INTRODUCTION The Dinarides belong to the Meso-Cenozoic Alpine- Himalaya collisional belt, derived from the Mesozoic to Tertiary convergence between the Adria and the Eurasia Plates. They are connected northwards with the Car- pathians, whereas southwards they are linked by the Shkoder-Peja fault with the Albanides-Hellenides (fig. 1). In the classical reconstructions, the evolution of the Dinarides started with a rifting stage mainly developed during the Early Triassic (DIMITRIJEVIC, 1982; PAMIC et alii, 2002; BORTOLOTTI et alii, 2004), along the northern margin of Gondwanaland. The rifting process, characteri- zed by syn-rift deposits and magmatism, evolved in Midd- le to Late Triassic to oceanic spreading and drifting with development of a wide basin characterized by mid-ocean ridge (MOR) oceanic lithosphere (COLLAKU et alii, 1992; PAMIC et alii, 2002; BORTOLOTTI et alii, 2004). This ocea- nic basin, carrying (KARAMATA et alii, 2000; DIMITRIJEVIC, 2001) or not (PAMIC et alii, 1998; 2002) a microcontinent inside, was located between the Adria and Eurasia conti- nental margins. The convergence began during Early Ju- rassic, with the development of an intraoceanic subduc- tion followed by the formation of new oceanic lithosphere in the suprasubduction basin. As a consequence of con- vergence, obduction process developed, resulting in the emplacement of oceanic lithosphere slices onto the conti- nental margins of the Adria plate during Middle to Late Jurassic times (DIMITRIJEVIC, 2001). The convergence between Adria and Eurasia finally led to the continental collision during Upper Jurassic-Lower Cretaceous time span. After the continental collision and up to Neogene, a continuous convergence, still active today, affected the continental margin of the Adria Plate, that was progressi- vely deformed as a west-vergent fold-and-thrust belt. The continental collision was also characterized by the empla- cement of calc-alkaline granitoids, mainly of late Eocene- early Oligocene age (PAMIC, 1998). This long-lived geodynamic evolution produced the structural pattern of the Dinarides, represented by an as- semblage of northwest-southeast to north-south trending zones, corresponding to the modern concept of terranes (BORTOLOTTI et alii, 2004 and quoted references). Each zone consists of an assemblage of variably deformed and metamorphosed tectonic units of oceanic and/or conti- nental origin. These zones, from west to east, are: 1) the Deformed Adria Zone, 2) the External ophiolite Belt, 3) the Pelagonian-Korab-Drina-Ivanjica Zone and the 4) Vardar Zone. These zones are bounded to the west by the undeformed Adria Zone and to the east by the Serbo- Macedonian-Rhodope Massif, generally considered as the stable margin of the Eurasia Plate (fig. 1). The Deformed Adria Continental margin (i.e. South Adriatic zone, Budva zone, Dalmatian-Herzegovian zone, Sarajevo Sigmoid zone) is represented by a imbricate stack of west-verging tectonic units consisting of conti- nental carbonate succession lying over a Permo-Triassic siliciclastic succession with rift-related volcanic rocks co- vering a Middle Devonian-Middle Permian metamorphic basement affected by Variscan deformations. This succes- sion is topped by foredeep turbidites ranging in age from Late Cretaceous, in the internal zone, to Oligocene, in the external one. The Dinaric Ophiolitic Belt (cfr. Eastern Ophiolite Belt) is represented by large slabs of ophiolitic rocks ran- ging in age from Triassic to Jurassic lying over a mélange formed by both oceanic- and continental-derived rocks. Sometimes the base of the ophiolitic slabs is marked by metamorphic shear zones (amphibolitic metamorphic sole) generated under HT-LP conditions. The ophiolites are regarded as remnants of the eastern branch of Tethyan oceanic basin (AUBOUIN et alii, 1970; DIMITRIJE- VIC, 1982; BORTOLOTTI et alii, 1996) that experienced shortening since Early Jurassic as a result of convergence between Africa and Eurasia plates. The Dinaric Ophiolitic Belt is unconformably covered by Lower to Upper Creta- ceous sediments (JOVANOVIC, 1957; DIMITRIJEVIC & DIMI- TRIJEVIC, 1973; KARAMATA, 1988). The Dinaric Ophiolitic Belt could be correlated to the south with the Mirdita ophiolites in Albania and the Vourinos, Pindos, Othrys and Argolis ophiolites in Greece. The Drina-Ivanjica Zone is represented by a Paleo- zoic basement affected by pre-alpine deformation and metamorphism and is unconformably covered by Upper Permian-Lower Triassic siliciclastic shallow water depo- Rend. Soc. Geol. It., 6 (2008), Nuova Serie, 00-00, 2 figg. The geology of the Internal Dinarides in the Zlatibor-Maljen area (Central-Western Serbia) GIANFRANCO PRINCIPI (*), NICOLA LEVI (**), FRANCESCO MENNA (*), GIUSEPPE NIRTA (*), MICHELE MARRONI (**), LUCA PANDOLFI (**), BRANISLAV TRIVIC (***), MARCO CHIARI (****), EMILIO SACCANI (*****) & FRANCESCA GARFAGNOLI (*) (*) Dipartimento di Scienze della Terra, Università di Firenze, Via La Pira, 4 - 50121 Firenze, Italia. (**) Dipartimento di Scienze della Terra, Università di Pisa, Via S. Maria, 53 - 56126 Pisa, Italia. (***) Faculty of Mining and Geology, University of Belgrade, Djusina, 7 - 11000 Belgrade, Serbia. (****) Istituto di Geoscienze e Georisorse, CNR, Via La Pira, 4 - 50121 Firenze, Italia. (*****) Dipartimento di Scienze della Terra, Università di Fer- rara, Via Saragat, 2 - 44100 Ferrara, Italia. Principi Gianfranco: Tel. 055/2757524; gianfranco.principi@geo. unifi.it PRINCIPI