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'Verrucano' and 'Pseudoverrucano' in the Central-Western Mediterranean Alpine Chains: palaeogeographical evolution and geodynamic significance

V. PERRONE 1, A. MARTIN-ALGARRA 2, S. CRITELLI 3, F. A. DECANDIA 4, M. D'ERRICO 5, A. ESTEVEZ 6, A. IANNACE 5, A. LAZZAROTTO 4, M. MARTIN-MARTIN 6, I. MARTIN-ROJAS 6, S. MAZZOLI 5, A. MESSINA 7, G. MONGELLI 8, S. VITALE 5 & M. N. ZAGHLOUL 9 llstituto di Geologia dell'Universitgt 'Carlo Bo' di Urbino, Campus Scientifico Localit& Crocicchia, 61029 Urbino, Italy (e-mail: [email protected].) 2Departamento de Estratigraf{a y Palaeontolog{a de la Universidad de Granada, Campus de Fuentenueva, 18071 Granada, Spain 3Dipartimento di Scienze della Terra dell'Universitgt della Calabria, Via P. Bucci, 87030 Arcavacata di Rende, Italy 4Dipartimento di Scienze della Terra dell'Universitgt di Siena, Via Laterina 8, 53100 Siena, Italy 5Dipartimento di Scienze della Terra dell'Universitb 'Federico H' di Napoli, Largo San Marcellino 10, 80138 Napoli, Italy 6Departamento de Ciencias de la Tierra y del Medio Ambiente de la Universidad de Alicante, Campus de San Vicente, Apdo. Correos 99, 03080 Alicante, Spain 7Dipartimento di Scienze della Terra dell'Universitgt di Messina, Salita Sperone 31, 98166 Messina, Italy 8Dipartimento di Scienze Geologiche dell'Universit& della Basilicata, 85100 Potenza, Italy 9Ddpartement de Sciences de la Terre et d'Ocdanologie de l'Universitd 'Abdel Maleek Essfiadi' de Tanger, Tangier, Morocco

Abstract: The Anisian-Carnian Verrucano Group of the Tuscan Metamorphic Units and the Triassic-Hettangian Pseudoverrucano Formation of the homonymous unit are mainly continental redbeds occurring in Tuscany at the base of the Alpine orogenic cycle. A study carded out throughout the Apennine, Maghrebian and Betic Chains emphasized the presence in all these oro- genic belts of deposits more or less coeval and similar both to the metamorphic Verrucano and to the unmetamorphosed Pseudoverrucano. Thus, the distinction of Verrucano and Pseudoverrucano successions has a palaeogeographical and geodynamic importance at the scale of the Western Mediterranean. Both successions developed during the continental rift stage of Pangaea, which led to later break-up at the edges of a future microplate, interposed between the Europe, Africa and Adria-Apulia plates, but they are characterized by different tectonometamorphic evolution. Pseudoverrucano-like deposits, devoid of Alpine metamorphism, characterize the highest tectonic units of the nappe stack and they overthrust units bearing Verrucano-like deposits. These latter show an Alpine tectonometamorphic history marked during the Miocene by intense deformation and HP/LT metamorphism (at pressures in the range of 0.8-2 GPa), followed by a retrograde phase associated with decompression, suggesting subduction and subsequent exhumation of con- tinental crust. Intriguing palaeogeographical problems arise from the analysis of Verrucano- bearing units, because the same evolution seems to characterize both units considered to belong to a realm similar to that of the north-verging Austroalpine nappe system and some units referred to the south-verging fold-thrust belt derived from the Adria-Apulia palaeomargin.

From: MORATT[, G. & CHALOUAN,A. (eds) 2006. Tectonics of the Western Mediterranean and North Africa. Geological Society, London, Special Publications, 262, 1-43. 0305-8719/06/$15.00 9 The Geological Society of London 2006. Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

2 V. PERRONE ETAL.

The stratigraphic base of the Alpine Sedimentary representative both of late Hercynian molasses and Cycle in the Alpine Chains of the western and of the base of the Alpine Cycle sometimes occur in central Mediterranean is frequently formed by con- the same region and nappes (for a critical review, tinental redbeds that are known as 'Verrucano', a see Cassinis et al. 1979). term used for the first time by Savi (1832) for meta- In the Alps, Verrucano facies of Permian and Early morphosed continental clastic rocks underlying Triassic age are particularly well developed in the Mesozoic successions in Tuscany, particularly strongly deformed Internal Domains (Penninic, in par- well exposed in the Monte Pisano (Monte della ticular Brian~onnian, and Austroalpine nappes), Verruca) area. Everywhere, these facies are domi- although they are also known in some external nantly made of continental, reddish, purple and units, such as the Helvetic nappes of the Glarus Alps yellow-greenish sandstones, conglomerates and (Rutten 1969). Similarly to the time- and facies- mudrocks, with subordinate shallow marine evapor- equivalent Permian Rotliegende deposits of the ites and carbonates. They rest unconformably on Germanic Alpine foreland (Henningsen & Katzung Palaeozoic sedimentary, metasedimentary and plu- 1998), the continental redbeds known as Permian Ver- tonic rocks deformed during the Variscan Orogenic rucano Alpino (especially in the Southern Alps, where Cycle, and are covered by marine carbonate and they are also named Verrucano Lombardo, or Val clastic Mesozoic and Cenozoic strata, which may Gardena Sandstones: Bosellini et aL 1996), locally be as young as Aquitanian. reach enormous thickness and are associated with In the last century, however, the term Verrucano huge amounts of acidic to intermediate volcanic rocks. was used in all the chains of the Western Mediterra- The undeformed Permian redbeds and vulcanites nean, from the Alps to the Gibraltar Arc, as a of the extra-Alpine Rrt deposits are usually common term to identify lithostratigraphic units covered by thick Upper Permian salt deposits (Zech- resulting from the erosion of the Hercynian Chain stein), which underlie a new sedimentary cycle of and its subsequent volcanoes (Trumpy, cited Triassic continental redbeds, which forms the by Trevisan 1966). Thus, the term was generally lower unit of the Germanic Triassic facies belt, the employed for sedimentary rocks of Permian and Buntsandstein facies (Henningsen & Katzung Triassic age, deposited as continental redbeds in 1998). Southwards, towards the Alps, these deposits different geodynamic contexts (see Rutten 1969; change laterally to progressively more open marine Lemoine 1978; Cassinis et al. 1979, and references carbonates, which constitute the Alpine Triassic therein) and also for sediments representing late facies belt (Lemoine 1978). Hercynian molasses, such as the well-known In the Central-Western Mediterranean Chains, Verrucano of the Glarus Alps (Fisch & Ryf 1966). from the Betic Cordillera to the Northern In contrast, we agree with researchers who used the Apennines and from the Rif to Calabria, redbeds term Vermcano exclusively for prevailingly conti- considered as Verrucano facies are usually Triassic, nental deposits, unconformably overlying the Hercy- but they can exceptionally reach the earliest Juras- nian basement and representing the onset of the sic (Calabrian-Peloritanian Arc), and a Permian Alpine Cycle (see Cassinis et al. 1979). The Verru- age for the base cannot be excluded in the Betic cano clastic deposits are best interpreted as a tectofa- Cordillera and Rif. In addition, these deposits are cies testifying to the onset, in the first phases of Alpine vertically and laterally related to Triassic marine history, of early continental rifting in a wide area of carbonates with Alpine facies and are systemati- western Pangaea (Cassinis et al. 1979). This rifting cally found within tectonic units belonging to the aborted before oceanization (Cassinis et al. 1979; Internal Domains of all these chains. Nevertheless, Kligfield 1979; Passeri 1985; Rau et aL 1985; with the exception of the Apenninic and Sicilian Martini et al. 1986), because Jurassic-Cretaceous External Domains, whose Triassic deposits are rifting, and subsequent break-off and spreading, gen- marine with Alpine facies, redbeds in the Betic- erally did not follow previous structural strikes but Maghrebian External Domains and in their independent neoformed fractures. Iberian and African forelands belong to the The frequent inaccurate use of the term Vermcano Germanic and Germano-Andalusian Triassic facies can be explained taking into account two main reasons. belts. In Spain, very thick continental redbeds are (1) The age of the early intracontinental rifting, widely present both below and above Middle coeval with the deposition of Verrucano redbeds, is Triassic marine Muschelkalk carbonates, and are debated and difficult to define clearly in many areas, included either in Buntsandstein or in Keuper because of the scarcity of fossils. Moreover, a dia- facies (Sopefia et aL 1988; Prrez-Ldpez 1998). chronism is generally evident from place to place. However, in Tuscany, Lotti (1891) introduced (2) Large amounts of Verrucano-like redbeds the term 'Pseudoverrucano' to indicate a clastic were deposited, during the Permian and Triassic, in deposit, lithologically similar to the Tuscan Verru- the Western Pangaea areas. In addition, rocks cano sensu stricto, but not affected by Alpine Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

TRIASSIC REDBEDS IN WESTERN MEDITERRANEAN CHAINS 3 metamorphism. The Pseudoverrucano was con- (2) The unmetamorphosed Pseudoverrucano sidered by Lotti to be younger, probably Cretac- successions, characterizing the Pseudoverrucano eous in age, because it was interpreted to be tectonic unit, consist of Triassic-lowermost Juras- stratigraphically interposed between Liassic and sic reddish conglomerates and sandstones, in Eocene levels of the Tuscan successions. Today, which thin levels of Rhaetian marine sandy lime- these deposits are interpreted as representing the stones occur (Costantini et al. 1980a). The clastic Upper Triassic stratigraphic base of an indepen- deposits are followed by Liassic carbonate platform dent allochthonous tectonic unit named the Pseu- and basin deposits (Costantini et aL 1980a, b; doverrucano Unit. This unit is considered to be Decandia & Lazzarotto 1980). the uppermost tectonic unit that originated from A re-examination of the successions for which the the Tuscan Domain (Decandia et al. 1980). The term Verrucano has been used in the Western Med- term Pseudoverrucano has never been used for iterranean Alpine Chains, from the Betic Cordillera redbeds cropping out in other chains of the to the Apennines, has never been carried out. In our Western Mediterranean. opinion, such re-examination is necessary to better Studies on the North Apenninic Lower Mesozoic define the palaeogeographical evolution and the clastic successions, therefore, permit as to dis- geodynamic significance of rock successions that tinguish two Triassic stratigraphic sequences, were given this name and to verify if their history which have marked differences in their post- is concordant with that of the Verrucano in its type Triassic tectonosedimentary evolution. area of the Tuscan Northern Apennines. (1) the Verrucano Group successions (Ran & In this synthesis therefore, we re-examine the Tongiorgi 1974; Cassinis et al. 1979) are exclusive Alpine tectonosedimentaryevolution of all units con- of the Tuscan Metamorphic Units (Massa, Apuane taining Triassic redbeds and their metamorphic and Monticiano-Roccastrada Units) and are equivalents, from the Northern Apmmines to Anisian- Carnian in age. They consist mainly of the Betic Cordillera (Fig. 1). The aims of this continental clastic deposits, grading upwards to study are to verify whether: (1) Verrucano- and evaporitic-carbonatic deposits during the late Pseudoverrucano-like successions are also dis- Carnian-Norian. These rocks are followed tinguishable in other orogenic sectors of the by younger basinal sediments and experienced a Western Mediterranean chains; (2) these deposits Neogene metamorphism. have a Triassic and post-Triassic tectonosedimentary

Fig. 1. Geological sketch map of the Alpine Chains in the Central-Western Mediterranean region. Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

4 V. PERRONE ET AL.

evolution similar to those of the Tuscan Verrncano by pink limestone with Toarcian Ammonitico and Pseudoverrucano. Rosso facies (Costantini et al. 1980b). In the In our opinion, the available data allow us Collecchio locality, the Montebrandoli limestone is to hypothesize a common history for all the disconformably overlain by mainly calcareous units containing Verrncano-Pseudoverrucano-like heterometric megabreccias (Poggio Morcone brec- redbeds in the Western Mediterranean Alpine belts. cias), fed by the underlying formations, with a It is suggested that these units are representative of marly-calcareous red or pink matrix bearing one palaeogeographical domain, formed in the Posidonomya and rare ammonites of Mid-Jurassic Mid-Triassic or earlier, which underwent a similar age, capped by few beds of red or grey-green post-Triassic evolution up to the onset of conver- Upper Jurassic radiolarites (Costantini et al. 1980b). gence-related tectonics, which led to the accretion of the sedimentary successions to the developing Palaeogeographical evolution. The tectonosedi- chains. During the Cenozoic compressional tectonics, mentary evolution suggests the existence of a conti- however, Verrucano- and Pseudoverrucano-bearing nental area up to earliest Jurassic time, in which successions experienced a different deformation some marine episodes are indicated by rare thin history; this has resulted in the formation of two levels of Rhaetian Triasina limestones. From the different Verrucano and Pseudoverrucano subdo- Early Jurassic, the onset of extensional tectonics, mains. The results of the present research may related to the opening of the Tethyan Ocean, provide important constraints on palaeogeographical resulted in complex palaeoenvironmental con- and palaeotectonic reconstructions of the evolution ditions. Synsedimentary tectonics produced the of the Alpine circum-Mediterranean orogen. development of morpho-structural highs and lows in the basin floor and, consequently, of sudden ver- Pseudoverrucano-type successions tical and lateral changes, from neritic to pelagic environments, as indicated by the deposition of Northern Apennines Pliensbachian-Toarcian platform carbonates, pelagic marly and cherty limestones. Pseudoverrucano deposits (Triassic). The Pseudo- During the Mid-Jurassic, enhanced extensional verrucano Unit crops out exclusively in small and tectonics was responsible for the sedimentation of scattered areas of southern Tuscany (Fig. 2) and coarse calcareous breccias, followed by radiolarites this does not allow us to carry out a detailed recon- in the Late Jurassic. The lack of younger terrains struction of its evolution. Its stratigraphic or tectonic referable to the Pseudoverrucano Unit with cer- substratum is unknown. Stratigraphic successions tainty does not allow one to unravel its post-Jurassic and a palaeogeographical scheme are reported in evolution and to constrain its deformation age. Figure 3. The successions start with continental allu- However, it can be seen that the Pseudoverrucano vial and braided deposits, made up mainly of reddish Unit represents in the Northern Apennines the conglomerates and sandstones with minor and thin highest Tuscan tectonic unit. violet or yellowish pelitic beds. The outcrop thick- ness reaches 30 m. Conglomerate clasts consist of Southern Apennines-Sicilian Maghrebids white or pink quartz, subordinate quartzite, and red or black chert. The redbed succession is Pseudoverrucano-like deposits. Unmetamorphosed azoic, but in its upper part thin levels of limestones continental redbeds, which show lithological suc- bearing Triasina hantkeni are locally intercalated cessions and tectonosedimentary evolution compar- within the elastic rocks (Costantini et al. 1980b). able with that of the Tuscan Pseudoverrucano Unit, Consequently, the age of the clastic basal formation occur in some nappes of the Calabrian-Peloritanian (Pseudoverrucano Formation sensu stricto) is essen- Arc (Fig. 4). Nappes characterizing this orogenic tially Triassic, although an earliest Liassic age of the sector, made up of Palaeozoic basements and uppermost levels cannot be ruled out. Meso-Cenozoic cover, have been considered as the most internal units of both the Southern Apen- Post-Triassic succession (Lower Jurassic-Upper nines and Sicilian Maghrebids (Durand Delga & Jurassic). Redbed successions of the Pseudoverru- Fontbot6 1980; Bouillin et al. 1986; Guerrera cano Unit are followed by grey to pink thick- et al. 1993). bedded oolitic limestones (Montebrandoli locality) Middle?- Upper Triassic continental deposits and by dark grey marls and cherty limestones with occur at the base of the Meso-Cenozoic covers of ammonites (Punta delle Rocchette locality). These the Sila, Stilo, Piraino and Longi-Taormina Units rocks are Liassic in age and Domerian levels have (Fig. 4). Their stratigraphic successions (Fig. 5) been recognized with certainty. The upper part of are characterized by typical redbeds, unconform- the Montebrandoli oolitic limestone is cut by thin able on Hercynian phyllites and metarenites, neptunian dykes and shows karstic cavities filled intruded by late Hercynian granitoids. The redbed Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

TRIASSIC REDBEDS IN WESTERN MEDITERRANEAN CHAINS 5

Fig. 2. Schematic geological map of Tuscany. The TM-b Unit to the NW of the Livorno-Firenze alignment corresponds to the Massa Unit; the TM-b Unit to SE of this alignment corresponds to the Monticiano-Roccastrada Unit. Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

6 V. PERRONE ETAL.

MONTEBRANDOLI PUNTA DELLE COLLECCHIO ROCCHETTE L~ -7'_~ ~----~-~-~-~ cM

~...~: ~... "...... ~...... ,o

MONTEBRANDOL, I PUNTAROCCHETTE DELLE I COLLECCHIO

9..= .~..~ "...~ 9 .

Calcareous megabreccias and Marls and cherty limestones radiolarites (Middle-Upper Jurassic) (Lower Jurassic)

'~'I Oolitic limestones and calcarenites Red conglomerates, sandstones and (Lower Jurassic) pelites (Upper Triassic)

Fig. 3. Stratigraphic columns and Jurassic palaeogeographical schematic section of the Pseudoverrucano Unit in Southern Tuscany. Modified from Costantini et al. (1980a).

successions are exclusively made up of clastic rocks Post-Pseudoverrucano successions (Lower Jurassic- (red quartzarenites and minor quartzose conglomer- Aquitanian). Clastic deposits on top of redbeds in ates and red-pro'pie mudrocks). The most complete the Longi-Taormina Unit gradually change succession occurs in the Longi-Taormina Unit, upwards to neritic black limestones (Hettangian- where redbeds, up to 300 m thick, are topped by Sinemurian). The succession continues with c. 20 m of greyish sandstones, silty clays and yel- Upper Liassic to Oligocene slope and pelagic depo- lowish dolostones, in which Hettangian palinofloras sits (marls; marly, cherty and nodular limestones; have been recognized (Baudelot et al. 1988). In the scaglia-like red marls and limestones, rich in Sila Unit, redbeds occur in the Longobucco neritic re-sediments; Lentini 1975; Bonardi et al. Sequence (Young et aL 1986; Santantonio & 1976). A network of neptunian dykes, also Teale 1987): they lie on Palaeozoic metamorphites cutting across the Palaeozoic basement, suggests and granitoids and are followed by Hettangian that extensional tectonics clearly acted during and brown pelites, yellowish sandstones, conglomerates after Toarcian time. The succession ends with Aqui- and black pelites (Baudelot et al. 1988). At the base tanian siliciclastic turbidites (de Capoa et al. 1997). of the Mesozoic succession of the Stilo Unit, clastic In the Sila Unit, the Longobucco redbeds pass deposits are lacking or are reduced to a few metres upwards to Sinemurian neritic sandy limestones, of thin palaeosoils and/or sandstones and pelites. In rapidly grading to Pliensbachian-Toarcian slope the Tiriolo area, where the thickest succession marls and turbiditic sediments (Magri et al. occurs, continental redbeds, probably Late Triassic 1965). Deposits younger than Early Jurassic are in age, follow shallow-water sands and clays of few recognizable in the Caloveto Sequence, where metres in thickness (Critelli & Ferrini 1988). In the redbeds are lacking and Sinemurian carbonate Piraino Unit, which is made of several small tec- platform rocks directly lie on the Palaeozoic base- tonic slices (Cecca et al. 2002), typical purple ment. In the Caloveto Sequence, neritic carbonates conglomerates and sandstones, 20 m thick, charac- are followed by Pliensbachian-Toarcian slope terize the lowest slice. sediments and by Middle Jurassic-lowermost Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

TRIASSIC REDBEDS IN WESTERN MEDITERRANEAN CHAINS 7

Post-orogenic and volcanic terrains Plio-Quaternary +•.Etna and Aeolian volcanics ~ ~1 Lower Pliocene-Upper Tortonian I Southern Apennines IONIAN ~ External Units ~4" Sibari SEA I ~ ~ 1Lucanian Ocean Units Graben Calabria-Peloritani Arc Northern Sector I~ gungro-Verbicaro Unit ~ OphioliticUnits _][~ Castagna and Bagni Units l+*J ]II Sila Unit basement and cover Paola Calabda-Peloritani Arc Southern Sector ++++(+++~+ ~ 9 ~ Stilo-Capo d'OrlandoFormation + +,,11.4"+ + %+j + + § + § ...... Ali-Montagnareale Unit ~+* § + +~ § § § + ~::~ Longi-TaorminaUnit ~ Piraino Unit Croton~ Aspromonte, Mela, Mandanici, Fondachelli, Cardeto, Africo Units Stilo Unit Basement and cover Sicilian Maghrebids ~ External Units Maghrebian Flysch Basin Units Soverato Tropea

Aeolian Islands

TYRRHENIAN SEA

Capo IONIAN SEA

t t t t

4" 4- ~ " Taormina 0 30 km ......

Fig. 4. Schematic geologicalmap of the Calabrian-PeloritanianArc. Verrucano-likedeposits are present in the Lungro-Verbicaro, Bagni and A1]-MontagnarealeUnits; Pseudoverrucano-likedeposits occur in the Sila, Stilo, Longi-Taormina and Piraino Units.

Cretaceous pelagic deposits (marls, sandstones, related to the strong extensional tectonics associ- cherty limestones, nodular limestones, radiolarites ated with the Tethys opening, cuts across both and Calpionella limestones; Santantonio & Teale Mesozoic and Palaeozoic terrains (Bouillin & 1987). A prominent network of neptunian dykes, Bellomo 1990). Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

8 V. PERRONE ETAL.

SILA UNIT Longobucco Sequence

LONGI-TAORMINA UNIT

ats

cocm

mcpl

STILO UNIT Monte Stella Section

oat Impd oacs bxc STILO UNIT oml Tiriolo Section bxc PIRAINO UNIT _150 m ~ gcl ;pl Im SILA UNIT gcnl .100 m Caloveto Sequence JS pvr Inl cpl tgC .50m 200 m jpd Imt tgd pvr )Mr Inc pvr .Om f l00m ps

pal pal pal )al pal 0m

Fig. 5. Stratigraphic columns of the Pseudoverrucano-bearing units of the Calabrian-Peloritanian Arc (Longi- Taormina, Sila, Stilo and Piraino). pal, Palaeozoic epimetamorphites and granitoids; pvr, Upper Triassic redbeds; lnl, Hettangian-Sinemurian neritic limestones; lm, Pliensbachian slope marls; It, Domerian-Toarcian turbidites; lnc, Sinemurian neritic limestones; lmt, Pliensbachian-Toarcian slope marls and turbidites; jpd, Middle-Upper Jurassic pelagic sediments; cpl, Lower Cretaceous pelagic limestones; ps, palaeosoil; tgd, Upper Triassic-Lowermost Jurassic dolostones; gcnl, Jurassic-Cretaceous neritic limestones; bxc, bauxitic clays; oml, lower Oligocene marls and limestones; oacs, upper Oligocene-Aquitanian calcarenites and conglomerates; oat, Aquitanian turbiditic marls and sandstones; lmpd, Carixian-Upper Jurassic pelagic sediments; mcpl, Tithonian-Albian maiolica-like pelagic limestones; cocm, Cenomanian-Oligocene scaglia-like limestones and marls; ats, Aquitanian turbiditic sandstones; lds, Toarcian-Aalenian sandstones; jcd, Jurassic?-Cretaceous? dolostones.

The post-Triassic succession of the Stilo Unit is hardground, karst and bauxitic clay, and is topped the only one in the Calabrian-Peloritanian Arc by Aquitanian siliciclastic turbidites and marls made up of shelf and ramp carbonates. It is charac- (Bonardi et al. 2002, 2003). terized by Mesozoic dolostones, limestones and In the Piraino Unit, finally, the lowest slice calcareous breccias, and by Oligocene marsh forming the unit, made up of redbeds, is followed marls, calcareous conglomerates and calcarenites, by another slice where a siliciclastic formation sometimes rich in metamorphic and plutonic with upper Pliensbachian-middle Aalenian ammo- rock d~bris, shows repeated hiatuses, marked by nites, whereas Jurassic?-Cretaceous? crystalline Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

TRIASSIC REDBEDS IN WESTERN MEDITERRANEAN CHAINS 9 dolostones and Cretaceous nodular, crinoidal and with green and red pelites precedes the deposition cherty limestones constitute the uppermost slice of of Rhaetian-Lowermost Jurassic neritic carbon- the unit (Cecca et al. 2002). ates, represented by dark grey crystalline dolos- tones, dolomitic limestones and whitish massive Palaeogeographical evolution. As regards the Mid- limestones. Neritic sediments are replaced by Triassic-Jurassic interval, the tectonosedimentary pelagic deposits (marly, nodular and cherty lime- evolution in the Longi-Taormina, Sila and stones; marls) in the Pliensbachian, which persist Piraino successions is similar to that of the up to the Palaeogene. Neptunian dykes mark Juras- Tuscan Pseudoverrucano Unit. It can be summar- sic extension (Bouillin & Naak 1989). In many ized as follows: (1) deposition, during Mid-Late units (Kef Sebargoud, Rhedir, Tengout; Raoult Triassic times, of continental redbeds on a Variscan 1974), Jurassic and Cretaceous successions are basement, whose uppermost levels are represented characterized by hiatuses, mainly in the Upper Cre- by mid-Carboniferous clastic deposits of Culm taceous sequences. In these instances, Palaeogene facies (Bouillin et al. 1987; Spalletta & Vai sedimentation starts with calcareous breccias and 1989); (2) development of a carbonate platform massive limestones containing algae and larger for- during the Hettangian-Sinemurian transgression; aminifers (Raoult 1974). The most recent strata are (3) platform deepening and development of slope represented by sandstones (Nummulitique II; and basinal facies in the Pliensbachian; (4) develop- Raoult 1974) of Oligocene or possibly younger ment of breccias and neptunian dykes associated with age (Guerrera et al. 1993). extensional tectonics (Toarcian-Late Jurassic). In the Alpine metamorphism is lacking and the succes- Longi-Taormina Unit, pelagic sedimentation per- sions display a lithological and stratigraphic evol- sisted until the development of Aquitanian foredeep ution comparable with that of the units containing sediments predating the deformation (de Capoa Pseudoverrucano-type deposits. Coutelle (1987) et al. 1997). In the Stilo Unit the sedimentary evol- and Coutelle & Delteil (1989) showed similarities ution was different; the succession here consists of between the stratigraphic successions of some neritic and paralic sediments and is marked by Kabylian Units and those of the Calabrian- repeated hiatuses, hard-grounds and bauxitic clays. Peloritanian Arc and Tuscan Nappe. Those However, its foredeep deposits and subsequent defor- workers placed all these groups of units, passing mation are coeval with those of the Longi-Taormina one into the other, in the same palaeogeographical Unit (Bonardi et al. 2003). belt, named the Intermediate Continental Domain and considered as the western part of the Adria- Tellian Maghrebids Apulia Plate. In the Tellian sector of the Maghrebian Chain our own observations are sparse. Data from the litera- Rifian Maghrebids ture indicate that Triassic redbeds occur in the Pseudoverrucano-like deposits (Saladilla For- Internal Units of the Lesser and Greater Kabylias mation, Triassic). In the Rifian Maghrebids and in the Babors Units, these latter related to the (Fig. 6) Middle-Upper Triassic redbeds, which External Tellian Units. show Pseudoverrucano-like facies, occur at the Pseudoverrucano-like deposits. In Kabylias, base of the Meso-Cenozoic cover of both Ghomar- Middle-Upper Triassic redbeds (Raoult 1974; ide and Internal Dorsale Calcaire Units (Nold et al. Wildi 1983; Tefiani et al. 1991; Kotanski et al. 1981; Wildi 1983; Fig. 7) and, as their equivalent 2004), resting on Palaeozoic phyllites and metare- formations of the Betic Cordillera, have been nites (Ordovician-Carboniferous), characterize grouped in the Saladilla Formation (Martfn-Algarra the base of the Meso-Cenozoic covers of the et al. 1995; Maate 1996). This formation (Fig. 7) Dorsale Calcaire Units, which constitute the struc- rests on a Hercynian basement, whose uppermost tural lowest units of the Kabylide Complexes. strata are represented by middle Carboniferous The redbeds are mainly made up of red-violet clastic deposits of Culm facies. The Internal conglomerates, including quartz, quartzite and Dorsale Calcaire units are generally detached from black radiolarite clasts, sandstones and pelites. In their basement, similar to the Triassic redbeds, some sections, thin Middle Triassic carbonate beds which are completely unknown in the outermost testify to a local marine environment. Upwards, Internal Dorsale Calcaire units (Hafa Ferkennix the succession grades into red and greenish pelites, Nappe); however, they are widely present at the followed by whitish, pink and yellow quartzarenites. base of the innermost Internal Dorsale Calcaire units (El Babat Nappe) with a lithostratigraphy Post-Pseudoverrucano successions (Lower Jurassic- similar to the cover of Ghomarides sensu stricto, Oligocene?) and palaeogeographical evolution. but usually with finer-grained, more distal facies The appearance of beds of dolostones alternating and thickness up to 125 m. In few localities (south Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

10 V. PERRONE ET AL.

Fig. 6. Schematic geological map of the Rifian sector of the Maghrebian Chain and of the Internal Units of the Rifian Maghrebids. Modified from Suter (1980). Pseudoverrucano-like deposits occur in the Ghomaride and 'Dorsale Calcaire' Nappes; Verrucano-like deposits are present in the Upper Sebtide Units. The External Nappes are characterized by redbeds of Germano-Andalusian facies. Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

TRIASSIC REDBEDS IN WESTERN MEDITERRANEAN CHAINS 11

GHOMARIDE INTERNAL "DORSALE of Tetouan), E1 Babat Triassic redbeds lie uncon- NAPPES CALCAIRE" formably on Palaeozoic rocks of the Koudiat 2: EL BABAT NAPPE Tiziane Ghomaride Nappe, forming a single tec- tonic unit (Maate et al. 1993b; Martfn-Algarra et al. 1995; Maate 1996). The stratigraphic succession of the Saladilla Fm, up to 400 m thick (Fig. 7), starts with coarse quart-

0 zose conglomerates and/or coarse-grained red 0 sandstones, and continues with red quartzarenites ,.,I and mudrocks including channelized conglomerates Q: lU and sometimes basic volcanic flows (Chalouan 8: 1986). Although a Permian age was proposed for the lower part of this succession (Milliard 1959) it has not been confirmed by more recent studies, and late Anisian-early Ladinian pollen was found near the top of red sandstones of the lower half of the succession (Baudelot et al. 1984; Martfn- Algarra et al. 1995). The succession is followed by yellowish, white and pink sandstones alternating with red clays in which a 5-20 m thick interval of marls and sandy dolostones is locally present. The upper part of the succession is formed by yellowish quartz-rich conglomerates with rounded dolostone clasts alternating with, and changing upwards to, red, yellow and greenish sandstones and pelites, palynologically dated as late Carnian, with some dolostone and gypsum beds (Maate et al. 1993b; Martfn-Algarra et al. 1995; Maate 1996). The Saladilla Formation deposits are organized in two transgressive, thinning and fining upward megasequences of Mid-Triassic and Late Triassic age, respectively. The lower megasequence shows an evolution from alluvial and fluvial deposits to shallow marine carbonates upwards. Palaeocurrents indicate fiver flow towards the west and SW, and provenance of clastic deposits from erosion areas located towards the east (Maate 1996). The Late Triassic megasequence started after a regression followed by erosion and redeposition of Mid- Triassic carbonate clasts in high-energy, sandy con- glomeratic (beach) environments and, since the late Carnian, was followed by deposition in a wide pelitic coastal plain (mudflat) with some carbonate ~~~L ~ Microcodiumand and evaporite episodes. 9 - -Nummulites limestones ~ Pelagic limestones Post-Pseudoverrucano successions (Lower Jurassic- i~l [~ Massiveneritic limestones Aquitanian). The presence on top of the Saladilla and paleokarst Fm of undated dolostones, followed by shallow :~ $ Basicvolcanics marine white massive limestones suggests trans- gression and development of an Early Jurassic Dolostones ~ Sandstonesand pelites shallow carbonate platform dated as Sinemurian I,,'1 -" 1~'1 = = in the Ghomaride cover sensu stricto, where this Phyllites and I~iConglomerates ~ metarenites ~and breccias succession is only few tens of metres thick. In the Internal Dorsale Nappes the dolostones are much Fig. 7. Stratigraphic columns of the Rifian Ghomaride thicker (up to 200 m) and, in their lower part, cover and Internal 'Dorsale Calcaire' Nappes (not to scale). include isolated cross-bedded conglomerate Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

12 V. PERRONE ET AL. intervals with well-rounded white quartz clasts and Oligocene-Aquitanian synorogenic siliciclastic oolitic-bioclastic limestones bearing the Rhaetian sandstones and conglomerates were deposited foraminifer Triasina hantkeni; they are followed during deformation of the Ghomaride realm and by thick (up to 300 m) Hettangian-Sinemurian before the final emplacement of the E1 Babat and white massive neritic limestones (Maate 1996). Hafa Ferkennix Nappes (Maate 1996). In the This shallow marine platform underwent break- latter the conglomerates are associated with off, tilting and local development of palaeokarst upper Oligocene marls and calcareous sandstones surfaces during the Pliensbachian (Maate et al. reaching more than 200 m in thickness. The strati- 1991; Maate 1996). This event was followed graphic successions are capped by massive, clast- either in the Ghomaride cover sensu stricto or in supported, heterometric, Aquitanian conglomer- the E1 Babat Nappe by deposition of condensed ates and breccias rich in clasts of prealpine upper Pliensbachian-Toarcian silty and fine sandy (and subordinately alpinized) plutonic and cherty limestones and marls, and nodular lime- metamorphic rocks (Martfn-Algarra et al. 2000). stones, but no younger Mesozoic deposits are present (Maate et al. 1991; Maate & Martfn- Betic Cordillera Algarra 1992, 1993; Maate 1996). However, the succession of the Hafa Ferkennix Nappe is thicker Pseudoverrucano-like deposits ( Saladilla Formation, and less condensed: it includes Pliensbachian- Triassic). Triassic redbeds with Pseudoven'ucano- Toarcian cherty limestones, marls and nodular like facies and associated marine sediments occur limestones, Middle-Upper Jurassic radiolarites, in the highest tectonic units of the Betic Internal Tithonian-Neocomian greenish calcilutites, Domain, the Malaguide Complex (Fig. 8). They Lower Cretaceous calcareous breccias, and upper- are included in the Saladilla Formation, which most Cretaceous-Eocene pink and green marls was defined only in the Malaguide Units (Roep (Maate et al. 1993a; Maate 1996). 1972). The Malaguide Meso-Cenozoic stratigraphic In the Ghomaride cover sensu stricto and in some successions are similar to those of the Rifian Gho- Internal Dorsale Units Palaeocene-Eocene Micro- marides, thus testifying to an equivalent tectonose- codium, Alveolina and Nummulites limestones dimentary history and deformational evolution lie directly on Jurassic-Cretaceous rocks and later- (Martfn-Algarra 1987, 2004; Maate 1996). ally evolve to pelagic scaglia-like marls (Maate However, they are frequently thicker and stratigra- et al. 1991, 2000; Maate 1996). Upper phically more complete than the Ghomaride

Fig. 8. Schematic geological map of the Betic Cordilleras. Modified from Vera (2004). Verrucano-like deposits occur in the Alpujarride Complex; Pseudoverrucano-like deposits characterize the Malaguide Complex. The External Domains (Subbetic and Prebetic Units) are characterized by redbeds of Germano-Andalusian facies. Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

TRIASSIC REDBEDS IN WESTERN MEDITERRANEAN CHAINS 13

successions, especially in the Morrdn de Totana biomicritic, crinoidal and Lithiotis limestones. Unit of Sierra Espufia, in SE Spain (Martfn-Martfn After an unconformity on top of platform lime- 1996; Sanz de Galdeano et al. 2000; Mart/n- stones, Domerian-Toarcian cephalopod-rich yel- Martin et al. 2003; Caracuel et al. 2006). lowish nodular limestones with ferruginous Usually two transgressive megasequences (three in oolites were deposited. These condensed pelagic Sierra Espufia) can be distinguished in the Malaguide sediments are followed by Middle Jurassic micri- Triassic redbeds successions (Fig. 9). The first mega- tic, crinoidal and cherty limestones topped by sequence starts with red pelites with intercalated two hardgrounds of early Bajocian and early sandstones and quartz-rich polygenic conglomerates Callovian age, respectively. The Upper Jurassic in which coarse-grained and thicker-bedded intervals rocks are represented by middle Oxfordian marls frequently (but not always) concentrate in the strati- and marly limestones evolving to limestones, by graphically lower part, forming thinning and fining lower Kimmeridgian massive and nodular lime- upwards sequences, deposited in alluvial-fluvial stones and, finally, by upper Tithonian marls environments with more distal (floodplain) facies with crinoids and calpionellids, which are covered toward the top of the succession (Roep 1972; by limestones and marly limestones of early Martln-Algarra et al. 1995). Scarce palynological Berriasian age. A palaeokarst surface separates data indicate a Mid-Triassic (early Anisian) age for these Cretaceous rocks from glauconitic-phospha- this part of the succession (Simon & Kozur 1977; tic calcareous green sands, breccias and marls M~ikel & Rondeel 1979). Available palaeocurrent (Albian-Turonian) while a further unconformity measurements from cross-bedded sandstones occurs at the base of Upper Cretaceous white obtained in various Malaguide outcrops indicate pro- and pink, scaglia-like marls and marly limestones venances from an erosional area located to the south (Martfn-Algarra 2004). and SE (locally SW: Sierra Espufia), of the present- Following a further unconformity at the top of the day Saladilla Fm outcrops (MS_kel 1982, 1988; Mesozoic succession, Palaeocene deposits include Mill(el et al. 1984). Marine transgression is indicated Microcodium-rich shallow marine limestones and by massive to well-stratified dolostones (up to 160 m continental marls and conglomerates with garum- thick in Sierra Espufia) with shallow marine facies nian facies (Mart/n-Martin et al. 1998), whereas and Ladinian-early Carnian fossils (M/ikel 1985) Eocene and lower Oligocene rocks are represented on top of continental redbeds. by different shallow marine formations rich Ladinian-Carnian dolostones were partially in larger foraminifera (Mart/n-Martln et al. eroded (or totally in many outcrops) during 1997a,b). The succession (Fig. 9) is unconformably regression related to the beginning of the second capped by upper Oligocene to Aquitanian mainly transgressive megasequence. This starts with clastic deposits (Ciudad Granada Group; Guerrera mudflat varicoloured, mainly reddish, pelites and et al. 1993), which, in Sierra Espufia, rest on a sandstones with intercalated conglomerates first generation of Malaguide cover tectonic units bearing carbonate pebbles (up to 100 m thick in (Mart/n-Martin 1996; Martin-Martfn & Marffn- Sierra Espufia; Sanz de Galdeano et al. 2000), Algarra 2002), fan delta calcareous conglomerates, associated with yellow cross-bedded sandstones sandstones, limestones and marls (Bosque Fm) and with rounded dolostone clasts deposited in beach siliciclastic deep marine turbidites (immature sand- environments (Roep 1972). These coastal plain stones, pelites and polygenic conglomerates; Rio facies associations are covered by upper Carnian Pliego Fro). As their equivalent Ghomaride depos- shallow marine marls, marly limestones, limestones its, these conglomerates contain clasts of plutonic and dolostones, above which Lower Jurassic plat- and metamorphic rocks identical to those widely form carbonates are usually found (Mart/n-Algarra cropping out in the pre-Alpine basements of the et al. 1995). In Sierra Espufia these dolostones Calabrian-Peloritanian and Kabylian Units, a fact contain chert nodules and ribbons (MS.kel 1985) pointing towards a close proximity between all and are followed by cross-bedded sandstones and these domains up to, at least, the end of the Aquita- polygenic conglomerates, which represent the nian (Mart/n-Algarra et al. 2000; Careri et al. base of the third sequence, and by uppermost 2004). Triassic grey clays with gypsum beds (25 m thick) changing progressively to the Jurassic succession Petrology and sandstone detrital modes (Sanz de Galdeano et al. 2000). Triassic-Lowermost Jurassic continental redbeds Post-Pseudoverrucano successions (Lower of Pseudovermcano facies have been analysed to Jurassic-Aquitanian). The Malaguide Jurassic determine the sedimentary evolution, provenance (Mart/n-Algarra 2004; Caracuel et al. 2006) starts and burial history of this facies. with shallow marine dolostones (Hettangian?) The studies have been carried out both in the followed by Sinemurian white, oolitic-oncolitic, Internal Domains of the Mediterranean Chains Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

14 V. PERRONE ET AL.

Sierra Espuna (Morron'--I de Totana.... Unit) ,AN t ~ . =~ AQUtTANIAN- ."/ UPPER OLIGOCENE + ,//'J Velez Rubio __//# ~ LOWEROLIGOCENE- /'" PALEOCENE ..~" ,,* ...... M&laga ./"" "" --'" ) CRETACEOUS MALM

...... ! .- .-- DOGGER

I~E:::E~E~ i ...... LIASSIC

RHAETIAN NOR]AN

CARN1AN

x \ x x x x LADINIAN x ~x x

\ --x \

x 100m ",\ ANIStAN

0 PALAEOZOIC

~ Cher'tylimestones I Siliceous marls and dolostones ~ Clay with gypsum ~ Polygenic conglomerates Nodular limestones ~ Petites ;-~,-,~.~--~-.~--~ Turbiditic pelites Massive limestones Quartzarenitesand ~;~ and sandstones ~, ~~< ~ microconglomerates Carbonate Thin bedded limestones ~ Quartzose conglomerates , ,, conglomerates Marls and marly Dolostones ~ Grauwackes and limestones slates

Fig. 9. Synthetic stratigraphic columns of the Betic Malaguide Nappes. The Tertiary succession in Sierra Espufia corresponds to areas of reduced thickness. Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

TRIASSIC REDBEDS IN WESTERN MEDITERRANEAN CHAINS t5 from the Gibraltar Arc to the Calabrian- fragments include slate, radiolarian chert, argillac- Peloritanian Arc and in the Tuscan Pseudoverrucano eous chert and minor felsic volcanic rocks. Con- Unit. A significant number of sandstone and glomerate clasts consist mainly of quartz and mudrock specimens, sampled in three to five strati- include the same lithologies as the lithic fragments graphic sections in all these orogenic sectors, have in sandstones. been considered. The nature of the clastic deposits, both in sand- Pseudoverrucano sandstones range from pre- stone and conglomerate strata, suggests a prove- vailingly quartzarenite to quartzolithic (Fig. 10), nance dominantly from sedimentary and containing abundant monocrystalline and polycrys- metasedimentary rocks of the Palaeozoic basements talline quartz; feldspar is subordinate. Lithic of the redbeds, which include mainly Cambrian to

Qt Qm

F ~ ...... Lt

Qp Lm

L

Lvm '' ...... 'X~ ...... ' Lsm Lv ~'k/" ...... i Ls

Fig. 10. Qt-F-L, Qm-F-Lt, Qp-Lvm-Lsm and Lm-Lv-Ls triangular plots for redbed sandstones of the Betic Malaguide (o), Rifain Ghomaride-'Dorsale Calcaire' (o), Tuscany and Calabrian-Peloritanian Arc (.) Nappes. Qt, total (monocrystalline + polycrystalline) quartz including cherts; Qm, monocrystalline quartz; Qp, polycrystalline quartz including chert; F, feldspars; L, aphanitic lithic fragments (L = Lv + Lm + Ls); Lt, aphanitic lithic fragments + polycrystalline quartz; Lm, metamorphic lithic fragments; Lv, volcanic lithic fragments; Ls, sedimentary lithic fragments; Lvm, volcanic and metavolcanic lithic fragments; Lsm, sedimentary and metasedimentary lithic fragments. Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

16 V. PERRONE ET AL. mid-Carboniferous successions of clastic rocks reflect provenances within a continental block (dominantly metarenites and metapelites), subordi- (Fig. 10). A majority of the suites in all studied nate carbonates and radiolarian cherts. regions, in fact, show quartzose framework modes In these basements, Ordovician to Permian mafic reflecting derivation from stable parts of the conti- to felsic volcanic, subvolcanic and volcaniclastic nent. Only some suites in each region display rocks are scarce, whereas late Variscan, or older, slightly more feldspathic framework modes, charac- plutonites and high-grade metamorphic rocks are teristic of the transitional group derived from conti- known only in Calabria and Kabylias, which con- nental blocks. Continental block-derived sandstones tribute only subordinately as source terrains for are particularly evident in the Rifian and Betic the redbeds. Two alternative hypotheses could be redbed sandstones. Source areas for these latter put forward to explain the scarcity or absence of suites were probably characterized by somewhat plutonic and/or high-grade metamorphic rock frag- greater relief with respect to the cratonic prove- ments in both sandstones and conglomerates, crop- nance areas. In the Calabrian-Peloritanian Arc, ping out in regions where plutonic rocks are at quartz-rich sandstones of cratonic and transitional present widely exposed (such as the Calabrian- origin occur not only during Triassic continental Peloritanian Arc): (1) the plutonic bodies were not rift-valley sedimentation but also during following exposed at the time of deposition; or (2) strong Early-Mid-Jurassic passive margin turbiditic depo- chemical weathering conditions mask the prove- sition (Zuffa et al. 1980; Cecca et al. 2002). In all nance signal. Strong chemical weathering of pluto- regions, a few sandstone suites show frameworks nic rocks in a hot, episodically humid climate with a containing enough lithic fragments (quartzolithic prolonged dry season would produce illitization of sensu stricto) to plot within the provenance field silicate minerals, oxidation of iron and concen- for derivation from recycled orogens on either a tration of quartz in thick soil profiles, which, later QtFL or a QmFLt plot (Fig. 10; see the caption for denuded by fluvial erosion, would produce rela- explanation of recalculated parameters). In these tively mature quartz-rich red deposits. Geochemis- cases, the lithic fragments were derived from sedi- try of mudrock beds present in the sandstone mentary and metasedimentary rocks of the Variscan successions confirms these weathering processes and pre-Variscan orogenies, and local volcanic and the provenance from quartzose metasedimen- fields related to both Permian and Triassic rifting tary sources. events or to older Palaeozoic metavolcanic and vol- Redbed quartzose sandstones from all the studied canic suites. successions have been extensively modified by deep burial from diagenetic to anchimetamorphic Mineralogy and geochemistry of mudrocks zones. The related processes include compaction, pressure solution, precipitation of authigenic min- Chemical data from redbed mudrocks provide erals, dissolution of framework grains, and substan- informations about source-area composition, tial reduction of porosity. Most detrital grains show palaeoweathering, sorting and recycling. Mudrocks three or more contacts with neighbouring grains, were collected on Rif and Betic Chains and from indicative of mechanically consolidated sandstones. Calabrian-Peloritanian Arc (Longi-Taormina and Many mica grains and soft lithic grains (shale, slate Sila Units). and phyllite) and rip-up clasts have undergone ductile deformation to form pseudomatrix. Source-area weathering. Weathering processes that Sandstones display heterogeneous distribution of occurred in source rocks have been detected using authigenic quartz, kaolinite, illite and feldspar, with the Chemical Index of Alteration (CIA; Nesbitt & minor carbonate cementation. Authigenic quartz Young 1982), the Chemical Index of Weathering formed as zoned syntaxial overgrowths on detrital (CIW; Harnois 1988) and the Plagioclase Index of quartz is the principal cement of these sandstones. Alteration (PIA; Fedo et al. 1995). The CIA However, the occurrence of quartz cement varies values for redbeds are very low (66-73, in the studied samples depending on the presence average = 69.9 _ 1.7) and they plot in the A-K of continuous clay coats that may retard quartz side of the A-CN-K diagram, close to the musco- cementation. Extensive dissolution and kaoliniza- vite field (Fig. l la), suggesting a K enrichment tion of detrital feldspar, mica and clay pseudoma- during burial history. Redbeds have a uniform trix occurred probably under an eodiagenetic CIW (95-98, average ---- 97.1 __+ 0.65) close to the meteoric regime. K-feldspar overgrowth, feldspar A apex in the A-C-N plot (Fig. l lb), testifying albitization and minor albite overgrowth occur to intense weathering in steady-state conditions, in where pore-filling kaolinite is also abundant. which material removal rate matches the production The tectonic setting of the redbeds basins during of mineralogically uniform weathering products the Triassic to earliest Jurassic implies that sand- generated in the upper zone of the soil profile. stone composition from nearly all regions should Unweathered plagioclase have a PIA value of 50 Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

TRIASSIC REDBEDS IN WESTERN MEDITERRANEAN CHAINS 17

(a) A (b) A -100 .AKa, Ch, Gi 100-- / k

- 80 8~ s O O

...... Gr ~ ...... C N 5~ Fig. 11. (a) Ternary A-CN-K plot (A is A1203; CN, CaO + Na20; K, K20). The samples fall close to the A-K join along a trend indicating K addition during diagenesis. Gr, granite; Bi, biotite; Ms, muscovite; I1, illite; Ka, kaolinite; Ch, chlorite; Gi, gibbsite; S, smectite. (b) Ternary A-C-N plot (A is A1203; C, CaO; N, Na20). The samples fall close to the A apex, suggesting intense weathering at the source.

whereas the Post-Archaean Australian Shales recycling. This is also consistent with changes in (PAAS) have a PIA value of 79. Redbeds have the A1203-TiO2-Zr diagram (Fig. 12b). very high PIA values (93-97, average = 95.3-t- As for the provenance, the Eu anomaly, which is 1.08), suggesting that most of the plagioclase has retained as the more conservative proxy of parental been converted to clay minerals. Results from the affinity (McLennan et al. 1993; Mongelli et al. CIW and PIA, therefore, confirm intense weathering 1998; Cullers 2000), is slightly higher (average at the source area. Eu/Eu* =0.73 + 0.04) than the PAAS value (Eu/Eu* = 0.66). Thus, the average Eu/Eu* of Recycling and provenance. Ancient sediments may redbeds could monitor an important supply of low undergo recycling and the Zr/Sc v. Th/Sc diagram Eu/Eu* mafic detritus that compensates for the (Fig. 12a) is a useful tool to assess the recycling recycling effect by reducing Eu/Eu*. In our case, processes (McLennan et al. 1993). It can be however, the recycling effect on the Eu anomaly observed that the redbeds are not clustered along was minor and, in turn, the low Eu/Eu* mafic det- the primary compositional trend but fall along a ritus supply was also minor although not negligible. trend involving zircon addition and thus sediment The limited importance of a mafic supply is

(a) (b) 10AI20 3 10 ......

,~,~y ...-'uranit,

o ,d:~'~x~" """ t~*~*

!-- Andesite~,tG%~g Basalt =''"

0.1 ,,,,i i . . ill ~ ii~ .... 9 . .IHllll,~Hl,I, ..... 1 10 1100 Zr 200TiO 2 Zr/Sc Fig. 12. Th/Sc v. Zr/Sc (a) and ternary 10A1203-Zr-200 TiO2 (b) plots. PAAS, Post-Archaean Australian Shales. The samples depart from the compositional trend, indicating zircon addition suggestive of a recycling effect. Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

18 V. PERRONE ET AL.

La

lO 9 8 Ultramafic 7 6

0 4 3 2 1 ~\-.~,~ ao ..... GraniteQ 0 0 2 3 Th Sc Y/Ni

Fig. 13. Ternary La-Th-Sc (a) and Cr/V v. Y/Ni plots (b). PAAS, Post-Archaean Australian Shales. Both plots rule out a significant mafic-ultramafic supply. also confirmed by other provenance proxies includ- history. The estimated temperature experienced ing the La-Th-Sc plot and the Cr/V and Y/Ni by the Triassic to lowermost Jurassic redbeds, ratios. In the La-Th-Sc ternary diagram obtained by coupling data on the percentage of (Fig. 13a), which discriminates felsic sources illitic layers in I/S mixed layers with the values of from more mafic sources (e.g. Bhatia & Crook the Ktibler index, is in the range of 100-180 ~ 1986; Cullers 1994), the redbeds fall in a region, Starting from the temperature estimates obtained close to the PAAS point, that clearly rules out a pre- by geothermometers based on clay minerals, the dominantly mafic source. Finally, a significant diagenetic-tectonic evolution should correspond mafic-ultramafic supply is ruled out also on the to a lithostatic-tectonic loading of about 5-6 krn. basis of the mixing curve between granite and a The sedimentary evolution of Middle-Triassic- mafic-ultramafic end-member in the Y/Ni v. Cr/ Lowermost Jurassic quartzose redbeds is homo- V diagram (Fig. 13b). geneous in all outcrops of the studied orogenic To determine the degree of post-sedimentary sectors, suggesting a common palaeogeographical processes possibly affecting the samples analysed in and palaeotectonic evolution since break-up of the present study and the range of temperature they Pangaea. They can be considered as a regional petro- experienced, the X-ray diffraction (XRD)-based facies that outlines the onset of the continental illite 'crystallinity' technique (Merriman & Peacor rift valley stage of the Mesozoic taphrogenesis in 1999) was used. The illite crystallinity index (IC) Western Pangaea, which allowed the opening of and the percentage of illite in the illite-smectite the Western Neo-Tethys Ocean. Therefore, these (I/S) mixed layers were measured on the <2 txm redbeds could represent a key stratigraphic marker size fraction XRD patterns from oriented mounts to distinguish a particular continental block within for the clay-rich levels from the continental redbeds. the Western Mediterranean Domains. The percentage of illitic layers in I/S mixed layers, estimated following Moore & Reynolds (1997), is in the range of 70-90% (R = 1 and 3 ordering, Verrucano-type successions Reickeweite number). In aH the studied successions, the Ktibler index values range between 0.65 ~ and Northern Apennines 0.28 ~ A20 (average = 0.45~ 0.1 ~ A20). These values indicate conditions ranging from the diage- Stratigraphy of the Verrucano Group. The netic zone (0.45-0.65 ~ A20) to the anchizone Verrucano Group deposits occur in all the Tuscan (0.30-0.40 ~ A20). Metamorphic Units, particularly in the Massa and In conclusion, detrital modes and geochemistry of Monticiano-Roccastrada Units (Fig. 2). In all the Triassic to lowermost Jurassic continental these units the Verrucano deposits unconformably redbeds suggest a provenance dominantly from overlie a pre-Alpine basement, represented mainly Palaeozoic sedimentary and metasedimentary by Palaeozoic phyllites and metarenites with some rocks similar to those forming the pre-Alpine base- intercalated layers of metavolcanic rocks and meta- ments underlying redbeds. Petrography and miner- dolo-stones and, locally, post-Hercynian continental alogy of redbeds testify to a complex burial or marine deposits of Late Carboniferous-Permian Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

TRIASSIC REDBEDS IN WESTERN MEDITERRANEAN CHAINS 19 age. In the Monticiano-Roccastrada Unit, the meta- whitish quartzites, associated with light quartzose morphic Monte Argentario Sandstone Formation phyllites and violet or greenish phyllites. The litho- (Upper Permian-Lower Triassic) is interposed logical and sedimentological features of the between the Palaeozoic basement and the Verrucano Verruca Fm indicate continental environments Group deposits (Cirilli et al. 2002; Lazzarotto et al. evolving from alluvial fan to alluvial plain 2003). crossed by braided seasonal streams in a semi-arid The Verrucano Group mainly consists of detrital climate. In the overlying Quarziti di Monte Serra continental formations, deposited in an oxidizing Formation, between 280 and 480 m thick, made environment. Rau & Tongiorgi (1974) considered up mainly of micaceous quartzites, quartzose phyl- that the violet colour characteristic of some of lites and phyllites, it is possible to recognize four these deposits results from the metamorphic over- members indicating different transitional or print at the expense of Buntsandstein-type, orig- marine environments. From the bottom to top, one inally reddish sediments. can recognize the Scisti Verdi, Quarziti Verdi, In the most complete succession of the Northern Quarziti Bianco-rosa and Quarziti Viola Zonate Apennines (Massa Unit), two sedimentary cycles, Members, indicating lagoon-marine, sandy shore, separated by a disconformity surface, have been deltaic platform and coastal pond environments, distinguished (Passeri 1985; Rau et al. 1985; respectively. The last member of the Quarziti di Martfni et al. 1986). The lower cycle, Anisian- Monte Serra Formation is followed by the Norian Ladinian in age, is characterized by frequent marine dolostones of the Grezzoni Formation. strata and by alkaline metabasalts (Punta Bianca; The Verruca and Quarziti di Monte Serra Monte Brugiana). The upper cycle (Verrucano Formations are usually correlated with the upper Group sensu stricto) starts with upper Ladinian con- Ladinian(?)-Carnian upper cycle of the Punta tinental sediments, evolving in the late Carnian to Bianca promontory (see below). In the carbonate-evaporitic deposits. The Verrueano Monte Pisano area, therefore, Anisian-Ladinian Group is followed by Norian-Liassic platform car- rocks of the Verrucano Group should not be bonates grading, in the Middle Liassic, into basinal deposited. pelagic deposits. Two sedimentary cycles, as noted above, are In the Apuane Unit (Giannini & Lazzarotto 1975; recognizable in the succession of the Punta Bianca Fig. 14), the continental deposits are lacking or area (Passeri 1985; Rau et al. 1985; Martfni et al. limited to a few metres of Middle Triassic- 1986). Both cycles show a progressive evolution Carnian violet quartz-bearing metaconglomerates, from continental to marine environment. The rare quartzites and phyllites alternating with Anisian-Ladinian lower cycle (Fig. 14) starts grey-reddish carbonate quartzites, microcrystalline with alluvial fan conglomerates, unconformable dolostones, grey and greenish phyllites (Carnian; on Palaeozoic phyllites, fed by the underlying base- Vinca Fm), followed by Norian hypersaline plat- ment, which grade to a coastal plain sandy-silty form dolostones (Grezzoni Fm; Ciarapica & sequence followed by clayey limestones and well- Passeri 1978). bedded limestones rich in dasycladacean algae, The Verrucano of the Massa Unit was described indicating the progressive development of a in detail by Rau & Tongiorgi (1974) and Tongiorgi restricted platform marine environment. Sedimen- et aI. (1977) in the Monti Pisani, but the most com- tation abruptly passes to turbiditic calcarenites and plete succession crops out at Punta Bianca sandstones and to clast-supported heterometric promontory. coarse white calcareous breccias, with interbedded In the Monti Pisani area, Rau & Tongiorgi (1974) calcarenites and calcareous mudstones. Clasts pre- distinguished in the Verrucano Group the continen- vailingly consist of Diplopora and crinoid lime- tal Middle Triassic Verruca Formation and the stones. The sequence continues with frequent Carnian Quarziti di Monte Serra Formation, in calcarenite beds, associated with lenticular con- which marine sedimentary facies are present glomerates, sandstones, violet or grey-greenish (Fig. 14). The Verruca Formation, unconformable siltstones and claystones, calcareous breccias, fol- on Palaeozoic phyllites and metarenites, includes lowed by a volcanic interval, made up by basaltic three members, from bottom to top: (1) Anageniti lavas, locally with pillows, and volcaniclastic Grossolane Member, made up of reddish coarse rocks, capped by thin beds of red cherts. The last conglomerates, 40-100 m thick, with a quartz- phase of the lower cycle is represented by a new micaceous sandy matrix; centimetre-sized clasts level of calcareous breccias, 15 m thick, whose are mainly of quartz and minor quartzites and rhyo- upper beds show palaeokarst structures indicating lites; (2) Scisti Violetti Member, formed by violet an abrupt emersion. pbyllites and quar-tzose phyllites, 180-200m The upper cycle (upper Ladinian?-Camian) is thick, with some intercalated beds or lenses of sand- almost exclusively made up of fluvial terrigenous stones and conglomerates; (3) Anageniti Minute sediments with, in the upper part, littoral and tidal Member, formed by 100-170 m of well-bedded sediments; that is, from bottom to top, violet siltites Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

20 V. PERRONE ET AL.

Fig. 14. Stratigraphic columns of Metamorphic Tuscan Units. Alpi Apuane Unit: Pal, Palaeozoic metamorphites; v, Middle-Upper Triassic Ven'ucano redbeds; gr, Norian dolostones; li, Hettangian-Sinemurian dolomitic and calcareous marbles; Is, Pliensbachian-Toarcian cherty metalimestones; m and d, Middle and Upper Jurassic calc- schists and radiolarites; ci, Lower Cretaceous crinoidal cherty metalimestones; cs and e, Upper Cretaceous-lower Oligocene calc-schists and calcarenites with nummulites; pmc, upper Oligocene-Aquitanian turbidite metasandstones. Massa Unit (Monte Serra Section): Pal, Palaeozoic metamorphites; Mid Triassic Verruca Formation: V~, coarse conglomerates (Anageniti Grossolane Member); V2, phyllites and sandstones (Scisti Violetti Member); V3, quartzites and phyllites (Anageniti Minute Member); Carnian Quarziti di Monte Serra Formation: $1, phyllites and micaceous quartzites (Scisti Verdi Member); $2, green quartzites (Quarziti Verdi Member); $3, light quartzites and phyllites (Quarziti Bianco-rosa Member); $4, hematitic micaceous quartzites (Quarziti Viola Zonate Member); gr, Norian dolostones. Massa Unit (Santa Maria del Giudice Section): Carnian Quarziti di Monte Serra Formation: $3, light quartzites and phyllites (Quarziti Bianco-rosa Member); $4, hematitic micaceous quartzites (Quarziti Viola Zonate Member); gr, Upper Carnian-Rhaetian dolostones; li, Hettangian-Sinemurian dolomitic and calcareous marbles; Is, Pliensbachian-Toarcian cherty metalimestones; mp, Middle Jurassic Posidonomya Marls; di and cp, Upper Jurassic Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

TRIASSIC REDBEDS IN WESTERN MEDITERRANEAN CHAINS 21 and claystones, passing to red-purple and violet et al. 2003) with the Verruca Fm of Monte Pisano sandstones and quartz clast-rich conglomerates, and with the lower part of the upper cycle of repeated alternations of quartzose sandstones, Punta Bianca and considered to be Ladinian in siltstones and slates, with some thin carbonate age, whereas the Tocchi Fm is considered to be beds in the uppermost levels. The sequence ends Carnian in age, on the basis of microfossils in with phyllites, fine-grained quartzose sandstones, some of the carbonate beds. carbonate phyllites and yellowish carbonates and The Triassic stratigraphic succession of the evaporites. Monticiano-Roccastrada Unit ends with Norian- Within the Monticiano-Roccastrada Unit, the Rhaetian grey dolostones and dolomitic limestones Ven'ucano Group (Costantini et al. 1987; Fig. 14) (Grezzoni Fro). consists of four formations, including the Tocchi Formation in the upper part. Below the Tocchi Post- Verrucano successions (Norian-Aquitanian ). Formation, three silicidastic formations, varying As noted above, in all the Tuscan Metamorphic from conglomerates to pelites, occur. Units the oldest post-Verrucano rocks are The stratigraphic succession starts with the represented by Norian-Rhaetian dolostones. Civitella Marittima Formation, made up of 200 m The post-Triassic succession of the Apuane Unit of thin-bedded green to light grey fine- to coarse- (Giannini & Lazzarotto 1975; Carmignani et al. grained metasandstones, intercalated with lenses 1987; Conti et al. 2004) continues with of metaconglomerates and minor grey or violet Hettangian-Sinernurian dolomitic marbles and cal- metasiltstones. Metaconglomerates, up to 60 m careous marbles (the 'Carrara Marbles'), followed thick, show white abundant quartz clasts, up to by cherty metalimestones and calc-schists ('Cipol- 15 cm in size, in a quartzose sandy matrix. This lini'; middle Lower to middle Middle Jurassic), formation has been considered Mid-Triassic in radiolarites ('Diaspri'; Callovian-Tithonian), and age and correlated (Lazzarotto et al. 2003) with cherty metalimestones bearing crinoids (Lower the lower cycle of Punta Bianca. Cretaceous). This prevailingly carbonate sequence The overlying Monte Quoio Formation, up to passes to Lower Cretaceous-lower Oligocene 200 m thick, consists of purple metasandstones and sericitic schists and calc-schists and it is closed metasiltstones intercalated with lenticular beds of by metasandstones of turbidite Pseudomacigno polygenic metaconglomerates. These latter are Formation (upper Oligocene-lower Miocene). characterized by centimetre-decimetre-sized clasts In the Massa Unit, the successive sedimentary of white and pink quartz, white, violet and green evolution of the Verrucano Group can be seen quartzites, and minor black siltites, violet phyllites in the northwestern side of Monte Pisano, in the and pink or red limestones with Anisian neritic Santa Maria del Giudice sequence (Rau & fossils. The Monte Quoio Fm grades into the Tongiorgi 1974). The Quarziti di Monte Serra Anageniti Minute Formation, consisting of yellowish Fm (Fig. 14) is followed by upper Carnian rauh- or whitish-pink quartzites and metaconglomerates wackes, Norian-Rhaetian dark grey dolostones intercalated with purple and minor grey-green (Grezzoni Fm) and metalimestones, lowermost metasiltstones and phyllites, followed by the Tocchi Jurassic marbles (Calcari Ceroidi) and cherty Formation, made up of breccias with clasts of limestones, Middle Jurassic Posidonomya marls, grey-greenish and violet phyllites in a yellowish Upper Jurassic radiolarites and multicoloured carbonate matrix, alternating with evaporitic sericitic schists (Cretaceous-lower Oligocene). limestones, metalimestones, quartzites and phyllites. The succession is capped by the turbidite The Monte Quoio and the Anageniti Minute sandstones of the Pseudomacigno Fm (upper Formations have been correlelated (Lazzarotto Oligocene-lower Miocene).

radiolarites and cherty metalimestones; cs, Cretaceous-lower Oligocene multicoloured sericitic schists; pmc, upper Oligocene-Aquitanian turbidite metasandstones. Massa Unit (Punta Bianca Section; according to Ran et al. 1985): Pal, Palaeozoic metamorphites; Anisian-Ladinian lower cycle: alc, alluvial fan conglomerates; cps, coastal plain sandstones and siltstones; rpl, restricted platform metalimestones; cbr, calcareous breccias and calcarenites; cvs, calcarenites, carbonatic shales, conglomerates and siltstones; db, calcareous breccias with diplopores; vc, basalts and volcanoclastic rocks; cb, carbonatic breccias; upper Ladinian?-Carnian upper cycle: vs, violet siltstones; vsc, violet quartzose sandstones and conglomerates; wss, white and violet quartzose sandstones and silstones; scl, sandstones and siltstones with thin carbonatic levels; cd, calcareous-dolomitic evaporite deposits. Monticiano-Roccastrada Unit: Pal, Palaeozoic metamorphites; cv, Middle Triassic metasandstones with metaconglomerate lenses; mq, Ladinian metasandstones and metasiltstones; am, Ladinian quartzites and violet phyllites; tc, Carnian breccias and evaporite carbonates; gr, Norian dolostones; m, lowermost Jurassic marbles; cm, di and sc, Lower Cretaceous cherty marbles, siliceous metapelites and varicoloured sericite schists. Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

22 V. PERRONE ET AL.

The post-Triassic stratigraphic succession of the us to completely rewrite the metamorphic history Monticiano-Roccastrada Unit above the Grezzoni of the Tuscan Metamorphic Units. In the eastern Fm continues with lowermost Jurassic massive part of Monte Argentario, the lower part of the Ver- yellow, pinkish and white marbles (Marmi Fm), fol- rucano succession of the Monticiano-Roccastrada lowed by some disconformable Upper Cretaceous Unit includes psammitic and pelitic metasediments heteropic formations consisting of well-bedded characterized by quartz, muscovite, hematite, chlori- cherty marbles, siliceous metapelites and metara- toid, sudoite, pyrophyllite, rare chlorite, kaolinite and diolarites, and varicoloured sericite schists and dolomite, and by quartz segregations with quartz, metamarls (Costantini et al. 1987). calcite, chlorite, cookeite, white mica, kaolinite and localized Mg- or Fe-carpholite (Theye et al. 1997). Tectonosedimentary evolution of the Tuscan The upper levels are characterized by a quartz-mus- Verrucano and comparison with that of the Tuscan covite-hematite assemblage with subordinate chlor- Pseudoverrucano. The tectonosedimentary evol- ite, paragonite, pyrophyllite and localized carpholite ution of the Tuscan Metamorphic Units is certainly in quartz segregations. more complex than that of the Pseudoverrucano The reconstructed polystage metamorphic evol- Unit. As regards the Triassic terrains, two sedimen- ution (Fig. 15) indicates a P-T path characterized tary cycles have been identified in the Punta by a first stage showing peak conditions at Bianca section (Fig. 14) of the Massa Unit and in P > 0.8 GPa and T = 300-400 ~ (Mg-carpholite, the Monticiano-Roccastrada Unit, whereas in the chlorite, quartz assemblage in the pyrophyllite stab- Apuane Unit and in the Monte Pisano area only ility field) in the lower levels, and at P > 0.7 GPa terrains referable to the upper cycle occur. The and T = 300-350 ~ (carpholite and pyrophyllite first marine beds, represented by neritic limestones, assemblage) in the upper levels. The second stage appear in the Anisian of the Punta Bianca section, (exhumation path) is marked by isothermal decom- and Anisian limestone clasts are also present in pression at P < 0.5 GPa (sudoite-pyrophyllite the Ladinian Monte Quoio Fm of the Monti- assemblage) and subsequent cooling at low T ciano-Roccastrada Unit. In the Punta Bianca (<300 ~ and P (late kaolinite). section, the Ladinian is almost entirely character- A similar evolution has been also reconstructed ized by calcareous neritic deposits and calcareous in the Mid-Tuscan Dorsal region (Monticiano- breccias, testifying to the rapid evolution and tec- Monte Leoni area; Giorgetti et al. 1998). Verrucano tonic fragmentation and resedimentation of carbon- metasediments consist of phyllites and Al-rich ate platforms as a result of a peak of tectonic quartzites including newly formed muscovite, activity which, during the late Ladinian, produces chlorite, chloritoid, pyrophyllite, sudoite, parago- basin uplifting and the disconformable deposition nite and kaolinite. Mg-carpholite is also present in of siliciclastic continental sediments of the synfolial quartz-calcite veins. upper cycle. Extensional tectonic activity is also Different stages in the P-T path have been marked by the occurrence of basic alkaline delineated. Peak conditions took place at volcanic rocks. P= 0.8-1.0GPa and T= 400-420~ in the After the late Ladinian?-Carnian, clastic deposits lower levels, and comparable or slightly lower P of the second cycle were covered by evaporitic- and T = 350-360 ~ in the upper levels (chlorite, carbonatic sediments, starting with deposition of phengite, chloritoid, pyrophyllite, Mg-carpholite; Carnian evaporites, followed by Norian dolostones syn- to post-kinematic assemblage). A retrograde and by Rhaetian-lowermost Jurassic neritic lime- isothermal path was followed during decompres- stones. From the Pliensbachian onwards, sedimen- sion at P < 0.5-0.6 GPa (sudoite and pyrophyllite tation becomes pelagic and is characterized by assemblage; late kaolinite). nodular, cherty and marly limestones and, even- In the Apuane Unit, peak metamorphic con- tually, by radiolarites. Marly-calcareous pelagic ditions were attained during the first deformation and turbidite sediments persist until the late phase and the occurrence of pyrophyllite + quartz Oligocene-early Miocene, when siliciclastic turbi- assemblages indicates P of 0.5-0.6 GPa and T dite sediments, deposited within the Apennine between 300 and 450 ~ (Di Pisa et al. 1985; foreland basin system, testify to the onset of com- Franceschelli et al. 1986, 1997; Schultz 1996; pressional deformation and the incorporation of the Molli et al. 2000b) or 0.6-0.8 GPa (Jolivet et al. Tuscan Metamorphic Units within the orogenic 1998). During the second deformation phase, edifice. T= 380 ~ in the eastern area and 340 ~ in the western area were reached (Molli et al. 2000a). Deformation and metamorphism of the Verrucano Metapelites of the Verrucano Formation in the Group. Miocene deformation was accompanied by Massa Unit (Molli et al. 2000b) result from two metamorphism. Recent petrological studies allow deformation phases. The D1 phase was responsible Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

TRIASSIC REDBEDS IN WESTERN MEDITERRANEAN CHAINS 23

Fig. 15. P-T paths of the Tuscan Metamorphic Units: dark shaded arrow indicates syncollisional peak stage; light shaded arrow indicates exhumation decompression stage. A, Monticiano-Roccastrada Unit; B, Alpi Apuane Unit; C, Massa Unit. Minerals of the metamorphic reactions: Qz, quartz; Kin, kaolinite; Prl, pyrophyllite; W, water; Car, carpholite; Phg, phengite; Chl, chlorite; Ms, muscovite; Chd, chloritoid; Ky, kyanite; And, andalusite; Stp, stilpnomelane; Bt, biotite, Sill, sillimanite. Petrogenetic grid is modified after Oberh~insli et al. (1995). for the development of the main foliation defined by with respect to the convergent tectonic stages, the quartz, white micas (muscovite _+ paragonite), Tuscan Metamorphic Units seem to have been chlorite, and chloritoid + kyanite. The same min- located in a more external position than the Pseudo- erals developed up to post-D1. The D2 phase was verrucano Sub-domain. responsible for the development of a crenulation cleavage marked by phyllosilicates. The recon- Southern Apennines-Sicilian Maghrebids structed thermobaric conditions indicate that the metamorphic peak occurred at P > 0.8 GPa and Verrucano-like successions. In the internal units of T=400-500~ (within the kyanite stability these orogenic sectors, cropping out in the field). The retrograde path involved a decrease of Calabrian-Peloritanian Arc, terrains comparable P and T with continued chloritoid development with the Verrucano of the Tuscan Metamorphic (within the pyrophyllite stability field). Units are recognizable only in the Bagni and Aft- These data indicate that during Neogene defor- Montagnareale Unit. Terrains correlatable to the mation in the Northern Apennines significant Verrucano are present also in the San Donato and crustal thickening occurred and the Tuscan conti- Verbicaro Units (Amodio Morelli et al. 1976), nental crust was underthrust to depths characterized recently redefined as the Lungro-Verbicaro Unit by pressures of 0.5-0.6 to 1.0 GPa. (Iannace et al. 2004b, 2005). This latter unit has This tectonometamorphic evolution, when it is been traditionally attributed to the Adria-Apulia considered within the general framework outlined margin and, therefore, considered as an external in this paper and compared with the other study Apenninic unit. This attribution has been only areas, may put into question the generally accepted recently discussed (Perrone 1996). location of the Tuscan Metamorphic Units on the The Bagni Unit (Amodio Morelli et al. Adria-Apulia continental margin. In any case, 1976) shows features similar to those of the Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

24 V. PERRONE ET AL.

Verrucano-bearing units, because its succession with abundant porphyroid levels, on which a few (Fig. 16) is affected by Alpine metamorphism and and scattered thin strips of Mesozoic cover occur. shows an early evolution to a marine environment The basal layers of this cover (Dietrich 1976) are (Upper Triassic dolostones; Scandone 1970). The represented by a few metres of red-purple meta- basement, widely cropping out in the Calabrian sandstones and metaconglomerates with violet Coastal Chain and in the Sila Massif (Fig. 4), is metasiltites, the latter forming the most frequent formed by Palaeozoic phyllites and metarenites, lithology. The Afi-Montagnareale Unit, cropping out in two small areas in the Peloritani Mountains Ali-Montagnareale (Fig. 4), also shows characteristics close to those Unit of the Verrucano, its succession being (Fig. 16) affected by metamorphism and showing an early evolution to a marine environment (Carnian evapor- CSC ites and Norian dolostones). The basement is made up of Lower Devonian-Carboniferous dark graph- ite phyllites, metarenites and metaconglomerates cpl with plant remains. The metamorphic Alpine cover starts with alternating reddish metapelites, metarenites and metaconglomerates (200-250 m thick), passing to 60 m of pinkish to yellowish rauh- wackes (Carnian) and Norian metadolostones. The Lungro-Verbicaro Unit (Iannace et al. 2004b, 2005) is widely exposed in northern Calab- nd ria (Fig. 4). The lowest levels of the stratigraphic succession crop out in the Monte Caramolo area tsr (Fig. 17), where they consist of a thick succession (at least 400 m) of grey, silvery and bluish phyllites, and minor metarenites, in which lenses of metali- mestones furnished Anisian-lower Ladinian algae (Bousquet & Dubois 1967; Iannace et al. 1995). Bagni Unit Phyllites pass to a thick formation of grey to black, sometimes nodular, marbles, which in the upper part of the formation grade laterally to a - 200 Ladinian-Carnian reef complex, consisting of . ....;...-~: :. vr boundstones with sponges and biogenic crusts, as

9oO , ,o.,- ooo" well as fore-reef breccias. The grey-black marbles are followed by upper Carnian-lower !'..:::.":..-:.'.il Norian metadolostones and laminated dolomitic - 100 metalimestones, deposited in a shallow open shelf and in a subtidal restricted environment, respect- ively. The sequence continues with typical Norian Pal Hauptdolomit facies. Megabreccias and neptunian dykes testify to a strong synsedimentary tectonics -Om in both the Ladinian and early Norian. Towards Fig. 16. Stratigraphic column of the Bagni and Ali- the south, in the Sant'Agata area, phyllites, calc- Montagnareale Unit. Bagni Unit: Pal, Palaeozoic phyllites schists, metarenites and metalimestones are inter- and metarenites; vr, Upper Triassic reddish metapelites, bedded with the upper Carnian dolostones metarenites and metaconglomerates; tsd, (Fig. 17) and these lithologies become dominant metadolostones; j 1, Jurassic metalimestones and cherty southwards, in the Coastal Chain Cetraro tectonic metalimestones; jlr, Upper Jurassic-Lower Cretaceous? window (Fig. 17). In both the Sant'Agata and cherty metalimestones and metaradiolarites. Ali- Cetraro areas the succession evolves to vacuolar Montagnareale Unit: Pal, Palaeozoic phyllites and brecciated dolostones passing to bedded evaporites, metarenites; vr, Middle Triassic reddish metapelites, followed by Norian Hauptdolomit and Rhaetian- metarenites and metaconglomerates; tsr, Camian calcareous-dolomitic evaporites; nd, Norian-lowermost lowermost Jurassic metalimestones with frequent Jurassic metadolostones and black metalimestones; jl, slumps, slump breccias and reddish metapelites. Jurassic marly and cherty metalimestones; cpl, Cretaceous Iannace et al. (2004a, 2005) have pointed out the pelagic metalimestones; csc, Cretaceous variegated huge thickness (over 1200 m) of Ladinian-Norian siliceous metaclaystones. carbonates in the Lungro-Verbicaro Unit. Within Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

TRIASSIC REDBEDS IN WESTERN MEDITERRANEAN CHAINS 25

8ant'Agata Sandy - peliUc tu d'Esaro turbidites ~ Rauhwackes zu.l Marly - calcareous turbidites ~ Bedded evaporites

Carbonate breccias ~ Evaporitestraces

iiiii m Radiolarites Phyllites ii 9..... i..i.. I . , i Cherty :? Z 71 7.T.'. Quartzites metalimenstones Bedded dark Metalimestones dolostones and marly metaUmestones Marly metalimestones LU I ~ Dolostones ~ I~ Reefal metalimestones 0 I ~ a ~ Slope breccias iI-I Monte "2,"t Caramolo ~ ~ ~ I~ -7--z--/-~I f I ~ Coastal Chain / I /_ Tectonic Windows i

L t 1 / / / Z / Z t re / / La Mula-Cozzo 1 t t I t t del Pellegrino 1

____- _~

I 100m

Fig. 17. Stratigraphic columns of the Lungro-Verbicaro Unit. Verrucano-like successions cover the Anisian-Carnian time span. Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

26 V. PERRONE ET AL. the Western Mediterranean, successions showing deformation phases (Somma et al. 2005). Petrologi- equivalent facies and thickness for the same interval cal data on metapelites indicate the occurrence of a occur only in the Alpujarride Units of the Betic polystage metamorphism: the first stage developed Cordillera. under P around 0.4GPa and T between 300 Post- Verrucano successions (Norian-Aquitanian). and 360 ~ (phengitic white mica (3.3-3.25 Si The post-Verrucano succession of the Bagni Unit contents p.f.u.) + paragonite + chlorite 4- quartz 4- (Dietrich 1976) starts with some metres of probably hematite + graphite + pyrophyllite assemblage). Upper Triassic grey and blackish, sometimes brec- The second stage took place at lower P and T ciated, saccharoid metadolostones. The dolostones conditions compared with the first stage. are followed by thin-bedded grey to light-coloured The rocks of the Lungro-Verbicaro Unit were metalimestones and cherty metalimestones with strongly deformed and affected by HP/LT meta- some beds of quartzose-calcareous microbreccias, morphism during Miocene tectonic phases grading upwards into alternations of grey and (Fig. 18). Their tectonometamorphic evolution is white cherty metalimestones and red, green and characterized by four deformation phases (D1 to black metaradiolarites, with thin layers of dark D4), three of them accompanied by metamorphism. metapelites and some beds of microbreccias. The Metamorphic index minerals of the FeO- calcareous succession, clearly turbiditic and up to MgO-AlzO3-SiOz-H20 (FMASH) system occur 120 m thick, is barren and a Jurassic to Early Cre- (Iannace et al. 2004b; Messina et al. 2004). These taceous age has been suggested on the basis of the deformation phases are constrained between the lithology and stratigraphic position. early Burdigalian age of the youngest levels of Above the Carnian rauhwackes, the stratigraphic the Lungro-Verbicaro Unit and the late Tortonian succession of the Alf-Montagnareale Unit continues age of the clastic deposits unconformable above it. with 100 m of grey to yellowish metadolostones In the upper levels of the unit these minerals and black metalimestones (Norian-lowermost Jur- are present in: (1) synfolial quartz veins, with assic), followed by 100 m of pelagic grey to bluish ferro- (XMg= 0.36-0.49) to Mg-carpholite marly and cherty metalimestones, metamarls with (XMg =- 0.51-0.57) 4- chlorite + phengite 4- carbo- intercalations of silicified metacalcarenites and nate 4- quartz assemblage; (2) phyllites associated microbreccias, and variegated siliceous metaclay- with quartz-carpholite veins, with chlorite + stones (Fig. 16). In these pelagic sequences, phengite + calcite 4- dolomite 4- quartz assemblage. Domerian to Lower Cretaceous levels have been In the quartz-carpholite veins, different caxpholite recognized (Somma et al. 2005). structural sites have been recognized: syn- to post- In the Lungro-Verbicaro Unit (Fig. 17), the D1 prismatic crystals, syn-D2 subgranular crystals Jurassic succession, lying above the Verrucano-like and syn-D2 to syn-D3 needle-like crystals. The repla- rocks and the already described Upper Triassic car- cement of carpholite in chlorite 4- phengitic white bonates, continues with cherty metalimestones and mica starts in late D3 and continues to D4. some metres of red and green radiolarites. A strati- In the lower levels of the Lungro-Verbicaro Unit, graphic gap and a disconfornaity separate the Jurassic metamorphic index minerals occur in quartz_ rocks from Upper Cretaceous-Oligocene coarse car- chlorite 4- chloritoid 4- phengitic white mica phyllites. bonate breccias, calcareous and marly-calcareous The first foliation, defined by phengitic white turbidites and, finally, lower Miocene metapelites mica, chloritoid and chlorite, is preserved in micro- and meta_renites. Basic lavas cross both Triassic and lithons, wrapped by the main foliation, $2, defined Jurassic layers. Successions characterized by similar by rotated chloritoid and recrystallized quartz, mus- stratigraphic development and referable to the covite and chlorite. Lungro-Verbicaro Unit have been recognized in tec- The P-T path of the metamorphic history of the tonic windows of the Calabrian Coastal Chain, up to Lungro-Verbicaro Unit is typical of a polystage the Catanzaro graben (Fig. 4). HP/LT event (Fig. 18). The first stage, related to syn- collisional peak conditions, took place during D1, at P Tectonometamorphic evolution. The deformation between 1.6 and 1.4 GPa and Taround 350 ~ (within and metamorphic evolution of the Bagni Unit the pyrophyllite stability field) in the upper levels of require new and detailed analyses, because no the unit, and it is defined by the quartz 4- phengite studies have been carried out after those of Bonardi (Si = 3.30-3.25 p.f.u.) 4- Fe-Mg-carpholite assem- et al. (1974), Dietrich (1976) and Colonna & blage in quartz veins, and by the phengite 4- chlorite Simone (1978). From a critical review of these assemblage in surrounding phyllites. In the lower papers, however, it seems possible to recognize HP levels of the unit, the first stage was reached at P Alpine metamorphic recrystallizations (presence of between 1.8 and 1.6 GPa and T around 420 ~ blue amphibole, phengitic white mica, etc.). (within the kyanite stability field) and it is marked The A1]-Montagnareale Unit displays ductile by the phengite 4- chloritoid + chlorite assemblage structures that developed during three Alpine in phyllites. The second stage involves several steps Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

TRIASSIC REDBEDS IN WESTERN MEDITERRANEAN CHAINS 27

Fig. 18. P-Tpath of the Lungro-Verbicaro Unit: dark shaded arrow indicates syncollisional peak stage; light shaded arrow indicates exhumation decompression stage. A, upper levels of the unit; B, lower levels of the unit. Minerals of the metamorphic reactions are as in Figure 15. Petrogenetic grid is modified after Oberh/insli et al. (1995).

of the exhumation path, which begins, during the D2 terrains now attributed to the Lungro-Verbicaro (first step), with a weak decompression, indicated Unit have to be referred to the Calabrian- by the decrease of celadonitic content in muscovite Peloritanian Arc. Therefore, like the other and by the absence of chloritoid and the presence of continental units of the arc, they would represent biotite in phyllites of the lower levels. It continues South-Apennine Internal Units, originating from a in the late D2 and in syn-D3 (second step), with an iso- continental block (Mesomediterranean Microplate; thermal decompression, starting in the upper levels at Guerrera et al. 1993) that separated different P < 0.6 GPa (within the pyrophyllite field), with the realms of the Tethys Ocean since the Jurassic. growth of chlorite + less phengitic white mica as the alteration products of carpholite, and in the lower Tellian Maghrebids levels at P < 0.8 GPa (within the kyanite stability field), with the development of chlorite + Verrucano-like Triassic metamorphic successions muscovite + opaque minerals after chloritoid. There- are up to now unknown in the Tellian Maghrebids. fore, subduction to considerable depths and sub- However, we consider that the Babors Units, sequent exhumation appears to have taken place for considered as Tellian Extemal Units back-thrust the rocks of the Lungro-Verbicaro Zone during over the Maghrebian Flysch Basin Units, have Miocene tectonism. some features that are worthy of analysis. The As for the Tuscan Metamorphic Units, the tecto- occurrence of (1) Triassic redbeds different from nometamorphic evolution outlined above may pose the typical Germano-Andalusian facies of the questions on the traditional attribution of the Tellian Extemal Units (Bourmouche et al. 1996), Lungro-Verbicaro and Coastal Chain Carbonate (2) Alpine metamorphism, and (3) a stratigraphic tectonic windows successions to the Adria- succession characterized by thick Camian evapor- Apulia continental margin and the consequent ites and Norian dolostones, Jurassic neritic and interpretation of these units as External South- pelagic limestones could put into question the attri- Appennine Units. According to Perrone (1996), the bution of the Babors Units to the Extemal Tellian Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

28 V. PERRONE ET AL.

BENI MZALA UNITS

TIZGARINE UNIT

BOQUETE D'ANJERA , ' i I I I I I v 1,, I UNIT ,,, , , 9 , ,

,. 9 ~ 9 9 9 9 9

- 400

i i i *." :,,,,r 9 9 .. 9 ., .f I .] '. i. I.I I .'. :.'...'.' .... "p .. 9 "....*. * - 300 **,...:.:...... *'~. l , i"'"9 * t d 9 9 t 0 m m 9 9 9.. **... - 200 ,o.', :~ o:o:qo ~ 9 9

- 100 -- --0m I~ Thick-bedded metalimestones Red and yellow metarenites (Upper Triassic) (Middle Triassic) --~ Dolostones and evaporites Red and violet metapelites (Upper Triassic) (Middle Triassic) ~ Thin-beddedmetalimestones Quartz-rich conglomerates (Middle Triassic) (Middle Triassic) Phyllites and metarenites ~ Quartzites (MiddleTriassic) (Palaeozoic)

Fig. 19. Stratigraphic columns of the Rifian Upper Sebtide Units (Federico Slices).

Units. Finally, according to Coutelle & Delteil main features can be summarized as follows: (1989), the stratigraphic succession of the Internal (1) the successions consist of only Middle-Upper Babors shows strong similarities to the Tuscan Triassic strata, unconformably lying on Middle(?) successions. Carboniferous metasedimentary rocks; (2) they start with some metres of coarse quartz-rich con- Rifian Maghrebids glomerates and are characterized mainly by violet, greenish, yellowish and silvery metapelites and In the Internal Rif, metamorphic successions metarenites with some conglomerate layers, fol- similar to the Tuscan Verrucano are present in the lowed by quartzites and thin-bedded metalimes- Upper Sebtide Units, known as Federico Slices. tones containing Middle-Triassic dasycladacean These units, underlying the Ghomaride and algae, Upper Triassic(?) evaporites and massive Dorsale Calcaire Nappes, crop out in two areas of dolostones, and eventually thick-bedded metali- the Northern Rif, west of Sebta (Beni Mzala mestones; (3) as in many Verrucano-type Apenni- window) and in a narrow belt parallel to the coast- nic and Betic successions, no rocks younger than line between Assifane and Oued Laou (Fig. 6). Triassic have been recognized; (4) the rocks have The successions of the Upper Sebtide Units, undergone HP/LT metamorphism, characterized which show similar lithostratigraphical sequences, by increasing pressure and temperature, from the are shown in Figure 19 (Zaghloul 1994). Their upper to the lower tectonic unit, with each unit Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

TRIASSIC REDBEDS IN WESTERN MEDITERRANEAN CHAINS 29

Fig. 20. P-Tpath of the Rifian Upper Sebtide Units (Federico Slices): dark shaded arrow indicates syncollisionalpeak stage; light shaded arrow indicates exhumation decompression stage. A, Tizgarine Unit; B, Boquete de Anjera; C, Upper Beni Mzala Unit (lower levels); D, Lower Beni Mzala Unit (lower levels). Minerals of the metamorphic reactions are as in Figure 15. Petrogenetic grid is modified after Oberh~insli et al. (1995). being characterized by its own peak pressure- Beni Mzala Unit indicates an early exhumation temperature conditions (Bouybaoubne 1993; Bouy- to 0.8 GPa, either isothermal or at slightly increas- baoubne et al. 1995; Goff6 et al. 1996). ing T. Further unloading with decreasing T corre- In particular, as regards the metamorphic evol- sponds to the crystallization of late paragonite, ution of the Federico Slices (Fig. 20), in the Tizgar- muscovite, chlorite, kaolinite and cookeite in both ine Unit, cookeite-pyrophyllite-phengite mineral the Lower Beni Mzala Unit and the Upper Beni assemblages indicate P = 0.1-0.5 GPa and Mzala Unit. T = 300 ~ In the Boquete de Anjera Unit, the The HP-LT metamorphism indicates an Alpine occurrence of sudoite + Mg-chlorite + phengite in subduction event and subsequent exhumation of the quartz veins, with chloritoid in the surrounding these units (Bouybaoubne et al. 1995; Golf6 et al. schists, suggests P close to 0.7 GPa and T = 300- 1996). 350 ~ In the Upper Beni Mzala Unit, Mg-carpho- lite relics in chloritoid-quartz or kyanite-quartz Betic Cordillera veins are typical of blueschist-facies conditions evolving from P = 0.8-1.0GPa and T= 380- In the Betic Cordillera (Fig. 8), successions showing 420 ~ to P = 1.2-1.5 GPa and T = 430-450 ~ lithological features, age, tectonosedimentary evol- In the Lower Beni Mzala Unit, Mg-carpholite ution and metamorphism similar to those of the relics in Mg-chloritoid + quartz veins, and talc + Apenninic Verrucano are widely present in the phengite assemblages in quartz + kyanite segre- units of the Alpujarride Complex, which underlies gations point to eclogite-facies conditions, extend- the Malaguide Complex (Delgado et al. 1981). ing from P = 1.2-1.5 GPa and T = 430-480 ~ These successions are especially well developed to P about 2.0 GPa and T = 550 ~ The retrograde in the Lower Alpujarride Units, but also in some P-T path is constrained only for the Beni Mzala Intermediate Alpujarride Units (Felix Unit from Units. The occurrence of tremolite + talc + Sierra de Gfidor, SE Spain; Martfn-Rojas 2004) phlogopite+chlorite assemblage in the Lower and in the Higher Alpujarride Units located close Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

30 V. PERRONE ET AL. to the outer border of the Internal Zones, from the Units, condensed pelagic sediments of Jurassic, Gibraltar Arc (Casares Slices, strictly equivalent to Cretaceous and Tertiary age, up to the early the Rifian Federico Slices) to the eastern Betic Cordil- Miocene, are also present above dated shallow lera (Sierra Espufia area), which show lithostrati- marine Rhaetian massive limestones (see Martfn- graphic and metamorphic features transitional to Algarra 2004, for a recent revision). those of the Malaguide Pseudoverrucano-like Triassic deposits (Sanz de Galdeano et al. 2000, 2001). Tectonometamorphic evolution. Many petrological studies, carried out on various units of the Alpuj~ir- Verrucano-like successions. Representative strati- ride Complex, showed HP/LT assemblages (Goff6 graphic successions of the Alpujarride Units are et al. 1989, 1996; Azafi6n et al. 1992, 1995, 1997, reported in Figure 21. Alpujarride Verrucano-like 1998; Azafi6n 1994; Azafi6n & Goff6 1997; successions lie on black schists attributed to Booth-Rea et al. 2002). Our new data, concerning the Palaeozoic and start with muscovite-rich in particular the Adra and Felix Units (Marffn light-coloured (from silvery grey to grey-green to Rojas 2004), enhance the previous knowledge. blue-violet), fine-grained micaschists, phyllites In the Salobrefia Unit (Fig. 22) a prograde blues- and quartzites, with abundant quartz veins stretched chist-facies metamorphic evolution has been recon- along the main Alpine foliation. They include structed (Azafi6n & Goff6 1997). It is marked by gypsum- and carbonate-bearing horizons dated as three assemblages: (1) Mg-carpholite + chlorite + Early-Mid-Triassic as well as basic subvolcanic chloritoid + quartz _ kyanite; (2) Mg-carpholite + and volcanic rocks, which are also present in the chlorite + kyanite § quartz; (3) kyanite § chlori- overlying Triassic carbonate successions (Delgado toid § chlorite. Sudoite occurs as an alteration of et al. 1981; Simon & Visscher 1983; Kozur et al. Mg-carpholite in assemblages (1) and (2), whereas 1985; Sanz de Galdeano 1997; Garcia-Tortosa phengite and paragonite are both main phases in 2002; Martfn-Rojas 2004). The metapelitic and the schists and late alteration products of carpholite quartzitic succession grades progressively upwards, and kyanite, in addition to chlorite, pyrophyllite or and laterally, to thick carbonate sequences, the cookeite. Margarite replaces chloritoid and very ensemble being more or less intensely recrystallized late kaolinite develops around kyanite and cookeite. as a result of the Alpine metamorphism. The reconstructed P-T conditions show that meta- The carbonate successions can be very thick in morphism evolves from 0.8 to 1.2 GPa and from several units (more than 2 km), especially in the 400 to 480 ~ Lower and Intermediate Alpujarrides, and always In The Adra Unit (Fig. 22), which, according to show mainly shallow marine Alpine Triassic Azafi6n et al. (1997) consists of a Palaeozoic base- facies and fossils. They are organized in two main ment and a Permian and/or Triassic cover, the transgressive-regressive cycles. The lower cycle HP/LT D l phase, related to thickening and conti- is transitional with the underlying phyllites and nental subduction, developed at P = 0.8 GPa and quartzites and is formed by Anisian massive to T = 430 ~ in the Fe-Mg-carpholite-bearing bedded, mainly shallow marine and sometimes Permo-Triassic schists and at P > 1.0 GPa and reefal (Braga & Martfn 1987a) dolostones and lime- T= 570 ~ in the kyanite-garnet schists of the stones, lower Ladinian hemipelagic marls and Palaeozoic basement. An almost isothermal cherty limestones, followed by a thick succession pressure decrease followed during the thinning of Ladinian bedded limestones with subordinate and associated vertical shortening (D 2 phase). lenticular decametric dolostone horizons, It was responsible for the $2 main foliation, frequently with zebra structures, which, toward marked by a prograde zoning from Permo-Triassic the upper part of the cycle (Ladinian-Carnian tran- schists (biotite § chloritoid) to garnet schists sition), contain important F-Pb-Zn (Ag) ore (biotite + garnet § staurolite) and sillimanite deposits. A regression on top of the mineralized schists (biotite § garnet + sillimanite) of the interval is marked by the presence of Carnian Palaeozoic basement. D 2 metamorphism occurred marls, clays and fine-grained sands with some dolo- at P < 0.65GPa in the whole unit and at stone and gypsum beds, followed by a thick succees- T = 420 ~ in the upper levels, and from 510 ~ sion (>1 km thick in many sites) of well-bedded to (garnet schists) to 700 ~ (sillimanite schists) in massive shallow marine to reefal dolostones the lower levels. A second thickening phase (D3 with Hauptdolomit facies and abundant fossils phase) was responsible for the $3 pressure-solution (benthic Foraminifera and dasycladacean algae; cleavage in the upper levels and for a crenulation e.g. Delgado et al. 1981; Braga & Martfn 1987b; cleavage in the lower levels. D3 phase occurred at Martin & Braga 1987) that allow them to be dated lower P-T conditions (P = 0.3 GPa; T from 500 as latest Carnian-Norian. No post-Triassic sedi- to 600 ~ ments are usually described in the Alpujarride An Alpine metamorphic evolution similar to that Complex but, in some northern Lower Alpujarride recognized in the Salobrefia and Adra Units occurs Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

TRIASSIC REDBEDS IN WESTERN MEDITERRANEAN CHAINS 31

Fig. 21. Stratigraphic columns for some Betic Alpujarride Units. Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

32 V. PERRONE ETAL.

Fig. 22. P-T path of the Betic Alpujarride Units: dark shaded arrow indicates syncollisional peak stage; light shaded arrow indicates exhumation decompression stage. A, Felix Unit Triassic upper levels; B, Felix Unit Triassic lower levels, Adra and Salobrefia Units upper levels. Minerals of the metamorphic reactions are as in Figure 15. Petrogenetic grid is modified after Oberh~insli et al. (1995). also in the Felix Unit (Fig. 22), which consists of a biotite). It is related to the end of the decompression Triassic cover and a Palaeozoic basement, the latter path and caused a continuous development of and- lacking the lowest levels (sillimanite-bearing alusite in the Palaeozoic basement. schists) occurring in the Adra Unit (Martfn Rojas Polystage HP/LT metamorphism has been 2004). The reconstructed metamorphic history testi- recognized also in other units of the Alpujarride fies to a prograde zoning increasing towards the base Complex, such as the Trevenque Unit (peak con- of the sequence. A first HP/LT stage, related to D1 ditions at P > 0.7-0.8 GPa and T 300-330 ~ thickening phase, occurred at P between 0.8 and marked by Fe-carpholite + chloritoid + chlorite + 1.0 GPa. T reached values <360 ~ in the highest aragonite assemblage; Goff6 et al. 1989), the levels of the Triassic phyllites (phengite + chlorite + Alcazar (= Escalate) Unit (P > 0.7-0.8 GPa, T carpholite? assemblage), between 360 and 420 ~ in around 450-500 ~ Mg-rich chloritoid + the lowest phyllite levels (phengite + chlorite + chlorite +kyanite +calcite assemblage; Goff~ chloritoid+ stilpnomelane or biotite) and 480- et al. 1989), the Escalate Unit (P between 0.7 500 ~ (phengite + chloritoid + biotite + garnet) in and 0.9GPa and T between 330 and 430~ the garnet schists of the Palaeozoic basement. Azafi6n & Goff~ 1997), and the Jubrique A second stage, related to the D2 isothermal and Benarrab~ Units (P around 0.8 GPa and decompression phase, was responsible for the $2 maximum T of 400 ~ in the upper levels and main foliation and developed at P < 0.8 GPa both P > 0.8 GPa and T < 450 ~ in the lower ones; throughout the Triassic phyllites (less phengitic Azafi6n et al. 1995). white mica, stilpnomelane and chloritoid destabili- The Alpine geodynamic evolution of Alpujarride zation) and in the Palaeozoic schists. A second Verrucano-like facies can be summarized as thickening D3 phase was responsible for the $3 clea- follows (Fig. 22): the HP/LT metamorphism vage, occurred at lower P-T conditions than $2 occurred at P between 0.7 and 1.2 GPa and T (according to zoning, white mica ___ chlorite + between 300-350 ~ and 420-480 ~ (first stage), Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

TRIASSIC REDBEDS IN WESTERN MEDITERRANEAN CHAINS 33

MLP/LT metamorphism developed at P between orogenic belt deriving from the deformation of the 0.6 and 0.2 GPa and T between 300 and 480 ~ Internal Domains was fragmented and the frag- (second stage), and LP/LT metamorphism took ments were dispersed around the Western Mediter- place at P < 0.2 GPa and T < 350 ~ In the Inter- ranean to form, today, independent and isolated mediate Alpujarride Complex, the HP/LT stage elements. The Triassic domain was characterized has been dated as latest Oligocene (25 Ma), by the deposition both of Pseudoverrucano lithofa- whereas the second stage has been dated as latest cies and of sedimentary precursors of the meta- Aquitanian-earliest Burdigalian (19Ma, Moni6 morphic Verrucano successions. However, the et al. 1991). Verrucano successions are characterized not only In conclusion, the Alpujarride Complex shows a by their original depositional features (similar to sedimentary and tectonometamorphic evolution those of Pseudoverrucano Triassic continental similar to that of the Verrucano-like successions redbeds) but also by their post-Triassic meta- in other Central-Western Mediterranean orogenic morphic evolution. This, being equivalent in the sectors, in particular to that of the Lungro- studied successions around the Western Mediterra- Verbicaro Unit of the Calabrian-Peloritanian nean, demonstrates their proximity to areas affected Arc, including (1) deposition of very thick by Tertiary subduction and Alpine orogenesis. The Anisian-Ladinian platform carbonates, (2) latest latter were responsible for transforming Triassic Oligocene-early Miocene underthrusting to very continental redbeds into carpholite-bearing, high- great depths, (3) HP/LT metamorphism and (4) sub- pressure-low-temperature metamorphic rocks. In sequent exhumation. short, it is necessary to clearly distinguish between the features associated with the post-depositional, Triassic and younger tectonic evolution, and the Discussion original depositional-palaeogeographical features of these rocks that formed during the Triassic and The Triassic (Pseudo-)Verrucano Domain: a subordinately during the early Jurassic. The latter palaeogeographical definition permit us to define a Triassic Verrucano-Pseudo- verrucano palaeogeographical domain, termed The comparative analysis and correlation of succes- hereafter the (Pseudo-)Verrucano Domain. sions marking the base of the Alpine cycle in the Triassic continental redbeds were also widely Western Mediterranean chains indicate that both present in the European Germanic Triassic, and in Pseudoverrucano-type deposits and its Verrucano the Iberian and North African Germano- metamorphic equivalent are not exclusive to the Andalusian Triassic facies belts, which were Northern Apennines: they are also recognizable in located close to large continental areas (from the tectonic units that originated from the Internal which the terrigenous clastic supply was derived). Domains of the South Apennine, Maghrebian and These, during later Tertiary orogenesis, constituted Betic Chains, and also in some units up to now the forelands to the Western Mediterranean Alpine attributed to the External Domains. It must be belts. In contrast, the Triassic (Pseudo-)Verrucano emphasized that the term Verrucano has been fre- Domain was palaeogeographically and palaeotecto- quently (and loosely) applied in these areas (in par- nically different from, and independent of, ticular, in the Betic Cordillera) to non-metamorphic these European-Iberian-African Germanic and Pseudoverrucano lithofacies in the same way as the Germano-Andalusian Triassic facies belts, from term is applied to Permian redbeds in the Alps, which it was completely isolated. Verrucano- whereas the metamorphic lithologies have been Pseudoverrucano successions, in fact, characterize usually named 'Permo-Weffenian', using an older a comparatively small area, which later formed Austroalpine-derived terminology (see Fallot the hinterland to the Western Mediterranean 1948, among many others). Alpine Belts. This hinterland, which since Mid- All the studied units can be joined together to Jurassic time was completely separated from the form a single Triassic palaeogeographical domain, Europe-Iberia, Africa and Adria-Apulia Plates to if the following aspects are considered: (1) there form a microcontinent in the Western Tethys are strong similarities between all the studied Trias- (Mesomediterranean Microplate; Guerrera et al. sic rock successions; (2) the Western Tethyan 1993; Bonardi et al. 2001; Michard et al. 2002), oceanic basins opened after the end of the Triassic; was completely destroyed during Alpine tectonic (3) the Late Cretaceous-Palaeogene-Early phases, forming the Internal Units of the Western Neogene geodynamic evolution was very complex Mediterranean Alpine Belts. but equivalent in all the studied areas, with different Therefore, the (Pseudo-)Verrucano Domain was phases of subduction, exhumation, thrusting and located around a small mountain area, from which subsequent orogenesis that affected all the Internal alluvial depositional systems provided siliciclastic Domains; (4) finally, during the Miocene, the supply to neighbouring nascent continental Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

34 V. PERRONE ET AL. sedimentary basins formed during Triassic tiffing. Cordillera and in the External Domains of the Petrographically, these clastic sediments were Southern Apennines and Sicily, as well as in the similar in the various studied areas. They reveal Betic Rondaide and Rifian External Dorsale Cal- the erosion of metamorphosed Palaeozoic succes- caire Units, whose lowest levels are late Carnian sions extensively intruded by felsic (tonalite, gran- in age. These latter have been also interpreted as a odiorite to granite) plutonic rocks; that is, rock part of the Sebtide-Alpujarride successions, associations very similar to those that crop out detached in correspondence to Carnian evaporites widely in the Calabrian-Peloritanian Arc and in and emplaced as 'frontal units' (Mart/n-Algarra the Kabylias. Strong chemical weathering of such 2004). In many places, all the above units are also rocks under tropical, hot and episodically humid associated with synsedimentary basaltic volcanism, climate with a prolonged dry season (BSh climate owing to the development of strongly subsiding according to the Krppen-Geiger classification) rift basins. Therefore, during the Mid-Triassic resulted in oxidation of iron and rubefaction of and, especially, the Late Triassic transgressions, soils and sediments (reddening), and caused illitiza- most continental areas of the (Pseudo-)Verrucano tion of silicate minerals and concentration of quartz Domain were invaded by the Alpine sea and trans- in thick soil profiles. These soils were later denuded formed to coastal to shallow-marine, carbonate to by fluvial erosion, producing relatively mature, evaporitic environments. quartz-rich red deposits. Further details can be In short, during the progressive development of added to this picture in the Betic Cordillera and the Triassic rift basins, emerged areas persisted in Rifian Maghrebids, where stratigraphic correlation the central part of the continental block that was reveals that Triassic Alpujarride and Sebtide otherwise covered by shallow-marine carbonate deposits of Verrucano-type metamorphic litho- platforms with Alpine facies. In the emerged facies were sedimentologically more distal and areas, crystalline rocks were eroded and provided closer to marine realms than Malaguide and terrigenous clastic deposits to surrounding conti- Ghomaride Pseudoven'ucano-type deposits nental rift basins of the (Pseudo-)Verrucano (Martfn-Algarra et al. 1995). Moreover, palaeocur- Domain. In our opinion, the same areas of high rent analysis clearly indicates that the terrigenous relief that provided terrigenous supply to the clastic deposits were derived from rapid erosion Betic-Rifian Verrucano-Pseudoverrucano basins of regions of high relief to the south and SE, and (or contiguous mountain areas located towards the to the east and NE of the present-day outcrops south and east of the former) also provided silicic- of the Malaguide and Ghomaride Reahns, respect- lastic sediments towards the south, SE and east, to ively, whereas in the other realms (Kabylias and feed the Pseudoverrucano-type deposits of the Calabrian-Peloritanian Arc) they were derived Kabylias and of the Calabrian-Peloritanian Arc form the north, NW and west. and, finally, towards the north and NE to form the The (Pseudo-)Verrucano Domain was already Northern Apenninic Verrucano sensu stricto and defined in Mid-Triassic times. Its differentiation Pseudoverrucano sensu stricto deposits. If the probably started in the Late Palaeozoic because, Permian-Triassic plate configuration is considered as pointed out by M. Durand Delga (in Baudelot (see, e.g. Ziegler 1988, 1993), it is clear that to et al. 1984), Upper Carboniferous-Permian the south and east of the Kabylian-Calabrian- clastic and volcanic successions, which are well Pelotitanian Psudoverrucano facies belt more developed in the neighbouring regions, are lacking distal, transitional and marine areas, characterized in the domain characterized by the studied by carbonate sedimentation, were widely present redbeds. This observation still can be accepted, (Fig. 23a-c). although in Tuscany recent studies pointed out the occurrence of Lower Triassic clastic deposits, Post-Triassic stratigraphic and geodynamic which constitute a sedimentary cycle interposed evolution between Palaeozoic terrains and the Middle Triassic Verrucano lithofacies (Cirilli et al. 2002; Lazzar- The palaeogeographically contiguous Verrucano otto et al. 2003). Locally, the (Pseudo-)Verrucano and Pseudoverrucano facies belts, already well continental redbeds changed progressively laterally characterized in the Mid-Triassic, show a similar and upwards to thick, Middle to Upper Triassic tectonosedimentary evolution from the Pliensba- marine carbonate deposits with typical Alpine chian onwards, during the opening of the lithofacies. These were deposited from at least the Neo-Tethys Ocean. This opening transformed early Anisian and, outwards of the future Alpine large continental crust areas, characterized by belt, laterally passed into Germano-Andalusian carbonate platform sedimentation, into pelagic facies belts. Such thick Alpine marine lithofacies basins within the complex, fault-controlled peri- are widely present in the Austroalpine Units Tethyan margins. During the Cenozoic collisional of the Alps, in the Alpujarride Units of the Betic events, in contrast, both facies belts underwent Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

TRIASSIC REDBEDS IN WESTERN MEDITERRANEAN CHAINS 35

different deformation history, which makes it necessary to distinguish between post-Triassic Verrucano and Pseudoverrucano sub-domains.

Pseudoverrucano Sub-domain. The oldest dated sediments recognized in the Pseudoverrucano Sub-domain are Mid-Triassic continental (fluvial and alluvial) redbeds dated with pollen in the Betic Cordillera and in the Rif (Simon & Kozur 1977; Miikel & Rondeel 1979; Baudelot et al. 1984; Mart/n-Algarra et al. 1995). Continental environments locally persisted until the Hettangian (Calabrian-Peloritanian Arc). Carbonate platform sedimentation covered these continental areas in the Sinemurian, but these shallow-marine deposits abruptly changed everywhere, from the Pliensba- chian to the Toarcian, into pelagic or turbidite sediments. Siliciclastic deposits testify to the pre- sence of emerged lands up to the Aalenian (Piraino Unit; Cecca et al. 2002), whereas mainly carbonate breccias and neptunian dykes Mid-Late Jurassic in age may be related to extensional tectonics associated with the opening of the Western Tethys Ocean. Pliensbachian to early Miocene facies zonation in the Betic-Rifian Mala- guide-Ghomaride belt reveals opening of the sedi- mentary environments towards areas located outwards of the internal domains; that is, towards the north and NW in the Betic Cordillera and towards the west and SW in the Rif. In the Kabylias and in the Calabrian-Peloritanian Arc the facies zonation also indicates more distal and deeper environments outwards of the internal domains, which, in this case, are located towards the south, SE and east. In Tuscany and the Calabrian-Peloritanian Arc, several stratigraphic successions end with Cretac- eous strata and, in Calabria, this evolution has been interpreted as an effect of Eo-Alpine tectonics (Bonardi et al. 2001). In contrast, other successions reach the late Oligocene-early Miocene, when they underwent deformation. In any case, the units containing the Pseudoverrucano lithofacies under- went deformation at shallow crustal levels and therefore they were not affected by Alpine metamorphism.

siliciclastic and evaporitic coastal plains (also continental basins in (b) and (c). Green: shallow-marine environments of Germanic (shadowed) and Alpine facies. Light blue: pelagic environments on continental crust (intraplatform basins and continental margins). Fig. 23. Ladinian (a), Norian (b) and Early Liassic (c) Red: volcanism. Eur, Europa Plate; Ib, Iberia Plate; Ad, palaeogeographical sketches of the westernmost Tethys Adria-Apulia Plate; Af, Africa Plate; CM, area (modified from Vera 2004). Grey: continents, MesomediterraneanContinent; DM, Malaguide Domain; erosion areas. Yellow: continental basins (including PI-AR, Alpujarride-Rondaide Platform; PS, South Pseudoverrucano-type environments). Orange: Iberian Palaeomargin; PR, Rondaide Palaeomargin. Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

36 V. PERRONE ETAL.

Verrucano Sub-domain. As mentioned above, the (pyrophyllite-phengite + chlorite-cookeite assem- Verrucano Sub-domain displays a more complex blage) are recorded. Triassic tectonosedimentary evolution, character- The exhumation-related second stage is marked ized by the development of locally thick Mid- by a retrograde greenschist- to sub-greenschist- Triassic carbonate platforms, calcareous breccias facies metamorphism at P < 0.6 GPa and, in most and basaltic volcanism, testifying to the onset instances, roughly constant T (isothermal decom- of an important early rift phase not only in conti- pression), mostly within the pyrophyllite field. nental but also in marine environments. This Rarely, decompression ends with cooling (third event is particularly clear in Tuscany, where an stage) to T < 300 ~ in the kaolinite stability field. intra-late Ladinian disconformity and subsequent In synthesis, the reconstructed metamorphic Carnian continental deposits mark the end of path indicates a geodynamic evolution marked by this early rifting phase before later Jurassic a high-pressure phase, implying subduction or col- rifting and subsequent break-up. Shallow-marine lision-related thickening of continental crust and carbonate sedimentation occurs again during underthrusting of Verrucano deposits to depths Carnian to Early Jurassic times with the depo- locally in excess of 50 kin, followed by a retro- sition of evaporites followed by platform dolomi- grade isothermal greenschist-facies metamorphism tic and calcareous deposits. Sedimentation associated with decompression. Occasionally, a continued with pelagic marly, carbonate and silic- late cooling phase records the final emplacement eous sediments, and locally turbidites, with small and exhumation of the studied units. changes to latest Oligocene-early Miocene time, An almost generalized d6collement along the when the Verrucano Sub-domain was involved Upper Triassic evaporites allowed the overlying in continental collision and thick synorogenic sili- Upper Triassic-lower Miocene successions to ciclastic turbidite successions started to accumu- detach from their substrata. As a result, many late within the Apennine foreland basin system units deriving from the Verrucano Sub-domain are and in the Maghrebian and Betic Flysch Troughs. formed only by Triassic and older strata. During the Palaeogene to Miocene convergence and collisional events, the units originating from Concluding remarks the Verrucano Sub-domain underwent polyphase deformation and metamorphism, indicating under- The distinction between Verrucano and Pseudoverru- thrusting at significant depths (involving continen- cano successions, first evidenced in the Triassic suc- tal subduction in most of the cases) and later cessions of the Northern Apennines, has a regional exhumation. The metamorphic evolution of Verru- importance at the scale of the Western Mediterranean, cano-like facies is marked by several steps in the because successions similar to the Verrucano and P-Tpath. For units such as the Upper Beni Mzala Pseudoverrucano are recognizable in all the Internal (Upper Sebtides, Morocco), Escalate, Salobrefia, Domains of the Betic, Maghrebian and Apenninic Adra, Felix (Alpujarride Spain), Monticiano- Chains. A different palaeogeographical and geody- Roccastrada (Northern Apennine), Lungro-Verbi- namic evolution is documented for Verrucano- caro (Calabrian-Peloritanian Arc), syn-conver- and Pseudoverrucano-bearing successions from the gence high-pressure peak conditions (first stage) Triassic to the beginning of the deformation leading reached P between 0.8 and 1.8 GPa with T to the building of the orogens. The differences between 300 and 430 ~ within the pyrophyllite were enhanced during the Cenozoic compressional or kyanite stability field (carpholite + chlorite § tectonics, when Verrucano- and Pseudoverrucano- pyrophyllite+chloritoid assemblage) typical of bearing successions experienced different blueschist-facies metamorphism. Otherwise the deformation histories. metamorphic peak reached T> 430 ~ (within However, the terms Verrucano and Pseudoverru- the Mg-chloritoid + kyanite stability field), as in cano can be correctly used to indicate the Triassic the Massa Unit (Northern Apennines), and redbeds of the Internal Domains of the Western maximum pressures reached values in the range of Mediterranean Chains, because these redbeds have 1.5-2.0Gpa, with T between 380 and 450 ~ the same age and meaning as those of the Tuscan (within the chloritoid+kyanite stability field; area where the terms were first defined. after Mg-carpholite development), typical of eclo- The similar sedimentary and tectonic evolution, gite-facies metamorphism, as in the Lower Beni unravelled for the units bearing Verrucano- and Mzala Unit (Upper Sebtides, Morocco). Pseudoverrucano-like successions in all the Alpine Locally, peak conditions were lower, such as Chains of the Western Mediterranean orogen, in the Tizgarine (Upper Sebtide, Morocco) and suggests a single Mesozoic palaeogeographical Ali-Montagnareale Units (Calabrian-Peloritanian domain for their original location, before the onset Arc), where P < 0.5 GPa and T = 300-360 ~ of convergence-related deformation. The basement Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

TRIASSIC REDBEDS IN WESTERN MEDITERRANEAN CHAINS 37 of this domain was a block of pre-Late Carbonifer- subduction to depths developing pressures of ous-Permian? continental crust that started to be 0.8-1.6 GPa for units referable to the Adria-Apulia detached from Pangaea after having been deformed fold-thrust belt. A viable alternative is represented during the Variscan Orogeny. This Mesomediterra- by the possibility that originally these units also nean Block was the Triassic precursor of the were located on the same palaeogeographical Jurassic-early Miocene Mesomediterranean Micro- element as the Sebtide and Alpujarride Units of plate, which, owing to the Jurassic-Cretaceous the Gibraltar Arc; that is, the Mesomediterranean opening of Neo-Tethys, separated the northern Pie- Microplate (Guerrera et al. 1993). Palaeogeographi- montese-Ligurian-Nevadofilabride Ocean from cal sketches are shown in Figure 23a-c. Finally, if the eastern and southern (Lucanian-Maghrebian) the Verrucano- and Pseudoverrucano-bearing succes- oceanic branch of Tethys (Martfn-Algarra 1987; sions are characteristic of the Mesomediterranean Guerrera et al. 1993; Perrone 1996; Bonardi et al. Microplate, some questions arise also for the Alps 2001; de Capoa et al. 2002; Michard et al. 2002). as regards the palaeogeographical location of the The Triassic Mesomediterranean Block had a Verrucano-bearing Pennidic and Austroalpine units central erosional mountain area (Mesomediterra- for which the term Verrucano is correctly used. nean Microcontinent), which provided terrigenous In conclusion, Verrucano and Pseudoverrucano sediments to surrounding intracontinental rift successions developed during the continental basins that formed the (Pseudo-)Verrucano rifting stage that led to the complete break-up and Domain. These continental basins with redbeds lat- disintegration of Pangaea. They were probably erally evolved to deeper zones in which marine located along the margins of a minor continental sediments were deposited from at least Mid- block interposed between the Europe, Africa and Triassic time. After having been deeply eroded Adria-Apulia Plates, which later, in Jurassic time, during the Triassic, the former mountain areas formed the Mesomediterranean Microplate. were transformed in a peneplaned continental area Remnants of this microplate occur exclusively in the of low relief, whereas the formerly continental internal tectonostratigraphic units of the Western (inner) and marine (outer) sedimentation areas Mediterranean orogenic system. They have been respectively evolved, from the beginning of the Jur- interpreted as originating from deformation and col- assic, to proximal and distal, outward deepening lision of the microplate with the Iberian, African continental margins dominated by carbonate and Adriatic-Apulian foreland regions. neritic to hemipelagic sedimentation. From the Based on the available data, it can be envisaged Late Cretaceous to the early Miocene, the Mesome- that the post-Triassic Mesomediterranean Micro- diterranean Microplate acted as the hinterland of the plate started to differentiate as a continental crust Western Mediterranean Alpine Belts, forming the block tectonically detached from the neighbouring overriding plate above subduction zones. This hin- domains (Sardinia-Corsica Block, Iberia, Africa, terland was completely destroyed during the Adria-Apulia) from the Mid-Triassic, because its Alpine tectogenetic phases, forming the Internal boundaries seem to coincide with those of the Units of the Western Mediterranean orogenic belt. basins in which Vermcano and Pseudoverrucano Finally, during late and post-orogenic extensional successions were deposited. The beginning of the tectonics after Miocene subduction, the formerly differentiation of the continental crust block that unique orogenic belt was disintegrated owing to was the precursor of the Mesomediterranean Micro- the Neogene opening of the Algerian-Balearic- plate and its detachment from Pangaea was prob- Provencal and Tyrrhenian Basins of the Western ably even earlier than the Mid-Triassic, as all the Mediterranean (Guerrera et al. 1993). domains located on it (excluding the Tuscan In the light of the proposed model, intriguing Domain) are characterized by the absence of palaeogeographical problems arise, because a Upper Carboniferous-Permian sedimentary and similar tectonosedimentary evolution seems to volcanic terrains. These latter terrains, however, characterize both (1) units considered to belong to are well developed in the Moroccan Atlas, Iberia, the Austroalpine nappe system (the Betic-Rifian Pyrenees, Languedoc, Provence, Sardinia and units derived from the Verrucano Sub-domain; Corsica: all these areas were external to the Wildi 1983; Martfn-Algarra 1987; Chalouan & Mesomediterranean Microplate and only subordi- Michard 1990, 2004; Michard et al. 2002), and nately implicated in the Alpine sedimentary evol- (2) units referred to the Adria-Apulia fold-thrust ution and the subsequent orogenesis. belt (Tuscan Metamorphic Units in the Northern Apennines and Lungro-Verbicaro Unit in the This research has been carried out within the MIUR- Calabrian -Peloritanian Arc). COFIN Project 2001.04.5835 'Eth e caratteri dei depositi As regards the Tuscan Metamorphic and Lungro- tipo Verrucano dall'Appennino Settentrionale alle Cordi- Verbicaro Units, it may be difficult to envisage gliere Betiche: implicazioni per l'evoluzione Downloaded from http://sp.lyellcollection.org/ by guest on September 27, 2021

38 V. PERRONE ET AL. paleogeografica e strutturale delle Catene Alpine del Med- BONARDI, G., PERRONE, V. • ZUPPETTA, A. 1974. iterraneo Centro-occidentale'(support to V. Perrone, Uni- I rapporti tra 'filladi', 'metabasiti' e 'scisti versity of Urbino). Financial support from MIUR-COFIN micacei' nell'area tra Paola e Rose (Calabria). Bol- Project 2002 (to F. A. Decandia, University of Siena) and lettino della Societh Geologica Italiana, 93, DGI-MEC Research project CGL 2005-03887 and from 245-276. Research Group no. 164 (4089) to A. Martfn-Algarra is BONARDI, G., GIUNTA, G., LIGUORI, V., PERRONE, V., also acknowledged. The authors are indebted to Russo, M. t~ ZUPPETTA, A. 1976. Schema geolo- G. Cassinis and S. Yanev for their constructive reviews, gico dei Monti Peloritani. Bollettino della Societ~ useful comments and suggestions. Geologica Italiana, 95, 49-74. BONARDI, G., CAVAZZA, W., PERRONE, V. & ROSSI, S. 2001. Calabria-Peloritani Terrane and Northern Ionian Sea. In: VAI, G. 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40 V. PERRONE ETAL.

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