Geological Field Trips

Società Geologica Italiana

2013 Vol. 5 (1.1) 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 The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction of the -Peloritani Orogen 86° Congresso Nazionale della Società Geologica Italiana Arcavacata di Rende (CS) 2012

DOI: 10.3301/GFT.2013.01 The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction of the Calabria-Peloritani Orogen R. Cirrincione - E. Fazio - P. Fiannacca - G. Ortolano - A. Pezzino - R. Punturo - V. Romano - V. Sacco GFT - Geological Field Trips geological fieldtrips2013-5(1.1) Periodico semestrale del Servizio Geologico d'Italia - ISPRA e della Società Geologica Italiana Geol.F.Trips, Vol.5 No.1.1 (2013), 73 pp., 65 figs. (DOI 10.3301/GFT.2013.01)

The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction of the Calabria-Peloritani Orogen 86° Congresso Nazionale della Società Geologica Italiana - Arcavata di Rende (CS), 18-20 settembre 2012

Rosolino Cirrincione, Eugenio Fazio, Patrizia Fiannacca, Gaetano Ortolano, Antonio Pezzino, Rosalda Punturo, Vanessa Romano, Valentina Sacco

University of Catania, Department of Biological, Geological and Environmental Sciences

Corresponding author e-mail address: [email protected] Responsible Director Editorial Board Claudio Campobasso (ISPRA-Roma) M. Balini, G. Barrocu, C. Bartolini, Editor in Chief D. Bernoulli, F. Calamita, B. 2 Gloria Ciarapica (SGI-Perugia) Capaccioni, Editorial Responsible W. Cavazza, F.L. Chiocci, Maria Letizia Pampaloni (ISPRA-Roma) R. Compagnoni, D. Cosentino, S. Critelli, G.V. Dal Piaz, C. D'Ambrogi, Technical Editor P. Di Stefano, C. Doglioni, E. Erba, publishing group Mauro Roma (ISPRA-Roma) R. Fantoni, P. Gianolla, L. Guerrieri, Editorial Manager M. Mellini, S. Milli, M. Pantaloni, Maria Luisa Vatovec (ISPRA-Roma) V. Pascucci, L. Passeri, A. Peccerillo, L. Pomar, P. Ronchi (Eni), Convention Responsible B.C. Schreiber, L. Simone, I. Spalla, Anna Rosa Scalise (ISPRA-Roma) L.H. Tanner, C. Venturini, G. Zuffa. Alessandro Zuccari (SGI-Roma) 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.2013.01 The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction of the Calabria-Peloritani Orogen R. Cirrincione - E. Fazio - P. Fiannacca - G. Ortolano - A. Pezzino - R. Punturo - V. Romano - V. Sacco geological fieldtrips2013-5(1.1)

INDEX Itinerary

Information DAY 1 Granitoid bodies intruded in the Aspromonte Peloritani Unit Riassunto...... 4 (APU) and the ductile shear zone (MSZ) Abstract...... 4 Stop 1.1 ...... 34 Stop 1.2...... 37 Informazioni generali...... 6 Stop 1.3...... 44 3 General info...... 6 Useful contacts...... 7 DAY 2 Madonna di Polsi Unit (MPU) surfacing in the Cardeto tectonic Excursion notes window (valley of S. Agata river) and the metamorphic zonation of the Unit (SU) 1 - Geological setting...... 8 Stop 2.1 ...... 48 Stop 2.2 ...... 53 2 - Structural framework of the Aspromonte Massif nappe-pile Stop 2.3 ...... 54 edific ...... 16 Stop 2.4 ...... 55 3 - Tectono-metamorphic and tectono-magmatic evolution of Stop 2.5 ...... 57 the Aspromonte Massif crystalline basement...... 19 Stop 2.6 ...... 58

Stop 2.7 ...... 59 index 4 - Madonna di Polsi Unit (MPU) ...... 20 Stop 2.8 ...... 61 5 - Aspromonte-Peloritani Unit (APU) ...... 24 Stop 2.9 ...... 63 6 - Stilo Unit (SU) ...... 28 References ...... 66

DOI: 10.3301/GFT.2013.01 geological field trips 2013 - 5(1.1)

4 information R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco Aspromonte, Orogene Calabro-Peloritano, zona di taglio, Orogenesi Alpina, zoneografia The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 Riassunto (Calabria meridionale), effettuata in occasione dell’86° Congresso nel Massiccio dell’Aspromonte L’escursione ad illustrare è volta Nazionale omonimo, cornice del Parco della Società Geologica Italiana, nella suggestiva tettono-metamorfica del basamento l’evoluzione diretta di alcune aree chiave, l’osservazione attraverso cristallino di questo settore dell’attuale catena appenninica, focalizzando l’attenzione sulla complessa storia ha guidato i polimetametamorfica-polifasica che, a partire almeno dal limite Precambriano-Cambriano, modellando altresì l’attuale assetto fisiografico principali processi petrogenetici delle rocce di basamento, dell’intero massiccio. (Sicilia) il settore meridionale dell’Orogene costituisce insieme ai Monti Peloritani Il Massiccio dell’Aspromonte a centrale nel Mediterraneo un segmento dell’attuale catena sud appenninica affiorante (Calabro-Peloritano), le fasi meso-cenozoiche dell’originale catena Ercinica sud europea durante seguito dello smembramento dell’orogenesi Alpina. può essere schematicamente descritta come un’articolata pila di del Massiccio dell’Aspromonte La struttura coperture sedimentarie falde tettoniche costituite da rocce di basamento metamorfico e frammentarie Le falde, dall’alto in basso corrispondono alle seguenti unità tettono-metamorfiche: l’Unità meso-cenozoiche. in tre finestre Quest’ultima unità affiora e l’Unità di Madonna Polsi. l’Unità Aspromonte-Peloritani di Stilo, a della struttura Al di sopra e Cardeto. Samo- Madonna di Polsi, tettoniche chiamate rispettivamente la successione silico-clastica oligo-miocenica della formazione Stilo-Capo d’Orlando che sutura falde troviamo le due falde tettoniche apicali. Quest’ultima formazione è parzialmente ricoperta in il contatto tra a tratti le verso evolvendo retroscorrimento dalla argille antisicilidi, che chiudono la sequenza a falde di ricoprimento, come ad esempio quelle riconducibili alla serie sedimentarie neo-autoctone, parti apicali con le sequenze ionico del massiccio aspromontano. sul versante ampiamente affioranti gessoso-solfifera, chiave: Parole metamorfica geological field trips 2013 - 5(1.1)

5 information R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco Aspromonte Massif, Calabria-Peloritani Orogen, shear zone, Alpine Orogeny, metamorphic The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 Abstract national park district, carried out for the field trip in the Aspromonte Massif within a suggestive The two-days the tectono-metamorphic history of is planned at illustrating 86° Congress of the Geological Society Italy, the metamorphic basement outcropping in this sector of southern Apennine chain trough direct obser- that, evolution sectors, focussing the attention on complex polymetamorphic-polyphase of some key vation the crystalline basement rocks petrogenetic evolution, driven have since the Precambrian-Cambrian boundary, The Aspromonte Massif massif physiography. features, producing the present-day as well the structural Mountains (Sicily) the southern sector of CPO (Calabria- (Calabria) constitutes together with the Peloritani Mediterranean Orogen), a segment of the actual southern Apennine chain outcropping in central Peloritani Alpine chain during Mesozoic-Cenozoic area due to the breakup of original Southern European Variscan orogeny. architecture of the Aspromonte Massif can be schematically described as a nappe-pile structural The overall sedimentary Mesozoic-Cenozoic by a fragmentary partly covered edifice made up by metamorphic terrains From top to the bottom tectonic slices of metamorphic units are named as follow: Stilo Unit cover. Unit (MPU). This last unit outcrops in three main Unit (APU) and Madonna di Polsi (SU), Aspromonte Peloritani The two uppermost tec- respectively. and Cardeto, Samo-Africo tectonic windows named as Madonna di Polsi, tonic slices are partly sutured by the Oligocene-Miocene silico-clastic Stilo-Capo d’Orlando formation (SCOF), which close the sequence of nappe- of the antisicilidi clays, in turn by the back-thrusting partly covered sedimentary sequences outcrop, at the top of sequence, neo-authoctonous pile tectonic stack. Finally, sedimentary sequences, widely outcropping along as for instance those represented by the Gessoso-Solfifera the Ionian flank of Aspromonte Massif. words: Key zonation geological field trips 2013 - 5(1.1)

6 information stops. - Field trip itinerary and location of - Field trip itinerary Fig. 1 R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 Informazioni generali 2 giorni Durata: dell'escursione (Fig. 1) Programma Giovanni Villa S. e arrivo: Partenza (RC) presso il piazzale antistante la stazione ferroviaria. 1°Itinerario: giorno) Villa S. Giovanni (RC), Montalto, Roberto (RC), S. Gambarie (RC) (pernottamento). 2° giorno) Gambarie (RC), Cardeto (RC), Salvo (RC), Melito Porto (RC). Giovanni Villa S. Indicazioni particolari Difficoltà escursione: medio-bassa; richieste particolari di assistenza (mobilità, alimentazione) saranno connesse alla disponibilità presso i luoghi visitati. General info 2 days Duration: (Fig. 1) Field trip programme Villa Departure and arrival: (RC) next to the Giovanni S. station square; railway geological field trips 2013 - 5(1.1)

7 information R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco Ente Parco Nazionale dell’Aspromonte Nazionale dell’Aspromonte Ente Parco Stefano in Aspromonte (RC) 1 – 89050 - Gambarie di S. Via Aurora, +39 0965 743 026 +39 0965 743 060; Fax Tel. E-mail: [email protected] www.parcoaspromonte.gov.it Website: CAI Club Alpino Italiano - Sezione Aspromonte Calabria (RC) 106 – 89127 - Reggio da Paola, Francesco Via S. E-mail: [email protected] www.caireggio.it Website: Group (MeIGePeG) Metamorphic and Igneous Geo-Petrology of Catania (Italy) at the University Corso Italia 57 -95129 Catania (CT) www.meigepeg.org Website: The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 Route: Route: Gambarie (RC) (night accommodation). (RC), Montalto, Roberto (RC), S. Giovanni Villa S. 1° day) (RC). Giovanni (RC), Villa S. Salvo Gambarie (RC), Cardeto Melito Porto 2° day) Additional information the support for peculiar requests will be strictly related to resources low-middle; Field trip difficult level: at each site. availability Useful contacts geological field trips 2013 - 5(1.1)

8 excursion notes - (a) Areal distribution of Alpine Fig. 2 et al. 2010; Cirrincione et al., 2011). et al. 2010; Cirrincione al., The present-day framework of the CPO framework The present-day oro- is mostly the result of Palaeozoic genic processes, renewed by the large-scale nappe and Alpine-Apennine tectonics, which also affected strike-slip ocean-derived part of the Mesozoic units and sedimentary sequences which locally produced a weak to perva- (Cirrincione metamorphic overprint sive 2008). et al., 2008, 2011; Fazio et al., The CPO is a composite segment of the Alpine chain, western Mediterranean mostly constituted by basement rocks multi- deriving from a poly-orogenic stage history which are currently or possibly Variscan, merged in several Pezzino, (e.g., sub-terranes older, belt in the central Mediterranean realm; (b) Mediterranean belt in the central map of Calabrian Geological sketch Orogen (CPO) (modified after Angì Peloritani R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 1 - Geological setting which represents one of the four main sectors The field trip area is located within the Aspromonte Massif, Orogen (CPO) (Fig. 2). From the north to south these sectors are: composing the Calabria-Peloritani the Mountains. Within the CPO, the Aspromonte Massif (Fig. 3) and Peloritani the Serre Massif, Sila Massif, than in Belt are recognisable in Sila and Serre Massifs, rather relics of the southern Variscan better preserved et Mountains, where a more intense Alpine reworking occurred (Pezzino the Aspromonte Massif and Peloritani 2008, 2011). 1994; Cirrincione et al., et al., 1991; Atzori 1990; Cirrincione & Pezzino, al., geological field trips 2013 - 5(1.1)

9 excursion notes - Geological sketch map of the Aspromonte Massif (after - Geological sketch Fig. 3 R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco Pezzino et al., 1990, 2008; Ortolano et al., 2005; Fazio et al., 2008). et al., 2005; Fazio 1990, 2008; Ortolano et al., et al., Pezzino cou- from order Lister, The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 1982; Atzori et al., 1984; Critelli, 1999; Ferla, et al., 1982; Atzori 2003; Micheletti et 2000; De Gregorio et al., 2011; Williams et al., 2007; Critelli et al., al., these basements were defini- 2012). Finally, thin by the Alpine-Apennine stacked tively in the central skinned thrusting events 2005; area (Ortolano et al., Mediterranean 2008). et al., Pezzino proposed different possi- Authors have Several ble paleo-geodynamic reconstructions of the & Alpine chains (Coward peri-mediterranean 1992; 1989; Vai, Dietrich, 1989; Dewey et al., 1998; 1992; Gueguen et al., Carmignani et al., 1999; Stampfli, 2000; Michard et al., Zeck, & 2003; Rosenbaum et al., 2002; Jolivet 2004; Franceschelli et al., 2005) starting et al., 2004; Franceschelli Ocean and other the closure of Tethys minor oceanic basins (AB: Algerian-Balearic basin) due to basin; LPB: Ligurian–Provençal the Africa–Europe convergence. position of of the pre-Alpine The restoration actually dis- terranes, Variscan the various area, is not persed around the Mediterranean because recent tectonics straightforward sea-floor pled with the spread of Tyrrhenian of the dismembered the initial framework have Alpine chain. It is therefore useful doing com- parisons between tectono-metamorphic evolu- rocks outcropping into differ- tions of Variscan area in ent sectors of the Mediterranean to establish potential connections between them geological field trips 2013 - 5(1.1) excursion notes 10 etrographic and petrological analogues of the meta- etrographic R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 and eventually compare their inferred P-T-t trajectories. compare their inferred P-T-t and eventually P morphic rocks outcropping in the Aspromonte Massif could be found in the Variscan terranes of the Sardinian- terranes morphic rocks outcropping in the Aspromonte Massif could be found Variscan basin. adjacent to the Calabria plate before opening of Tyrrhenian Corsica block, which was system questions are still debated about the geodynamics of Calabria-Peloritani several In this scenario, the processes leading to their thrusting and that include the origins of crystalline basement terranes, emplacement in to the Apennines, and their subsequent exhumation. geologists, whose pioneer been debated by many problems have the above Since the end of 19th century, 1904). Such studies resulted Cortese, 1896; De Lorenzo, based on autocthonistic theory (e.g., mapping was compared to the “usual” order, of the Calabrian crystalline basement rocks showing an inverse in a framework of deep gravity the hypothesis thereby leading to advance sequence recognised in other crystalline terranes, 1904). due to mega-refolding (De Lorenzo, rise to local overthrows processes, which gave Lugeon & Argand, for a few analytical studies at the beginning of last century (e.g., except years, many For only partially accepted. For 1913), a fold-nappe model for the genesis of CPO was 1906; Limanowsky, stable massif bordered by orogen as a relatively (1935) interpreted the Calabria-Peloritani example, Quitzow of plate tectonics the advent Later, by constant uplift since the Paleozoic. mobile boundaries, characterized proposed by Staub (1951). Based on this terranes the nappe interpretation of Calabria-Peloritani validated with interpretation, the Sorbonne Geodynamic School directed by Glangeaud (1952), in collaboration which consisted geology, new interesting insights into Calabria-Peloritani et al. (1961) provided Grandjaquet African thrust front, represented composed of: a) an advanced in the reconstruction of a pre-orogenic framework b) an oceanic hiatus (Sangineto Line); by the sialic block of Serre Massif ( crustal thinned zone); c) weakly deformed Apennine continental crust. studies (from local to regional scale) geological and petrographic structural, several In the last forty years, followed. Based on the geosynclinal model, early works by Ogniben (1960; 1969) interpreted have Calabride Complex as an internal crystalline basement made of four nappes sutured by Oligocene late-orogenic piling up of the Sicilide basin pelite sequence. by the retrovergence partly covered flysch deposits, successively Ogniben (1973) tried to find a correlation between the palinspastic model based upon geosynclinal theory and et al. (1961), which ascribed the crystalline Calabria- the plate-tectonic reconstruction of Grandjacquet modifying previous interpretations and inferring rela- orogenic segment to the Alpine system s.s., Peloritani tionships among Calabria, Corsica, Liguria and the western Alps. A review study by Amodio-Morelli et al. from both orogen consisting of units derived (1976) interpreted the Calabride Complex as a Europe-verging geological field trips 2013 - 5(1.1) excursion notes 11 R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 the oceanic crust and continental crystalline nappes of Austroalpine domain. The Complex would studies (e.g., the Apennine-Maghrebian chain. Recent of the Alpine chain overriding represent a fragment complex relations among different sectors of the 2005) demonstrated 2001; Ortolano et al., Bonardi et al., of original crustal segments that caused separation fragmentation Orogen, due to Jurassic Calabria-Peloritani Indeed, each segment consists of nappe-emplaced slices tectonic nappes during the Alpine orogeny. into several of units. In this scheme, the subdivision into basement, whose different classifications caused a plethora correlate the crystalline it difficult to unequivocally 1982) makes Tortorici, northern and southern sectors (e.g., interpretation of the role Alpine of this orogenic system because the controversial basement terranes 2005). In the northern sector, 2001; Ortolano et al., Bonardi et al., metamorphism in these two sectors (e.g., extending from the Sangineto line to Catanzaro trough, Alpine ophiolite units are present; they 2000; Dijk et al., in age from 60 to 35 Ma (Schenk, 1980; Van metamorphism ranging by HP-LT characterized by the line, is characterized extending to the Taormina the southern sector, 2001). In contrast, et al., Rossetti clear evidence about early alpine metamorphism. absence of ophiolite units; this does not provide role in a key It is to be pointed up that the reconstruction of alpine tectonics Aspromonte Massif plays been proposed by different interpretations have the understanding of regional geodynamics and that contrasting Authors, leading to two main hypothese. refers to the geological outline proposed by Bonardi et al. (1982; 1984a, 1984b), Graessner The first hypothesis & Schenk (1999) and Messina et al. (1990; 1992). According to their proposal, the Aspromonte Massif is com- to amphi- low-greenschist posed of three tectonic slices as follows: the uppermost Stilo Unit made up Variscan bolite facies metapelites. The Aspromonte Unit occupies an intermediate geometrical position and is composed bodies, partly to totally re- granitoid amphibolite-facies metamorphic rocks intruded by late-Variscan of Variscan 1984a; Bonardi et al., area of the sanctuary Madonna di Polsi; during the Alpine orogenesis (e.g., equilibrated metapelites character- Platt & Compagnoni, 1990). The lowest tectonic slice is represented by greenschist-facies it outcrops into two tectonic windows near to the vil- metamorphism with an Alpine overprint; by Variscan ized considered the extension of this sequence was lages of Cardeto and Africo (Fig. 3). In the area Cardeto, & Schenk, 1980; Graessner position (Bonardi et al., Mandanici Unit that outcrops in Sicily the same structural considered an incertae sedis unit affected by Variscan 1999). The succession that surfaces in nearby Africo was 1987). Messina & Somma (2002), interpreted the lowest tectonic slice as com- metamorphism (Bonardi et al., with only the Cardeto Unit tectonic units (Africo and Cardeto Units, respectively), Variscan posed of two separate being affected by a weak alpine metamorphic overprint. geological field trips 2013 - 5(1.1) excursion notes 12 - Skematic cross section showing the main - Skematic Fig. 4 Unit), MU (Mandanici Unit). tectonic slices composing the Alpine edifice of 2008). et al., Aspromonte Massif (modified after Pezzino A possible correlation of this nappes piling with Peloritani Mountains in Sicily is also assumed. SU (Stilo Unit), APU Unit), MPU (Madonna di Polsi (Aspromonte-Peloritani R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 Alternatively, according to Pezzino et al. (1990, 1992), Fazio (2005), Ortolano et al. Cirrincione et al. (1990, 1992), Fazio according to Pezzino Alternatively, of the Aspromonte Massif is result et al. (2008), the geological framework (2008), and Fazio defined by previous Authors; b) the intermediate Aspromonte-Peloritani stacking of: a) the Stilo Unit, as it was Unit, mostly corresponding to the Aspromonte Unit of previous Authors; c) underlying metamorphic affected by alpine metamorphism. This sequence outcrops at the three tectonic sequence, exclusively been named after the localities where they surface (i.e. Cardeto and Africo villages, as windows, which have to the interpretation by first group of Authors, it would correspond area). Referring well as, Madonna di Polsi metapelite sequence of the Africo and Cardeto Unit, together with Alpine re-equilibrated to the Variscan 1984a; of the Aspromonte Unit (Bonardi et al., zone Platt & Compagnoni, 1990). These interpretations for the suggested two different tectonic frameworks Orogen, which southern sector of the Calabria Peloritani as follows: a) it represents a stacked can be synthesized to the basement rocks linked structure of several (partly to totally) during locally reworked cycle, Variscan Alpine shearing phase during late an extensive Oligocene - early Miocene orogenic exhumation (Platt & Compagnoni, 1990); or b) it is the result of a complete basement Variscan involving Alpine orogenic cycle, sedimentary sequences. These rocks as well Mesozoic thinned sequences correspond to a portion of an active continental margin which, following subduction, was along a late extruded along the suture of a collision zone in a shear zone Oligocene-early Miocene retrograde 1990). et al., compressional regime (Pezzino et al. (2008), by taking into In this context Pezzino (2005), Ortolano et al. account recent studies by Fazio et al. (2008), as well new structural., (2005) and Fazio petrological and thermobarometric data, proposed, for a new simplified geological and the Aspromonte Massif, model (Fig. 4), where the lowest metamorphic structural geological field trips 2013 - 5(1.1) excursion notes 13 deformation in 4 ), related to pro- 1-2 shearing phase, can be considered consistent with olsi Unit (MPU). As a consequence, this model deformation, pervasively overprinting the previous overprinting deformation, pervasively 3 3-4 R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco ), associated with D 3-4 The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 an uplifting tectonic channel linked with a high displacement rate. This last event evolved to D evolved This last event with a high displacement rate. an uplifting tectonic channel linked Aspromonte Massif resembles the classical corner-flow model (e.g., Shreve & Cloos, 1986). The geo-petrologi- Shreve model (e.g., Aspromonte Massif resembles the classical corner-flow et al. paths reconstructed by Ortolano et al. (2005), Cirrincione (2008), and Fazio cal features and P-T of the MPU metapelites, are consistent with this the tectono-metamorphic evolution (2008) which constrain (M are recognised: a) the former cycle model. Indeed two polyphase metamorphic cycles structures characterized by compressive exhumation along a mylonitic shear zone, was responsible for rapid was shear zone, exhumation along a mylonitic by compressive structures characterized decompression path, the D extrusion along a quasi-adiabatic gressive subsiding of sedimentary successions forming the MPU tectonic wedge, which attained relatively HP subsiding of sedimentary successions forming the MPU tectonic wedge, which attained relatively gressive of thinned con- can be considered consistent with under-plating peak metamorphic conditions (up to 1.35 GPa), tinental crust; b) the later one (M sequences are unified into a sole unit, named Madonna di P facilitates the comparison with the Peloritani Mountain belt (Cirrincione et al., 2011) and, at the same time, Mountain belt (Cirrincione et al., facilitates the comparison with Peloritani contributes to our understanding of the location this orogenic sector in wider geodynamic puzzle area. western Mediterranean Evidence for a complicated structure and polyphase tectono-metamorphic history of the Southern CPO, different Authors (e.g. Bouillin, has been obtained by many events and pre-Variscan Alpine, Variscan involving 1994; Graessner et al, 1990, 1994; Acquafredda al., 1982; Atzori 1978, 2000; Del Moro et al., 1987; Ferla, 2008, 2008; Fiannacca et al., 2007; Bonardi et al., 2000; De Gregorio et al, 2003; Micheletti al., et al., mentioned the geological 2012). As above 2011; Williams et al., 2010; Appel et al., 2013; Heymes et al., et al. (1990, 2008), Ortolano (2005), Cirrincione (2008) scheme arising from the studies by Pezzino the uppermost the presence of three polyphase metamorphic complexes: et al. (2008) hypothesizes and Fazio Unit (APU), and the underlying Madonna the intermediate Aspromonte-Peloritani Stilo Unit (SU) at the top, by different metamorphic histories, are Unit (MPU). The last two units (APU and MPU), characterised di Polsi metamorphic to the south, high-grade Farther shear horizon. along a thick mylonitic tectonically overlapped Mountain belt and represent the of Messina up to the Peloritani rocks of the APU extend across Strait sequence of the phyllite the Variscan This unit overlies highest unit of the nappe-edifice cropping out in Sicily. 1975). called Alì sequence (Lentini & Vezzani, cover, Mandanici Unit and a terrigenous-carbonate Mesozoic sub-greenschist to greenschist metamorphic Both the Mandanici Unit and Alì sequence exhibit neo-alpine 1994). et al., ages; Atzori assemblages dated at 26 ± 1 Ma (white mica Rb-Sr et al. (2008) for exhumation of HP rocks the by Pezzino In detail, the tectonic model hypothesized geological field trips 2013 - 5(1.1) excursion notes 14 This tectonic reconstruction also 1. R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco ) in a range of T=350-480 °C and P=0.32-0.62 GPa, well constrained in well constrained of T=350-480 °C and P=0.32-0.62 GPa, ) in a range 4 (APU) and the thinned crust (MU) with its sedimentary cover. This kind of subduction involved (APU) and the thinned crust (MU) with its sedimentary cover. s.s. The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 low-greenschist facies conditions (M low-greenschist both the sedimentary cover (e.g., MPU and AU) and underlying basement rocks (e.g., MU), presently forming MPU and AU) underlying basement rocks (e.g., (e.g., both the sedimentary cover The early Alpine compressional regime was the tectonic wedge that constitutes most of Aspromonte Massif. of new structures causing different interference patterns with pre-existing ones accompanied by: 1) development Alpine-type metamorphism affecting both basement rocks (MU) basement rocks, and 2) HP-LT in the Variscan the Mandanici Unit, which had previously experienced rel- (MPU and AU). Unlike sedimentary cover and overlying represents, event 1994), this HP-LT et al., metamorphism (Atzori Variscan-type greenschist-facies low-P atively for the MPU rocks, oldest recognizable evidence of metamorphism M the MPU metapelites. By taking into account 60-70° counter-clockwise rotation of the Aspromonte Massif since the MPU metapelites. By taking into account 60-70° counter-clockwise 2004), & Lister, 1994; Rosenbaum late Oligocene, affecting the entire CPO (Scheepers, 1994; Scheepers et al., orogenic can be related to accretionary processes responsible for Oligocene-Miocene Africa-verging this cycle consistent with change from compressional to extensional tectonics The previous interpretation was transport. of the CPO from Sardinia block (Gueguen with final separation for the CPO since Late Burdigalian, coeval brittle normal extensional tectonics is expressed as NE-SW 1998). In the southern sector of CPO, et al., 1982). 1981; Tortorici, fault system (Ghisetti & Vezzani, transtensional faulting, accommodated by a NW-SE probably represented by the Mandanici ence of a thinned continental margin, whose crystalline basement was is represented by the sedimentary cover Mountain belt. The Mesozoic Unit (MU) that crops out in the Peloritani convergence Following Mountains and the MPU in Aspromonte Massif. Alì series (AU) in the Peloritani between the con- at the transition became active between the African and European plates, a subduction zone tinental crust explains why no mineralogical assemblages of Variscan relics occur within the metamorphic rocks of MPU, as well relics occur within the metamorphic rocks of MPU, assemblages of Variscan no mineralogical explains why as the geometric position of this complex below APU crystalline tectonic nappe. Along with progressive and African plates, the tectonic wedge com- between the Eurasian to convergence incremental shortening linked (late Alpine phase). shallower crustal levels out toward driven posed of metapelites the MPU was and the APU MU (Cirrincione & Pezzino, block and the MU, the MPU-AU between the APU and MPU, rocks widespread in the Aspromonte Massif by the mylonitic 1994). Evidence of this exhumation is provided HP assemblages crystallization superposed over Mountains, and by the presence of retrograde and Peloritani within this tectonic 2005). Finally, 1994; Ortolano et al., et al., 1991, 1994; Atzori (Cirrincione & Pezzino, Mountains Alì sequences outcropping in the Peloritani reconstruction, the original location of Mesozoic The tectonic model here proposed (after Pezzino et al., 2008 and Cirrincione et al., 2011) is based on the pres- 2008 and Cirrincione et al., et al., The tectonic model here proposed (after Pezzino Exhumation of the deepest rocks was sustained by activation of shear zones (neo-Alpine phase), which developed (neo-Alpine of shear zones sustained by activation Exhumation of the deepest rocks was geological field trips 2013 - 5(1.1) excursion notes 15 R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 (Sicily) is constrained. This series, according to Cirrincione & Pezzino (1991) and Atzori et al. (1994) is inter- (1991) and Atzori This series, according to Cirrincione & Pezzino (Sicily) is constrained. thinner of the Mandanici Unit, since wedge was preted as the weakly metamorphosed sedimentary cover Mountains, a few kilometers from the Alì series, carbonate rock bands interbedded In the Peloritani southward. 1994). (Cirrincione & Pezzino, of the Mandanici Unit show a weak Alpine metamorphic overprint into phyllites of sedimentary cover been interpreted as the fragmentary et al. (1984), they have In agreement with Atzori the Mandanici Unit. The pre-Alpine geodynamic setting would see a thinned continental margin made of Variscan basement and geodynamic setting would see a thinned continental margin made of Variscan The pre-Alpine during the been involved, Such a margin would have terrigenous-carbonate sedimentary cover. Mesozoic phase, in a subduction process underneath the European continent; this would be responsible meso-Alpine of the Mandanici Unit, as well for Alpine affecting metamorphic terranes for the metamorphic overprint in its sedimentary cover. northward, metamorphism, with increasing gradient extrusion finally exhumed following syn-convergent During the Oligocene-Miocene, entire block was model of Chemenda et al. (2000). The Aspromonte Unit acted as a back-stop consistent with the corner-flow in the final involved to the Alpine accretionary wedge along European continent; this unit, therefore, was for the a new geodynamic framework providing event), (i.e. mylonitic stages of the Alpine orogenic cycle Orogen. Calabrian-Peloritani et al. (2008) to crystalline basement rocks outcropping in Sicily (i.e. Extending the model proposed by Pezzino belt may could be made. The entire Peloritani considering the MPU analogous to AU) some considerations 1994; et al., (Fig. 5) with different tectono-metamorphic histories (Atzori be subdivided into two complexes 2011). The lower complex, exposed in the southern part of 1994; Cirrincione et al., Cirrincione & Pezzino, Cambrian–Carboniferous sequences, which were affected by belt, comprises volcano-sedimentary Peloritani by unmetamor- sub-greenschist to greenschist facies metamorphism and which now are covered Variscan sediments. The upper complex, in the north-eastern part of belt, consists phosed Mesozoic–Cenozoic greenschist to amphibolite facies Unit), showing Variscan two units (Mandanici Unit and Aspromonte–Peloritani alpine greenschist facies metamorphic overprint metamorphism, which in part are also affected by a younger cover of a metamorphosed Mesozoic–Cenozoic 1994). Fragments et al., 1991; Atzori (Cirrincione & Pezzino, Unit. It has been correlated (AU) occur interposed between the Mandanici Unit and Aspromonte–Peloritani tectonic Alpine unit exposed in several 2011) to the exclusively 2008 and Cirrincione et al., et al., (Pezzino windows in the Aspromonte Massif (MPU). as well of the nappe-pile edifice Aspromonte Massif, framework In the following sections structural tectonic slices will be briefly outlined. features of the various and structural as the main petrographic geological field trips 2013 - 5(1.1) excursion notes 16 ) a – Fig. 5 ) simplified 2011). Schematic profile of Peloritani Mountains based on the geological discussed overview in the text; b geological map of Peloritani Mountains and Aspromonte Massif, where upper and lower Complexes outcrop (after Cirrincione et al., R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 2 - Structural framework of the Aspromonte Massif nappe-pile edifice 2008 and references therein), the Aspromonte Massif is made et al., According to our interpretation (Pezzino by different tectono-metamorphic up of three main tectonic slices corresponding to units, characterised type (Fig. 6). The tectonic slices are the uppermost by tectonic contacts of various and separated evolutions unit (APU) metamorphism, the intermediate Aspromonte-Peloritani Variscan Stilo Unit (SU) with exclusively Unit (MPU) affected and Alpine metamorphism, the lowermost Madonna di Polsi with both Variscan by Alpine metamorphism. exclusively and the Upper Oligocene - Lower Miocene turbidite sequence of Stilo-Capo conglomerates Syn-collisional sequence of both the Aspromonte Massif and d’Orlando formation (SCOF) cap the tectono-stratigraphic at the strata 1997). Pelagic et al., 1988; Cavazza 1980, 2001; Cavazza, Mountains (Bonardi et al., Peloritani geological field trips 2013 - 5(1.1) excursion notes 17 MPU consists of lower-green- characterised by a polyphase ret- characterised APU (Pezzino et al., 1990, 2008; et al., APU (Pezzino – Schematic relationships between the Aspromonte Massif Alpine edifice. pile-nappes consituting the framework of pile-nappes consituting the framework Fig. 6 R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen thrusting (Argille Varicolori of Ogniben, 1960) or as a thrusting (Argille Varicolori olistostrome of clay-rich mélange (Cavazza et al., 1997). et al., mélange (Cavazza olistostrome of clay-rich DOI: 10.3301/GFT.2013.01 schist to lower-amphibolite facies metapelitic metapsammitic sequences, schist to lower-amphibolite alpine metamorphism which has not been detected into the overlying rograde 2008). 2005; Cirrincione et al., Ortolano et al., mainly dedicated to the tectonic contact being the first day of the field trip, roughly the itinerary Following we will be first focusing the attention on salient between the two lowermost tectonic units, APU and MPU, tectonic contact between them. This is features of these two units, in particular on the mylonitic top of the sequence have been interpreted as the result either top of the sequence have of back- large sedimentary deposits are the Lower Pleistocene The youngest i.e. high planes) presently (named “piani alti”, marine terraces testifying a strong uplift of the south- located at 1300 m a.s.l., ern Calabria region by means of recent faults forming horst and structures. graben to low The uppermost Stilo unit is made up of low greenschist- metamorphic rocks (Crisci et al., amphibolite-facies Palaeozoic & Schenk, 1999). Late 1984a, Graeßner 1982; Bonardi et al., magmatic bodies, intruded into metapelites produced Variscan and a thermal metamorphic aureole (biotite, muscovite andalusite blastesis). The SU lies through a brittle tectonic con- Unit (APU), which is made the Aspromonte-Peloritani tact over up of amphibolite-facies metamorphic rocks intruded by late by both locally overprinted granitoids, peraluminous Variscan at about 36-22 Ma Alpine type metamorphism which developed 2010). 2008; Heymes et al., (Bonardi et al., marks the tectonic contact between horizon A thick mylonitic metamorphic to middle- grade the APU and underlying low- tec- Unit (MPU) outcropping in several rocks of Madonna di Polsi tonic windows: a) the Cardeto metamorphic complex, which Unit (Pezzino 2008); b) the Madonna dei Polsi et al., 1980; Fazio outcrops in the western sector (Bonardi et al., 2005). complex (Ortolano et al., 1990, 2008) and c) the Samo-Africo et al., geological field trips 2013 - 5(1.1) excursion notes 18 ), charac- 1MPU ), linked to the ), linked m ) (Bonardi et al., 1987; Pezzino et al., 1990; et al., 1987; Pezzino ) (Bonardi et al., ), with associated typical shear structures on m 2APU R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco ) and a pervasive stretching lineation (L ) and a pervasive m The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen , Fig. 7) evolving to a retrograde crenulation phase (D to a retrograde , Fig. 7) evolving 1APU DOI: 10.3301/GFT.2013.01 both meso- and microscopic scale (i.e. ribbon-like quartz, sigmoid biotite and muscovite flakes, rotating flakes, quartz, sigmoid biotite and muscovite both meso- and microscopic scale (i.e. ribbon-like which allowed the sense of shear structures into feldspar grains), and bookshelf-sliding porphyroclasts to be terised by a Grt+Ms+Pg+Bt±Pl±Amph±Tur±Rt±Ttn assemblage. A subsequent shear phase (D terised by a Grt+Ms+Pg+Bt±Pl±Amph±Tur±Rt±Ttn exhumation of the basement rocks, is responsible for the emplacement of the APU above the MPU (Pezzino et the MPU (Pezzino exhumation of the basement rocks, is responsible for emplacement APU above by deep seated shear structures, produces a pervasive shear phase, characterised 1990, 2008). This mylonitic al., foliation (S mylonitic marked by a wide horizon of mylonitic rocks showing distinctive features of a ductile shear zone, affected by features of a ductile shear zone, rocks showing distinctive of mylonitic by a wide horizon marked et and subsequent to the nappe-emplacement (Pezzino a series of deformation and blastesis episodes linked these rocks show locally a static blastesis of 1990, 2008). Nearest to the shear horizon al., probably induced by the adiabatic uplift chloritoid+quartz+sericite+oligoclase±biotite±staurolite±paragonite 2005). 1990, 2008; Ortolano et al., et al., connected to the exhumation of chain (Pezzino of the APU upon garnet-mus- paragneisses contact between the sillimanite-andesine-bearing The mylonitic 1990) is widely exposed in the north- et al., bearing schists of the MPU (Pezzino and garnet-amphibole covite the same south-east it is also possible to observe eastern part of the Aspromonte Massif (Fig. 3). Towards metapelites to upper greenschist facies mylonitic contact between the APU and underlying lower- mylonitic outcropping in the southernmost tectonic window of massif (Ortolano complex (SAC), of the Samo-Africo Here, the Cardeto observed. in the Cardeto area, a similar tectonic situation was 2005). Westwards, et al., 2008, 2009, 2010), essentially made by garnet mica-schists and et al., metamorphic complex (CMC) (Fazio from greenschist to lower amphibolite facies, surfaces into two minor tectonic windows characterised phyllites APU terrains. tectonic contact with the overlying by a cataclastic to mylonitic 2008), which thrusted the APU onto MPU, 2005, Cirrincione et al., (Ortolano et al., event The mylonitic and metamorphic history of these two units (Fig. 7). Before this marks the beginning of joint structural evolutions. the two units underwent distinct tectonic-metamorphic event, most commmonly recognised in the intermediate unit (APU) relates Indeed, the earliest metamorphic evolution metamorphism and is testified by the alignment of relic isoclinal folding Variscan retrograde to a polyphase HT-LP (D Puglisi & Pezzino, 1994; Ortolano et al., 2005). By contrast, the earliest evolution of the MPU is characterised the earliest evolution 2005). By contrast, 1994; Ortolano et al., Puglisi & Pezzino, metamorphism (Late early-Alpine to lower-amphibolite-facies lower-greenschist HP prograde by a relatively 2008, 2009) et al., Cretaceous?). This evidence is well testified in the metapelitic Cardeto tectonic window (Fazio where it is possible to recognise relics of isoclinal folds related the first deformational phase (D geological field trips 2013 - 5(1.1) excursion notes 19 R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco established. The thickness of the shear zone, where several established. The thickness of the shear zone, from a few ranging variable, been planned, is rather stops have meters to about 0.6 km (east Mt. Montalto). The observed microstructures indicate a deformation regime from `brittle- et 2009; Fazio to plastic (Cirrincione et al., plastic transition’ of recrystallization 2007, 2010), with the development al., quartz aggregates, blastesis of structures (i.e. polycrystalline in the pressure shadows of rotated new quartz and mica grains in the deepest portions of unit. porphyroclasts) 3 - Tectono-metamorphic and tectono-magmatic evolution of the Aspromonte Massif crystalline basement and assisted by petrographical field-investigation Structural minerochemical analysis of the rock types composing three tectono-metamorphic units constituting the Aspromonte Massif in order to high- been here summarized nappe-pile edifice have stages which light the main blasto-deformational evolutionary evolution the specific pressure-temperature characterized have of the single unit. According to most Authors, the dominant metamorphism in due to southern sector of the CPO basement rocks is generally in the southern Aspromonte However, orogeny. the Variscan fab- clearly the variscan only the SU metapelites display Massif, in the APU and MPU ric, whereas the dominant fabrics observed deforma- alpine mylonitic due to pervasive rocks are generally et al., 1987; Pezzino tion of Late Oligocene age (Bonardi et al., 2005). 1990, 1992; Platt & Compagnoni, 1990; Ortolano et al., HT- relics found in the APU are related to variscan Pre-mylonitic relics are LP metamorphism whereas MPU pre-mylonitic metamorphism. early-alpine ascribed to early LT-HP The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen – Tectono-metamorphic evolution of evolution – Tectono-metamorphic Fig. 7 al., 2005). al., Aspromonte-Peloritani Unit (APU) and Madonna di Aspromonte-Peloritani Unit (MPU) outcropping within the Samo- Polsi Africo tectonic window (modified after Ortolano et DOI: 10.3301/GFT.2013.01 geological field trips 2013 - 5(1.1) excursion notes 20 mylonitic 3 ) is occasion- . 2 2 ), which commonly caused developed syn-tectonically developed 3 2 ), ilmenite, epidote, chlorite and ). A new surface (S 1 0.15-0.02 XPyr 0.74-0.43 XAlm R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco . A subsequent shear event produced a pervasive mylonitic foli- mylonitic produced a pervasive . A subsequent shear event 1 0.38-0.07 ) consists of LT-HP metamorphism (0.95-1.35 GPa at 400°-600 °C), metamorphism (0.95-1.35 GPa ) consists of LT-HP 1 XGrs (Fig. 9). 2 0.23-0.05 ) ranging from 480 to 610 °C and 0.50 to 0.95 GPa linked to late Oligocene linked from 480 to 610 °C and 0.50 0.95 GPa ) ranging of isoclinal folds produced during the first deformational phase D 3 1 The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen (mean 122°/22° in the right-hand-rule notation), a stretching lineation Ls (mean 225°/20° as dip direc- (mean 122°/22° in the right-hand-rule 3 crystallization episode. These minerals grew along with crenulation cleavage S grew along with crenulation cleavage crystallization episode. These minerals 2 DOI: 10.3301/GFT.2013.01 tion/dip, DD/D), syn-tectonic intrafolial asymmetrical folds evolving to rod structures Lr (mean 135°/8°, DD/D), asymmetrical folds evolving DD/D), syn-tectonic intrafolial tion/dip, S-C fabrics and an oblique foliation. A fourth phase caused asymmetrical to isoclinal folding of the S foliation and was followed by a fifth brittle deformational phase that generated a pervasive fracture cleavage fracture a pervasive followed by a fifth brittle deformational phase that generated foliation and was into thrust planes (Fig. 8). (mean 105°/85°, RHR) and folds evolving The early recognised metamorphic episode (M with the second deformational phase D ation S metamorphism (M Syn-mylonitic A weakly developed assemblage composed of white mica, plagioclase, chlorite and ilmenite corresponds to the A weakly developed M 4 - Madonna di Polsi Unit (MPU) schists (Qz + Wm Pl ± Bt Grt constituting the MPU consists of muscovite-garnet The main rock-types schists (Qz + Wm Anf Pl± Bt ± Chl Ep Grt Ti Rt), Chl ± Ep Ti Rt), muscovite-amphibole schists, schists (Qz + Wm Bt ± Pl Chl Rt Grt), and subordinate chlorite-muscovite biotite-muscovite amphibole fels and amphibolites (Anf ± Pl Qz Bt Grt Ep Ti Chl Wm), leucogneiss (Qz + Wm ± Bt Anf) and marbles (Cc + Qz Wm Flog Ab ± Ti Ep opaques). major deformational episodes (Figs. 7, 8): a first isoclinal folding, indicated by MPU rocks show evidence of five produced an axial plane foliation (S layers, hinge relics of quartz within phyllite white mica characterized by moderate to high-phengite content (phengite substitution range: 3.04 to 3.35 Si to high-phengite content (phengite substitution range: by moderate white mica characterized just This assemblage is usually preserved Local growth of apatite, plagioclase, biotite and amphibole occur. p.f.u.). whereas it is seldom preserved defining inclusion trails, (Fig. 10) as minerals inside the garnet porphyroblasts along the axial planar foliation S ally recorded that formed due to crenulation of S (1994) and Cirrincione et al. (2008), occurred which, according to Puglisi & Pezzino related to crustal thickening, (Fig. 9) is represent- to this event assemblage linked mineralogical during early Alpine deformation. The relevant ed by rich-spessartine garnet (XSps transposition of earlier surfaces. White mica (phengite substitution range: 3.01 to 3.24 Si p.f.u.) and biotite laths 3.01 to 3.24 Si p.f.u.) of earlier surfaces. White mica (phengite substitution range: transposition Alpine deformation caused deep-seated compressional shear zones along with uplift and exhumation of the crys- Alpine deformation caused deep-seated compressional shear zones foliation (S mylonitic talline basement rocks occurs. All of the samples show a marked geological field trips 2013 - 5(1.1) excursion notes 21 ). ) h 0.27-0.01 0.21-0.04 XPyr 0.85-0.52 ) syn-D1 isoclinal a ) syn- to late-D3 rod, e XAlm garnet porphyroblasts. 1 0.28-0.02 parallel to this foliation, alter- parallel nating with mm-thick ribbon- quartz bands, represent like the main syn-shear minerals. White mica in these mylonites usually shows the classical asymmetric fish shape, which the syn-mylonitic verifies to the nature of its tails parallel shear plane. Other minerals grown during this phase are plagioclase (albite paragonite, to oligoclase), ilmenite, epi- dote, chlorite, tourmaline, amphibole (essentially tscher- makites), and garnet with low spessartine content (XSps XGrs Usually, these garnets appear as these garnets appear Usually, small crystals surrounding larg- er M ) mesoscopic aspect of a garnet-bearing b ) syn-D5 mesoscopic verging fold (B5 axis); ) syn-D5 mesoscopic verging g ) Structural features and related mineral assemblages features and related mineral ) Structural i R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco ) shear bands (c’ surfaces) and s-c texture developed during the D3 shear phase; ) shear bands (c’ surfaces) and s-c texture developed d The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen ) post-mylonitic syn-D4 fold from the area of Madonna di Polsi; syn-D4 fold from the area of Madonna di Polsi; ) post-mylonitic ) effects of shearing. Asymmetric folds give a dextral shear sense (top to N-E of in current geographic a dextral ) effects of shearing. Asymmetric folds give f – Main deformational features of MPU. a-h) Field evidences of deformational phases (D1-D5): – Main deformational features of MPU. c Fig. 8 5 = deformational phases; M1-4 metamorphic episodes. sketched for the three tectonic windows (Madonna di Polsi Unit, Samo-Africo complex and Cardeto metamorphic complex). D1- Unit, Samo-Africo for the three tectonic windows (Madonna di Polsi sketched folding of S1 (B1 axis). S3 mylonitic foliation is parallel to the transposed S1; to the transposed foliation is parallel folding of S1 (B1 axis). S3 mylonitic foliation. Sample collected near the tectonic contact between APU and deriving from an asymmetric folding of the mylonitic lineation (L3r), which is usually the most evident in marked generate unit in the area of Cardeto village. Rods overlaying the field; folds. of syn-D5 verging brittle thrust representing the evolution coordinates); phyllite; phyllite; DOI: 10.3301/GFT.2013.01 geological field trips 2013 - 5(1.1) excursion notes 22 4 3 parallel to parallel 4 metamorphism 4 doesn’t show any 5 – Isoclinal folds D4 within schist of MPU. Fig. 11 straints, pressure-tempera- straints, ture paths depicted for samples collected into the three tectonic windows of by a MPU are characterized (Fig. 12). clockwise trajectory obtained using dif- Results ferent techniques indicate that, during the progressive of the tectonic- thickening wedge, the pelitic sediments the axial surface of these folds are plagioclase, white of 350-480°C range mica, chlorite and epidote. A P-T has been obtained for the M and 0.32-0.62 GPa developed coevally with respect to the fourth defor- coevally developed mational phase, which is responsible for the asym- foliation S metric to isoclinal folding of the mylonitic (Fig. 11). Minerals forming schistosity S (Fig. 11). Minerals assemblage. mineralogical blastesis because it essentially developed in a brittle blastesis because it essentially developed regime, producing only cataclastic effects superposed rocks. Based on this chemical con- on mylonitic Porphyroblasts enveloped by the mylonitic foliation, by the mylonitic enveloped Porphyroblasts with unambiguous pre-kinematic features, are usual- amphiboles and feldspars; ly garnets, with sporadic from sub-mm to cm scale. diameter ranges The assemblage grown during M The last deformational episode D R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco – Blasto-deformational relationships of MPU The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen metapelites (after Ortolano et al., 2005). metapelites (after Ortolano et al., – Garnet of MPU rocks showing Fig. 9 Fig. 10 area (parallel polars, 50 X). area (parallel complex inclusion trails marked essentially marked complex inclusion trails by alignment of quartz and ilmenite crystals from the Cardeto village within a phyllites DOI: 10.3301/GFT.2013.01 geological field trips 2013 - 5(1.1) excursion notes 23 ) geological c ) integration of estimated P-T paths (black arrows) and of estimated P-T ) integration d R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco ) Geological-structural map of SAC and sample locations; map of SAC ) Geological-structural b ) Geological sketch-map of Aspromonte Massif and location Samo-Africo ) Geological sketch-map a – Fig. 12 representative sample along A–A′–A″ geological profile of c. sample along A–A′–A″ representative profile A-A’-A’’ of map b; profile A-A’-A’’ with related location of each interpretation of APU and MPU metamorphic evolution Complex (SAC). Complex (SAC). 1 ). 1 meta- devel- 3 3 ) attained 1 , representing deformation 4 1 crenulation cleav- The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen 2 axes) and related axes) 1 ) at relatively high pres- ) at relatively 1-2 DOI: 10.3301/GFT.2013.01 age, commonly symmetric, represents a subsequent stage of deformation. The third M metamorphic event 400-600°C at 0.95-1.35 mainly coin- This event GPa. cided with D (MPU) were metamorphosed (M leading to S morphic episode is situated in of 0.50-0.95 GPa the PT range and 480-610°C. Starting from the thermal peak of MPU metamorphic rocks, the P-T paths follow nearly adiabatic decompression, probably linked to a fast exhumation process, to D which evolved and is related to under-plat- with ing (early Alpine event) of isoclinal development folds (B sure. Early recognized meta- sure. Early recognized (M morphic event axial-planar foliation (S the retrograde part of the path. the retrograde oped coevally with shear zones oped coevally constituting the uplifting tec- tonic channel. The M Successive micro-folding of S Successive geological field trips 2013 - 5(1.1) excursion notes 24 folding omonte This stage APU 1 consisting of static ± K-feldspar. This stage K-feldspar. ± s.s , connected to the first Hercynian deformational stage 1E R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco (Sicily) has the largest areal extension of outcrop. The main (Sicily) has the largest areal extension of outcrop. represented by paragneiss and micaschist (Qz + Pl Bi Ms ± represented by paragneiss and syn-kinematic growth of quartz, oligoclase, biotite, almandine s.s. ). Regarding the pre-mylonitic tectono-metamorphic evolution of the Aspr tectono-metamorphic evolution the pre-mylonitic ). Regarding APU 1 The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen ), are found aligned along the mylonitic foliation. According to Bonardi et al. (1987), the D ), are found aligned along the mylonitic APU 1 DOI: 10.3301/GFT.2013.01 Peloritani Unit (APU) it may be described as the result of earliest amphibolite facies metamorphism. Unit (APU) it may Peloritani assemblages consisting of quartz, andesine, almandine garnet (with rel- by relic mineralogical is characterised low grossular and high spessartine contents), sillimanite, biotite, muscovite atively (E1), marked by lepidoblastic micaceous levels alternated with quartz-feldspar lenses (Puglisi & Pezzino, 1994). lenses (Puglisi & Pezzino, alternated with quartz-feldspar by lepidoblastic micaceous levels (E1), marked aggre- of microcline or sometimes by eterogranular Augen gneisses, are constituted mainly by poikilitic eyes layers. of lepidoblastic biotite + muscovite gates of microcline, quartz and oligoclase, surrounded by trails The amphibolites and amphibolic gneisses, are frequently composed of alternating bands rich in hornblende and, by lighter bands enriched in quartz, plagioclase and biotite. melanocratic prevalently plagioclase layers 2008) et al., Unit (Pezzino In the field trip area APU is sandwiched between lowermost Madonna di Polsi by strong alpine and the uppermost Stilo Unit (Figs. 3, 6, 12). The rocks of APU are locally characterised close to the tectonic contact with underlying basement rocks foliation, which becomes pervasive mylonitic deformational phase relics of early isoclinal folding, related to the first Variscan Nevertheless, of the MPU. (D 5 - Aspromonte-Peloritani Unit (APU) Unit (APU), cropping out in the Aspromonte Massif of southern Calabria and The Aspromonte–Peloritani Mountains north-eastern part of the Peloritani rock-types which constitute APU are mainly rock-types Sill + Kfs ± Grt And) and by augen gneiss (Qz Pl Bi Ms), weakly to strongly foliated leucogneiss (Qz + Pl ± Kfs Bi Ms), amphibolites and amphibole gneiss (Amph Qtz Ttn Ep) intruded trondhjemites (Qz + Pl Bi Ms ± Kfs Sill Grt) and strongly peraluminous by weakly peraluminous (Qz + Pl Kfs Ms Bi ± Sill And Crd) of late Hercynian age. and granites leucogranodiorites types and a grano- structure in the less evolved granoxenoblastic and micaschist show a prevalent Paragneiss types, such a structure is in the most evolved blastic structure with evidence of subordinate leucosome layer to the foliation S layering by sub-parallel characterized event is ascribable to the Variscan orogeny, peaking at 330 Ma, which produced the oldest identifiable orogeny, is ascribable to the Variscan event metamorphic surface (S partly evolved to a retrograde phase characterised by greenschist facies assemblage phase characterised to a retrograde partly evolved muscovite blastesis of coarse-grained garnet (with lower grossular and spessartine contents) and andalusite. A subsequent mylonitic shearing stage garnet (with lower grossular and spessartine contents) andalusite. A subsequent mylonitic The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction of the Calabria-Peloritani Orogen R. Cirrincione - E. Fazio - P. Fiannacca - G. Ortolano - A. Pezzino - R. Punturo - V. Romano - V. Sacco gave rise to a pervasive overprint producing a new mineralogical assemblage characterised by quartz, albite, low phengite white mica, clinozoisite, ilmenite, chlorite and biotite. The attitudes of the Sm foliation have an geological fieldtrips2013-5(1.1) average strike direction of N45, with dips of 20°-80° to the SE or NW. The stretching lineation (Lm) is oriented approximately SW-NE, plunging 15-35° alternatively SW or NE in both units. In the present-day geographic coordinates, several types of kinematic indicators show a top-to-NE sense of shear also well observable in the mylonitic micaschist of the underlying MPU. Under the microscope, the metapelites of the APU show a syn-kinematic assemblage (Fig. 13) of Qtz + Pl1 + Bt1 + Wm1 + Grt1 ± Kfs1 ± Sil1 defining the S1APU surface, replaced by widespread coarse-grained recrystalli- sation of Wm2, which developed during late-stage rehydration of the Kfs1+Sil1 assemblage. Locally, late por- phyroblasts of And1 also occur. During the D1APU event, amphibolites and amphibole-bearing gneiss developed a Qtz + Pl1 + Bt1 + Hbl1 ± Grt1 assemblage, with local retrograde flakes containing oligoclase (Pl2) and acti- nolite (Amph2). The microcrenulation of S1APU represents the subsequent deformation phase (D2APU), locally producing a S2APU schistosity, given by the aligned growth of Qtz + Pl3 + Wm3 ± Bt2 ± Grt2 ± Chl1 ± And2. The subsequent deformation phase (Dm) developed during the Late Oligocene-Early Miocene overthrust of the APU upon the MPU, along a deep-seated compressional shear zone. In the rocks of both units, the effect of the consequent mylonitization produces both a pervasive mylonitic foliation (Sm) and a pervasive stretching lin- 25 eation (Lm). Locally, Dm totally replaces the pre-existing foliations and produces a great reduction in grain size, especially in the leucocratic gneiss of the APU. A post-mylonitic phase produces isoclinal folding of previous fabric and a new axial plane foliation (S4a, Fig. 14).

In order to reconstruct the P-T path of the APU excursion notes metamorphic evolution (Fig. 12), Cirrincione et al. (2008) performed a detailed study by means of pseudosection approach applied to paragneisses close to the mylonitic tectonic contact with the underlying MPU. The first selected samples exhibits a well-preserved HT/LP prograde mineral assem- blage evolution with a weak mylonitic overprint; Fig. 13 – Blasto-deformational relationships of APU (after Ortolano et al., 2005). while the second one shows strong syn-mylonitic

DOI: 10.3301/GFT.2013.01 geological field trips 2013 - 5(1.1) excursion notes 26 R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco greenschist facies re-equilibration over the relict of ear- over greenschist facies re-equilibration lier amphibolite facies assemblage. tectono-metamorphic estimates for the Variscan P–T Aspromonte of the rocks APU in Central evolution (Ortolano between 650–675°C at 0.4–0.5 GPa Massif range 2008). A final widespread 2005, Cirrincione et al., et al., under decreasing temperatures episode of hydration emplacement probably caused by the massive (480°C) was late-Variscan of metaluminous to strongly peraluminous data on micas; Rottura at about 290 Ma (Rb–Sr granitoids et al. Atzori also occur. overprints 1990). Tertiary et al., (1990) indicated a common metamorphic history for augen from the north-eastern gneisses and associated paragneisses with Rb/Sr ages on micas of 280–292 Ma, inter- Peloritani metamorphism. preted as cooling ages after the Variscan 2000) for similar et al., U–Pb monazite ages (Graeßner of the Aspromonte Massif amphibolite facies paragneisses indicated a metamorphic peak at 295 to 293 ± 4 Ma (with for the base of conditions of 620°C at ca. 0.25 GPa P–T and xenotime U–Pb ages and whole-rock and mineral Rb–Sr ages; Borsi & Dubois, 1968; Rb–Sr U–Pb ages and whole-rock mineral and xenotime metamorphic peak was nearly synchronous with the bulk of granitoid intrusions at 303–290 Ma nearly synchronous with the bulk of granitoid metamorphic peak was peak temperature of 690–800°C at 0.55–0.75 GPa (Graessner et al., 2000 and reference et al., (Graessner of 690–800°C at 0.55–0.75 GPa peak temperature The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen – Isoclinal folds (D4) within a biotite axial plane schistosity (crossed polars). Fig. 14 sillimanite paragneisses of APU developing a new of APU developing sillimanite paragneisses DOI: 10.3301/GFT.2013.01 Borsi et al., 1976, Schenk, 1980; Del Moro et al., 1982; Graessner et al., 2000; Fiannacca et al., 2008). 2000; Fiannacca et al., et al., 1982; Graessner 1976, Schenk, 1980; Del Moro et al., Borsi et al., emplacement and granitoid et al. (2000) the massive & Schenk (1999) and Graessner According to Graessner occurred under static responsible for a regional scale late-stage metamorphism. This event crystallization was almost all the assemblages erasing recrystallisation of the mineral conditions and resulted in extensive Caggianelli et (e.g., preserved evidence of previous tectono-metamorphic stages, which are now only rarely 2011). Despite the absence of detailed geochronological constraints, 2010; Appel et al., 2007; Angì et al., al., rocks of the Aspromonte Massif and Peloritani paths inferred for the medium-to high-grade clockwise P–T–(t) and during early- been considered to be consistent with processes of crustal thickening Mountains have upper crust), coeval with the lower crust (exposed in the Serre Massif, southern Calabria), the latter charac- with the lower crust (exposed in Serre Massif, upper crust), coeval by aterized therein). This (zircon, monazite geological field trips 2013 - 5(1.1) excursion notes 27 con- indi- and Schenk indicate a late R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 verted into augen gneisses during the Variscan metamorphic evolution. The only previous geochronological metamorphic evolution. into augen gneisses during the Variscan verted ages from Mountains are hornblende Ar–Ar in the APU of northern Peloritani events cations of pre-Variscan of hornblende formed generation two amphibolites that were interpreted as mixing ages between a younger at ca. 600 Ma with older cores, and a titanite U-Pb age of 1.8–1.6 Ga from one those samples (De Gregorio (1989) rocks are long known in southern Calabria, where Schenk & Todt 2003). Pre-Variscan et al., that zircon U-Pb ages for gneisses from different crustal levels reported several (1990) have reported latest Micheletti et al. (2007) have More recently, event. (0.6–0.5 Ga) crust-forming Neoproterozoic protoliths of augen gneisses bodies from the Precambrian to early Cambrian SIMS zircon ages for the granitic Unit, which are the same of those found by Fiannacca et Aspromonte Massif side of the Aspromonte-Peloritani counterparts. al. (in press) for the Peloritanian weakly to strongly peraluminous The metamorphic rocks of APU are diffusely intruded by late-Variscan 2008). Late-Variscan 2005a, 2005b, 1993; Fiannacca et al., et al., 1982; Rottura et al., (D’Amico granitoids in two main groups: a suites (representing ca. 70% of the from the CPO can be framed granitoids to granodiorites quartz-diorites exposed rocks) mostly composed of metaluminous to weakly peraluminous and a second suite comprising weakly to strongly peraluminous forming batholits in the Serre and Sila Massif, and were probably are late to post-tectonic which form small scale intrusions. The granitoids granitoids leucocratic 1990; Caggianelli et et al., connected to an extensional regime (Rottura emplaced along ductile shear zones are granitoids, small plutons, composed of weakly to strongly peraluminous 2000, 2007). Only relatively al., middle-Variscan collisional stages, followed by crustal thinning, granitoid intrusion and unroofing during collisional stages, followed by crustal thinning, granitoid middle-Variscan 2010). 2007; Angì et al., 2004; Caggianelli et al., et al., Festa extensional stages (e.g., late-Variscan 1984; Ioppolo & et al., Atzori history of the APU basement rocks, some Authors (e.g., As for the pre-Alpine Mountains, where- origin for those cropping out in the Peloritani Puglisi, 1989) proposed an entirely Variscan 1994) suggested that most of 1978, 2000; Bouillin, 1987; Acquafredda et al., as other Authors (e.g. Ferla, De Gregorio et al. (2003) suggested that the basement. Most recently, those rocks were part of a pre-Variscan terranes and Variscan pre-Variscan Unit resulted from the amalgamation of various Aspromonte Peloritani portions origin of widely separated Evidence for a pre-Variscan Orogeny. during the last stages of Variscan Mountains has now been obtained by zircon SHRIMP U-Pb of the basement north-eastern Peloritani 2013). The lat- 2012; Fiannacca et al., and augen gneisses (Williams et al., studies of amphibolite facies para- Cambrian age, of ~ 545 Ma, for both the tim- a late-Neoproterozoic-early indeed provided ter two studies have later and of the intrusion original granitoids, metamorphism in the paragneisses ing of high-grade geological field trips 2013 - 5(1.1) excursion notes 28 R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 exposed within the medium high-grade basement of the Aspromonte–Peloritani Unit. Among these granitoids, basement of the Aspromonte–Peloritani exposed within the medium high-grade magmatism by most of the of the late-Variscan trondhjemites, not included in the frame weakly peraluminous previous Authors, crop out as small plutons and stocks, other than dm to m discordant sub-concordant 2005a). The emplacement of one the largest trondhjemite bodies, (Fiannacca et al., leucosomes and dykes Mountains has been dated at 314±4 Ma (SHRIMP U-Pb zircon ages; cropping out in the north-eastern Peloritani magmatism in 2008; Fig. 15), predating of 10-14 Ma the bulk strongly peraluminous Fiannacca et al., been have granitoids 2008). The strongly peraluminous 2000; Fiannacca et al., et al., Graessner the APU (e.g., a mixed 1990) or as having et al., 1982; Rottura et al., (D’Amico interpreted as either typical S-type granites 1991, 1993). A recent petrological and SHRIMP zircon study of the Villa S. et al., mantle-crust origin (Rottura from anatexis of a metasedimentary evidence for their derivation has provided leucogranodiorites Giovanni showed a strict similarity between the in press) have source and newly acquired zircon data (Fiannacca et al., and those of the detrital zircon in paragneisses age clusters of the inherited zircon in leucogranodiorites could be dominant components of the Mountains suggesting that those paragneisses from the Peloritani and magma source. A similar genetic link has been found between the same paragneisses leucogranodiorites 2012; Fiannacca et al., (Williams et al., protoliths of the APU augen gneisses from Peloritani the granitoid 2013). 6 - Stilo Unit (SU) of this field trip is focused on the uppermost unit pile-napped edifice, Stilo Unit The second day Alpine metamorphic re-equi- (SU) which, differently from the two underlying units, did not undergo to any in cataclastic shear zone only involved, it was Indeed, during the Oligocene-Miocene evolution, libration. processes localised at its base, producing cataclastic rocks, currently visible the tectonic contact between SU and APU. In the Aspromonte Massif (Fig. 2), uppermost Stilo Unit is made up of low-greenschist-to-low-amphibo- by a dis- bodies and covered granitoid rocks, intruded by late-to-post-orogenic Paleozoic lite-facies Variscan continuous sedimentary succession made up essentially of limestones, dolostones and marls. (Qtz+Ms+Ep+Pl±Grt) more diffused in the Aspromonte The basement rocks (Fig. 16) are mostly phyllites passing to micaschists (Qtz+Bt+Ms+Grt±St±And) and paragneisses Massif southern sector, sequence, presently of the deeper part psammitic-pelitic (Qtz+Pl+Bt+Ms+Ep±Amph±Grt) representative the Aspromonte Massif northern sector. majorly outcropping correspondent towards geological field trips 2013 - 5(1.1) excursion notes 29 – SHRIMP Fig. 15 ) From left to right: ) From left to right: ) From left to right: 7 Ma. zircon data for APU and gneisses granitoids (after Williams et al., 2012; Fiannacca et al., 2008, 2013). a cathodoluminescence images, U-Pb concordia and age- diagram probability plot for zircon from the grains sample leucogranodiorite VSG-1. The emplacement age is 300 ± 4 Ma. b cathodoluminescence images, U-Pb concordia and age- diagram probability plot for zircons from the augen gneiss sample FIU-11. The emplacement age of the protolith is granitoid 545± 5 Ma. c cathodoluminescence images, U-Pb concordia and age- diagram probability plot for zircons from the biotitic FIU-7. The paragneiss deposition age of the protolith of greywacke is 545 ± the paragneiss R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 geological field trips 2013 - 5(1.1) excursion notes 30 1S – Main ) the crenu- 2S Fig. 16 mm). deformational features of the Stilo Unit (SU). Microphotos at the bottom right corner depict mylonitic near paragneisses Chorio village (scale bar 0.5 ); (D 1S ) isoclinal folding (B 1S ) with an associated microfolds hinge lin- 2S R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco ) structures related to this event are not easily recognizable into true ) structures related to this event mS ), involving the formation of a new axial plane foliation (S ), involving 0S ) a further folding episode producing chevron geometry type folds (without associ- 4S ) a shear deformational phase leading to the formation of mylonitic rocks, with development ) a shear deformational phase leading to the formation of mylonitic 3S , which creates a new crenulation cleavage foliation (S , which creates a new crenulation cleavage The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen ); (D 1 2S DOI: 10.3301/GFT.2013.01 metapelites (i.e. phyllonites), but they are evident in the interbedded fine grained albite-paragneisses and albite-paragneisses but they are evident in the interbedded fine grained metapelites (i.e. phyllonites), (D phyllites; quartz-rich ated blastesis) from meter to decameter wavelength scale, probably related to the overthrusting at upper scale, probably related to the overthrusting ated blastesis) from meter to decameter wavelength Unit. the Aspromonte-Peloritani of the entire Stilo Unit above crustal levels The main deformational events (Fig. 16) recognized in the SU and entirely ascribable to the Variscan orogeny in the SU and entirely ascribable to Variscan (Fig. 16) recognized The main deformational events in press) are: (D et al., 2004; Fazio 1984; Fazio, 1982; Bonardi et al., (Crisci et al., axis) of a previous surface (S of a new mylonitic foliation (S of a new mylonitic lation of S eation (B geological field trips 2013 - 5(1.1) excursion notes 31 – Metamorphic zonation of the Stilo Unit – Metamorphic zonation Fig. 17 Aspromonte Massif (after Fazio, 2004). Aspromonte Massif (after Fazio, (SU) recognized in the southern sector of (SU) recognized ) ms R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco , Wm ms replacing garnet porphyroclasts The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 wrapping pre-kinematic rounded albite porphyro- wrapping association mineralogical clasts. Retrograde (Chl+Wm+Qtz±Bt±Pl) The metamorphic equilibria related to the Variscan meta- The metamorphic equilibria related to the Variscan within rocks of the Stilo are well-preserved morphic cycle by Unit. In this area, SU resulted indeed characterised highlighted by the with a metamorphic gradient terrains (chlorite, occurrence of four metamorphic isograds which can be eas- biotite, garnet, staurolite-andalusite), miner- of some key ily mapped in the field via in-curves & Schenk, 1999) (Fig. 17). als (Graessner between deformational stages and crystal- Relationships as follows. The sedi- lization episodes are summarized mentary surface, appears at mesoscopic scale as quart- isoclinally folded, leading to the formation of layers zose in a new axial plane foliation (S1s); it is still preserved of the the upper and less metamorphosed levels cropping out in the metapelitic sequence (chlorite zone) area near the village of Chorio southern investigated assemblage (Qtz+Ilm+Wm+Bt+Pl) (Fig. 18). The sin-S1s is accompanied by the growth of different minerals (Chl+Ep+Grt+St) according to the metamorphic increasing meta- conditions (biotite, garnet, staurolite-andalusite and the chemical bulk composition of morphic zone) such as chlorite (Chl), white mica (Wm) system. Minerals on the crenulation cleav- and biotite (Bt) were observed during the age foliation (S2s). The developed recognized third deformational phase of shear (D3s), was near Chorio paragneisses only in the albitic fine-grained by the sin-kine- villages, and is marked Lorenzo and S. matic growth of chlorite and white mica (Chl geological field trips 2013 - 5(1.1) excursion notes 32 , and 1s 2s , Wm//S 1s – Microstructural ). 3s ) were distinguished. More and S was also observed (Fig. 19). also observed was observations The petrographic thin sections of several allowed the reconstruction of a inside metamorphic zonation the metapelitic sequence of static 2s Fig. 18 S features of a phyllite from the chlorite features of a phyllite of the Stilo Unit (SU). Three zone (S been recognized foliations have ) have a lesser amount of Si and Fe+Mg compared to a lesser amount of Si and Fe+Mg ) have 1s R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco besides static crystals (Wm ms ). Trioctahedral micas are exclusively siderophyllites. Almandine is siderophyllites. micas are exclusively ). Trioctahedral 3s the Stilo Unit. This zonation is exposed between the villages of Chorio the Stilo Unit. This zonation (chlorite, and , it is made by four metamorphic zones distinguished by the zones) biotite, garnet, staurolite-andalusite temperature a northward revealing of new index minerals, appearance increase. the presence if sillimanite crystals occur in the SU paragneisses, Even & as suggested by Graessner of a fifth sillimanite metamorphic zone, not here sustained because none Schenk (1999) for the same area, was body of sillimanite bearing schist near the intrusive of the observed from lower metamorphic zones, shows relics of minerals Punta d’Atò suggesting their pertinence to a different metamorphic unit, the Unit. Aspromonte Peloritani groups of white micas Wm//S Three different texturally Wm//S phengitic compositions were observed in albitic paragneissic samples in albitic paragneissic phengitic compositions were observed of white showing shear deformation features. The first generation micas (sin-D which are growing during the shear phase that of third generation (D The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen – Garnet crystal (parallel Fig. 19 southern coast of Calabria. polars, 50X) with inclusion trails suggesting a syn-crystallization clockwise of SU from rotation within a phyllite village area near the the DOI: 10.3301/GFT.2013.01 geological field trips 2013 - 5(1.1) excursion notes 33 – P-T paths of the Stilo Unit (SU) – P-T Fig. 20 the Serre Massif (Angì et al., 2010). the Serre Massif (Angì et al., reconstructed via pseudosection tool for samples collected in the area of 2012) and et al., Aspromonte Massif (Fazio )were 3 ) in the 1 deformation R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Sacco 1s deformation phase, which causes the develop- 3s The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 phase developed under metamorphic conditions (M phase developed obtained for D ment of the shear zone. the more abundant component into garnet with moderate content of spessartine and subordinate amount the more abundant component into garnet with moderate maps is clearly visible a dou- largest garnets (800 microns of diameter) on X-ray grossular and pyrope. For by enriched manganese and calcium ble stage of growth, often visible also under microscope, characterized cores compared to iron and magnesium enriched rims. An increase in spessartine content the outer region An also observed. was of garnet in contact with matrix minerals visi- internal foliation of small aligned quartz and apatite grains ble inside the inner shell of garnets is lacking in outer shell. are almost entirely albitic plagioclase with an increas- Feldspars ing anorthite content from chlorite to staurolite-andalusite of oligoclase in the with first appearance metamorphic zone, a common ripidolitic composition. Chlorites have garnet zone. of metamorphic conditions principal deformation PT ranges phases of the Stilo Unit, are shown in Fig. 20. D range of 0.35-0.7 GPa of pressure and 480-550 °C tempera- of 0.35-0.7 GPa range metamorphism described of Variscan-type ture, characteristics Variscan Authors for european and north-African by several of 570°C (M and temperature belts. Pressure of 0.7 GPa geological field trips 2013 - 5(1.1) itinerary 34 – Route of first day) Villa S. Giovanni (RC), S. Roberto (RC), S. Giovanni Villa S. of first day) – Route R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Fig. 21 (RC), Montalto, Gambarie (RC) (night accommodation). (RC), Montalto, (~35 vol. %) + (~35 vol. The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 DAY 1 Granitoid bodies intruded in the Aspromonte Peloritani Unit (APU) and the Montalto ductile shear zone (MSZ) for the (Fig. 21), except The following itinerary times the first Stop (Fig. 22), will touch several tectonic contact between the two distinct tectono-metamorphic units (APU and MPU) occurring at the bottom of Aspromonte by a Massif edifice. They are separated (Montalto shear zone, shear zone mylonitic of pervasively by a wide level MSZ) marked rocks, showing asymmetric foliated mylonitic pre- structures that transpose folds and shear, vious metamorphic foliation. Stop 1.1: The Villa S. Giovanni leucogranodiorites at Melia S. Roberto coordinates: Geographic Lat: 38°12’39’’ N; Long: 15°41’45’’ E; Altitude: 187 m.a.s.l. intruded in Lithotypes: Leucogranodiorites migmatitic paragneisses assemblage:Mineralogical Pl Qtz (~35 vol. %) +Kfs (~15 vol.%) +Bt (~8 %) +Kfs (~15 vol.%) Qtz (~35 vol. %) ± %) + Sill (~1 vol. %) +Ms (~6 vol. vol. And ± Crd Grt geological field trips 2013 - 5(1.1) itinerary 35 ) Mica aggregates with c ) euhedral to subhedral plagioclase to subhedral ) euhedral a ) Muscovite rich of fibrolitic sillimanite ) Muscovite – features of VSG Microstructural ) euhedral to subhedral zoned plagioclase zoned to subhedral ) euhedral d b Fig. 23 nicols, 20x). R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Petrographic and microstructural features (Fig. 23): and microstructural Petrographic for rocks, sometimes heterogranular Medium-grained crystals. Rocks K-feldspar the occurrence of cm-sized a weakly foliated and have locally, are isotropic or, texture with to sub-hypidiomorphic hypidiomorphic plagioclase and biotite, subhe- to subhedral euhedral microcline and moslty anhedral to anhedral dral Plagioclase crystals commonly quartz and muscovite. show simple twinning and a nicely defined idiomor- addition- microcline may Tartan-twinned phic zoning. be simple twinning, or perthites, may ally display poikilitc including plagioclase, biotite and quartz. Biotite mostly occurs in single platelets, at places The lat- muscovite. by, intergrown with, or overgrown platelets, sometimes in asso- sudhedral ter forms rare interstitial more commonly, ciation with biotite or, patches often including abundant sillimanite needles. symplectites are also muscovite-quartz Fine-grained leucogranodiorites. leucogranodiorites. crystals, with simple twinning (in the centre of image) surrounded by and a barely visible concentric zoning, (crossed quartz grains and strongly fractured anehdral nicols, 5x); quartz and microcline. The microcline crystals with anhedral crystal is partly bordered by biotite-muscovite-sillimanite aggregates (crossed nicols, 5x); crystals (crossed biotite typically enclosed in muscovite nicols, 5x); rounded quartz crystals. Sillimanite also inclusions wrapping (crossed occurs as widespread needles in the quartz grains The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen – The at S. leucogranodiorites (Stop 1.1). Roberto Fig. 22 DOI: 10.3301/GFT.2013.01 geological field trips 2013 - 5(1.1) itinerary 36 – Outcrop view of the VSG granitoids. Fig. 24 R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano . Contacts with the paragneiss wall rocks (mineralogical wall . Contacts with the paragneiss 2 The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 assemblage: Pl + Bt Qtz ± Ms Kfs Sill Crd) are usually sharp and discordant. Country rock enclaves, as well rocks. Micro-xenoliths, are common inside the granitoid from cm-scale to about 5 meters in size, the latter consisting of aggregates formed by rounded pla- restites of mm to cm size, strongly peraluminous also occur commonly. by muscovite-K-feldspar-sillimanite, gioclase and quarz wrapped setting, probably along exten- magmas were all emplaced in a post-collisional granitoid The CPO late-Variscan common. Quartz is mostly present as highly large grains. relatively fractured Sillimanite is often present and particularly abundant in some samples, where it occurs as large fibrolitic aggregates enclosed in patches, or as smaller scale the muscovite aggregates and single needles also in other phases. The main accessory phase mineral oxides. Fe-Ti are zircon, monazite and tiny are mostly unaltered, with only a lit- Rocks tle amount of sericite and chlorite replacing On the feldspars and biotite, respectively. all the rocks are intensely frac- contrary tured, at the microscope to outcrop scale (Fig. 24). (VSG) leucogranodi- Giovanni The Villa S. orites originated from the late-Variscan magmatism affecting calcalkaline granitoid This magmatism produced 10-13 kilometre-thick zoned the CPO in upper Carboniferous-Early Permian. to strongly peraluminous quartz-diorites batholiths, comprising metaluminous to weakly peraluminous of isolated plutons, stock and dykes Calabria, as well smaller-scale in northern and central syenogranites, 2005a, 2008), and of trondjemites, documented only in the APU (Fiannacca et al., weakly peraluminous 1982; et al., scattered along the whole CPO (D’Amico leucotonalites to monzogranites, strongly peraluminous 2008). 2003; Fiannacca et al., 1993; Caggianelli et al., et al., Rottura of which represent one the granitoids, belong to the strongly peraluminous The VSG leucogranodiorites an area of about 40 km largest bodies covering geological field trips 2013 - 5(1.1) itinerary 37 R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 sional shear zones (e.g., Rottura et al., 1990; Caggianelli et al., 2007). Muscovite and biotite Rb-Sr cooling and biotite Rb-Sr 2007). Muscovite 1990; Caggianelli et al., et al., Rottura (e.g., sional shear zones suggesting to the Authors ages of 286-282 Ma were obtained by Del Moro et al. (1982) for the VSG granitoids, an emplacement age of about 295 Ma. A SHRIMP zircon U-Pb 300.2 ± 3.8 Ma has been recently ID-TIMS 2008), in agreement with the monazite and xenotime obtained for the same rocks (Fiannacca et al., plutons of et al. (2000) for the strongly peraluminous ages of 303-302 ± 0.6 Ma obtained by Graessner sector of the Aspromonte Massif, cropping out in the northern and central-southern and Punta d’Atò, respectively. an example of the undeformed protoliths mylonitic could provide The VSG leucogranodiorites part of the Aspromonte Massif during latest stages Alpine leucogneisses formed in the central 2010). Indeed, differently from the isotropic to slightly foliated Heymes et al., Orogenesis (33-28 Ma; e.g., rocks, were locally together with their amphibolite facies wall granitoids, other late-Variscan VSG granitoids, cut, for 2008). Ductile shear zones et al., (Pezzino shear zones retrogressed along neo-alpine and variably foliation and to partial isotopic of a mylonitic leading to the development granitoids example, the Punta d’Atò 2010). Light-colored total fusion age of 235±0.2 Ma; Heymes et al., (Ar-Ar resetting of magmatic muscovite assemblages and relic and with mineralogical defomed granitoids, gneisses similar to the Puntà d’Atò mylonitic in the Montalto Shear Zone crop out extensively with those of the VSG granitoids, features comparable textural the leucogneisses of MSZ are result a 2009). In particular, 1990; Cirrincione et al., et al., (Pezzino almost completely the original magmat- reworking that obliterated and intense mylonitic particularly pervasive together with a porphyroclasts, K-feldspar the occurrence of cm-sized features. Nevertheless, ic textural similarity with bulk rock composition of the MSZ leucogneisses and with observed strongly peraluminous results consistent with the possibility that undeformed protoliths of granitoids, the deformed Punta d’Atò granitoids. strongly peraluminous been “VSG-type” late Variscan leucogneisses could have the mylonitic Stop 1.2: Mylonitic paragneisses and leucocratic gneisses (APU) of the Montalto Shear Zone (MSZ) outcropping at the panoramic site of Pietra Impiccata coordinates: Lat: 38°09’54’’ N; Long: 15°55’24’’ E; Altitude: 1760 m.a.s.l. Geographic of amphibolites gneisses with minor layers and leucocratic by banded paragneisses Lithotypes: Mostly given from centimetre-decimetre to metre scale. and amphibole-gneisses with thickness varying rocks, which belong to APU (Fig. 7a). They are characte- features: Medium to high metamorphic grade Structural and annealed the former metamorphic foliation. A Lm foli- foliation (Sm) which developed by a mylonitic rized rocks. The next deformation feldspar-bearing on the Sm foliation, mostly affecting quartz- ation develops geological field trips 2013 - 5(1.1) itinerary 38 140°/20°SW – Alternation laminated Fig. 26 isoclinal fold axes. between gneisses leucocratic and mylonitic exhibiting paragneisses isoclinal folding (centimetric scale bar). The stretching lineation appears dispersed around post-mylonitic R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano The APU outcrop of this Stop (Figs. 25-26) is characterised foliation oriented about mylonitic by pervasive stretching lineation at about (azimuth/dip) and a marked 185°/18° (dip direction/dip). A gneissic fabric outlined by Hand samples feldspar augen up to 1 cm is widely observed. – (Stop 1.2). Montalto shear zone The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen Fig. 25 DOI: 10.3301/GFT.2013.01 The upper unit (APU), made up of medium-to-high-grade metamorphic rocks (paragneiss, mica schist, augen metamorphic rocks (paragneiss, The upper unit (APU), made up of medium-to-high-grade plutonic rocks, is gneiss, amphibolite and amphibole gneiss) intruded by late Variscan gneiss, leucocratic on the APU affects metamorphism. The Alpine overprint Variscan-type by polyphase retrograde characterized all rock suites. event (Dm+1) affected both Sm and Lm, producing the Lm+1 intersection lineation, parallel to the axes of the to the axes (Dm+1) affected both Sm and Lm, producing the Lm+1 intersection lineation, parallel event isoclinal folds (Fig. 7d). gneisses: (Qtz+Pl+Kfs+Wm±Bt±Tur); (Qtz+Pl+Kfs+Wm±Sil±And); leucocratic paragneisses Petrography: amphibolites (Horn+Pl+Qtz±Ttn). mostly include chlorite, visible at the next Stop, the lower metapelite sequences of MPU, By contrast, gneiss schists; amphibole schist, leucocratic and amphibole-muscovite garnet-muscovite epidote-muscovite, early Alpine HP metamorphism rang- by prograde These sequences are characterized and marble are minor. retrograde affected by the same Neo-Alpine facies, successively to low-amphibolite ing from low-greenschist APU. the overhanging that involved shear zone geological field trips 2013 - 5(1.1) itinerary 39 – Highly laminated ortho-gneisses Fig. 27 near the Cardeto village (see stop 2.2). of APU with an evident lineation on the main area. This foliation (Sm) at the Mount Fernia lineation (195°/5° or 20°/5° in dip direction/dip notation) is due to a closely spaced folding of the foliation (190°/15° in right hand rule) and is to hinges of these micro-folds as occur parallel R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano well as pegmatitic lenses characterised by well as pegmatitic lenses characterised flakes of mica are frequently observed. flakes The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 Eastward with respect to this Stop, in the Mount Fernia area in the Mount Fernia with respect to this Stop, Eastward (Lat: 38°06’58.83” N; Long: 16°01’3.74” E; Altitude: 1100 m.a.s.l.) the same tectonic contact between rocks of Unit (APU) and the metapelites of Aspromonte Peloritani (Fig. 27), is mylonites window (MPU), generating Samo-Africo also well exposed. show a well-defined compositional layering characterisedshow a well-defined compositional layering by representing layers, and quartz-rich alternating feldspar- the mylonitic to the parallel rich-layers foliation. Tourmaline main foliation as centimetre-sized (up to 3 cm) form sigma- large tourmaline grains Sporadically consist of small type objects. Other interbedded dark layers garnet (diameter lower than 500 microns) ordered with- sized in the foliation plane. natu- (MSZ) represents an excellent The Montalto shear zone compositional and microstructur- site for studying textural, ral et sheared rocks (Fazio al modifications within progressively 2010). 2007, Cirrincione et al., al., In a recent study Cirrincione et al. (2010) selected the within leucogneisses of APU in Montalto shear zone mylonitic (Figs. increasing strain by progressive a domain characterised relationships between the bulk seis- 28-33) in order to reveal features which define the mic anisotropy and fabric-related Usually between them a parallel anisotropy. bulk textural to this rule is The exception is observed. towards behaviour dataset, by sample M4 which, represented, in the investigated although is the most deformed one, registers lower value This fact can be explained by reactions of seismic anisotropy. localiza- induced by channelling of fluids coupled with strain geological field trips 2013 - 5(1.1) itinerary 40 ) Contour plots of main structural features: mylonitic ) Contour plots of main structural R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano b the other samples. This consideration is very plausible because phyllosilicates, having a having plausible because phyllosilicates, is very the other samples. This consideration ) Outcrop view of APU mylonitic leucogneisses; ) Outcrop view of APU mylonitic a – The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen foliation and stretching lineation (Schmidt diagram – lower hemisphere) (after Cirrincione et al., 2010). – lower hemisphere) (after Cirrincione et al., foliation and stretching lineation (Schmidt diagram Fig. 28 DOI: 10.3301/GFT.2013.01 tion, operating into tabular domain during shear zone evolution profoundly and selectively changed physical profoundly and selectively evolution into tabular domain during shear zone tion, operating low abundance of mica in this sample is considered properties of the initial rock. As a matter fact very decrease of bulk seismic factors responsible for the drastic governing to be one of the most representative anisotropy compared to strong planar shape that is easily and promptly oriented under stress condition, are furthermore characterized of the single crystal. high anisotropy value by a very is located at about two kilometres ESE with respect to Mt. Montalto (geo- The outcrop of studied mylonites regular structur- by a very coordinates: 38°9’1.13” N, 15°56’42.16” E) (Fig. 28) and is characterised graphic foliation with a monotone attitude that, on the whole, is poorly affected by al setting, identified by a pervasive further deformation phases. geological field trips 2013 - 5(1.1) itinerary 41 : sin- M4 : K-feldspar M13 : Pre-mylonitic low : Pre-mylonitic M8 : Relics of pre-mylonitic garnet of pre-mylonitic : Relics M3 – %) abundances (volume Mineral – photomicrographs Representative Fig. 30 Fig. 29 inferred by whole rock and mineral chemistry. inferred by whole rock and mineral like quartz and albite. like of mylonitic leucogneisses of APU (after of mylonitic 2010). Cirrincione et al., and white mica within the fine grained matrix and white mica within the fine grained (quartz plus phengite and albite). porphyroclast wrapped by quartz and phengitic wrapped porphyroclast white mica aggregate. by ribbon-like phengite white mica wrapped quartz levels. micro-crystalline aggregate of ribbon- mylonitic R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano poikilo- The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 These leucocratic gneisses are characterized by the presence of gneisses are characterized These leucocratic 2-5 mm diameter augens, represented by feldspars blasts (Fig. 29). The common assemblage is Qtz+Wm+Pl+K- (Fig. 30). All of studied rocks show feld(Grt+Bt+Ep+Chl+Tur) foliation. S-C and S-C’ textures, mica- mylonitic a pervasive quartz are widespread. fish (Fig. 32), ribbon-like domains are related to different Microstructures in quartz-rich rotation bulging, subgrain recrystallization mechanisms like recrystalliza- boundary migration recrystallization, and grain tion (Fig. 32). geological field trips 2013 - 5(1.1) itinerary 42 ) relationship between a ) Vp-anisotropy pattern at ) Vp-anisotropy b – Fig. 31 ) Comparison between petrophysical On samples collected in this site microstructural a quantitative study has been conducted too. axis orientation Crystallographic has been of quartz grains obtained optically (Fig. 33) by the CIP method (Panozzo- 1993; Heilbronner & Pauli, pole 2000). c-axis Heilbronner, in figure 33 figures illustrated ori- were calculated from c-axis entation images obtained from selected micro domains. In all agreement. increasing strain and mean aspect ratio increasing strain for radii together with mean equivalent the quartz population. Seismic properties determined at 400 Mpa 2010); (modified after Cirrincione et al., c and properties determined at 400 MPa calculations carried out on the basis of It is chemistry. whole rock and mineral evident from the picture the good modal amounts of the main constituents and Vp patterns according of the rock frame to the structural (X=lineation, Y= perpendicular to lineation within the foliation plane, Z= pole to foliation). Below the diagram, APU mylonites pictures of investigated disposed in order of increasing strain are shown; R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 geological field trips 2013 - 5(1.1) itinerary 43 ) spatial b ) Microphoto of a quartz-rich domains where ) Microphoto of a quartz-rich a – Fig. 33 R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano axes used in the stereoplot of quartz c-axis patterns. used in the stereoplot of quartz c-axis axes grains having different crystallographic preferred orientations different crystallographic having grains are enanched by color coding scheme after applying the CIP an oblique foliation; technique and reveal orientation of structural features with respect to X,Y and Z orientation of structural ) Quartz b ) detail of b. Note the ribbon like ) detail of b. c ) Large micaceous crystals showing a The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen – Fig. 32 of the picture. characteristic sigmoidal shape (mica fish) within mylonitic characteristic gneiss of APU collected at this stop; leucocratic domain showing subgrain rotation recrystallization and domain showing subgrain oblique foliation; foliation in the lower part to the mylonitic quartz parallel DOI: 10.3301/GFT.2013.01 of the pictures reference foliation and lin- foliation eation corresponding to the mylonitic horizon- and stretching lineation, are respectively directed. Different types of c-axis tal and E-W patterns were obtained from CIP method, all of them reportable to a non-coaxial progressive from basal to rhomb deformation. An evolution from resulting slip system could be hypothesized patterns. c-axis geological field trips 2013 - 5(1.1) itinerary 44 – (Stop 1.3). Montalto shear zone Fig. 34 R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano The tectonic contact between APU and MPU refolded at decameter scale (Malonome The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen water locality) DOI: 10.3301/GFT.2013.01 Stop 1.3: coordinates: Lat 38°09’13’’ N; Long 15°58’2’’ E; Altitude: 1285 m.a.s.l. Geographic gneis bearing schists (MPU) and laminated leucocratic Lithotype: Alternation between muscovite-amphibole occur as well (Fig. 34). of foliated calc-schists es (APU). Minor levels scales. at various be observed features: Within the lithotypes of both units, shear structures may Structural It is also rocks occur. and ultramylonitic as well S-C structures in mylonitic Indeed, sigmoidal porphyroclasts spectacular examples of complex folds. within the calc-schists, possible to observe, Petrography: Gneisses: Qtz+Pl+Kfs+Wm±Bt±Tur Leucocratic schists: Qtz+Pl+Grt+Wm+Amph+Ep±Chl±Rt±Ttn±Ilm Muscovite-amphibole schists: Qtz+Pl+Grt+Wm+Ep+Chl±Rt±Ttn±Ilm Muscovite-garnet schists: Qtz+Pl+Chl+Wm+Ep±Grt±Rt Muscovite-epidote Cc+Qtz+Wm±Amph Calc-schists: the MPU Most widespread lithotypes characterizing the mesoscopic and micaschists. At are phyllites locally spot- scale, these rocks are usually grayish, protruding from the ted with garnet porphyroblasts erosion surface, which commonly coincides with foliation. Quartz lenses are widespread in mylonitic all of the litho-types. They are usually unique mark- relics of folds, giving information ers, which preserve outcrop scale, isoclinal about early deformation. At par- limbs of folded quartz bands, which developed evidence for allel to the main foliation, provide of the early Alpine metamorphic folia- transposition tion. It is worth noting that the most evident sur- face, both at outcrop and hand-sample scales, usu- foliation (Fig. 35). This ally coincides with mylonitic is sometimes difficult to distinguish at the meso- from the tectonic scopic scale, especially far away spring geological field trips 2013 - 5(1.1) itinerary 45 ) defined 1 identified in 1 between APU and MPU, whereas it is usu- between APU and MPU, – Shear bands in micaschists of MPU (Lat: – a mega-porphyroclast Montalto shear zone: Fig. 36 Nevertheless, many shear related structures are many Nevertheless, visible in the field (Fig. 8) next to tectonic con- stretching lineation, preferred orienta- tact (e.g., shear bands, S-C fabric, intrafo- tion of minerals, folds, asymmetric folds and sigma- liar verging pronounced and delta-type objects). A variably (from range crenulation, with wide wavelength structures. the above mm to dm) overprints Fig. 7c) related to major post-mylonitic folds. Fig. 7c) related to major post-mylonitic in the southern sector by low-grade mineral in the southern sector by low-grade assemblages (chlorite and epidote-muscovite contact ally more recognizable at the microscopic scale. Another good site where rocks belonging to MPU of Buonamico River are well exposed is in the valley Luca(S. area, Fig. 36):micaschist showing clear shear related structures here garnet amphibole outcrop. The oldest deformation phase D the MPU is represented by isoclinal folds (Fig. 8), producing an axial planar foliation (S 38°08’20”; Long: 16°02’38”; altitude: 170 mt) exposed Luca village area). A (S. at the Buonamico river subsequent folding phase is also visible in this outcrop minor sym-metrical to asymmetrical folds (shown in like Fig. 35 the mylonitic leucocratic gneisses (APU). leucocratic the mylonitic in schists (MPU) at the contact with the muscovite-garnet R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 geological field trips 2013 - 5(1.1) itinerary 46 ) 3 ) on 3r ) consist of millime- 2 crenulation cleavage, 2 ), more evident along the 3S are variable over the main foliation over are variable ), producing S 3r 2 , developed during a deep-seated com- , developed 3 and L 3S . This was responsible for genesis of pervasive . This was 3 R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano – schists of MPU: delta-type Microphoto of epidote-muscovite Fig. 38 mylonitic structures and S-C structures within ribbon-like quartz level. structures and S-C within ribbon-like mylonitic ter-wavelength folds (B ter-wavelength commonly weakly developed in the field, even if locally lead- in the field, even commonly weakly developed facies crystallization. ing to low-greenschist These structures were affected by late Alpine deformational phase D the main foliation (Fig. 8). The intersection angles between two lineations L pressional shear stage that produced at the same time a per- stretching lineation (L vasive contact of APU upon MPU (Fig. 37). This last event overthrust features identified in the corresponds to the main structural quartz field and is microscopically highlighted by ribbon-like sigma- or delta-type porphyro- variable-size bands, draping Near the clasts (Fig. 32), alternating with micaceous layers. sliding feldspars and S-C fabric tectonic contact, book-shelf coordinates. a NE sense of shear in present geographic give fold (B of intrafoliar Close to the tectonic contact, axes schists), evolving in the northern sector into higher-grade schists), evolving and amphibole-muscovite assemblages (garnet-muscovite suggests the existence, within schists). This evolution of early Alpine relict metamorphism, with an increasing MPU, the north. The next meso-structures formed toward gradient during a second deformational episode (D mylonitic foliation S mylonitic plane. This kind of structure with flattened pencil shape is bet- in the area of Cardeto village, near tec- ter developed Other typical structures APU. tonic contact with the overlying locally evolved into rods, producing a marked lineation (L into rods, producing a marked locally evolved The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen – of complex folds in calc-schists Very Fig. 37 field of view about 1 meter). MPU near the tectonic contact with APU (horizontal DOI: 10.3301/GFT.2013.01 geological field trips 2013 - 5(1.1) itinerary 47 axes) with axes) 4 visible on the . 4 3 – to fold (B4 axis) evolving Verging mational phase typical of brittle regime. Fig. 39 a small-scale thrust linked to the last defor- a small-scale thrust linked , locally producing a new axial-plane foliation 3 R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano gave rise to a new intersection lineation L gave 4 and S 3 affecting these rocks led to asymmetric isoclinal folds (B 4 , essentially in a brittle regime, produced meter wavelength verging folds verging , essentially in a brittle regime, produced meter wavelength 5 The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen (Fig. 8). The intersection between S 4 DOI: 10.3301/GFT.2013.01 evolving to thrusts and cataclastic bands at low angle to the mylonitic foliation. Locally, the effects related to foliation. Locally, to thrusts and cataclastic bands at low angle the mylonitic evolving locally masking early mylonitic to the entire outcrop, a reasonable cataclastic appearance this last episode give by a compression- is characterized structures. This last event m-to- hec- by SE-verging al thrust system, characterized axis orientations tometer asymmetrical folds with average system produced The thrust-sheet to SW-NE. from WSW-ENE a conjugate secondary brittle thrust system at different SE or NW scale, oriented N45-N65 and plunging alternatively the earlier ductile (Fig. 39). This thrust system reactivated the tectonic contact between APU transposing shear zone, of the mylonitic and causing pronounced thickening and MPU, from 0.5 to 0.8 km. A NE-SW band, which currently ranges extensional fault system marks the change from compres- sional to extensional tectonic regime, accommodated by a fault system. The normal-fault system transtensional NW-SE also responsible for longitudinal uplift of the Aspromonte was basin structures, which cross the Massif and transversal northern sector of the Aspromonte Massif horst structure 1990). et al., (Pezzino The above structural data, together with syn-kinematic Rb-Sr white-mica ages of 25-30 Ma (Bonardi et al., data, together with syn-kinematic Rb-Sr structural The above by taking into account that orogenic transport, 1987), are consistent with Oligocene-Miocene Africa-verging rotation (60°-70°) since the late Oligocene affected by main counter-clockwise the Aspromonte Massif was 2004). The & Lister, 1994; Rosenbaum of the CPO (Scheepers, 1994; Scheepers et al., south-east migration subsequent episode of deformation D S linked to the third deformational event consist of shear bands. The mylonitic foliation is deflected between paral- consist of shear bands. The mylonitic to the third deformational event linked lel shear bands, which appear as cm-spaced domains, forming an angle of about 40° with the S wavelengths ranging from 2 to 30 cm. They caused folding of S ranging wavelengths mylonitic surface. Beautiful examples of these kinds folds are exposed near the Sanctuary Madonna di mylonitic in the area of Mt. Montalto. of the shore Buonamico River, built on a fluvial terrace Polsi, The final deformational episode D geological field trips 2013 - 5(1.1) itinerary 48 Argille varicolori Argille – Location of the field trip area and stops. Fig. 40 R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano -con- . quasi ) having a ) having 3 valley of S. surfacing in (Fig. 40) ) and the metamorphic zona- The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen Cardeto tectonic window ( DOI: 10.3301/GFT.2013.01 tion of the Stilo Unit (SU) Agata river Stop 2.1: Asymmetrical folding developing rods near the tectonic contact between MPU and APU (Campi di S. Agata) masking true stretching lineation DAY 2 Madonna di Polsi Unit (MPU) coordinates: Geographic Lat: 38°05’39.09” N; Long:15°48’5.70” E Altitude: 1150 m.a.s.l. this Stop (Fig. 41) highly deformed micaschists At of MPU near the tectonic contact with overlay- to rods ing APU show asymmetrical folds evolving highlighted by quartz lenses (Fig. 42). this Stop major tectonic structures have At regu- A very good homogeneity and continuity. foliation (S mylonitic lar pervasive mean orientation 122°/22° and a stant lineation (135°/8°) defined by the inter- section of quartz rods and the main foliation are evident in the field. These rods (Fig. 43), with the shear phase, devel- probably coeval oped as the result of a tight folding intrafo- are lial asymmetrical folds whose hinge zones are typical structures of Folds quartz-enriched. com- and are very shear zone the investigated the geological field trips 2013 - 5(1.1) itinerary 49 Mylonitic to cataclastic rocks of m.a.s.l.). – (a) Highly compressed folds (B3 axes) Fig. 42 (S3). marked by quartz levels (MPU metapelites); (b) Narrow by quartz levels marked Agata near the tectonic at Campi di S. shear zone contact between APU and MPU close to the village of Cardeto (Lat: 38°05’46.44”N; Long: 15°47’34.36”E; Altitude: 1180 APU (alternation of ortho- and para-gneisses): in the APU (alternation of ortho- and para-gneisses): of this photo it is possible to observe level leucocratic bands) in gray-coloured of quartz (sub-horizontal layers to the main foliation millimetre thickness almost parallel R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano – (Stop 2.1). Montalto shear zone Fig. 41 The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 geological field trips 2013 - 5(1.1) itinerary 50 mon at the outcrop scale. Their wave- length is usually <5 mm and their fold to the correspond approximately axes direction of maximum quartz-rod the mesoscopic scale a elongation. At char- compositional layering marked the rocks of selected acterizes and phyllosilicate- Quartz- outcrop. rich domains constitute the main foli- quartz lenses are ation. Rod-shaped to folds axis. Even sub-parallel 800 structural though approximately measurements of stretching lineations collected in the surroundings areas of these lin- value an average give eations at N45°/25 SW with a general top to the NE sense of shear (Ortolano 2008; et al., 2005; Fazio et al., 2008), the stretching et al., Pezzino lineation is hardly discernible into these sheared metapelites both at the outcrop and at hand sample scale. It is assumed that in the study area (Fig. 44) the stretching lineation maybe oriented, similar to the rocks NW-SW et in other parts of the MPU (Pezzino in the 1990, 1992). However, al., selected outcrop the most prominent lineation is defined by the NW-SE which masks the trending quartz-rods stretching lineation. The true stretch- R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano ) detail of a c ) quartzite rods forming an b , a – Outcrop features: The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen Fig. 43 ) Structural data (lower hemisphere, equal area projection). N= ) Structural with rods. intersection lineation with the main (mylonitic) foliation; intersection lineation with the main (mylonitic) classical asymmetrical fold, showing a top-to-north-east sense of shear; d number of measurements. Lineation (intersection lineation) coincides DOI: 10.3301/GFT.2013.01 geological field trips 2013 - 5(1.1) itinerary 51 R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano ) b ) Quartz c- d ) Photograph of the ) Photograph c ) Schematic geological map of S. a The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen – Fig. 44 and NS oriented, modified after Fazio et al., 2010). et al., and NS oriented, modified after Fazio Schematic drawing of the studied specimen and its Schematic drawing orientation referred to the sense of shear at outcrop scale. The YZ plane is orthogonal to foliation to rod lineation. The XZ plane is and parallel perpendicular to YZ plane and at right angle with respect to the rod elongation; studied specimen and its quartz bands; axis patterns distribution on various planes (YZ, XZ, axis patterns distribution on various Agata River (Cardeto area) with stop location; Agata River DOI: 10.3301/GFT.2013.01 ing lineation orientation has been estab- lished by means of a quantitative study dealing with textures microstructural of quartz domains. Quartz fabrics (Figs. 44, in two mutually orthogo- 45) investigated an asymmetrical nal thin sections gives pattern indicating top-to-the-North sense of shear (Fig. 44). The data were generat- ed using classical (manual measurements using U-stage) and modern of quartz c-axis Computer Integrated methods (CIP, Microscopy). Both these sec- Polarization tions show oblique foliations at ca. 40° from the main shear plane, implying that the actual X direction (stretching lineation that is absent on the mesoscopic scale) must lie between these two sections. This quartz c- confirmed by investigating was axis patterns in a section striking NS and perpendicular to the foliation. geological field trips 2013 - 5(1.1) itinerary 52 ) grain boundary map (manual tracing) of a folded boundary map (manual tracing) ) grain a R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano ) aspect ratio (AR) and angle w/r mylonitic foliation of dectected quartz (AR) and angle w/r mylonitic ) aspect ratio b The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen ) histogram showing particle size distribution. showing particle size ) histogram – analysis of sample at this stop: microstructural Quantitative c Fig. 45 grains; grains; quartz layer (main foliation horizontally oriented); (main foliation horizontally quartz layer DOI: 10.3301/GFT.2013.01 geological field trips 2013 - 5(1.1) itinerary 53 ) APU ) outcrop b d - c ) Fold interference pattern; ) Fold a R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano – Marbles of the MPU: Fig. 46 850 m) showing an evident isoclinal folding. at the S. Agata river (Lat: 38°05’26.20” N; Long: 15°49’1.01” E; Altitude: Agata river at the S. mylonitic leucocratic gneisses levels interbedded to calchschists; gneisses levels leucocratic mylonitic The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 Stop 2.2: Marbles of MPU at the small quarry of Campi di S. Agata (near Cardeto village) coordinates: Geographic Lat: 38°5’46.00” N; Long: 15°48’13.09” E; Altitude: 1195 m.a.s.l. quarry of marbles spectac- In this tiny patterns ular interference structural (refolded folds) are exposed (Fig. 46). of metapelitic levels Some enclaves rocks of granitic and small fragments inside the carbonaceous trapped as rigid objects during matrix behave activation. the shear zone of quartz Some interbedded levels with show different erosion rate respect to the adjacent carbonaceous layers. geological field trips 2013 - 5(1.1) itinerary 54 ) ) c b ) Very d (Fig. 47) ) General view of ) General a – Fig. 47 (right hand rule notation). the outcrop at Stop 2.3. Cataclastic aspect of quartz-levels interbedded into micaceous layers. are tourmaline-rich Dark layers bands (centimetre scale bar). side View of the outcrop at dextral (Lat: 38° Agata river of the S. 05’02”; Long: 15° 46’17”; Altitude: 580 mt) that shows intense to a more cataclastic effects linked recent tectonic activity. strong lineation (Lm+1) plunging at 160°/5° (dip direction/dip to rods. This notation) evolves lineation is clearly visible on the foliation and seems to be mylonitic to syn- post-mylonitic linked orientation of folds. The average the main foliation is 140°/15° R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano exposed at this Stop. Near the Cardeto Village leucocratic The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 Stop 2.3: The classical alternation of leucocratic gneisses and darker paragneiss the Aspromonte-Peloritani Unit (APU) is gneisses of the Aspromonte Peloritani Unit (APU) are also exposed at S. Agata river Geographic coordinates: Geographic Lat: 38°05’01” N; Long: 15°45’04” E; Altitude: 605 m.a.s.l. geological field trips 2013 - 5(1.1) itinerary 55 ) Relics of ) Relics b - a – study of these metapelites 2009) revealed et al., (Fazio of gar- generations several net as well a multistage crystallization process (Figs. 50, 51). Fig. 49 asymmetrical folding (B3 axis). isoclinal folds (B1 axis) related to the first deformational episode. The limbs of these folds are to the main mylonitic parallel foliation which is affected by an Stop 2.4: Garnet bearing mica-schists of the MPU (S. Agata River) coordinates: Lat: 38°05’11.94” N; Geographic Long: 15°46’57.95” E; Altitude: 655 m.a.s.l. The main lithotype of the Cardeto Metamorphic Complex is here exposed (Figs. 48, 49). Garnet bearing micaschists with millimetre thick lenses of quartz show an asymmetrical folding over an early axial plane foliation imposed above foliation (S3). The to the mylonitic (S1) parallel latter is the most evident surface at outcrop scale. The orientation of the hinges asymmet- rical folds is 310°/35° (dip direction/dip) and it to the orientation of lineation is sub-parallel by the rods seen at previous (Lm+1), marked and chemical A detailed microstructural Stop. R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano – Agata (Stop 2.4). at S. Garnet-mica-schists The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen Fig. 48 DOI: 10.3301/GFT.2013.01 geological field trips 2013 - 5(1.1) itinerary 56 ) Layer c ). 4 ) Layer of smaller ) Layer d – Sketch-drawing – of various Microphotographs ) Type 2 garnets embedded into ) Type b Fig. 50 Fig. 51 deformational episode (D ) Type 1a garnet porphyroblast (plane- 1a garnet porphyroblast ) Type (after Fazio et al., 2009). et al., (after Fazio of relationships between garnet growth stages and deformation history of sheared metapelites Type 2 garnets, folded during the last Type composed by Type 2 garnets aligned parallel composed by Type to the main S3 foliation. type of garnet recognized within MPU rocks. type of garnet recognized a light) with a rim composed by polarized 2 smaller Type coalescing of several crystals. layers parallel to the mylonitic foliation to the mylonitic parallel layers 1b porphyroblast deflected around a Type (right area of the picture). R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 geological field trips 2013 - 5(1.1) itinerary 57 – Field aspect of the intrusive Near this Stop, at the Portella Near this Stop, it is possible to locality, Zagaria between the transition observe augen orthogneisses to biotite- The lat- of the APU. paragneisses ter are affected at least by a defor- mational phase responsible of iso- clinal folds at different scales. Fig. 53 and host rocks (APU paragneisses). contact between Punta d’Atò granitoids contact between Punta d’Atò – (Stop 2.5). granitoids Punta d’Atò R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Fig. 52 made by (Fig. 52). Is The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 Stop 2.5 : Magmatic intrusions of Punta d’Atò coordinates: Lat: 38°02’44’’ N; Geographic Long: 15°48’36’’ E; Altitude: 1040 m.a.s.l. Angelo the Punta d’Atò In the vicinity of Monte S. body is exposed granitoid a small to medium grain size biotite granite, size a small to medium grain often preserving septa of host rocks (parag- neisses) (Fig. 53). The whole outcrop is highly and intense retrogressed due to the pervasive brittle deformation. This phases often contacts between original intrusive obliterates a folia- and host rocks. Sporadically granitoids within magmatic rocks (Fig. tion is preserved 54). geological field trips 2013 - 5(1.1) itinerary 58 – and Staurolite-andalusite Fig. 55 garnet zones of the Stilo Unit (Stop 2.6). garnet zones R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Stop 2.6: Staurolite-andalusite and garnet zones of the Stilo Unit (area north to Bagaladi village) coordinates: Lat: 38°02’13’’ N; Geographic Long: 15°48’36’’ E; Altitude: 970 m.a.s.l. from phyllites outcropping in this area are variable Rocks microscopic scale, within phyl- to schists (Figs. 55, 56). At interbedded with biotite and lites, quartz forming layers is characterized white mica enriched lepidoblastic levels, Within schists meter wave- sizes. different grain by very to the first deformational episode lenght folding linked appears evident. These structures are isoclinal folds with oriented axis averagely sharp hinge profile, sub-horizontal N 300°/15°. The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen – near of Punta d’Atò granitoids Foliated Fig. 54 area. the intrusive contact with Aspromonte Peloritani the intrusive exposed north to Bagaladi village Unit paragneisses DOI: 10.3301/GFT.2013.01 geological field trips 2013 - 5(1.1) itinerary 59 – of SU Paragneisses – contact at Intrusive north to Bagaladi village. Mount Scafi (Stop 2.7). Fig. 56 Fig. 57 R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano Altitude: 930 m.a.s.l. The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 Stop 2.7: Intrusive contact (Mount Scafi area) coordinates: Lat: 38°02’10’’ N; Long: 15°51’51’’ E; Geographic A field situation analogous to the last Stop occurs in northern area of Monte Scafi, where grani- leucocratic a muscovite it is possible to observe of the Stilo Unit. Again and paragneisses toid body intruded within phyllites septa of metamorphites occur within the plutonic body (Fig. 58). The thermal effects related to plutonic bodies intruded within APU and SU host rocks are visible as static blastesis of biotite, white mica in the accompanied at times by andalusite and cordierite spots in the phyllites, paragneisses. and pegmatites are also widespread near the intrusive Quartz veins up to one metre in dykes granitoid contact as well paraconcordant assemblages associated to this thermal thickness. The mineralogical geological field trips 2013 - 5(1.1) itinerary 60 ). b foliation modification ); Septa of a – body granitoid Leucocratic lineation coinciding with micro- Of course these thermal effects are The dominant lithotype is given by The dominant lithotype is given Fig. 58 event are extremely different reach- event ing the maximum conditions of hornblend cornubianite facies. less evident in the paragneisses producing only a small to the initial assemblage, whereas are more apparent in the phyllites. Wm, (Qtz, Ab, phyllites fine-grained Chl, Bt, Grt), (Fig. 59) often showing metamorphites within the plutonic mass intruded within SU phyllites intruded within SU phyllites – belonging to aspect of phyllites Typical Shear structures probably related to a defor- Fig. 59 main foliation (photo taken at Portelle Scafi). at Portelle main foliation (photo taken quartz lenses forming bouden like structures quartz lenses forming bouden like to the main field elongated parallel (S1). Sometimes a crenulation cleavage (S2) (S1). Sometimes a crenulation cleavage developing a folds hinges (B2) is visible. N 95°E/20°. They are oriented on average at the brittle-duc- mational phase developed are better recorded by quartz tile transition oriented 160/40 with S1 is averagely levels. plunge of N 30°E/25°. having B1 axes the SU with classical lenses of quartz parallel to the the SU with classical lenses of quartz parallel R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 geological field trips 2013 - 5(1.1) itinerary 61 quartz-feldspar aggre- quartz-feldspar – view of the General They are set in a ground- Fig. 61 gradient is evident in the field. gradient gle crystals of K-feldspar, or gle crystals of K-feldspar, sometimes plagioclase or polycr- crystalline gates. outcrop at this stop (front of exposed rocks is ca. 7 mt). Narrow affecting paragneisses, shear zone gneisses and augen leucocratic A strain gneisses of the APU. – body intruded granitoid Leucocratic Fig. 60 within the plutonic mass (right). within SU phyllites (left); Septa of metamorphites R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen ugen gneisses from the APU are coarse to very coarse grained rocks composed of quartz, plagioclase, micro- coarse grained ugen gneisses from the APU are coarse to very DOI: 10.3301/GFT.2013.01 cline, biotite and muscovite, and mostly of granite to granodiorite composition. The augens mostly consist of sin- to granodiorite and mostly of granite cline, biotite and muscovite, Stop 2.8: Narrow shear zone within APU (northwest to ) coordinates: Lat: 38°03’8.92’’ N; Geographic Long: 15°52’26.04’’ E; Altitude: 1120 m.a.s.l. rocks of the APU crop out in area Medium-high grade del Greco village. They are essentially around Roccaforte gneisses leucocratic augen gneisses, paragneisses, Variscan and mica schists, locally affected by Alpine reworking foliation in of a mylonitic responsible for the development (Fig. 61). gradient with evident strain narrow shear zones phase Isoclinal metric folds ascribable to a post-mylonitic affect both lithotypes. partitioning foliation and the effects of strain The mylonitic are both particularly well visible in the augen gneisses (Fig. 62 a, b), where they are higlhighted by strong flattening as well by porphyroclasts and alignment of the K-feldspar reduction. size evident grain A geological field trips 2013 - 5(1.1) itinerary 62 ) K- d ) mylonitic a – features of APU Structural ) chessboard pattern extinction in c Fig. 62 white mica (crossed polars; 10x). ) strain partitioning within sub-horizontal ) strain mass composed of fine to coarse quartz, plagioclase and K- grained feldspar and medium to coarse aggregates of biotite, with grained plates, that small muscovite rarer the augen. The commonly wrap augens are sometimes bordered by bands of fine-medium mm-sized aggregates granoblastic grained size deriving from tectonic grain reduction and later recrystallisation of rim portions original megacrysts megacrysts. K-feldspar are usually up to 5 cm in length and a quart grain (crossed polars; 10x); a quart grain feldspar augen bordered by quartz and foliation marked by elongated K-feldspar; foliation marked b levels; mylonitic augen gneiss: mylonitic R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen DOI: 10.3301/GFT.2013.01 occasionally have an idiomorphic shape and simple twinning. A relic hypidiomorphic texture is indeed pre- an idiomorphic shape and simple twinning. A relic hypidiomorphic occasionally have in rock microdomains less affected by deformation. served ion probe dating of zircon from APU augen gneisses in both southern Calabria and north-eastern Sicily Recent in press) has shown that the protoliths of APU augen gneisses, (Micheletti et al. 2007; Fiannacca al., as well of similar gneisses from Sila and Castagna units in northern Calabria, were late Proterozoic-early mostly emplaced at about 560-540 Ma. granitoids Paleozoic The granitoids were later affected by Variscan metamorphism, under amphibolites facies conditions, that were later affected by Variscan The granitoids stage. into augen gneisses. Finally the rocks were affected by Alpine mylonitic turned the granitoids geological field trips 2013 - 5(1.1) itinerary 63 – (a-b) Variscan Fig. 64 isoclinal fold relics (B1s). – of SU (Stop 2.9). Chlorite zone Fig. 63 R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano visible at aller grain The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen enses within phyllites (Fig. 65) suggest enses within phyllites DOI: 10.3301/GFT.2013.01 Stop 2.9: Chlorite zone of the Stilo Unit, Chorio Village - road n.183 (at km 60) with Bt- interlayered This outcrop shows phyllites schists with right sense of shear structures given by sigmoidal quartz lenses within main mylonitic times it is possible to observe foliation (Fig. 64). At microscopic earlier isoclinal folds relics (B1s). At by syn- scale these rocks shows a foliation marked kinematic crystals of biotite and quartz, rarely by smwhite mica often characterized size. Cataclastic shear zones are Cataclastic shear zones size. microscopic scale too. Similar rocks are also exposed in the area close to metapsammites, village (phyllites, San Lorenzo chlorite schists). quartzites, and muscovite Quartz l geological field trips 2013 - 5(1.1) itinerary 64 s – (a-b) Asymmetrical ) are preserved. In this area is ) are preserved. 1 Fig. 65 feldspar porphyroclasts. centimetre wavelenght verging folds verging centimetre wavelenght widely occur in the area near San village. Also microstructures Lorenzo testify this shear deformational phase with crystallization of white mica within tails around quartz and R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano ). Sometimes relics of earlier isoclinal folding (B 1 The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen INGRAZIAMENTI CKNOWLEDGMENTS DOI: 10.3301/GFT.2013.01 also appreciated. R the foliation coincides with the earlier iso- occurrence of a shearing deformation episode. The main mylonitic clinal axial plane foliation (S A wa Critelli for the review of manuscript. The editorial handling Gloria Ciarapica to Salvatore are extremely grateful We per gli utili Gloria Ciarapica Ringraziamo Critelli per la revisione del manoscritto. a Salvatore Siamo estremamente grati suggerimenti editoriali. very common to observe chevron type folds with sub-horizontal axial surfaces with metric wavelenght scale axial surfaces with metric wavelenght chevron type folds with sub-horizontal common to observe very in the SU rocks. to the last deformational episode recognized linked The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction of the Calabria-Peloritani Orogen R. Cirrincione - E. Fazio - P. Fiannacca - G. Ortolano - A. Pezzino - R. Punturo - V. Romano g e o l o g i c a l

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DOI: 10.3301/GFT.2013.01 geological field trips 2013 - 5(1.1) references 66 a rom nce, e V., Martini R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen Piccarreta G., Russo M., Scandone P., Zanettin Lorenzoni E. & Zuppetta A. (1976) - L’arco calabro-peloritano nell’orogene E. & Zuppetta A. (1976) - L’arco Lorenzoni Zanettin Scandone P., M., Russo Piccarreta G., 17: 1-60. appenninico-maghrebide. Mem. Soc. Geol. It., from the Serre and petrological constraints Orogen (southern Italy): structural upper crust in the Alpine Calabria-Peloritani Massif metapelites. Lithos, 115: 237-262. 101: 259-274 Boll. Soc. Geol. Ital., palinspastic restoration. Arc in a semiquantitative Peloritani southern Italy). Boll. Soc. Geol. It., Composite Terrane, in the Aspromonte Nappe (Calabria–Peloritani metamorphic overprint 127: 173–190. 42: 301. SIMP, Calabria Meridionale. Rend. dell’Unità dell’Aspromonte, (Southern Italy). Terra Nova, 6: 582-594. Nova, (Southern Italy). Terra Mountains (southern Italy): another example of resetting monazite electron microprobe dating of monazite in the Peloritani 100: 107–123. Earth Sci. (Geol Rundsch), rocks. Int. J. ages in high-grade Mountains (Sicily), 63: 113–125. in south-eastern sector of the Peloritani event 2: 363–371. Mineral, J. Eur. Mountains (Calabrian Arc), Italy. nappe) of the north-eastern Peloritani of the Geol. Soc. London, 141: 137-145. Jour. Arc, southern Italy: a review. Peloritan Scale 1: 50,000. London, 287-306. Basins. Kluwer Academic Publisher, of a Mountain: the Apennines and adjacent Mediterranean (eds.) Anatomy DOI: 10.3301/GFT.2013.01 Angì G., Cirrincione R., Fazio E., Fiannacca P., Ortolano G. & Pezzino A. (2010) - Metamorphic evolution of preserved Variscan of preserved A. (2010) - Metamorphic evolution Ortolano G. & Pezzino Fiannacca P., E., Fazio Cirrincione R., Angì G., of continental crust f evolution on Late Paleozoic A. (2011) - Age constraints & Pezzino Fiannacca P. Cirrincione R., Appel P., on the Alpine age constraints (2008) - Rb–Sr V. Messina A. & Perrone Macaione E., Del Moro A., Compagnoni R., Bonardi G., tettonico-metamorfiche alpine (1987) - Riequilibrazioni V. Messina A. & Perrone Del Moro A., Compagnoni R., Bonardi G., metamorfiche di probabile età alpina nell’Unità (1984b) - Riequilibrazioni V. Messina A. & Perrone Compagnoni R., Bonardi G., Amodio Morelli L., Bonardi G., Colonna V., Dietrich D., Giunta G., Ippolito F., Liguori V., Lorenzoni S., Paglionico A., Perron A., Paglionico S., Lorenzoni Liguori V., Ippolito F., Giunta G., Dietrich D., Colonna V., Bonardi G., Amodio Morelli L., metamorphic and geochronologic features of the Alpine A. (1994) - Structural, Del Moro A. & Pezzino Cirrincione R., P., Atzori metamorphic rocks (Aspromonte data from medium- to high grade A. (1990) - Rb/Sr radiometric Del Moro A. & Rottura P., Atzori Orogen along the Calabrian- of the Variscan A. (1984) - Remnants Piccarreta G. & Rottura A., Paglionico P., Ferla P., Atzori Flore S.EL.CA., L. (1983) - Carta geologica del bordo occidentale dell’Aspromonte A. & Vezzani, Pezzino Ghisetti F., P., Atzori & I.P. Vai and northern . In: G.B. terrane (2001) - Calabria-Peloritani S. & Rossi V. Perrone W., Cavazza Bonardi G., of the northern sector Calabri E. & Zuppetta A. (1982) - The evolution Turco L., Tortorici V., Perrone Cello G., Bonardi G., References Arc of the Calabrian-Peloritan sequences and evolution E. (1994) - Palaeozoic Lorenzoni & Zanettin S. Lorenzoni Acquafredda P., geological field trips 2013 - 5(1.1) references 68 - - ). el tal rfica in Le . Ital., R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano www.caireggio.it The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen nental crust: compatibility with post-collisional extensional tectonics. Terra Nova, 19: 502–514. Nova, extensional tectonics. Terra nental crust: compatibility with post-collisional 12. 109-16. Nova, Terra an example from Calabria, southern Italy. levels: 113: 195–203. Peloritano, Boll. Soc. Geol. It., 103: 279-309. Boll. Soc. Geol. It., Peloritano, 266: 72-75. Sci. Paris, 95: 219-244. Boll. Soc. Geol. It., Serre (Calabria, Italy). Geological, petrological, geochronological characters. 106: 683–698. Boll. Soc. Geol. It., dans leur cadre structural. Calabro-Peloritain Mitt, 83: 301–316. Petrogr. metamorphism in the Sila basement (Calabria, Italy). Schweiz. Mineral. high-temperature 47: 263–272. orientali). Mem. Soc. Geol. It., di Mandanici (Peloritani Rend. Soc. Geol. It., 3: 3-4 Soc. Geol. It., Rend. Sassi (Eds.). Contributions to the Geology of Italy with special basement of Sardinia. In: L. Carmignani, F.P. for the Variscan 276, Newsletter 5, 61-82; Cocozza. IGCP No. dedicated to Tommaso basements. A volume regard to the Paleozoic 11, 35-38 Soc. Geol. It., Rend. Calabro-Peloritano. dell’Arco 116, 51-77. Boll. Soc.Geol. It., sedimentaria oligocenico-quaternaria del bacino calabro-ionico. 174: 397-409. data. Earth Planet Sci. Lett., modelling, geological and geophysical dell’Aspromonte–Arco Calabro Peloritano: Rendiconti Soc. It. di Min. e Petr., 39: 613–628. Soc. It. di Min. e Petr., Rendiconti Calabro Peloritano: dell’Aspromonte–Arco DOI: 10.3301/GFT.2013.01 Caggianelli A., Prosser G. & Rottura A. (2000) – Thermal history vs. fabric anisotropy in granitoids emplaced at different crus A. (2000) – Thermal history vs. fabric anisotropy in granitoids Prosser G. & Rottura Caggianelli A., CAI Club Alpino Italiano - Sezione Aspromonte Website: Borsi S. & Dubois R. (1968) - Données géochronologiques sur l’histoire hercynienne et alpine de la Calabre centrale. Cr Acad. & Dubois R. (1968) - Données géochronologiques sur l’histoire hercynienne et alpine de la Calabre centrale. Borsi S. Unit E. (1976) - Stilo Unit and “Dioritic-Kinzingitic” Zanettin A. & Lorenzoni Paglionico S., Lorenzoni Merlin H.O., Borsi S., de l’Arc C. (1987) - Les fomations paleozoique Cygan C. & Fournier-Vinas Baudelot S., Majeste-Menjoulas C., Bouillin J.P., genesis connected with low-pressure A. (2003) - Leucogranite Prosser G. & Rottura Di Battista P., Del Moro A., Caggianelli A., of the late Hercynian Calabria conti evolution G. (2007) - Pressure–temperature Prosser G. & Ranalli Liotta D., Caggianelli A., Cirrincione R. & A. Pezzino - (1994) Nuovi orientali. metamorfiche dei Monti Peloritani dati sulle successioni mesozoiche Boll. Soc. Geol Bonardi G., Messina A., Perrone V., Russo S. & Zuppetta A. (1984a) - L’unita di Stilo nel settore meridionale dell’Arco Calabro di Stilo nel settore meridionale dell’Arco & Zuppetta A. (1984a) - L’unita S. Russo V., Perrone Messina A., Bonardi G., strutturale di Stilo-Capo d’Orlando: un possibile strumento per lo studio dell’evoluzione (1988) - La Formazione W. Cavazza e sedimentologia della sequenza E.G. (1997) - Stratigrafia & Reinhardt R.T. Patterson Decelles P.G., Blenkinsop J., W., Cavazza system: geopoem based on new model of the Himalaya-Tibet & Mattauer M. (2000) - Evolutionary Burg J.P. Chemenda A.I., di Alì e nella Unità metamo alpino nella serie mesozoica dell’evento strutturali A. (1991) - Caratteri Cirrincione R. & Pezzino Carmignani L., Barca S., Cappelli B., Di Pisa A., Gattiglio M., Oggiano G. & Pertusati P.C. (1992) - A tentative geodynamic mod (1992) - A tentative P.C. Oggiano G. & Pertusati Gattiglio M., Di Pisa A., Cappelli B., Barca S., Carmignani L., Bonardi G., Messina A., Perrone V., Russo M., Russo S. & Zuppetta A. (1980) - La finestra tettonica di Cardeto ( tettonica di Cardeto (Reggio & Zuppetta A. (1980) - La finestra S. Russo M., Russo V., Perrone Messina A., Bonardi G., geological field trips 2013 - 5(1.1) references 69 - - u- nts ela- phic abro aly). R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano an overview. In: Coward M.P., Dietrich D. & Park R.G. (eds.), 1989, Alpine & Park Dietrich D. M.P., In: Coward an overview. The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen phic evolution of an accretionary wedge in a collisional belt, NE Sicily, Inter. Geol. Rev., DOI:10.1080/00206814.2011.623022. Geol. Rev., Inter. of an accretionary wedge in a collisional belt, NE Sicily, phic evolution 38, (3): 989-1014. S.I.M.P., Rend. grafico. 10: 257-326. Mem. Acc. Naz. Lincei, IV fascicolo, thern Apennines foreland basin system, Italy. 2 (ed. By Schattner U.) In: Tectonics sequences in foreland setting: the Southern Apennines basin system, Italy. Chapter 6: Intech Open Access Publisher [ISBN 979-953-307-199-1], 121-170. 38: 35-52. Petrol., Soc. It. Mineral. Rend. Earth Sci. 92: 852–872. Int. J. Sicily. Mts., 38: 1015-1026. Petrol., Soc. Ital. Mineral. Rend. Peloritano. tectonics, Geol. Soc. Sp. Publ., 45: 1-29. Publ., tectonics, Geol. Soc. Sp. stic anisotropy of naturally deformed leucogneiss from a shear zone in Montalto (southern Calabria, Italy). From: Spalla M.I., deformed leucogneiss from a shear zone stic anisotropy of naturally 332: London, Spec. Publ., in Interpretation of Geological Processes. Geol. Soc., Marotta A.M. & Gosso G. (Eds.) Advances 49–68. doi: 10.1144/SP332.4. for orogenetic exhumation modelling of HP rocks: The example of southern Calabria Peloritani Orogen (Western for orogenetic exhumation modelling of HP rocks: The example southern Calabria Peloritani 22–24 September 2008. Boll. Geof. in GeoMod 2008, Third International Geomodelling Conference, Firenze, Mediterranean), 49, 2: 141–146. e Appl., Teor. 166: 995-1010. doi (Southern Calabria – Italy). Pure and Applied Geophysics, Leucogneiss from an Alpine Shear Zone 10.1007/s00024-009-0483. DOI: 10.3301/GFT.2013.01 Cortese E. (1896) - Sulla geologia della Calabria settentrionale. Boll. Soc. Geol. It., 15, 3: 310-313. Cortese E. (1896) - Sulla geologia della Calabria settentrionale. Boll. Soc. Geol. It., (1989) - Alpine tectonics & Dietrich D. M.P. Coward sequences in the so of lithospheric flexure and thrust accomodation in forming stratigraphic (1999) - The interplay Critelli S. between lithospheric flexure, thrust tectonics and stratigra (2011) - Relationships F. & Perri V. Tripodi Muto F., Critelli S., arc (Southern It suite of Calabria-Peloritani granitic Maccarrone E. & Puglisi G. (1982) - Peraluminous A., Rottura C., D’Amico metamorphic units of the Peloritani & Villa I.M. (2003) - Geochronology of the medium to high grade S.G. Rotolo De Gregorio S., fisica dell’Italia Meridionale. Ed. Laterza, Bari. G. (1904) – Geologia e geografia De Lorenzo Cal dell’Arco peraluminosi Rb/Sr di granitoidi A. (1982) - Studio radiometrico G. & Rottura Pardini Maccarrone E., Del Moro A., Crisci G. M., Donati G., Messina A., Russo S. & Perrone V. (1982) - L’Unità superiore dell’Aspromonte. Studio geologico e petro superiore dell’Aspromonte. (1982) - L’Unità V. & Perrone S. Russo Messina A., Donati G., Crisci G. M., Cirrincione R., Fazio E., Ortolano G., Pezzino A. & Punturo R. (2011) - Fault-related rocks: deciphering the structural–metamor A. & Punturo R. (2011) - Fault-related Pezzino Ortolano G., E., Fazio Cirrincione R., Cirrincione R., Fazio E., Fiannacca P., Ortolano G. & Punturo R. (2009) - Microstructural Investigation Of Naturally Deformed Of Naturally Investigation Ortolano G. & Punturo R. (2009) - Microstructural Fiannacca P., E., Fazio Cirrincione R., A. & Punturo R. (2010) - Microstructure and Pezzino Ortolano G., Mengel K., H., Kern Heilbronner R., E., Fazio Cirrincione R., Cirrincione R., Fazio E., Fiannacca P., Ortolano G., Pezzino A. & Punturo R. (2008) - Petrological and microstructural constrai and microstructural A. & Punturo R. (2008) - Petrological Pezzino Ortolano G., Fiannacca P., E., Fazio Cirrincione R., geological field trips 2013 - 5(1.1) references 70 - oc. on- Unit mig- ni seg- R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano www.parcoaspromonte.gov.it The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen matites from north-eastern Peloritani (North-Eastern Sicily): preliminary data. Boll. Acc. Gioenia Sc. Nat, 38 (365): 151-172. matites from north-eastern Peloritani ment of the Alpine chain, southern Italy. An overview. Period Mineral, 73: 57–71. Mineral, Period An overview. ment of the Alpine chain, southern Italy. 84: 19–45. Petrol., Mineral. Sicily. genesis: evidence from Aspromonte Unit, north-eastern Peloritani, Geol. It., 55: 87-93. Geol. It., ships between isolated porphyroblasts and coalescing euhedral crystals. Periodico di Mineralogia, 78, 1: 3-18. di Mineralogia, crystals. Periodico and coalescing euhedral ships between isolated porphyroblasts Classical to Modern Geology-From (Calabria, southern Italy): clues for hidden shear flow direction. Special Issue “Structural Geol. Soc. India, 75: 171-182. Concepts“. J. 2007 - 16° Conference on Deformation southern Italy). DRT (Aspromonte Massif, leuco-gneisses from the Montalto shear zone 5: 87-88. Soc. Geol. It., 27 Settembre - 2 Ottobre 2007. Rend. Milano, Mechanisms, Rheology and Tectonics. 34: 55-74. SIMPAL, Rend. Peloritani. graphic features and geothermobarometric implications. Plinius, 31: 112-118. graphic Special meeting of crystalline complexes. Calabria) and correlations with analogue Sardinian Variscan (Aspromonte Massif, 1: 111-113. Gèologie de la France, Sassari, Italy. May-22-23 2012”, French and Italian Geological Societies “Variscan 93: 111-142. and Petrology, Calabria). Mineralogy the tectonic windows of Cardeto area (southern Aspromonte Massif, D. Dietrich & R.G. Park (Eds.), Alpine Tectonics, Geol. Soc. Spec. Publ., 45: 265-283. Geol. Soc. Spec. Publ., (Eds.), Alpine Tectonics, Dietrich & R.G. Park D. of Catania. ed implicazioni termobariche. Unpublished PhD Thesis, University petrografica caratterizzazione dell’Aspromonte: DOI: 10.3301/GFT.2013.01 Fiannacca P., Brotzu P., Cirrincione R., Mazzoleni P. & Pezzino A. (2005a) - Alkali metasomatism as a process for trondhjemite & Pezzino P. Mazzoleni Cirrincione R., Brotzu P., Fiannacca P., and geochemical features of Hercynian A. & Sergi (2005b) - Petrographic Pezzino A., Mazzoleni Cirrincione R., Fiannacca P., Festa V., Messina A., Paglionico A., Piccarreta G. & Rottura A. (2004) - Pre-Triassic history recorded in the Calabria–Pelorita A. (2004) - Pre-Triassic Piccarreta G. & Rottura A., Paglionico Messina A., V., Festa Fazio E., Cirrincione R. & Punturo R. (2010) - Quartz c-axis texture mapping of mylonitic metapelite with rods structures texture mapping of mylonitic Cirrincione R. & Punturo (2010) - Quartz c-axis E., Fazio deformed of naturally characterization study and petrophysical Heilbronner R. & Punturo (2007) - Microstructural E., Fazio e significato geodinamico del magmatismo pre-ercinico presente nelle filladi semiscisti dei monti (1978) – Natura P. Ferla Mountains (Sicily). Mem. S in the geological history of Peloritani (2000) - A model of continental crust evolution P. Ferla Fazio E., Casini L., Cirrincione R., Massonne H.-J. & Pezzino A. (2012) - P-T estimates for the metamorphic rocks of Stilo A. (2012) - P-T & Pezzino Massonne H.-J. Cirrincione R., Casini L., E., Fazio conditions of Alpine-type metamorphism using multistage garnet in A. (2008) - Estimating P-T Cirrincione R. & Pezzino E., Fazio A. (2009) - Garnet crystal growth in sheared metapelites (southern Calabria – Italy): relati Cirrincione R. & Pezzino E., Fazio Ente Parco Nazionale dell’Aspromonte Website: Website: Nazionale dell’Aspromonte Ente Parco mapping of metapelitic units the southern sector Aspromonte Massif: petro E. (2005) - Geological and structural Fazio Dewey J., Helman M.L., Turco E., Hutton D.H.W. & Knott S.D. (1989) - Kinematics of the western Mediterranean. In: N.P. Coward, In: N.P. (1989) - Kinematics of the western Mediterranean. & Knott S.D. Hutton D.H.W. E., Turco Helman M.L., Dewey J., nell’area meridionale del massiccio delle unità metapelitiche affioranti geologico-strutturale E. (2004) - Rilevamento Fazio geological field trips 2013 - 5(1.1) references 71 n elt a). ra- 1514. Western m in the R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano data in the Aspromonte Massif area. Lithos, 114: 451-472. Ar /39 Ar The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen Arc (Southern Italy). J. Struct. Geol., 3: 371-381. Struct. Geol., Arc (Southern Italy). J. section, XVII, 71. XVe Alger, Gëol. Intern., Congr. 17 Metam. Geol., Jour. orogeny. in the Calabrian crustal cross-section during Variscan for the thermal evolution straints (2): 157-172. 18: 409-421. Metam. Geol., cooling in the Hercynian crustal cross-section of Calabria. J. morphism and post-metamorphic 4 (3): 131-147. Geol. Dyn., Phys. Geogr. 298: 259-269. Tectonophysics, 17: 4. Nova, geodynamics. Terra Mediterranean (Maghrebian Flysch Basin and Lucanian Ocean): consequences for Western Tethys 22: 969-981. Geology, tion images. Journal Structural Southern Calabria Peloritani Orogen, Southern Italy: Petrogenetic Inferences and the Gondwana Connection. J. Petrol., 49: 1897- Petrol., Connection. J. Inferences and the Gondwana Orogen, Southern Italy: Petrogenetic Southern Calabria Peloritani margin at the end of Precambrian. Gondwana of the northern Gondwana evolution nitoid magma production during rapid doi:10.1016/j.gr.2012.05.019. Research, Electronic Edition, ISSN Virtual Explorer, belt. J. (Eds.): The southern Variscan Iacopini & G. Rosenbaum Carosi, R. Dias, D. 1441-8142, 19, 2, 23:782-796. (southern Italy): New 40 Rend. Soc. Ital. Mineral Petrol 43: 643–656. Petrol Soc. Ital. Mineral Rend. Sci. 303: 353-409. orogens. Am. Jour. phic rocks in the Mediterranean DOI: 10.3301/GFT.2013.01 Glangeaud L. (1952) - Les eruptions tertiaires nord-africaines et leurs relations avec la tectonique méditerranéenne. C.R. IXe la tectonique méditerranéenne. et leurs relations avec Glangeaud L. (1952) - Les eruptions tertiaires nord-africaines pelites in the Aspromonte, southern Calabria: con- metamorphism of Palaeozoic (1999) - Low-pressure & Schenk V. T. Graessner magmatism, meta- on timing of granitoid M. & Mezger K. (2000) - Geochronological constraints Brocker Schenck V., T., Graessner Dubois R. & Caire A. (1961) - Hypothèse sur la structure profonde de Calabre (Italie). Rev. Glangeaud L., C., Grandjacquet of the western Mediterranean. M. (1998) - On the post 25 Ma geodynamic evolution Doglioni C. & Fernandez Gueguen E., of the of the southern branch evolution M. (2005) - Tectono-sedimentary & Tramontana V. Perrone Martìn-Martìn M., F., Guerrera or orienta- analysis using polarization micrographs size boundary detection and grain Heilbronner R. (2000) - Automatic grain b & Compagnoni R. (2010) - Alpine tectonics in the Calabrian–Peloritan Bouillin J.P. Pêcher A., Arnaud N., Monié P., Heymes T., Fiannacca P., Williams I.S., Cirrincione R. & Pezzino A. (2013) - The augen gneisses of the Peloritani Mountains (NE Sicily): g A. (2013) - The augen gneisses of the Peloritani Cirrincione R. & Pezzino Williams I.S., Fiannacca P., Franceschelli M., Puxeddu M. & Cruciani G. (2005) - Variscan metamorphism in Sardinia, Italy: review and discussion. In: R. M. & Cruciani G. (2005) - Variscan Puxeddu M., Franceschelli of the Calabria analysis to understanding the geodynamic evolution L. (1981) - Contribution of structural & Vezzani Ghisetti F. Fiannacca P., Williams I.S., Cirrincione R. & Pezzino A. (2008) - Crustal Contributions to Late Hercynian Peraluminous Magmatis A. (2008) - Crustal Contributions to Late Hercynian Peraluminous Cirrincione R. & Pezzino Williams I.S., Fiannacca P., Ioppolo S. & Puglisi G. (1989) - Studio petrologico di alcune metamorfiti erciniche dei Monti Peloritani nord orientali (Sicili & Puglisi G. (1989) - Studio petrologico di alcune metamorfiti erciniche dei Monti Peloritani Ioppolo S. Jolivet L., Faccenna C., Goffé B., Burov E. & Agard P. (2003) - Subduction tectonics and exhumation of high-pressure metamor- E. & Agard P. Burov Goffé B., C., Faccenna L., Jolivet geological field trips 2013 - 5(1.1) references 72 - s is. ne (Sicilia). www.meigepeg.org R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen scopy: J. Structural Geology, 15: 369-382. Geology, Structural scopy: J. 1: 35-50. Min., Per. for the southern sector of Calabria-Peloritani metamorphism in the Aspromonte Massif: implications for a new framework 50: 423-441. Geol. Review, Orogen (Italy). Inter. Unit (Lower Unit) in the central Unit (Upper Unit) and Madonna dei Polsi contact between the Aspromonte - Peloritani 109: 455-469. Aspromonte area (Calabria). Boll. Soc. Geol. It., Plinius, 28: 214-216. 109: 655-673. Arc, Southern Italy). Boll. Soc. Geol. It., Mts. (Calabria-Peloritani Aspromonte nappe of northeastern Peloritani 5: 353-379, Siena. 276, Newsletter, Arc – southern Italy): IGCP, the Aspromonte Unit (Calabrian Peloritan (Sicilia nord-orientale). Boll. Soc. Geol. It., 94: 537–554. (Sicilia nord-orientale). Boll. Soc. Geol. It., 173 (1): 3-15; DOI: 10.2113/173.1.3. Bull. Soc. Geol. France, terra- of the peri-Gondwana microplate in the evolution of augen gneisses from Calabria (Italy), with inference to the Alboran 96: 843-860. Earth Scien., Jour. nes. Inter. 85-1: 31-56. Mitt., Petrogr. (Calabria - Italy). Schweiz. Mineral. DOI: 10.3301/GFT.2013.01 Pezzino A. (1982) - Confronti petrografici e strutturali tra i basamenti metamorfici delle unità inferiori dei Monti Peloritani tra e strutturali A. (1982) - Confronti petrografici Pezzino Ortolano G. & Punturo R. (2008) - Alpi Lo Giudice A., Fiannacca P., E., Fazio E., De Vuono Cirrincione R., Angì G., A., Pezzino of the & Lo Giudice A. (1990) - Geometry and metamorphic environment Ioppolo S. P., Atzori Puglisi G., S., Pannucci A., Pezzino Messina A. & Somma R. (2002) - Pre-Alpine and Alpine Tectonics in the Southern Sector of the Calabria-Peloritani Arc (Italy). in the Southern Sector of Calabria-Peloritani and Alpine Tectonics Messina A. & Somma R. (2002) - Pre-Alpine in the A.M. & Giacobbe A. (1990) – Alpine metamorphic overprint De Francesco S., Russo Compagnoni R., Messina A., in the crystalline basement of (1992) - Alpine metamorphic overprint S. A.M. & Russo De Francesco Compagnoni R., Messina A., of Catania (Italy) Website at the University Group (MeIGePeG) Metamorphic and Igneous Geo-Petrology Limanowsky M. (1913) - Die grosse Kalabrische Decke: Bulletin Societe Cracovie, Cl. Sc. Math., Nat., Serie, v. 6: 370–385. Serie, v. Nat., Cl. Sc. Math., Bulletin Societe Cracovie, Decke: Limanowsky M. (1913) - Die grosse Kalabrische 142: 966-968. 1001-1009, Par phénomènes de charriage en Sicilie. C. R. Acad. Sc., Lugeon M. & Argand E. (1906) – Sur les grands Piccarreta G. & Deloule E. (2007) - Latest Precambrian to Early Cambrian U–Pb zircon age A., Fornelli Barbey P., Micheletti F., 64 – 65: 183-212. Min. Sic., dello schema geologico della Sicilia nord-orientale. Riv. Ogniben L. (1960) - Nota illustrativa 8: 453–763. Mem. Soc. Geol. It., alla geologia del confine calabro-lucano. Ogniben L. (1969) – Schema introduttivo 12, 243–585. Ogniben L. (1973) – Schema geologico della Calabria in base ai dati odierni. Geol. Romana, of alpine metamorphism in the southern Aspromonte Massif evolution A. (2005) - P-T Cirrincione R. & Pezzino Ortolano G., micro by computer-aided spatial and orientation analysis of quartz c-axes C. (1993) - Integrated Heilbronner R. & Pauli Panozzo Lentini F. & Vezzani L. (1975) - Le unità meso-cenozoiche della copertura sedimentaria del basamento cristallino peloritano della copertura L. (1975) - Le unità meso-cenozoiche & Vezzani Lentini F. R. (2002) - How does the Alpine belt end between Spain and Morocco? & Montigny Goffé B. H., Feinberg Chalouan A., Michard A., geological field trips 2013 - 5(1.1) references 73 l. ic ]: m ra a- nian ment ships . (1990) R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen crust. In: M.H. Salisbury, Fountain D.M. (Eds.). Exposed Cross Sections of the Continental Crust. Dordrecht: Kluwer, 21-42. (Eds.). Exposed Cross Sections of the Continental Crust. Dordrecht: Kluwer, D.M. Fountain crust. In: M.H. Salisbury, of the Serra, Southern Calabria (Italy). Contrib. Mineral. Petrol., 73: 23-38. Petrol., Mineral. Southern Calabria (Italy). Contrib. of the Serra, Abstracts, 1: 350. Abstracts, between intermediate and acidic rocks in orogenic granitoid suite: petrological, geochemical and isotopic (Sr, Nd, Pb) data fro suite: petrological, geochemical and isotopic (Sr, between intermediate and acidic rocks in orogenic granitoid 92: 153-176. (Southern Calabria, Italy). Chem. Geol., Capo Vaticano 352 p. Geologica Ultraiectina, The Netherlands, Utrecht University, 230: 19–48, doi: 10.1016/0040-1951(94)90145-7. block (Southern Italy): Tectonophysics, tion of the Calabro-Peloritan segnature of the Sila Piccola Massif nappe stack (Calabria, Italy): Insights for the tectonic evolution of the Calabrian Arc, segnature of the Sila Piccola Massif nappe stack (Calabria, Italy): Insights for tectonic evolution 20: 112–133. Tectonics, Lithos, 24: 97-119. from the Calabrian Arc, Southern Italy. Hercynian granitoids of contrasting – Petrogenesis 5: 737-754. Mineral., J. Eur. Calabrian Arc, Italy. trale. Geometria dei loro rapporti, ambientazione metamorfica del loro contatto e caratteri petrografici delle metamorfiti. Bol petrografici ambientazione metamorfica del loro contatto e caratteri Geometria dei loro rapporti, trale. 111, 69–80. Soc. Geol. It.,: 83: 41-58. south Italy). Eclogae Geol. Helv., 63: 153-168. Min., tionships. Per. s. 3, 13: 63-179. Berlin. kl., doi:10.1029/2003TC001518. 23, TC1013, Sicilian Maghrebides Tectonics, DOI: 10.3301/GFT.2013.01 Schenk V. (1990) - The exposed crustal cross section of southern Calabria, Italy: structure and evolution of a segment Hercy (1990) - The exposed crustal cross section of southern Calabria, Italy: structure and evolution Schenk V. Schenk V. (1980) - U-Pb and Rb-Sr radiometric dates and their correlation with metamorphic events in the granulitic-facies base in the granulitic-facies dates and their correlation with metamorphic events radiometric (1980) - U-Pb and Rb-Sr Schenk V. Scheepers P.J.J. (1994) - Tectonic rotations in the Tyrrhenian arc system during the Quaternary and late Tertiary [Ph.D. thesis [Ph.D. arc system during the Quaternary and late Tertiary rotations in the Tyrrhenian (1994) - Tectonic Scheepers P.J.J. evidence for a Pleistocene clockwise rot (1994) - Paleomagnetic & Hilgen F. J.D.A. Zijderveld Langereis C.G., Scheepers P.J.J., from U–Pb zircon data. Ter (1989) - The age of the Adriatic crust in Calabria (southern Italy): constraints W. & Todt Schenk V. Rottura A., Bargossi G. M., Caironi V., Del Moro A., Maccarrone E., Macera P., Paglionico A., Petrini R., Piccareta G. & Poli G Piccareta G. & Poli R., Petrini A., Paglionico P., Macera Maccarrone E., Del Moro A., Caironi V., Bargossi G. M., A., Rottura from the granites of Hercynian peraluminous Campana R. & Del Moro A. (1993) – Petrogenesis Caggianelli A., A., Rottura Bargossi G. & Piccarreta (1991) - Relation Caggianelli A., A., Peccerillo R., Petrini Pinarelli L., Del Moro A., A., Rottura Platt J.P. & Compagnoni R. (1990) – Alpine ductile deformation and metamorphism in a Calabrian basement nappe (Aspromonte, Platt J.P. and petrogenetic rela- Aspromonte area: geological, mineralogical A. (1994) - Metamorphism in the central Puglisi G. & Pezzino Abh. Ges. Wiss. Gottingen, Mat. Phys. Massivs und seiner Randgebiete. des Kalabrischen (1935) – Der deckenbau H.W. Quitzow Sea, the Apennines, and of the Tyrrhenian G. & Lister (2004) - Neogene and Quaternary rollback evolution Rosenbaum and metamorph Funiciello R. & Mattei M. (2001) - Alpine structural Argentieri A., Monié P., Goffé B., C., Faccenna F., Rossetti Pezzino A., Puglisi G., Pannucci S. & Ioppolo S. (1992) - Due unità cristalline a grado metamorfico diverso in Aspromonte cen- metamorfico diverso (1992) - Due unità cristalline a grado & Ioppolo S. S. Pannucci Puglisi G., A., Pezzino geological field trips 2013 - 5(1.1) references 74 1: oscano C. R. Cirrincione - E. Fazio P. Fiannacca G. Ortolano A. Pezzino Punturo V. Romano The Alpine evolution of the Aspromonte Massif: contraints for geodynamic reconstruction Calabria-Peloritani Orogen Res., 91: 10,229-10,245. Res., 173: 1-23. Publ., 44, 1: 29–130. Eclogae Geol. Helv., 109-129. 324: 267-320. model for the northern sector of Calabrian Arc. Tectonophysics, A. (2000) - A new structural & Zerilli 22: 855-865. Research. Mountains. Gondwana A zircon tale from the basement of Peloritani extension within the Alpine Orogen). Geol. Soc. basins; Tertiary slab roll-back and detachment (in The Mediterranean 156: 109-120. Special Publ., DOI: 10.3301/GFT.2013.01 Stampfli G. (2000) - Tethyan oceans (in Tectonics and magmatism in Turkey and the surrounding area). Geol. Soc. London, Spec. and magmatism in Turkey oceans (in Tectonics Stampfli G. (2000) - Tethyan Staub R. (1951) - Uber die Beziehungen zwischen Alpen und Appennin Gestaltung der alpinen Leitlinien, Europas: 4: 927-940. Petr., Soc. It. Mineral. Rend. Calabro Peloritano. dell’Arco L. (1982) - Lineamenti geologico-strutturali Tortorici 11 Disaggregazione palinspastica. Boll. Soc. Geol. It., (1992) - Il segmento calabro-peloritano dell’orogene ercinico. G.B. Vai T S., Toricelli M., Riva Merlini S., Golfetto F., Frixa A., Costa V., Cantarella G., G.P., Brancaleoni Bello M., Dijk J.P., van origin and early geodynamic history of NE Sicily: A. (2012) - Peri-Gondwanan Cirrincione & Pezzino Fiannacca P., Williams I.S., subduction regime followed by a westward-directed (1999) - Alpine plate kinematics in the western Mediterranean; H.P. Zeck Shreve R.L. & Cloos M. (1986) - Dynamics of sediment subduction, melange formation, and prism accretion: Journal Geoph. Shreve