Journal cover Journal topic
Solid Earth An interactive open-access journal of the European Geosciences Union
Journal topic
SE | Articles | Volume 11, issue 6
Solid Earth, 11, 2377–2409, 2020
© Author(s) 2020. This work is distributed under
the Creative Commons Attribution 4.0 License.

Special issue: The Iberian Massif in the frame of the European Variscan...

Solid Earth, 11, 2377–2409, 2020
© Author(s) 2020. This work is distributed under
the Creative Commons Attribution 4.0 License.

Research article 11 Dec 2020

Research article | 11 Dec 2020

Comparative geochemical study on Furongian–earliest Ordovician (Toledanian) and Ordovician (Sardic) felsic magmatic events in south-western Europe: underplating of hot mafic magmas linked to the opening of the Rheic Ocean

Comparative geochemical study on Furongian–earliest Ordovician (Toledanian) and Ordovician (Sardic) felsic magmatic events in south-western Europe: underplating of hot mafic magmas linked to the opening of the Rheic Ocean
J. Javier Álvaro1, Teresa Sánchez-García2, Claudia Puddu3, Josep Maria Casas4, Alejandro Díez-Montes5, Montserrat Liesa6, and Giacomo Oggiano7 J. Javier Álvaro et al.
  • 1Instituto de Geociencias (CSIC-UCM), Dr. Severo Ochoa 7, 28040 Madrid, Spain
  • 2Instituto Geológico y Minero de España, Ríos Rosas 23, 28003 Madrid, Spain
  • 3Dpt. Ciencias de la Tierra, Universidad de Zaragoza, 50009 Zaragoza, Spain
  • 4Dpt. de Dinàmica de la Terra i de l'Oceà, Universitat de Barcelona, Martí Franquès s/n, 08028 Barcelona, Spain
  • 5Instituto Geológico y Minero de España, Plaza de la Constitución 1, 37001 Salamanca, Spain
  • 6Dpt. de Mineralogia, Petrologia i Geologia aplicada, Universitat de Barcelona, Martí Franquès s/n, 08028 Barcelona, Spain
  • 7Dipartimento di Scienze della Natura e del Territorio, 07100 Sassari, Italy

Correspondence: J. Javier Álvaro (

Back to toptop

A geochemical comparison of early Palaeozoic felsic magmatic episodes throughout the south-western European margin of Gondwana is made and includes (i) Furongian–Early Ordovician (Toledanian) activities recorded in the Central Iberian and Galicia–Trás-os-Montes zones of the Iberian Massif, and (ii) Early–Late Ordovician (Sardic) activities in the Eastern Pyrenees, Occitan Domain (Albigeois, Montagne Noire and Mouthoumet massifs) and Sardinia. Both phases are related to uplift and denudation of an inherited palaeorelief, and stratigraphically preserved as distinct angular discordances and paraconformities involving gaps of up to 22 million years. The geochemical features of the predominantly felsic Toledanian and Sardic activities point to a predominance of magmatic byproducts derived from the melting of metasedimentary rocks, rich in SiO2 and K2O and with a peraluminous character. Zr  TiO2, Zr  Nb, Nb  Y and Zr vs. Ga  Al ratios, and rare-earth element (REE) and εNd(t) values suggest the contemporaneity, for both phases, of two geochemical scenarios characterized by arc and extensional features evolving to distinct extensional and rifting conditions associated with the final outpouring of mafic tholeiite-dominant lava flows. The Toledanian and Sardic magmatic phases are linked to neither metamorphism nor penetrative deformation; on the contrary, their unconformities are associated with foliation-free open folds subsequently affected by the Variscan deformation. The geochemical and structural framework precludes subduction-generated melts reaching the crust in a magmatic arc-to-back-arc setting and favours partial melting of sediments and/or granitoids in the lower continental crust triggered by the underplating of hot mafic magmas related to the opening of the Rheic Ocean.

1 Introduction
Back to toptop

A succession of early Palaeozoic felsic magmatic episodes, ranging in age from Furongian (formerly “late Cambrian”) to Late Ordovician, are widespread along the south-western European margin of Gondwana. Magmatic pulses are characterized by preferential development in different palaeogeographic areas and linked to the development of stratigraphic unconformities, but they are related to neither metamorphism nor penetrative deformation (Gutiérrez Marco et al., 2002; Montero et al., 2007). In the Central Iberian Zone of the Iberian Massif (representing the western branch of the Ibero-Armorican Arc; Fig. 1a–b), this magmatism is mainly represented by the Ollo de Sapo Formation, which has long been recognized as a Furongian–Early Ordovician (495–470 Ma) assemblage of predominantly felsic volcanic, subvolcanic and plutonic igneous rocks. This magmatic activity is contemporaneous with the development of the Toledanian phase, which places Lower Ordovician (upper Tremadocian–Floian) rocks onlapping an inherited palaeorelief formed by Ediacaran–Cambrian rocks and involving a sedimentary gap of ca. 22 million years. This unconformity can be correlated with the “Furongian gap” identified in the Ossa-Morena Zone of the Iberian Massif and the Anti-Atlas of Morocco (Álvaro et al., 2007, 2018; Álvaro and Vizcaïno, 2018; Sánchez-García et al., 2019), and with the “lacaune normande” in the central and North Armorican domains (Le Corre et al., 1991).

Figure 1(a) Pre-Variscan reconstruction of the Variscan tectonostratigraphic units bearing Cambro-Ordovician exposures reported in this work, from the south-western European margin of Gondwana; based on Pouclet et al. (2017) and Álvaro et al. (2020). (b) Setting of samples in the Central Iberian and Galicia–Trás-os-Montes zones; 59 – Carrascal, 68 – Guadarrama, 70 – Sanabria, 74 – Miranda do Douro, 77 – Ollo de Sapo, 79 – Portalegre, 82 – Saldanha, 84 – San Sebastián, 90 – Urra, BCSZ – Badajoz-Córdoba Shear Zone, Ce – Cévennes Massif, CIZ – Central Iberian Zone, CZ – Cantabrian Zone, GAPL – Grimaud–Asinara–Posada Line, GTMZ – Galicia–Trás-os-Montes Zone, ME – Maures-Estérel Massif, Mo – Mouthoumet Massif, NPFT – North Pyrenean Fault thrust, OD – Occitan Domain, OMZ – Ossa-Morena Zone, PTFSZ – Pyrenean Domain of the Porto–Tomar–Ferreira do Alentejo Shear Zone, Sa – Sanabria, SAD – South Armorican Domain, SASZs – South Armorican Shear Zone southern branch, SHF – Sillon Houiller Fault, SISZ – South-Iberian Shear Zone, SPFT – South Pyrenean Fault thrust, WALZ – West Asturian–Leonese Zone; modified from Sánchez-García et al. (2019). (c) Setting of samples in the Montagne Noire and Mouthoumet massifs; Am1-2 Larroque hamlet (Ambialet), Stg – St-Géraud, Sta – St-André, Mj – Montjoi, Qu – Quintillan, GL – Roque de Bandies, VLR – Villerouge-Termenès, VIN – Le Vintrou, HER – Gorges d'Héric (Caroux Massif), Ax1 – southern Mazamet (Nore Massif), Ax2 – (Rou) S Rouairoux (Agout Massif); modified from Álvaro et al. (2016). (d) Setting of Pyrenean samples; AB-08-01, 02, 03 – Albera metavolcanics, AB-08-05 – Albera orthogneisses, BN-1 – Andorra rhyolites, fc-1803 – Pallaresa rhyolites; modified from Casas et al. (2019). (e) Setting of Sardinian samples; CS – Capo Spartivento, T2 – Tuerredda, CC5 – Cuile Culurgioni, MF1 – Monte Filau, MFS1 – Monte Setti Ballas, PB – Punta Bianca; modified from Oggiano et al. (2010).

Another predominantly felsic magmatic event, although younger (Early–Late Ordovician) in age, has been recognized in some massifs situated along the eastern branch of the Variscan Ibero-Armorican Arc, such as the Pyrenees, the Occitan Domain and Sardinia (Fig. 1a, c–e). This magmatism is related to the Sardic unconformity, where Furongian–Lower Ordovician rocks are unconformably overlain by those attributed to the Sandbian–lower Katian (formerly Caradoc). The Sardic phase is related to both (i) a sedimentary gap of ca. 16–20 million years, along with an unconformity that geometrically ranges from 90 (angular discordance) to 0 (paraconformity) (Barca and Cherchi, 2004; Funneda and Oggiano, 2009; Álvaro et al., 2016, 2018; Casas et al., 2019), and (ii) a Middle Ordovician development of cleavage-free folds lacking any contemporaneous metamorphism (for an updated revision, see Casas et al., 2019). The associated magmatic activity took place during a time span of about 25–30 million years (from 475 to 445 Ma), so broadly contemporaneous with the sedimentary gap.

Although a general consensus exists associating this Furongian–Ordovician magmatism with the opening of the Rheic Ocean and the drift of Avalonia from north-western Gondwana (Díez Montes et al., 2010; Nance et al., 2010; Thomson et al., 2010; Álvaro et al., 2014a), the origin of this magmatism has received different interpretations. In the Central Iberian Zone, for instance, several geodynamic models have been proposed, such as (i) subduction-related melts reaching the crust in a magmatic arc-to-back-arc setting (Valverde-Vaquero and Dunning, 2000; Castro et al., 2009), (ii) partial melting of sediments or granitoids in the lower continental crust (LCC) affected by the underplating of hot mafic magmas during an extensional regime (Bea et al., 2007; Montero et al., 2009; Díez Montes et al., 2010) and (iii) post-collisional decompression melting of an earlier thickened continental crust without significant mantle involvement (Villaseca et al., 2016). In the Occitan Domain (southern French Massif Central and Mouthoumet massifs) and the Pyrenees, Marini (1988), Pouclet et al. (2017) and Puddu et al. (2019) have suggested a link to mantle thermal anomalies. Navidad et al. (2018) proposed that the Pyrenean magmatism was induced by progressive crustal thinning and uplift of lithospheric mantle isotherms. In Sardinia, Oggiano et al. (2010), Carmignani et al. (2001), Gaggero et al. (2012) and Cruciani et al. (2018) have suggested that a subduction scenario, mirroring an Andean-type active margin, caused the main Mid-Ordovician magmatic activity. In the Alps, the Sardic counterpart is also interpreted as a result of the collision of the so-called Qaidam Arc with the Gondwanan margin, followed by the accretion of the Qilian Block (Von Raumer and Stampfli, 2008; Von Raumer et al., 2013, 2015). This geodynamic interpretation is mainly suggested for the Alpine Briançonnais–Austroalpine basement, where the volcanosedimentary complexes postdating the Sardic tectonic inversion and folding stage portray a younger arc–arc oblique collision (450 Ma) of the eastern tail of the internal Alpine margin with the Hun terrane, succeeded by conspicuous exhumation in a transform margin setting (430 Ma) (Zurbriggen et al., 1997; Schaltegger et al., 2003; Franz and Romer, 2007; Von Raumer and Stampfli, 2008; Von Raumer et al., 2013; Zurbriggen, 2015, 2017).

Until now the Toledanian and Sardic magmatic events had been studied in different areas and interpreted separately, without taking into account their similarities and differences. In this work, the geochemical affinities of the Furongian–Early Ordovician (Toledanian) and Early–Late Ordovician (Sardic) felsic magmatic activities recorded in the Central Iberian and Galicia–Trás-os-Montes zones, the Pyrenees, the Occitan Domain and Sardinia are compared. The re-appraisal is based on 17 new samples from the Pyrenees, Montagne Noire and Sardinia, completing the absence of analysis in these areas, and a wide-ranging dataset of 93 previously published geochemical analyses throughout the study region in south-western Europe. This comparison may contribute to a better understanding of the meaning and origin of this felsic magmatism and, thus, to a discussion on the geodynamic scenario of this Gondwana margin (Fig. 1a) during Cambrian–Ordovician times, bracketed between the Cadomian and Variscan orogenies.

2 Emplacement and age of magmatic events
Back to toptop

This section documents the emplacement (summarized in Fig. 2) and age (Fig. 3) of the Toledanian and Sardic magmatic events throughout the south-western basement European Variscan Belt, in the north-western margin of Gondwana during Cambro-Ordovician times.

Figure 2Cambro-Ordovician lithostratigraphic chart of the areas studied in this work from the Central Iberian Zone, Galicia–Trás-os-Montes Zone, Occitan Domain, Eastern Pyrenees and Sardinia; modified from Álvaro et al. (2014b, 2016, 2018), Pouclet et al. (2017) and Sánchez-García et al. (2019); other lithostratigraphic sketches – such as those of the Ciudad Rodrigo–Hurdes–Sierra de Gata Domain (Díez Balda et al., 1990) and the Portuguese sector (Medina et al., 1998; Meireles et al., 2013) in the Central Iberian Zone, the Central Pyrenees (Zwart, 1979; Laumonier et al., 1996), the Albigeois Mountains in the Occitan Domain (Guérangé-Lozes and Alsac, 1986; Pouclet et al., 2017) and northern Sardinia (Elter et al., 1986) – are not included here; abbreviations: A-08 – Albera orthogneisses and metavolcanics (ca. 465–472 Ma; Liesa et al., 2011), Ag – Agualada, BN-1 – Andorra rhyolites, Ca – Campelles ignimbrites (ca. 455 Ma; Martí et al., 2019), CD – Cadí gneiss (456 ± 5 Ma; Casas et al., 2010), Cg – Canigó gneiss (472–462 Ma; Cocherie et al., 2005; Navidad et al., 2018), Co – Cortalets metabasite (460 ± 3 Ma; Navidad et al., 2018), Cs – Casemí gneiss (446 ± 5 and 452 ± 5 Ma; Casas et al., 2010), Es – Estremoz rhyolites (499 Ma; Pereira et al., 2012), fc-1803 – Pallaresa rhyolites (ca. 453 Ma; Clariana et al., 2018), Ga – Galiñero, GA – Golfo Aranci orthogneiss (469 ± 3.7 Ma; Giacomini et al., 2006), GH – Gorges d'Héric orthogneiss (450 ± 6 Ma; Roger et al., 2004), La – Larroque volcanic complex, LA – La Aquiana limestone, Ma – Marialles microdiorite (453 ± 4 Ma; Casas et al., 2010), Lo – Lodè orthogneiss (456 ± 14 Ma; Helbing and Tiepolo, 2005), MF – Monte Filau–Capo Spartivento orthogneiss (449 ± 6 Ma according to Ludwing and Turi, 1989; 457.5 ± 0.3 and 458.2 ± 0.3 Ma according to Pavanetto et al., 2012), Mo – Mora (493.5 ± 2 Ma; Dias Da Silva et al., 2014), Nu – Núria gneiss (457 ± 4 Ma; Martínez et al., 2011), OS – Ollo de Sapo rhyolites and ash-fall tuff beds (ca. 477 Ma; Gutiérrez-Alonso et al., 2016), Pe – Peso volcanic complex, PL – Pont-de-Larn orthogneiss (456 ± 3 Ma; Roger et al., 2004), Qb – Queralbs gneiss (457 ± 5 Ma; Martínez et al., 2011), PB – Punta Bianca orthogneiss (broadly Furongian–Tremadocian in age), PC – Porto Corallo dacites (465.4 ± 1.9 and 464 ± 1 Ma; Giacomini et al., 2006; Oggiano et al., 2010), Ri – Ribes granophyre (458 ± 3 Ma; Martínez et al., 2011), Rf – Roc de Frausa gneiss (477 ± 4, 476 ± 5 Ma; Cocherie et al., 2005; Castiñeiras et al., 2008a), So – Somail orthogneiss (471 ± 4 Ma; Cocherie et al., 2005), Sa – Saldanha (483.7 ± 1.5; Dias da Silva, 2014), SE – Saint Eutrope gneiss (455 ± 2 Ma; Pitra et al., 2012), Ta – Tanaunella orthogneiss (458 ± 7 Ma; Helbing and Tiepolo, 2005), Tr – Truchas, Ur – Urra rhyolites, and uUP – undifferentiated Upper Ordovician.


Figure 3Relative probability plots of the age of the Cambrian–Ordovician magmatism for (a) the Ollo de Sapo domain from the Central Iberian Zone and (b) the Pyrenees (Guilleries and Gavarres massifs), French Central Massif (including Montagne Noire), Sardinia, Corsica and Sicily (n: number of analyses). Data obtained from references cited in the text.


2.1 Iberian Massif

In the Ossa-Morena and southern Central Iberian zones of the Iberian Massif (Fig. 1a–b), the so-called Toledanian phase is recognized as an angular discordance that separates variably tilted Ediacaran–Cambrian Series 2 rifting volcanosedimentary packages from overlying passive-margin successions. The Toledanian gap comprises, at least, most of the Furongian and basal Ordovician, but the involved erosion can incise the entire Cambrian and the upper Ediacaran Cadomian basement (Gutiérrez-Marco et al., 2019; Álvaro et al., 2019; Sánchez-García et al., 2019). Recently, Sánchez-García et al. (2019) have interpreted the Toledanian phase as a break-up (or rift/drift) unconformity with the Armorican Quartzite (including the Purple Series and Los Montes beds; McDougall et al., 1987; Gutiérrez-Alonso et al., 2007; Shaw et al., 2012, 2014) sealing an inherited Toledanian palaeorelief (Fig. 2).

The phase of uplift and denudation of an inherited palaeorelief composed of upper Ediacaran–Cambrian rocks is associated with the massive outpouring of predominantly felsic calc-alkaline magmatic episodes related to neither metamorphic nor cleavage features. This magmatic activity is widely distributed throughout several areas of the Iberian Massif, such as the Cantabrian Zone and the easternmost flank of the West Asturian–Leonese Zone, where sills and rhyolitic lava flows and volcaniclastics mark the base of the Armorican Quartzite (dated at ca. 477.5 Ma; Gutiérrez-Alonso et al., 2007, 2016), and the lower Tremadocian Borrachón Formation of the Iberian Chains (Álvaro et al., 2008). Similar ages have been reported from igneous rocks of the basal allochthonous units and the Schistose Domain in the Galicia–Trás-os-Montes Zone (500–462 Ma; Valverde-Vaquero et al., 2005, 2007; Montero et al., 2009; Talavera et al., 2008, 2013; Dias da Silva et al., 2012, 2014; Díez Fernández et al., 2012; Farias et al., 2014) and different areas of the Central Iberian Zone, including the contact between the Central Iberian and Ossa-Morena zones, where the Carrascal and Portalegre batholiths are intruded and the felsic volcanosedimentary Urra Formation marks the unconformity that separates Cambrian and Ordovician strata (494–470 Ma; Solá et al., 2008; Antunes et al., 2009; Neiva et al., 2009; Romaõ et al., 2010; Rubio-Ordóñez et al., 2012; Villaseca et al., 2013) (Fig. 1b).

The most voluminous Toledanian-related volcanic episode is represented by the Ollo de Sapo Formation, which crops out throughout the north-eastern Central Iberian Zone. It mainly consists of felsic volcanosedimentary and volcanic rocks, interbedded at the base of the Lower Ordovician strata and plutonic bodies. The volcanosedimentary Ollo de Sapo Formation has long been recognized as an enigmatic Furongian–Early Ordovician (495–470 Ma) magmatic event exposed along the core of a 600 km long antiform (labelled as 77 in Fig. 1b) (Valverde-Vaquero and Dunning, 2000; Bea et al., 2006; Montero et al., 2007, 2009; Zeck et al., 2007; Castiñeiras et al., 2008a; Díez Montes et al., 2010; Navidad and Castiñeiras, 2011; Talavera et al., 2013; López-Sánchez et al., 2015; Díaz-Alvarado el al., 2016; Villaseca et al., 2016; García-Arias et al., 2018). The peak of magmatic activity was reached at ca. 490–485 Ma, and its most recognizable characteristic is the presence of abundant megacrysts of K-feldspar, plagioclase and blue quartz. There is no evident space–time relationship in its distribution (for a discussion, see López-Sánchez et al., 2015), and, collectively, the Ollo de Sapo Formation rocks record a major tectonothermal event whose expression can be found in most of the Variscan massifs of continental Europe, including the Armorican and Bohemian massifs (e.g. von Quadt, 1997; Kröner and Willmer, 1998; Linnemann et al., 2000; Tichomirowa et al., 2001; Friedl et al., 2004; Mingram et al., 2004; Teipel et al., 2004; Ballèvre et al., 2012; El Korh et al., 2012; Tichomirowa et al., 2012; for a summary, see Casas and Murphy, 2018). The large volume of magmatic rocks located in the European Variscan Belt has led some authors to propose the existence of a siliceous large igneous province (LIP) (Díez Montes et al., 2010; Gutiérrez-Alonso et al., 2016), named Ibero-Armorican LIP by García-Arias et al. (2018).

The Sardic phase has been proposed, marking a stratigraphic discontinuity close to the Middle–Upper Ordovician boundary interval in some areas of the Central Iberian Zone (e.g. Buçaco and Truchas Syncline; Martínez Catalán et al., 1992; Días da Silva et al., 2016) and the Morais allochthonous complex of the Galicia–Trás-os-Montes Zone (Días da Silva, 2014; Días da Silva et al., 2014, 2016). In the Truchas Syncline, the significance of the discontinuity (or discontinuities) was questioned by a biostratigraphic study of conodonts and the re-interpretation of some of these scouring surfaces as the result of Hirnantian glaciogenic incisions (Sarmiento et al., 1999). The pre-Hirnantian discontinuities have been interpreted as linked to the development of “horsts and half-grabens of local extent”, as a result of which “tilting and gentle folding of the Lower–Middle Ordovician strata, due to the rotation of individual half-grabens and horsts, create the Sardic unconformity in Iberia” (Dias da Silva et al., 2016: p. 1131 and p. 1143). However, the presence of synsedimentary listric faults associated with local outpouring of a basic volcanism, related to extensional pulses in the Ordovician passive-margin platform fringing north-western Gondwana, cannot be associated with the Sardic phase. As summarized in this work, the Sardic phase is characterized by generalized cortical uplift, denudation of exposed uplifted areas under subaerial exposure, stratigraphic gaps of about 25–30 million years, broad intrusion of felsic granitic plutons (now orthogneisses after Variscan deformation and metamorphism) with calc-alkaline affinity and a record of alluvial-to-fluvial deposits onlapping the unconformity. These are the features that characterize the Ordovician Sardic phase, not the record of Ordovician volcanism associated with local listric faults (e.g. Casas et al., 2010, 2019; Álvaro et al., 2016).

In contrast, the Sardic aftermath is represented by predominantly basic volcanic activity, mainly of tholeiitic affinity, and lining rift branches highlighting the onset of listric-fault networks; this event could be geodynamically compared with some processes recorded in the Central Iberian and the Galicia–Trás-os-Montes zones, but not with the Sardic phase. Therefore, the presence of the Sardic phase in the Iberian Massif has already been ruled out by the information published during the last 2 decades and should not be maintained unless the above-reported tectonothermal events are really found. The presence of an Ordovician volcanism associated with listric faults is not an argument in support of the record of the Sardic phase.

2.2 Central and Eastern Pyrenees

In the Central and Eastern Pyrenees (Fig. 1d), earliest Ordovician volcanic-free passive-margin conditions, represented by the Jujols Group (Padel et al., 2018), were succeeded by a late Early–Mid-Ordovician phase of uplift and erosion that led to the onset of the Sardic unconformity (Fig. 2). Uplift was associated with magmatic activity, which continued until Late Ordovician times. An extensional interval took place then, developing normal faults that controlled the sedimentation of post-Sardic siliciclastic deposits infilling palaeorelief depressions. Acritarchs recovered in the uppermost part of the Jujols Group suggest a broad Furongian–earliest Ordovician age (Casas and Palacios, 2012), conterminous with a maximum depositional age of ca. 475 Ma, based on the age of the youngest detrital zircon populations (Margalef et al., 2016). On the other hand, a ca. 459 Ma U–Pb age for the Upper Ordovician volcanic rocks overlying the Sardic unconformity has been proposed in the Eastern Pyrenees (Martí et al., 2019), and ca. 452–455 Ma in the neighbouring Catalan Coastal Range, which represents the southern prolongation of the Pyrenees (Navidad et al., 2010; Martínez et al., 2011). Thus, a time gap of about 16–23 million years can be related to the Sardic phase in the Eastern Pyrenees and the neighbouring Catalan Coastal Range.

Coeval with the late Early–Mid-Ordovician phase of generalized uplift and denudation, key magmatic activity led to the intrusion of voluminous granitoids, about 500 to 3000 m thick and encased in strata of the Ediacaran–Lower Cambrian Canaveilles Group (Fig. 2). These granitoids constitute the protoliths of the large orthogneissic laccoliths that punctuate the backbone of the Central and Eastern Pyrenees. These are, from west to east (Fig. 1d), the Aston (467–470 Ma; Denèle et al., 2009; Mezger and Gerdes, 2016), Hospitalet (about 472 Ma; Denèle et al., 2009), Canigó (472–462 Ma; Cocherie et al., 2005; Navidad et al., 2018), Roc de Frausa (477–476 Ma; Cocherie et al., 2005; Castiñeiras et al., 2008b) and Albera (about 470 Ma; Liesa et al., 2011) massifs, which comprise a dominant Floian–Dapingian age. It is noticeable that only a minor representation of coeval basic magmatic rocks are outcropped. The acidic volcanic equivalents have been documented in the Albera Massif, where subvolcanic rhyolitic porphyroid rocks have yielded similar ages to those of the main gneissic bodies at about 474–465 Ma (Liesa et al., 2011). Similar acidic byproducts are represented by the rhyolitic sills of Pierrefitte (Calvet et al., 1988).

The late Early–Mid-Ordovician (“Sardic”) phase of uplift was succeeded by a Late Ordovician extensional interval responsible for the opening of (half-)grabens infilled with the basal Upper Ordovician alluvial-to-fluvial conglomerates (La Rabassa Conglomerate Formation). At map scale, a set of NE–SW-trending normal faults abruptly controlling the thickness of the basal Upper Ordovician formations can be recognized in the La Cerdanya area (Casas and Fernández, 2007; Casas, 2010). Sharp variations in the thickness of the Upper Ordovician strata have been documented by Hartevelt (1970) and Casas and Fernández (2007). Drastic variations in grain size and thickness can be attributed to the development of palaeotopographies controlled by faults and subsequent erosion of uplifted palaeoreliefs, with subsequent infill of depressed areas by alluvial fan and fluvial deposits, finally sealed by Silurian sediments (Puddu et al., 2019). A Late Ordovician magmatic pulse contemporaneously yielded a varied set of magmatic rocks. Small granitic bodies are encased in the Canaveilles strata of the Canigó Massif. They constitute the protoliths of the Cadí (about 456 Ma; Casas et al., 2010), Casemí (446 to 452 Ma; Casas et al., 2010), Núria (ca. 457 Ma; Martínez et al., 2011) and Canigó G1-type (ca. 457 Ma; Navidad et al., 2018) gneisses.

The lowermost part of the Canaveilles Group (the so-called Balaig Series) host metre-scale thick bodies of metadiorite sills related to an Upper Ordovician protolith, (ca. 453 Ma, SHRIMP U–Pb in zircon; Casas et al., 2010). Coeval calc-alkaline ignimbrites, andesites and volcaniclastic rocks are interbedded in the Upper Ordovician succession of the Bruguera and Ribes de Freser areas (Robert and Thiebaut, 1976; Ayora, 1980; Robert, 1980; Martí et al., 1986, 2019). In the Ribes area, a granitic body with granophyric texture, dated at ca. 458 Ma by Martínez et al. (2011), intruded at the base of the Upper Ordovician succession. In the La Pallaresa dome, some metre-scale rhyodacitic-to-dacitic subvolcanic sills, Late Ordovician in age (ca. 453 Ma; Clariana et al., 2018), occur interbedded within the pre-unconformity strata and close to the base of the Upper Ordovician.

2.3 Occitan Domain: Albigeois, Montagne Noire and Mouthoumet massifs

The parautochthonous framework of the southern French Massif Central, named Occitan Domain by Pouclet et al. (2017), includes, among others, from south to north, the Mouthoumet, Montagne Noire and Albigeois massifs. The domain represents the south-eastern prolongation of the Variscan South Armorican Zone (including south-western Brittany and Vendée). Since Gèze (1949) and Arthaud (1970), the southern edge of the French Massif Central has been traditionally subdivided, from north to south, into the northern, axial and southern Montagne Noire (Fig. 1c). The Palaeozoic succession of the northern and southern sides includes sediments ranging from late Ediacaran to Silurian and from Terreneuvian (Cambrian) to Visean in age, respectively. These successions are affected by large-scale, south-verging recumbent folds that display a low-to-moderate metamorphic grade. Their emplacement took place in late Visean to Namurian times (Engel et al., 1980; Feist and Galtier, 1985; Echtler and Malavieille, 1990). The axial zone consists of plutonic, migmatitic and metamorphic rocks forming a regional ENE–WSW-oriented dome (Fig. 1c), where four principal lithological units can be recognized: (i) schists and mica schists, (ii) migmatitic orthogneisses, (iii) metapelitic metatexites, and (iv) diatexites and granites (Cocherie, 2003; Faure et al., 2004; Roger et al., 2004, 2015; Bé Mézème, 2005; Charles et al., 2009; Rabin et al., 2015). The Rosis mica schist synform subdivides the eastern axial zone into the Espinouse and Caroux sub-domes, whereas the south-western edge of the axial zone comprises the Nore Massif.

In the Occitan Domain, two main Cambro-Ordovician felsic events can be identified giving rise to the protoliths of (i) the Larroque metarhyolites in the northern Montagne Noire and Albigeois Mountains, thrusted southward from Rouergue, and (ii) the migmatitic orthogneisses that form the axial zone of the Montagne Noire (Fig. 2).

  • i.

    The Larroque volcanosedimentary complex is a thick (500–1000 m) package of porphyroclastic metarhyolites located on the northern Montagne Noire (Lacaune Mountains), Albigeois Mountains (St-Salvi-de-Carcavès and St-Sernin-sur-Rance nappes) and Rouergue; the Variscan setting of the formation is allochthonous in the Albigeois Mountains and parautochthonous in the rest. This volcanism is encased in the so-called “Série schisto-gréseuse verte” (see Guérangé-Lozes et al., 1996; Guérangé-Lozes and Alabouvette, 1999; Pouclet et al., 2017) (Fig. 2). The Larroque volcanic rocks consist of deformed porphyroclastic rhyolites rich in largely fragmented, lacunous (rhyolitic) quartz and alkali feldspar phenocrysts. The metarhyolites occur as porphyritic lava flows; sills; and other associated facies, such as aphyric lava flows, porphyritic and aphyric pyroclastic flows of welded or unwelded ignimbritic types, fine-to-coarse tephra deposits, and epiclastic and volcaniclastic deposits. These rocks are named “augen gneiss” or augengneiss and do not display a high-grade gneiss paragenesis but a general lower-grade metamorphic mineralogy. The Occitan augengneisses mimic the Ollo de Sapo facies from the Central Iberian Zone because of their large bluish quartz phenocrysts. Based on geochemical similarities and contemporaneous emplacement, Pouclet et al. (2017) suggested that this event also supplied the Davejean acidic volcanic rocks in the Mouthoumet Massif, which represent the southern prolongation of the Montagne Noire (Fig. 2), and the Génis rhyolitic unit of the western Limousin sector.

  • ii.

    Some migmatitic orthogneisses make up the southern axial zone, from the western Cabardès to the eastern Caroux domes. The orthogneisses, derived from Ordovician metagranites bearing large K-feldspar phenocrysts, were emplaced at about 471 Ma (Somail orthogneiss; Cocherie et al., 2005), 456 to 450 Ma (Pont-de-Larn and Gorges d'Héric gneisses, Roger et al., 2004) and ca. 455 Ma (Saint Eutrope gneiss; Pitra et al., 2012). They intruded a metasedimentary pile, traditionally known as “Schistes X” and formally named St-Pons–Cabardès Group (Fig. 2). The latter consists of schists, greywackes, quartzites, and subsidiary volcanic tuffs and marbles (Demange et al., 1996; Demange, 1999; Roger et al., 2004; Cocherie et al., 2005). The group is topped by the Sériès tuff, dated at about 545 Ma (Lescuyer and Cocherie, 1992), which represents a contemporaneous equivalent of the Cadomian Rivernous rhyolitic tuff (542.5 to 537.1 Ma) from the Lodève inlier of the northern Montagne Noire (Álvaro et al., 2014b, 2018; Padel et al., 2017). The age of migmatization has been inferred from U–Pb dates on monazite from migmatites and anatectic granites at 333 to 327 Ma (Bé Mézème, 2005; Charles et al., 2008); as a result, the 330–325 Ma time interval can represent a Variscan crustal melting event in the axial zone.

As in the Pyrenees, the Middle Ordovician is absent in the Occitan Domain. Its gap allows distinction between a Lower Ordovician pre-unconformity sedimentary package para- to unconformably overlain by an Upper Ordovician–Silurian succession (Álvaro et al., 2016; Pouclet et al., 2017).

2.4 Sardinia

In Sardinia the Cambro-Ordovician magmatism is well represented in the external (southern) and internal (northern) nappe zones of the exposed Variscan Belt (Fig. 1e), and ranges in age from late Furongian to Late Ordovician. Furongian–Tremadocian (ca. 491–480 Ma) magmatic activity, predating the Sardic phase, is mostly represented by felsic volcanic and subvolcanic rocks encased in the sandy San Vito Formation. The Sardic-related volcanic products differ from one nappe to another: intermediate and basic (mostly metandesites and andesitic basalts) are common in the nappe stacking of the central part of the island (Barbagia and Goceano), whereas felsic metavolcanites prevail in the south-eastern units. Their age is bracketed between 465 and 455 Ma (Giacomini et al., 2006; Oggiano et al., 2010; Pavanetto et al., 2012; Cruciani et al., 2018) and matches the Sardic gap based on biostratigraphy (Barca et al., 1988).

Teichmüller (1931) and Stille (1939) were the first to recognize in south-western Sardinia an intra-Ordovician stratigraphic hiatus. Its linked erosive unconformity is supported by a correlatable strong angular discordance in the Palaeozoic basement of the Iglesiente–Sulcis area, external zone (Carmignani et al., 2001). This major discontinuity separates the Cambrian–Lower Ordovician Nebida, Gonnesa and Iglesias groups (Pillola et al., 1998) from the overlying coarse-grained (“puddinga”) Monte Argentu metasediments (Leone et al., 1991, 2002; Laske et al., 1994). The gap comprises a chronostratigraphically constrained minimum gap of about 18 million years that includes the Floian and Dapingian (Barca et al., 1987, 1988; Pillola et al., 1998; Barca and Cherchi, 2004) (Fig. 2). The hiatus is related to neither metamorphism nor cleavage, though some E–W folds have been documented in the Gonnesa Anticline and the Iglesias Syncline (Cocco et al., 2018), which are overstepped by the puddinga metaconglomerates. Both the E–W folds and the overlying metaconglomerates were subsequently affected by Variscan N–S folds (Cocco and Funneda, 2011, 2017). Sardic-related volcanic rocks are not involved in this area, but Sardic-inherited palaeoreliefs are lined with breccia slides that include metre-to-decametre-scale carbonate boulders (“olistoliti”), some of them hosting synsedimentary faults contemporaneously mineralized with ore bodies (Boni and Koeppel, 1985; Boni, 1986; Barca, 1991; Caron et al., 1997). The lower part of the unconformably overlying Monte Argentu Formation was deposited in alluvial to fluvial environments (Martini et al., 1991; Loi et al., 1992; Loi and Dabard, 1997).

A similar gap was reported by Calvino (1972) in the Sarrabus-Gerrei units of the external nappe zone. The so-called “Sarrabese phase” is related to the onset of thick (up to 500 m thick) volcanosedimentary complexes and volcanites (Barca et al., 1996; Di Pisa et al., 1992) with a Darriwilian age for the protoliths of the metavolcanic rocks (465.4 to 464 Ma; Giacomini et al., 2006; Oggiano et al., 2010). In the Iglesiente–Sulcis region (Fig. 1e), Carmignani et al. (1986, 1992, 1994, 2001) suggested that the “Sardic-Sarrabese phase” should be associated with the compression of a Cambro-Ordovician back-arc basin that originated the migration of the Ordovician volcanic arc toward the Gondwanan margin.

Some gneissic bodies, interpreted as the plutonic counterpart of metavolcanic rocks, are located in the Bithia unit (e.g. the Monte Filau area, 458 to 457 Ma, surrounded by a Middle Ordovician andalusite thermal aureole; Pavanetto et al., 2012; Costamagna et al., 2016) and in the internal units (Lodè orthogneiss, ca. 456 Ma; Tanaunella orthogneiss, ca. 458 Ma, Helbing and Tiepolo, 2005; Golfo Aranci orthogneiss, ca. 469 Ma, Giacomini et al., 2006).

The Sardic palaeorelief is sealed by Upper Ordovician transgressive deposits. The sedimentary facies show high variability, but the – mostly terrigenous – sediments vary from fine-to-medium-sized grey sandstones to muddy sandstones and claystones. They are referred to as the Katian Punta Serpeddì and Orroeledu formations (Pistis et al., 2016). This post-Sardic sedimentary succession is coeval with a new magmatic pulsation represented by alkaline to tholeiitic within-plate basalts (Di Pisa et al., 1992; Gaggero et al., 2012).

3 Geochemical data
Back to toptop

3.1 Materials and methods

The rocks selected for geochemical analysis (231 samples; see tectonostratigraphic location in Fig. 1 and stratigraphic emplacement in Fig. 2) have recorded different degrees of hydrothermalism and metamorphism, as a result of which only the most immobile elements have been considered. The geochemical calculations, in which the major elements take part, have been made with values recalculated to 100 in volatility-free compositions; Fe is reported as FeOt.

The geochemical dataset of the Central Iberian Zone includes 152 published geochemical data, from which 85 are plutonic and 67 are volcanic and volcaniclastic rocks from the Ollo de Sapo Formation (Galicia, Sanabria and Guadarrama areas), and the contact between the Central Iberian and Ossa-Morena zones (Urra Formation and Portalegre and Carrascal granites). Other data were yielded from six volcanic rocks of the Galicia–Trás-os-Montes Zone (Saldanha area) (Supplement).

The dataset of the Eastern Pyrenees consists of 38 samples, of which 6 are upper Lower Ordovician volcanic rocks and 7 are upper Lower Ordovician plutonic rocks, together with 9 Upper Ordovician volcanic and 14 Upper Ordovician plutonic rocks (Supplement). New data reported below include two samples of subvolcanic sills intercalated in the pre-Sardic unconformity succession (Clariana et al., 2018; Margalef, unpublished, Table 1).

Table 1Chemical analyses of magmatic rocks. ICP and ICP-MS methods at ACME Laboratories in Canada.

Download Print Version | Download XLSX

The study samples from the Occitan Domain comprise six metavolcanic rocks, four from the Larroque volcanosedimentary complex in the Albigeois Mountains and northern Montagne Noire and two from the Mouthoumet Massif (Pouclet et al., 2017) (Supplement), and four new samples for the axial zone gneisses (Table 1).

In the Sardinian dataset, 25 published analyses are selected: 5 correspond to the Golfo Aranci orthogneiss (Giacomini et al., 2006), 6 to metavolcanics from the central part of the island (Giacomini et al., 2006; Cruciani et al., 2013), and 5 to metavolcanics and 1 to gneisses from the Bithia unit (Cruciani et al., 2018) (Supplement). Ten new analyses are added from the Monte Filau and Capo Spartivento gneisses of the Bithia unit, and from the Punta Bianca gneisses embedded within the migmatites of the high-grade metamorphic complex from the inner zone (Table 1).

Whole-rock major and trace elements and rare-earth element (REE) compositions were determined at ACME Laboratories, Vancouver, Canada. LiBO2 fusion followed by X-ray fluorescence spectroscopy (XRF) analysis was used to determine major elements. Rare-earth and refractory elements were measured by inductively coupled plasma–mass spectrometry (ICP-MS) following lithium metaborate–tetraborate fusion and nitric acid digestion on a 0.2 g sample. For base metals, a 0.5 g sample was digested in aqua regia at 95 C and analysed by inductively coupled plasma–atomic emission spectrometry (ICP-AES). Analyses of standards and duplicate samples indicate precision of better than 1 % for major oxides and 3–10 % for minor and trace elements.

Additional Sm–Nd isotopic analyses were performed at the Centro de Geocronología y Geoquímica Isotópica of the Complutense University in Madrid. They were carried out in whole-rock powders using a 150Nd 149Sm tracer by isotope dilution–thermal ionization mass spectrometry (ID-TIMS). The samples were first dissolved through oven digestion in sealed Teflon bombs with ultra-pure reagents to perform two-stage conventional cation-exchange chromatography for separation of Sm and Nd (Strelow, 1960; Winchester, 1963), and subsequently analysed using a VG Micromass Sector 54 multicollector spectrometer. The measured 143Nd 144Nd isotopic ratios were corrected for possible isobaric interferences from 142Ce and 144Sm (only for samples with 147Sm 144Sm < 0.0001) and normalized to 146Nd 144Nd = 0.7219 to correct for mass fractionation. The La Jolla Nd international isotopic standard was analysed during sample measurement and gave an average value of 143Nd 144Nd = 0.5114840 for nine replicas, with an internal precision of ± 0.000032 (2σ). These values were used to correct the measured ratios for possible sample drift. The estimated error for the 147Sm 144Nd ratio is 0.1 %.

A general classification of the analysed samples, following Winchester and Floyd (1977), can be seen in Fig. 4a–b, and the geographical coordinates of the new samples in Table 1. For geochemical comparison (summarized in Table 2), two large groups or suites are differentiated in order to check the similarities and differences between the magmatic rocks, and to infer a possible geochemical trend following a palaeogeographic SW–NE transect. The description reported below follows the same palaeogeographic and chronological order.

Figure 4(a) SiO2 vs. Zr  TiO2 and (b) Zr  TiO2 vs. Nb  Y plots (Winchester and Floyd, 1977) showing the composition of new samples (purple diamonds) and those taken from the literature (green triangles).


Table 2Summarized geochemical features of the Furongian and Ordovician felsic episodes described in the text; data from Lancelot et al. (1985), Calvet et al. (1988), Valverde-Vaquero and Dunning (2000), Roger et al. (2004), Vilà et al. (2005), Giacomini et al. (2006), Díez-Montes (2007), Montero et al. (2007, 2009), Solá (2007), Zeck et al. (2007), Castiñeiras et al. (2008b), Talavera (2009), Casas et al. (2010), Navidad et al. (2010, 2018), Liesa et al. (2011), Martínez et al. (2011, 2019), Navidad and Castiñeiras (2011), Gaggero et al. (2012), Talavera et al. (2013), Villaseca et al. (2016), Pouclet et al. (2017), Cruciani et al. (2018) and this work. Abbreviations: CIZ – Central Iberian Zone, GTOMZ – Galicia–Trás-os-Montes Zone, OCC – Occitan Domain, PYR – Pyrenees, and SAR – Sardinia. * sensu Guitard (1970). A  CNK ratio is always peraluminous.

Download Print Version | Download XLSX

3.2 Furongian–Middle Ordovician suite

In the Central Iberian and Galicia–Trás-os-Montes zones, the Furongian-to-Middle Ordovician magmatic activity is pervasive. Their main representative is the Ollo de Sapo Formation, which includes volcanic and subvolcanic rocks (67 samples) as well as plutonic rocks (85 samples) (data from Murphy et al., 2006; Díez-Montes, 2007; Montero et al., 2007, 2009; Solá, 2007; Solá et al., 2008; Talavera, 2009; Villaseca et al., 2016). From the parautochthonous Schistose Domain from the Galicia–Trás-os Montes Zone, six samples of rhyolite tuffs of the Saldanha Formation (Dias da Silva et al., 2014) are selected, which share geochemical features with the Ollo de Sapo Formation. In summary, five facies are differentiated in the Central Iberian and Galicia–Trás-os Montes zones: the Ollo de Sapo orthogneisses, some leucogneisses, metagranites and volcanic rocks, and the San Sebastián orthogneiss (for a geochemical characterization, see Table 2).

In the Central and Eastern Pyrenees, Early–Mid-Ordovician magmatic activity gave rise to the intrusion of voluminous (about 500–3000 m in size) aluminous granitic bodies, encased in the Canaveilles beds (Álvaro et al., 2018; Casas et al., 2019). They constitute the protoliths of the large orthogneissic laccoliths that form the core of the domal massifs scattered throughout the backbone of the Pyrenees. Rocks of the Canigó, Roc de Frausa and Albera massifs have been taken into account in this work, in which volcanic rocks of the Pierrefite and Albera massifs, and the so-called G2 and G3 orthogneisses by Guitard (1970) are also included. All subgroups vary compositionally from subalkaline andesite to rhyolite, as illustrated in the Pearce (1996) diagram of Fig. 5 (data compiled from Vilà et al., 2005; Castiñeiras et al., 2008b; Liesa et al., 2011; Navidad et al., 2018).

Figure 5Zr  Ti vs. Nb  Y discrimination diagram (after Winchester and Floyd, 1977; Pearce, 1996). (a) Lower–Middle Ordovician rocks of the Iberian Massif (Central Iberian and Galicia–Trás-os-Montes zones). (b) Middle–Upper Ordovician rocks of the Eastern Pyrenees. (c) Middle Ordovician rocks of the Occitan Domain. (c–d) Middle–Upper Ordovician rocks of Sardinia.

Although most rocks in this area are acidic, the presence of minor mafic bodies is remarkable (Cortalet and Marialles metabasites, not studied in this work), which could indicate a mantle connection with parental magmas during the Mid and Late Ordovician. Additionally, it should be noted that there are no andesitic rocks in the area.

In the Occitan Domain, six samples of the Larroque volcanosedimentary complex (early Tremadocian in age) represent basin floors and subaerial explosive and effusive rhyolites (Pouclet et al., 2017). The porphyroclastic rocks of the Larroque metarhyolites were sampled in the Saint-Géraud and Larroque areas from the Saint-Sernin-sur-Rance nappe and the Saint-André klippe above the Saint-Salvi-de-Carcavès nappe (Pouclet et al., 2017).

In the Middle Ordovician rocks of Sardinia, 11 samples are selected, 5 of which correspond to orthogneisses of the Aranci Gulf, in the inner zone of the NE island (Giacomini et al., 2006), completed with 6 volcanic rocks of the external zone (Giacomini et al., 2006; Cruciani et al., 2018) (Table 2).

3.3 Upper Ordovician suite

In the Central and Eastern Pyrenees, four Upper Ordovician subgroups are distinguished based on their field occurrence and geochemical and geochronological features: the G1-type orthogneisses (sensu Guitard, 1970), the Cadí and Casemí orthogneisses and the metavolcanic rocks that include the Ribes de Freser rhyolites, the Els Metges volcanic tuffs, and the rhyolites from Andorra and Pallaresa areas (the latter dated at ca. 453 Ma; Clariana et al., 2018) (Table 2). The suite is completed with the Somail orthogneisses of the axial Montagne Noire (dated at ca. 450 Ma at Gorges d'Héric; Roger et al., 2004) and the orthogneisses from the Sardinian external zone (dated at ca. 458–457 Ma at Monte Filau; Pavanetto et al., 2012) and the volcanic rocks from the Sardinian nappe zone (Table 2).

4 Geochemical framework
Back to toptop

A geochemical comparison between the Furongian–Ordovician felsic rocks of all the above-reported groups offers the opportunity to characterize the successive sources of crust-derived melts along the south-western European margin of Gondwana.

The geochemical features point to a predominance of materials derived from the melting of metasedimentary rocks, rich in SiO2 and K2O (average K2O  Na2O = 2.25) and peraluminous (0.4 < Cnorm < 4.5 and 0.94 < A / CNK > 3.12), with only three samples with A / CNK < 1 (samples 10 0786 of the Casemí subgroup, and T26 and T27 of the San Sebastián subgroup).

The result of plotting the REE content vs. average values of continental crust (Rudnick and Gao, 2003; Fig. 6) yields a flat spectrum and a base level shared by most of the considered groups. The total content in REE is moderate to high (average REE = 176 ppm, ranging between 482.2 and 26.0 ppm; Fig. 7), with a maximum in the subgroup of the Middle Ordovician volcanic rocks from Sardinia (average REE = 335 ppm, VOL-SMO), and with light rare-earth element (LREE) values more fractionated than heavy rare-earth element (HREE) ones, and negative anomalies of Eu, which would indicate a characteristic process of magmatic evolution with plagioclase fractionation. These features are common in peraluminous granitoids.

Figure 6Upper-crust-normalized REE patterns (Rudnick and Gao, 2003) with average values for all distinguished groups; symbols as in Fig. 4.


All subgroups display similar chondrite-normalized REE patterns (Fig. 7), with an enrichment in LREE relative to HREE, which should indicate the involvement of crustal materials in their parental magmas. Nevertheless, some variations can be highlighted, such as the lesser fractionation in REE content of some subgroups. These are the leucogneisses from the Iberian Massif (LG, La  Ybn= 2.01), the Upper Ordovician orthogneisses from Sardinia (OG-SUO, La  Ybn= 2.94), the Casemí orthogneisses (La  Ybn= 4.42) and the Middle Ordovician volcanic rocks from Sardinia (OG-SUO, La  Ybn= 2.94). This may be interpreted as a greater degree of partial fusion in the origin of their parental magmas (Rollinson, 1993).

Figure 7Chondrite-normalized REE patterns (Sun and McDonough, 1989) for all study samples.


There are three geochemical groups displaying (Gd  Yb)n values > 2 and (La  Yb)n values  9. These groups are OSS (Central Iberian Zone), VOL-OD (Occitan Domain) and G1 (Pyrenees), and they share higher-alkalinity features.

Some V1 rocks from the Pyrenees (Pierrefite Formation) show no negative anomalies in Eu. Their parental magmas could have been derived from deeper origins and related to residual materials of the lower continental crust, in areas generating K-rich granites (Taylor and McLenan, 1985).

The spider diagrams (Fig. 8), however, exhibit strong negative anomalies in Nb, Sr and Ti, which indicate a distinct crustal affiliation (Díez-Montes, 2007). Only the San Sebastián orthogneisses (OSS) show distinct discrepancies with respect to the remaining samples from the Ollo de Sapo Formation. They display lower negative anomalies in Nb and a more alkaline character by comparison with the rest of the Ollo de Sapo rocks, which point to alkaline affinities and greater negative anomalies in Nb.

Figure 8Multi-element diagram normalized to the primitive mantle of Palme and O'Neill (2004) for all study samples.


Despite some small differences in the chemical ranges of some major elements, most felsic Ordovician rocks from the Iberian Massif (Central Iberian and Galicia–Trás-os Montes zones), the Eastern Pyrenees, the Occitan Domain and Sardinia share a common chemical pattern. The Lower–Middle Ordovician rocks of the Eastern Pyrenees show less variation in the content of Zr and Nb (Fig. 8b). The volcanic rocks of these groups show a different REE behaviour, which would indicate different sources. Two groups are distinguished in Fig. 7, one with greater enrichment in REE and a negative Eu anomaly, and another with less HREE content and without Eu negative anomalies.

Figure 9 illustrates how the average of all the considered groups approximates the mean values of the upper continental crust (UCC) of Rudnick and Gao (2003). In this figure, small deviations can be observed, some of them toward lower continental crust (LCC) values and others toward bulk continental crust (BCC), indicating variations in their parental magmas but with quite similar spectra. Overall chondrite-normalized patterns are close to the values that represent the upper continental crust, with slight enrichments in the Th  Nb, Th  La and Th  Yb ratios.

Figure 9Chondrite-normalized isotope ratio patterns (Sun and McDonough, 1989) for standard comparison for all study samples. Blue area: limits of continental crust values (lower and upper) of Rudnick and Gao (2003).


Finally, in the Occitan volcanic rocks (VOL-OD) the rare-earth elements are enriched and fractionated (33.2 ppm < La < 45.6 ppm; 11.2 < La  Yb < 14.5). The upper-continental-crust-normalized diagram exhibits negative anomalies of Ti, V, Cr, Mn and Fe associated with oxide fractionation; of Zr and Hf linked to zircon fractionation; and of Eu related to plagioclase fractionation. The profiles are comparable to the Vendean Saint-Gilles rhyolitic ones. The Th vs. Rb / Ba features are also similar to those of the Saint-Gilles rhyolites, and the Iberian Ollo de Sapo and Urra rhyolites (Solá et al., 2008; Díez Montes et al., 2010).

5 Discussion
Back to toptop

5.1 Inferred tectonic settings

In order to clarify the evolution of geotectonic environments, the data have been represented in different discrimination diagrams. The Zr  TiO2 ratio (Lentz, 1996; Syme, 1998) is a key index of compositional evolution for intermediate and felsic rocks. In the Syme diagram (Fig. 10), most rocks from the Central Iberian Zone represent a characteristic arc association, although there are some contemporaneous samples characterized by extension-related values (Zr  Ti = 0.10, LG). The rocks of the Middle–Ordovician San Sebastián orthogneisses (OSS) show values of Zr  Ti = 0.08, intermediate between extensional and arc conditions. This could be interpreted as a sharp change in geotectonic conditions toward the Mid-Ordovician (Fig. 10a). For a better comparison, the samples of the San Sebastián orthogneisses (OSS) and the granites (GRA) have been distinguished with a shaded area in all the diagrams, since they have slightly different characteristics to the rest of the samples from the Ollo de Sapo Group. The samples G1 (Pyrenees) and VOL (Central Iberian Zone) broadly share similar values, as a result of which the three latter groups (OSS, G1 and VOL) are arranged following a good-correlation line. The same trend seems to be inferred in the Eastern Pyrenees (Fig. 10b), where the Middle Ordovician subgroups display arc features, but half of the Upper Ordovician subgroups show extensional affinities (G1 and Casemí orthogneisses). In the case of the Occitan orthogneisses (Fig. 10c), they show arc characteristics, which contrast with the contemporaneous volcanic rocks displaying extensional values of Zr  Ti = 0.10. This disparity between plutonic and volcanic rocks could be interpreted as different conditions for the origin of these magmas. In Sardinia (Fig. 10d), the same evolution from arc to extensional conditions is highlighted for the Upper Ordovician samples, although some Middle Ordovician volcanic rocks already shared extensional patterns (Zr  Ti = 0.09). In summary, there seems to be a geochemical evolution in the Ordovician magmas grading from arc to extensional environments.

Figure 10Tectonic discrimination diagram of Zr vs. TiO2 (Syme, 1998) for all study samples. Double-sided arrows indicate ranging of different fields: rhyolites in tholeiitic and calc-alkaline arc suites have Zr  TiO2 ratios ranging from about 0.016 to 0.04, and extension-related rhyolites from about 0.13 to 0.28 (Syme, 1998).


In the Nb–Y tectonic discrimination diagram of Pearce et al. (1984) (Fig. 11), most samples are plotted in the volcanic-arc type, though some subgroups are projected in the within-plate and anomalous ocean ridge granites (ORG). The majority of samples display very similar Zr  Nb and Nb  Y ratios, typical of island arc or active continental-margin rhyolites (Díez-Montes et al., 2010). Only some samples are plotted separately: OSS samples with the highest Nb contents (> 20 ppm) and some volcanic rocks of the Occitan Domain (average Nb = 16.87 ppm). In the Eastern Pyrenees, the Middle Ordovician rocks are plotted in the volcanic-arc field, whereas the Upper Ordovician ones point to the ORG type, except the Casemí samples. This progress of magmatic sources agrees with the evolution seen in Fig. 10. In the Occitan Domain, VOL-OD samples share values with those of the San Sebastián orthogneiss, while OG-OD shares values with those of OG from the Central Iberian Zone.

Figure 11Tectonic discrimination diagram of Y vs. Nb (Pearce et al., 1984) for all study samples.


The Zr–Nb diagram (Leat et al., 1986; modified by Piercey, 2011) (Fig. 13) illustrates how magmas evolved toward richer values in Zr and Nb, which is consistent with what is observed in the Syme diagram (Fig. 10). Figure 12a documents how most samples show a generally positive correlation. These different groups correspond to the OSS and Portalegre granites, highlighted in the figure. The two groups indicate a tendency toward alkaline magmas. Some samples – such as the Pyrenean G1, some Occitan VOL-OD samples and some Sardinian OG-SUO samples – share the same affinity, clearly distinguished from the general geochemical trend exhibited by the Central Iberian Zone.

Figure 12Zr vs. 104 Ga  Al discrimination diagram (Whalen et al., 1987) for all study samples.


On a Zr vs. Ga / Al diagram (Whalen et al., 1987) (Fig. 13), the samples depict an intermediate character between anorogenic or alkaline (A type) and orogenic (I and S type). In the Central Iberian Zone, samples from the San Sebastián orthogneisses and Portalegre granites show characters of A-type granites, while the remaining samples display affinities of I- and S-type granites. For the Central Iberian Zone, a clear magmatic shift toward more extensional geotectonic environments is characterized. For the Eastern Pyrenees, we find the same situation as in the Central Iberian Zone, with a magmatic evolution toward A-type granite characteristics, indicating more extensional geotectonic environments. In the Occitan Domain, the samples show a clear I- and S-type character. In the Sardinian case, the same seems to happen as in the Central Iberian Zone: the Upper Ordovician orthogneisses suggest a more extensional character.

Figure 13Zr–Nb plot diagram (Leat et al.,1986; modified by Piercey, 2011) for all study samples.

In summary, all the reported diagrams point to a magmatic evolution through time, grading from arc to extensional geotectonic environments (with increased Zr  Ti ratios) and to A-type granite characteristics. This geotectonic framework is consistent with that illustrated in Fig. 10. The geochemical characters of these rocks show a rhyodacite-to-dacite composition, peraluminous and calc-alkaline K-rich character, and a volcanic-arc affinity for most of samples but without intermediate rocks associated with andesitic types. Hence a change in time is documented toward more alkaline magmas.

5.2 Interpretation of εNd values

εNd(t) values are useful for interpreting the nature of magmatic sources. Most samples of the above-reported groups show no significant differences in isotopic εNd(t) values and NdCHUR model ages (Fig. 14). Some exceptions are related to granites from the southern Central Iberian Zone, which display positive values (from +2.6 to 2.4) and TDM values from 0.90 to 3.46 Ga. These granites, space-related to calc-alkaline diorites and gabbros, were interpreted by Solá et al. (2008) as the result of underplating and temporal storage of mantle-derived magmas as a potential source for the intrusive “orogenic melts” during early Palaeozoic extension.

Figure 14εNd(t)–age diagram (DePaolo and Wasserburg, 1976; DePaolo, 1981) for all study samples. (a) Central Iberian and Galicia–Trás-os-Montes zones. (b) Eastern Pyrenees. (c) Occitan Domain. (d) Sardinia. See references in the text.


Some samples from (i) the Central Iberian Zone, such as VI-3 (Leucogneiss subgroup) and PORT2 and PORT15 (Granite subgroup); (ii) the Eastern Pyrenees, such as samples 99338 (G1 subgroup) and 100786 (Casemí subgroup); and (iii) the Sardinian CS5, CS8 and CC5 samples (Upper Ordovician orthogneiss subgroup) display anomalous TDM values and 147Sm 144Nd ratios > 0.17 (Table 2; Fig. 14), a characteristic relatively common in some felsic rocks (DePaolo, 1988; Martínez et al., 2011). According to Stern (2002), these values should not be considered, but a possible explanation for these high ratios may be related to the M-type tetrad effect (e.g. Irber, 1999; Monecke et al., 2007; Ibrahim et al., 2015), which affects REE fractionation in highly evolved felsic rocks due to the interaction with hydrothermal fluids. This process can be reflected as an enrichment of Sm related to Nd. Other authors, however, explain this enrichment as a result of both magmatic evolution (e.g. McLennan, 1994; Pan, 1997) and weathering processes after exhumation (e.g. Masuda and Akagi, 1989; Takahashi et al., 2002).

In the granites of the southern Central Iberian Zone and the volcanic rocks of Sardinia, positive values in εNd(t) could be interpreted as a more primitive nature of their parental magmas, even though the samples with highest TDM values are those that display higher 147Sm 144Nd ratios (> 0.17; Table 2).

The volcanic rocks of the Central Iberian Zone display some differences following a N–S transect, with εNd(t) values being less variable in the north (εNd(t): 4.0 to 5.0) than in the south (εNd(t): 1.6 to 5.5). The isotopic signature of the volcaniclastic Urra rocks is compatible with magmas derived from young crustal rocks, with intermediate-to-felsic igneous compositions (Solá et al., 2008). The volcanic rocks of the northern Central Iberian Zone could be derived from older crustal rocks (Montero et al., 2007). The isotopic composition of the granitoids from the southern Central Iberian Zone has more primitive characteristics than those of the northern Central Iberian Zone, suggesting different sources for both sides (Talavera et al., 2013). OSS shows lower inheritance patterns, more primitive Sr–Nd isotopic composition than other rocks of the Ollo de Sapo suite, and an age some 15 million years younger than most meta-igneous rocks of the Sanabria region (Montero et al., 2009), likely reflecting a greater mantle involvement in its genesis (Díez-Montes, 2007).

According to Talavera et al. (2013), the Cambro-Ordovician rocks of the Galicia–Trás-os-Montes Zone schistose area and the magmatic rocks of the northern Central Iberian Zone are contemporary. Both metavolcanic and metagranitic rocks almost share the same isotopic compositions.

The Upper Ordovician orthogneisses from the Occitan Domain show very little variation in εNd(t) values (3.5 to 4.0), typical of magmas derived from young crustal rocks. The variation in depleted mantle model age (TDM) values is also small (1.4 to 1.8 Ga), indicating similar crustal residence times to other rock groups.

In Sardinia, εNd(t) values present a greater variation (1.6 to 3.3), but they are also included in the typical continental crust range. As noted above, anormal TDM values (between 1.2 and 4.5 Ga) may be due to post-magmatic hydrothermal alteration processes.

6 Geodynamic setting
Back to toptop

In the Iberian Massif, the Ediacaran–Cambrian transition was marked by paraconformities and angular discordances indicating the passage from Cadomian volcanic arc to rifting conditions. The axis of the so-called Ossa-Morena Rift lies along the homonymous zone (Quesada, 1991; Sánchez-García et al., 2003, 2008, 2010) close to the remains of the Cadomian suture (Murphy et al., 2006). Rifting conditions were accompanied by a voluminous magmatism that changed from peraluminous acid to bimodal (Sánchez-García et al., 2003, 2008, 2016, 2019). Some authors (Álvaro et al., 2014a; Sánchez-García et al., 2019) propose that this rift resulted from a SW-to-NE inward migration, toward innermost parts of Gondwana, of rifting axes from the Anti-Atlas in Morocco to the Ossa-Morena Zone in the Iberian Massif. According to this proposal the rift developed later (in Cambro-Ordovician times) in the Iberian, Armorican and Bohemian massifs.

The Furongian–Ordovician transition to drifting conditions is associated – in the Iberian Massif, the Occitan Domain, the Pyrenees and Sardinia – with stepwise magmatic activity contemporaneous with the record of the Toledanian and Sardic unconformities. These, related to neither metamorphism nor penetrative deformations, are linked to uplift, erosion and irregularly distributed mesoscale deformation that gave rise to angular unconformities up to 90. The time span involved in these gaps is similar (22 million years in the Iberian Massif, 16–23 million years in the Pyrenees and 18 million years in Sardinia). This contrasts with the greater time span displayed by the magmatic activity (30–45 million years), which started before the unconformity formation (early Furongian in the Central Iberian Zone vs. Floian in the Pyrenees, Occitan Domain and Sardinia), continued during the unconformity formation (Furongian and early Tremadocian in the Central Iberian Zone vs. Floian–Darriwilian in the Pyrenees, Occitan Domain and Sardinia) and ended during the sealing of the uplifted and eroded palaeorelief (Tremadocian–Floian volcaniclastic rocks at the base of the Armorican Quartzite in the Central Iberian Zone vs. Sandbian–Katian volcanic rocks at the lowermost part of the Upper Ordovician successions in the Pyrenees, Occitan Domain and Sardinia; Gutiérrez-Alonso et al., 2007, 2016; Navidad et al., 2010; Martínez et al., 2011; Álvaro et al., 2016; Martí et al., 2019). In the Pyrenees, Upper Ordovician magmatism and sedimentation coexist with normal faults controlling marked thickness changes of the basal Upper Ordovician succession and cutting the lower part of this succession, the Sardic unconformity and the underlying Cambro-Ordovician sequence (Puddu et al., 2018, 2019).

Although the Toledanian and Sardic phases reflect similar geodynamic conditions in two distinct palaeogeographic areas, at present forming the western and eastern branches of the Variscan Ibero-Armorican Arc, they display different peaks in magmatic activity with minor chronological overlapping (Fig. 3). This may reflect a SW-to-NE “zip-like” propagation of the latest Ediacaran–Terreneuvian rift axes in the so-called Atlas–Ossa-Morena Rift.

6.1 Toledanian phase

The Early Ordovician (Toledanian) magmatism of the Central Iberian Zone evolved to a typical passive-margin setting, with geochemical features dominated by acidic rocks, peraluminous and rich in K, and lacking any association with basic or intermediate rocks. Some of the orthogneisses of the Galicia–Trás-os-Montes Zone basal and allochthonous complex units share these same patterns. This fact has been interpreted by some authors as a basin environment subject to important episodes of crustal extension (Martínez-Catalán et al., 2007; Díez-Montes et al., 2010). In contrast, Villaseca et al. (2016) interpreted this absence as evidence against rifting conditions, though the absence of contemporary basic magmatism may be explained by the partial fusion of a thickened crust, through recycling of Neoproterozoic crustal materials. The thrust of a large metasedimentary sequence could generate dehydration and metasomatism of the rocks above this sequence, triggering partial fusion at different levels, although the increase in peraluminosity with the basicity of the orthogneisses is against any assimilation-fractional crystallization process involving mantle materials. However, this increase in peraluminosity with the basicity has not been revealed in the samples studied above. Following the model of Villaseca et al. (2016), a flat subduction of the southern part of the Central Iberian Zone would have taken place under its northern prolongation, whereas the reflection of such a subduction is not evident in the field. The calc-alkaline signature of this magmatism has also been taken into account as proof of its relationship with volcanic-arc environments (Valverde-Vaquero and Dunning, 2000). However, calc-alkaline features may also be interpreted as a result of variable degrees of continental crust contamination and/or a previously enriched mantle source (Sánchez-García et al., 2003, 2008, 2016, 2019; Díez-Montes et al., 2010). Finally, other granites not considered here of Tremadocian age have been reported in the southern Central Iberian Zone, such as the Oledo Massif and the Beira Baixa–central Extremadura, which display an I-type affinity (Antunes et al., 2009; Rubio Ordóñez et al., 2012). These granites could represent different sources for the Ordovician magmatism in the Central Iberian Zone.

Sánchez-García et al. (2019) have proposed that the anomaly that produced the large magmatism throughout the Iberian Massif could have migrated from the rifting axis to inward zones, and the acidic, peraluminous, K-rich rocks of Mid Ordovician age should represent the initial stages of a new rifting pulse, resembling the peraluminous rocks of the Early Rift Event (sensu Sánchez-García et al., 2003) from the Cambrian Epoch 2 of the Ossa-Morena Rift.

In the parautochthon of the Galicia–Trás-os-Montes Zone, the appearance of tholeiitic and alkaline–peralkaline magmatism in the Middle Ordovician would signal the first steps toward extensional conditions (Díez Fernández et al., 2012; Dias da Silva et al., 2016). In the Montagne Noire and the Mouthoumet massifs, contemporaneous tholeiitic lava indicates a similar change in the tectonic regimen (Álvaro et al., 2016). This gradual change in geodynamic conditions is also marked by the appearance of rocks with extensional characteristics in some of the subgroups considered here, such as the Central Iberian Zone (San Sebastián orthogneisses), Eastern Pyrenees (Casemí orthogneisses and G1), volcanic rocks of the Occitan Domain, and the orthogneisses and volcanic rocks from Sardinia.

6.2 Sardic phase

In the Eastern Pyrenees, two peaks of Ordovician magmatic activity are observed (Casas et al., 2019). Large Lower–Middle Ordovician peraluminous granite bodies are known, representing the protoliths of numerous gneissic bodies with laccolithic morphologies. In the Canigó Massif, the Upper Ordovician granite bodies (protoliths of Cadí and Casemí, G1) are encased in sediments of the Canaveilles and Jujols groups. During this time span, there was generalized uplift and erosion that culminated with the onset of the Sardic unconformity. The Sardic phase was succeeded by an extensional interval related to the formation of normal faults affecting the pre-unconformity strata (Puddu et al., 2018, 2019). The volcanic-arc signature can be explained by crustal recycling (Navidad et al., 2010; Casas et al., 2010; Martínez et al., 2011), as in the case of the Toledanian phase in the Central Iberian Zone, although, according to Casas et al. (2019), the Pyrenees and the Catalan Coastal Range were probably fringing the Gondwana margin in a different position than that occupied by the Iberian Massif. As a whole, the Ordovician magmatism in the Pyrenees lasted about 30 million years, from ca. 477 to 446 Ma, in a time span contemporaneous with the formation of the Sardic unconformity (Fig. 2). Recently, Puddu et al. (2019) proposed that a thermal doming, bracketed between 475 and 450 Ma, could have stretched the Ordovician lithosphere. The emersion and denudation of the inherited Cambrian–Ordovician palaeorelief would have given rise to the onset of the Sardic unconformity. According to these authors, thermal doming triggered by hot mafic magma underplating may also be responsible for the late Early–Late Ordovician coeval magmatic activity.

In the Occitan Domain, there was a dramatic volcanic event in early Tremadocian times, with the uprising of basin floors and the subsequent effusion of abundant rhyolitic activities under subaerial explosive conditions (Larroque volcanosedimentary complex in the Montagne Noire and Davejean acidic volcanic counterpart in the Mouthoumet Massif). Pouclet el al. (2017) interpreted this as a delayed Ollo de Sapo-style outpouring where a massive crustal melting required a rather significant heat supply. Asthenospheric upwelling leading to the interplay of lithospheric doming, continental break-up and decompression-driven mantle melting can explain such a great thermal anomaly. The magmatic products accumulated on the mantle–crust contact would provide enough heat transfer for crustal melting (Huppert and Sparks, 1988). Subsequently, a post-Sardic reactivation of rifting conditions is documented in the Cabrières klippes (southern Montagne Noire) and the Mouthoumet Massif. There, a Late Ordovician fault-controlled subsidence linked to the record of rift-related tholeiites (Roque de Bandies and Villerouge formations) was contemporaneous with the record of the Hirnantian glaciation (Álvaro et al., 2016). Re-opening of rifting branches (Montagne Noire and Mouthoumet massifs) was geometrically recorded as onlapping patterns and final sealing of Sardic palaeoreliefs by Silurian and Lower Devonian strata.

Sardinia illustrates an almost complete record of the Variscan Belt (Carmignani et al., 1994; Rossi et al., 2009). Some plutonic orthogneisses of the inner zone belong to this cycle, such as the orthogneisses of Golfo Aranci (Giacomini et al., 2006). Gaggero et al. (2012) described three magmatic cycles. The first cycle is well represented in the Sarrabus unit by Furongian–Tremadocian volcanic and subvolcanic interbeds within a terrigenous succession (San Vito Formation) which is topped by the Sardic unconformity. Some plutonic orthogneisses of the inner zone belong to this cycle, such as the orthogneisses of Golfo Aranci (Giacomini et al., 2006) and the orthogneiss of Punta Bianca (PB). The second Middle Ordovician cycle, postdating the previous cycle by about 50 million years, is of a volcanic-arc type with calc-alkaline affinity and acidic-to-intermediate composition. The acidic metavolcanites are referred to in the literature as “porphyroids”, which crop out in the external nappe zone and some localities of the inner zone. The intermediate-to-basic byproducts are widespread in central Sardinia (Serra Tonnai Formation). Some plutonic rocks (Mt Filau orthogneisses and Capo Spartivento) of the second cycle are discussed above. The third cycle consists of alkalic meta-epiclastites interbedded in post-Sandbian strata and metabasites marking the Ordovician–Silurian contact and reflecting rifting conditions. In this work only the first two cycles are considered. Giacomini et al. (2006) cite coeval mafic rocks of felsic magmatism of Mid-Ordovician age (Cortesogno et al., 2004; Palmeri et al., 2004; Giacomini et al., 2005), although they interpret a subduction scenario of the Hun terrain below Corsica and Sardinia in the Mid-Ordovician.

6.3 Origin of intracrustal siliceous melts

In this scenario, the key to generating large volumes of acidic rocks in an intraplate context would be the existence of a lower–middle crust, highly hydrated, in addition to a high-heat flow, possibly caused by mafic melts (Bryan et al., 2002; Díez-Montes, 2007). This could be the scenario initiated by the arrival of a thermal anomaly in a subduction-free area (Sánchez-García et al., 2003, 2008, 2019; Álvaro et al., 2016). The formation of large volumes of intracrustal siliceous melts could act as a viscous barrier, preventing the rise of mafic magmas within volcanic environments and causing the underplating of these magmas at the contact between the lower crust and the mantle (Huppert and Sparks, 1988; Pankhurst et al., 1998; Bindeman and Valley, 2003). The cooling of these magmas could lead to crustal thickening, and in this case the volcanic-arc signature can be explained by crustal recycling (Navidad et al., 2010; Díez-Montes et al., 2010; Martínez et al., 2011).

Sánchez-García et al. (2019) have proposed that the anomaly that produced the large magmatism throughout the Iberian Massif could have migrated from the rifting axis to inward zones, and the acidic, peraluminous, K-rich rocks of Mid Ordovician age should represent the initial stages of a new rifting pulse, resembling the peraluminous rocks of the Early Rift Event (sensu Sánchez-García et al., 2003) from the Cambrian Epoch 2 of the Ossa-Morena Rift. In the parautochthon of the Galicia–Trás-os-Montes Zone, the appearance of tholeiitic and alkaline–peralkaline magmatism in the Middle Ordovician would signal the first steps toward extensional conditions (Díez Fernández et al., 2012; Dias da Silva et al., 2016). In the Montagne Noire and the Mouthoumet massifs, contemporaneous tholeiitic lava indicates a similar change in the tectonic regimen (Álvaro et al., 2016). This change in geodynamic conditions is also marked by the appearance of rocks with extensional characteristics in some of the subgroups considered here, such as the Central Iberian Zone (San Sebastián orthogneisses), Eastern Pyrenees (Casemí orthogneisses and G1), volcanic rocks of the Occitan Domain, and the orthogneisses and volcanic rocks from Sardinia. In the Pyrenees, Puddu et al. (2019) proposed that a thermal doming, between 475 and 450 Ma, should have stretched the Ordovician lithosphere, leading to emersion and denudation of a Cambrian–Ordovician palaeorelief and giving rise to the onset of the Sardic unconformity. According to these authors, thermal doming triggered by hot mafic magma underplating may also be responsible for the late Early–Late Ordovician coeval magmatic activity

A major continental break-up, leading to the so-called Tremadocian Tectonic Belt, was suggested by Pouclet et al. (2017), which was initiated by upwelling of the asthenosphere and tectonic thinning of the lithosphere. Mantle-derived mafic magmas were underplated at the mantle–crust transition zone and intruded the crust. These magmas provided heat for crustal melting, which supplied the rhyolitic volcanism. After emptying the rhyolitic crustal reservoirs, the underlying mafic magmas finally rose and reached the surface. According to Pouclet et al. (2017), the acidic magmatic output associated with the onset of the Larroque metarhyolites resulted in massive crustal melting requiring a rather important heat supply. Asthenospheric upwelling leading to lithospheric doming, continental break-up, and decompression-driven mantle melting can explain such a great thermal anomaly. Magmatic products accumulated on the mantle–crust contact, providing enough heat transfer for crustal melting.

7 Conclusions
Back to toptop

A geochemical comparison of 231 plutonic and volcanic samples of 2 major suites, Furongian–Mid Ordovician and Late Ordovician in age, from the Central Iberian and Galicia–Trás-os-Montes zones of the Iberian Massif and in the Eastern Pyrenees, the Occitan Domain (Albigeois, Montagne Noire and Mouthoumet massifs) and Sardinia points to a predominance of materials derived from the melting of metasedimentary rocks, peraluminous and rich in SiO2 and K2O. The total content in REE is moderate to high. Most felsic rocks display similar chondrite-normalized REE patterns, with an enrichment of LREE relative to HREE, which should indicate the involvement of crustal materials in their parental magmas.

Zr  TiO2, Zr  Nb, Nb  Y and Zr vs. Ga  Al ratios, and REE and εNd values reflect contemporaneous arc and extensional scenarios, which progressed to distinct extensional conditions finally associated with outpouring of mafic tholeiite-dominant rifting lava flows. Magmatic events are contemporaneous with the formation of the Toledanian (Furongian–Early Ordovician) and Sardic (Early–Late Ordovician) unconformities, related to neither metamorphism nor penetrative deformation. The geochemical and structural framework precludes subduction-generated melts reaching the crust in a magmatic arc-to-back-arc setting. On the contrary, it favours partial melting of sediments and/or granitoids in a lower continental crust triggered by the underplating of hot mafic magmas related to the opening of the Rheic Ocean as a result of asthenospheric upwelling.

Data availability
Back to toptop
Data availability. 

All data are included in the paper and in the Supplement.

Back to toptop

The supplement related to this article is available online at:

Author contributions
Back to toptop
Author contributions. 

JJA, TSG and JMC led the methodology and wrote, reviewed and edited the original draft. CP, ADM, ML and GO supported the same processes.

Competing interests
Back to toptop
Competing interests. 

The authors declare that they have no conflict of interest.

Special issue statement
Back to toptop
Special issue statement. 

This article is part of the special issue “The Iberian Massif in the frame of the European Variscan Belt”. It is not associated with a conference.

Back to toptop

The authors thank Laura Gaggero (Genoa, Italy) and Jochen Mezger (Fairbanks, USA) for their constructive and useful revisions. This paper is a contribution to IGCP project 683. We acknowledge support regarding the publication fee by the CSIC Open Access Publication Support Initiative through its Unit of Information Resources for Research (URICI).

Financial support
Back to toptop
Financial support. 

This research has been supported by the Spanish Ministry of Science and Innovation (grant nos. CGL2017-87631-P and PGC2018-093903-B-C22), and the CSIC Open Access Publication Support Initiative through its Unit of Information Resources for Research (URICI).

Review statement
Back to toptop
Review statement. 

This paper was edited by Juan Gómez-Barreiro and reviewed by Jochen Mezger and Laura Gaggero.

Back to toptop

Álvaro, J. J. and Vizcaïno, D.: The Furongian break-up (rift-drift) transition in the Anti-Atlas, Morocco, J. Iberian Geol., 44, 567–587,, 2018. 

Álvaro, J. J., Ferretti, F., González-Gómez, C., Serpagli, E., Tortello, M. F., Vecoli, M., and Vizcaïno, D.: A review of the Late Cambrian (Furongian) palaeogeography in the western Mediterranean region, NW Gondwana, Earth-Sci. Rev., 85, 47–81,, 2007. 

Álvaro, J. J., Ezzouhairi, H., Ribeiro, M. L., Ramos, J. F., and Solá, A. R.: Early Ordovician volcanism of the Iberian Chains (NE Spain) and its influence on preservation of shell concentrations, Bull. Soc. géol. Fr., 179, 569–581,, 2008. 

Álvaro, J. J., Bellido, F., Gasquet, D., Pereira, F., Quesada, C., and Sánchez-García, T.: Diachronism of late Neoproterozoic-Cambrian arc-rift transition of North Gondwana: a comparison of Morocco and the Iberian Ossa-Morena Zone, J. Afr. Earth Sci., 98, 113–132,, 2014a. 

Álvaro, J. J., Bauluz, B., Clausen, S., Devaere, L., Gil Imaz, A., Monceret, E., and Vizcaïno, D.: Stratigraphy of the Cambrian-Lower Ordovician volcanosedimentary complexes, northern Montagne Noire, France, Stratigraphy, 11, 83–96, (last access: 30 November 2020), 2014b. 

Álvaro, J. J., Colmenar, J., Monceret, E., Pouclet, A., and Vizcaïno, D.: Late Ordovician (post-Sardic) rifting branches in the North Gondwanan Montagne Noire and Mouthoumet massifs of southern France, Tectonophysics, 681, 111–123,, 2016. 

Álvaro, J. J., Casas, J. M., Clausen, S., and Quesada, C.: Early Palaeozoic geodynamics in NW Gondwana, J. Iberian Geol., 44, 551–565, 2018. 

Álvaro, J. J., Cortijo, I., Jensen, S., Lorenzo, S., Palacios, T., and Pieren, A.: Updated stratigraphic framework and biota of the Ediacaran and Terreneuvian in the Alcudia-Toledo Mountains of the Central Iberian Zone, Spain, Est. Geol., 75, e093,, 2019. 

Álvaro, J. J., Casas, J. M., and Quesada, C.: Reconstructing the pre-Variscan puzzle of Cambro-Ordovician basement rocks in the southwestern European margin of Gondwana, in: Pannotia to Pangaea: Neoproterozoic and Paleozoic Orogenic Cycles in the Circum-Atlantic Regional, edited by: Murphy, J. B., Strachan, R., and Quesada, C., Geological Society London Special Publications, London, UK,, 2020. 

Antunes, I. M. H. R., Neiva, A. M. R., Silva, M. M. V. G., and Corfu, F.: The genesis of I- and S-type granitoid rocks of the Early Ordovician Oledo pluton, Central Iberian Zone (central Portugal), Lithos, 111, 168–185,, 2009. 

Arthaud, F.: Etude tectonique et microtectonique comparée de deux domaines hercyniens: les nappes de la Montagne Noire (France) et l'anticlinorium de l'Iglesiente (Sardaigne), PhD thesis, University of Montpellier, France, 178 pp., 1970. 

Ayora, C.: Les concentrationes metàlliques de la Vall de Ribes. PhD thesis, University of Barcelona, Spain, 248 pp., 1980. 

Ballèvre, M., Fourcade, S., Capdevila, R., Peucat, J. J., Cocherie, A., and Mark Fanning, C.: Geochronology and geochemistry of Ordovician felsic volcanism in the Southern Armorican Massif (Variscan belt, France): Implications for the breakup of Gondwana, Gondwana Res., 21, 1019–1036,, 2012. 

Barca, S.: Phénomènes de resédimentation et flysch hercynien à faciès Culm dans le “synclinal du Sarrabus” (SE de la Sardaigne, Italie), C. R. Acad. Sci., 313, 1051–1057, 1991. 

Barca, S. and Cherchi, A.: Regional geological setting, in: Sardinian Palaeozoic Basement and its Meso–Cainozoic Cover (Italy), edited by: Barca, S. and Cherchi, A., 32nd Int. Geol. Congress. Field Trip Guide Book, 3–8, 2004. 

Barca, S., Cocozza, T., Del Rio, M., Pillola, G. L., and Pittau Demelia, P.: Datation de l'Ordovicien inférieur par Dictyonema flabelliforme et acritarches dans la partie supérieure de la formation “cambrienne” de Cabitza (SW de la Sardaigne, Italie): conséquences géodynamiques, C. R. Acad. Sci., 305, 1109–1113, 1987. 

Barca, S., Del Rio, M., and Pittau Demelia, P.: New geological and stratigraphical data and discovery of Lower Ordovician acritarchs in the San Vito Sandstone of the Genn'Argiolas Unit (Sarrabus, Southeastern Sardinia), Riv. It. Paleontol. Stratigr., 94, 339–360, 1988. 

Bea, F., Montero, P., Talavera, C., and Zinger, T.: A revised Ordovician age for the Miranda do Douro orthogneiss, Portugal. Zircon U-Pb ion-microprobe and LA-ICPMS dating, Geol. Acta, 4, 395–401, 2006. 

Bea, F., Montero, P., González Lodeiro, F., and Talavera, C.: Zircon inheritance reveals exceptionally fast crustal magma generation processes in Central Iberia during the Cambro-Ordovician, J. Petrol., 48, 2327–2339,, 2007. 

Bé Mézème, E.: Contribution de la géochronologie U-Th-Pb sur monazite à la compréhension de la fusion crustale dans la chaîne Hercynienne française et implication géodynamique, PhD thesis, University of Orléans, France, 250 pp., 2005. 

Bindeman, I. N. and Valley, J. W.: Rapid generation of both high- and low-δ18O, large-volume silicic magmas at the Timber Mountain/Oasis Valley caldera complex, Nevada, Geol. Soc. Am. Bull., 115, 581–595,<0581:RGOBHA>2.0.CO;2, 2003. 

Boni, M.: The Permo-Triassic vein and paleokarst ores in southwest Sardinia: contribution of fluid inclusion studies to their genesis and paleoenvironment, Mineral. Deposita, 21, 53–62, 1986. 

Boni, M. and Koeppel, V.: Ore-lead isotope pattern from the Iglesiente-Sulcis area (SW Sardinia) and the problem of remobilization of metals, Mineral. Deposita, 20, 185–193, 1985. 

Bryan, S. E., Riley, T. R., Jerram, D. A., Stephens, C. J., and Leat, P. T.: Silicic volcanism: An undervalued component of large igneous provinces and volcanic rifted margins, in: Volcanic Rifted Margins, edited by: Menzies, M. A., Klemperer, S. L., Ebinger, C. J., and Baker, Geological Society of America Special Publication, Boulder, Colorado, USA, 99–120,, 2002. 

Calvet, P., Lapierre, H., and Chavet, J.: Diversité du volcanisme Ordovicien dans la région de Pierrefitte (Hautes Pyrénées): rhyolites calco-alcalines et basaltes alcalins, C. R. Acad. Sci., 307, 805–812, 1988. 

Calvino, F.: Note Illustrative della Carta Geologica d'Italia, Muravera. Servizio Geologico d'Italia, Roma, Foglio 227, 1972. 

Carmignani, L., Cocozza, T., Ghezzo, C., Pertusati, P. C., and Ricci, C. A.: Guide-book to the Excursion on the Palaeozoic Basement of Sardinia, IGCP, Paris, France, 1986. 

Carmignani, L., Pertusati, P. C., Barca, S., Carosi, R., Di Pisa, A., Gattiglio, M., Musumeci, G., and Oggiano, G.: Struttura della catena ercinica in Sardegna, Guida all'escursione del Gruppo Informali di Geologia Strutturale in Sardegna, Centrooffset Siena, Italy, 1992. 

Carmignani, L., Carosi, R., Di Pisa, A., Gattiglio, M., Musumeci, G., Oggiano, G., and Pertusati, P.: The hercynian chain in Sardinia (Italy), Geodin. Acta, 7, 31–47,, 1994. 

Carmignani, L., Oggiano, G., Barca, S., Conti, P., Salvadori, I., Eltrudis, A., Funedda, A., and Pasci, S.: Geologia della Sardegna, Note illustrative della Carta Geologica della Sardegna a scala 1:200.000, Memorie Descrittive della Carta Geologica d'Italia, Servizio Geologico, Instituto Poligrafico e Zecca dello Stato, Roma, 2001. 

Caron, C., Lancelot, J., Omenetto, P., and Orgeval, J. J.: Role of the Sardic tectonic phase in the metallogenesis of SW Sardinia (Iglesiente): lead isotope evidence, European J. Miner., 9, 1005–1016, 1997. 

Casas, J. M.: Ordovician deformations in the Pyrenees: new insights into the significance of pre–Variscan (“sardic”) tectonics, Geol. Mag., 147, 674–689,, 2010. 

Casas, J. M. and Fernández, O.: On the Upper Ordovician unconformity in the Pyrenees: New evidence from the La Cerdanya area, Geol. Acta, 5, 193–198,, 2007. 

Casas, J. M. and Murphy, J. B.: Unfolding the arc: the use of pre-orogenic constraints to assess the evolution of the Variscan belt in Western Europe, Tectonophysics, 736, 47–61,, 2018. 

Casas, J. M. and Palacios, T.: First biostratigraphical constraints on the pre-Upper Ordovician sequences of the Pyrenees based on organic-walled microfossils, C. R. Geosci., 344, 50–56,, 2012. 

Casas, J. M., Castiñeiras, P., Navidad, M., Liesa, M., and Carreras, J.: New insights into the Late Ordovician magmatism in the Eastern Pyrenees: U-Pb SHRIMP zircon data from the Canigó massif, Gondwana Res., 17, 317–324,, 2010. 

Casas, J. M., Álvaro, J. J., Clausen, S., Padel, M., Puddu, C., Sanz-López, J., Sánchez-García, T., Navidad, M., Castiñeiras, P., and Liesa, M.: Palaeozoic basement of the Pyrenees, in: The Geology of Iberia: A Geodynamic Approach, edited by: Quesada, C. and Oliveira, J. T., Springer, Heidelberg, Germany, 229–259, 2019. 

Castiñeiras, P., Villaseca, C., Barbero, L., and Martín-Romera, C.: SHRIMP U-Pb zircon dating of anatexis in high-grade migmatite complexes of Central Spain: implications in the Hercynian evolution of Central Iberia, Int. J. Earth Sci., 97, 35–50,, 2008a. 

Castiñeiras, P., Navidad, M., Liesa, M., Carreras, J., and Casas, J. M.: U-Pb zircon ages (SHRIMP) for Cadomian and Lower Ordovician magmatism in the Eastern Pyrenees: new insights in the pre-Variscan evolution of the northern Gondwana margin, Tectonophysics, 46, 228–239,, 2008b. 

Castro, A., García-Casco, A., Fernández, C., Corretgé, L. G., Moreno-Ventas, I., Gerya, T., and Löw, I.: Ordovician ferrosilicic magmas: experimental evidence for ultrahigh temperaturas affecting a metagreywacke source, Gondwana Res., 16, 622–632,, 2009. 

Charles, N., Faure, M., and Chen, Y.: The emplacement of the Montagne Noire axial zone (French Massif Central): New insights from petro-textural, geochronological and AMS studies, 22ème Réunion des Sciences de la Terre, Nancy, France, 155, 2008. 

Charles, N., Faure, M., and Chen, Y.: The Montagne Noire migmatitic dome emplacement (French Massif Central): New insights from petrofabric and AMS studies, J. Struct. Geol., 31, 1423–1440,, 2009. 

Clariana, P., Valverde-Vaquero, P., Rubio-Ordóñez, A., Beranoaguirre, A., and García-Sansegundo, J.: Pre-Variscan tectonic events and Late Ordovician magmatism in the Central Pyrenees: U-Pb age and Hf in zircon isotopic signature from subvolcanic sills in the Pallaresa massif, J. Iberian Geol., 44, 589–601,, 2018. 

Cocco, F. and Funedda, A.: New data on the pre-Middle Ordovician deformation in SE Sardinia: a preliminary note, Rend. online Soc. Geol. It., 15, 34–36, 2011. 

Cocco, F. and Funneda, A.: The Sardic Phase: field evidence of Ordovician tectonics in SE Sardinia, Italy, Geol. Mag., 156, 25–38,, 2017. 

Cocco, F., Oggiano, G. Funedda, A., Loi, A., and Casini, L.: Stratigraphic, magmatic and structural features of Ordovician tectonics in Sardinia (Italy): a review, J. Iberian Geol., 44, 619–639,, 2018. 

Cocherie, A.: Datation avec le SHRIMP II du métagranite oeillé du Somail-Montagne Noire, C. R. technique ANA–ISO/NT, repport of the French Geological Survey (BRGM), 2003. 

Cocherie, A., Baudin, T., Guerrot, C., Autran, A., Fanning, M. C., and Laumonier, B.: U-Pb zircon (ID-TIMS and SHRIMP) evidence for the early Ordovician intrusion of metagranites in the late Proterozoic Canaveilles Group of the Pyrenees and the Montagne Noire (France), Bull. Soc. Géol. France, 176, 269–282,, 2005. 

Cortesogno, L., Gaggero, L., Oggiano, G., and Paquette, J. L.: Different tectono-thermal evolution paths in eclogitic rocks from the Axial Zone of the Variscan Chain in Sardinia (Italy) compared with the Ligurian Alps, Ofioliti, 29, 125–144, 2004. 

Costamagna, L. G., Elter, F. M., Gaggero, L., and Mantovani, F.: Contact metamorphism in Middle Ordovician arc rocks (SW Sardinia, Italy): New paleogeographic constraints, Lithos, 264, 577–593,, 2016. 

Cruciani, G., Franceschelli, M., Musumeci, G., Spano, M. E., and Tiepolo, M.: U-Pb zircon dating and nature of metavolcanics and metarkoses from the Monte Grighini Unit: new insights on Late Ordovician magmatism in the Variscan belt in Sardinia, Italy, Int. J. Earth Sci., 102, 2077–2096,, 2013. 

Cruciani, G., Franceschelli, M., Puxeddu, M., and Tiepolo, M.: Metavolcanics from Capo Malfatano, SW Sardinia, Italy: New insight on the age and nature of Ordovician volcanism in the Variscan foreland zone, Geol. J., 53, 1573–1585,, 2018. 

Demange, M.: Evolution tectonique de la Montagne noire: un modèle en transpression, C. R. Acad. Sci., 329, 823–829, 1999. 

Demange, M., Guérangé-Lozes, J., and Guérangé, B.: Notice explicative de la feuille de Lacaune (987) au 1:50 000, BRGM, Orléans, 1996. 

Denèle, Y., Barbey, P., Deloule, E., Pelleter, E., Olivier, P., and Gleizes, G.: Middle Ordovician U-Pb age of the Aston and Hospitalet orthogneissic laccoliths: their role in the Variscan evolution of the Pyrenees, Bull. Soc. Géol. France, 180, 209–221,, 2009. 

DePaolo, D. J.: Neodymiun isotopes in the Colorado Front Range and crust-mantle evolution in the Proterozoic, Nature, 291, 193–196,, 1981. 

DePaolo, D. J.: Neodymium isotope geochemistry, An introduction, Springer, Berlin, Germany, 1988. 

DePaolo, D. J. and Wasserburg, G. J.: Nd isotopic variations and petrogenetic models, Geophys. Res. Lett., 3, 249–252, 1976. 

Dias da Silva, Í.: Geología de las Zonas Centro Ibérica y Galicia-Tras-os-Montes en la pate oriental del Complejo de Morais, Portugal/España, Serie Nova Terra, Laboratorio Xeolóxico de Laxe, A Coruña, 45, 1–424, 2014. 

Dias da Silva, I., Valverde-Vaquero, P., González-Clavijo, E., Díez-Montes, A., and Martínez-Catalán, J. R.: Structural and stratigraphical significance of U-Pb ages from the Saldanha and Mora volcanic complexes (NE Portugal, Iberian Variscides), Géol. France, 1, 105–106,, 2012. 

Dias da Silva Í., Valverde-Vaquero, P., González Clavijo, E., Díez-Montes, A., and Martínez Catalán, J. R.: Structural and stratigraphical significance of U-Pb ages from the Mora and Saldanha volcanic complexes (NE Portugal, Iberian Variscides), in: The Variscan Orogeny: Extent, Timescale and the Formation of the European Crust, edited by: Schulmann, K., Martínez Catalán, J. R., Lardeaux, J. M., Janousek, V., and Oggiano, G., Geological Society of London Special Publications, London, UK, 115–135,, 2014. 

Dias da Silva, I., Díez Fernández, R., Díez Montes, A., González Clavijo, E., and Foster, D. A.: Magmatic evolution in the N-Gondwana margin related to the opening of the Rheic Ocean – evidence from the Upper Parautochthon of the Galicia-Trás-os-Montes Zone and from the Central Iberian Zone (NW Iberian Massif), Int. J. Earth Sci., 105, 1127–1151,, 2016. 

Díaz-Alvarado, J., Fernández, C., Chichorro, M., Castro, A., and Pereira, M. F.: Tracing the Cambro-Ordovician ferrosilicic to calc-alkaline magmatic association in Iberia by in situ U-Pb SHRIMP zircon geochronology (Gredosmassif, Spanish Central System batholith), Tectonophysics, 681, 95–110,, 2016. 

Díez Balda, M. A., Vegas, R., and González Lodeiro, F.: Central Iberian Zone, Structures, in: Pre-Mesozoic Geology of Iberia, edited by: Dallmeyer, R. D. and Martínez García, E. Springer, Berlin, Germany, 172–188, 1990. 

Díez Fernández, R., Castiñeiras, P., and Gómez Barreiro, J.: Age constraints on Lower Paleozoic convection system: Magmatic events in the NW Iberian Gondwana margin, Gondwana Res., 21, 1066–1079,, 2012. 

Díez-Montes, A.: La Geología del Dominio “Ollo de Sapo” en las Comarcas de Sanabria y Terra do Bolo, PhD thesis, University of Salamanca, Spain, 506 pp., 2007. 

Díez Montes, A., Martínez Catalán, J. R., and Bellido Mulas, F.: Role of the Ollo de Sapo massive felsic volcanism of NW Iberia in the Early Ordovician dynamics of northern Gondwana, Gondwana Res., 17, 363–376,, 2010. 

Di Pisa, A., Gattiglio, M., and Oggiano, G.: Pre-Hercynian magmatic activity in the nappe zone (internal and external) of Sardinia: evidence of two within plate basaltic cycles, in: Contributions to the Geology of Italy with Special Regard to the Paleozoic Basements, edited by: Carmingnani, L. and Sassi, F. P., Newsl. IGCP, University of Siena, Siena, 276, 107–116, 1992. 

Echtler, H. and Malavieille, J.: Extensional tectonics, basement uplift and Stephano-Permian collapse basin in a late Variscan metamorphic core complex (Montagne Noire, southern Massif Central), Tectonophysics, 177, 125–138,, 1990. 

El Korh, A., Schmidt, S. T., Ballèvre, M., Ulianov, A., and Bruguier, O.: Discovery of an albite gneiss from the Ile de Groix (Armorican Massif, France): geochemistry and LA-ICP-MS U-Pb geochronology of its Ordovician protolith, Int. J. Earth Sci., 101, 1169–1190,, 2012. 

Engel, W., Feist, R., and Franke, W.: Le Carbonifère anté-stéphanien de la Montagne Noire: rapports entre mise en place des nappes et sédimentation, Bull. BRGM, 2, 341–389, 1980. 

Elter, F. M., Francescherelli, M., Ghezzo, C., Memmi, I., and Ricci, C. A.: The geology of northern Sardinia, IGCP Project n. 5 Newsletter, 87–102, 1986. 

Farias, P., Ordoñez-Casado, B., Marcos, A., Rubio-Ordóñez, A., and Fanning, C. M.: U-Pb zircon SHRIMP evidence for Cambrian volcanism in the Schistose Domain within the Galicia-Trás-os-Montes Zone (Variscan Orogen, NW Iberian Peninsula), Geol. Acta, 12, 209–218,, 2014. 

Faure, M., Ledru, P., Lardeaux, J. M., and Matte, P.: Paleozoic orogenies in the French Massif Central. A cross section from Béziers to Lyon, 32nd Int. Geol. Congress Florence, Italy, 20–28 August 2004, B22, B16–B33, 2004. 

Feist, R. and Galtier, J.: 1985. Découverte de flores d'âge namurien probable dans le flysch à olistolithes de Cabrières (Hérault). Implications sur la durée de la sédimentation synorogénique dans la Montagne Noire (France Méridionale), C. R. Acad. Sci., 300, 207–212, 1985. 

Franz, L. and Romer, R. L.: Caledonian high-pressure metamorphism in the Strona-Ceneri-Zone (Southern Alps of southern Switzerland and northern Italy), Swiss J. Geosci., 100, 457–467,, 2007. 

Friedl, G., Finger, F., Paquette, J. L., von Quadt, A., McNaughton, N. J., and Fletcher, I. R.: Pre-Variscan geological events in the Austrian part of the Bohemian Massif deduced from U-Pb zircon ages, Int. J. Earth Sci., 93, 802–823,, 2004. 

Funedda, A. and Oggiano, G.: Outline of the Variscan basement of Sardinia, in: The Silurian of Sardinia, Volume in Honour of Enrico Serpagli, edited by: Corradini, C., Ferretti, A., and Štorch, P., Rendiconti della Società Paleontologica Italiana, Roma, 23–35, 2009. 

Gaggero L., Oggiano G., Funedda A., and Buzzi, L.: Rifting and arc-related Early Paleozoic volcanism along the North Gondwana margin: Geochemical and geological evidence from Sardinia (Italy), J. Geol., 120, 273–292,, 2012. 

García-Arias, M., Díez-Montes, A., Villaseca, C., and Blanco-Quintero, I. F.: The Cambro-Ordovician Ollo de Sapo magmatism in the Iberian Massif and its Variscan evolution: A review, Earth-Sci. Rev., 176, 345–372,, 2018. 

Gèze, B.: Etude géologique de la Montagne Noire et des Cévennes méridionales, Mém. Soc. géol. France, Paris, 62, 1–215, 1949. 

Giacomini, F., Bomparola, R. M., and Ghezzo, C.: Petrology and geochronology of metabasites with eclogite facies relics from NE Sardinia: constraints for the Palaeozoic evolution of Southern Europe, Lithos, 82, 221–248,, 2005. 

Giacomini, F., Bomparola, R. M., Ghezzo, C., and Guldbransen, H.: The geodynamic evolution of the Southern European Variscides: constraints from the U/Pb geochronology and geochemistry of the lower Palaeozoic magmatic-sedimentary sequences of Sardinia (Italy), Contrib. Miner. Petr., 152, 19–42,, 2006. 

Guérangé-Lozes, J. and Alabouvette, B.: Notice explicative, Carte géol. France (1/50 000), feuille Saint-Sernin-sur-Rance (960), BRGM, Orléans, 1999. 

Guérangé-Lozes, J. and Alsac, C.: Les nappes varisques de l'Albigeois cristallin. Lithostratigraphie, volcanisme et déformations, Géol. France, 3, 309–337, 1986. 

Guérangé-Lozes, J., Guérangé, B., Mouline, M. P., and Delsahut, B.: Notice explicative, Carte géol. France (1/50 000), feuille Réalmont (959), BRGM, Orléans, 1996. 

Guitard, G.: Le métamorphisme hercynienmésozonal et les gneiss oeillés du masif du Canigou (Pyrénées orientales), Mém. BRGM, 63, 1–353, 1970. 

Gutiérrez-Alonso, G., Fernández-Suárez, J., Gutiérrez-Marco, J. C., Corfu, F., Murphy, J. B., and Suárez Martínez, S.: U-Pb depositional age for the upper Barrios Formation (Armorican Quartzite facies) in the Cantabrian zone of Iberia: implications for stratigraphic correlation and paleogeography, in: The Evolution of the Rheic Ocean: from Avalonian-Cadomian Active Margin to Alleghenian-Variscan Collision, edited by: Linnemann, R. D., Nance, P., and Kraft, G. Z., The Geological Society London, UK, 287–296,, 2007. 

Gutiérrez-Alonso, G., Gutiérrez-Marco, J. C., Fernández-Suárez, J., Bernárdez, E., and Corfu, F.: Was there a super-eruption on the Gondwanan coast 477Ma ago?, Tectonophysics, 681, 85–94,, 2016. 

Gutiérrez-Marco, J. C., Robardet, M., Rábano, I., Sarmiento, G., San José Lancha, M. A., Herranz Araújo, P., and Pieren Vidal, A.: Ordovician, in: The Geology of Spain, edited by: Gibbons, W. and Moreno, The Geological Society, London, UK, 31–49, 2002. 

Gutiérrez-Marco, J. C., Piçarra, J. M., Meireles, C. A., Cózar, P., García-Bellido, D. C., Pereira, Z., Vaz, N., Pereira, S., Lopes, G., Oliveira, J. T., Quesada, C., Zamora, S., Esteve, J., Colmenar, J., and Bernárdez, E.: Early Ordovician-Devonian passive margin stage in the Gondwanan units of the Iberian massif, in: The Geology of Iberia: A Geodynamic Approach, edited by: Quesada, C. and Oliveira, Springer, Heidelberg, Germany, 75–98,, 2019. 

Hartevelt, J. J. A.: Geology of the upper Segre and Valira valleys, central Pyrenees, Andorra/Spain, Leid. Geol. Meded., 45, 167–236, 1970. 

Helbing, H. and Tiepolo, M.: Age determination of Ordovician magmatism in NE Sardinia and its bearing on Variscan basement evolution, J. Geol. Soc., 162, 689–700, , 2005. 

Huppert, H. E. and Sparks, R. S. J.: The generation of granitic magmas by intrusion of basalt into continental crust, J. Petrol., 29, 599–624, 1988. 

Ibrahim, M. E., El-Kalioby, B. A., Aly, G. M., El-Tohamy, A. M., and Watanabe, K.: Altered granitic rocks, Nusab El Balgum Area, Southwestern Desert, Egypt, Mineralogical and geochemical aspects of REEs, Ore Geol. Rev., 70, 252–261,, 2015. 

Irber, W.: The lanthanide tetrad effect and its correlation with K/Rb, Eu/Eu*, Sr/Eu, Y/Ho, and Zr/Hf of evolving peraluminous granite suites, Geochim. Cosmochim. Ac., 63, 489–508,, 1999. 

Kröner, A. and Willner, A. P.: Time of formation and peak of Variscan HP-HT metamorphism of quartz-feldspar rocks in the central Erzgebirge, Saxony, Germany, Contrib. Mineral. Petrol., 132, 1–20,, 1998. 

Lancelot, J. Allegret, A., and Iglesias Ponce de León, M.: Outline of Upper Precambrian and Lower Paleozoic evolution of the Iberian Peninsula according to U-Pb dating of zircons, Earth Planet. Sci. Lett., 74, 325–337, 1985. 

Laske, R., Bechstädt, T., and Boni, M.: The post-Sardic Ordovician series, in: Sedimentological, stratigraphical and ore deposits field guide of the autochtonous Cambro-Ordovician of Southeastern Sardinia, edited by: Bechstädt, T. and Boni, M., Istituto Superiore per la Protezione e la Ricerca Ambientale, Roma, 115–146, 1994. 

Laumonier, B., Abad, A., Alonso, J. L., Baudelot, S., Bessière, G., Besson, M., Bouquet, C., Bourrouilh, R., Brula, P., Carreras, J., Centène, A., Courjault-Radé, R., Courtessole, R., Fauconnier, D., García-Sansegundo, J., Guitard, G., Moreno-Eiris, E., Perejón, A., and Vizcaïno, D.: Le Paléozoïque Inférieur, in: Synthèse géologique et géophysique des Pyrénées, edited by: Barnolas, A. and Chiron, J. C., BRGM and IGME, Paris and Madrid, 157–209, 1996. 

Leat, P. T., Jackson, S. E., Thorpe, R. S., and Stillman, C. J.: Geochemistry of bimodal basalt-subalkaline/peralkaline rhyolite provinces within the Southern British Caledonides, J. Geol. Soc., 143, 259–273, 1986. 

Le Corre, C., Auvray, B., Ballèvre, M., and Robardet, M.: Le Massif Armoricain, Sci. Géol., Bull., 44, 31–103, 1991. 

Lentz, D.: U, Mo and REE mineralization in late-tectonic granite pegmatites, south-west Grenville Province, Canada, Ore Geol. Rev., 11, 197–227,, 1996. 

Leone, F., Hamman, W., Laske, R., Serpagli, E., and Villas, E.: Lithostratigraphic units and biostratigraphy of the post-Sardic Ordovician sequence in south-west Sardinia, Boll. Soc. Paleontol. It., 30, 201–235, 1991. 

Leone, F., Ferretti, A., Hammann, W., Loi, A., Pillola, G. L., and Serpagli, E.: A general view of the post-Sardic Ordovician sequence from SW Sardinia, Rend. Soc. Paleontol. It., 1, 51–68, 2002. 

Lescuyer, J. L. and Cocherie, A.: Datation sur monozircons des métadacites de Sériès: arguments pour un âge protérozoïque terminal des “schistes X” de la Montagne Noire (Massif central français), C. R. Acad. Sci., 314, 1071–1077, 1992. 

Liesa, M., Carreras, J., Castiñeiras, P., Casas, J. M., Navidad, M., and Vilà, M.: U-Pb zircon age of Ordovician magmatism in the Albera Massif (Eastern Pyrenees), Geol. Acta, 9, 1–9,, 2011. 

Linnemann, U., Gehmlich, M., Tichomirowa, M., Buschmann, B., Nasdala, L., and Jonas, P., Lützner, H., and Bombach, K.: From Cadomian subduction to early Palaeozoic rifting: the evolution of Saxo-Thuringia at the margin of Gondwana in the light of single zircon geochronology and basin development (Central European Variscides, Germany), in: Orogenic Processes: Quantification and Modelling in the Variscan Belt, edited by: Franke, W., Haak, V., Oncken, O., and Tanner, D., The Geological Society London Special Publications, London. UK, 131–153,, 2000. 

Loi, A. and Dabard, M. P.: Zircon typology and geochemistry in the palaeogeographic reconstruction of the Late Ordovician of Sardinia (Italy), Sediment. Geol., 112, 263–279,, 1997. 

Loi, A., Barca, S., Chauvel, J. J., Dabard, M. P., and Leone, F.: Analyse de la sédimentation post-phase sarde les dépôts initiaux à placers du SE de la Sardaigne, C. R. Soc. Géol. France, 315, 1357–1364, 1992. 

López-Sánchez, M. A., Iriondo, A., Marcos, A., and Martínez, F. J.: A U-Pb zircon age (479 ± 5 Ma) from the uppermost layers of the Ollo de Sapo Formation near Viveiro (NW Spain): implications for the duration of rifting-related Cambro-Ordovician volcanism in Iberia, Geol. Mag., 152, 341–350,, 2015. 

Ludwig, K. R. and Turi, B.: Paleozoic age of the Capo Spartivento Orthogneiss, Sardinia, Italy, Chem. Geol., 79, 147–153,, 1989. 

Margalef, A., Castiñeiras, P., Casas, J. M., Navidad, M., Liesa, M., Linnemann, U., Hofmann, M., and Gärtner, A.: Detrital zircons from the Ordovician rocks of the Pyrenees: Geochronological constraints and provenance, Tectonophysics, 681, 124–134,, 2016. 

Marini, F.: “Phase“ sarde et distension ordovicienne du domaine sud-varisque, effets de point chaud? Une hypothèse fondée sur les données nouvelles du volcanisme albigeois, C. R. Acad. Sci., 306, 443–450, 1988. 

Martí, J., Munoz, J. A., and Vaquer, R.: Les roches volcaniques de l'Ordovicien supérieur de la région de Ribes de Freser-Rocabruna (Pyrénées catalanes): caractères et signification, C. R. Acad. Sci., 302, 1237–1242, 1986. 

Martí, J., Solari, L., Casas, J. M., and Chichorro, M.: New late Middle to early Late Ordovician U-Pb zircon ages of extension-related felsic volcanic rocks in the Eastern Pyrenees (NE Iberia): tectonic implications, Geol. Mag., 156, 1783–1792,, 2019. 

Martínez, F., Iriondo, A., Dietsch, C., Aleinikoff, J. N., Peucat, J. J., Cirès, J., Reche, J., and Capdevila, R.: U-Pb SHRIMP-RG zircon ages and Nd signature of lower Paleozoic rifting-related magmatism in the Variscan basement of the Eastern Pyrenees, Lithos, 127, 10–23,, 2011. 

Martínez Catalán, J. R., Hacar Rodríguez, M. P., Villar Alonso, P., Peréz-Estaún, A., and González Lodeiro, F.: Lower Paleozoic extensional tectonics in the limit between the West Asturian-Leonese and Central Iberian Zones of the Variscan Fold-Belt in NW Spain, Geolog. Runds., 81, 546–560,, 1992. 

Martínez Catalán, J. R., Arenas, R., Díaz García, F., Gómez Barreiro, J., González Cuadra, P., Abati, J., Castiñeiras, P., Fernández-Suárez, J., Sánchez Martínez, S., Andonaegui, P., González Clavijo, E., Díez-Montes, A., Rubio pascual, F. J., and Valle Aguado, B.: Space and time in the tectonic evolution of the northwestern Iberian Massif. Implications for the comprehension of the Variscan belt, J. R. Geol. Soc. Am., 200, 403–423,, 2007. 

Martini, I. P., Tongiorgi, M., Oggiano, G., and Cocozza, T.: Ordovician alluvial fan to marine shelf transition in SW Sardinia, Western Mediterranean Sea: tectonically (“Sardic phase”) influenced clastic sedimentation, Sediment. Geol., 72, 97–115,, 1991. 

Masuda, A. and Akagi, T.: Lanthanide tetrad effect observed in leucogranites from China, Geochem. J., 23, 245–253,, 1989. 

McDougall, N., Brenchley, P. J., Rebelo, J. A., and Romano, M.: Fans and fan deltas – precursors to the Armorican Quartzite (Ordovician) in western Iberia, Geol. Mag., 124, 347–359,, 1987. 

McLennan, S. M.: Rare earth element geochemistry and the “tetrad” effect, Geochim. Cosmochim. Ac., 58, 2025–2033,, 1994. 

Medina, J., Rodríguez Alonso, M. D., and Alonso Gavilán, G.: Sedimentação em plataforma siliciclástica do Grupo das Beiras (CXG) na região de Caramulo – Buçaco (Portugal Central), Comun. Inst. Geol. Min., 85, 39–71, 1998. 

Meireles, C., Sequeira, A. J. D., Castro, P., and Ferreira, N. I.: New data on the lithostratigraphy of Beiras Group (Schist Greywacke Complex) in the region of Góis-Arganil- Pampilhosa da Serra (Central Portugal), Cuad. Lab. Xeol. Laxe, 37, 105–124, 2013. 

Mezger, J. and Gerdes, A.: Early Variscan (Visean) granites in the core of central Pyrenean gneiss domes: implications from laser ablation U-Pb and Th-Pb studies, Gondwana Res., 29, 181–198,, 2016. 

Mingram, B., Kröner, A., Hegner, E., and Krentz, O.: Zircon ages, geochemistry, and Nd isotopic systematics of pre-Variscan orthogneisses from the Erzgebirge, Saxony (Germany), and geodynamic interpretation, Int. J. Earth Sci., 93, 706–727,, 2004. 

Monecke, T., Dulski, P., and Kempe, U.: Origin of convex tetrads in rare earth element patterns of hydrothermally altered siliceous igneous rocks from the Zinnwald Sn-W deposit, Germany, Geochim. Cosmochim. Ac., 71, 335–353,, 2007. 

Montero, P., Bea, F., González-Lodeiro, F., Talavera, C., and Whitehouse, M. J.: Zircon ages of the metavolcanic rocks and metagranites of the Ollo de Sapo Domain in central Spain: implications for the Neoproterozoic to Early Palaeozoic evolution of Iberia, Geol. Mag., 144, 963–976,, 2007. 

Montero, P., Talavera, C., Bea, F., Lodeiro, F. G., and Whitehouse, M. J.: Zircon geochronology of the Ollo de Sapo Formation and the age of the Cambro-Ordovician rifting in Iberia, J. Geol., 117, 174–191,, 2009. 

Murphy, J. B., Gutiérrez-Alonso, G., Nance, R. D., Fernández-Suárez, J., Keppie, J. D., Quesada, C., Strachan, R. A., and Dostal, J.: Origin of the Rheic Ocean: rifting along a Neoproterozoic suture?, Geology, 34, 325–328,, 2006. 

Nance, R. D., Gutiérrez-Alonso, G., Keppie, J. D., Linnemann, U., Murphy, J. B., Quesada, C., Strachan, R. A., and Woodcock, N. H.: Evolution of the Rheic Ocean, Gondwana Res., 17, 194–222,, 2010. 

Navidad, M. and Castiñeiras, P.: Early Ordovician magmatism in the northern Central Iberian Zone (Iberian Massif): new U-Pb (SHRIMP) ages and isotopic Sr-Nd data, Cuadernos del Museo Geominero 14, 391–398, Instituto Geológico y Minero de España, Madrid, 2011. 

Navidad, M., Castiñeiras, P., Casas, J. M., Liesa, M., Fernández-Suárez, J., Barnolas, A., Carreras, J., and Gil-Peña, I.: Geochemical characterization and isotopic ages of Caradocian magmatism in the northeastern Iberia: insights into the Late Ordovician evolution of the northern Gondwana margin, Gondwana Res., 17, 325–337,, 2010. 

Navidad, M., Castiñeiras, P., Casas, J. M., Liesa, M., Belousova, E., Proenza, J., and Aiglsperger, T.: Ordovician magmatism in the Eastern Pyrenees: Implications for the geodynamic evolution of northern Gondwana, Lithos, 314/315, 479–496,, 2018. 

Neiva, A. M. R., Williams, I. S., Ramos, J. M. F., Gomes, M. E. P., Silva, M. M. V. G., and Antunes, I. M. H. R.: Geochemical and isotopic constraints on the petrogenesis of Early Ordovician granodiorite and Variscan two-mica granites from the Gouveia area, central Portugal, Lithos, 111, 186–202,, 2009. 

Oggiano, G., Gaggero, L., Funedda, A., Buzzi, L., and Tiepolo, M.: Multiple early Paleozoic volcanic events at the northern Gondwana margin: U-Pb age evidence from the southern Variscan branch (Sardinia, Italy), Gondwana Res., 17, 44–58,, 2010. 

Padel, M., Álvaro, J. J., Clausen, S., Guillot, F., Poujol, M., Chichorro, M., Monceret, E., Pereira, M. F., and Vizcaïno, D.: U-Pb laser ablation ICP-MS zircon dating across the Ediacaran-Cambrian transition of the Montagne Noire, southern France, C. R. Geosci., 349, 380–390,, 2017. 

Padel, M., Clausen, S., Álvaro, J. J., and Casas, J. M.: Review of the Ediacaran-Lower Ordovician (pre-Sardic) stratigraphic framework of the Eastern Pyrenees, southwestern Europe, Geol. Acta, 16, 339–355,, 2018. 

Palme, H. and O'Neill, H. S. C.: Cosmochemical estimates of mantle composition, in: Treatise on Geochemistry 2, edited by: Holland, H. D. and Turekian, K. K., Elsevier-Pergamon, Oxford, UK, 1–38, 2004. 

Palmeri, R., Fanning, M., Franceschelli, M., Memmi, I., and Ricci, C. A.: SHRIMP dating of zircons in eclogite from the Variscan basement in northeastern Sardinia (Italy), N. Jb. Miner., Mh., 6, 275–288,, 2004. 

Pan, Y.: Controls on the fractionation of isovalent trace elements in magmatic and aqueous systems: evidence from Y/Ho, Zr/Hf, and lanthanide tetrad effect – a discussion of the article by M. Bau, 1996, Contrib. Mineral. Petrol., 128, 405–408,, 1997. 

Pankhurst, R. J., Rapela, C. W., Saavedra, J., Baldo, E., Dahlquist, J., Pascua, I., and Fanning, C. M.: The Famatinian magmatic arc in the central Sierras Pampeanas, and Early to Middle Ordovician continental arc on the Gondwana margin, in: The Proto-Andean Margin of Gondwana, edited by: Pankhurst, R. J. and Rapela, C. E., The Geological Society of London Special Publications, London, UK, 343–367,, 1998. 

Pavanetto, P., Funedda, A., Northrup, C. J., Schmitz, M., Crowley, J., and Loi, A.: Structure and U-Pb zircon geochronology in the Variscan foreland of SW Sardinia, Italy, Geol. J., 47, 426–445,, 2012. 

Pearce, J. A.: Sources and settings of granitic rocks, Episodes, 19, 120–125,, 1996. 

Pearce, J. A., Harris, N. B. W., and Tindle, A. G.: Trace element discrimination diagrams for the tectonic interpretation of granitic rocks, J. Petrol., 25, 956–983,, 1984. 

Pereira, M. F., Solá, A. R., Chichorro, M., Lopes, L., Gerdes, A., and Silva, J. B.: North-Gondwana assembly, break-up and paleogeography: U-Pb isotope evidence from detrital and igneous zircons of Ediacaran and Cambrian rocks of SW Iberia, Gondwana Res., 22, 866–881,, 2012. 

Piercey, S. J.: The setting, style, and role of magmatism in the formation of volcanogenic massive sulphide deposits, Miner. Deposita, 46, 449–471,, 2011. 

Pillola, G. L., Leone, F., and Loi, A.: The Cambrian and Early Ordovician of SW Sardinia, Gior. Geol., 60, 25–38, 1998. 

Pistis, M., Loi, A., and Dabard, M. P.: Influence of relative sea-level variations on the genesis of palaeoplacers, the examples of Sarrabus (Sardinia, Italy) and the Armorican Massif (western France), C. R. Geosci., 348, 150–157,, 2016. 

Pitra, P., Poujol, M., Den Driessche, J. V., Poilvet, J. C., and Paquette, J. L.: Early Permian extensional shearing of an Ordovician granite: the Saint-Eutrope “C/S-like” orthogneiss (Montagne Noire, French Massif Central), C. R. Geosci., 344, 377–384,, 2012. 

Pouclet, A., Álvaro, J. J., Bardintzeff, J. M., Gil Imaz, A., Monceret, E., and Vizcaïno, D.: Cambrian-Early Ordovician volcanism across the South Armorican and Occitan Domains of the Variscan Belt in France: Continental break-up and rifting of the northern Gondwana margin, Geosci. Front., 8, 25–64,, 2017. 

Puddu, C., Álvaro, J. J., and Casas, J. M.: The Sardic unconformity and the Upper Ordovician successions of the Ribes de Freser area, Eastern Pyrenees, J. Iberian Geol., 44, 603–617,, 2018. 

Puddu, C., Álvaro, J. J., Carrera, N., and Casas, J. M.: Deciphering the Sardic (Ordovician) and Variscan deformations in the Eastern Pyrenees, J. Geol. Soc., 176, 1191–1206,, 2019. 

Quesada, C.: Geological constraints on the Paleozoic tectonic evolution of tectonostratigraphic terranes in the Iberian Massif, Tectonophysics, 185, 225–245,, 1991. 

Rabin, M., Trap, P., Carry, N., Fréville, K. Cenki-Tok, B. Lobjoie, C. Gonçalves, P., and Marquer, D.: Strain partitioning along the anatectic front in the Variscan Montagne Noire massif (southern French Massif Central), Tectonics, 34, 1709–1735,, 2015. 

Robert, J. F.: Étude géologique et métallogénique du val de Ribas sur le versant espagnol des Pyrénées catalanes, PhD thesis, University of Franche-Comté, France, 294 pp., 1980. 

Robert, J. F. and Thiebaut, J.: Découverte d'un volcanisme acide dans le Caradoc de la région de Ribes de Freser (Prov. de Gérone), C. R. Acad. Sci., 282, 2050–2079, 1976. 

Roger, F., Respaut, J. P., Brunel, M., Matte, P., and Paquette, J. L.: Première datation U-Pb des orthogneiss oeillés de la zone axiale de la Montagne Noire (Sud du Massif central): nouveaux témoins du magmatisme ordovicien dans la chaîne varisque, C. R. Geosci., 336, 19–28,, 2004. 

Roger, F., Teyssier, C., Respaut, J. P., Rey, P. F., Jolivet, M., Whitney, D. L., Paquette, J. L., and Brunel, M.: Timing of formation and exhumation of the Montagne Noire double dome, French massif Central, Tectonophysics, 640/641, 53–69,, 2015. 

Rollison, H. R.: Using Geochemical Data: Evaluation, Presentation, Interpretation, Longman Group, London, UK, 1993. 

Romão, J., Dunning, G., Marcos, A., Dias, R., and Ribeiro, A.: O lacólito granítico de Mação-Penhascoso: idade e as suas implicações (SW da Zona Centro-Ibérica), e-Terra, 16, 1–4, 2010. 

Rossi, P., Oggiano, G., and Cocherie, A.: A restored section of the “southern Variscan realm” across the Corsica-Sardinia microcontinent, C. R. Geosci., 224–238,, 2009. 

Rubio-Ordóñez, A., Valverde-Vaquero, P., Corretgé, L. G., Cuesta-Fernández, A., Gallastegui, G., Fernández-González, M., and Gerdes, A.: An Early Ordovician tonalitic-granodioritic belt along the Schistose-Greywacke Domain of the Central Iberian Zone (Iberian Massif, Variscan Belt), Geol. Mag., 149, 927–939,, 2012. 

Rudnick, R. L. and Gao, S.: Composition of the Continental Crust, in: Treatise on Geochemistry, edited by: Holland, H. D. and Turekian, K. K., Elsevier-Pergamon, Oxford, UK, 1–64, 2003. 

Sánchez-García, T., Bellido, F., and Quesada, C.: Geodynamic setting and geochemical signatures of Cambrian-Ordovician rift-related igneous rocks (Ossa-Morena Zone, SW Iberia), Tectonophysics, 365, 233–255, 2003. 

Sánchez-García, T., Quesada, C., Bellido, F., Dunning, G., and González de Tánago, J.: Two-step magma flooding of the upper crust during rifting: the Early Paleozoic of the Ossa-Morena Zone (SW Iberia), Tectonophysics, 461, 72–90,, 2008. 

Sánchez-García, T., Bellido, F., Pereira, M. F., Chichorro, M., Quesada, C., Pin, C., and Silva, J. B.: Rift-related volcanism predating the birth of the Rheic Ocean (Ossa-Morena zone, SW Iberia), Gondwana Res., 17, 392–407,, 2010. 

Sánchez-García, T., Quesada, C., Bellido, F., Dunning, G. R., Pin, C., Moreno-Eiris, E., and Perejón, A.: Age and characteristics of the Loma del Aire unit (SW Iberia): Implications for the regional correlation of the Ossa-Morena Zone, Tectonophysics, 681, 58–72,, 2016. 

Sánchez-García, T., Chichorro, M., Solá, R., Álvaro, J. J., Díez Montes, A., Bellido, F. et al.: The Cambrian – Early Ordovician Rift Stage in the Gondwanan Units of the Iberian Massif, in: The Geology of Iberia: A Geodynamic Approach, edited by: Quesada, C. and Oliveira, J. T., Springer International Publishing, Heidelberg, 27–74,, 2019. 

Sarmiento, G. N., Gutiérrez-Marco, J. C., and Robardet, M.: Conodontos ordovícicos del noroeste de España. Aplicación al modelo de sedimentación de la región limítrofe entre las zonas Asturoccidental-Leonesa y Centroibérica durante el Ordovícico Superior, Rev. Soc. Geol. España, 12, 477–500, 1999. 

Schaltegger, U., Abrecht, J., and Corfu, F.: The Ordovician orogeny in the Alpine basement: constraints from geochronology and geochemistry in the Aar Massif (Central Alps), Schweizerische Miner. Petrogr. Mitteil., 83, 183–195, 2003. 

Shaw, J., Johnston, S., Gutiérrez-Alonso, G., and Weil, A. B.: Oroclines of the Variscan orogen of Iberia: paleocurrent analysis and paleogeographic implications, Earth Planet. Sci. Lett., 329–330, 60–70,, 2012. 

Shaw, J., Gutiérrez-Alonso, G., Johnston, S., and Pastor Galán, D.: Provenance variability along the early Ordovician north Gondwana margin: paleogeographic and tectonic implications of U-Pb detrital zircon ages from the Armorican Quartzite of the Iberian Variscan belt, Geol. Soc. Am. Bull., 126, 702–719,, 2014. 

Solá, A. R., Relações Petrogeoquímicas dos Maciços Graníticos do NE Alentejano, PhD thesis, University of Coimbra, Portual, 404 pp., 2007. 

Solá, A. R., Pereira, M. F., Williams, I. S., Ribeiro, M. L., Neiva, A. M. R., Montero, P., Bea, F., and Zinger, T.: New insights from U-Pb zircon dating of Early Ordovician magmatism on the northern Gondwana margin: the Urra formation (SW Iberian Massif, Portugal), Tectonophysics, 461, 114–129,, 2008. 

Stern, R. J.: Crustal evolution in the East African Orogen: a neodymium isotopic perspective, J. African Earth Sci., 34, 109–117,, 2002. 

Stille, H.: Bemerkungen betreffend die “Sardische” Faultung und den Ausdruck “Ophiolitisch”, Zeits. Deuts. Gess. Geowiss., 91, 771–773, 1939. 

Strelow, E. W. E.: An ion exchange selectivity scale of cations based on equilibrium distributions coefficients, Anal. Chem., 32, 1185–1188, 1960, 

Sun, S. S. and McDonough, W. F.: Chemical and isotopic systematics of oceanic basalts: implications for mantle composition and processes, in: Magmatism in the Ocean Basins, edited by: Saunders, A. D. and Norry, M. J., The Geological Society of London Special Publications, London, UK, 13–345,, 1989. 

Syme, E. C.: Ore-Associated and Barren Rhyolites in the central Flin Flon Belt: Case Study of the Flin Flon Mine Sequence, Manitoba Energy and Mines, Open File Report OF98-9, 1–32, 1998. 

Takahashi, Y., Yoshida, H., Sato, N., Hama, K., Yusa, Y., and Shimizu, H.: W- and M-type tetrad effects in REE patterns for water-rock systems in the Tono uranium deposit, central Japan, Chem. Geol., 184, 311–335,, 2002. 

Talavera, C.: Pre-Variscan magmatism of the Central Iberian Zone: chemical and isotope composition, geochronology and geodynamic significance, PhD thesis, University of Granada, Spain, 2009. 

Talavera, C., Bea F., Montero P., and Whitehouse, M.: A revised Ordovician age for the Sisargas orthogneiss, Galicia (Spain). Zircon U-Pb ion-microprobe and LA-ICPMS dating, Geol. Acta, 8, 313–317,, 2008. 

Talavera, C., Montero, P., Bea, F., González Lodeiro, F., and Whitehouse, M.: U-Pb zircon geochronology of the Cambro-Ordovician metagranites and metavolcanic rocks of central and NW Iberia, Int. J. Earth. Sci., 102, 1–23,, 2013. 

Teichmüller, R.: Zur Geologie des Thyrrhenisgebietes, Teil 1: Alte und junge Krustenbewegungen im südlinchen Sardinien, Abh. Der wissen. Gess. Göttingen, 3, 857–950, 1931. 

Teipel, U., Eichhorn, R., Loth, G., Rohrmüller, J., Höll, R., and Kennedy, A.: U-Pb SHRIMP and Nd isotopic data from the western Bohemian Massif (Bayerischer Wald, Germany): Implications for Upper Vendian and Lower Ordovician magmatism, Int. J. Earth Sci., 93, 782–801,, 2004. 

Thompsom, M. D., Grunow, A. M., and Ramezani, J.: Cambro-Ordovician paleogeography of the Southeastern New England Avalon Zone: Implications for Gondwana breakup, Geol. Soc. Am. Bull., 122, 76–88,, 2010. 

Tichomirowa, M., Berger, H. J., Koch, E. A., Belyatski, B., Götze, J., Kempe, U., Nasdala, L., and Schaltegger, U.: Zircon ages of high-grade gneisses in the Eastern Erzgebirge (Central European Variscides) – constraints on origin of the rocks and Precambrian to Ordovician magmatic events in the Variscan foldbelt, Lithos, 56, 303–332,, 2001. 

Tichomirowa, M., Sergeev, S., Berger, H. J., and Leonhardt, D.: Inferring protoliths of high-grade metamorphic gneisses of the Erzgebirge using zirconology, geochemistry and comparison with lower-grade rocks from Lusatia (Saxothuringia, Germany), Contrib. Mineral. Petrol., 164, 375–396,, 2012. 

Valverde-Vaquero, P. and Dunning, G. R.: New U-Pb ages for Early Ordovician magmatism in Central Spain, J. Geol. Soc. London, 157, 15–26,, 2000. 

Valverde-Vaquero, P., Marcos, A., Farias, P., and Gallastegui, G.: U-Pb dating of Ordovician felsic volcanism in the Schistose Domain of the Galicia-Trás-os-Montes Zone near Cabo Ortegal (NW Spain), Geol. Acta, 3, 27–37,, 2005. 

Valverde-Vaquero, P., Farias, P., Marcos, A., and Gallastegui, G.: U-Pb dating of Siluro-Ordovician volcanism in the Verín synform (Orense, Schistose Domain, Galicia-Trás-os-montes Zone), Geogaceta, 41, 247–250, 2007. 

Vilà, M., Pin, C., Enrique, P., and Liesa, M.: Telescoping of three distinct magmatic suites in an orogenic setting: Generation of Hercynian igneous rocks of the Albera Massif (Eastern Pyrenees), Lithos, 83, 97–127,, 2005. 

Villaseca, C., Castiñeiras, P., and Orejana, D.: Early Ordovician metabasites from the Spanish Central System: A remnant of intraplate HP rocks in the Central Iberian Zone, Gondwana Res., 27, 392–409,, 2013. 

Villaseca, C., Merino Martínez, E., Orejana, D., Andersen, T., and Belousova, E.: Zircon Hf signatures from granitic orthogneisses of the Spanish Central System: Significance and sources of the Cambro-Ordovician magmatism in the Iberian Variscan Belt, Gondwana Res., 34, 60–83,, 2016. 

Von Quadt, A.: U-Pb zircon and Sr-Nd-Pb whole-rock investigations from the continental deep drilling (KTB), Geol. Rundsch., 86, 258–271,, 1997. 

Von Raumer, J. F. and Stampfli, G. M.: The birth of the Rheic Ocean – early Palaeozoic subsidence patterns and tectonic plate scenarios, Tectonophysics, 461, 9–20,, 2008. 

Von Raumer, J. F., Bussy, F., Schaltegger, U., Schulz, B., and Stampfli, G.: Pre-Mesozoic Alpine basements: their place in the European Paleozoic framework, Geol. Soc. Am. Bull., 125, 89–108,, 2013. 

Von Raumer, J. F., Stampfli, G. M., Arenas, R., and Sánchez Martínez, S.: Ediacaran to Cambrian oceanic rocks of the Gondwanan margin and their tectonic interpretation, Int. J. Earth Sci., 104, 1107–1121,, 2015. 

Whalen, J. B., Currie, K. L., and Chappell, B. W.: A-type granites: Geochemical characteristics, discrimination and petrogenesis, Contr. Miner. Petrol., 95, 407–419,, 1987. 

Winchester, J. W.: Rare earth chromatography using bis-(2-ethylhexyl) (orthophosphoric acid), J. Chromatogr., 10, 502–506, 1963. 

Winchester, J. A. and Floyd, P. A.: Geochemical discrimination of different magma series and their differentiation products using immobile elements, Chem. Geol., 20, 325–343,, 1977. 

Zeck, H. P., Whitehouse, M. J., and Ugidos, J. M.: 496 ± 3 Ma zircon ion microprobe age for pre-Hercynian granite, Central Iberian Zone, NE Portugal (earlier claimed 618 ± 9 Ma), Geol. Mag., 144, 21–31, 2007.  

Zurbriggen, R.: Ordovician orogeny in the Alps – a reappraisal, Int. J. Earth Sci., 104, 335–350,, 2015. 

Zurbriggen, R.: The Cenerian orogeny (early Paleozoic) from the perspective of the Alpine region, Int. J. Earth Sci., 106, 517–529,, 2017. 

Zurbriggen, R., Franz, L., and Handy, M. R.: Pre-Variscan deformation, metamorphism and magmatism in the Strona-Ceneri Zone (southern Alps of northern Italy and southern Switzerland), Schweiz. Miner. Petrograph. Mitteil., 77, 361–380,, 1997. 

Zwart, H. J.: The Geology of the Central Pyrenees, Leidse Geol. Meded., 50, 1–74, 1979. 

Publications Copernicus
Short summary
A geochemical comparison of early Palaeozoic felsic magmatic episodes throughout the south-western European margin of Gondwana is analysed and includes data from the Iberian Massif, the Eastern Pyrenees, southern France and Sardinia. This dataset favours partial melting of sediments and/or granitoids in the lower continental crust during extensional movements related to the opening of the Rheic Ocean.
A geochemical comparison of early Palaeozoic felsic magmatic episodes throughout the...