Geological Field Trips

Società Geologica Italiana

2015 Vol. 7 (2.2) ISPRA Istituto Superiore per la Protezione e la Ricerca Ambientale

SERVIZIO GEOLOGICO D’ITALIA Organo Cartografico dello Stato (legge N°68 del 2-2-1960) Dipartimento Difesa del Suolo

ISSN: 2038-4947

A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from the foreland peri-Ionian margin to the backarc Tyrrhenian margin 86° Congresso Nazionale della Società Geologica Italiana - , 2012

DOI: 10.3301/GFT.2015.04 A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from the foreland peri-Ionian margin to the backarc Tyrrhenian margin F. Muto - S. Critelli - G. Robustelli - V. Tripodi - M. Zecchin - D. Fabbricatore - F. Perri GFT - Geological Field Trips geological fieldtrips2015-7(2.2) Periodico semestrale del Servizio Geologico d'Italia - ISPRA e della Società Geologica Italiana Geol.F.Trips, Vol.7 No.2.2 (2015), 65 pp., 38 figs. (DOI 10.3301/GFT.2015.04)

A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from the foreland peri-Ionian margin to the backarc Tyrrhenian margin 86° Congresso Nazionale della Società Geologica Italiana, Cosenza 18-20 settembre 2012

Francesco Muto(1), Salvatore Critelli(1), Gaetano Robustelli(1), Vincenzo Tripodi(1), Massimo Zecchin(2), Davide Fabbricatore(1), Francesco Perri(1) 1 Università della , Dipartimento di Biologia, Ecologia e Scienze della Terra, Arcavacata di - 87036 Cosenza. 2 Istituto Nazionale di Oceanografia e di Geofisica Sperimentale - OGS, Borgo Grotta Gigante, 42/c - 34010 Sgonico, Trieste. Corresponding Author e-mail address: [email protected]

Responsible Director Claudio Campobasso (ISPRA-Roma) Editorial Board Editor in Chief Gloria Ciarapica (SGI-Perugia) M. Balini, G. Barrocu, C. Bartolini, 2 Editorial Responsible D. Bernoulli, F. Calamita, B. Capaccioni, Maria Letizia Pampaloni (ISPRA-Roma) W. Cavazza, F.L. Chiocci, R. Compagnoni, D. Cosentino, Technical Editor S. Critelli, G.V. Dal Piaz, C. D'Ambrogi, Mauro Roma (ISPRA-Roma) P. Di Stefano, C. Doglioni, E. Erba, publishing group R. Fantoni, P. Gianolla, L. Guerrieri, Editorial Manager Maria Luisa Vatovec (ISPRA-Roma) M. Mellini, S. Milli, M. Pantaloni, V. Pascucci, L. Passeri, A. Peccerillo, Convention Responsible L. Pomar, P. Ronchi, B.C. Schreiber, Anna Rosa Scalise (ISPRA-Roma) L. Simone, I. Spalla, L.H. Tanner, Alessandro Zuccari (SGI-Roma) C. Venturini, G. Zuffa. ISSN: 2038-4947 [online]

http://www.isprambiente.gov.it/it/pubblicazioni/periodici-tecnici/geological-field-trips

The Geological Survey of , the Società Geologica Italiana and the Editorial group are not responsible for the ideas, opinions and contents of the guides published; the Authors of each paper are responsible for the ideas, opinions and contents published. Il Servizio Geologico d’Italia, la Società Geologica Italiana e il Gruppo editoriale non sono responsabili delle opinioni espresse e delle affermazioni pubblicate nella guida; l’Autore/i è/sono il/i solo/i responsabile/i. DOI: 10.3301/GFT.2015.04 A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from the foreland peri-Ionian margin to the backarc Tyrrhenian margin F. Muto - S. Critelli - G. Robustelli - V. Tripodi - M. Zecchin - D. Fabbricatore - F. Perri geological fieldtrips2015-7(2.2)

INDEX

Information Day 2 - The Crati basin ...... 35

Abstract ...... 4 STOP 2.1: Arente River (Crati Valley, CS). The eastern Lower Riassunto ...... 5 Pleistocene Crati basin infill ...... 40 Program ...... 6 STOP 2.2: Noggiano (Rende). Pleistocene-recent normal Safety/Accomodation ...... 8 fault in the western margin ...... 44 STOP 2.3: Villa Miceli- (CS). Transpressive N-S Excursion notes trending fault at the western margin of the Crati basin ...... 44 Tectono-stratigraphic architecture of the Geological setting ...... 9 perityrrhenian basin ...... 45 STOP 2.4: (CS). Tectono-stratigraphic Itinerary architecture of the Serravallian-Tortonian Amantea basin infill 3 (Cozzo Varallo section) and post infill tectonics ...... 49 Day 1 - The Cirò and basin ...... 16 STOP 2.5: Regastili (CS). Transpressive fault zone at the northern margin of the Amantea basin ...... 53 STOP 1.1: (CS). Thrust between the STOP 2.6: Serra d’Aiello (CS). Tortonian extensional tectonics “ Nappe” and the marginal in the Amantea basin infill ...... 54 Serravallian-Messinian successions ...... 21 STOP 2.7: Torrente Scala (CS). Rotated extensional faults STOP 1.2: (CS). The allochthonous and rollover anticline ...... 56 Oligocene-Middle Miocene succession ...... 22 STOP 1.3: Geometry and kinematics of NW oriented References ...... 58 transpressive fault ...... 23 The Plio-Pleistocene succession of the Crotone basin ..24 index STOP 1.4: The Pliocene south of ...... 29 STOP 1.5: Zinga (KR). Timpa di Cassiano and the western side of the Vitrano Valley ...... 31 STOP 1.6: The Serra Mulara formation ...... 32

DOI: 10.3301/GFT.2015.04 A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from the foreland peri-Ionian margin to the backarc Tyrrhenian margin F. Muto - S. Critelli - G. Robustelli - V. Tripodi - M. Zecchin - D. Fabbricatore - F. Perri

Abstract geological fieldtrips2015-7(2.2)

The fieldtrip corresponds to a transect across the northeastern to the western Calabria. The two-days fieldtrip illustrates the Miocene to Quaternary tectono-stratigraphic features of the two distinctive Calabria margins. Sedimentary architecture and tectonic activity are testified in the infill of basins. Some structural features of the Calabrian Neogene basins cropping out in the northern sector of Calabria are exposed. The first day concerns the Neogene structural and stratigraphic evolution of the eastern Calabria margin in the peri-Ionian piedmont. The fieldtrip focus on the effects of the tectonic deformation during Neogene sedimentation in the Rossano and Crotone basins. Typical foreland-basins characterized by clastic sediments were derived from uplifted fold-thrust belts exposing sedimentary, metasedimentary and plutonic source rocks. The entire stratigraphic, structural and compositional data set are interpreted using new general models of sequential evolution of foreland basin systems. The asymmetric fold growths, are also responsible of the progressive unconformities observed in the Rossano and Crotone basins. Facies associations record strong erosion and cannibalization processes of the lower stratigraphic unit, whereas a marine clastic sedimentation persisted in the Cirò basin. The exposed stratigraphic and structural architecture are related to the offshore borehole and 4 seismic stratigraphy, suggesting the presence of structural highs, interpreted as thrust and folds and having the main onshore evidence in the “Cariati Nappe”. During the fieldtrip, some outcrops of the margin flexure and related progressive unconformities in the succession and major backthrust can be looked. Pliocene- Quaternary sedimentary architecture and tectonic activity will be observed in the Crotone basin. In the second day, the fieldtrip is mainly concentrated on the western margin of Coastal Chain along the Amantea basin. In this day other stops in the Crati basin on temporal and spatial distribution of transtensional and transpressional information faulting involving the metamorphic units of the Coastal Chain and the Pliocene-Pleistocene deposits can be observed. To the north of the Amantea village, the marginal facies of the infill outcrop and the basin margin has been offset along the major fault zone. To the south of the Amantea village, tectono-stratigraphic assemblage of the second sequence and Tortonian growth faults can be observed. Panoramic view of the western Coastal Range piedmont zone will be shown during the Stop in the village.

Keywords: Calabria, west-east geological transect, back-arc region, foreland region, Neogene stratigraphy, basin analysis. DOI: 10.3301/GFT.2015.04 A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from the foreland peri-Ionian margin to the backarc Tyrrhenian margin F. Muto - S. Critelli - G. Robustelli - V. Tripodi - M. Zecchin - D. Fabbricatore - F. Perri

Riassunto geological fieldtrips2015-7(2.2)

L’escursione consiste in una geotraversa che unisce i margini orientale e occidentale della Calabria. Durante i due giorni di escursione vengono illustrati i caratteri tettono-stratigrafici dei bacini miocenici peri-ionici e peri- tirrenici attraverso la successione di riempimento plio-pleistocenica del bacino del Fiume Crati posto tra i due margini. I caratteri strutturali dei bacini neogenici sono ben esposti nel settore settentrionale della Calabria. La prima parte dell’escursione è dedicata ai bacini peri-ionici con particolare riferimento alla porzione neogenica del bacino di Rossano-Cirò e del Bacino crotonese. I tipici bacini di foreland caratterizzati da sedimentazione clastica derivano dall’uplift degli orogeni con l’esposizione delle rocce sedimentarie, metasedimentarie e plutoniche. I dati stratigrafici, strutturali e composizionali sono stati interpretati usando nuovi modelli generali dell’evoluzione sequenziale dei sistemi di bacini di foreland. La crescita di pieghe asimmetriche è responsabile delle unconformity progressive osservabili nei bacini di Rossano e Crotone. Le associazioni di facies registrano una forte erosione e processi di cannibalizzazione della prima unità deposizionale, mentre nel bacino di Cirò persisteva una sedimentazione clastica marina. L’architettura stratigrafica e strutturale esposta è stata correlata ai pozzi e alle stratigrafie sismiche presenti in offshore, suggerendo la presenza di alti strutturali, interpretati 5 come thrust e pieghe aventi la maggiore evidenza a terra nella “Falda di Cariati”. In alcuni stops possono essere osservati il margine deformato e le relative discordanze progressive nella successione legate ai back-thrust principali. L’architettura deposizionale plio-pleistocenica e l’attività tettonica sono osservabili nella successione del bacino crotonese. Durante il secondo giorno, l’escursione è principalmente concentrata sul margine occidentale della Catena costiera lungo il bacino di Amantea. Lungo l’itinerario è possibile osservare la distribuzione spazio-temporale della deformazione transtensiva e transpressiva all’interno del bacino del Crati, che coinvolge sia il substrato metamorfico della Catena costiera, sia la successione plio-pleistocenica. A nord information della cittadina di Amantea, le facies marginali del riempimento miocenico del bacino di Amantea sono deformate lungo il sistema di faglia principale. A sud della cittadina, viene osservata l’architettura tettono-stratigrafica della seconda sequenza e le faglie di crescita tortoniane. Una visione panoramica generale del margine occidentale della Catena costiera è osservabile dal paese di Fiumefreddo Bruzio.

Parole chiave: Calabria, transetto geologico ovest-est, back-arc, foreland, stratigrafia neogenico-quaternaria, analisi di bacino. DOI: 10.3301/GFT.2015.04 A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from the foreland peri-Ionian margin to the backarc Tyrrhenian margin F. Muto - S. Critelli - G. Robustelli - V. Tripodi - M. Zecchin - D. Fabbricatore - F. Perri

Program geological fieldtrips2015-7(2.2)

The field trip consists in a geological transect starting from the north-eastern and eastern Ionian margin of Calabria, crossing the central area of the Crati Valley and ending in the Tyrrhenian margin of Calabria. The fieldtrip illustrates the Neogene to Quaternary tectono-stratigraphic evolution of the two distinctive Calabria margins.

The first day concerns the Neogene structural and stratigraphic outline of the eastern Calabria margin. From the Mandatoriccio village (Stop 1.1) is possible to recognize outcrops of the autochthonous Middle Miocene deposits accumulated in longitudinal wedge-top depozones and the main onland outcrop of the allochthonous succession represented by the so-called Cariati nappe. Tectonic assemblage and structural kinematics of the back-thrust and major transcurrent faults are detailed in the village of Scala Coeli (Stops 1.2) and near San Morello (Stops 1.3). After the lunch, the fieldtrip continues in the Crotone basin, where the Lower Pliocene and late Pliocene basin infill is outlined. Stratigraphic and tectonic architecture of the northern side of the basin is well documented in the Stop 1.4, near Casabona (Casabona horst and the South Casabona half-graben). The deposition of the Spartizzo clay (middle Pliocene) was controlled by the activity of the fault bounding the south Casabona half-graben, favouring the 6 accumulation of a relatively thick succession. The Stop 1.5 concerns the western side of the Vitravo Valley where crops out prograding forced-regressive wedges of the Zinga sandstone. The architecture was controlled by the growth of a NE-trending non-cylindrical anticline (Russomanno anticline), while the Belvedere formation, within the Belvedere half-graben, was linked to the activity of NE-trending listric normal growth fault. The structures represent the effect of deformation induced by salt tectonics. The first day end with the oucrop of the Serra Mulara formation (Stop 1.6), a middle Pleistocene coarse-grained canyon fill succession. information The second day starts crossing the Sila Massif and reaches the Crati Valley basin. The field trip starts in a quarry located on the eastern margin of the Crati basin. In the Stop 2.1 is well exposed the architecture of the lower Pleistocene marginal delta type deposits. Facies associations of the clastic infill with spectacular normal and strike-slip faults are exposed. Crossing the Crati Valley reach the Stops 2.2 and 2.3. In these stops the temporal and spatial distribution of transtensional and transpressional faulting, involving the metamorphic units of the Coastal Chain and the Pliocene-Pleistocene deposits, can be observed. The field trip continues crossing the Coastal Range and arriving to Fiumefreddo Bruzio for the lunch and for the visit to the Medieval DOI: 10.3301/GFT.2015.04 A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from the foreland peri-Ionian margin to the backarc Tyrrhenian margin F. Muto - S. Critelli - G. Robustelli - V. Tripodi - M. Zecchin - D. Fabbricatore - F. Perri Castle. The field trip moves for the village of Belmonte Calabro where the Serravallian-Tortonian sequences of the Amantea basin infill are well cropping out in the Stop 2.4. To the north of the Belmonte Calabro village geological fieldtrips2015-7(2.2) (Regastili site, Stop 2.5) the marginal facies of the infill crops out and the basin margin is offset by a major transpressional fault zone. The last stops are located to the south of the Amantea village (Stops 2.6 and 2.7). The tectono-stratigraphic architecture of the Tortonian sequence is characterized by growth faults and roll-over anticline belonging to the opening of the Tyrrhenian back-arc basin.

7 information

Fig. 1 – Geographical location of the field trip area, roadmap and Stops. DOI: 10.3301/GFT.2015.04 A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from the foreland peri-Ionian margin to the backarc Tyrrhenian margin F. Muto - S. Critelli - G. Robustelli - V. Tripodi - M. Zecchin - D. Fabbricatore - F. Perri Safety Visits geological fieldtrips2015-7(2.2) Hardhat, hat, hiking shoes, sunglasses, are strongly - Librandi (Cirò) Wine farm, SS 106 - C.da San recommended. Gennaro, 88811 - Cirò Marina (KR). Depending on the weather conditions, the path in the www.callmewine.com/it/cantina/librandi.html San Morello (CS) stops could be slippery. Reflective - Medieval Castle of Fiumefreddo Bruzio (CS). vest for stops along the road. http://www.calabriaintour.it/fiumefreddo-bruzio.asp

Hospital During the field trip the Stop 2.1 requires permission to enter in the Arente River quarry. - Ospedale Civile di (CS), Via Gramsci. Phone 0984 9790. Field Trip Sponsors - Ospedale Annunziata, Via Migliori 1, 87100 - Cosenza. Phone 0984 6811. - University of Calabria; - Department of Biology, Ecology and Earth Sciences; Emergency Contact Numbers - Librandi (Cirò Marina, KR) Wine farm; - Hotel Biafora (San Giovanni in Fiore, CS); 8 - Medical Emergencies 118; - Municipality of Fiumefreddo Bruzio (CS). - Fire Department 115; - State Police 113.

Accomodation

Biafora Resort & SPA in Sila, S.S. 107 - Locality Torre information Garga 9, 87055 - San Giovanni in Fiore (CS) Phone 0984 970078. A list of farmhouse in the Crotone province is available at the website: http://www.provincia.crotone.it/agriturismo/ The farm resort very close to the crotonese outcrops is: http://www.dattilo.it/#_=_ DOI: 10.3301/GFT.2015.04 geological field trips 2015 - 7(2.2)

9 excursion notes an margin , Savelli & , Savelli e.g. F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri Critelli & Le Pera, 1998). Several Pliocene-Pleistocene basins cross-cut the Apennines and northern 1998). Several Critelli & Le Pera, A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 Wezel, 1980; Barone et al., 1982; Sartori, 1982, 1990). 1980; Barone et al., Wezel, of the Calabrian Arc towards migration combined with the progressive Since Middle Miocene, overthrusting 1986; Dewey et al., & Ryan, Basin (Malinverno associated with the opening of Tyrrhenian southeast was 1989; Decandia et al., outcrops 1998). Thick and continuous successions of Miocene basins occur in several Marittimo basins). In the same area and Belvedere margin of Calabria (Amantea, Paola along the Tyrrhenian slope basin (Argnani constitute the thick sedimentary succession of Paola the Pliocene-Pleistocene strata Calabria thrust pile; among these, the Mercure basin and the Crati basin are the most important in Calabria Calabria thrust pile; among these, the Mercure basin and Crati 1995; Schiattarella, 1998; et al., 1993; Colella, 1994; Tortorici 1990; Cinque et al., et al., (e.g. Turco 1998). & Pasqui, Tavarnelli area,On the back-arc 1995), such as the submarine et al., Pliocene-Pleistocene basins (Tortorici fault-controlled margin ( basin and the Gioia basin, represent synrift troughs of eastern Tyrrhenian Paola Geological setting form an arcuate mountain belt that lies between the thrust belts of Apennines to The Calabrian Terranes on the agreement in the literature the north and Maghrebian Chain to south. There is a general geometrical position of the Calabrian Arc units, and on their ages. ophiolites, carbonates, Mesozoic Mesozoic are observed paragneisses orthogneisses, and Paleozoic slates and metapelites, Paleozoic Paleozoic-Mesozoic sedimentary successions. by Meso-Cenozoic from bottom to top; these units are frequently covered Ma geodynamic processes in and geology of Calabria are the results post-30 The modern physiography along the eastern flank (northern ), and which synchronous accretionary processes were active Margin). rifting processes along the western flank (Eastern Tyrrhenian by Pliocene- and covered frontal edge of the accretionary wedge is buried below sea-level The active by uplift and ridge to the west is characterized Quaternary foreland deposits, whereas the main elevated of the thrust belt includes wedge-top depozone extensional processes. The modern basin configuration and (the Gulf of basins), the marine and subaerial foredeep depozone (the Corigliano- basin), the forebulge (the Gallipoli river the Bradano (the southern Adriatic Sea; basin) and the back-bulge e.g., geological field trips 2015 - 7(2.2) excursion notes 10 Mattei ; an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 & Trincardi, 1988; Milia et al., 2009). Since Late Miocene, the ancient reverse contacts responsible for the 2009). Since Late Miocene, the ancient reverse 1988; Milia et al., & Trincardi, 2001 et al., by extensional tectonics (Rossetti building of the Calabrian nappe complex were reactived et al., 2002; Cifelli et al., 2007b). 2002; Cifelli et al., et al., basement units, belonging to the The Calabrian orogenic belt is composed by a thrust sheet of Palaeozoic since Oligocene, ophiolite bearing units of the Neo-Tethys margin, over-thrusting, former European-Iblean 1989). Since the Middle Miocene, 1976; Dewey et al., domain (Ogniben, 1973; Amodio Morelli et al., such carbonate rocks of the Apenninic Maghrebide Chain. In particular, Mesozoic tectonic edifice tectonically covered striking, the Neogene to Quaternary history of orogenic edifice is mainly controlled by activity NW-SE 2000), driving the differential south-eastwards Dijk et al., 1993; Van (Catalano et al., shear zones sinistral of the foreland basin system of the Calabrian Arc Neogene foredeep and wedge-top depozones migration margin (Critelli & Adria passive the growing orogenic belt and flexed 1998). The geodynamic evolution Le Pera, between collisional processes and extensional is the result of complex interactions Mediterranean of the central convergencetectonics controlled by the Cenozoic 1989). plates (Dewey et al., between African and Eurasian by these processes since the Neogene,The main tectonic elements generated are the southern Apennine- subduction of the Adriatic to the westward Basin, both linked back-arc Maghrebian Chain and the Tyrrhenian discontinuous, with area was extension in the Tyrrhenian and Ionian lithospheres (Fig. 2). The back-arc of the locus extension with time, and it accompanied shortening in Apennine-Maghrebian migration &fold and thrust belt (Malinverno directed toward 2005a, b). This extension was 1986; Finetti et al., Ryan, the SE during late sub-basin, and toward the Vavilov to early Pliocene, generating the east from Tortonian et al, 1990; Sartori, 2003). opened (Patacca Pliocene-early Pleistocene, when the Marsili sub-basin was attributed to the interference of retreating oceanic extension was back-arc Episodicity in the Tyrrhenian blocks), leading to continental foreland lithosphere (Apulian and Pelagian buoyant slab with intervening stop or strong slowing-down of the subduction (Argnani &temporary 1999; Sartori, 2003). Slab Savelli, for the subsequent resumption of flow are commonly invoked tearing episodes accompanied by mantle lateral 2008). et al., 2004; Chiarabba et al., the subduction (Faccenna of Terrane (the Calabria-Peloritani the Calabrian Arc represents an independent arcuate terrane In this frame, southern Apennine Chain and the E-trending Sicilian 2001) that connects the NW-trending Bonardi et al., basins (Fig. 2). It is composed of a pile pre-Mesozoic the Ionian and Tyrrhenian Maghrebides, and separates geological field trips 2015 - 7(2.2) excursion notes 11 an margin , 1999), et al., Lickorish e.g. F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 produces the arcuate shape exhibited by the central sector of the Calabrian Arc (Fig. 2), through both produces the arcuate shape exhibited by central (southern Apennines) rotations in a “saloon-door”clockwise (Sicily and Calabria) counter-clockwise 2002; Speranza et al., (Rosenbaum fashion until early Pleistocene, as testified by paleomagnetic investigations the SE caused a fragmentation toward 2007). The movement 2007a; Mattei et al., 2003; Cifelli et al., et al., of which controlled the development shear zones, of the arc in individual blocks bounded by NW-trending 1991; Lentini et al., sides of Calabria (Knott & Turco, basins located along both the Ionian and Tyrrhenian and northern parts of the in the central movement by left-lateral are characterized 1995). These shear zones 2007; et al., Dijk, 1991, 1994; Tansi 1991; Van in the south (Knott & Turco, movement arc, and right-lateral is shear zone 2013). The northernmost NW-trending et al., 2012; Tripodi et al., 2008; Turco Del Ben et al., produced by continental oblique collisional processes, line, the major shear zone represented by the Pollino the Calabrian Arc from southern Apenninesseparating (Fig. 2). a thick and wide accretionary wedge composed of The offshore external region of the Calabrian Arc displays sediments belonging to the African plate, that shapes with a rugged and Cenozoic deformed Mesozoic by the sea-floor of Ionian Sea from Malta to Apulia escarpments, and is characterized topography 2011). The Messinian salinity crisis is inferred to have et al., front in the Ionian abyssal plain (Polonia an active up onto the Messinian salt deposits, of the wedge, as basal decollement ramps influenced the evolution of the frontal thrust and consequent underplating crustal progradation producing a fast forward ionian sequence during trench rollback (Minelli & 2010). Faccenna, polymetamorphic nappes comprising large sheets of an Hercynian crystalline basement (forming the Sila and succession, considered by some authors to Cenozoic Aspromonte Massifs) and local remnants of a Mesozoic sedimentary sequence of the upon the Triassic-Miocene of the Alpine belt overthrusted as a fragment 1976). Apennine-Maghrebian Chain during Miocene (Amodio Morelli et al., in response to the subduction of from mid-Miocene onwards south-eastward The Calabrian Arc migrated & (Malinverno Benioff zone W-dipping Ionian oceanic lithosphere along a deep and narrow, 1986; Ryan, 2005a). The diachronous 2001, 2004; Sartori, 2003; Finetti et al., et al., 2001; Faccenna Bonardi et al., block collision between the Apennine-Maghrebian Chain and Apulian foreland to north, Pelagian of propagation the thrust front ( to the south, coupled with a different velocity geological field trips 2015 - 7(2.2) excursion notes 12 an margin Fig. 2 - Geological sketch-map of the central Fig. 2 - Geological sketch-map and Van Dijk et al., 2000, modified). Dijk et al., and Van Mediterranean area, with geological section on bottom Mediterranean Dijk & Scheepers, 1995 2007; after Van et al., (Tansi The modern physiography and geology of The modern physiography Calabria are the result of Miocene geodynamic processes in which synchronous accretionary along the eastern flank processes were active (northern Ionian Sea), and rifting processes along the western flank (Eastern Tyrrhenian thrusts (i.e. with margin). Double verging coherent and opposite to the vergence been documented accretionary wedge) have 1992, et al., (Roveri in the Ionian off-shore 2000). Dijk et al., 1999; Van Doglioni et al., similar structures are not clearly However, on- constrained described and structurally and structural land. The on-shore stratigraphic the geometries and research better constrain timing of deformation in the wedge-top basin. The modern setting includes two different styles of basins: A) the Corigliano basin, on the Ionian side, is a wedge-top depozone, of the Calabrian thrust-sheets located above B) the Arc and southern Apennines terranes; side, is a slope basin, on the Tyrrhenian Paola basin located on the eastern margin of Tyrrhenian back-arc Basin (Critelli, 1999). F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 geological field trips 2015 - 7(2.2) excursion notes 13 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 The tectono-sedimentary evolution of the basin successions cropping out along northeastern Calabrian margin The tectono-sedimentary evolution 2011). Middle Miocene (Critelli, 1999; Critelli et al., describing timing, style and tectonic evolution investigated, was of the calabrian foreland basin system, partitioned in deposits accumulated in a longitudinal wedge-top depozone Cirò and Crotone depocentres: Rossano, three distinctive basins. In the ionian side of Calabrian Arc (Amodio cover Mesozoic alpine units and their relative Paleozoic Neogene and Quaternary basin successions overlie 1976). The Late Oligocene-Lower MioceneMorelli et al., 2005) unconformably formation (Bonardi et al., formation rocks and crops out along the eastern sector of northern Calabria. The Paludi pre-Tertiary overlies to reddish and green marls siltstones with interbedded and breccias evolving consists of alluvial conglomerates On top of both crystalline rocks calcarenites, turbiditic sandstones and silty marls with vulcanoclastic levels. graded to Pliocene terrigenous and carbonate sequences constitute the infilling of and Oligocene flysch, a Serravallian Calabrian foreland, which can be subdivided in three main depozones. thrust-controlled The Amantea 1974; Colella, 1995) is one of the main Neogene basins et al., basin (Di Nocera along the margin of Calabria. The onset the basin occurred in response to tectonic subsidence related Tyrrhenian 2001; Muto & et al., (Critelli, 1999; Rossetti Tortonian extensional faulting during the Serravallian-Early Perri, main depositional units, bounded by stratigraphic 2002). The sedimentary infill has been subdivided into five 2002; Muto &discontinuities (Colella, 1995; Mattei et al., 2002), Perri, underlying sediments and bedrock. marine Middle Pliocene to Pleistocene deposits, made of thick conglomerate-sand-sandstone-clay successions, represent the basin-fill deposits of main tectonic depressions (Crati basin, Catanzaro trough). 2007b; (Lanzafame & graben 2005, 2007; Cifelli et al., The Crati et al., 1981; Tansi 1981; Tortorici, Tortorici, quaternary faults, which trending transtensional by N-S 2011) is characterized 2010; Spina et al., et al., Pepe in rocks of the Calabrian Terranes and Mesozoic Late Miocene-Quaternary deposits from the Paleozoic separate on its western and eastern margins, respectively. the Coastal Chain and in Sila Massif, of the Crotone stratigraphy The Serravallian-Tortonian basin is similar to that of the Rossano basin, at least until In the Crotone Formation. deposition of the Tripoli by clastic successions is overlain Formation basin, the Tripoli to gypsrudites–gypsarenites and gypsum-bearing sandstones consisting of limestone breccias grading blocks of by deposits consisting of meter-scale inferiore unit”). These successions are overlain (“evaporitica limestone, gypsarenite breccias, and slumps (“detritico-salina unit”) (Roda, 1964). In this basin, halite places and show evidence for diapiric emplacement local salt tectonics. An deposits crop out in several superiore (“evaporitica Upper Messinian succession consisting of shale, sandstone, and minor gypsarenite levels geological field trips 2015 - 7(2.2) excursion notes 14 an margin includes two thinning and fining upward units, includes two thinning and fining upward F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri auct. Ogniben, 1969) have been observed along the Ionian been observed Ogniben, 1969) have , overthrusted on the Upper Tortonian-Messinian sequences on the Upper Tortonian-Messinian , overthrusted sensu Ogniben, 1969) have been observed within Late Miocene been observed Ogniben, 1969) have auct. sensu , Pescatore & Senatore, 1986; Romagnoli & Gabbianelli, 1990). & Senatore, 1986; Romagnoli , Pescatore e.g. A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 (Muto et al., 2009; Tripodi et al., 2009, 2011). The succession was involved in oblique back thrusting related to involved 2009, 2011). The succession was et al., 2009; Tripodi (Muto et al., The “Cariati Nappe” regional oblique tectonic arrangement. 1992; et al., 1967; Roveri formation (Roda, of the Paludi the Oligocene siliciclastic strata unconformably covering and sandstones recording 2011). The succession starts with conglomerates 2000; Critelli et al., Dijk et al., Van striking shear fluvial and deltaic facies associations, passing to prodelta turbiditic bodies. The NW-SE braided highs and wedge-top partitioning during the Neogene (Van structural of intrabasinal led to the configuration zone 2008). 2000; Barone et al., Dijk et al., faults and associate thrust characterise A complex network of strike-slip the entire Ionian side of northern Calabria. rocks composed of variegated of sicilide-derived Huge volumes been emplaced matrix and large blocks of limestone sandstones have clay during Late Tortonian-Early thrusts, or to the thrust Messinian. The latter bodies can be related to the accommodation due out-of-sequence Throughout along the Ionian side of northern Calabria, bodies propagation of the “Sicilide Complex”. Complex” (“Anti-Sicilide clays varicoloured unit”) with a “Lago-Mare” fauna onlaps the detritico-salina unit at the top. An erosional surface marks the unit”) with a “Lago-Mare” fauna onlaps the detritico-salina unit at top. deltaic sand lobes and fluvial boundary between these uppermost Messinian deposits from the overlying unit. The sedimentary succession of the Crotone and Rossano conglomerate of the Carvane conglomerates basins to of Serravallian bounded by unconformities, a first cycle can be subdivided into two main sedimentary cycles are 2008). These cycles of Early to Late Messinian age (Barone et al., Early Messinian age and a second cycle capped in the Crotone marl unit and a thick Pliocene- deposits of the Cavalieri outer-shelf basin by transgressive area (Cirò et al. 2004a, 2012). In the central 1999; Zecchin Quaternary succession (Massari et al., basin) a thick siliciclastic succession, known as “Cariati Nappe” deposits. Varicoloured clays (“Anti-Sicilide Complex” (“Anti-Sicilide clays deposits. Varicoloured coast of the northern Calabria and are associated with basement slices composed black slates limestone internally with respect to the accretionary Basin develops 2000). The Ionian fore-arc Dijk et al., breccias (Van &wedge since Late Oligocene along the Ionian side of Calabrian arc (Cavazza DeCelles, 1993; Bonardi et al., &2001; Cavazza uplifted and cropping-out along the Barone, 2010). It is composed of some parts nowadays basin). The area (the Crotone-Spartivento Ionian coast, such as the Crotone basin, and of a main active offsets the accrectionary front of chain and fault zone activity of the transversal neotectonic transcurrent (Amendolara, zone depressions in on-shore and off-shore pull-apart high separating structural provides Cariati, Cirò Ridges) ( Rossano, geological field trips 2015 - 7(2.2) excursion notes 15 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 Since Middle Pleistocene, the Calabrian Arc experienced a rapid uplift up to ca. 1Since Middle Pleistocene, the Calabrian Arc experienced a rapid 1993) mm/yr (Westaway, along the coast. Some hypotheses flights developed as documented by marine terrace that persists today, been proposed to explain this uplift, such as an isostatic rebound that follows the breaking of have removal & Spakman, 2000) or a convective 1993; Wortel subducted Ionian crust (Spakman, 1986; Westaway, of the deep root and consequent decoupling arc from subducting plate (Doglioni, 1991; Gvirtzman & & 2001; D’Agostino Nur, locally accommodated by repeated displacement 2004). The uplift was Selvaggi, faults (Monaco &along the major active 2003). Pulsating tectonics and recent 2000; Catalano et al., Tortorici, 2009. et al., tectonics is documented on the eastern calabrian margin by Ferranti transpressional and active called shear zones, left-lateral The Crotone basin is bounded to the north and south by two NW-trending Dijk, 1990, 1991, 1986; Van (Meulenkamp et al., fault respectively Nicola fault and Petilia-Sosti Rossano-San Dijk &1994; Van basin by some thrust from the Crotone-Spartivento 1991), and is currently separated Okkes, fronts (Fig. 2). The Crotone 1964; Van time (Roda, and Tortonian basin began to open between Serravallian by a dominant extensional tectonic regime that was characterized Dijk, 1990), and its tectonic history was phases in middle Messinian, Middle short compressional or transpressional interrupted periodically by relatively 2004a, 2012; et al., Dijk, 1990, 1991; Zecchin Pliocene and Middle Pleistocene times (Van Massari et al., uplift led to 2010). Since Middle Pleistocene, a main shift from dominant subsiding conditions to generalized 2012). Tectonic 2004b, et al., 1989; Zecchin the emergence of basin (Gliozzi, 1987; Cosentino et al., south- structures strongly controlled the geometry of Neogene basin as consequence progressive shifting of the Calabrian Arc. eastwards geological field trips 2015 - 7(2.2) itinerary 16 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri Day 1 The Cirò and Crotone basins A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 The San Nicola dell'Alto formation (Ogniben, 1955; Roda, 1964) and the Clypeaster sandstone formation formation (Ogniben, 1955; Roda, The San Nicola dell'Alto Calabrian thrust belt. These (Cotecchia, 1963) represent the onset of foreland basin system on advancing et al., sedimentary facies associations, representing a depositional sequence (Roveri include several strata trend, in fining and thinning upward an overall 1992), and they are interpreted as a turbiditic system, having 1992). et al., 1000 m; Roveri the Crotone basin (with a thickness over 1992). In the other et al., area (Roveri of dry gas in the off-shore The formations constitute the main reservoir deposits (alluvial fans), nearshore and shallow-water include also continental strata areas, these strata turbiditic systems and by shelfal by fine-grained are overlain (between and Campana). These strata formation correspond to the Ponda These strata the thrust culminations of Sila Massif. deposits toward basin, 1964) of the Crotone basin, or Argilloso-Marnosa formation (Ogniben, 1955) Rossano (Roda, 1992). During late Tortonian-early et al., (Roveri systems tract represents deposition during low-stand and may olistostroma of sicilide-derived huge volumes abruptly received wedge-top depozone Messinian, the Rossano matrix and large blocks clay "Argille Scagliose formation" (Ogniben, 1955, 1962) composed by variegated (similar to the Albanella-Colle Cappella (olistholiths) of Cretaceous-Oligocene limestone, Miocene quartzolithic be related to an out flow deposits may sandstones (Numidian sands). These gravity sandstones) and quartzose formation has similar of the sicilide unit. The Castelvetere of sequence thrust accommodation or to a back-thrust 1995b). (Critelli & Le Pera, within the foredeep depozone olistostrome layers 1967a; Ogniben, 1973), rests tectonically on the a sedimentary allochthonus succession (Roda, The “Cariati Nappe”, (to the north) and Crotone south) basins. This succession is made up of turbiditic successions of the Rossano in backthrust starting from Late Tortonian age, involved trend of Langhian-Serravallian bodies with thinning-upward basin (Figs. 3, 4, 5). The “Cariati Nappe” units in the Rossano and post evaporitic the evaporitic and involving an Oligocene to Burdigalian siliciclastic includes a Middle to Upper Miocene clastic succession unconformably covering continuity in the flysch. The Miocene and post Messinian emplacement of the “Cariati Nappe” interrupts lateral sector of the area and affects sedimentary supply a such configured wedge-top basin. The Messinian central salinity crisis. The evaporites deposits which records the Mediterranean by evaporite sequence is characterized geological field trips 2015 - 7(2.2) itinerary 17 an margin sequence (Roveri et al., 1992). This et al., sequence (Roveri unconformity overlying the evaporite unconformity overlying depositional sequence consists of a basal is well cropping out, and an outer external juxtaposition of basinal successions (Rossano and Crotone successions) (Rossano 1964) (Roveri et al., 1992). The et al., 1964) (Roveri the Cariati nappe would suggest basin set on sicilidi units and conglomerate and sandstone strata with and sandstone strata conglomerate argillose dei Cavalieri formation; Roda, argillose dei Cavalieri Calabrian Arc units which the western edge Crotone basin, is marked by an erosional Crotone basin, is marked fining-upward trend (transgressive systems trend (transgressive fining-upward shales (highstand systems tract; marne shales (highstand systems tract; tract; Carvane conglomerate formation; conglomerate Carvane tract; Roda, 1964), overlain by basin-wide marine by basin-wide 1964), overlain Roda, detection, during the Serravallian-Tortonian, of detection, during the Serravallian-Tortonian, contest; a basin on the inner set of Fig. 3 - Stratigraphic columnar sections of the Fig. 3 - Stratigraphic the sedimentary basins developed in different the sedimentary basins developed Rossano and Crotone basin fill, after Barone et al., 2008. and Crotone basin fill, after Barone et al., Rossano formation. Therefore, the Cariati nappe would to Pliocene depositional sequence within the F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri Nocera et al., 1974). The base of the late Messinian et al., Nocera beds (Ogniben, 1955; Roda, 1964; Romeo, 1967; Di 1964; Romeo, beds (Ogniben, 1955; Roda, thin mudstone interval, and thin clastic evaporite thin mudstone interval, mainly consist of gypsum and halite, followed by a A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 geological field trips 2015 - 7(2.2) itinerary 18 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri Fig. 4 - Stratigraphic columns of the “Cariati Nappe” and comparison three basin Fig. 4 - Stratigraphic successions (from Muto et al., 2009; Muto et al., 2013). 2009; Muto et al., successions (from Muto et al., A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 geological field trips 2015 - 7(2.2) itinerary 19 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri Fig. 5 – with relative et al., 2013). et al., sections (from geological cross Arso rivers area Arso rivers Muto et al., 2009 Muto et al., maps of the Nicà- the Cirò basin and detailed geological modified and Muto Geolocical maps of A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 geological field trips 2015 - 7(2.2) itinerary 20 Fig. 6 – an margin Geological al., 2013). al., et al., 2011 et al., section E-E’ and Muto et of the fig. 5, (from Tripodi F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 give the meaning of a backthrust of Tortonian age, related to the upper-middle Miocene accretionary phases age, related to the upper-middle the meaning of a backthrust Tortonian give Because that sharing the foreland basin system of intersection southern Apennines-Calabrian terrane. similarities with the tectonostratigraphic of its sedimentary succession, the Cariati nappe would include many sedimentary successions of the upper Ionian Calabria and Lucania, which identify area & Imperiale ridge (Zuppetta et alii, 1984; Mostardini & Merlini, 1986; Patacca --Rocca 2011), Scandone, 1987, 2001; Carbone & Lentini, 1990; Cinque et alii, 1993; Critelli, 1999; Critelli al., where on the successions of Albidona formation and hight portion sicilidi units, rest formation and and arenaceous turbiditic deposits belonging to Serravallian-Tortonian conglomeratic formation. conglomerates Nocara a regional scale, major tectonic structures At of the main and the evolution control the configuration 1991). The NW- basins in the northern Calabrian Arc (Knott & Turco 2000) is a zone Dijk et al., (Van Nicola fault zone SE striking Rossano-S. affects Neogene- of deformation exposed along the Ionian side northern Calabria. This fault zone Quaternary deposits belonging to the Calabrian foreland basin system and controlled, in a sector of fault features of the Plio-Quaternary Crotone basin, to south. Transpressional releasing bend, the configuration faults and offset the Miocene fault- strike-slip partitioning along left lateral formed as result of strain high is represented by the Cariati nappe. propagation-folds. The main onland transpressional structure made up of allochthonous siliciclastic successions is represented by the Cariati nappe. It A positive an Oligocene to Burdigalian includes a Middle to Upper Miocene clastic succession unconformably covering and sandstones units made of conglomerates siliciclastic flysch. It shows two thinning and fining-upward to prodelta turbiditic bodies. The nappe fluvial and deltaic facies associations, evolving showing braided geological field trips 2015 - 7(2.2) itinerary 21 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 overthrust Tortonian and Early Messinian sequences in the Cirò basin. The progressive growth of these and Early Messinian sequences in the Cirò basin. The progressive Tortonian overthrust structures compartmentalised the formerly continuous basin, leading to formation of distinct compressive and asymmetric depocentres during Messinian Pliocene. The Miocene post emplacement of continuity and affects the sector of the study area interrupts lateral the “Cariati Nappe” in central sedimentary supply of a such configured foreland basin. The Cirò basin, located in an intermediate position Dijk & Scheppers, (Van and Crotone basins, is missing by the Messinian evaporites between the Rossano wrenched in sub-basins recording a 1995). This suggests that a larger and previously continuous basin was an allochthonous series (Cotecchia, interpreted like 2008). This succession was tectonic history (Barone et al., data show 1967). Structural (post Messinian) terrigenous sediments (Roda, on post evaporitic 1963) staying striking, bends of the NW-SE structure formed along restraining that the “Cariati Nappe” is a transpressive (Stop 1.1). This structure represents the distal sediments of Nicola fault zone Rossano-S. left-lateral, bedrock (“Sicilide Complex”). Along the outer front of Miocene basin infill, together with its back-thrust produced regional wrenching of the Miocene basins and regional fault zones, northern Calabria, strike-slip the “Cariati Nappe”) related to backthrust and highs (like structural of intrabasinal controlled the development in some sectors. The “Cariati Nappe” can be considered as exposed analogue of producing tectonic inversion highs, it is pointed out that at the scale of whole basin, major compressional structural the off-shore structures are time dependent, as they Middle Miocene in age within the Crotone basin (see Luna Field), 2013). The tectono-sedimentary date latest Miocene within the Cirò basin (Muto et al., and they likely affected by of the inner portions late Miocene southern Italy foreland-basin system was evolution uplift of mid-crustal blocks, and the tectonic partitioning due to continuation of accretionary processes, rapid 2014). superposition of oblique tectonics (Muto et. al., STOP 1.1: Mandatoriccio (CS). Thrust between the “Cariati Nappe” and marginal Serravallian- Messinian successions. view successions. The general outline of the relationships between two stratigraphic This Stop is the first general from W to E. Are cropping out the, on the right of figure, gently is introduced from the village of Mandatoriccio, directy onlapping the Sila basement. These form a steep monoclinal strata, est dipping Serravallian-Messinian the hanging-wall interrupted, to the est, by a thrust surface. The tectonic contact separates flexure zone succession of the (Oligocene-Middle Miocene Cariati Nappe succession, Fig. 4) from the Serravallian-Messinian geological field trips 2015 - 7(2.2) itinerary 22 village. an margin from Scala Coeli (CS) Fig. 8 - Panoramic view, Fig. 8 - Panoramic F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri this stop is possible to observe the progressive transition from an oblique thrust, left- transition the progressive this stop is possible to observe A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni Fig. 7 - General view, from the Mandatoriccio (CS) village, of relations between “Cariati Nappe” deposits and view, Fig. 7 - General Serravallian-Messinian successions (modified from Muto et al., 2009). successions (modified from Muto et al., Serravallian-Messinian DOI: 10.3301/GFT.2015.04 Cirò basin (Fig. 4, 5). In STOP 1.2: Scala Coeli (CS). The allochthonous Oligocene-Middle Miocene succession. Cirò basin succession and of the and tectonic relations between the Serravallian-Messinian View of stratigraphic thrust contact is well exposed. In the area comprised between Cariati nappe. In this Stop the transpressive and Scala Coeli (Fig. 9A), the tectonic contact is made up of high angle faults 9B) villages of block) from the Cariati nappe and Cirò basins (footwall the successions of Rossano that displace and separate lateral component of motion, on the right of figure 7, to the N-S trending frontal thrust ramp, on the left of Fig. 7. trending frontal thrust ramp, component of motion, on the right figure 7, to N-S lateral assemblage of eastern basin infill and the major backthrust in onland is outlined from Stop 1.1. General geological field trips 2015 - 7(2.2) itinerary 23 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri Particular of the transpressive strike slip fault bordering the main contact (modified from Muto et al., 2014). slip fault bordering the main contact (modified from Muto et al., strike of the transpressive Particular B) Line drawing showing stratigraphic and tectonic relations between the Cirò basin succession “Cariati Nappe” showing stratigraphic Line drawing A) A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni Fig. 9 - dell’Avvoltoio. dell’Avvoltoio. strata; in the hanging-wall, unconformity between Burdigalian flysch and Langhian conglomerates cropping out in the Timpa unconformity between Burdigalian flysch and Langhian conglomerates in the hanging-wall, strata; DOI: 10.3301/GFT.2015.04 succession (hanging-wall block). The tectonic contact between the two succession consists in subvertical faults block). The tectonic contact between the two succession consists in subvertical succession (hanging-wall displacement (Fig. 9B). kinematics with a component of vertical strike-slip left lateral exhibiting prevalent with an evident angular Oligocene-Burdigalian flysch, correlated to the Albidona formation, is overlain (Fig. 9A). conglomerates unconformity by the Langhian Timpa dell’Avvoltoio STOP 1.3: Geometry and kinematics of NW oriented transpressive fault faults (Figs transpressive compatibility between the NW-SE In this Stop is possible to understand the structural of the “Cariati Nappe” (Fig. 10A). The fault is characterized oblique thrust ramp 10B and C) the NNW-SSE component of slip. with significant reverse movement by left-lateral along of the Cariati nappe strata conglomerates steepening of the Langhian-Serravallian In the hanging-wall, anticline related to an E-dipping belong to the forelimb of a west verging the major tectonic contact. Strata (Fig. 10A). Formation and the Tripoli clayes plane and are thrust on the Upper Tortonian geological field trips 2015 - 7(2.2) itinerary 24 an margin kinematic indicators C) Vertical Langhian conglomerates Vertical A) F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri Particular of the transpressive fault zone and fault zone of the transpressive Particular B) A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni Fig. 10 - Particular of geometry and kinematics of the transpressive fault zone. fault zone. of geometry and kinematics the transpressive Fig. 10 - Particular on the fault plane. on the fault plane. overthrust on the upper Tortonian clayes and Tripoli. and Tripoli. clayes on the upper Tortonian overthrust DOI: 10.3301/GFT.2015.04 The Plio-Pleistocene succession of the Crotone basin (Stops 1.4, 1.5, 1.6) Cavalieri marl and clay These deep-marine units form an apparently continuous Plio-Pleistocene succession up to 1200 m thick in the coastal and locally continental deposits are and southern part of the basin, whereas shallow-marine, central the basin margin (Fig. 11). Despite this apparent commonly interposed between the two units toward by an unconformity that is well seismic data show that the two formations are separated continuity, geological field trips 2015 - 7(2.2) itinerary 25 an margin Fig. 11 – Stratigraphic column of the Crotone basin (modified from et al., Zecchin 2012). F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 recognizable at outcrop near the basin margin, where a few hundreds thickness of both units does not exceed of meters. both consist of gray marl and the Cutro clay The Cavalieri and siltstones and light brown monotonous claystones calcareous nannofossils and mollusc rich in foraminifera, shells, accumulated at distal shelf to slope depth (Roda, 2003, 2004a, 2012; Massari et al., et al., 1964; Zecchin Well 2010), which occasionally exhibit faint stratification. and outcrop data document that the formations contain interpreted as turbidites, which exhibit an sand layers distribution. vertical erratic marl crops In the northern part of basin, Cavalieri out north of the Murgie mountain and between Zinga di Spinello villages, and its base coincides and Belvedere with a sharp boundary at the top of Messinian in age continental deposits. The formation is Zanclean 2003, et al., Dijk, 1990; Zecchin 1964; Van (Roda, marl interfingers 2004a, 2012) (Fig. 11). The Cavalieri by the with the Zinga sandstone and is overlain formation and the Murgie sandstone (see Belvedere facies relationships between the below) (Fig. 11). Lateral marl and Murgie formations the Cavalieri Belvedere are not visible at outcrop. 1964) is exposed discontinuously (Roda, The Cutro clay between in the whole basin, and its age ranges 2012) (Fig. 11). As et al., Piacenzian and Ionian (Zecchin at outcrop the contact with mentioned above, marl is undetectable in the distal underlying Cavalieri geological field trips 2015 - 7(2.2) itinerary 26 an margin Zecchin, 2007a). The boundary Zecchin, sensu F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri (Zecchin et al., 2004a, 2012). The unit pinches-out to the SE et al., (Zecchin Cerastoderma edule A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 area, whereas it is marked by a coarse-grained lag and local fluvial sedimentation in the area. The by a coarse-grained area, whereas it is marked interfingers with the sandstone in northern part of basin. Higher succession, Cutro clay and into the San Mauro formation north of the Neto river, Mulara the unit passes abruptly into Serra sandstone to the west (Fig. 11). Zinga sandstone corner of the basin, and is The Zinga sandstone, up to 300 m thick, is recognizable in the north-western and locally wedge formed by shoreface to deltaic deposits, overlying interpreted as a composite prograding 2003, 2004a) (Fig. 11). The unit rapidly et al., marl (Zecchin interfingering with the upper part of Cavalieri ( small-scale cycles and is composed of seven pinches-out basinwards with the overlying Montagnola clay is very sharp and locally marked by thin fluvial and tidally-influenced fluvial by thin fluvial and tidally-influenced sharp and locally marked is very Montagnola clay with the overlying 2004a). The accumulation of the Zinga sandstone is interpreted as result et al., deposits (Zecchin decreasing accommodation and forced regression due to local uplift aided by halokinesis, possibly coupled with 2003, 2004a, 2012). The formation is inferred to be et al., tectonics (Zecchin eustasy and/or larger-scale 2003, 2004a, 2012). et al., in age (Zecchin Zanclean Montagnola clay the Zinga sandstone up to 100 m thick, is a lagoonal unit that overlies Montagnola clay, The inferred Zanclean and siltstones containing an oligotypic fauna and brown claystones gray (Fig. 11), and consists of stratified, assemblage dominated by formation. Belvedere and is erosionally truncated by the overlying Belvedere formation corner of the basin, between age crops out along the north-western This unit of inferred Zanclean di Spinello and San di Spinello villages, and in the western part, between Belvedere Casabona and Belvedere et al., between 50 and 450 m due to synsedimentary normal faulting (Zecchin Its thickness varies Mauro. bioclastic and siliciclastic formation is composed of well cemented, mixed 2004a, 2006). The Belvedere 2004a; et al., (Zecchin stacked that are vertically cycles to form meter-scale shoreface deposits organized component is a typical feature of the formation (Zecchin, 2005) (Fig. 11). Such an aggradational Zecchin, either by an up angular unconformity is recognizable, and it overlain 2007b). A prominent intra-formational geological field trips 2015 - 7(2.2) itinerary 27 an margin , very similar to that , very Cerastoderma edule F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 to 100 m thick succession containing sand waves in its lower half or by lagoonal deposits up to 25 m thick. to 100 m thick succession containing sand waves The upper boundary of the formation corresponds to one most important unconformities found in 2012). et al., Crotone basin fill (Zecchin Murgie sandstone This unit, up to 300 m thick, is present in the northern part of basin, near Strongoli village, and 2006) (Fig. 11). An intra- et al., (Zecchin mostly composed of shoreface sandstones and conglomerates by cemented shell beds. The formational angular unconformity found in the upper part of unit is overlain component aggradational The unit exhibits a marked upper boundary corresponds to a major unconformity. 2006). Such a fault et al., due to the activity of a listric normal fault that controlled deposition (Zecchin unconformity marl. The recognition of the intra-formational contact with the Cavalieri places the unit in lateral to the equivalent and of the top unconformity suggests that Murgie Sandstone is at least in part lateral formation (Fig. 11), whereas its lower part possibly correlates with the Montagnola and Zinga Belvedere deposits, is by ca. 20 m thick fluvial, coastal and shallow-marine overlain formations. Another unconformity, 2006). et al., present to the east in uppermost part of formation (Zecchin Spartizzo clay 2005) is exposed between the 1964; Mellere et al., (Ogniben, 1955; Roda, clay The lagoonal Spartizzo from ca di Spinello villages in the northern part of basin, and its thickness varies Casabona and Belvedere and brown layered 10 to 150 m due synsedimentary normal faulting. This unit is composed of dark gray mudstone containing an oligotypic fauna assemblage dominated by characterizing the Montagnola clay. The Spartizzo clay sharply overlies the Belvedere formation and the Belvedere sharply overlies clay The Spartizzo the Montagnola clay. characterizing deposits of the Scandale sandstone, and it is inferred as with the shallow-marine interfingers laterally 2012) (Fig. 11). et al., 2005; Zecchin Piacenzian in age (Mellere et al., Scandale sandstone 2006) is found in the et al., 2005; Zecchin 1964; Mellere et al., The Scandale sandstone (Ogniben, 1955; Roda, depending on the location. northern and western parts of the basin shows a complex architecture that varies 2012). et al., di Neto (Zecchin Casabona, Strongoli and Rocca three members were recognized: Overall, geological field trips 2015 - 7(2.2) itinerary 28 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 Casabona member: the member represents lower part of Scandale sandstone, and consists wedges that interfinger with the prograding forming decameter-scale shoreface sandstones and conglomerates, 2005) (Fig. 11). The 1965; Mellere et al., di Neto and Casabona areas (Roda, in the Rocca clay Spartizzo of shelf siltstones that interval to decameter-scale by a meter- uppermost shoreface tongue is sharply overlain and the Casabona member of Scandale clay The Spartizzo part of the Cutro clay. represent the proximal between 30 and 180 m due to sandstone, therefore, form together a package showing thickness that varies that testify to a deepening- cycles transgressive-regressive synsedimentary tectonics, which is composed of five 2006, 2012). Although et al., 2005; Zecchin trend during middle to late Piacenzian time (Mellere et al., upward 2005). package is found also north of the Zinga village (Mellere et al., the same deepening-upward thinner, formerly referred to as the Strongoli sandstone Strongoli member: the member or tongue was 2006) oriented et al., (Ogniben, 1955), consisting of a discontinuous shoreface to inner shelf belt (Capraro in the area of Strongoli village. This unit, early Gelasian age to the SSE and prograding ENE-WSW 2012) (Fig. 11), is up to 60 m thick and pinches-out distally within the et al., 2006; Zecchin et al., (Capraro Cutro clay. locality only, di Neto member is found at the homonymous di Neto member: The late Gelasian Rocca Rocca shoreface tongues interfingering with distal shelf to slope to decameter-scale and consists of meter- mudstones and documenting a local alternation between the uppermost Scandale sandstone Cutro 2012) (Fig. 11). et al., (Zecchin clay Serra Mulara formation to sandy and mudstone body elongated for ca. 4 km the south-east, This unit consists of a conglomerate erosional surface delta. The lower boundary is represented by a broad concave-up lying west of the Neto river by fluvial deposits. The The upper boundary consists of an erosional surface overlain cutting the Cutro clay. to trend, with a reversal fining-upward formation is 178 m thick and exhibits an overall Mulara Serra fill (Fig. 11) composed of density-flow in the upper 15 m. The unit represents a canyon coarsening-upward glacio- 2011). These deposits record both high-amplitude et al., deposits and minor hemipelagites (Zecchin 2011, 2012). et al., eustatic changes and the onset of uplift this part Calabrian Arc (Zecchin geological field trips 2015 - 7(2.2) itinerary 29 an margin Fig. 12 - The Casabona horst and the thick succession. South Casabona half-graben. The deposi- South Casabona half-graben. (middle Pliocene) clay tion of the Spartizzo controlled by the activity of fault was bounding the south Casabona half-graben, the accumulation of a relatively favouring South of Casabona and Montagna Piana, NE-trending synsedimentary normal faults bound the South Casabona and sub-basins during half-graben Zoiaretto clay deposition of the lagoonal Spartizzo Scandale and of the shallow-marine sandstone (Fig. 12), which are F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 San Mauro sandstone (1964) and The San Mauro sandstone is found only in the western part of basin, as documented by Roda (Fig. 11), the Cutro clay Massari et al. (2002, 2010). The unit, up to ca. 200 m thick, conformably overlies cycles in transgressive-regressive shoreface, lagoonal and fluvial deposits organized and consists of shelf, 2002, 2010). tectonics (Massari et al., recording both glacio-eustasy and synsedimentary transtensional STOP 1.4: The Pliocene south of Casabona. of the uppermost lower Pliocene and late basin fill south Casabona. Observation can be observed formation accumulated within the Montagna Piana half-graben succession of the Belvedere The cyclic formation is characterized from the Stop (Fig. 12). An angular unconformity is found within unit. The Belvedere of accommodation due to a long-term balance between the rate stacking pattern of minor cycles by an aggradational The formation is topped by a major unconformity of basinal scale that the creation and that of sediment supply. and the early Piacenzian. response of an important tectonic phase occurred between the late Zanclean geological field trips 2015 - 7(2.2) itinerary 30 an margin Fig. 13 - Correlation of sections measu- Mellere et al., 2005). Mellere et al., red on the middle Pliocene deposits located east of Casabona. The succession is compo- the Scandale san- clay, sed of the Spartizzo dstone, and the lower part of Cutro clay. The succession deposited within the South sub- half-graben Casabona and Zoiaretto basins is subdivided into six high-frequency sequences. The fault that bound the Zoiaretto ceased the activity during half-graben (modified from deposition of the last cycle F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 accumulated after renewed subsiding conditions that followed the middle Pliocene tectonic phase. The lower part and representing the of this succession consists a backstepping wedge showing high-frequency cyclicity of the Piacenzian (Fig. 13). The upper part Scandale sandstone represents a forced interval transgressive during Gelasian time (Fig. 13). by the deep-marine Cutro clay deposit, transgressed regressive in correspondence of part the former Montagna Piana half- The Casabona horst, to the north, is developed during the Piacenzian normal faulting (Fig. 12). graben geological field trips 2015 - 7(2.2) itinerary 31 ing en was an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni Fig. 14 - The western side of the Vitravo Valley. Note (right) the prograding forced-regressive wedges of the Zinga sandstone. forced-regressive Note (right) the prograding Valley. Fig. 14 - The western side of the Vitravo linked to the activity of a NE-trending listric normal growth fault (modified from Zecchin et al., 2004). et al., to the activity of a NE-trending listric normal growth fault (modified from Zecchin linked deposition of the Montagnola clay. Deposition of the thick succession of the Belvedere formation within the Belvedere half-grab formation within the Belvedere Deposition of the thick succession Belvedere deposition of the Montagnola clay. The geometry was controlled by the growth of a NE-trending non-cylindrical anticline (Russomanno anticline), that continued dur controlled by the growth of a NE-trending non-cylindrical anticline (Russomanno The geometry was DOI: 10.3301/GFT.2015.04 STOP 1.5: Zinga (KR). Timpa di Cassiano and the western side of Vitrano Valley. of the Lower Pliocene succession western side observation and panoramic Crotone basin overview Valley. Vitravo This Stop offers a spectacular view of the Lower Pliocene succession (Fig. 14). The slope to shelf mudstones shoreface sandy wedges of the Zinga sandstone, which into the prograding marl merge upward of the Cavalieri wedges was The deposition of the prograding is about 300 m thick (Fig. 14). The wedges pinch-out southward. anticline), probably associated with salt controlled by the growth of a NE-trending anticline (the Russomanno anticline (about 250 m) marl at the Russomanno tectonics (Fig. 14). The great thickness of the Cavalieri during the deposition of Zinga sandstone, and continued suggests that the growth started later, deposition of the lagoonal Montagnola clay. geological field trips 2015 - 7(2.2) itinerary 32 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 The top of the Zinga sandstone is a subaerial unconformity locally marked by thin fluvial and tidally-influenced The top of the Zinga sandstone is a subaerial unconformity locally marked (about 100 m thick), which in turn is sharply into the Montagnola clay fluvial deposits, passing upward formation (Fig. 14). The latter shows a strong deposits of the Belvedere by the shallow-marine overlained thickness in the southern part (roughly up to 450 m SW of Timpa di Cassiano mountain), due activity (Fig. 14). half-graben of a NE-trending synsedimentary listric normal fault bounding the Belvedere during the active Timpa di Cassiano is bounded in the south by another NE-trending normal fault that was units (Fig. 14). deposition of younger STOP 1.6: The Serra Mulara formation. fill. submarine canyon of a coarse-grained Observation formation) crops out in the Mulara fill succession (the Serra canyon A middle Pleistocene coarse-grained the opportunity to study a northern sector of the Crotone basin (Figs 15 and 16). This succession provides elongated body (4.25 km fill, which consists of a NW-SE submarine canyon field example of coarse-grained and silty succession located behind clayey confined by a deep-water long and up to 1.5 km wide) laterally the modern Neto delta (north of Crotone) (Figs 15 and 16). The thickness unit reaches 178 meters. deposits containing abundant to sandy density-flow fill is dominated by gravely The lower part of the canyon into a succession composed of metre- to decimetre-scale passing upwards and gastropod fragments, bivalve deposits forming sandstone-mudstone couplets (Fig. 15). Sandstone are mostly density-flow record hemipelagic deposition during steady state layers structureless and planar laminated, while the clayey structureless sandstones by a succession composed of thicker, phases. This succession is overlained of interlaminated mudstones and sandstones, which contain leaf remnants alternating with layers to sandy by gravely fill is overlain floods. The canyon to river and are directly linked ostracods freshwater Figs 15 and 16) recording a later stage of emergence. continental deposits (part of the Cutro terrace, analysis, together with micropalaeontologic data from the hemipelagic units, suggest that studied Facies sea-level relative during deposition due to an overall material cut-off gravel fill records a progressive canyon systems, and of sediment in fluvial to shallow-marine increasing entrapment rise, leading to progressive lowering. This trend probably reflects high-magnitude glacio- sea-level relative a generalized successively emergence. eustatic changes combined with the regional uplift of region, later determining definitive geological field trips 2015 - 7(2.2) itinerary 33 2011). deposits Fig. 15 - area and an margin Serra Mulara Serra column of the Zecchin et al., Zecchin (modified from sedimentological the Serra Mulara the Serra Geological map of F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 geological field trips 2015 - 7(2.2) itinerary 34 an margin and later in & Bridgland, 2007), F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri 1993; Westaway 1993; Westaway A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni Fig. 16 - View of the Serra Mulara formation and the Cutro clay (modified from Zecchin et al., 2011). et al., (modified from Zecchin formation and the Cutro clay Mulara Fig. 16 - View of the Serra DOI: 10.3301/GFT.2015.04 the Crotone area. In particular, Zecchin et al. (2011) estimated that the beginning of uplift Crotone Zecchin the Crotone area. In particular, basin occurred between 0.4 Ma and 0.45 Ma, that is Marine Isotope Stage (MIS) 12 11. This into account the time necessary to fill, takes canyon Mulara estimation, based on data collected in the Serra of 1 m/ka, which is close to the calculated long- assuming an uplift rate upper slope deposits at sea level raise 2004b). et al., since MIS 7 (Zecchin term uplift rate Considering the whole Calabrian Arc, the onset of the uplift was diachronous, as it has been dated approximately Considering the whole Calabrian Arc, onset of uplift was near the end of early Pleistocene in some areas (Westaway, geological field trips 2015 - 7(2.2) itinerary 35 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri Day 2 The Crati basin A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 The Crati graben (Lanzafame & Tortorici, 1981; Tortorici, 1981; Tansi et al., 2005a, 2007) is characterized by N-S 2005a, 2007) is characterized et al., 1981; Tansi 1981; Tortorici, (Lanzafame & Tortorici, graben The Crati Late Miocene-Quaternary deposits from the Calabrian Quaternary faults, which separate trending transtensional cropping out in the Coastal Chain and Sila Massif (Fig.17), on its western eastern margins, terranes by a Middle Pliocene-Middle Pleistocene zone, Such deposits are represented, in the depocentral respectively. marine succession, closed at the top by Late Pleistocene-Holocene alluvial deposits. N- conglomerate-sand-clay 1985; (Postpischl, MCS events as testified both by historical IX-X S normal faults show seismogenic activity, these faults 1990). Morphologically, (Moretti et al., 1995, 1997) and by instrumental earthquakes Boschi et al., alluvial fans, bounding the uplifted footwalls. by active are represented by sharp rectilinear escarpments, marked fault by 300–400 m high cumulative of about 700 m, and are characterized The mountain fronts reach elevations facets (70–100 m high) are found. An antecedent drainage escarpments along which triangular/trapezoidal on the uplifted network flows perpendicular to the fault segments; it is made of deeply entrenched canyons the 2005a). At et al., 1995; Tansi et al., on the down-thrown blocks (Tortorici blocks, and of flat valleys to oblique with subvertical to NNE-SSW, normal faults show fault planes striking from N-S mesoscopic-scale, component of motion related to an extensional direction (σ3) oriented indicating a right-lateral slickensides, by of the Calabrian Arc and were characterized and the migration N125E. They strongly control the evolution and the dissection basin development 2000), responsible for the Crati Dijk et al., (Van episodes of transtension 1981; Turco 1981; Tortorici, of the interior Calabrian Arc (Lanzafame & Zuffa, 1976; Lanzafame Tortorici, 2011). 2007; Spina et al., et al., 2007b; Tansi 1990; Cifelli et al., et al., & Knott, 1988; Turco basin are formed by the crystalline rocks of Sila Massif at east, The margins of the Crati at the west and south, by sedimentary rocks of Pollino and sedimentary rocks of the Coastal Range oriented Sibari trough and the E-W oriented Crati and can be divided into the N-S unit at the north. It is L-shaped 1987), as a result of strong tectonic control; the Sibari trough represents main depocentral (Colella et al., exploration. area, as suggested by the 1000 m thick Plio-Quaternary succession drilled for hydrocarbon trough can be divided into succession of the Crati (1981), the stratigraphic According to Lanzafame & Tortorici along three sedimentary units. The lowermost part of the succession, Pliocene in age, crops out extensively geological field trips 2015 - 7(2.2) itinerary 36 an margin Fig. 17 - Structural sche- Fig. 17 - Structural (after Tansi et al., 2007). et al., (after Tansi me of the western Calabria in which are indicated the left- and the shear zone lateral basin Crati transtensional F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 geological field trips 2015 - 7(2.2) itinerary 37 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri Fig. 18 – Stratigraphic column showing the distribution of dif- Fig. 18 – Stratigraphic the southern-central Crati basin (after Spina et al., 2011). basin (after Spina et al., Crati the southern-central ferent stratigraphic formations and their relationships as observed in formations and their relationships as observed ferent stratigraphic the western side of basin and consists a fining the bedrock (fig. 18). A Plio- sequence overlaying upward Pleistocene succession occur unconformably on Pliocene deposits and directly onto the bedrock, in response to basin subsidence that starts at the west and proceeded diachronous transgression causing an eastward eastwards, (Burton, 1971; Lanzafame & Zuffa, 1976; 1981). The Plio-Pleistocene 1980; Tortorici, Tortorici, deposits consist of a complex sequence whose topmost into deposits grading part is constituted of clayey referred to Emilian and sandstones and conglomerates 1981). The (Lanzafame & Tortorici, Sicilian, respectively mostly match to the sandstones and conglomerates delta and shore deposits well documented coarse-grained 1987; Colella, 1988, by previous works (Colella et al., 1994; Carobene & Damiani, 1985), cropping out along the margins of basin. extensively this sector experienced a From Middle Pleistocene onwards, 1981) that promoted the partial uplift (Tortorici, marked dissection of the Plio-Pleistocene deposits and successively by a thick succession of fluvial conglomerate its covering 2011), well exposed in the southernmost part (Fabbricatore, right side; a Valley trough, along the Crati of the Crati is to be found on the eastern framework similar stratigraphic 2009). et al., side of the Sila Massif (Robustelli A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 geological field trips 2015 - 7(2.2) itinerary 38 delta. Fig. 19 – an margin Schematic Gilbert-type development of development F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 According to Lanzafame & Tortorici (1981), the topmost part of Pleistocene deposits consists clayey According to Lanzafame & Tortorici In that are Emilian and Sicilian in age, respectively. into sandstones and conglomerates sediments grading delta and shore deposits cropping correspond to the coarse-grained sandstones and conglomerates particular, 1987; along the margins of basin ad already described by previous works, (Colella et al., out extensively Colella, 1988, 1994; Carobene & Damiani, 1985). significant component of the Crati deltas represent a volumetrically Gilbert-type coarse-grained In particular, trough, trough sedimentary infill; such a depositional system dominates along the western side of Crati delta where the depositional architecture of deltaic deposits is represented by a series forward-stepping of basin depocentre in response to coastal uplift. migration sequences producing an eastward groups of foreset beds (Fig. 19); in small scale, tectonic control is also highlighted by two or more stacked At geometries major bounding surfaces and stratal this case, basal unconformity is well noticeable. The overlying so that the clinoform wedge is composed of a and progradation, indicate alternating episodes of aggradation This particular by oblique to sigmoidal geometry. units characterised stack of unconformity-bounded represents the sedimentary response to high (unconformity) and slow (complex sigmoid-oblique arrangement delta system fault. displacement along the back-edge geometry) vertical geological field trips 2015 - 7(2.2) itinerary 39 an margin in the Crati basin. in the Crati Fig. 20 – Gilbert-type delta Fig. 20 – Gilbert-type F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 Detailed sedimentological studies of the Gilbert-type fan deltas of the eastern margin of the Crati trough have fan deltas of the eastern margin Crati Detailed sedimentological studies of the Gilbert-type architecture of shoal water 1987) but facies analysis and stratigraphic been previously published (Colella et al., been mostly neglected. Such a depositional system crops out along the southeastern margin of deltas have trough. the Crati geological field trips 2015 - 7(2.2) itinerary 40 system. an margin Pleistocene the Sila Massif (blue southeastern side of lines). In red, Lower of the Arente River); synsedimentary fault Fig. 21 - Shoal water widespread along the sediments rest directly delta deposits are very Crati basin (the picture Crati Crati Valley normal fault Valley Crati on crystalline bedrock of belonging to the eastern Lower Pleistocene deltaic is taken on the right side is taken F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 STOP 2.1: Arente River (Crati Valley, CS). The eastern Lower Pleistocene Crati basin infill. been used to group them in facies associations, related relationships among the facies have and lateral The vertical to their spatial distribution and genesis,showing the main depositional setting. These assemblages correspond distal mouth bar and sandstones (FA3), (FA1) mouth bar conglomerates facies associations: proximal seven distal delta front sandstone (FA4), delta front sandy conglomerates proximal and sandstone (FA3), conglomerates and prodelta muddy sandstones (FA7). delta front sandstone (FA6) wave-influenced (FA5), geological field trips 2015 - 7(2.2) itinerary 41 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 Facies association FA1 is characterised by clast-supported, granule- to cobble-size conglomerates organised conglomerates to cobble-size granule- by clast-supported, is characterised association FA1 Facies symmetrical or asymmetrical having gravel, units. Planar cross-stratified into lenticular and sheet-like sandstones of facies association on stratified This facies association rests erosively base also occur. concave-up into facies association FA2. basinward and grades FA3 beds. They sandstone and conglomerate stratified by planar-parallel is characterised association FA2 Facies dimensions for to broadly lenticular geometry and distinct diffuse boundaries. Typical show a sheet-like extent. to tens of metres in lateral from centimetres to 0.5 m in thickness and generally individual units range and upward trend and grades and thinning upward fining upward This facies association shows an overall into facies association FA4. laterally is mainly composed of sand. This facies association represents a wedge-shaped unit, association FA3 Facies It is mainly constituted by large-scale cross-bedded and FA2. enclosed between facies associations FA1 sandstones delta. In particular, sandstones interpreted as sand-dominated mouth-bar wedges of a shoal-water mouth-bars deposited by fluvial processes at the mouth of a secondary of low-relief are representative distributary channels within a protected area. and downdip to distal delta front deposits (northwestwards) and passes laterally overlaps association FA4 Facies sand and pebbly and trough cross stratified This facies association primarily consists of planar-parallel (FA5). sheets and lenses lesser amounts of ripple cross-laminated sandstone sandy gravel sand, with rare packages, i.e. bedsets, stacking of fining-upward feature consists in the vertical mudstone. The main architectural by a wedge-shaped form. and cross bedding locally characterised planar-parallel frequently displaying and downdip into northwards is constituted the main sandstone outcrops, passes laterally association FA5 Facies is quite bioturbated facies association. The FA5 extension of FA4 prodelta fines and is seen as direct basinward fining within the deposits of A westward fossils such as Thalassinoides, Ophiomorpha and Skolithos. with trace is composed of the east. FA5 are present towards is clearly recognizable, as more conglomerates the FA5 sandstones, which alternate and to poorly sorted fine- medium-grained moderately medium- to thick-bedded, to pebble conglomerates. interfinger along dip with granule It is is typically alternated with prodelta deposits which become dominant basinwards. association FA6 Facies sandstones; they are alternated by amalgamated sandy beds, consisting of medium- to thick-bedded characterized beds and conglomerate ungraded sandstone and fine-grained, and interfingered with hummocky cross-stratified fossils in this facies are giving a mottled structure to some beds. Trace lenses. Bioturbation is well developed Scolicia and Cruziana. Ophiomorpha, Skolithos, represented by Thalassinoides, Planolites, Teichichnus, geological field trips 2015 - 7(2.2) itinerary 42 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri Facies association FA7, interpreted as prodelta sediments, association FA7, Facies well exposed along the right side of Crati is generally and consists of interbedded mudstone, siltstone River thin sandstone. Updip it is alternated with sandstones of distal delta front facies association and wedged out. in deltaic architecture – The main control on the variation deltas, to to the North, shoal water from Gilbert-type, the South - is related to tectonically-influenced differences in accommodation, being sediment supply of low rates along the margin. In particular, comparable subsidence coupled with high sediment supply derived catchments, should result in from large fault tip drainage the deltas. Nevertheless, strongly progradational foremost noticeable feature of the succession is its deltaic stacking pattern, with successive retrogradational through time, onlapping fault units stepping landwards stepped, retreating bedrock. It is also worth emphasizing that the retrogradational of the succession is punctuated by regressive character possible to divide internally the delta episodes; this make sequences. The complex into transgressive-regressive architecture of the succession landward-stepping stacked here represents more phases of E-directed retrogradation, surfaces or erosive capped by hardground horizons formed during the subsequent flooding phases. Therefore, tectonics is to be considered as a causative rise, onto which factor in the Early Pleistocene sea-level changes are sea-level short-lived climate-driven, superimposed. quarry. Fig. 22 - along the the Arente Stratigraphic logs measured western side of A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 geological field trips 2015 - 7(2.2) itinerary 43 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni Fig. 23 – NW-trending left lateral strike-slip fault in the metamorphic substrate of the Arente River area (Crati Valley). area (Crati of the Arente River fault in the metamorphic substrate strike-slip left lateral Fig. 23 – NW-trending DOI: 10.3301/GFT.2015.04 geological field trips 2015 - 7(2.2) itinerary 44 e an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni Fig. 24 - View from the north of the western border of the Crati basin; fault separates the Miocene-Quaternary deposits from th basin; fault separates Fig. 24 - View from the north of western border Crati Coastal Range rocks. Coastal Range DOI: 10.3301/GFT.2015.04 STOP 2.2: Noggiano (Rende). Pleistocene-recent normal fault in the western margin of crati basin. trending major fault of the N-S basin infill outcrops along the hanging-wall The western Lower Pleistocene Crati arenites formed to mixed from the Pliocene clay In this stop is possible to view the transition Valley. of the Crati carbonates. This unit is correlated to the lower Pleistocene deposits of Stop 2.1 by siliciclastic and intrabasinal infilling fault high. Post and represents the first sedimentary input, in basin, of Coastal Chain structural is well exposed in the same stop. STOP 2.3: Villa Miceli-San Fili (CS). Transpressive N-S trending fault at the western margin of Crati basin. faults border the contact between metamorphic units of Coastal basin, reverse In the western margin of Crati faults are exposed transpressive right lateral N-S Chain and the Miocene deposits (Fig. 25, Stop 2.3). In particular, fault are present in the High angle transpressive fault bordering the eastern Coastal Range. along the major N-S Lower Pleistocene marginal deposits in the same area, and are responsible for their deformation (Fig. 26). geological field trips 2015 - 7(2.2) itinerary 45 ). C , B an margin , A ). D F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri Fig. 26 - East dipping Lower Pleistocene mixed deposits along the Fig. 26 - East dipping Lower Pleistocene mixed Stereographic projection of reverse N-S trending faults ( N-S projection of reverse Stereographic major N-S trending fault, on the left. Mesoscale east dipping reverse major N-S basin deposits ( faults in the Plio-Quaternary Crati Tectono-stratigraphic architecture of the perityrrhenian Amantea basin (Stops 2.4, 2.5, 2.6, 2.7). 1979; 1974; Ortolani et al., et al., The Amantea basin (Di Nocera Neogene basins along the Colella, 1995) is one of many margin of Calabria. The onset the basin occurred Tyrrhenian A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni Fig. 25 - Miocene conglomerates dipping to the Fig. 25 - Miocene conglomerates N-S trending fault. N-S east along the western Crati basin fault system. east along the western Crati transpressive rotated normal fault; below, Above, DOI: 10.3301/GFT.2015.04 geological field trips 2015 - 7(2.2) itinerary 46 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 in response to tectonic subsidence induced by extensional faulting during the Serravallian-early Tortonian in response to tectonic subsidence induced by extensional faulting during the Serravallian-early main depositional units, bounded by 2002). The sedimentary infill has been subdivided into five (Mattei et al., (2002) and in three depositional sequences by Mattei et al. discontinuities by Muto & Perri stratigraphic in age, is strongly influenced by a combination of and Longhitano & Nemec (2005). The first unit, Serravallian of the architecture and sedimentary evolution the structural tectonic activity and eustatic rise in sea level; in age, from alluvial fan to submarine deltas. The second unit, Tortonian basin is time-transgressive and 2002), due to the fall of sea level the first with an angular unconformity and hiatus (Mattei et al., overlies by a synsedimentary activity of normal faults. This unit is constituted by alluvial fan deposits overlain the carbonate shelf depositional system. During the deposition of second unit in middle and late Tortonian, of 1998) with the development deformation (Colella & Longhitano, affected by local contractional basin was synchronous normal faulting. The sedimentation and the architecture of basin were abruptly influenced by numerous unconformities, As a consequence, in the sedimentary sequences developed tectonic activity. component of motion along NW-SE related with the growth of local and fault folds (transpressive the same time, a new sea trending normal faults). At anticline in listric N-S trending major fault, and roll-over adjacent over rise caused the drowning of basinal area as well subsequent transgression level (Figs 27, 28). Local emergence of basin-fill, caused by growth anticlinal structures, continental zones fan at the base of third sediments, and the deposition of a coarse-grained produced intrabasinal 2002). The fourth depositional unit is represented by a thin evaporitic depositional unit (Muto & Perri, succession which lies with an angular unconformity on the underlying sediments and bedrock. These facies highs related to growth of accompanied by structural associations can be explained by the drop in sea level 1993) or to extensional uplifted blocks. Thrust activity is recorded in onland the folds (Butler & Grasso, 2010; Spina et et al., 2007; Pepe et al., basin (Tansi in the Paola been recognized Miocene deposits and have of the Calabrian Arc thrust sheet, when event 2011) probably testifying the last contractional al., The uplift of the trending shear zones. of NW-SE by the development deformation began to be characterized is testified by marine sediments, described as Amantea basin probably occurs in the Pleistocene. This event & Sylvester, (Sorriso Valvo levels topographic 2002), lying at various the fifth depositional unit (Muto & Perri, Tyrrhenian by extensional fault systems dipping towards 1993). The last deformation phase, characterized back arc rift system on Sea, realised the basin emergence and represents propagation of Tyrrhenian 2002). 2002; Muto & Perri, the western Calabrian margin (Mattei et al., geological field trips 2015 - 7(2.2) itinerary 47 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni Fig. 27 – Stratigraphic columns of the Amantea basin after Mattei et Fig. 27 – Stratigraphic al., 2002 (on the left) and Longhitano & Nemec, 2005 right). al., DOI: 10.3301/GFT.2015.04 geological field trips 2015 - 7(2.2) itinerary 48 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri Perri, 2002). Perri, Fig. 28 – Geological map of the Amantea column (after Muto & basin and stratigraphic A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 geological field trips 2015 - 7(2.2) itinerary 49 an margin Fig. 29 - Panoramic the second sequences. view from Belmonte Calabro of the Cozzo section. Varallo contact Stratigraphic between the first and F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 STOP 2.4: Belmonte Calabro (CS). Tectono-stratigraphic architecture of the Serravallian-Tortonian Amantea basin infill (Cozzo Varallo section) and post tectonics. the nord (Fig. 29), in which two older stop is located at the Belmonte Calabro village towards The panoramic by an angular unconformity sequences of Amantea basin succession are exposed. The separated 2012). The basins (Colella, 1995; Morrone, 1991; Longhitano et al., in all coeval recognized section Varallo Cozzo geological field trips 2015 - 7(2.2) itinerary 50 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni Fig. 30 - Particular of the unconformity between the two Serravallian and Tortonian sequences. and Tortonian of the unconformity between two Serravallian Fig. 30 - Particular DOI: 10.3301/GFT.2015.04 shows the vertical and lateral transition between the lower first sequence made up of proximal, conglomerates between the lower first sequence made up of proximal, transition and lateral shows the vertical and the upper second sequence made up basal fossil-bearing on the top, and deltaic sands, with ash layer bioclastic- mixed, sandstones and cross-stratified normal-graded to massive, upward breccia, evolving by a strong 2012) (Figs 29, 31). The two sequences are separated siliciclastic sandstones (Longhitano et al., erosional discontinuity and angular unconformity (Figs 29, 30). This section records two tectonic phases: the sequence in a compressional complex pattern, inducing folds and thrust coassial the Serravallian first involves sequence is affected 2007), the second Tortonian et al., (Tansi trending fault zone NW-SE with major strike-slip activity of the fault system is testified east dipping normal faults. Synsedimentary high and low-angle by N-S 2002; (Mattei et al., arrangement in the second sequences and entire basin. Domino-like extensively the lower 2012) is the result of block rotations basal primary normal faults involving Longhitano et al., geological field trips 2015 - 7(2.2) itinerary 51 an margin Belmonte Calabro area (Fig. 32). Fig. 31 - Sedimentary features of the second sequence Tidal (Tortonian). dominated mixed deposits. F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri sequence. Faults detached the over-thrusted alpine units respect the Mesozoic dolostone unit, alpine units respect the Mesozoic detached the over-thrusted sequence. Faults A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 part of the second identifing two different margins and provenance, composition of sediments during Tortonian and Messinian. The composition of sediments during Tortonian identifing two different margins and provenance, structures are displaced by high angle Quaternary normal faults particularly cropping out in the Tortonian geological field trips 2015 - 7(2.2) itinerary 52 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 Fig. 32 - trending Extensional N-S fault system in the Belmonte Calabro area, deposits. cross-cutting the Tortonian geological field trips 2015 - 7(2.2) itinerary 53 an margin Fig. 34 – Particular of the northern margin Fig. 34 – Particular contact. Amantea basin and the transpressive tectonic Amantea basin and the transpressive F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni Fig. 33 – Tectonic contact between the basal conglomerates of contact between the basal conglomerates Fig. 33 – Tectonic substrate (Paleozoic). substrate the first stratigraphic sequence (Serravallian) and the metamorphic sequence (Serravallian) the first stratigraphic DOI: 10.3301/GFT.2015.04 STOP 2.5: Regastili (CS). Transpressive fault zone at the northern margin of Amantea basin. (2002) in by Muto & Perri been survived structures, faults and folds, have sedimentary infill contractional Post wrench tectonic the Amantea basin and related, probably during Pliocene-lower Pleistocene, to a prevailing Dijk has been argued by Van fault zone strike-slip deformation. The Neogene-Quaternary activity of major NW-SE faults et al. (2007). On the northern margin of Amantea basin transpressive et al. (2000) and by Tansi (Figs 33, 34). conglomerates and the Serravallian the relationships between metamorphic substrate inverted trending thrust faults with related west N-S Moreover, folds, offset the Neogene deposits along western verging area of the basin (Fig. 35). geological field trips 2015 - 7(2.2) itinerary 54 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni Fig. 35 – N-S, E-dipping reverse faults and W-verging related folds along the western margin of Coastal Range. faults and W-verging E-dipping reverse Fig. 35 – N-S, Tortonian deposits on the left, Serravallian on the right. deposits on the left, Serravallian Tortonian DOI: 10.3301/GFT.2015.04 STOP 2.6: Serra d’Aiello (CS). Tortonian extensional tectonics in the Amantea basin infill. by pulsating compressional and extensional phases (Fig. 36). history of the Amantea basin is characterised Tectonic on west In the figure 37, outcrop, tectonic activity. view of the Tortonian and excellent a general The stop give high formed by the lowermost metamorphic unit of chain, while, to est, are cropping out a structural belonging to the second sequence of Amantea basin infill (Figs 27, 28). The Torrente strata the Tortonian Scala fault is a synsedimentary extensional fault, dipping to the Est, which related synsedimentay unconformities. of progressive folding and the development faults, causing direct (Fig. 37) or time, as reverse after the Tortonian The same fault system, is reactived, architecture of the the tectonostratigraphic tectonics in the Amantea basin that improve indirect inversion slope basin. Pliocene-Pleistocene Paola geological field trips 2015 - 7(2.2) itinerary 55 an margin Fig. 37 – General view of the Torrente Scala cachment with synsedimentary low angle Tortonian of faults. Footwall fault system is made up of ophiolitic unit, is hanging-wall made up of the second Tortonian sequence covering the Stilo unit. Fig. 36 – E-W geological section of the Amantea basin (for orientation of section see Fig. 28, after Muto & Perri, 2002). F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni DOI: 10.3301/GFT.2015.04 geological field trips 2015 - 7(2.2) itinerary 56 an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni Fig. 38 – Particular of rotated synsedimentary Tortonian normal faults and intra-formational progressive unconformities. progressive normal faults and intra-formational of rotated synsedimentary Tortonian Fig. 38 – Particular DOI: 10.3301/GFT.2015.04 STOP 2.7: Torrente Scala (CS). Rotated extensional faults and rollover anticline. sequence of the Amantea basin infill, extentional faults are followed by growing sedimentary wedge In the Tortonian folds accompained sedimentation in forming growing testifying the presence of a western paleomargin. Roll-over of the synsedimentary faults (Fig. 38). unconformities in the hanging-wall sedimentary wedges and progressive A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from the foreland peri-Ionian margin to the backarc Tyrrhenian margin F. Muto - S. Critelli - G. Robustelli - V. Tripodi - M. Zecchin - D. Fabbricatore - F. Perri g e o l o g i c a l

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DOI: 10.3301/GFT.2015.04 geological field trips 2015 - 7(2.2) references 58 . ra ini the e V., lts in al 461 al 1990, an margin F. Muto - S. Critelli G. Robustelli V. Tripodi M. Zecchin D. Fabbricatore Perri A Neogene-Quaternary Geotraverse within the northern Calabrian Arc from foreland peri-Ionian margin to backarc Tyrrheni characterization of the Messinian salinity crisis in Mediterranean.characterization 420, 135-148. Geol. Soc. Am. Bull., 78, 693–711. italy: Compositional record of wedge-top partitioning. Journal Sedimentary Research, 3, 207-221. Sc., Calabrian Arc. Earth-Evolution Norwell, MA, 287–306. Basins. Kluwer Acad., of an Orogen: The Apennines and the Adjacent Mediterranean (Eds.), Anatomy J.P. Arc. Ter in the northern sector of Calabria–Peloritani orogenic transport to the beginning of Apulia-verging constraint 17, 331-337. Nova, Bologna, 970. to 1980), n. 1 CD-ROM. ING-SGA, in Italy from 461 b.C. a. C. al 1980 (Strong earthquakes Bologna, 644. 2), n. 1 CD-ROM. 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