported by the “Laboratory of Geodynamics, Geo-Paleobiology and Earth Surface Processes” of the Departmemnt of Biology, Ecology and Earth Sciences at the University of Calabria. F. Perri and G. Campilongo helping on drawing figures. I gratefully acknowledge discussions in the field and constructive criticism of J. Arribas, C. Doglioni, A. Martin-Algarra, M. Martin-Martin, F. Muto, F. Perri, V. Perrone, N. Zaghloul and G.G. Zuffa. Author thank J. Arribas, T. Lawton and M. Martini for reviewing an early version of the manuscript, and M. Martin-Martin and G. Mongelli for final review of the manuscript. This paper is dedicated to Bill Dickinson whose ideas were important and influenced the methodological conception of this work. References Alcalá, F.J., Guerrera, F., Martín-Martín, M., Raffaelli, G., Serrano, F., 2013. 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