J. geol. Soc. London, Vol. 141, 1984, pp. 137-145, 5 figs. Printed in Northern Ireland.

Remnants of the Hercynian orogen along the ‘Calabrian-Peloritan arc’, southern : a review

P. Atzori, P. Ferla, A. Paglionico, G. Piccarreta & A. Rottura

SUMMARY: Remnants of the Hercynian orogen, disturbed by Alpine tectonics, occur widely alongthe ‘Calabrian-Peloritan arc’. Indications of former oceanic conditions, for example Palaeozoic ophiolites and original deep water sediments, are lacking. Metamorphism developed under intermediate to low pressure conditions; the post-metamorphic plutonism appears to be morecompatible with intracontinental orogenic processes than with an active continental margin. The possible evolution of this segment of the Hercynian orogen is discussed.

The ‘Calabrian-Peloritan arc’ is a complex structure, morphism in orderto understand the significance of made up of Palaeozoic. Mesozoic and Recent terrains Palaeozoicelements occurring along the Calabrian- which connect the NW-SE trending Apennines with Peloritanarc. Attention will befocused on the the E-W Maghrebide chain of (Fig. 1). The arc Hercynian magmatic and metamorphic events. results from the progressive bending and disruption of a previous continent-continent collisional belt (Scan- Pre-Hercynian events done1983). Current opinions are that the structure represents, either in total or in part (northern sector), A poly-metamorphic,pre-Alpine evolution has been a fragmenta of theCretaceous-Palaeogene Alpine suggested by someauthors for some tectonic units chain,made up of Pennineand Austro-alpine ele- cropping out along the Calabrian-Peloritan arc. The ments thrust on the Apennines in Early Miocene time poly-metamorphicinterpretation has been based on (e.g.Haccard etal. 1972;Scandone etal. 1974; mineralassemblages and textural features which Alvarez 1976; Amodio Morelli et al. 1976; Bonardi & suggestdifferent metamorphic imprints (e.g. Ferla Giunta1982; Zanettin Lorenzoni 1982; Scandone 1974; AmodioMorelli etal. 1976;Dubois 1976; 1983).There is noagreement, however, about the Paglionico & Piccarreta1978; Zanettin Lorenzoni origin of the arc (e.g. Amodio Morelli et al. 1976 and 1980).Unfortunately, there are no confirming references therein; Scandone 1979; Zanettin Lorenzo- geochronological data. Only one zircon age of 450 Ma ni1982), or onthe palaeogeography and structural (Schenk 1980, 1981) has been determined for granulite organization of some units. It has also been debated facies metabasites of the Polia-Copanello Unit (Serre, whether or not a Hercynianchain occurs in the Calabria),which is considered,according tothe Calabrian-Peloritanarc (e.g. Lorenzoni & Zanettin geophysicalcrustal models (Schwarz 1978; Schutte Lorenzoni1979; Bonardi et al. 1976,1980; Zanettin 1978),to be a fragment of Palaeozoiclower crust Lorenzoni 1982). (Schenk1980, 1981). This age was interpreted by ThePalaeozoic rocks cropping out along the arc Schenk(1980) as a minimum age for the magmatic consist of meta-sedimentary and meta-igneous litholo- crystallization of theprotolith. He also proposed a gies,ranging from low to very high metamorphic Caledonianmetamorphism prior to theHercynian gradegranuliteto(up facies) andgranitic- imprint(Schenk 1981). Besides the pre-Hercynian granodioritic plutonics with subordinate tonalites (e.g. metabasitesoccurring in the Polia-Copanello Unit, AmodioMorelli et al. 1976;Atzori etal. 19826; othermeta-igneous rocks affected by theHercynian D’Amico etal. 1982; Gurrieri etal. 1982).Nappe metamorphism,found along the Calabrian-Peloritan structures of Hercynianage have been described in arc,are augen-gneiss, tonalitic gneiss and amphibo- these terrains (e.g. Colonna etal. 1973; Atzori etal. lites,which might indicate pre-Hercynian magmatic 1977;Gurrieri etal. 1978;Lorenzoni & Zanettin activity. The meta-igneous rocks analysed so far range Lorenzoni 1979; Gurrieri et al. 1982), similar to those frombasic to acidic composition, comparable with generally occurring elsewhere in the European Hercy- those of magmaticproducts at modern converging nian orogen (e.g. Carmignani et al. 1978, 1980; Zwart plates(Atzori et al. 1982b).However, acomplete & Dornsiepen 1978; Weber 1981; Vai et al. 1982). The range of theserocks has not yet been analysed. Hercynian structural arrangement was greatly affected Fragments of maficlayered meta-gabbros, originally by theAlpine tectonics, which gave rise to complex intrudedinto a supra-crustal sequence of granulite nappestructures which obscure the Hercynian struc- faciesmeta-sediments plus meta-volcanics (Dubois ture. 1976; Moresi et al. 1978; Paglionico & Piccarreta 1978; The aim of this work is to synthesize the available Maccarrone et al. 1983),occur in the north-western data concerning the Palaeozoic magmatism and meta- Serre (Southern Calabria). They display calc-alkaline

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0 AEOLIANISLANDS 0

FIG. 1. Location of the Calabrian-Peloritan arc: (1) Sedimentary terrain; (2) metamorphic terrain (pre-Alpine and Alpine) and sedimentary cover of the Stilo Unit; (3) meso-aluminous plutonites; (4) per-aluminous plutonites. featuresand overall similarities with the‘Main Peloritan Range (i.e. - unit: Bonardi et Gabbro’ of the layered complex of the Ivrea zone in al. 1976;Southern Peloritan complex: Ferla 1974). thewestern Alps (Garuti et al. 1980).Since the Various sills and dykes with minor lavas and hyaloclas- layeredmeta-gabbroic rocks experienced Hercynian tites,contemporaneous with sedimentation of the metamorphism (Paglionico & Piccarreta 1978; Moresi tentaculitid-bearing limestones (Ferla 1978) of Middle et al. 1978; Schenk 1980, 1981), their age of emplace- Devonian age, display basic alkaline features compa- ment may be Hercynian or older. rableto ‘intraplate’ volcanics in extensional settings (Figs 2, 3; cf. Ferla 1978). The activity which followed Hercynian Magmatism unfortunately lacks any age data. A minimum age of LowerCarboniferous can beinferred, asthese Some Hercynian magmatic phases are recorded in the meta-volcanics,which range from basalts to dacites, Calabrian-Peloritan arc. The earliest phase preceded wereaffected by Hercynianmetamorphism. The theHercynian metamorphism and the latest one eruptionmay have been syn-orogenic in view of the followedit. The oldest pre-metamorphic magmatic association with graywackes and pelites. The chemistry activityhas been recognized so faronly inthe of the meta-volcanics is comparable with the modern

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0.1

0.05

,-1- -. I I 0.01 t 0 000 0 Q 08 ope, 00 80 0.005 @,P I I 101 I SUB-ALKALINE ' I ALKALI I BASALT BASALT I l1' 11 l I1 II I Nb/Y I l I* Oll 0.5 1.0 5.0 10.0

FIG. 2. Zr/(Ti02 X 10') vs. NbiY plot (Winchester & Floyd 1976) relative to Hercynian meta-igneous rocks from Peloritani mountains. Circles. meta-volcanites (n = 35) associated with tentaculitid bearing limestones (Ferla 1978): dots, meta-igneous rocks (n = 81) associatedwith the overlying meta-psammites and meta-pelites (Atzori et al. 19824.

orogenicextrusives (Figs 2, 3). In particular.these intrusions. Dykes of aplites. pegmatites and porphyries rocks display Zr values close to those of many modern cut the plutonics. The plutons were intruded into low- to active margin extrusives (Jakes & White 1972; Pearce medium-grade to high-grade metamorphics, generally C? Norry 1979), reaching contents as high as 300ppm at highcrustal levels. The intrusions cut across the in dacites.in Locally occurring meta-volcanics of regional structures discordantly in contrast with Pitch- rhyodaciticto rhyolitic composition have been inter- er's scheme (1979, p. 653) relative to the characteris- preted as products of localanatexis related to rising tics of the Hercynian orogen. The plutonics belong to calc-alkalinemagmas (Ferla 1978; Ferla & Azzaro twoseparate suites (e.g. Paglionico & Rottura1979; 1978;Atzori & Ferla1979). Insome Calabrian D'Amico et al. 1982):a meso-aluminous suite and a tectonic units (e.g. Bagni Unit and Longobucco Unit) per-aluminous suite (Fig. 4), the latter forming smaller composed of low-grademetamorphic rocks, dacitic, intrusions (cf. Lorenzoni et al. 1979;D'Amico et al. rhyodaciticand minor andesitic meta-volcanics (Gur- 1982; Del Moro et al. 1982). The meso-aluminous suite rieri et al. 1978;Ferla & Azzaro1978; Colonna & covers a surface of about 1700 km2, forming composite Simone1978; Colonna et al. 1982)are interbedded bodies with multiple intrusions, with meta-aluminous withmeta-arenites and meta-pelites and seem to be toper-aluminous composition (Fig. 4). characterized chemicallycomparable to those cropping out in the by frequent, possibly primary, muscovite and scarcity Peloritani area. The post-metamorphic magmatism is or absence of hornblende;biotite is theusual of Permo-Carboniferousage, from 295 f 2*Ma to ferromagnesian mineral (Crisci et al. 1980; Lorenzoni 270 f 5 Ma based on RbiSr whole rock and minerals et al. 1979; Gurrieri et al. 1982). The commonest rock ages and also U-Pb zircon ages according to Borsi & typesare granodiorites (70%) followed by tonalites Dubois (1968). Borsi et al. (1976), B. Wieland (pers. (20%) and a few granites (10%), all of which display comm. 1979), Schenk (1980) and Del Moroetal. (1982). calc-alkalineaffinities (Crisci et al. 1980),with re- Thismagmatic activity produced widespread granitic lativelyhigh K20/Na20ratios (also intonalites, K20/Na20- 1, unpublished data). The per-aluminous rocks form smaller intrusions, up to about 150 km2, at most, with monzo-granitic to leuco-granodioritic com- * Recalculated using AX7Rb= 1.42 X 10-" y-' positionsand crop out over about 400 km' (Fig.1).

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/ I I I , Zr 10 30 50 Y. 3

FIG. 3. Zr-Tii100-Y X 3 plot (Pearce &k Cann 1973)relative to Hercynian meta-igneous rocksfrom Peloritani Mountains. Dashed arearepresents field of meta-igneous rocks (n = 31) associatedwith meta-psammites and meta-pelites; spotted area encloses meta-volcanites (n = 26) associated with tentaculitid bearing limestones (Ferla 1978).

They locallyintrude the meso-aluminous plutonic suites. In particular, the per-aluminous suite matches rocksand contain primary muscovite together with the S-type granites (Chappell & White, 1974), whereas sillimanite (fibrolite) and sometimes cordierite, andalu- the meso-aluminous oneis ambiguous in this classifica- siteand garnet (e.g. D’Amico et al. 1982).The tion. The two granitic suites are likely to have been textural,mineralogical and geochemical features, as derivedfrom partial melting of differentcrustal wellas the available initial SrX7/Srx6 isotopic data on materials (D’Amico et al. 1982). The meso-aluminous meso-aluminous(0.710-0711 calculated by Schenk suite requires further investigation. The experimental (1980)for tonalites) and per-aluminous rocks (0.710 results in particular (Wyllie 1977) point to a possible according to Wieland (pers. comm. 1979) and Moro Del mantle involvement via thermal input andior magma et al. 1982), point to a crustal anatectic origin for both ascentinthe formation of thetonalites. Both meso-aluminousand per-aluminous Hercynian pluto- nics showsome degree of mineralization.Sulphide mineralization is in the form of molybdenite, sphaler- 20 ite,galena, chalcopyrite, pyrrhotite, arsenopyrite, all Mesoalurninous occurring with subordinate barite, fluorite or uranium (Bonardi etal. 1982; S. Lorenzonipers. comm.). In -UI 15 particular,molybdenite and chalcopyrite are mainly a associatedwiththemeso-aluminous granitoids. E According to Bonardi et al. (1982), this mineralization v) - 10 mightbe considered to be aHercynian porphyry 0 coppermolybdenum ‘system’, which Pitcher (1979) L na, consideredmore typical of I-granitesthan of S- E 35 granites.According to Wallace etal. (1978),the Z ‘porphyrymolybdenum’ systems might be associated withmagmas generated by ‘hot-spots’in continental crust.On the other hand, the MO-W mineralization 0.7 1.0 1.3 1.6 occurs in the S-type granites of the Bohemian Massif A’203/iCa0+Na,0+K~0) (Sattran1982). This mineralization of theCalabrian FIG. 4. Histogram of AI,O,/(Na,O + K20+CaO) granitoidsdoes not seem to conflict with a possible molecular ratio for the per-aluminous and meso- crustalgenesis. Traces of magmatism.following the aluminous granitoids of Calabrian Peloritan arc. plutonism, are present along the Calabrian Peloritan Data on meso-aluminous granitoids are relative to chainin different tectonic units (e.g. Stilo, Monte the Serre area only (from D’Amico et al. 1982). Gariglione, Longobucco Units and Aspromonte nappe

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auctorum)and occur as porphyry and felsite dykes, facies types and is made up of meta-sedimentary and withgranodioritic to granitic compositions and high meta-igneous lithologies. Some units experienced only K20/Na20ratios (De Fino & La Volpe 1970; theHercynian metamorphism but others were sub- et al. 1974;Borsi et al. 1976) in boththe meso- jected to a more complex history. The nature of the aluminousand in the per-aluminous granitic rocks. Hercynianmetamorphism, including geothermal gra- This magmatism is considered to be late Hercynian in dients and deformations, can be inferred from anchi- age, but the only age date is of 236 Ma (Rb-Sr age on metamorphictogreenschist-facies rocks, some of biotitefrom a porphyritic dyke of theStilo Unit in whichare definitely Hercynian in age and others Borsi et al. 1976). Pebbles ranging in composition from probably Hercynian, which crop out widely in Calab- andesiteto dacite, with calc-alkaline to K-andesitic ria (Stilo Unit pro parte, Bocchigliero Unit) and Sicily features,are common in the Lower Miocene con- (Longi-TaorminaUnit; Bonardi et al. 1982;southern glomerates of thePeloritani Mountains and central Peloritan Complex: Ferla 1974). They form sequences Sicily (Ferla & Alaimo 1976). Unfortunately, only one of phyllites and meta-arenites with local intercalations whole rock K-Ar date is available, 200 Ma. More data of tentaculitid-bearingmeta-limestones and of meta- are clearly needed, but these products might represent igneous rocks. Structural analyses of Hercynian meta- post-orogenicmagmatism with the pebbles derived morphicsare scarce. Pezzino (1982) has pointed out from complete erosion of a tectonic unit high in the three phases of folding with variably-trending axes in CalabrianPeloritan chain (e.g. Ferla 1978). This the Peloritani Range. The first phase produced open magmatismcould berelated tosimilar Permian isoclinal folds with an axial-plane foliation; the second activity in other segments of the European Hercynian phase folded SI and developed a crenulation-cleavage; orogen:for example, the southern Alps, Sardinia, thethird one produced centimetric- to metric-scale southernFrance and southwestern Germany (e.g. noncylindricfolds of similarand chevron type. with Ghezzo et al. 1979; D’Amico et al. 1980; Schleicher & axial plane foliation. The blastic events in these rock Lippolt 1981). typeswere essentially syn-kinematic and took place, according to Atzori & Ferla (1979). under conditions of T-350°Cand P>2 kbar,as deduced from the Features of the Hercynian occurrence of paragonite plus quartz or pyrophyllite in metamorphism meta-pelites.Additional information can be inferred from the celadonite content in muscovite from meta- TheCalabrian-Peloritan metamorphic belt includes pelites(Velde 1965). Under certain specified condi- rocksranging from anchi-metamorphic to granulite- tions, the bo-values of muscovite are proportional to

MINERALS SYNKINEM. CRYST. POSTKINEM. CRYST.

quartz

plagioclase An 15

white mica

chlorite

biotite

garnet

chloritoid

staurolite

cordierite

FIG. 5. Synopsis of mineral assemblage and of deformation-crystallizationrelationships in the meta-pelites (Peloritani Mountains, Sicily) after Pezzino (1982).

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theceladonite content (e.g. Guidotti &L Sassi1981). neitherPalaeozoic ophiolites nor original sedi- The muscovites from meta-pelites of the Calabria and ments of deep water type have been found. Peloritani Mountains di2play bo values mostly ranging (2) The metamorphism displays syn-kinematic effects from8.995 A to 9.005 A(Dietrich etal. 1976;Ferla of intermediatePIT character, followed by later 1978;Colonna etal. 1979; DiPierro et a/. 198q; regional effects of relatively lower PIT type. Pezzino1982), with a mean value around 9.000 A (3) The Devonian-Carboniferous (?) volcanism seems which, according to Guidotti & Sassi (1981), points to to be indicative of diverse geodynamic conditions, agradient of about34"C/km. This gradient is quite from'intraplate' to'orogenic'. The 'orogenic' similar to that inferred for the Hercynian metamorph- volcanicsare geochemically similar to those of ism of theAustrides (Guidotti & Sassi1981). active continental margins. Radiometricdata on blastic events and deformation (4)The per-aluminous granitoids are clearly derived phasesare lacking. Piccarreta etal. (1983) believed from crustal anatexis. The meso-aluminous pluto- thatthe main Hercynian deformation phases took nicsdisplay calc-alkaline affinities with overall place from Narnurianto Westphalian. The higher-grade high K20/Na20 ratios similar to the plutonics of rocksare various kinds of phyllites,mica-schists, the European Hercynian massifs (cf. D'Amico & para-gneisses,augen-gneisses, marbles and basic to Siena 1977; Ghezzo & Orsini 1982; Autran etal. acidic meta-volcanics, ranging from greenschist-facies 1980 cited in Ghezzo & Orsini op. cit.), different to amphibolite-facies grade. Several authors (D'Amico fromthe batholiths of theactive continental et al. 1972; Ferla 1974; Maccarrone et al. 1975; Atzori margins in the western USA and Andean regions. et al. 1976; Lorenzoni & Zanettin Lorenzoni 1979; De Also the granitoids do not show the well-defined Vivo et al. 1980; Pezzino & Puglisi 1980; Pezzino 1982) space-timerelationship between S- andI-types have pointed out both Hercynian syn-kinematic blastic that is a characteristic at converging plate bound- effects, connected with the deformational phases, and aries(Beckinsale 1979; Mitchell & Beckinsale alsolate- post-kinematicto features. The syn- 1982). The post-metamorphic plutonism therefore kinematic metamorphic phases range from greenschist showsfeatures quite similar tothose of the to amphibolite facies (muscovite + fibrolite or, more Hercynianplutonism in Europe, which seems to rarely,kyanite subfacies) and took place generally morebecompatible withintra-continental underconditions of intermediatePIT (gradient of orogenicprocesses (e.g. Zwart & Dornsiepen about 3&35"C/km). The late- to post-kinematic effects 1978;Pitcher 1979; Michard Vitrac et al. 1980; generallytook place under amphibolite-facies condi- D'Amico et a/. 1982) than with the active margins. tions of lower PIT and are characterized by plentiful (S) The plutonics considered here were intruded into crystallization of biotite,staurolite, andalusite and an edifice built up of several superimposed nappes sometimescordierite, K-feldspar and fibrolite in of metamorphics of different grade. meta-pelitesand meta-graywackes. The formation of (6) Volcanic activity with calc-alkaline to K-andesitic andalusitefrom sillimanite has been also observed, affinities probably took place in Permian times. even if rarely (Maccarrone et al. 1975). In some rocks Summarizing, we are dealing with a continental area themesostasis keeps its syn-kinematic phyllitic tex- affected by riftingand formation of ensialicbasins ture,in spite of theabundant crystallization of the during Devonian times, characterized by calc-alkaline aboveminerals. The late to post-kinematic phases magmatism, crustal shortening and, finally, plutonism wereprograde in some structural units (Fig. 5) and mainlyrelated to crustal anatexis. This could be isograde,or even retrograde. in others. The rela- consistent with: tionshipsbetween deformation phases and blastic (1)an active continental margin regime, assuming events are still poorly known in the polymetamorphic that the area represents a relatively external part granulite-facies rocks of the Calabrian-Peloritan arc. of a former palaeo-European continental margin, TheHercynian metamorphism of theCalabrian- far removed from the trench, as suggested by one Peloritanarc was therefore polyphase and, in some of the authors (Ferla 1974, 1978; Ferla et al. 1982); rock-types, plurifacial also. These features are similar or tothose of other segments of theEuropean Hercy- (2)an ensialic development, with some mantle in- nides (e.g. Vai et a/. 1982; Franceschelli er al. 1982). volvementtoexplain the nature of thepre- orogenic and syn-orogenic volcanic products and, possibly. the generation of tonalites, as suggested Some features of the by the other authors, since the available data are Hercynian orogeny well in agreementwith the model proposed for othersegments of theEuropean Mediterranean Anygeodynamic interpretation of theHercynian Hercynianorogen (e.g. Nicolas 1972; Vai 1979; orogenin this sector must account for the following Ghezzo et a/. 1980;Michard Vitrac er al. 1980; points: Behr etal. 1980;Rau & Tongiorgi1981; Weber (1) There is no geological evidence of oceanic rocks; 1981; Carmignani et al. 1981; Vai et a/. 1982).

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Furtherdata are necessary to test the models magmatism in the European Hercynian orogen sug- suggested.Under any circumstances the post- gests that Pitcher’s scheme ought to be revised. orogenic, high-K volcanic activity of probable Permian age, which occurs as dykes in granites or pebbles in conglomeratesin the Calabrian-Peloritan area, seems ACKNOWLEDGMENTS, We thank G, B, Vai for the helpful to contrastto with scheme (1979, P. 653) discussion and referees for constructive criticism, The work relativeto the magmatic activities Occurring in the was supported by the Italian C.N.R. and is related to the Hercynian orogen. The widespread occurrence of thisI.G.C.P. No. 5. References ALVAREZ,W. 1976. A former continuation of the Alps. Bull. CIAMPO.G. 1980. Osservazioni sull’evoluzione dell’arco geol. Soc. Am. 87, 891-6. calabro-peloritano ne1 Miocene inferiore: La formazione AMODIOMORELLI, L., BONARDI, G., COLONNA, V.,DIET- di Stilo-Capo d’Orlando. Boll. Soc. geol. Ital. 89, 365-93. 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Received 27 January 1983; revised typescript received 25 July 1983. P. ATZORI, Dipartimentodi Scienze della Terra, Universita di Catania, Italy. P.FERLA, Istituto di Mineralogia, Petrografia e Geochimica, Universitadi , Italy. A. PAGLIONICO& G. PICCARRETA,Istituto diMineralogia e Petrografia, Universith di Bari, Piazza Umberto I, 70121 Bari, Italy. A. ROTTURA, Istitutodi Mineralogia e Petrografia, UniversitA di Bologna, Italy.

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