Lithos 123 (2011) 218–224

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Geodynamic control on orogenic and anorogenic magmatic phases in Sardinia andSouthern Spain: Inferences for the Cenozoic evolution of the western Mediterranean

L. Beccaluva a,⁎, G. Bianchini a,b, C. Natali a, F. Siena a

a Dipartimento di Scienze della Terra, Università di Ferrara, Italyb Istituto di Geoscienze e Georisorse, Consiglio Nazionale delle Ricerche, Sezione di Pisa, Italy

⁎ Corresponding author.E-mail address: bcc@unife.it (L. Beccaluva).

0024-4937/$ – see front matter © 2011 Elsevier B.V. Aldoi:10.1016/j.lithos.2011.01.007

a b s t r a c t

a r t i c l e i n f o

Article history:Received 13 May 2010Accepted 23 January 2011Available online 31 January 2011

Keywords:Orogenic magmasAnorogenic magmasMantle dynamicsSubduction roll-backCenozoic Mediterranean volcanism

The genetic relationships between orogenic (i.e. subduction related) and anorogenic (i.e. intra-plate) Cenozoicigneous phases have been investigated in two regions of thewesternMediterranean area: Sardinia and SouthernSpain. In Sardinia the ‘orogenic’magmatism (38–12 Ma) is followed by the ‘anorogenic’ volcanism, mostly sinceabout 6 Ma,whereas in Southern Spain the ‘anorogenic’ volcanism follows the ‘orogenic’ phase (34–6 Ma) after agap of 0–4 Ma in the Betic–Calatrava districts.The older orogenicmagmatism (tholeiitic, calcalkaline andmore potassic products) of both areas is related to thesubduction of the Ionian oceanic lithosphere which developed beneath the Paleo-European-Iberian continentalmargin probably sinceMiddle-Late Eocene. This subduction systemmigrated southeastwardswith time up to itspresent position in the Eolian–Calabrian Arc and the Betic–Alboran regions along the Apennine–Maghrebidebelt. Relics of subducted lithosphere are geophysically recorded as nearly-vertical bodies down to 500–600 km,flattening for several hundreds of kilometres under the Tyrrhenian–Sardinia and Betic–Calatrava areas,respectively. These relics of subducted slabs,which pond over large areas of themantle transition zone, appear toplay a significant role also in the genesis of the younger anorogenic magmas, whose major volcanic fields lieabove the frontal part of the subducted slabwhere convective instabilities and upwardmantle flow componentsare geophysically supported by laboratory and 3D numerical models. This dynamic response to subduction,involving localised mantle upwellings and remobilization of pre-existing mantle components, may have been afundamental factor in the generation of anorogenic magmas. Due to slab roll-back and inter-arc extension inboth Eolian–Tyrrhenian and Betic–Alboran regions, the magma sources of the previous orogenic phases can becompletely replaced by “fresh” mantle diapirs from whic\h anorogenic magmas will be generated. Thesemagmas are invariably characterised by OIB isotopic signatures (HIMU and EMI) which are classicallyinterpreted as long-term recycling of oceanic crust (plus variable sedimentary components) via ‘ancient’ pre-Paleozoic subduction events. We propose that the ‘recent’ Cenozoic subduction from which the orogenic serieswas generated, also had a dynamic influence on the younger anorogenic magmatism by remobilization of long-term isolated mantle components which resulted in the secular evolution of OIB-type magmas.In this view, the on-going subduction processes of the Mediterranean orogenic belts did not provide chemical“ingredients” to themantle sources of the anorogenic magmas, but induced reactivation of older metasomatisedmantle domains ultimately triggering magma genesis.

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1. Introduction

The common occurrence of igneous activity with ‘anorogenic’geochemical characteristics, following (or partially coeval with) anolder orogenic subduction-related magmatism, has been a matter ofconsiderable debate, particularly in the last decade (e.g., Beccaluva et al.,2005a,b; Bianchini et al., 2008; Lustrino et al., 2007b;Maury et al., 2000;Wilson and Bianchini, 1999). This debate has led to various petrogeneticmodels which fall into two main groups: 1) heterogeneous magma

sources in the supra-subduction mantle wedge favoured by mantleupwellings during slab retreat (De Ignacio et al., 2001; Duggen et al.,2003; Gill et al., 2004; Wallace and Carmichael, 1999), 2) existence ofslab detachments/windows allowing inflow of fluids/melts frombeneath the slab into the overlying mantle wedge (D'Orazio et al.,2000; Márquez et al., 1999).

During the Cenozoic, in the Mediterranean and surrounding areas,the systematic evolution from orogenic to anorogenic magmatismoccurred in the Carpathian–Pannonian region (Harangi and Lenkey,2007 and references therein), in the Anatolian–Aegean area (Agostiniet al., 2007and references therein), in theMaghrebian belt (Maury et al.,2000), in Sardinia (Beccaluva et al., 2005a,b; Lustrino et al., 2007b andreferences therein) and in Southern Spain (Doblas et al., 2007 and

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references therein). Cenozoic suites in Sardinia and Southern Spain areparticularly convenient cases studies because the orogenic andanorogenic magmatic phases are well-constrained in space and timeand are correlated with regional tectonics. Moreover geophysical dataindicate that flattened relics of the Cenozoic Apennine–Maghrebiansubduction still exist below Sardinia and the Betic–Calatrava districts inSouthern Spain (Piromallo and Morelli, 2003; Spakman, 1990).Therefore, we focus on the orogenic and anorogenic magmatic phasesof these two areas in order to: 1) define the tectono-magmaticsignificance of this temporal evolution, 2) clarify its causative processesand 3) present a geodynamic evolutionary model that accounts for thesystematic variation from orogenic to anorogenic magmatism.

2. Cenozoic volcanism in the western Mediterranean area

Cenozoic volcanism in the western Mediterranean, which extendsfrom Provence to Sardinia and to Southern Spain, can be roughlysubdivided in two phases often overlapped in space but generallydistinct in time and magmatic affinity (Beccaluva et al., 1989, 2005a,b;Lustrino et al., 2011): 1) orogenic magmatic activity – includingtholeiitic, calcalkaline, shoshonitic and ultrapotassic products – devel-oped mostly during Late Eocene–Miocene times and 2) anorogenicmagmatism –with tholeiitic to Na-alkaline products – occurring duringLate Miocene–Quaternary times.

The discussion below is focussed on the petrological andgeochemical characteristics of the various igneous associations (andtheir inferred mantle sources), in order to assess their tectono-magmatic significance.

For orogenic magmas, the distinctive geochemical features arerepresented by subduction-related components, which variously addLow Field Strength Elements (LFSE, such as K, Rb, Cs, Sr, Ba, U and Th)to the supra-subduction mantle wedge also in relation to the natureand mode of the subducted slab. The gradual enrichment of theseelements, coupled with 87Sr/86Sr increase and 143Nd/144Nd decrease isgenerally recorded from tholeiitic/calcalkaline, to more potassicmagmas (high-K calcalkaline/shoshonitic/ultrapotassic), dependingon the mode of subduction, which becomes progressively steeper, upto sub-vertical in the final stages of convergence (Avanzinelli et al.,2009; Beccaluva et al., 1991, 1994, 2005a; Conticelli et al., 2007).

For anorogenicmagmas, thegeochemical characterisation (Beccaluvaet al., 2005b; Lustrino and Wilson, 2007) mainly relies on theconventional OIB (Ocean Island Basalts) mantle end-members, such asHIMU (and FOZO) and Enriched Mantle EMI and EMII (Carlson, 1995;Hofmann, 1997; Weaver, 1991; Zindler and Hart, 1986) which areconsidered to originate in the sublithospheric uppermantle as the resultof long-term recycling of ancient subducted slabs. HIMU would resultfrom recycling of altered oceanic crust, whereas EMI and EMII require, inaddition, lower continental crust/pelagic components or terrigenoussediments, respectively (Carlson, 1995; Stracke et al., 2005; Weaver,1991; Willbold and Stracke, 2010).

These geochemical components are also recognised in lithosphericmantle xenoliths entrained in alkaline lavas from the same anorogenicprovinces, thus providing additional evidence for the composition ofthe underlying mantle section (Beccaluva et al., 2001, 2004, 2007a;Bianchini et al., 2007, 2008, 2010a,b, in press). It should be noted thatfor both orogenic and anorogenic igneous provinces, the addition ofsuch components, as metasomatic agents in mantle sources, signif-icantly lower the solidus temperature and therefore represent,together with concomitant heat transfer and diapiric decompression,the most effective mechanisms triggering magma-genesis in themantle (Beccaluva et al., 1998, 2005a,b, 2007b,c).

2.1. Orogenic magmatic phase

In the western Mediterranean area, along the European–Iberianmargin, Cenozoic magmatic activity with orogenic geochemical

affinity developed in Provence, the Ligurian–Provençal Basin, theValencia Trough, Sardinia, Corsica, and the Southern Spain. InProvence, the Cenozoic orogenic sub-volcanic and volcanic rocks aremainly represented by tholeiitic/calcalkaline microdiorites, basalts,andesites, dacites and ignimbrites from Estèrel (~34–20 Ma: Bellon,1981), which are typical of the initial orogenic magmatic stages inactive continental margins (Beccaluva et al., 1989, 1994, 2005a).These characteristics imply that the paleo-European continentalmargin was affected by subduction of oceanic lithosphere at leastfrom the Middle-Late Eocene. Calcalkaline (to shoshonitic) basalts,andesites and dacites have also been recovered in the Ligurian–Provençal Basin, with K–Ar ages spanning between 19 and 15 Ma(Sosson et al., 1998). A southwestward extension of this magmatismis represented by calcalkaline volcanics (andesites, dacites andrhyolites) outcropping in the island of Mallorca and offshore in theValencia Trough (~24–19 Ma; Martì et al., 1992). In Sardiniamagmaticactivity started about 38 Ma (Lustrino et al., 2009), mainly developingbetween 32 and 26 Ma with tholeiitic/calcalkaline basalt and andesitelavas (Beccaluva et al., 1989, 1994, 2005a). Between 23 and 12 Ma,large eruptions of rhyodacitic ignimbrites alternated with basaltic–andesitic lavas marked the last period of volcanic activity in Sardinia(Beccaluva et al., 1985a; Lustrino et al., 2009). The climax of theignimbritic eruptions between 21 and 19 Ma in both Provence andSardinia (Beccaluva et al., 1989, 2005a; Bellon, 1981), and theoccurrence of high-Mg calcalkaline basalts in Sardinia (~18 Ma;Lecca et al., 1997; Morra et al., 1997) suggest remarkable extensionaltectonics, which accompanied the opening of the Ligurian–ProvençalBasin and drifting and anticlockwise rotation of the Sardinia–Corsicablock (Burrus, 1984; Chamot-Rooke et al., 1999; Cherchi andMontadert, 1982; Montigny et al., 1981; Vigliotti and Langenheim,1995). The increasing occurrence of high-K calcalkaline andshoshonitic lavas during this phase indicates a more mature stage ofthe orogenic magmatism with time (Beccaluva et al., 1989, 1994,2005a). Middle-Late Miocene volcanic activity also occurred offshoreof Corsica, with calcalkaline (s.l.) andesites (~17–16 Ma; Rossi et al.,1998) and shoshonitic products in the Sardinia Channel (~13–12 Ma;Mascle et al., 2001). In Southern Corsica, rhyolitic ignimbrites(~19 Ma) are reported by Ottaviani-Spella et al. (1996), whilelamproites (~14 Ma) occurred at Sisco in the northern part of theisland, suggesting the onset of collisional tectonics (Civetta et al.,1978; Conticelli et al., 2009). In Southern Spain, orogenic volcanismtook place during Oligo-Miocene times in the Betic–Alboran region(Benito et al., 1999; Duggen et al., 2005; Turner et al., 1999). Thesevolcanic events include arc-tholeiitic dykes (near Malaga) showingmagmatic ages in the time span 34–27 Ma (Duggen et al., 2004;Turner et al., 1999), calcalkaline (e.g., at Cabo de Gata) and high-Kcalcalkaline (e.g., at El Hoyazo, Mazarron, Mar Menor) productserupting between 15 and 6 Ma, as well as shoshonites (e.g., atCartagena, Vera, Mazarron) and ultrapotassic lamproites (e.g., atCartagena, Fortuna, Vera, Jumilla) erupting between 12 and 6 Ma(Benito et al., 1999; Conticelli et al., 2009; Duggen et al., 2004, 2005;Turner et al., 1999).

Geochemical characteristics of the orogenic magmas suggest anevolution of the mantle sources involving subduction of oceaniclithosphere followed by collision and recycling of continental crustalcomponents back into the mantle. 87Sr/86Sr and 143Nd/144Nd isotopicratios of these orogenic magmas show a general displacement towardhigher 87Sr/86Sr and lower 143Nd/144Nd compositions with respectto the anorogenic mantle array of the Mediterranean area (Beccaluvaet al., 2005a; Bianchini et al., 2008; Lustrino and Wilson, 2007),indicating that fluids/melts released by the slab into the overlyingmantle wedge, could be derived from subducted oceanic lithospherewith variable involvement of continental crust materials. Accordingly,orogenic mafic rocks from Provence, characterised by 87Sr/86Srbetween 0.7045 and 0.7058, and 143Nd/144Nd between 0.51292 and0.51265 (Galassi, 1995), are consistent with generation from mantle

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sources solely enriched by fluids driven off the subducted oceaniclithosphere. On the other hand, the Sr–Nd isotopic systematics ofmafic volcanics from Sardinia indicate a more complex picture: therelatively low 87Sr/86Sr (b0.706) and high 143Nd/144Nd (N0.5126) arecompatible with the subduction of oceanic lithosphere, whereas thehigher 87Sr/86Sr (up to 0.7113) and lower 143Nd/144Nd (down to0.51219), cannot be due only to fluids released by oceanic lithosphere,but imply source contamination by continental crust components(Beccaluva et al., 1994, 2005a; Downes et al., 2001; Franciosi et al.,2003). Similarly, orogenic rocks from the Betic Cordillera show highlyvariable Sr–Nd isotopic composition (Conticelli et al., 2009; Duggenet al., 2004): 87Sr/86Sr 0.70459–0.71187 and 143Nd/144Nd 0.51290–0.51222 for the tholeiitic Malaga dykes; 87Sr/86Sr 0.70986–0.71365and 143Nd/144Nd 0.51243–0.51212 for calcalkaline and shoshoniticrocks; 87Sr/86Sr 0.71642–0.72259 and 143Nd/144Nd 0.51205–0.51201for ultrapotassic lamproites. Therefore, the petrological and geochem-ical variations of orogenic magmatism in the western Mediterraneancan be accounted for by: 1) heterogeneous subduction-relatedmetasomatic processes induced in the mantle wedge by fluids drivenoff subducted oceanic lithosphere in the early stages (tholeiitic andcalcalkaline magmatism), accompanied by continental crust-derivedcomponents (probably terrigenous sediments) in the late stages ofconvergence (high-K series) and 2) the resulting nearly coevalgeneration of both calcalkaline and more potassic magmas fromdifferent depths and source composition, beside a sub-verticalsubducted slab (Betic Cordillera).

2.2. Anorogenic magmatic phase

Anorogenic intra-plate volcanism developed closely related in spaceand timewith the orogenicmagmatismdescribed above in Sardinia andSouthern Spain (Fig. 1).

In Sardinia, Late Miocene–Quaternary volcanism took place duringextensional tectonics which also involved the adjoining Tyrrhenianarea, and produced a wide range of alkaline to tholeiitic basic lavas,covering an area of ca. 2000 km2. This activity, although sporadic,started at 12 Ma and mainly developed in the time span 6 to b0.2 Ma(Beccaluva et al., 1985a, 1989; Lustrino et al., 2007a,b). Sr–Nd–Pbisotopic data for the mafic lavas show a wide compositional range(Beccaluva et al., 2005b; Gasperini et al., 2000; Lustrino et al., 2000,2002, 2007a,b): 87Sr/86Sr 0.70315–0.70534; 143Nd/144Nd 0.51289–0.51235; and 206Pb/204Pb 17.5–18.0. These data indicate an EMIaffinity for most Sardinian magmas, although an HIMU-like signaturehas been recorded in few samples cropping out in the southern sectorof the island (Lustrino et al., 2000). Petrological and geochemicalcharacteristics of Sardinian anorogenic volcanism and associatedmantle xenoliths led to the conclusion that primary magmas, fromtholeiites through alkali basalts to basanites, were generated bydecreasing degrees of melting of progressively deeper lithosphericmantle sources (at depths between ca. 30 to 100 km) which werecharacterised by a prevalent EMI signature and, to much lesser extent,by HIMU (Beccaluva et al., 2005b).

In Southern Spain, intra-plate volcanism occurred during the LateMiocene–Early Quaternary in the Calatrava district (4000 km2), whereearlier sporadic leucitite products with EM affinity were followed by anassociation of nephelinite, melilitite, and alkali-basaltic lavas character-ised by an HIMU isotopic fingerprint (Cebriá and Lòpez-Ruiz, 1995 andreferences therein). In the Betic Cordillera, anorogenic volcanismfollowed the orogenic igneous cycle, after a gap of ~4 Ma producingNa-alkaline basaltic centres near Tallante (2.3 Ma; Duggen et al., 2005;Cebriá et al., 2009), with their abundant mantle xenoliths (Beccaluvaet al., 2004; Bianchini et al., in press).

Systematic investigations of mantle peridotite xenoliths entrainedby alkaline lavas from Sardinia (Beccaluva et al., 2001), Calatrava(Bianchini et al., 2010b) and Tallante (Beccaluva et al., 2004; Bianchiniet al., in press) indicate that metasomatising agents had a prevailing

HIMU imprint for Calatrava, whereas a predominant EMI componentis observed for Sardinia and Tallante. Alpine-type peridotites fromLherz, Lanzo and Ronda massifs show enrichment trends from DM toEM (Bodinier et al., 1991; Downes, 2001; Downes et al., 1991;Reisberg et al., 1989 and references therein), implying that theEuropean lithosphere was enriched by EM metasomatic componentsat least since the mid-Mesozoic. On the other hand, the addition ofHIMU-like components seems to have been present in both Europeanand North-African lithosphere since the Late Cretaceous (Beccaluvaet al., 2007a,c, 2008; Wilson and Bianchini, 1999), as indicated by theubiquitous presence of this component in the sources of Cenozoicanorogenic volcanic provinces. Seismic tomography suggests that thiscomponent, also referred to as the European AsthenosphericReservoir (EAR: Cebriá andWilson, 1995) or Low Velocity Component(LVC: Hoernle et al., 1995), could be related to common sheet-like(Hoernle et al., 1995) or diapir-like (Granet et al., 1995) sublitho-spheric mantle domains, which extend from Eastern Atlantic toEurope, Mediterranean and North Africa (Piromallo et al., 2008).Consequently, the HIMU-like metasomatising agents rising from theconvecting mantle appear to have accumulated in the lowerlithospheric portions (i.e. Thermal Boundary Layer), whereas oldermetasomatic components (e.g. EMI) may have been better preservedin the upper, more rigid lithospheric mantle (i.e., MechanicalBoundary Layer; Beccaluva et al., 1998, 2007c; Wilson et al., 1995).

3. Geodynamic control on magma activities

In a discussion of the geodynamic evolutionary model of thewestern Mediterranean area, the space–time distribution of bothorogenic and anorogenic magmatism, the structure of the underlyinglithosphere, as well as the lithospheric relics of previous subductions,must first be taken into consideration (Beccaluva et al., 1985b, 1989,1994, 2005a; Carminati and Doglioni, 2004; Jolivet et al., 1999;Malinverno and Ryan, 1986; Piromallo and Morelli, 2003; Wilson andBianchini, 1999; Wortel and Spakman, 2000). Moreover, to highlightthe possible genetic relationships between orogenic and anorogenicmagmatism in Sardinia and Southern Spain, several issues should beaddressed regarding: 1) the significance of the temporal gap (0–6 Ma)after which anorogenic volcanism replaces orogenic magmatism inthese regions; 2) the complete replacement of orogenic mantlesources by anorogenic magma sources; and 3) the triggeringmechanisms which cause the anorogenic volcanism to occur in thesame region where orogenic activity ended. These issues and therelative tectonomagmatic constraints are discussed below.

The geological evolution of the western Mediterranean may beconsidered the result of a single subduction process of the Ionian oceaniclithosphere, which probably started in the Middle-Late Eocene beneaththe Paleo-European continental margin and migrated southeastwardswith time. The progressive migration of this subduction system wasaccompanied by the opening of the Ligurian–Balearic and Tyrrhenianinterarcoceanicbasins (Beccaluvaet al., 1989, 1994, 2005a; Lustrinoet al.,2009). The early orogenic magmatism took place in a NE–SW belt, alongthe Paleo-European-Iberian continental margin, and developed with arctholeiitic/calcalkaline magmas in Provence and Sardinia (~38–26Ma),and in the Betic Cordillera (Malaga Dikes, 34–27Ma). Petrological andisotopic characteristics of these rocks reflect initial stages of arcmagmatism related to the subduction of oceanic lithosphere. Inter-arcrifting of the Paleo-European-Iberian continental margin developed atleast from the Early Miocene, leading to the opening of the Ligurian–Balearic oceanic basin and ultimately resulting in the southeastwarddrifting and rotation of the Sardinia–Corsica block (Fig. 1A). The orogenicvolcanic activity gradually ended in Sardinia (about 12 Ma) and in theBetics (about 6 Ma) with high-K2O calcalkaline, shoshonite andultrapotassic products, and was accompanied by a marked steepeningof the subduction during the late stages of convergence. From LateMiocene, southeastward slab retreat and roll-back induced rifting along

Fig. 1. (A) Tectonomagmatic sketch map of the Western Mediterranean. Upper mantle cross-sections beneath the Alboran–Betic–Calatrava (B) and the Calabria–Tyrrhenian–Sardinia (C) regions. 1 — lithosphere. 2 — Balearic and Tyrrhenian interarc basins. 3 — Cenozoic orogenic volcanism and related mantle sections. 4 — Late Miocene–Quaternaryanorogenic volcanism and related mantle sections. 5— inferred boundary of the subduction system at different ages; open triangles refer to slab detachments/windows according toWortel and Spakman (2000). 6— compressional thrust front of the Alps, Betic Cordillera and Apennines–Maghrebian chain. 7—mantle peridotite massifs of Ronda and Beni Bousera.8 — convective instabilities and mantle flow components triggered at the front and edges of the subducted slabs.

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the Internal Apennines and the Calabrian Alps leading to the opening ofthe Tyrrhenian basin and the southeastward migration of the Calabrianarc up to its present position. The potassic character and the isotopicfeatures of the orogenic magmas along the eastern peri-Tyrrhenianborder (from the Eolian arc to the Roman Province) and in the Betic

Cordillera have to be related to accentuated steepening of the subductedlithosphere, as well as the progressive involvement of terrigenoussediments in the supra-subduction mantle wedge (Avanzinelli et al.,2009; Beccaluva et al., 1991, 2005a; Conticelli et al., 2007). Accordingly,relics of these subducted slabs are shown by seismic tomography images

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(Piromallo and Morelli, 2003; Spakman, 1990; Wortel and Spakman,2000) plunging almost vertically beneath the Eolian–Calabrian arc andthe Betic–Alboran area. Geophysical modelling based on density andviscosity contrasts (Giunchi et al., 1996) and laboratory simulations(scaled analogue models; Faccenna et al., 2001) show goodcorrespondence with seismic tomography (Lucente et al., 1999;Piromallo and Morelli, 2003; Spakman, 1990; Wortel and Spakman,2000), and depicts a nearly vertical, still seismically active subducted slabdown to 500 km, and its bending and flattening in the upper mantle ataround the 660 km discontinuity. This model is in agreement with thetectonomagmatic scenario proposed by Beccaluva et al. (2005b) wherethe approximately 800-km long lithospheric slab, consumed during theentire subduction process since the Eocene, currently dips beneath theAeolian–Calabrian arc as a single body flattening westward under theTyrrhenian basin and the adjacent Sardinia block (Fig. 1C). A similarconfiguration of subducted slab, butwith lesser extension, is recorded byseismic tomography (Piromallo andMorelli, 2003;Wortel and Spakman,2000) dipping northwards to a depth of about 500 km and flatteningbeneath Southern Spain for about 200 km toward the Calatrava district(Fig. 1B).

These relics of subducted slabs which pond over large areas of themantle transition zone seem to play a significant role in the genesis ofanorogenic magmas shortly after the end of an orogenic magmaticcycle, as observed in Sardinia and in the Betic–Calatrava districts. Inboth regions, themajor anorogenic volcanic fields lie above the frontalpart of the subducted slab where convective instabilities could haveplayed a significant role in triggering the melting process in theshallower mantle. Significant upward flow components close to theslab edges are indicated by laboratory and 3D numerical models,showing the importance of toroidal/vertical mantle flow componentsaround the edges of a retreating subducted slab (Faccenna et al., 2010;Kincaid and Griffiths, 2003). Convective instabilities, generated as adynamic response to subduction, have recently been referred to as“splash plumes” (Davies and Bunge, 2006) involving localised mantleupwellings and remobilization of deep mantle domains from the topof the transition zone (410–660 km depth) to the overlying uppermantle/lithosphere (Bianchini et al., 2010a and b; Lustrino andWilson, 2007; Wilson and Downes, 2006).

In Fig. 1B and C, the generation of anorogenic magmas isconsidered the result of mantle upwelling/decompression, heattransfer and reactivation of older (Pre-Paleozoic) metasomatisingcomponents which take place at the periphery of the subducted slab.The delineated slab configuration accounts for the occurrence of bothorogenic and anorogenic igneous phases in the Betics and in Sardinia,and may also explain the absence of the orogenic volcanism atCalatrava which lies just at the extreme edge of the subducted slab.

With respect to the orogenic igneous phase, these processes tookplace after a gap of about 6 Ma in Sardinia (disregarding the sporadicevent at 12 Ma) and 0–4 Ma in the Betic–Calatrava districts. Due to slabroll-back and inter-arc extension, the magma sources of the precedingorogenic cycle are completely replaced by “fresh”mantle material fromwhich anorogenic magmas were then generated. The ubiquitous OIB(HIMU-like and EMI) signatures of anorogenic magmatism in thewestern Mediterranean area are in agreement with the above model,given that these mantle end-members are classically interpreted to bethe result of long-term recyclingof alteredoceanic basalts/gabbros (plusvariable sedimentary components) within the mantle via ancientsubduction (Bianchini et al., 2010a and b; Carlson, 1995; Hofmann,1997; Stracke et al., 2005; Weaver, 1991). In fact, the time-integratedgenesis of these mantle end-members precludes a direct connectionwith the Cenozoic subduction processes, and Wilson and Downes(1991) suggested 400–500 Ma as a proper time span required tomaturate similar isotopic compositions.

In this view, the Cenozoic anorogenic volcanismmay be interpretedto be a far-field consequence of the Mediterranean orogenic processes.This interpretation also means that the on-going subduction along the

Apennine–Magherbian belt doesn't provide chemical “ingredients” tothe mantle sources of the anorogenic magmas, but represents adynamic factor that triggers magma-genesis remobilizing old metaso-matised mantle domains.

4. Conclusions

Subducted slab relics, ponding over large areas of the mantletransition zone, appear to play a significant role also in the genesis ofanorogenicmagmas,whichoccurred shortly after the endof anorogenicmagmatic activity in Sardinia and in Southern Spain.

In these regions, major anorogenic volcanic fields lie above thefrontal part of the subducted slab flattening for several hundredkilometres under the Tyrrhenian–Sardinia and the Betic–Calatravaareas, suggesting that convective instabilities, originated at the edges ofa retreated subducted slab, could have triggered partial melting in theoverlying upper mantle/lithosphere.

Due to slab roll-back and inter-arc extension in both Eolian–Tyrrhenian and Betic–Alboran regions, the magma sources of theprevious orogenic cycles were completely replaced by “fresh” mantleupwellings which could have been the fundamental factor in favouringthe formation of anorogenic magmas.

In this view the anorogenic volcanism may be interpreted to be afar-field dynamic (not compositional) response to recent subductionprocesses characterised by roll-back and flattening of the subductedslab at the mantle transition zone.

Therefore, in order to maturate the OIB components whichcharacterise the studied intraplate magmatism, multiple geodynamicevents (and deep crustal recycling into the upper mantle) are requiredat least since Pre-Paleozoic times. This explains why OIB-like magma-tism becomes progressivelymore important during the Phanerozoic (atleast b1 Ga; Condie, 1985) in relation to the secular evolution of therelated mantle sources.

Acknowledgements

The authors are grateful to M. Lustrino and an anonymousreviewer for their constructive criticism and to B. Murphy andJ. Dostal for their encouragement and careful editorial handling.

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