Geological Field Trips

Società Geologica Italiana

2013 Vol. 5 (1.2) ISPRA Istituto Superiore per la Protezione e la Ricerca Ambientale

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

ISSN: 2038-4947

From the upper to the lower continental crust exposed in Calabria 86° Congresso Nazionale della Società Geologica Italiana Arcavacata di Rende (CS) 2012

DOI: 10.3301/GFT.2013.02 From the upper to the lower continental crust exposed in Calabria A. Caggianelli - G. Prosser - V. Festa - A. Langone - R. Spiess

GFT - Geological Field Trips 5(1.2) - 2013 trips field geological Periodico semestrale del Servizio Geologico d'Italia - ISPRA e della Società Geologica Italiana Geol.F.Trips, Vol. 5 No.1.2 (2013), 49 pp., 26 figs., 2 tabb. (DOI 10.3301/GFT.2013.02) From the upper to the lower continental crust exposed in Calabria

86° Congresso Nazionale della Società Geologica Italiana-Arcavacata di Rende (CS), 18-20 settembre 2012 Alfredo Caggianelli (1), Giacomo Prosser (2), Vincenzo Festa (1), Antonio Langone (3), Richard Spiess (4)

(1) Dipartimento di Scienze della Terra a Geoambientali, Università di Bari, via Orabona 4, 70125 Bari (2) Dipartimento di Scienze della Terra, Università della Basilicata, Macchia Romana 1, 85100 Potenza (3) IGG CNR, via Ferrata 1, 27100 Pavia (4) Dipartimento di Geoscienze, Università di Padova, via Gradenigo 6, 35131 Padova Corresponding author e-mail address: [email protected]

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

ISSN: 2038-4947 [online] http://www.isprambiente.it/site/it-IT/Pubblicazioni/Periodici_tecnici/Geological_Field_Trips

The Geological Survey of Italy, 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.2013.02 From the upper to the lower continental crust exposed in Calabria A. Caggianelli - G. Prosser - V. Festa - A. Langone - R. Spiess geological fieldtrips2013-5(1.2)

INDEX Itinerary

DAY 1 Stilo area...... 21 Stop 1.1 ...... 22 Stop 1.2 ...... 23 Information Pietragrande and Squillace area...... 24 Stop 1.3...... 26 Riassunto...... 4 Stop 1.4 ...... 27 Abstract...... 4 General Info...... 5 DAY 2 3 Capo Vaticano area...... 28 Stop 2.1...... 29 Excursion notes Palmi area...... 30 Stop 2.2 ...... 32 1 - Introduction...... 7 Stop 2.3 ...... 33 2 - Crust composition...... 7 Stop 2.4 ...... 34 3 - Timing of the Hercynian metamorphic and magmatic events in the continental crust...... 12 DAY 3 4 - Hercynian P-T evolution...... 14 Curinga area...... 35 4.1 - Lower crust...... 14 Stop 3.1 ...... 35

4.2 - Upper to intermediate crust...... 15 Girifalco area...... 38 index 5 - Crust exhumation...... 17 Stop 3.2 ...... 38 5.1 - Late Paleozoic - Mesozoic evolution...... 18 Stop 3.3 ...... 41 5.2 - Eocene - Early Oligocene contractional tectonics...... 18 5.3 - Oligocene to Miocene evolution...... 19 References ...... 44

DOI: 10.3301/GFT.2013.02 geological field trips 2013 - 5(1.2)

4 information A. Caggianelli - G. Prosser V. Festa Langone R. Spiess From the upper to lower continental crust exposed in Calabria ertiary geological evolution that brought to the surface different cru- ertiary geological evolution ata durante il ciclo orogenico ercinico. Questa circostanza particolare è stata il ciclo orogenico ercinico. ata durante Calabria, crosta continentale, orogenesi ercinica, granitoidi, metamorfismo di contatto, granuliti DOI: 10.3301/GFT.2013.02 Riassunto un profilo completo della che rappresentano In Calabria sono esposte sezioni del basamento pre-Mesozoico crosta continentale struttur causata dalla tettonica terziaria che ha determinato l’esumazione dei diversi livelli di crosta. L’escursione livelli causata dalla tettonica terziaria che ha determinato l’esumazione dei diversi possa essere utile per tarare della crosta continentale che si spera a fornire un quadro generale mira si snoda nella parte centro-meridionale della Calabria modelli geochimici, reologici e geofisici. L’itinerario e di Monte Sant’Elia. il Massiccio delle Serre ed i promontori di Capo Vaticano e principalmente attraverso dei e strutturali compositive i tre giorni di escursione è possibile esaminare le caratteristiche Durante rocce quella inferiore. Si possono osservare di crosta, a partire da quella superiore verso livelli diversi dei gra- distintive ed apprezzare le caratteristiche sino alla facies granulitica metamorfiche dal basso grado profondità. Gli effetti dell’intensa perturbazione termica causata dalla messa in nitoidi intrusi a diversa nella netta sia nella crosta superiore che in quella inferiore, ovvero sono osservabili posto dei granitoidi anche la visita prevede L’itinerario rispettivamente. migmatitica di bordo, aureola di contatto e nella zona risultano ben visibili gli effetti della deformazione localizzata, prodotta dalla tettonica terzia- ove di zone che duttili. sia in condizioni fragili ria sulle rocce paleozoiche chiave: Parole Abstract of the whole Hercynian continental crust are expo- basement, representative Outcrops of the pre-Mesozoic sed in Calabria. This is the result of T picture of the continental crust that hopeful- a general This geological field trip aims to provide stal levels. models. The itinerary for geochemical, rheological and geophysical represent a reference frame ly may and southern parts of Calabria, namely in the Serre massif promontories in central develops fea- and Monte Sant’Elia. it is possible to examine compositional and structural In three days Capo Vaticano facies metamor- to granulite low-grade tures across an entire crust section. Thus rocks affected by very geological field trips 2013 - 5(1.2)

5 information upper Finally, A. Caggianelli - G. Prosser V. Festa Langone R. Spiess From the upper to lower continental crust exposed in Calabria els. The venue of the 2012 Congress Italian Geological Society in Cosenza was els. The venue Calabria, continental crust, Hercynian orogeny, granitoids, contact metamorphism, granulites DOI: 10.3301/GFT.2013.02 and in the lower crust, in a sharp metamorphic aureole and in a migmatitic border zone, respectively. and in the lower crust, a sharp metamorphic aureole migmatitic border zone, tectonics in the rocks with strongly partitioned deformation, produced by Tertiary some cases of Paleozoic brittle and the ductile domains, can be observed. words: Key General info continental crust are exposed from the Calabria is one of the few sites where cross-sections Paleozoic upper to the lower lev phism and distinctive features of granitoids emplaced at different structural levels will be examined. The levels emplaced at different structural features of granitoids phism and distinctive emplacement are visible both in the effects of the intense thermal perturbation produced by granitoid the ideal opportunity to take this field trip and to visit some of the most interesting sections. the ideal opportunity to take the intermediate and lower crust across the Serre massif, focussed on the upper, The field trip lasts three days and Mt. Sant’Elia promontories. Capo Vaticano emplaced in the intermediate crust and facies rocks and migmatites of the lower crust, granitoids Granulite sequences affected by contact metamorphism in the upper crust are examined three days. Paleozoic picture of the Calabria continental crustal section and to pro- The goal of the field trip is to outline a general models. Although the main theme of and geophysical for geochemical, structural vide a reference frame is the Hercynian continental crust, selected Stops include also some outcrops with notable exam- excursion ples of Alpine deformation. in six can be observed features of the rocks belonging to different crustal levels and structural Petrographic selected areas (Fig. 1), following this sequence: – Squillace area (Stops 1.3 and 1.4), during the whole first day; Stilo area (Stops 1.1 and 1.2) Pietragrande area (Stops 2.2 - 2.4), during the whole second day; area (Stop 2.1) and Palmi Capo Vaticano Curinga area (Stop 3.1) and Girifalco (Stops 3.2 3.3), during the first half of third day. It is The field trip starts from Stilo (RC), a historical village famous for the nice byzantine church “Cattolica”. the next the first night there. For before the start of field trip and to stay suggested to reach Stilo the day two nights the suggested locality is village of Ricadi (VV) and neighbourhood (Fig. 1), offering a wide range geological field trips 2013 - 5(1.2)

6 information area Stops of the 3in the Girifalco day area A. Caggianelli - G. Prosser V. Festa Langone R. Spiess From the upper to lower continental crust exposed in Calabria 3.3 - An outline of the itinerary followed in the three days of the field trip. of the field trip. followed in the three days - An outline of the itinerary Fig. 1 DOI: 10.3301/GFT.2013.02 of accommodation options. From the last Stop field trip it is possible to reach in about 45 minutes station in Calabria (Fig. 1). Lamezia Sant’Eufemia, the location of main airport and railway will be of about are foreseen for each Stop and the maximum elevation In the field trip short and easy trails for the essential hiking boots and rain It is not required a particular equipment, except see level. 900 m above or poncho. jacket geological field trips 2013 - 5(1.2)

7 excursion notes A. Caggianelli - G. Prosser V. Festa Langone R. Spiess From the upper to lower continental crust exposed in Calabria ature related to Calabria (see Amodio Morelli et al., 1976 ature related to Calabria (see Amodio Morelli et al., : : ertiary tectonics and to significant exposures of the lower crust detailed by researchers Bari University DOI: 10.3301/GFT.2013.02 1 - Introduction feature in the geological frame Continental crust sections across the Calabria massifs represent a distinctive of the region. Examining plentiful scientific liter & 1978; Paglionico 1973; Moresi et al., Amodio Morelli et al., under the guidance of Giuseppe Piccarreta (e.g., 2002) and by Schenk (see references cited in the et al., 1991; Fornelli Piccarreta, 1978; Caggianelli et al., Introduction). The continental crust exposed in the Serre Massif can be simplified as follows, from top to bottom: Upper crust and Bonardi et al., 2001 for a review), a role of precursor in drafting continuous sections of the pre-Mesozoic 2001 for a review), role of precursor in drafting and Bonardi et al., Schenk Volker Dubois, 1970, 1971, 1976). Afterwards, Dubois (e.g., basement should be ascribed to Roland Schenk, 1980, 1981, 1984, 1989, studies (e.g., starting from the eighties, detailed in several and co-workers, 2000) continental crustal sections in the Serre, 1990; Grässner & Schenk, 1999, 2001; Grässener et al., Aspromonte and Sila massifs made them well known to a worldwide scientific community. basement exposed vision of the Palaeozoic an integral fundamental in providing Merit of these scientists was in Calabria, obscured when numberless tectonic domains and units, sometimes with different suggested pro- been proposed. have venance, are by Dubois (1971) and Schenk (1980) for the Sila Serre massifs, respectively, Cross-sections, provided shown in Fig. 2. 2 - Crust composition structure by disturb produced on the Palaeozoic The Serre crustal section is best known, owing to the weaker T 1) phyllites and slates with intercalations of metavolcanics and marbles; and slates with intercalations of metavolcanics 1) phyllites 2) micaschists and paragneisses. Intermediate crust 3) isotropic to weakly foliated granodiorites; geological field trips 2013 - 5(1.2)

8 excursion notes B 3 A 2 4 1 5 2 3 5 6 5 st u w er st niens l o cr y rite erc er cr u h oic cor d i é ic si ll l asite ranite es upp f à a e ric d es et ists eso z /G t h h one fè res /m z ites cco -py /M - si l-Kf s -q t z x or ph i qu g neiss a phyll b oni d esc bu g ranite l ite ite m oic ents d iorite d-b t e ul d e ariant yp - cr d i m on g o l eo z eta p e A. Caggianelli - G. Prosser V. Festa Langone R. Spiess mé ta ni v L - t etro g ra a ona l ite ïd scar d eanate se pp e G ran R U g rt G neisses o f P M D ioritic T G rano S l o ul ites d e B ) is modified after Grässner & Schenk, e v ri vé s ranito ran in z i g ites an d e n ias ) massifs, respectively (modified after b ) massifs, respectively dé -E 2-G 1-L 3 5-K 6-G 4-B E S oic ites l eo z a NE Phyll P

des From the upper to lower continental crust exposed in Calabria a ) and Serre (

phylla reo l e 10 km Au C ontact

CALCAIRE 1999. PHYLLADIQUE 5

S

LIA 0 G ranites NW S ona l ite T - section z nit

e U G neiss Qu art D ioritic

itesarit é i d r

co l ite anatex nit U eta p e Si l across M Serre- section cross

es

it g i l asite

inz ric k nit -Py U

ites ul ite

ul - Cross-sections by Dubois and Schenk for the Sila ( G ran

OCLE ANTE HERCYNIENgran COUVERTURE S d e Fig. 2 ists neisses h a b W Sc N Dubois, 1971 and Schenk, 1980). The geological map of Southern Calabria in ( etro g ra S R AB an dG DOI: 10.3301/GFT.2013.02 geological field trips 2013 - 5(1.2)

9 excursion notes 30 ' 0' 0' 4 5 38 ° 38 ° 38 ° 30 ' Pietragrande ° 1 6 A. Caggianelli - G. Prosser V. Festa Langone R. Spiess 0' 2 ° 1 6 From the upper to lower continental crust exposed in Calabria l t s i c r o c k s i c contacts and fau u r a s s -J o s t P T e c t o n 00 ' ° 1 6 - Geological sketch map of the Serre Massif, Capo Vaticano and Sant’Elia promontories (modified Capo Vaticano map of the Serre Massif, - Geological sketch from: Borsi et al., 1976; Fornelli et al., 1994; Grässner & Schenk, 1999; Rottura et al., 1991). et al., 1994; Grässner & Schenk, 1999; Rottura et al., 1976; Fornelli from: Borsi et al., 30 ' Fig. 3 38 ° DOI: 10.3301/GFT.2013.02 geological field trips 2013 - 5(1.2) excursion notes 10 : A. Caggianelli - G. Prosser V. Festa Langone R. Spiess - Schematic lithological column for the Serre crustal section (modified from Festa et al., 2004). et al., crustal section (modified from Festa Fig. 4 4) peraluminous K-feldspar megacrystal – bea- K-feldspar 4) peraluminous and granodiorites; ring granites 5) foliated tonalites and quartz diorites. Lower crust 6) migmatitic border zone and garnet-bearing 6) migmatitic border zone quartz diorites; 7) migmatitic paragneisses; 8) felsic granulites; 9) mafic granulites. Additional information can be gained examining map of Fig. 3 and the the geological sketch lithological column of Fig. 4. Owing to the tecto- tilting produced by Tertiary crust-scale nics, the lithological succession can be followed on map (Fig. 3) from the SE (top) to NW (bottom). Thickness of the exposed lower, intermediate and upper crust are about 8, 13 (Fig. 4). Spinel perido- and 3 km, respectively tites occur as intercalations in the lower crust and do not represent the evidence for Therefore, the real transition. crust-mantle thickness of the former lower crust can be lar- The same holds for the upper crust, where ger. limestones and thin siliciclastic depo- Mesozoic contact with the basement. sits are in erosive - - From the upper to lower continental crust exposed in Calabria e - i tes ; v - one ; n i t ; agne i sses e tecton i c li tes i nc l ud ng n i t ; lli tes w i th nter er U y iv zz ano comp l ex ; d i or tes to tona li - i c li mestones co z- i to ds ; l um i nous gran o l can i tes be ong ng to li tes ; e l s i c granu R Pomo v - fe l dspar megacryst urass Pera K n i t ;

metagabbro i c rocks l ayered and sp i ne l per dot tes ; 12 - C astagna U 13 – 14 – Pre -i ntrus iv contact ; 15 – Al p i ne tecton c contact . 11 - Maf i c granu L egend 1 – J r i ng the basement of S il a U 2 - i or tes and gran 3 - Granod 4 - i or tes ; bear i ng granod 5 - Quart w i th nterbedded ( a ) marb l es and ( b ) metabas i tes ; 1 0 - F bedded ( a ) marb l es and b meta the St il o - Pa i s 7 - M i casch sts and paragne ses be l ong i ng to the Mammo a comp l ex ; 8 - M i gmat t c border z 9 - M i gmat t c par tes ; 6 - S l ates , ph

S I L A U N I T I N U A L I S

T S U R C L NTINENTA O C CYNIAN R ATE-HE L R E PP U O T R E LOW 8 9 10 11 2 3 4 5 6 7 1 12 13 14 15 a b a a

b b bathozone

S E RR

m k 0 2 m k 7 DOI: 10.3301/GFT.2013.02 geological field trips 2013 - 5(1.2) excursion notes 11 content 3 O 2 A. Caggianelli - G. Prosser V. Festa Langone R. Spiess From the upper to lower continental crust exposed in Calabria ) peraluminous granites compositionally restricted, essentially two-micas granites ) peraluminous ii ) metaluminous granitoids, compositionally ranging from tonalite to granite and including more mafic rocks such from tonalite to granite compositionally ranging ) metaluminous granitoids, i DOI: 10.3301/GFT.2013.02 monzogranites with Al-silicates. Both granitoid types have in most cases a hybrid mantle-crust signature, and, the- in most cases a hybrid types have with Al-silicates. Both granitoid monzogranites to partial melting of mantle or continental crust refore, genesis of parental magma cannot be attributed exclusively source rocks. or paragneiss, and phyllite granodiorites and upper crustal rocks, involving The contact between granitoids andalusite-cordierite metamorphic aureole (Colonna et al., by a well developed is sharp and characterized 1973). can be applied also to the Sila Massif. with few variations, The simplified scheme outlined above, granites The thickness of the exposed crust is lower and can be estimated to about 20 km. Among granitoids, 1994) are present. tonalites. In addition, mafic bodies of olivine-norite (Caggianelli et al., over prevail been made by chemical composition of the Calabria continental crust have to estimate the overall Attempts for the Sila and Serre mas- Schenk (1990), Caggianelli & Prosser (2001), Acquafredda et al. (2003). Results 1. A comparison with worldwide compilations by Christensen & Mooney (1995) in Table sifs are portrayed by a distinctly higher Al & Gao (2003) shows that Calabria crust is characterized and Rudnick as gabbros, diorite and quartz diorite; ( The contact between the lower crust and the granitoids, usually involving migmatitic paragneisses and tonali- migmatitic paragneisses usually involving The contact between the lower crust and granitoids, are Here, paragneisses and can be described as a migmatitic border zone. tes/quartz diorites, is transitional affected by a higher degree of partial melting and tonalites include abundant metamorphic basement xenoliths and giant crystals of garnet. in several by Alessandro Rottura in Calabria has been given study of granitoids A strong impulse on the advanced et al.,papers (e.g. Rottura 1990, 1991, 1993). Broadly, types: can be attributed to two main calc-alkaline granitoids ( and by lower contents in MgO and CaO. These differences reflect the abundance of metapelites both in and by lower contents in MgO CaO. They appe- granites. peraluminous lower and upper crust of Calabria possibly the presence several are more abundant than tonalites. Another intere- where granites ar more pronounced in the Sila Massif, heat production, resulting from of radiogenic sting feature of the crust exposed in Calabria is high value such as allanite, zircon and and the widespread presence of accessory minerals, the abundance of granitoids of abundant also in the migmatitic paragneisses monazite and zircon are relatively monazite. In particular, the lower crust. geological field trips 2013 - 5(1.2) excursion notes 12 crust Lower 0.92 0.19 5.6 1.2 1.3 0.2 49 11 Bulk crust 456 259 320 148 0.20 0.13 0.10 -3 Bulk crust crust Lower 1.48 1.03 crust Lower A. Caggianelli - G. Prosser V. Festa Langone R. Spiess Bulk crust - Estimates of the chemical composition 12 3 45 67 0.83 0.805.94 1.08 5.74 1.1 7.53 9.2 0.90.14 0.72 6.89 0.14 0.82 6.71 0.15 8.57 Bulk 64.93 64.7418.56 61.55 17.37 56.0 18.69 62.4 20.0 60.6 14.9 53.4 15.9 16.9 crust 3 From the upper to lower continental crust exposed in Calabria t 5 O 2.16 2.49 2.05 2.1 3.6 3.07 2.65 2 2 O 2 Table 1 O 3.38 2.78 1.99 2.1 2.1 1.81 0.61 O 2 (2003). 2 2 continental crust for the Sila (1) and Serre (2-4) sections. of the bulk (5, 6) and lower comparison, global averages For Compositions in columns 1 to (7) continental crust are provided. 3 recalculated anhydrous. heat production in µW m * Bulk radiogenic 1 - Caggianelli & Prosser (2001); 2, 3 – Acquafredda et al. (2003); & Gao 4 – Schenk (1990); 5 - Christensen & Mooney (1995); 6, 7 Rudnick A* 2.11 1.73 U 2.72 1.68 Th 14.8 14.1 14.0 Al MnOMgO 0.08CaO 2.37Na 0.10 1.59 2.37 0.12 3.46 3.28ppm 3.57 4.9Ba 4.4Rb 3.1 585 0.10Sr 137 5.8 0.10 4.66 844 126 0.10 6.41 7.24 83 204 724 9.59 58 217 P TiO FeO K wt.% SiO y, the Calabria y, DOI: 10.3301/GFT.2013.02 3 - Timing of the Hercynian metamorphic and magmatic events in the continental crust that shaped The ages obtained for the events the Calabria crustal sections are presented. Before the Hercynian orogen crust underwent some significant geological episodes witnessed by the occurrence of fre- to Silurian ages obtai- quent neo-Proterozoic and paleontological ned both from radiometric here for methods. Only a short account is given a detailed discussion, the these older ages. For reader should refer to the paper by Micheletti et al., (2007) and Williams et al. (2011). A neo- magmatism with bimo- Proterozoic-Cambrian has been extensively dal chemical character documented in Calabria (e.g. Micheletti et al., 2011). Mafic et al., 2007; 2008; 2011; Fornelli magmatic bodies emplaced between 593±14 and 574±18 Ma whereas felsic ones provided ages between 562±15 and 526±10 Ma. Also in gra- Mountains, neo-Proterozoic the Peloritani been recognized nitoids (~565-545 Ma) have augen gneisses as protoliths of granitic 2011), whereas felsic igneous, (Williams et al., an give rocks (“porphyroids”), usually volcanic age of 456-452 Ma (U-Pb Upper Ordovician 2004). Inherited zir- et al., data by Trombetta

geological field trips 2013 - 5(1.2) excursion notes

13

y it l i b a ob r p e v ati l re 8 0 0 6 4 03 03 a age ,M anitoids g r 0 300 3 2 8 2 d y kes 0 A. Caggianelli - G. Prosser V. Festa Langone R. Spiess 2 6 - Spectrum of the Hercynian ages (n=44) 4 03 2 Fig. 5 0 8 4

granitoids and dykes are also indicated. and dykes granitoids

recorded in the Serre and Sila lower crust. All ages were determined by U-(Th)-Pb method on zircon and monazite. Number of ages related to each peak of ages for are detailed in the text. Ranges

2 16 12 s age of er umb n From the upper to lower continental crust exposed in Calabria DOI: 10.3301/GFT.2013.02 con and/or xenocrystic zircon cores from both metasedimentary rocks and orthogneisses confirm a wide- con and/or xenocrystic of these rocks suggest also a reworking The spectra magmatic activity. spread Cambrian-neo-Proterozoic of older basement rocks. only geochronological data obtained with comparable discussion on Hercynian events, a comprehensive For focused showing similar properties as geochronometers were considered. We methods and applied on minerals and SIMS methods on zircon and/or EMPA LA-ICP-MS, our discussion on U-(Th)-Pb data obtained by TIMS, rocks from Starting from 1980, geochronological studies were directed to high grade monazite and/or xenotime. metamor- the lower crust segments. Among high grade phic rocks, more attention has been paid to the Serre Massif. to the other lower crustal Geochronological data relative Northern Calabria) or lac- rocks are scarce (e.g. Sila Massif, area, Southern Calabria). A few data are availa- king (Palmi facies rocks of the ble also for the greenschist-amphibolite data for the grani- Instead, radiometric upper crustal levels. toids of the intermediate crust are homogeneously distribu- ted among the Calabria massifs. Large part of these data are explicitly attributed to the late stage of Hercynian metamor- by decompression, high-T characterised orogeny magmatism. phism and granitoid (zircon, monazite U-(Th)-Pb data from different minerals metamor- point to a major high temperature and xenotime) This boundary. at the Carboniferous-Permian phic event is recorded by metasediments of both the lower and event upper crustal rocks. The data set for the lower crust exposed in Serre and representation and Sila massifs is adequate for a graphical (Fig. 5). to outline an age spectrum of the Hercynian events of ages falls bet- It is evident that the major concentration ween 290 and 305 Ma (n = 20). Three other peaks are also geological field trips 2013 - 5(1.2) excursion notes 14 A. Caggianelli - G. Prosser V. Festa Langone R. Spiess T paths are here grouped for the lower and From the upper to lower continental crust exposed in Calabria 4 - Hercynian P-T evolution upper to intermediate crust, respectively. upper to intermediate crust, respectively. 4.1 - Lower crust the lower crust numerous determination are now For path starting from the classical Serre P-T-t available, by by Schenk (1989; Fig. 6). This is characterized facies metamorphic conditions of 790 ± peak granulite at 300 ± 10 Ma. In this state 30 °C and 750 ± 50 MPa the fertile lower crust underwent widespread partial melting. Metapelites were mostly affected by this pro- cess with a maximum degree of melting 50-60% left after melting 1991). Restites (Caggianelli et al., P-T evolution has been determined for various levels has been determined for various evolution P-T of the continental crust exposed in Calabria mas- sifs. The P- 0 00 9 8 2 00 ± 10 3

700

l P

Cpx

+

x

+ l

o

00 D Op l Ca

Grt

+ 6

450 +

Tr

Fo

+

i D 0 215 500 °C , T 400 00 3 25 110 145 1 8 200 - Classical P-T-t path defined by Schenk - Classical P-T-t 15 100 10

00 00

Fig. 6

200 400 6 8 MPa , P Numbers along the path indicate time in Ma. (1989) for the deeper level of the Serre lower crust. The (1989) for the deeper level of the Serre lower crust twin path for the top level proposed in the original figure has been here omitted. DOI: 10.3301/GFT.2013.02 present, located approximately at 280 (n = 10), 320 Ma 6) and 260 4). Minor peaks (n=2), present, located approximately history. different steps in the prograde indicate, together with the 320 ma event, 370 and 345 Ma may between 319 and 359 Ma, are recorded also in metamorphic rocks of early Hercynian events, Interestingly, 2008). 1994; Grande, dates and chemical dating of monazite (e.g. Acquafredda et al., the upper crust by Rb-Sr recorded in the Magmatic activity appears to be synchronous with the two main metamorphic events of the intermediate crust fall mostly in 290-305 Ma lower crust. In fact, ages related to granitoids of the Sila and Serre mas- whereas zircon U-Pb ages, recently obtained for late magmatic dykes range et 2010; Romano et al., magmatic activity (Festa sifs, are close to 280 Ma and mark the Lower Permian 2011). al., geological field trips 2013 - 5(1.2) excursion notes 15 A. Caggianelli - G. Prosser V. Festa Langone R. Spiess From the upper to lower continental crust exposed in Calabria DOI: 10.3301/GFT.2013.02 are massive rocks (fels) with high content in garnet and sillimanite or cordierite. After peak meta- are massive morphism, rocks of the lower crust underwent a nearly isothermal decompression followed by significant iso- by recognition of reaction textures (Schenk, 1984) related to were constrained baric cooling. Both trajectories equilibria: + plagioclase = orthopyroxene garnet + clinopyroxene (in mafic rocks, Fig. 6), and garnet + sillimanite = cordierite spinel (in metapelites) took place between 300 ± 10 and 290 Ma whereas isobaric cooling proceeded Decompression from 750 to 550 MPa tectonics promoted final exhumation of the lower crust. slower pace, up to 25 Ma when Tertiary at a progressively In of P and T. peak values by more elevated paths recently published are more complex and characterized P-T evo- et al. (2011), outlines for the lower crust a step-wise path, recently proposed by Fornelli addition, a P-T lution with two distinct episodes of decompression (Fig. 7a). Schenk (1990) suggested that paths and geologic evolution? What is the relationship between lower crust P-T continen- facies metamorphism is an active of granulite geological setting for the development the most likely a subduction zone. tal margin overlying The question has been also addressed by Caggianelli et al. (2007) through numerical modelling. result by magmas emplaced in the intermediate crust reproduce that extensional tectonics and heat advected was paths outlined by Schenk (1989) and Grässner & (2001). satisfactorily the P-T 4.2 - Upper to intermediate crust A peculiar characte- of Fig. 7b. diagram the upper to intermediate crust, three paths are shown in P-T For lacking in trajectory, of the prograde paths is the preservation ristics of the upper to intermediate crust P-T in the paths of Fig. 7b is characterized trajectory facies metamorphism. Prograde rocks affected by granulite crustal thickening. relevant to very by a moderate feature both for the Sila and Serre massifs, such as Aspromonte (Grässner & Schenk, 1999) is A distinctive reaches in Calabria the metamorphism. This gradient typical of basements affected by low-P high thermal gradient, geological field trips 2013 - 5(1.2) excursion notes 16 b ) crust. °C T, A. Caggianelli - G. Prosser V. Festa Langone R. Spiess

a ) and upper to intermediate (

- Available P-T paths for the Serre and P-T - Available

MPa , P Fig. 7 Numbers in the oval frame indicate time in Ma. frame Numbers in the oval Sila lower ( From the upper to lower continental crust exposed in Calabria °C

T,

a MP , P DOI: 10.3301/GFT.2013.02 geological field trips 2013 - 5(1.2) excursion notes 17 oic continental rifting, A. Caggianelli - G. Prosser V. Festa Langone R. Spiess From the upper to lower continental crust exposed in Calabria ) a further thinning and erosion episode during the evolu- ) a shortening episode, related to the incorporation of the ii ) a shortening episode, related to the incorporation iii ) a first thinning episode during the Mesoz i DOI: 10.3301/GFT.2013.02 leading to the opening of the Tethys Ocean; leading to the opening of Tethys Calabria crust in the Alpine/Apennine belt; basins and the Apennine Chain. tion of the western Mediterranean remarkable value of 60 °C/km (Grässner & Schenk, 1999) and is generally ascribed to the heat advectively tran- ascribed to the heat advectively of 60 °C/km (Grässner & Schenk, 1999) and is generally remarkable value 1986). Lux et al., sported by the ascent and emplacement of magmas into intermediate to upper crust (e.g., regional to contact metamor- from low-P A typical question related to the upper crust context is transition conditions peak P-T phism. According to the Serre path, contact metamorphism is anticipated by Barrovian metamorphic history in the Sila Massif 2010). In contrast, decompression (Angì et al., and by a considerable 1992; Langone et al., by reduced exhumation (Borghi et al., conditions and is characterized is mostly in low-P by a sharp T spike place in the final part of exhumation and is marked 2010). Contact metamorphism takes in the Serre path, but by absent (1) or smoother (2) discontinuities Sila paths (Fig. 7b). regional to contact metamorphism evidence of two distinct processes or alter- from low-P Is the transition A possible answer to lower crustal levels? the result of a single process acting at progressively natively bodies in this question comes from the analysis of effects produced by emplacement granitoid pluton growth can be a process of the granitoids, the intermediate crust. Considering notable size and accompanied by extensional tectonics, we If this process is favoured lasting for some million years. the elements to obtain in a single path both exhumation and heating/cooling. The intensity of have the pluton grows, place and on the way in which takes dependent on the crustal level last effect is however unpu- (Annen, 2011). A numerical model (Caggianelli et al., or by over-accretion i.e. by under-accretion assumes that pluton growth took place by over- blished material, 2012) based on these considerations and con- These results indicate that low-P of 5-10 Myr. accretion during crustal extension in a time interval tact metamorphism can be considered the product of same geological process where extension and magma injection are acting at the same time. 5 - Crust exhumation the Calabria crust underwent cooling and exhu- After the Hercynian metamorphic and magmatic events mation during three main episodes: geological field trips 2013 - 5(1.2) excursion notes 18 ; -1 A. Caggianelli - G. Prosser V. Festa Langone R. Spiess From the upper to lower continental crust exposed in Calabria DOI: 10.3301/GFT.2013.02 5.1 - Late Paleozoic – Mesozoic evolution metapelites exposed in Northwestern Calabria (Catena Costiera The emplacement of gabbros in the high-grade rifting event be considered the first evidence of crustal thinning indicating onset Tethyan area) may sandsto- conglomerates, 2011). The presence of Late Triassic times (Liberi et al., during the Permian-Triassic in the Sila and Serre massifs (Amodio Morelli phyllites Paleozoic nes and siltstones, lying unconformably above Triassic and the early-middle 1988), indicates that during the Late Paleozoic 1976; Critelli & Ferrini, et al., crustal thickness (about 6- affected by erosional processes. The moderate times the Hercynian basement was (0.05 mm yr sedimentation is consistent with slow erosion rates 7 km) eroded before the late Triassic Caggianelli et al., 2000). The relatively thin succession of Jurassic and Cretaceous limestones in the Stilo area thin succession of Jurassic 2000). The relatively Caggianelli et al., and frequent hiatuses, possibly related to uplift phases (Amodio Morelli is consistent with slow subsidence rate in northeastern Sila (Young half grabens thick terrigenous deposits filling Early Jurassic 1976). However, et al., 1988) clearly indicate that in Northern Calabria the former Hercynian crust under- 1986; Boullin et al., et al., injected into normal faults went extensional tectonics. In the same area, presence of neptunian dykes, document that extensional tectonics lasted up to the phyllites, limestones and Paleozoic crosscutting Jurassic followed by sea-floor spreading during the 1990). Rifting was times (Bouillin & Bellomo, Middle-Late Jurassic 2006, and references therein), as testified by the presen- Cretaceous times (Liberi et al., Late Jurassic-Early ce of widespread ophiolites in Northern Calabria and Southern Apennines. 5.2 - Eocene Early Oligocene contractional tectonics oceanic crust took place since Late Cretaceous, pro- After the sea-floor spreading, subduction of Tethyan margin (Knott, 1987; Cello deformation in the former passive ducing an accretionary wedge and contractional 2001). This process led to the formation of Alpine peri-Mediterranean et al., 1999; Faccenna & Mazzoli, belt. belt part of the peri-Mediterranean lines of evidence indicate that the Calabria continental crust was Several 2006; Heymes et al., 2001, 2004; Langone et al., et al., during the Eocene-Late Oligocene times (Rossetti the SE has been estimated in Serre and directed towards thrust transport 2010). An overall 2008), whereas in Northern Calabria (Sila and 2006; Heymes et al., Aspromonte area (Langone et al., the NE. In Serre and Sila massifs this direction is oriented towards the thrust transport Catena Costiera) Bagni Castagna Unit and the low-grade responsible for underthrusting of the medium-grade process was geological field trips 2013 - 5(1.2) excursion notes 19 A. Caggianelli - G. Prosser V. Festa Langone R. Spiess From the upper to lower continental crust exposed in Calabria ) slab retreat leading to the formation of the Western Mediterranean basins (Malinverno & Ryan, basins (Malinverno Mediterranean ii ) slab retreat leading to the formation of Western DOI: 10.3301/GFT.2013.02 Unit at the base of Hercynian crustal section. The main thrust contact, known as Curinga-Girifalco basement units line, has been compared to the Insubric Line of Alps (Schenk, 1981), since it separates units (the Hercynian crustal section) from medium to low grade almost unaffected by an alpine overprint (the Castagna and Bagni units). In Northern Calabria this pile of tec- showing a significant alpine overprint oceanic domain. from subduction of the Tethyan ophiolites derived tonic units rests above ages from sheared gneisses of the Aspromonte and Serre massifs indicate that this defor- radiometric Available ages are 43±1 Ma in the Serre massif mation took place essentially during the middle Eocene. More specifically, method on K-feldspar; method on biotite; Schenk, 1980) and about 45 Ma in the Aspromonte massif (Ar-Ar (Rb-Sr been obtained for the crustal have ages, about the Eocene-Oligocene boundary, 2010). Younger Heymes et al., by Bonardi et 2004). A different interpretation, provided et al., episode in Northern Calabria (Rossetti thickening al. (2008), indicates a Late Oligocene - Early Miocene age for the Alpine stacking in Aspromonte massif. corresponds to a karstic or ero- event of the thickening Looking at the sedimentary record, time interval ero- indicating absence of sedimentation or moderate interval, sional surface comprising the Paleocene-Eocene sion. This surface is usually located between the Cretaceous carbonates and basal Capo D‘Orlando conglo- 1997). et al., (Cavazza merate 5.3 - Oligocene to Miocene evolution The final exhumation stage of the Hercynian crust is connected with extension and erosion after Eocene - Extensional tectonics during the Oligocene - Early Miocene is documented Early Oligocene crustal thickening. and faults in the Serre Aspromonte massifs Palmi by the presence of low angle shear zones et al., 2008; Grande 2006; Heymes et al., area (Platt & Compagnoni, 1992; Thomson, 1998; Langone et al., area indicates in the Palmi pseudotachylites dating of fault-related 2010). Direct Ar-Ar 2009; Heymes et al., since the Early Oligocene (33.55 ± 0.21 Ma; in the Calabria terrane active that extensional tectonics was 2009). In the Serre area, an E-trending normal fault offsets pre-existing Curinga-Girifalco et al., Grande 2006). Zircon and apatite fis- (Langone et al., thrust, uplifting the Castagna and Bagni units at footwall uplift took place during the early Miocene (18 to 15 Ma). ages indicate that footwall sion-track oceanic crust has been referred to: subduction of the Tethyan Extension in the upper plate of NW-dipping 1993; Thomson, et al., instability of the Calabria accretionary wedge (Knott, 1987; Wallis ( i ) gravitational 1994); ( geological field trips 2013 - 5(1.2) excursion notes 20 A. Caggianelli - G. Prosser V. Festa Langone R. Spiess From the upper to lower continental crust exposed in Calabria DOI: 10.3301/GFT.2013.02 1986; Gueguen et al., 1998; Faccenna et al., 2001). This latter process is responsible for the migration of the 2001). This latter process is responsible for the migration et al., 1998; Faccenna 1986; Gueguen et al., the SE, first during counterclockwise rotation of Corsica-Calabria block and towards Calabria terrane sea. then during the formation of Tyrrhenian associated with fast erosion during the Oligocene-Miocene time (about extension was In the Calabria terrane by Thomson (1994). Exhumation and erosion took ages provided 35 to 15 Ma) as indicated by the fission-track the SE of Calabria basement, producing a higher exhumation rate tilting towards place during an overall by sedimentation of in the NW sector (Thomson, 1994). Intense erosion of Hercynian crust is marked followed by thick terrigenous deposits of Late Oligocene - Early Miocene age (Stilo- abundant conglomerates, 2005). 1989; Bonardi et al., Capo D’Orlando formation, Cavazza, and the between the Calabria terrane by the interaction during the middle-late Miocene is driven The evolution western margin of the Adriatic plate. geological field trips 2013 - 5(1.2) itinerary 21 - Geological sketch map and - Geological sketch cross-section of the Stilo area. A. Caggianelli - G. Prosser V. Festa Langone R. Spiess Fig. 8 From the upper to lower continental crust exposed in Calabria aleozoic metasedimentary succession aleozoic DOI: 10.3301/GFT.2013.02 DAY 1 Stilo area In the Stilo area a P intruded by the shallower granitoids of the Serre batholith intruded by the shallower granitoids are mainly repre- crops out (Fig. 8). Granitoids extensively by a nearly isotropic characterized sented by granodiorites, 1994). et al., 1976; Fornelli magmatic fabric (Borsi et al., levels Magmas intruded rocks of middle- to upper-crustal 2000) belonging to the Stilo-Pazzano (Caggianelli et al., to the Mammola paragneiss Unit and southwards phyllite 1973). Hercynian tectonics was Unit (Colonna et al., responsible for juxtaposition of these two units, subsequen- magmas. tly affected by the emplacement of granodiorite on low-grade Contact metamorphism sharply developed Unit phyllite metamorphic rocks of the Stilo-Pazzano 1973). (Colonna et al., belong to a former sedimentary succession of Phyllites - Carboniferous age including pelite, siltstone and Ordovician shifting with time arenite with intercalations of mafic lavas 1994). from tholeiitic to alkaline series (Acquafredda et al., sedimentary succes- A detailed description of the Paleozoic by Bouillin et al. (1987; Fig. 9) and sion is provided is Acquafredda et al. (1994). A relic sedimentary layering that were affected by two still recognizable in the phyllites, main dynamic phases during Carboniferous regional meta- contact metamorphism promoted blastesis morphism. Later, hornfelses of biotite, andalusite and cordierite, generating and spotted schists. The metamorphic aureole trends rou- geological field trips 2013 - 5(1.2) itinerary 22 g an i c l s l eve r nts i enne ” o d o yd i n Gr io ttes ” o “L “ type) n ” ned meta - aren i te i can i c l ast cs l m ol nes ( v type) wi th C o - iol ar i tes ( ” oi ds aren i tes affected by ne -g ra nes i n - li te rph i sm Ampe wi th Cr l acklli tes phy r i ch -li mest o i te ( “ lli te c l asts ( “ Cu g reen i sh meta ne l us b d io r ar meta -li mest o l o o lli tes and f i us dark meta - rad zi te i sts and meta o du ntact metam o o -li mest o b l acklli tes phy and meta - wi th phy n s ili ce mater i a sch c o g ran type) phy aren i tes type) and s ili ce q uart g rey i sh meta

metabas i te meta A. Caggianelli - G. Prosser V. Festa Langone R. Spiess

m) 00 (1

m) 0 (25 AN I ON V DE AN I UR IL S m) 00 (2 AN I C VI ORDO - CAMBRO

EROUS IF CARBON

ON I SUCCESS I ONG IV B From the upper to lower continental crust exposed in Calabria ); Across the Serre area (modified from Bouillin et al., 1987). area (modified from Bouillin et al., ( N 38° 28’ 5”; E 16° 24’ 37” - Stratigraphy of the Paleozoic succession in the Stilo of the Paleozoic - Stratigraphy Fig. 9 DOI: 10.3301/GFT.2013.02 ghly parallel to the intrusive contact, with a slightly varia- to the intrusive ghly parallel of ~ 1800 m ble thickness that reaches a maximum value estimated on geological sections (Fig. 8). Adjacent to the rocks are injected by grani- wall contact with granodiorite, filled with as well by veinlets toid and pegmatite dykes, 1973). quartz (Colonna et al., hydrothermal contact can be represented by a surface The intrusive the contact sur- an complex shape. Consequently, having at or southeastward, face dips either northeastward (Fig. 8). respectively South and North of the Stilaro River, Stop 1.1: contact metamorphic aureole along the southern flank of Monte Campanaro (Fig. 8). 110 of of this Stop starts from the old S.S. The intinerary of km 62. It in proximity “Monte Cucco e Monte Pecoraro” stretches across the metamorphic aureole, from gra- nodiorite to the phyllites. shows a clear The hornblende-bearing biotite granodiorite weak preferred magmatic texture with an absent or very orientation of feldspars and biotite (Fig. 10a). It contains of the and also xenoliths some magmatic mafic enclaves contact with the the intrusive rocks. In this zone wall and dips NE-SW Unit strikes phyllite Stilo-Pazzano the batholith (Fig. 8). towards geological field trips 2013 - 5(1.2) itinerary 23 2 and rela- 1 crenulation and the S 2 ); Paleozoic low grade rocks low grade ); Paleozoic A. Caggianelli - G. Prosser V. Festa Langone R. Spiess From the upper to lower continental crust exposed in Calabria ( N 38° 29’ 13”; E 16° 27’ 37” Decimetre- to meter-thick granodioritic and pegmatitic dykes are and pegmatitic dykes granodioritic Decimetre- to meter-thick diffusely present within the host rock close to margin of batholith, making up a typical injection zone. Spotted schist is the most common rock in contact aureole (Fig. progres- 10b). Spots are mostly made up of cordierite and their size hornfels can be from the pluton. True away decreases moving sively close to granodiorite. only very observed produced a mineral metamorphism of 570-590 °C at 210 MPa Peak biotite, cordierite and assemblage including quartz, muscovite, in the inner part be present exclusively andalusite. The latter may of the aureole whereas cordierite is widely distributed up to an clearly Spots and porphyroblasts external and narrow biotite zone. on the main foliation labelled S grew post-kinematically to hinge lines and axial These fabric elements are parallel cleavage. suggesting that they surfaces of the large-scale folds, respectively, shor- A lateral were produced during the same deformation event. tening of about 50% has been estimated for the deformed aureole. Stop 1.2: ted to an early stage of Hercynian deformation. perturbation related to magma emplacement produced a Tectonic deformation in the aureole, here manifested by a synform with an contact (Fig. 8). to the intrusive parallel axis trending approximately The synform asymmetry and the attitude of fold axial plane are of the country rocks consequent to coherent with the viscous drag component of displacement during pluton growth. an upward related to pluton shortening, generally The component of lateral emplacement, is in turn outlined by the L of the upper crust at Ponte Vina, in the neighbourhood of Bivongi of the upper crust at Ponte village (Fig. 8). ) Close up photo- b ) Close up photograph of ) Close up photograph - ( a Fig. 10 b a outer darker rim having a lobate outline. rim having outer darker the Serre granodiorite outcropping in the the Serre granodiorite Stilo area. Absence of an evident foliation shape of and the common euhedral biotite are evident. ( cordierite spots. A of the zoned graph grey elliptical core is surrounded by an DOI: 10.3301/GFT.2013.02 geological field trips 2013 - 5(1.2) itinerary 24 b ) 0 0. 5cm to axial 1 - Relationships between S - Relationships foliations in a metapelite thin 1 Fig. 11 b planes of isoclinal folds is evident. section ( a ) and in metacarbonatic of S rocks. The parallelism and S A. Caggianelli - G. Prosser V. Festa Langone R. Spiess 2 From the upper to lower continental crust exposed in Calabria is still recognizable 1 cleavage, mainly defined cleavage, 1 foliation, are characterized by foliation, are characterized 1 ) is still recognizable where former 0 , subparallel to axial surfaces of isoclinal folds. , subparallel 1 deformation event, under very low grade metamorphic low grade under very deformation event, 1 foliation. Differentiation between cleavage domains and foliation. Differentiation between cleavage 2 DOI: 10.3301/GFT.2013.02 A relic sedimentary layering (S A relic sedimentary layering conditions. The cleavage domains, located in the flanks of asym- conditions. The cleavage metric microfolds of the earlier S microlithons, although not fully developed, is related to formation microlithons, although not fully developed, mechanisms. of crenulation and solution transfer Pietragrande and Squillace area are essen- outcropping between Squillace and Soverato Granitoids tially tonalites with minor gabbros, quartz diorites, leucotonalites by the pre- characterized Tonalites, granites. and peraluminous sence of amphibole (hornblende ± cummingtonite), are common in the northern area (Fig. 12), whereas biotite tonalites, someti- are typical of the southern zone. of muscovite, mes with traces by sericite and secondly chlorite. This S This Stop is located, along the road to byzantine church of San A por- Theresti soon after the bridge on Stilaro river. Giovanni and slates succession made up of phyllites tion of the Paleozoic with intercalations of metacarbonate rocks can be observed. sericite + assemblage of fine-grained contain a mineral Phyllites on the quartz + albite chlorite. The evident foliation observed outcrops is the S domains. Blastesis of sericite and chlorite occurred cleavage during D within albite + quartz enriched microlithons bounded by spaced S an enrichment of sericite, with flakes preferentially oriented along an enrichment of sericite, with flakes the S compositional layering was present (Figs. 11a, b). At the thin sec- present (Figs. 11a, b). At was compositional layering a continuous S tion scale it is observed geological field trips 2013 - 5(1.2) itinerary 25 A. Caggianelli - G. Prosser V. Festa Langone R. Spiess Among accessory minerals, epidote is parti- Among accessory minerals, cularly abundant and is mostly of magmatic with allanite-rich origin, sometimes zoned emplaced at a considerable core. Tonalites depth with P conditions of 650 ± 60 MPa by 2000), constrained (Caggianelli et al., the Al-in-hornblende barometre and by presence and composition of magmatic epi- by a are characterized dote. Tonalites in melt-present strong fabric, developed and solid state conditions at decreasing temperatures. Emplacement of tonalites has been defined by zircon U-Pb method at 293 ± 2 Ma. Rb-Sr biotite – whole rock ages span from 141 to 160 Ma and are interpreted as cooling ages, implying that tonalites resided at temperatu- re higher than 250 – 300 °C (biotite closure for a long time. Magma range) temperature acidic differentiation followed a trend towards melts through compaction of a plagio- low-K clase, biotite and hornblende crystal mush. It proposed that emplacement of tonalites was took place in an extensional tectonic setting 2007) that in lower crustal (Caggianelli et al., rocks is recorded by a decompression episode between 300 ± 10 and 290 Ma (Schenk, analysis is compatible with 1989). Structural this interpretation, and kinematic indicators suggest a top-to-East shear sense. From the upper to lower continental crust exposed in Calabria Ionian Sea - Geological map of the Squillace – Pietragrande area - Geological map of the Squillace – Pietragrande Quaternary sedimentary units Pliocene sedimentary units Messinian sedimentary units Late Hercynian foliated biotite- amphibole tonalite Litho-stratigraphic contact Attitude of stratal surface Attitude of magmatic foliation Attitude of magmatic lineation Post-Messinian normal fault Traces of borders offault pre-Messinian zone Fig. 12 modified after Caggianelli et al. (2005) and Gerik (2010). DOI: 10.3301/GFT.2013.02 geological field trips 2013 - 5(1.2) itinerary 26 a c m 5 A. Caggianelli - G. Prosser V. Festa Langone R. Spiess c From the upper to lower continental crust exposed in Calabria c ) - ( a ) The ) Oblate mafic b Fig. 13 inner margin. b tonalite of Pietragrande. ( injec- Pseudotachylite in tonalite tion veins outcropping along the old national road between Pietragrande and Copanello. The road is in some stretches closed to car access, due to rock falls. A safety helmet must be used when approaching the road enclaves are parallel to are parallel enclaves the magmatic fabric outlined by tabular plagioclase crystals. ( ); Foliated N 38° 44’ 28”; ( DOI: 10.3301/GFT.2013.02 tonalites at Pietragrande (Fig. 13). Stop is located on Pietra- cliffs, that can be grande easily reached from S.S. 106 between Montepaone Lido and Copanello. Stop In the Pietragrande the main characteristics of biotite tonalites with amphibole can be rare (Fig. 13a). A observed well defined fabric, expressed in a foliation (dip direction and plunge ~ 090°/36°) and a linea- tion (trend and plunge ~ 110°/31°), originated in the magmatic state, as indicated by the preferred orientation of euhedral plagioclase crystals (Fig. 13b). A schlieren layering, defined by biotite-rich streaks is sometimes visi- ble; it is related to magma and compaction. flowage Solid-state deformation Stop 1.3: E 16° 33’ 31” geological field trips 2013 - 5(1.2) itinerary 27 A. Caggianelli - G. Prosser V. Festa Langone R. Spiess ); Foliated cummingtonite-bearing tona- ); Foliated developed at progressively lower temperatu- at progressively developed res down to greenschist facies conditions. quantified by the Fry anisotropy was Fabric method analysing plagioclase distribution on an X/Z ratio oriented rock slabs and provided of 1.31 (Di ellipsoid axes of the strain Battista, 1997). of tonalite to quartz diorite Mafic enclaves common (Fig. 13b) and composition are very and oblate ellipsoid shape. size variable display a short distance from the Pietragrande At tectonics can be cliffs, the effects of Tertiary From the upper to lower continental crust exposed in Calabria ( N 38° 46’ 52”; E 16° 31’ 6” lites at the Squillace Castle (Fig. 12). located beneath the Squillace Castle (Fig. 14a), tonalites are cha- In this Stop, prismatic amphiboles (Fig. content in coarse grained by a relevant racterized that amphiboles are 14b). A careful examination with the aid of a lens reveals with a lighter cummingtonite core. The surrounding amphibole is zoned zoned clearly observed in the form of pseudotachylite veins (Fig. 13c) and neptunian veins in the form of pseudotachylite clearly observed are mostly made up of plagioclase microlites, biotites, Pseudotachylites dykes. stages of devitrification. Plagioclase quartz and glass at more or less advanced in spherulitic texture around ‘resorbed’ microlites are frequently arranged took place during veins quartz. It is supposed that genesis of pseudotachylite of 250-300 Oligocene at a depth of ~ 10 km and an ambient temperature produced a peak tempe- during the frictional sliding event °C. Heat generated plagioclase melting by massive of at least 1470 °C constrained rature are mostly made up of diatomites 2005). Neptunian dykes (Caggianelli et al., respon- carbonates and are related to Messinian tectonic events, and evaporitic sible also for the origin of neighbouring Catanzaro graben. Stop 1.4: b a b ) A some amphiboles displaying a green displaying ) Tonalite rock - ( a ) Tonalite Fig. 14 hornblende. makes up the basement of makes the Squillace castle. ( closer view shows that by a tonalite is characterized strong fabric with a preferred orientation of plagioclase and prismatic amphibole. With the aid of a lens it is possible to that observe are zoned, core of cummingtonite and a dark shell of tschermakitic DOI: 10.3301/GFT.2013.02 geological field trips 2013 - 5(1.2) itinerary 28 - Al. to VI w- i or tes o i ts; 8 d i or tes Al z IV ar i aquart M i c rocks;M-l LG S anta - ocene to Quaternary depos li tes; 3 7-Mi - grade metamorph Capoi cano Vat tona li tes and granod - l otona i gh h 5 i or tes; oppo . -I A. Caggianelli - G. Prosser V. Festa Langone R. Spiess 2 i crocks i ds; HG M- i at co tona li tes; i to gran B r - - Geological sketch map of the Capo Vaticano - Geological sketch - i cai t cgranod porphyr - m ade metamorph promontory, modified after Rottura et al. (1991). modified after Rottura promontory, t w o - Fig. 15 i gmat t ci sses; paragne From the upper to lower continental crust exposed in Calabria i um - gr m sed i ments; G - - med 1 (a); 6 fau l ts S andli tes; tona 4 (Fig. -type porphyroclasts (hornblende or plagioclase) and tiled plagioclases. -type porphyroclasts σ overprint. Best outcrops, as overprint. subsolidus anitoids outcropping in the Capo Vaticano pro- anitoids outcropping in the Capo Vaticano DOI: 10.3301/GFT.2013.02 DAY 2 Capo Vaticano area Gr montory are mainly tonalites and peraluminous megacrystals with K-feldspar granodiorites from Mg-Hornblende to Tschermakite, a compositional variation governed by the exchange: Si Mg = by the exchange: governed a compositional variation from Mg-Hornblende to Tschermakite, 15). A detailed petrological and geochemical study et al. (1991). From their done by Rottura was be concluded that both tonalites and results it may from crystallized granodiorites peraluminous man- magmas. The mixing process involved hybrid magmas and melts with a more or less tle-derived pronounced crustal parentage. be weak and exclusi- may of the granitoids Fabric strong with a of magmatic origin or very vely marked usual in Calabria, are located along the coast. The rocks with the wall relationships of the granitoids contact with the exposed. A transitional are rarely metamorphic basement can medium- high-grade Rock fabric is here very strong and mainly manifest as a lineation trending ~ 100° with small plunge of 10°. fabric is here very Rock analysed in a neighbouring outcrop with the Fry method applied to plagioclase distribution anisotropy was Rock of 1.98 (Di Battista, 1997). of the X/Z ratio a value and provided showed mono- of Squillace. Stereogram determined on a sample from the zone distribution was Quartz c-axis reached considering other clinic symmetry coherent with top-to-East shear sense. The same conclusion was kinematic indicators, such as geological field trips 2013 - 5(1.2) itinerary 29 A. Caggianelli - G. Prosser V. Festa Langone R. Spiess Metamorphic xenoliths derive from the nei- derive Metamorphic xenoliths ghbouring metamorphic basement, and are chiefly metapelites and amphibolites. Concerning the origin of coarse garnets, a and performed by Clarke detailed study was (1994), and only a short account of the Rottura here. Garnets in quartz main results is given by a different compo- diorites are characterized rocks sition with respect to garnet in wall These gar- (mainly migmatitic paragneisses). from the metapelitic xenoliths nets developed (Bt + Crd Sil) as a consequence of the heat released by the crystallizing quartzdioritic can be found as magma. They characteristically From the upper to lower continental crust exposed in Calabria presence of abundant garnet crystals. Foliation is weak presence of abundant garnet crystals. Foliation by the preferred orientation of plagioclase, and is revealed The dip direction of and sometimes by a schlieren layering. the foliation planes is ~ 350°, with a plunge of 30°. The of emplacement the quartz diorites, estimated by level amounts to a depth of 19 km. Along Al-in-Hbl barometry, the Santa Maria beach blocks deriving from migmatitic can be seen (Fig. 16a). They are mostly gra- border zone, and nitoids containing abundant metamorphic xenoliths outstanding coarse garnets (Fig. 16b). ); Migmatitic border zone at Santa Maria beach (Fig. 15). ); Migmatitic border zone b ( N 38° 36’ 45”; E 15° 50’ 33” - ( a ) Fig. 16 migmatite block. Blocks of the migmatitic border along the zone Santa Maria beach. ( b ) Garnet trails around metamorphic in a xenoliths DOI: 10.3301/GFT.2013.02 a be observed in the Capo Vaticano zone. In a typical migmatitic border zone, tonalites and quartz diorites inclu- In a typical migmatitic border zone, zone. in the Capo Vaticano be observed and coarse garnet crystals (see Stop 2.1). de metamorphic xenoliths Stop 2.1: This Stop is located a short distance from the head of the Capo Vaticano promontory. Here, quartz diorites and promontory. This Stop is located a short distance from the head of Capo Vaticano and by the size, by a coarse grain crop out. They are characterized tonalites from the migmatitic border zone geological field trips 2013 - 5(1.2) itinerary 30 - Phase relations Fig. 17 Rottura (1994) paper. Rottura in the pseudoternary Kfs-Opx- Als system. Liquid path (in red), in case of equilibrium melting of a source rock made up Bt, Crd and Sil (blue circle), starts from R1 invariant reaction point. Garnet place when formation takes reaction point R2 (Bt invariant + Crd = Grt L) is reached. When all biotite is consumed (ca. 20% partial melting) R2 and eventually liquid leaves proceeds along Grt = Crd + L and Redrawn reaction curve. & modified from the Vielzeuf (1988) diagram Holloway & proposed in the Clarke i l l s S - A gne i ss p l a a - C rd A. Caggianelli - G. Prosser V. Festa Langone R. Spiess r S P t B p a M 99 4) C rd ( 1 00 a 5 = Grt +L Rottur

+L P

pl &

S l s A +L rke

C l a

From the upper to lower continental crust exposed in Calabria +L Op x

C rd Grt fter

a t x+L Op R 1 B i ed i f R 2 +L t mod B +L fs K fs K DOI: 10.3301/GFT.2013.02 laces surrounding the metapelite The main garnet-forming xenoliths. Bt + Crd Qtz -> Grt reaction was + Kfs melt (*). In the initial sta- ges, the proportion of melt was and garnet could not develop low, shapes. In a more advan- euhedral ced melting stage, garnet growth in the anatectic melt, advanced of euhedral with free development shapes. This interpretation is based Opx-Kfs-Als on the phase diagram (1988). In & Holloway by Vielzeuf of Figure 17 it is outlined evolution melt composition starting from a made source xenolith hypothetical up of Bt, Crd and Sil. with the quartzdioritic magma, composition of system became unfa- When the anatectic melt mixed the garnet started to be consumed, as indicated by presence of for garnet growth. Eventually, vourable of the reaction (*). at the expense of garnet by inversion biotite or amphibole rims. Biotite developed Instead, formation of tschermakitic hornblende is related to the mixing anatectic melt with a larger pro- along the cliff will show a pitted quartz diorite surface. The portion of the Ca-rich quartzdioritic magma. A walk erosion. by wave holes represent former garnets removed Palmi area basement and tonalites is exposed (Fig. 18). Strongly folia- area the contact between high-grade In the Palmi 1985). They contain ted amphibole-bearing tonalites crop out in the southernmost part of area (Rottura, and coarse garnet in the and include metamorphic xenoliths abundant and flattened magmatic mafic enclaves geological field trips 2013 - 5(1.2) itinerary 31 A. Caggianelli - G. Prosser V. Festa Langone R. Spiess From the upper to lower continental crust exposed in Calabria vicinity of the wall rocks. Tonalites emplaced at conside- rocks. Tonalites vicinity of the wall depths, as indicated by P conditions of 610 ± 60 rable obtained by Al-in-Hornblende barometry MPa 1997). Widespread presence of dyna- (Caggianelli et al., quartz indicates that the intense mically recrystallized mostly at the solid state. Several foliation developed related to post- shear zones, pseudotachylite-bearing Hercynian deformations at the brittle-ductile transition, occur within tonalites. The best outcrop can be observed in the Marinella locality. The metamorphic basement consists mostly of migmati- augen gneisses and marbles is tic paragneisses, 1968; Baldanza & intruded by minor diorites (Faraone, of the dominant 1972). Migmatitic layering Faraone, by late- lithology is often folded and transposed conditions. The Hercynian deformation in high-grade best outcrops are on the cliffs near Taureana. Ca-silicate marbles are particularly frequent at the con- tact between tonalites and migmatitic paragneisses. of Ca-silicate rocks that can be They contain fragments during the interpreted as former skarns, crystallized a crucial role intrusion of the tonalites. Marbles played that allowed in this area, representing a weak horizon Hercynian deforma- localization during the post- strain This produced a 400 m thick shear zone tion events. 2003) according to Prosser et al., shear zone (the Palmi of peg- where marbles, together with stretched layers and augen migmatitic paragneisses matites, granitoids, intense foliation, lineation and struc- gneisses, display tures typical of non-coaxial deformation. ' U ' - Geological sketch map of the Palmi - Geological sketch area, modified after Prosser et al. (2003). Fig. 18 DOI: 10.3301/GFT.2013.02 geological field trips 2013 - 5(1.2) itinerary 32 - (a) Panoramic view of Scoglio - (a) Panoramic the migmatitic paragneiss. A. Caggianelli - G. Prosser V. Festa Langone R. Spiess Fig. 19 b dell’Isola. (b) Stubby prism of sillimanite in a - σ From the upper to lower continental crust exposed in Calabria ); Migmatitic paragneiss of the lower crust at Scoglio dell’Isola (Fig. 18, 19a). ); Migmatitic paragneiss O -> Bt + Sil Qtz 2 ) are flattened and sometimes assume, together 74-86 N 38° 23’ 41”; E 15° 51’ 42” ( DOI: 10.3301/GFT.2013.02 with biotite pressure shadows, a monoclinic symmetry, typical of with biotite pressure shadows, a monoclinic symmetry, type porphyroclasts. Frequently garnet contains inclusions of biotite, type porphyroclasts. quartz, sillimanite and plagioclase. Sillimanite can be found in stub- and by prismatic crystals, reaching a length of 7 cm. Sharp mineral stretching lineations (175°/10°) are clearly visible on the exposed surfaces and are related to high temperature migmatitic layering deformation. that biotite, sillimanite with the microscope reveal Observations in a symplectite texture. and quartz are sometimes involved (2006) pro- analysis, Pascazio On the basis of microstructural posed that the following reactions were crossed during metamor- phic evolution: (1) Bt + Sil Qtz Pl -> Grt Kfs melt (2) Bt + Sil Qtz Pl -> Grt Crd Kfs melt (3) Spl + Qtz -> Grt Sil (4) Grt + Kfs H This Stop is located at Tonnara, a locality that can be reached from Palmi following direction to Lido di Palmi and following direction to Lido di Palmi a locality that can be reached from Palmi This Stop is located at Tonnara, coast immediately to the north of Palmi. then to the Tyrrhenian augen gneiss and Ca-silicate marble. Metamorphic rocks outcropping along the coast are migmatitic paragneiss, is the dominant rock type making up cliffs Migmatitic paragneiss assembla- tower and Scoglio dell’Isola. Peak beneath the Taureana garnet and sillimanite. A migmatitic ge includes biotite, K-feldspar, by the alternance of gar- foliation of a stromatite type, characterized leucosomes with biotite, sillimanite, quartzofeldspathic net-bearing is coarse and size garnet ± cordierite spinel melanosomes. Grain can be outstanding both for garnet and sillimanite. Coarse crystals (Alm Stop 2.2: geological field trips 2013 - 5(1.2) itinerary 33 A. Caggianelli - G. Prosser V. Festa Langone R. Spiess From the upper to lower continental crust exposed in Calabria ); Palmi shear zone (Fig. 18). shear zone ); Palmi ( N 38° 22’ 50”; E 15° 51’ 31” DOI: 10.3301/GFT.2013.02 Reaction (1) to (3) are mainly favoured by a decompression from 800 to 400 MPa at high-T conditions (T > at high-T by a decompression from 800 to 400 MPa (1) to (3) are mainly favoured Reaction 750 °C), whereas reaction (4) is related to isobaric cooling and hydration. Stop 2.3: From the Tonnara locality the Palmi shear zone can be observed at the southern termination of beach, just can be observed shear zone locality the Palmi From the Tonnara belt (Fig. 20a). Sheared Ca-silicate bearing marbles occur in a WNW-trending in front of the Scoglio dell‘Ulivo to the Malopasso and Sidaro localities. The following description is taken that extends from Scoglio dell’Ulivo mostly from Prosser et al. (2003). and contain clasts of Ca-silicates. from fine inclusions of graphite colour derived a dark gray Marbles display assemblage includes diopside, anorthite, grossular ± scapolite, hornblende. Using amphi- The peak mineral bole and plagioclase composition fixing pressure conditions as those estimated for the nearby tonalites a of 783 °C can be obtained with the edenite-richterite thermometer (Holland & Blundy, peak temperature been dismembered and rounded within the car- have minerals 1994). During Alpine shearing high temperature conditions during the Alpine deformation can be estimated using bonate matrix. Pressure and temperature slices coupled with calcite thermometry in the carbona- granitoid assemblage of mylonitic syntectonic mineral allows to estima- granitoids te matrix. The presence of phengitic white mica along foliation planes mylonitic Rb-Sr of about 400 °C, as deduced from calcite thermometry. at temperatures te pressures of about 600 MPa ages of 51 and 56 Ma, provided granitoids from samples of mylonitic age determinations of biotite separated corresponding to the Early Eocene. stretching linea- foliation planes and horizontal by nearly vertical is characterized the shear zone Normally, to steeply-plun- shallow- at Scoglio dell‘Ulivo However, or W-SW. plunges to the E-SE tions, showing moderate lineations. Outstanding kinematic indicators, such ging lineations are closely associated with nearly horizontal within the weak carbonate matrix, as sigma- and delta-clasts (Fig. 20b) formed by rigid Ca-silicate fragments lineations and south-side up along nearly vertical along horizontal show that shear sense is mostly sinistral outcrop can from shallow to steeply dipping lineations in the Scoglio dell’Ulivo variation lineations. The gradual and dip-slip components during a single deformation episode. By this be explained by partitioning of strike-slip by defor- belt accommodating strain transpressive is seen as a sinistral shear zone interpretation the Palmi of the tonalites with movement allowing the relative mation partitioning. Marbles acted as a lubricating layer, respect to the neighbouring migmatitic paragneisses. geological field trips 2013 - 5(1.2) itinerary 34 ): Pseudotachylite veins at veins ): Pseudotachylite A. Caggianelli - G. Prosser V. Festa Langone R. Spiess From the upper to lower continental crust exposed in Calabria ( N 38° 21’ 8”; E 15° 50’ 11” Stop 2.4: Marinella di Palmi (Fig. 18). Marinella di Palmi and Marinella di Palmi In the cliffs comprised between Scoglio dell’Ulivo crosscut the foliated tona- fault zones pseudotachylite-bearing several lites. The best outcrops are visible in the tonalites that border 2009). et al., Marinella beach (Grande betwe- show SE-dipping foliation planes, with inclinations ranging Tonalites in the northern part of observed en 10° to 40°. Steeper dips are generally are obser- Pseudotachylites shear zone. close to the Palmi the tonalite body, and to ENE-WSW oriented from NE-SW fault zones, in nearly parallel ved are located within the tona- spaced about 1 km apart. Most of the fault zones also in faults are observed some pseudotachylite-bearing lites; however, Generally, shear zone. within the Palmi sheared migmatitic paragneisses to the foliation of tonalites. However, attitude of faults is nearly parallel faults crosscut the pseudotachylite-bearing shear zone within the Palmi and tonalites. This indi- foliation of migmatitic paragneisses steep mylonitic postdated ductile pseudotachylites generating cates that seismic events shear zone. deformation along the Palmi lineations. Most of the fault planes show NE-trending nearly horizontal by ductile deformation with gene- are frequently overprinted veins Fault Kinematic indicators, such as S-C and S-C’ com- of ultramylonites. ration shea- folds, are all consistent with SW-directed posite foliations and drag to the NE-SW, from nearly E-W faults strike ring. In the Marinella locality, the S and SW. to steep dips (up 60°) towards with moderate unfoliated; pull- are generally fault and injection veins Pseudotachylite apart structures and synthetic microfaults are consistent with S- to SW- oblique-slip movements. directed shearing, indicating dextral-normal consist of a microcrystalline matrix containing varia- Pseudotachylites ble amounts of clasts made up quartz, plagioclase, lithic fragments biotite and amphibole. The matrix is com- with subordinate K-feldspar, - a) Panoramic view Fig. 20 shear sense. of Scoglio dell’Ulivo. foliation related to subvertical The can be observed. the shear zone in the (b) Delta porphyroclast Ca-silicate-bearing mylonitized marbles suggesting sinistral a b DOI: 10.3301/GFT.2013.02 geological field trips 2013 - 5(1.2) itinerary 35 A. Caggianelli - G. Prosser V. Festa Langone R. Spiess From the upper to lower continental crust exposed in Calabria ); Granulites of the Turrino quarry (Fig. 21). of the Turrino ); Granulites cursion notes, the most complete cross-section of lower continental crust ( N 38° 49’ 25” E 16° 17’ 50” DOI: 10.3301/GFT.2013.02 posed of microlitic biotite and plagioclase, forming frequently spherulitic textures around quartz plagiocla- is indicated by the presence of flattened micro- a ductile overprint se rounded clasts. In some pseudotachylites indicate that age determinations on pseudotachylites rock. Ar-Ar lites and clasts near the contact with wall 2009). This result is consistent et al., faulting took place during the Middle Oligocene (33.55±0.21 Ma; Grande ages, indicating the onset of cooling and exhumation in Calabria basement at with zircon fission track area mark the onset of extensional in the Palmi about 35 Ma (Thomson, 1994). Therefore, pseudotachylites area. Mediterranean of exhumation and erosion, in the Central tectonics, connected with increasing rates DAY 3 Curinga area As already introduced in the ex is exposed in the Serre. The composition of the main lithologies is reported in Table 2. is exposed in the Serre. The composition of main lithologies reported Table The lower crust crops out in the NW sector of Serre Massif and has an estimated thickness 7-8 km (Schenk, 1984; Kruhl & Huntemann, 1991). The base of the lower crust is represented by metagabbroic rocks, unit (~ 2-3 km thick). The chemical com- belonging, according to Schenk (1980), the granulite-pyriclasite 1991). affinity (Caggianelli et al., position of the metagabbroic rocks indicates a calc-alkaline Stop 3.1: The best outcrops of the lowermost crustal levels are located near Curinga (Fig. 21), where metagabbroic rocks The best outcrops of the lowermost crustal levels plun- by an evident compositional layering (Fig. 22). All rocks are here characterized lie below felsic granulites dip of the whole Serre crustal section. This fea- the general SE of about 40°, that is approximately ging towards that is cut in a metagabbroic body (Fig. 23a), along the also on the front of a big quarry, ture can be observed left bank of the Strofolio stream (Fig. 21). In quarry rocks are crushed to produce materials for ballast. The whole succession exposed in the quarry has a thickness of ~170 m (Fig. 22). The main rock type is a laye- of metapy- metagabbro ± amphibole garnet. Other lithologies are represented by layers red two-pyroxene and lenses of spinel peridotite. In metagabbros, the original magmatic laye- and meta-anorthosite, roxenite spans from cen- The thickness of single layers ring (Fig. 23b) due to crystal settling is locally well preserved. geological field trips 2013 - 5(1.2) itinerary 36 ) is locally preserved n (Fig. 23e). n+1 A. Caggianelli - G. Prosser V. Festa Langone R. Spiess Although the foliation of the felsic granulites is Although the foliation of felsic granulites contains an evident it rarely well developed, lineation. When visible, it is defined by the ali- gnment of stretched quartz crystals, showing a within the thickened hinge zones of intrafolial, hinge zones within the thickened as the isoclinal folds, we identify the layering main foliation S timeter to meter scale. The presence of large garnets in gabbroic rocks with a lower color index (Fig. 23c) is confined to the upper part of (Fig. the succession, where felsic granulites 23d), made up of quartz, feldspars, and garnet are more abundant. These ± orthopyroxene, features are compatible with a contamination of the former gabbroic magma by host metase- dimentary rocks. Minor intercalations of felsic can be also found within the meta- granulites gabbros (Fig. 22) and their repeated occurren- be sometimes related to isoclinal fol- ce may ding (Fig. 23e). Since an older foliation (S From the upper to lower continental crust exposed in Calabria 9.34 1.25 0.68 0.68 0.19 7.26 2.89 1.32 13 73 292 534 197 164 1.05 1.30 7.23 2.57 0.13 0.13 3.21 2.18 10.23 2.42 56 75 67 236 716 238 1.68 0.25 1.83 0.04 0.27 4.40 2.22 0.50 6 96 29 308 148 298 1.84 0.52 1.78 0.09 0.30 6.56 4.17 1.42 99.72 99.98 99.81 100.00 14.05 15.06 50.0118.98 43.68 30.05 64.87 14.72 48.61 17.55 70 16 173 287 156 481 - Composition of the main rock types exposed in 1.68 0.08 Serre lower crust (from Caggianelli et al., 1991). Serre lower crust (from Caggianelli et al., 11.24 53.90 18.73 Migmatitic Grt-Crd-rich Grt-Sil-rich Felsic Metagabbroic paragneisses rocks rocks granulites rocks 3 Tab. 2 t 5 O 1.48 2 2 O 2 O 3.10 O 2 2 2 DOI: 10.3301/GFT.2013.02 Sr 224 P wt.% SiO Al L.O.I.tot 1.62 ppm Cr 99.73 Ni 114 82 Rb 80 Zr 228 Ba 731 MnOMgOCaO 0.18 Na 5.70 2.02 K TiO FeO dip azimuth towards SSW and a plunge of about 10°. SSW dip azimuth towards quartz of deformation under which the main foliation developed, In order to obtain indications on the temperature of Kruhl (1996) suggest that deforma- based on the diagram been carried out. Results measurements have c-axis facies conditions. tion took place under granulite U-Pb zircon ages, According to conventional The emplacement age of the magmatic protholith is controversial. recent zircon spot analy- emplacement of the gabbros took place at about 550 Ma (Schenk, 1980). However, and 2008; Langone, 2011) with some Ordovician a wide age spectrum (e.g. Micheletti et al., ses reveal the problem still open. This aspect is of critical importance for Carboniferous concordant ages that make of the crustal section and for comparison with interpretation of the metamorphic and geological evolution geological field trips 2013 - 5(1.2) itinerary 37 A. Caggianelli - G. Prosser V. Festa Langone R. Spiess From the upper to lower continental crust exposed in Calabria - Geological sketch map of the Curinga area. - Geological sketch Fig. 21 DOI: 10.3301/GFT.2013.02 the Ivrea crustal section, where lower gabbros underplated during late Hercynian stage (Voshage 1990). et al., at 300 Ma, accor- metamorphism during the Late Hercynian phase reached a T of 790 °C and P 750 MPa Peak Pl, Opx and Amph (Fig. 23c) can be found between ding to Schenk (1989). Outstanding symplectites involving They are related to the reaction Grt + Cpx -> Pl Opx ± Amph (Schenk, 1984; garnet and clinopyroxene. between of about 200 MPa, 2008), that took place during a significant decompression event Acquafredda et al., crossed during the cooling episode (Fig. 6). reversely 300 and 290 Ma (Schenk, 1989). This reaction was geological field trips 2013 - 5(1.2) itinerary 38 - o l o i t e i ng l i t e t i e e r u at l s i c a quarry. n e i d o a Fig. 22 f g abb r r s p i n g m g abb r - b e g r t p e p e e n me ta r Stratigraphy of the Stratigraphy me ta lower crust succession exposed in the Turrino g a A. Caggianelli - G. Prosser V. Festa Langone R. Spiess From the upper to lower continental crust exposed in Calabria ); Mylonitic orthogneisses of the Castagna Unit N 38° 49’ 19”; E 16° 25’ 13” ( DOI: 10.3301/GFT.2013.02 Girifalco area rocks by cataclastic and mylonitic The Curinga-Girifalco Line (CGL) is characterized mainly consists of in a 400 m thick belt (Fig. 24). The deformation zone arranged of the lower crust (Polia- migmatitic paragneisses overprint that generally mylonites orthogneisses of an 1976) and granitoid Copanello Unit of Amodio Morelli et al., grey cataclasites a few Alpine nappe (Castagna Unit). Thin bands of incohesive metres thick, produced at low T conditions, are visible near the contact between units. Schenk (1981) compared the CGL to a segment of Insubric Line that in to the South, unaffec- the crustal section of Ivrea zone western Alps separates by intense to the North, overprinted from the Sesia zone ted by the Alpine event, method on biotite yielded an Eocene age (43±1 Ma) Alpine metamorphism. Rb–Sr orthogneiss from the Castagna Unit (Schenk, 1980). on a mylonitic and the main contact dips The Curinga-Girifalco Line is roughly oriented WNW–ESE faults showing is offset by younger (197°N; Fig. 24). The shear zone 37° to the SSW of the lower crust are or extensional kinematics. Migmatitic paragneisses strike-slip of the Castagna whereas orthogneisses and paragneisses present in the hangingwall, Outcropping conditions are quite Alpine nappe are mostly located in the footwall. around the Girifalco However, the entire area from Curinga to Girifalco. good over power sta- church and the hydroelectric village two localities, close to the Addolorata tion (Fig. 24), resulted of particular interest. Stop 3.2: (Addolorata church; Fig. 24). (Addolorata Orthogneisses of the Castagna Unit are main lithology affected by shearing in mostly composed of quartz + K-fel- of the CGL. These are metagranitoids footwall + biotite ± garnet, epidote and plagioclase (Fig. 25a). dspar + muscovite Amphibolite lenses, consisting of hornblende + plagioclase quartz epidote phengite ±biotite, chlorite and sphene, are closely associated with the orthogneis- is here not in migmatitic paragneisses, ses. The Hercynian foliation, locally observed geological field trips 2013 - 5(1.2) itinerary 39 ) e ) Typical m d c cm 1 1c b ) Compositional ) Reaction texture in c ) Reaction foliations can be observed. ) Panoramic view of the - ( a ) Panoramic n+1 and S Fig. 23 n A. Caggianelli - G. Prosser V. Festa Langone R. Spiess S Turrino quarry front. ( Turrino in crossed by a pegmatite dyke layering ( the metagabbro. metagabbro close to the garnet-bearing Radial contact with felsic granulite. plagioclase, symplectite seam involving surrounds hornblende and orthopyroxene coarse garnet crystals. ( ( of felsic granulites. appearance both metagabbro Isoclinal fold involving between Relationships and felsic granulite. - a c met g abb ro nulite a gr From the upper to lower continental crust exposed in Calabria felsi c n

S

n+1 S e b a d DOI: 10.3301/GFT.2013.02 geological field trips 2013 - 5(1.2) itinerary 40 A. Caggianelli - G. Prosser V. Festa Langone R. Spiess From the upper to lower continental crust exposed in Calabria - Geological sketch map of the Girifalco area. - Geological sketch Fig. 24 DOI: 10.3301/GFT.2013.02 recognizable and the main fabric is related to the Alpine metamorphic event. In the orthogneisses K-feldspar recognizable and the main fabric is related to Alpine metamorphic event. defining an anastomosing folia- of micas and quartz grains by thin layers wrapped are generally porphyroclasts size foliation, reduction of porphyroclast determined the formation of a mylonitic tion. The ductile Alpine event Mylonitization is accompanied by crystallization of small fla- veins. pseudotachylite of rare and development reactions, such as chloritization of biotite, white mica and epidote along the foliation planes. Retrograde kes The presence of stable biotite on the foliation are locally observed. of biotite and sericitization K-feldspar, geological field trips 2013 - 5(1.2) itinerary 41 ); E 16° 24’ 7”

38° 49’ 10”;

N ( 25b, c). Mylonites of the interme- 25b, diate nappe typically show over- growths on hornblende and garnet with tschermakite and grossular- rich compositions, respectively c and d). The Alpine (Fig. 25b, assemblage indicates that mineral deformation took place in epidote- amphibolite facies at pressures from 750 to 900 MPa. ranging Stop3.3: Mylonitic migmatitic paragneisses of the veins with pseudotachylite power station (Fig. hydroelectric 24). power sta- Near the hydroelectric tion the most beautiful outcrop of migmatites of the Serre mylonitic The lower crust can be observed. tectonic contact with the ortogneis- ses of the Castagna Alpine nappe is 150 river, exposed along the Pesipe meters below the power station. A. Caggianelli - G. Prosser V. Festa Langone R. Spiess d ) Ca-rich From the upper to lower continental crust exposed in Calabria a ) and c ) and ( - Fig. 25 c respectively. Photomicrographs of mylonitic Photomicrographs orthogneiss ( amphibolite ( b ). SEM-BSE images of tschermakitic amphibole ( garnet overgrowths in garnet overgrowths amphibolite and orthogneiss, DOI: 10.3301/GFT.2013.02 planes indicates temperatures higher than 400 °C. The widespread evidence of dynamic recrystallization by planes indicates temperatures of about 400–500 °C. rotation in quartz is consistent with deformation taking place at temperatures subgrain mica, garnet and sillimanite show mainly microfaulting, kinking phases such as feldspar, Other mineral In amphibolite lenses hor- in K-feldspars. deformation is locally observed boudinage. Incipient intracrystalline (Fig. and epidote grains by mica flakes with a sigmoidal shape, wrapped up porphyroclasts nblende makes geological field trips 2013 - 5(1.2) itinerary 42 b A. Caggianelli - G. Prosser V. Festa Langone R. Spiess the migmatitic paragneisses (b). the migmatitic paragneisses - Scan of rocks slices showing the mylonitic Fig. 26 From the upper to lower continental crust exposed in Calabria fabric (a) and the occurrence of pseudotachylite veins within veins fabric (a) and the occurrence of pseudotachylite a CKNOWLEDGEMENTS DOI: 10.3301/GFT.2013.02 The Hercynian mineral paragenesis of migmatitic paragneisses mainly consists of quartz + garnet sillimani- of migmatitic paragneisses paragenesis The Hercynian mineral facies conditions. amphibolite to granulite and plagioclase defining transitional te + biotite ±K-feldspar (300–290 Ma), by Spiegel (2003). During the late-Hercynian evolution Cordierite has been locally recognized of of 680–800 °C and a P range metapelites underwent peak metamorphic conditions in a T range high grade experienced a (Schenk, 1984,1990). During the Alpine orogenesis, migmatitic paragneisses 550–750 MPa conditions (Fig. 26a). The Alpine metamorphic and deformation at lower temperature metamorphic overprint Chloritization of biotite and garnet, formation white mica re-equilibration. caused a partial mineral event Sillimanite breakdown is incom- and sillimanite are locally observed. and quartz at the expense of K-feldspar plete, as documented by well recognisable prismatic crystals that are commonly boudinaged with precipitation in necks and extensional fractures. of white mica, biotite and oxides with thickness veins, Widespread pseudotachylite paral- from few cm to 1 m, are generally ranging foliation and lel or at low angles to the mylonitic fabric (Fig. 26b). an ultramylonitic often display Matrix mainly contains biotite, whereas clasts are represented by sillimanite, quartz and feldspar, both as single crystals and aggregates. The pre- in sence of ductilely deformed pseudotachylites of T conditions typical is indicative the mylonites where pseudota- of the brittle–ductile transition, are intermittent in an ove- events chylite-forming 1985). Incomplete ductile regime (Passchier, rall reactions and abundance of pseudota- retrograde indicate that deformation took place veins chylite 1985). conditions (Passchier, in water-deficient A the manuscript of this guide. Compagnoni for the careful revision that helped to improve to Roberto are grateful We wish to thank for their interest and kindness all the participants field trip held occasion of We 2012 Congress of the Italian Geological Society. From the upper to the lower continental crust exposed in Calabria A. Caggianelli - G. Prosser - V. Festa - A. Langone - R. Spiess g e o l o g i c a l

f i e l d

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43 m e m o r a n d u m

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