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Journal of Geodynamics 66 (2013) 120– 133

Contents lists available at SciVerse ScienceDirect

Journal of Geodynamics

j ourna l ho me pag e: ht tp : / /www.e lsev ier .com/ locate / jog

eformation and stratigraphic evolution of the Ligurian Accretionaryomplex in the southern Apennines (Italy)

tefano Vitale ∗, Sabatino Ciarcia, Francesco D’Assisi Tramparuloipartimento di Scienze della Terra, dell’Ambiente e delle Risorse (DiSTAR), Università di Napoli Federico II, Largo San Marcellino 10, 80138, Naples, Italy

r t i c l e i n f o

rticle history:eceived 29 November 2012eceived in revised form 21 February 2013ccepted 24 February 2013vailable online 5 March 2013

eywords:ord-Calabresearasicilide

a b s t r a c t

This work provides a structural analysis and a stratigraphic revision of the sedimentary successions ofthe Ligurian Accretionary Complex (LAC) cropping out in the southern Apennines along the boundarybetween Campania, Lucania and Calabria regions. Two fold and thrust sets characterize the progressivedeformation related to the Early Miocene inclusion of these successions in the tectonic accretionarywedge. A third deformation stage, affecting also the Middle-Upper Miocene unconformable wedge-topbasin deposits, is associated to the thrust front eastward migration. In this orogenic phase the Apen-nine thrust sheet pile, formed by LAC and Apennine Platform Units, tectonically covered the successionslocated in the westernmost sector of the Lagonegro-Molise Basin. Finally a Pliocene-Middle Pleistocene

icilideaghrebian Flysch Basin

tructural geologytratigraphy

regional fold set deformed the whole orogenic prism as consequence of a thick-skinned tectonicsexpressed by means of deeply rooted thrusts in the buried Apulian Platform carbonates. MaghrebianFlysch Basin and LAC successions show a similar stratigraphy indicating continuity between paleogeo-graphic basin domains, as well as between the Paleogene-Lower Miocene succession of Sicilide Unit andthe corresponding deposits of Lagonegro-Molise Basin as consequence of drowning of the interposedPanormide Platform starting from the uppermost Cretaceous.

. Introduction

The Ligurian Accretionary Complex (LAC) is a thrust sheet pileormed by deep basin successions, locally including oceanic to con-inental lithospheric rocks, cropping out from northern Calabriap to the northern Apennines (Fig. 1). In the southern Apennines

t occupies the highest tectonic position encompassing: (i) unitsetached from their pre-Cretaceous successions (Nord-Calabrese,arasicilide and Sicilide Units, Bonardi et al., 1988a; Monaco et al.,991; Ciarcia et al., 2009, 2012 and references therein) and (ii) theP/VLT Frido Unit characterized by an OCT (Ocean Continent Tran-

ition) basement and a metasedimentary basin succession (Knott,987, 1994; Vitale et al., 2013). The former units were piled upy means of frontal accretion mechanisms in the Burdigalian timeCiarcia et al., 2012), whereas the Frido Unit subducted in theate Oligocene and successively exhumed and intruded into theectonic prism before the middle Tortonian (Vitale et al., 2013).n turn LAC overlays an orogenic wedge formed by Mesozoic-

ertiary successions, more or less detached from their Paleozoicubstrate, encompassing both platform carbonates (Apulian andpennine Platforms, Mostardini and Merlini, 1986; Vitale and

∗ Corresponding author. Tel.: +39 812538124.E-mail address: stefano.vitale@unina.it (S. Vitale).

264-3707/$ – see front matter © 2013 Elsevier Ltd. All rights reserved.ttp://dx.doi.org/10.1016/j.jog.2013.02.008

© 2013 Elsevier Ltd. All rights reserved.

Ciarcia, 2013) and basin successions (Lagonegro and Molise BasinUnits, Mostardini and Merlini, 1986), here named External Units(Fig. 1) in analogy with the tectonic units occupying the same struc-tural position in other circum-Mediterranean chains (e.g. Guerreraet al., 2005). In Sicily analog basin successions are present (Troina-Tusa and Monte Soro Units, de Capoa et al., 2002), historicallycorrelated to those spread out from northern Tunisia, Algeria andMorocco up to the Betic Cordillera in Spain, all together originatedin a common basin domain (Maghrebian Flysch Basin; Guerreraet al., 2005). Following Vitale and Ciarcia (2013), the Late Oligocenepaleogeography of the proto-Central-Western Mediterranean Seais characterized by (i) a basin, including the Ligurian Domain in thenorthern-central sector and the Maghrebian Flysch Basin to south-west, separating, (ii) Apulian-African and (iii) European continentslocated to S/SE and N/NW, respectively. Following the W-directedsubduction and consumption of the oceanic-transitional litho-sphere (Ligurian Domain) under the European plate, the LAC,mainly structured in the Early Miocene, overthrust the westernsector of the Apennine Platform. Subsequently the whole tectonicwedge piled up onto more external domains (eastward located),incorporating progressively younger foredeep deposits (Bonardi

et al., 2009; Vitale and Ciarcia, 2013). Unconformable wedge-topbasin deposits, spanning in age from Middle Miocene up to Mid-dle Pleistocene, progressively covered the whole thrust sheet pile(Vitale and Ciarcia, 2013).

S. Vitale et al. / Journal of Geodynamics 66 (2013) 120– 133 121

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saoL

2

wVBMtfs2VoA(e21E(t2C

bmssS(

Fig. 1. Schematic tectonic map of the circum-Mediterranean

The LAC Units, cropping out in the southern Apennines, weretudied by several authors (e.g. Spadea, 1982; Bonardi et al., 1988a,993; Knott, 1987, 1994; Monaco et al., 1991; Monaco and Tortorici,995; Mazzoli, 1998; Critelli, 1999). However only in the last yearsomplete studies addressing the stratigraphy and deformation forhe successions of Nord-Calabrese and Parasicilide Units croppingut in the Campania (Sele River valley and Cilento; Ciarcia et al.,009, 2012; Vitale et al., 2010, 2011) and the Frido Unit locatedlong the Calabria–Lucania border (Vitale et al., 2013) were carriedut.

This work arises from the need to extend this analysis also to theedimentary successions cropping out in the southern Campania,long the Calabria–Lucania border and in the Lucania (Fig. 2) inrder to provide a coherent geodynamic evolution for the wholeAC in the southern Apennines.

. Geological setting

The geologic features of the investigated area (Fig. 2) wereidely studied in the past half century (among others Selli, 1962;ezzani, 1968; Ogniben, 1969; Bousquet, 1973; Spadea, 1982;onardi et al., 1988a, 1993; Knott, 1987; Monaco et al., 1991;onaco and Tortorici, 1995; Mazzoli, 1998; Critelli, 1999). Here

he LAC tectonically overlays the External Units (Fig. 3), derivedrom the deformation of Apulian continental margin, includingeveral deep to shallow water successions (Vitale and Ciarcia,013). The latter encompass the HP/LT metamorphic Lungro-erbicaro Unit (Iannace et al., 2007) and sedimentary successionsf Pollino-Ciagola (Iannace et al., 2007; Vitale and Mazzoli, 2009),lburno-Cervati (Bonardi et al., 2009), Monti della Maddalena

Patacca et al., 1990), Lagonegro (Scandone, 1967, 1972; Pescatoret al., 1999; Patacca and Scandone, 2007), Sannio (Pescatore et al.,000; Patacca and Scandone, 2007) and Monte Alpi (Bonardi et al.,988b) Units. According to the ages of their foredeep deposits, thexternal Units were stacked from the Early Miocene to the PlioceneVitale and Ciarcia, 2013) with prevalence of thick- or thin-skinnedectonics for the stiffer carbonate platform successions (Cippitelli,007; Shiner et al., 2004) and the softer basin sequences (Vitale andiarcia, 2013), respectively.

The sedimentary rocks of the LAC (topic of this paper) show aroadly comparable stratigraphy (Fig. 4), characterized by a com-on Upper Cretaceous (?)-Middle Eocene dominantly argillitic

uccession upward passing to a calcareous, marly and clayeyequence. Finally, the (i) Nord-Calabrese and (ii) Parasicilide andicilide Units end with (i) Aquitanian-lowermost Burdigalian andii) Burdigalian foredeep sandstones, respectively.

nic belts (modified after Mazzoli and Martin-Algarra, 2011).

The Parasicilide Unit crops out mainly in the Campania region,whereas the Nord-Calabrese Unit is exposed in Cilento (southernCampania) and, extensively, along the Calabria–Lucania border,while the Sicilide Unit is exposed only in the Lucania region (Fig. 2).

3. Stratigraphy of LAC Units

The Nord-Calabrese Unit includes the formations of Crete Nereand Saraceno (Fig. 4; Bonardi et al., 1988a). The Crete Nere succes-sion consists, in the lower part, of oceanic and continental masses(Spadea, 1982), the former formed by ophiolites locally preser-ving a coherent succession (“Timpa delle Murgie” ophiolites, Fig. 5aand b; Bonardi et al., 1988a), including gabbros, dolerites, pillowlavas, pillow breccias, and a deep basin cover formed by argillites,quartz-arenites, jaspers and allodapic limestones. The latter, namedalso “Calcari di Mezzana” (Bousquet, 1973), correspond to scaglia-type deposits, directly covering pillow lavas and pillow breccias(Fig. 5c). Continental bodies consist of subcontinental serpentinites,gneisses and amphibolites cropping out only in the “Timpa diPietrasasso” locality (Fig. 6). The succession continues at the basewith dark-brownish argillites alternated to gray-greenish quartz-arenites, followed by a thick succession of black shales (Fig. 5d)with intercalations, in the upper part, of arenites and calcareousbeds. The age of the middle-upper part of this formation is MiddleEocene; however the age of the lower part could reach the UpperCretaceous as suggested by Bonardi et al. (1988a). The Crete NereFm. gradually passes upward to the Saraceno Fm. consisting of fourmembers (Ciarcia et al., 2012), from bottom to top: (i) calciclas-tic, locally silicified, arenitic turbidites with dark chert lenses andrare lithic sandstones (Punta Telegrafo member, Fig. 5e); (ii) thinlayers of calciclastic, pelitic and arenitic turbidites with lenses andnodules of dark chert and subordinately arkosic-lithic sandstones(Fig. 5f, Terranova di Pollino member); (iii) alternance of marly,silty and arenitic beds, occasionally with dark chert nodules andlayers of microbreccia at the top (Carpineta member); finally (iv)thinly layered immature sandstones (Sovereto Member; Bonardiet al., 2009) (Fig. 4). The age of the Saraceno Fm. is Upper Eocene-lowermost Burdigalian (?) (Di Staso and Giardino, 2002; Bonardiet al., 2009). The thickness of the whole succession is more than1200 m (Bonardi et al., 1988a).

The Parasicilide Unit (Fig. 4) is characterized by four formations(Ciarcia et al., 2009), from bottom to top: (i) clays and slates of the

Postiglione Fm.; (ii) marls and limestones of Monte Sant’ArcangeloFm.; (iii) whitish marls and marly limestones of Contursi Fm.; and(iv) foredeep deposits of the “Arenarie di Albanella” Fm. (Donzelliand Crescenti, 1962). The thickness of the whole succession exceeds

122 S. Vitale et al. / Journal of Geodynamics 66 (2013) 120– 133

ection

8ar(

dtasF

FS

Fig. 2. Geological map of southern Apennines and cross s

00 m. The age of these deposits ranges between the Middle Eocenend the Burdigalian, even though the lower undated deposits couldeach the Upper Cretaceous in analogy to the Crete Nere Fm.Bonardi et al., 1988a; Guerrera et al., 2005).

The Sicilide Unit (Fig. 4), analogously to the Parasicilide Unit, isivided in four formations (Guerrera et al., 2005), from bottom to

op: (i) clays and slates of Argille Scagliose Fm. (Fig. 5g); (ii) marlsnd limestones of Monte Sant’Arcangelo Fm.; (iii) clays and marls,omewhere calcarenites rich in foraminifera, of Argille Varicolorim. (Fig. 5h); and (iv) foredeep deposits of the “Arenarie di Corleto”

ig. 3. Tectonic scheme of Calabria–Lucania–Campania border (modified after Vitale and

ic: Sicilide; LV: Lungro-Verbicaro; PC: Pollino-Ciagola; MM: Monti della Maddalena; Lag

(modified after Vitale et al., 2013; Mazzoli et al., 2008).

or “Tufiti di Tusa” Fms. (Fig. 4). The thickness is about 1000 m(APAT, 2005). The age of these deposits ranges between the UpperCretaceous (?) and the Burdigalian.

The Frido Unit (Fig. 4) is characterized by a metamorphicand highly deformed succession (Vitale et al., 2013) consistingof oceanic crust (metagabbros, metadolerites and metapil-

lows; “Timpa della Guardia” Fm.) and continental lithosphere(serpentinized peridotites, metagranitoids, gneisses, amphi-bolites, granofels and metacarbonates; Timpa Rotalupo Fm.)covered by a deep basin metasedimentary succession formed by

Ciarcia, 2013). Go: Gorgoglione Fm.; Fr: Frido; NC: Nord-Calabrese; PS: Parasicilide;: Lagonegro; Sa: Sannio; Alp: Monte Alpi.

S. Vitale et al. / Journal of Geodynamics 66 (2013) 120– 133 123

F in dep

m((Fstaco

TRltLapc1(onumR

4

bPA(2

ig. 4. Schematic stratigraphic logs of LAC successions and Miocene wedge-top bas

etaradiolarites, calcschists, phyllites, quartzites and metapelitesSan Severino Fm.) and finally by Upper Oligocene calcschistsMonte Caramola Fm.; Bonardi et al., 1993; Vitale et al., 2013). Therido Unit tectonically covers the Nord-Calabrese Unit in the SEector (“Timpa delle Murgie” area, Fig. 6) whereas is placed belowhe Nord-Calabrese and Parasicilide Units in the NW sector (Selucirea; Fig. 6). The Frido Unit experienced an HP/VLT metamorphismharacterized by a pressure peak of ca. 1.2 GPa with temperaturef ca. 350 ◦C (Vitale et al., 2013).

The LAC is unconformably covered by a Langhian-lowermostortonian succession named Cilento Group (Amore et al., 1988;usso et al., 1995), including arenitic and marly deposits of Pol-

ica and San Mauro Fms. (Ietto et al., 1965), and correspondingo the clastic undifferentiated succession of the Albidona Fm. inucania region (Selli, 1962; Bonardi et al., 1985). In the studyrea further wedge-top basin successions, unconformable on therevious units, and characterized by dominantly coarse-grainedlastic deposits, include the Upper Miocene Perosa (sensu Vezzani,966) and Oriolo (Selli, 1962) Fms. (Fig. 4). In the study areaFig. 6), the Lagonegro-Molise Basin successions extensively croput, with the Triassic-Cretaceous lower part mainly exposed in theorth-western sector (Mt. Sirino area), and the Paleogene-Miocenepper part (Flysch Rosso, Numidian sandstones and post-Numidianarls) spread out especially in the south-eastern sector, i.e. Ferro

iver Valley (Fig. 5i), Valsinni ridge and Rotondella area.

. Structural architecture of the Calabria–Lucania border

The deep crustal structure of the southern Apennines is markedy the superposition from bottom to top of (i) buried Apulian

latform carbonates; (ii) Lagonegro-Molise Basin successions; (iii)pennine Platform carbonates; and finally (iv) LAC successions

e.g. Shiner et al., 2004; Mazzoli et al., 2008; Vitale and Ciarcia,013). The thin-skinned tectonics dominated the thrust sheet

osits. PT: Punta Telegrafo; TP: Terranova di Pollino; CA: Carpineta; SO: Sovereto.

piling up both for the LAC and the Lagonegro-Molise Basin succes-sions, whereas the thick-skinned tectonics ruled the overthrustingof (i) Apennine carbonates and their pre-Triassic basement ontoLagonegro-Molise Basin strata (Cippitelli, 2007) and (ii) thrustimbrication within the buried Apulian Platform (Shiner et al., 2004).

In order to illustrate the structural architecture of theCalabria–Lucania–Campania border, three cross sections are fur-nished (Fig. 7).

The Apulian Platform carbonates are always buried beneathallochthonous units, except in the Monte Alpi where theCretaceous-Miocene Apulian succession was exhumed (Fig. 7a) bymeans of the interplay of normal faults and deep-seated thrusts(Mazzoli et al., 2006). The Lagonegro-Molise Basin Units crop outin the tectonic windows of Mt. Sirino, Castelsaraceno village, FerroRiver Valley, Valsinni ridge and Rotondella area (Figs. 6 and 7a).In the southwestern sector of the study area the HP/LT Lungro-Verbicaro Unit (western margin of the Apennine Platform; Iannaceet al., 2007) tectonically covers the Pollino-Ciagola Unit that,together the Alburno-Cervati Unit, form a ca. 65 km long WNW-ESEcarbonate ridge (Fig. 6). In the area between Timpone Spagnolo-Mt.Carnara and Castroregio-Farneta (Fig. 6), the well log data indicatethat the Apennine Platform carbonates die out eastward, as shownin the B–B’ and C–C’ sections (Fig. 7b and c).

The Ligurian Accretionary Complex widely crops out in the studyarea. The Nord-Calabrese Unit is exposed in the whole analyzedarea from Sapri and Torraca villages located in the westernmostsector (Fig. 6) up to the Castroregio village in the eastern side (Fig. 6).In the Seluci area it tectonically overlays both the Parasicilideand Frido Units as well as the Apennine Platform carbonates. TheFrido Unit, normally covering the Pollino-Ciagola Unit, in the Timpa

delle Murgie area overthrusts the Nord-Calabrese and Sicilide Units(Fig. 6). Finally in the Castroregio area, the Nord-Calabrese Unitis piled up on the Sicilide Unit, in turn tectonically covering theLagonegro-Molise Basin succession (Figs. 6 and 7b and c).

124 S. Vitale et al. / Journal of Geodynamics 66 (2013) 120– 133

Fig. 5. Examples of stratigraphic features. Nord-Calabrese Unit: (a) Timpa delle Murgie hill view showing the stratigraphic boundary between pillow lavas and breccias, anddeep basin sedimentary cover; (b) pillow lavas of Timpa delle Murgie; (c) slumping in the scaglia-type deposits (“Calcari di Mezzana”, Mezzana); (d) black shales in CreteN rafo MF ille ScL h Ross

5

tisUw

ere Fm. (road between Terranova di Pollino and S. Lorenzo Bellizzi); (e) Punta Telegm. (Sarmento River Valley). Sicilide Unit: (g) Silicified marly clays and slates of Argagonegro Unit: (i) Reddish calcilutites, jaspers and slates in the lower part of Flysc

. Structural analysis

In the following paragraphs a description of the main meso-scaleectonic structures and their orientations is provided. Deformation

n all analyzed successions is not homogeneous, and normally atrain gradient is present between these units. The Nord-Calabresenit shows highly deformed levels especially in the lower parthereas the Parasicilide Unit is characterized by a lower grade

ember of Saraceno Fm. (Sarmento River Valley); (f) Terranova Member of Saracenoagliose Fm. (Roseto Capo Spulico); (h) Argille Varicolori Fm. (Roseto Capo Spulico).o Fm. (Ferro River Valley).

of deformation, though it may show some argillitic sectors com-pletely disrupted. Finally the Sicilide Unit shows a weak internaldeformation.

5.1. Nord-Calabrese Unit

Several papers from the 70s to the 90s (e.g. Guzzetta andIetto, 1971; Mauro and Schiattarella, 1988; Zuppetta and Mazzoli,

S. Vitale et al. / Journal of Geodynamics 66 (2013) 120– 133 125

odified

1at

pftrlm

baT

Fw

Fig. 6. Tectonic map of Calabria–Lucania–Campania border (m

997; Mazzoli, 1998) showed that the Nord-Calabrese Unit wasffected by a poly-phased deformation evolution characterized byhe superposition of structures of different generations.

In order to provide a coherent structural analysis with those pro-osed by Vitale et al. (2010, 2011) and Ciarcia et al. (2009, 2012)or analog successions cropping out northward of the analyzed area,hree rheologically homogeneous sequences were analyzed sepa-ately: (i) argillites and black shales of the Crete Nere Fm.; (ii) thinlyayered calcareous turbidites of Punta Telegrafo member and (ii)

arls and arenites of the middle-upper part of the Saraceno Fm.

According to the overprinting relationships, all structures have

een associated with three main folding stages (D1-D2-D3) char-cterized by different grades of coaxiality in every analyzed part.he third deformation phase is normally recorded as macro-scale

ig. 7. Geological cross sections of the study area (traces and legend are shown in Fig. 6as calibrated according to the numerous well log data (Società Geologica Italiana, 2013)

after Bonardi et al., 1988b; Iannace et al., 2007; ISPRA, 2009).

folds. A further folding (D4) is related to deeply rooted thrusts andback thrusts involving the buried Apulian Platform carbonates anddeforming the whole thrust sheet pile, especially in the outer sectorof the Apennine Chain (e.g. Piedilato and Prosser, 2005).

In the Crete Nere Fm. early tectonic structures consist of tightto isoclinal somewhere intrafolial F1

CN folds (Fig. 8a and b). Theassociated foliation (S1

CN) is an axial plane slaty cleavage in theargillitic layers, and a spaced disjunctive convergent fan cleavagein the arenitic and calcareous beds. Close to tight folds usually witha kink shape, verging both to SE and NW (Fig. 8c and d), charac-

CN

terize the second fold set. Locally F2 folds are associated withmeso-scale thrust faults (Fig. 8d). Crenulation cleavage (S2

CN) andcrenulation lineation (CL2

CN), well-developed in the argillitic lay-ers, occur. These two fold sets (F1

CN and F2CN) show a weak

. Part of A–A’ cross section is modified after Mazzoli et al., 2006). The B–B’ section re-interpreted for this work.

126 S. Vitale et al. / Journal of Geodynamics 66 (2013) 120– 133

Fig. 8. Examples of tectonic structures in the Nord-Calabrese Unit. Crete Nere Fm.: (a) F1 recumbent isoclinal fold (Destra delle Donne, Terranova di Pollino); (b) F1 tightf d F2 c( (f) F1

d .

ctTa(

(doSFtp(

(n

old (Terranova di Pollino); (c) interference pattern of type 2 between F1 isoclinal ane) pencil cleavage (Terranova di Pollino). Punta Telegrafo member (Saraceno Fm.):uplex structure in argillitic layers embedded in calcareous strata (Sarmento River)

oaxiality with an interference pattern (Fig. 8c) ranging betweenhe types 2 and 3 of the Ramsay’s classification (Ramsay, 1967).he overprinting between these two tectonic foliations generates

characteristic pencil cleavage especially in the argillitic layersFig. 8e).

Poles to bedding (S0CN) are scattered (Fig. 9a); F1

CN fold hingesA1

CN) and crenulation lineations (CL1CN) show a NW–SE main

irection (Fig. 9b) whereas related axial plane poles (AP1CN) spread

ut around a NE–SW directed roughly vertical cyclograph (Fig. 9c).1

CN cleavage poles indicate NW–SE about vertical planes (Fig. 9d).2

CN fold hinges (A2CN) and crenulation lineations (CL2

CN) are scat-ered, though a mean NE–SW trend results (Fig. 9e). Related axiallane poles (AP2

CN) indicate a mean SW gently dipping plane

Fig. 9f).

The calcareous turbidites of the lower part of Saraceno Fm.Punta Telegrafo member) are deformed by an early tight and isocli-al folding (Fig. 8f). A boudinage is associated to this deformation

lose folds (Terranova di Pollino); (d) meso-scale thrust fault (San Lorenzo Bellizzi);tight chevron folds (Sarmento River); (g) asymmetric boudin (Sarmento River); (h)

stage, which affects the long limbs of F1SA folds with stretching

direction orthogonal to fold axes, where competent layers maylocally form asymmetric boudins (Fig. 8g). Often a further syn-cronous extension, orthogonal to the previous, forms a chocolatetablet boudinage. Meso-scale thrust faults occasionally developedduplex structures in pelitic interlayers (Fig. 8h), whereas the cal-careous beds, embedded in pelitic layers, locally host pre-bucklethrusts. Early structures are deformed by the second phase open totight, normally verging to SE, folds (F2

SA) with the development of acrenulation cleavage (S2

SA) and crenulation lineation (CL2SA). Like-

wise of the Crete Nere Fm., also the interference pattern betweenthe two fold sets varies between types 2 and 3. Rare meso-scalefolds associated to the third deformation stage (D3) superpose onto

the previous tectonic structures.

The middle-upper part of the Saraceno Fm. (Terranova,Carpineta and Sovereto members) is less deformed with respect tothe lower part. The first deformation stage (D1) includes chevron

S. Vitale et al. / Journal of Geodynamics 66 (2013) 120– 133 127

F wer hp

tasdFsiptp(fo

tgpgdh(dm(

5

caos(

ig. 9. Stereographic projections of analyzed structures of Nord-Calabrese Unit (lolane; CL: crenulation lineation. CN: Crete Nere Fm.; SA: Saraceno Fm.

o rounded, tight to isoclinal folds F1SA (Fig. 10a–d). A slaty cleav-

ge S2SA is well-developed in the pelitic interlayers. The previous

tructures are deformed by open to tight folds (F2SA) (Fig. 10c and

) with associated crenulation cleavage and crenulation lineation.2

SA folds are often overturned both to SE and NW (Fig. 10c and d),howing a kink geometry. Pre-buckle thrusts are normally hostedn arenitic layers embedded in pelitic interlayers. Similarly to therevious successions, fold axes of the two superposed deforma-ion, vary between almost orthogonal, generating an interferenceattern of type 2 (Fig. 10d), and parallel with patterns of type 3Fig. 10c). The third deformation is recorded only as macro-scaleolds, often overturned, affecting also the wedge-top basin depositsf the Albidona Fm.

Poles to bedding (S0SA) for the whole Saraceno Fm. are scat-

ered, however they lie around an almost vertical N10 strikingreat circle (Fig. 9g). F1

SA fold hinges are random (Fig. 9h), whereasoles to axial planes spread out around a sub-vertical NNE–SSWreat circle with a maximum frequency peak given by southeastipping planes (Fig. 9i). Also F2

SA fold hinges (A2SA) are dispersed,

owever showing main W/SW-trending sub-horizontal clustersFig. 9j). Poles to axial planes (AP2

SA) lie along an ENE moderatelyipping cyclograph (Fig. 9k). Rare F3

SA fold hinges (A3SA) show a

ean NNW–SSE trend (Fig. 9l), whereas related axial plane polesAP3

SA) spread out around a NNE–SSW great circle (Fig. 9m).

.2. Parasicilide and Sicilide Units

The Parasicilide Unit shows a heterogeneous deformation espe-ially localized in the argillitic layers where more competent beds

re completely dismembered giving to the rocks an appearancef a “broken formation” (e.g. Mattioni et al., 2006). The first foldet (F1

PS) consists of chevron to rounded, tight to isoclinal foldsFig. 10e). The associated foliation is an axial plane cleavage in

emisphere, Schmidt net). S0: bedding; S1: tectonic foliation; A: fold axis; AP: axial

argillites, whereas is a disjunctive convergent fan cleavage in themore competent layers. Locally F1

PS folds are related to meso-scalethrust faults. These structures are deformed by open to tight folds(F2

PS) (Fig. 10e), often with a kink conjugate geometry. The interfer-ence pattern is intermediate between 2 and 3 types of the Ramsay’sclassification (Fig. 10e).

F1PS fold hinges are very scattered (Fig. 11a) such as the poles

to axial planes (Fig. 11b). F2PS fold hinges (Fig. 11c) indicate a large

dispersion with two main clusters, E–W and N–S directed. Polesto axial planes (Fig. 11d) indicate a main gently N dipping plane.F3

PS fold hinges (Fig. 11e) show a mean NNE–SSW trend with axialplanes mainly dipping to N (Fig. 11f).

The Sicilide succession is characterized, like the previous units,by the superposition of three meso-scale fold sets. The rare earlygenerally isoclinal folds F1

SI (Fig. 10f) are deformed by a morefrequent second fold set (F2

SI) showing open to close geometries(Fig. 10f). The third fold set (F3

SI) consists of open to close folds oftenassociated with thrust faults both verging to NE and SW (Fig. 10gand h). Poles to bedding (S0

SI) spread out around an almost verti-cal NNE–SSW cyclograph (Fig. 11g). F1

SI fold hinges are scattered(Fig. 11h), whereas the poles to axial planes lie along a NNE–SSWalmost vertical great circle (Fig. 11i). F2

SI fold hinges show a meanE–W trend (Fig. 11j), whereas the poles to axial planes are scattered(Fig. 11k). Finally F3

SI fold hinges (Fig. 11l) indicate a mean NW–SEtrend and the poles to axial planes (Fig. 11m) are located around aN–SW vertical cyclograph.

6. Discussion

This work follows recent studies on (i) analog successions crop-ping out in Cilento and Sele River Valley (Fig. 1, Campania region;Vitale et al., 2010, 2011; Ciarcia et al., 2009, 2012) and (ii) tectonicunits located at Calabria–Lucania boundary such as Frido (Vitale

128 S. Vitale et al. / Journal of Geodynamics 66 (2013) 120– 133

F l fold

o (d) inp ttern o

eVialMBFnsn

ig. 10. Examples of tectonic features. Terranova Mb. (Saraceno Fm.): (a) F1 isoclinaf type 3 between F1 tight and F2 open folds (San Lorenzo Bellizzi). Carpineta Mb.:attern of type 2 between F1 isoclinal and F2 open folds (Torraca); (f) interference pa

t al., 2013), Pollino-Ciagola (Vitale and Mazzoli, 2009) and Lungro-erbicaro (Iannace et al., 2007) Units. The study area is character-

zed by the superposition of LAC on Apennine Platform carbonatesnd Lagonegro-Molise Basin strata (Fig. 6). The latter are usuallyocated at the footwall of the former successions, though around the

t. Sirino (Fig. 6), the LAC tectonically covers the Lagonegro-Moliseasin rocks by means of low-angle normal faults (e.g. Cogliandrino

ault, Mazzoli et al., 2006) with the tectonic elision of the Apen-ine Platform carbonates (Fig. 7a). On the other hand, in the easternector (Rotondella-Montegiordano area, Fig. 6), a main thrust faultears LAC over the Lagonegro-Molise Basin succession. Around the

(Ferro River Valley); (b) F1 chevron fold (Ferro River Valley) (c) interference patternterference pattern of type 2 (Sapri). Parasicilide and Sicilide Units: (e) Interferencef type 3 (Farneta); (g and h) F3 meso-scale folds associated to thrust faults (Farneta).

Ferro River Valley (Fig. 6), the Lagonegro-Molise Basin strata (FlyschRosso Fm. and Numidian Sandstones) crop out on the hanging wallof a deeply rooted thrust. Similarly, Numidian Sandstones and post-Numidian deposits of Lagonegro-Molise Basin Units emerge in thetectonic windows near Valsinni Ridge and Rotondella (Fig. 6). Theseregional structures, lifted the Apulian Platform carbonates of theMonte Alpi, and probably resulted from the Pliocene-Early Pleis-

tocene thick-skinned tectonic involving the buried Apulian Plat-form carbonates (Carbone et al., 1987; Shiner et al., 2004; Vitale andCiarcia, 2013). This tectonic event was coeval with the sedimen-tation within the Sant’Arcangelo wedge-top basin (Fig. 6), where

S. Vitale et al. / Journal of Geodynamics 66 (2013) 120– 133 129

F e UniP

st

ssaanispPt

Ft

ig. 11. Stereographic projections of analyzed structures in Parasicilide and Sicilidarasicilide Unit; SI: Sicilide Unit.

yntectonic unconformities indicate a progressive deformation andilting of this succession (Zuppetta et al., 2004; Ascione et al., 2012).

The analyzed successions show a deformation consisting of theuperposition of several sets of folds and thrust faults. The first twotages, in every succession, share several common features suchs the structural orientations, suggesting that they were part of

same progressive deformation, although occurred as heteroge-eous, often localized only in some levels, and highly variable in

ntensity. The Nord-Calabrese Unit is the most deformed succes-

ion, where the deformation is principally focused in the upperart of Crete Nere Fm. and the lower part of Saraceno Fm. (i.e.unta Telegrafo Mb.). The remnant sectors host sporadic folds andhrust faults (middle-upper part of Saraceno Fm.) or a pervasive

ig. 12. Comparison of schematic stratigraphic logs between Sicilide, Troina-Tusa/Montehe Late Oligocene paleogeography (modified after Vitale and Ciarcia, 2013).

ts (lower hemisphere, Schmidt net). S0: bedding; A: fold axis; AP: axial plane. PS:

cleavage such as in the black shales and argillites (Crete Nere Fm.).The Parasicilide and Sicilide Units are lesser deformed with respectthe previous unit, however locally the deformation, localized insome argillitic levels, produced a complete bedding disruption.

The synoptic view of the fold axis directions in all analyzed suc-cessions (Fig. 6), marks the variability of fold orientations. However,at Terranova di Pollino, San Lorenzo Bellizzi, Fiumara Saraceno andAmendolara areas (Fig. 6) the early folds show prevailing E–W orNW–SE trends, whereas the second phase folds indicate N–S or

NE–SW directions and the third phase fold axes show a dominantNW–SE trend. Similar directions of the first and second (F1 andF2) fold sets are also present in the area of Sapri and Castelsara-ceno (Fig. 6). The fold axes hosted in the Albidona wedge-top basin

Soro, Panormide Platform, Imerese and Lagonegro Units, and their localization in

1 eodyn

dU

Stcits(boaTFtu2

ltbsssFsisfi

cCfH

Fa

30 S. Vitale et al. / Journal of G

eposits (Cesarano et al., 2002) and those in the Pollino-Ciagolanit (Iannace et al., 2007) are also shown in the map of Fig. 6.

In analogy with the LAC Units cropping out in the Cilento andele River Valley (Ciarcia et al., 2009, 2012; Vitale et al., 2010, 2011),he successions analyzed in this study indicate a tectonic evolutiononsisting of (i) two progressive folding stages related to the build-ng of the thrust sheet pile in the Burdigalian time, i.e. followinghe foredeep deposition (Tufiti di Tusa Fm.) and before the Langhianedimentation of the wedge-top basin deposits (Albidona Fm.); andii) a third folding and thrusting stage affecting also the wedge-topasin deposits of the Albidona Fm. and the underlying carbonatesf the Pollino-Ciagola Unit. The successive deformation (D3) prob-bly occurred before the deposition of the unconformable upperortonian-lower Messinian wedge-top basin deposits of Oriolom. This tectonic stage was synchronous with the early deforma-ion of Lagonegro Units as consequence of the accretion of thesenits within the Apennine thrust sheet pile (Vitale and Ciarcia,013).

As previously pointed out, in the Monte Alpi, Ferro River Val-ey, Farneta, Valsinni Ridge and Rotondella areas (Fig. 6), the wholehrust sheet pile and the Miocene wedge-top deposits are deformedy deeply rooted thrusts and back-thrusts characterized by a con-tant NE–SW shortening (e.g. Piedilato and Prosser, 2005). For theake of completeness a further deformation stage is described byeveral authors (e.g. Catalano et al., 1993; Bonini and Sani, 2000;erranti et al., 2009) at the Lucania–Calabria border and the externalector of the Lucanian Apennines. Such a Pleistocene deformations expressed as a strike-slip faulting with a mean NW–SE compres-ion that may locally have distorted the orientation of pre-existingolds and to be the cause of the dispersion of fold hinges as shownn the map of Fig. 6.

The term Parasicilide Unit (or “terreni ad affinità Sicilide”)

orresponding to the basin succession cropping out at thealabria–Lucania border, was introduced by Bonardi et al. (1988a)or marking the stratigraphic differences with the Sicilide Unit.owever the similarities are more than the differences, hence

ig. 13. Tectonic scheme of the area comprised between Sele River Valley, Cilento and Calafter Vitale et al., 2011).

amics 66 (2013) 120– 133

according to (i) the stratigraphic and deformation evolution of theParasicilide and Sicilide successions, such as described in this paperand in Ciarcia et al. (2009, 2012); (ii) the structural position i.e.both below the Nord-Calabrese Unit; and (iii) the lacking of a cleartectonic feature between them, these deposits can be consideredas a single succession although characterized by significant lat-eral facies heteropies. It is worth to note as these two successionsform together the most widespread basin deposits in the southernApennines cropping out from Campania up to northern Lucania andCalabria regions (Fig. 2).

The stratigraphic similarity existing also for the Sicilide Unitand the Paleogene-Lower Miocene succession of Lagonegro-MoliseBasin Units (Flysch Rosso; Scandone, 1967) (Fig. 12), induceda notable ambiguity in the literature, comprising also the newItalian geological cartography (CARG project). As consequence, dif-ferent interpretations about origin of such rocks, are furnishedby different authors, also in the same area (e.g. Ogniben, 1969;Zuppetta et al., 1984, 2004; Pescatore et al., 1988, 1999; Lentiniet al., 2002; Pescatore, 2005; Carbone and Lentini, 2011). Thecomparable deposition of such successions could be the conse-quence of the connection between the W-located MaghrebianFlysch Basin and the Lagonegro-Molise and Imerese Basins to the E(Fig. 12), following the drowning of the Panormide Platform sincethe uppermost Cretaceous, as testified by the deposition of scaglia-type deposits of the Amerillo Fm. (Grasso et al., 1978; Accainoet al., 2011;Fig. 12). Summarizing considering the Late Oligocenepaleogeography of the central sector of the proto-wester-central-Mediterranean Sea (Fig. 12), a single wide basin, including theMaghrebian Flysch, Ligurian, Lagonegro-Molise, Imerese and Ioniandomains, divided the Apennine and Apulian Platforms, north-ward located, from the African margin, in the southern sector.This basin was characterized by a common silico- and volcano-

clastic sedimentation until the Burdigalian, after which the westernareas were gradually incorporated into the Apennine-Maghrebianaccretionary wedge (Accaino et al., 2011; Vitale and Ciarcia,2013).

bria–Lucania boundary showing tectonic transport vectors (the NW sector modified

eodyn

mweatQ(MMat

tpstlvUtl(se

7

1

2

3

4

S. Vitale et al. / Journal of G

Grouping all tectonic vergences, such as result from the kine-atic analysis of brittle and ductile structures related to tectonicedge accretion, for (i) LAC Units (from Ciarcia et al., 2012; Vitale

t al., 2013); (ii) Lungro-Verbicaro Unit (Iannace et al., 2007; Vitalend Mazzoli, 2009) and (iii) Lagonegro-Molise Basin Units in threeemporal stages (Early-Middle Miocene, Late Miocene and Plio-uaternary) from the Sele River Valley and Cilento up to study area

Fig. 13), a complex kinematic pattern appears: (i) Early-Middleiocene vergences indicate a mean SE tectonic transport; (ii) Lateiocene vergences are scattered between NW to NE forming an

rcuate belt; (iii) Plio-Quaternary vergences indicate a constant NEectonic transport.

As concerning the meaning of the crystalline rocks at base ofhe Nord-Calabrese succession, recently Shimabukuro et al. (2012)rovided a 40Ar–39Ar dating of 193 ± 2 Ma for the amphibolitesampled in the Timpa di Pietrasasso (Fig. 6). The authors suggesthat this post-Hercinian age is related to the exhumation of theower continental crust during a Jurassic early rifting stage, as pre-iously proposed by Piccardo (2009) for the corresponding Liguriannits cropping out in the northern Apennines. On the other hand

he association of subcontinental serpentinites, gabbros, pillowavas, gneisses and amphibolites covered by a deep basin successionSpadea, 1982; Bonardi et al., 1988a), indicate an OCT environmentuch as suggested for the basement rocks of Frido Unit by Vitalet al. (2013).

. Concluding remarks

) Sedimentary successions of the LAC show a similar deforma-tion evolution characterized by the superposition of main fourfold and thrust sets (D1–D4). The first two stages show com-mon features indicating a progressive deformation especiallylocalized in less competent rocks, with an overall strain gradientexisting from the more deformed Nord-Calabrese Unit to lesserdeformed Parasicilide and Sicilide Units.

) The Nord-Calabrese Unit was deformed by early (F1NC) folds

characterized by isoclinal to tight geometry and a related slatycleavage in argillites and a disjunctive foliation in competent lay-ers. Successive folds (F2

NC) show open to tight, often kink shapes,locally related to meso-scale thrust faults with minor displace-ments. These two fold sets show a variable coaxiality, formingdifferent interference patterns, which end-members are rep-resented by the types 2 and 3 of the Ramsay’s classification.Minor tectonic structures occur such as pre-buckle thrusts incompetent layers embedded in pelitic interstrata, duplex struc-tures localized in pelitic layers and boudins especially along thestretched limbs of F1

NC folds.) Such as the previous succession, the Parasicilide and Sicilide

Units are characterized by an early deformation (D1) expressedby mostly isoclinal folds (F1

PS-SI) with associated a weakly devel-oped axial plane cleavage. Successive open to tight folds (F2

PS-SI)show a variable coaxiality with the former fold stage, produc-ing an interference pattern ranging between 2 and 3 type ofthe Ramsay’s classification. Third deformation stage (D3), well-developed in the Sicilide succession, consists of thrusts andrelated folds verging both to NE and SW.

) The deformation evolution described in this work for the basinsuccessions belonging to the LAC can be compared with thatof analog successions cropping out northward in the Campaniaregion (e.g. Ciarcia et al., 2012). The progressive deformationmainly recorded as two superposed fold sets (D1–D2), for all ana-

lyzed successions, was related to the building of the thrust sheetpile in the Burdigalian time, whereas the third fold and thrustset (D3), recorded also the wedge-top basin deposits of AlbidonaFm. and the underlying carbonates of the Pollino-Ciagola Unit,

amics 66 (2013) 120– 133 131

was associated to the overthrusting of the Apennine wedgeonto the eastern sector of the Apulian domain and the inclu-sion of Lagonegro Units in the tectonic prism (Vitale and Ciarcia,2013). The latter event probably occurred before the depositionof the unconformable upper Tortonian-lower Messinian wedge-top basin deposits of Oriolo Fm. A further deformation (D4) wasexpressed by long wavelength-high amplitude folds, related todeeply rooted thrusts, deforming the whole thrust sheet pileand producing, in the easternmost sector of the analyzed area,the tectonic windows of Valsinni and Rotondella, where Numid-ian Sandstones (Lagonegro-Molise Basin Units) crop out. Thisthick-skinned thrusting, synchronous with the Pliocene-MiddlePleistocene filling of the Sant’Arcangelo wedge-top basin, wasresponsible also of the uplifts of Castroregio, Farneta and MonteAlpi in the central sector of the study area.

5) All the analyzed LAC Units show a similar stratigraphyand a strong correspondence exists between the UpperCretaceous-Lower Miocene deposits of Sicilide Unit and theLagonegro-Molise Basin successions (Flysch Rosso Fm.). Thisrelation is probably associated with the paleogeographic evolu-tion of this sector, where the Panormide Platform, that separatedthe Ligurian/Maghrebian Flysch and Lagonegro-Molise/Imeresebasins, starting from the uppermost Cretaceous, drowned andallowed the joining of these two basins.

6) Finally tectonic vergences, recorded in different thrust sheetsand unconformable wedge-top basin deposits, indicate: (i) anEarly-Middle Miocene mean SE tectonic transport for the LACsuccessions; (ii) a Late Miocene transport from NW to NEfor the LAC Units, overlying Albidona Fm., Apennine Platformand Lagonegro-Molise Basin Units; and finally (iii) a constantNE–SW shortening for the tectonic structures related to the Plio-Quaternary thick-skinned thrusting.

Acknowledgments

We are grateful to Giulio Fittipaldi for helping us in the field-work, Stefano Mazzoli and Mohamed Najib Zaghloul for the usefuldiscussions and suggestions. Finally we wish to thank an anony-mous reviewer and the Editor-in-Chief Randell Stephenson thatcontributed to greatly increase the quality of this work.

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