1. Introduction
The Pyrenees, the E–W-trending orogenic belt that runs parallel to the French–Spanish border, were raised in response to the convergence of the Iberian and European plates in Cenozoic times. A main feature of this belt is its asymmetric fan shape with opposed vergences of the principal Alpine structures that rework previous Variscan ones. The North and South Pyrenean Zones, where sedimentary rocks of Mesozoic and Cenozoic ages predominate, border the Axial Zone of the Pyrenees. The Pyrenean Axial Zone is a fragment of the European Variscan belt incorporated into the core of the Pyrenean mountain range from Cretaceous to Miocene times (Mattauer, Reference Mattauer1968; Matte, Reference Matte1991). The rocks that currently make up the Axial Zone experienced a complex Variscan tectonothermal evolution resulting from overall compressional tectonics dominated by dextral transpression (e.g. Bouchez & Gleizes, Reference Bouchez and Gleizes1995; Gleizes et al. Reference Gleizes, Leblanc, Bouchez, Holdsworth, Strachan and Dewey1998 a; Carreras & Druguet, Reference Carreras, Druguet, Schulmann, Martínez Catalán, Lardeaux, Janousek and Oggiano2014). The main Variscan tectonic phase, D2 (Gleizes et al. Reference Gleizes, Leblanc, Bouchez, Holdsworth, Strachan and Dewey1998 a), corresponds to a transpressional event characterized by N120° E-directed great hectometric tight folds verging southwest. A penetrative foliation (S2) develops parallel to the axial plane of these folds, temporally close to the thermal peak of the metamorphism (Gleizes et al. Reference Gleizes, Leblanc, Santana, Olivier and Bouchez1998 b). Late tectonic phases generated localized strike-slip ductile shear zones in granitoids and high-grade metamorphic rocks (Carreras & Capellà, Reference Carreras and Capellà1994). In this context, the Variscan magmatism in the Pyrenees is mainly represented by calc-alcaline plutons of granite to granodiorite compositions emplaced into intermediate to shallow structural levels.
Structural and anisotropy-of-magnetic-susceptibility (AMS) studies of the granitoids in the Pyrenees (Porquet et al. Reference Porquet, Pueyo, Román-Berdiel, Longares, Cuevas and Ramajo2017) have demonstrated that their emplacement was coeval with the main Variscan D2 transpressive event (see Bouchez & Gleizes, Reference Bouchez and Gleizes1995; Carreras & Druguet, Reference Carreras, Druguet, Schulmann, Martínez Catalán, Lardeaux, Janousek and Oggiano2014). Most plutons are of Carboniferous age and their emplacement age extends over 70 Myr from 339–337 Ma (granite stocks situated in the core of the Ordovician Aston and Bossòst domes; Mezger & Gerdes, Reference Mezger and Gerdes2016) to 267 ± 1 Ma (Aya pluton in the Western Pyrenees; Denèle et al. Reference Denèle, Paquette, Olivier and Barbey2012). This long timespan makes it difficult to establish an accurate time relationship between the development of S2 and the emplacement age for any given pluton from geological constraints alone.
In this work, we present new U–Pb sensitive high-resolution ion microprobe (SHRIMP) and laser ablation inductively coupled plasma mass spectrometry (LA-ICP-MS) analyses of zircons from a diorite sample of the Posets pluton (PO-52) to determine the precise age for the emplacement of the pluton.
2. Geological setting
The Posets pluton has a slightly elliptical shape on a map, with an aspect ratio (short to long axis quotient) of 0.85 and a N130° E elongation (Fig. 1). From the petrographic point of view, it displays a normal and concentric compositional zoning (Fig. 2), with a gradual transition ranging from granodiorite in the inner part to tonalite towards peripheral zones (Enrique, Reference Enrique1989; A Hilario, unpub. PhD thesis, Univ. Basque Country, 2004). Diorite is locally found in the border tonalite zone. All of these facies have a very homogeneous fine-grained holocrystalline (c. 2–3 mm) texture and include microgranular enclaves with angular borders and xenoliths from the country rocks that preserve S2, and even S2-related folds occasionally. The dominant mineralogical composition in the Posets pluton consists of quartz, plagioclase, K-feldspar, biotite, amphibole and sphene. Geochemical data from 12 igneous samples reflect calc-alkaline and alumino-cafemic trends and point to a hybrid magmatic source for the Posets pluton (A Hilario, unpub. PhD thesis, Univ. Basque Country, 2004). P–T estimations of two samples from the Posets pluton using the ‘amphibole–plagioclase’ geothermometer (Blundy & Holland, Reference Blundy and Holland1990) and ‘Al-in-hornblende’ geobarometer (Schmidt, Reference Schmidt1992) yielded temperatures and pressures of 719 ± 30 °C / 1.9 ± 0.2 kbar and 728 ± 20 °C / 1.6 ± 0.2 kbar, respectively (A Hilario, unpub. PhD thesis, Univ. Basque Country, 2004).
Schematic geological map of the Central Pyrenees with the Posets pluton location (modified from Vissers, Reference Vissers1992).
Structural map (modified from A Hilario, unpub. PhD thesis, Univ. Basque Country, 2004) and synthetic cross-section (A–B) of Posets pluton. The star indicates the analysed sample location. Foliation data of the country rocks were also compiled from Ríos et al. (Reference Ríos, Lanaja, Rios and Marín1982, Reference Ríos, Galera, Barettino and Hernán2002).
The Posets granite intrudes into slates and limestones of Silurian to Lower–Medium Devonian age (Figs 1 and 2). The contact with the country rocks is sharp and generally concordant with the bedding and the main tectonic foliation (S2) of the country rocks. This foliation is an axial-planar cleavage associated with isoclinal upright folds next to the northern pluton contact and tight, south-verging folds in the southern contact zone. These structures form part of a progressive process of coaxial deformation that led to fold interference patterns of type 3. As the dominant foliation is linked to the youngest folding stage, it is referred to as S2. There is a previous cleavage (S1) that can be recognized in the field, crenulated by S2 in hinges of D2-folds. The preservation of S1 is fairly widespread at the thin-section scale, as a residual foliation crenulated by S2 in intrafoliar folds in samples from the limbs of young folds. At the regional scale, the strike of S2 ranges between N90° and N120° E, with an average dip of 50° N (Fig. 2). The trajectories of the S2 cleavage are, however, distorted at the eastern and western edges of the Posets pluton, where foliation triple points developed (Fig. 2). The country rocks were affected by a weak regional metamorphism that reached green-schist facies conditions. The pluton intrusion also produced a metamorphic aureole of 1 km thickness (Fig. 2), represented by andalusite/cordierite-bearing or even sillimanite-bearing hornfels very near the intrusive contact and mineral associations with garnet ± diopside ± epidote and minor olivine in the marbles (A Hilario, unpub. PhD thesis, Univ. Basque Country, 2004). In most areas of the metamorphic aureole these minerals grow on S2 as idiomorphic porphyroblasts with random orientations, but they appear as porphyroclasts with pressure shadows in a narrow fringe (nearly 10 m thick) on the innermost southern aureole. This solid-state deformation has its counterpart in sparse dextral S-C mylonites developed in tonalites that are in contact with the country rocks.
Field and AMS data from the Posets pluton (García Maiztegi et al. Reference Aranguren and Tubía1991; A Hilario, unpub. PhD thesis, Univ. Basque Country, 2004) reveal a concentric structural pattern, defined by spatial variations in the orientation of the magmatic and magnetic foliations (Fig. 2). The internal structure is roughly parallel to the pluton border. The foliation trajectories display a NW–SE ellipsoidal geometry with variable NNE dips, moderate dips and steep dips dominating in the southern and northern part of the pluton, respectively (Fig. 2). In contrast, the N- and NE-plunging magnetic lineation outlines S-shaped sigmoidal patterns (A Hilario, unpub. PhD thesis, Univ. Basque Country, 2004).
3. U–Pb SIMS SHRIMP dating
A diorite sample (PO-52: 42° 38′ 3.52″ N, 0° 27′ 8.52″ E) was processed according to routine zircon mineral separation (crushing, grinding, sieving under 250 μm, Wilfley table, Frantz isodynamic magnetic separator and methylene iodide) at the University of the Basque Country (UPV/EHU). The selected zircon crystals were placed in epoxy resin together with the TEMORA 1 and 91500 reference zircons, sectioned approximately in half, polished and analysed on a SHRIMP-II SIMS at the Centre of Isotopic Research (CIR) at VSEGEI (St Petersburg). The results were obtained following the procedure described by Larionov et al. (Reference Larionov, Andreichev, Gee, Gee and Pease2004). The U–Pb ion microprobe data were processed with the SQUID 1.02 (Ludwig, Reference Ludwig2001) and Isoplot/Ex 3.00 (Ludwig, Reference Ludwig2003) software using the decay constants of Steiger and Jäger (Reference Steiger and Jäger1977) and are presented in Appendix Table 1 (in the Supplementary Material available online at https://doi.org/10.1017/S0016756821000686). Cathodoluminescence images were used to select target areas for analysis.
Most of the analysed zircon crystals are devoid of inherited cores and present: (1) prismatic and euhedral morphologies, (2) concentric undisturbed oscillatory growth zoning (both in Fig. 3) and (3) high Th/U ratios, scattered between 0.42 and 0.76 (Fig. 4). The few composite zircons that display inherited xenomorphic cores (e.g. zircon crystals 3.1 and 10.1 in Fig. 3) are surrounded by an external rim with concentric oscillatory zoning. These cores display corroded and rounded geometries, oscillatory zoning and high Th/U ratios (0.87). Ten local analyses were carried out (online Appendix Table 1, in the Supplementary Material available online at https://doi.org/10.1017/S0016756821000686) in the oscillatory zoned parts of single zircons and in the external parts of composite zircon crystals (zircon crystals 3.1 in Fig. 3). These analyses yielded a 238U–206Pb Concordia age of 302 ± 2 (2σ) Ma (Fig. 5). Otherwise, the spot analyses taken from a xenomorphic and rounded core afford a Neoarchaean age (online Appendix Table 1, in the Supplementary Material available online at https://doi.org/10.1017/S0016756821000686).
Cathodoluminescence images of analysed zircon crystals by SHRIMP.
Discriminatory and compositional U vs Th diagram of the analysed zircon crystals
Tera–Wasserburg plot of the analysed zircon crystals by SHRIMP.
4. U–Pb LA-ICP-MS dating
Zircon crystals were analysed by LA-ICP-MS at the University of the Basque Country (SGIker) using a 213 nm New Wave Nd:YAG laser with a pulse energy density of ∼4 J cm−2 and a frequency of 10 Hz coupled to a Thermo Fisher XSeries-2 quadrupole ICP-MS. The analytical spot size was 40 μm in diameter, and in most cases the zircon crystals were completely pierced through. Analytical acquisition times were up to 56 s. The external calibration was performed to GJ-1 zircon, and the laboratory staff reduced the data using the Iolite 2.5 software package (Paton et al. Reference Paton, Hellstrom, Paul, Woodhead and Hergt2011; Paul et al. Reference Paul, Paton, Norris, Woodhead, Hellstrom, Hergt and Greig2012).
Following the acquisition of the electron backscattered images with a JEOL 6400-JSM of the University of the Basque Country (UPV/EHU-SGIker), only the prismatic zircon crystals with oscillatory zoning (Fig. 6) were selected as targets. These prismatic zircons also have high Th/U ratios (0.28–0.50; Appendix Table 2, in the Supplementary Material available online at https://doi.org/10.1017/S0016756821000686; Fig. 4). Thirty zircon crystals were analysed and seven of them were rejected, due to their discordant ages, for the geological interpretation (online Appendix Table 2, in the Supplementary Material available online at https://doi.org/10.1017/S0016756821000686). Data from the analysed spots were projected on a 207Pb/206Pb vs 238U/206Pb diagram (Tera & Wasserburg, Reference Tera and Wasserburg1972). Twenty-three of the 30 analyses (online Appendix Table 2, in the Supplementary Material available online at https://doi.org/10.1017/S0016756821000686) yielded a lower interception age of 302 ± 3 (2σ) Ma (Fig. 7). The weighted average 206Pb–238U age of 301 ± 3 (2σ) Ma (Fig. 7) also agrees with the result obtained by means of U–Pb SHRIMP analysis.
Backscattered electron images of zircon crystals analysed by LA-ICP-MS.
Tera–Wasserburg plot and weighted average U–Pb age of the analysed zircon crystals by LA-ICP-MS.
5. Discussion
The 3-D geometry of the Posets pluton is well constrained as an asymmetric inverted drop tilted towards the south (A Hilario, unpub. PhD thesis, Univ. Basque Country, 2004), which is also consistent with the southward vergence of the major Variscan folds and the N-dipping associated slate cleavage, S2, in the country rocks (Fig. 2). The pressure crystallization conditions specified for the Posets pluton suggest an emplacement level at depths of c. 4 km (A Hilario, unpub. PhD thesis, Univ. Basque Country, 2004). An issue that requires further clarification is the temporal relationships between the emplacement and the development of the metamorphic aureole at this shallow level with the inclusion of metamorphic roof-pendants that preserve the S2 and S1 cleavages. Gleizes et al. (Reference Gleizes, Leblanc, Santana, Olivier and Bouchez1998 b) reported similar observations in the country rocks of the Cauterets–Panticosa pluton. This observation would apparently conflict with a synkinematic emplacement during D2 and could be interpreted as evidence of a postkinematic emplacement. However, the following structural and regional arguments seem to support its emplacement during an event of dextral transpression associated with D2: (1) the Posets pluton is confined between two other granites (Fig. 1), 2 km to the SW of the Lys pluton (Hilario et al. Reference Hilario, Aranguren, Tubía and Pinotti2003) and 1 km to the NE of the Millares pluton (Román-Berdiel et al. Reference Román-Berdiel, Casas, Oliva-Urcia, Pueyo, Liesa and Soto2006), the emplacement of which took place under dextral transpression at the end of D2; (2) the emplacement ages of the Posets (this work) and Lys (Esteban et al. Reference Esteban, Aranguren, Cuevas, Hilario, Tubía, Larionov and Sergeev2015) plutons agree within the error limits; and (3) the existence of S-shaped lineation patterns in the Posets pluton is similar, in both its layout and orientation (Fig. 2), to sigmoidal lineation patterns that have been linked with dextral transpression in many other synkinematic Pyrenean granites (Bouchez & Gleizes, Reference Bouchez and Gleizes1995; Gleizes et al. Reference Gleizes, Leblanc, Santana, Olivier and Bouchez1998 b; Román-Berdiel et al. Reference Román-Berdiel, Casas, Oliva-Urcia, Pueyo and Rillo2004; Porquet et al. Reference Porquet, Pueyo, Román-Berdiel, Longares, Cuevas and Ramajo2017). It thus seems reasonable to consider the Posets pluton as a syn- to late-kinematic granite emplaced during the dextral transpression triggered at the end of the long-lasting Variscan deformational event (D2). Therefore, the foliation in the roof-pendants and xenoliths would correspond to incipient stages in the development of the S2 foliation within the framework of a long-lasting regional stress field, whereas the pluton emplacement and the development of the metamorphic aureole are short-lived processes that took place in a subsequent stage.
Our new geochronological data (U–Pb SHRIMP and LA-ICP-MS zircon analyses) from the Posets pluton provide a fairly accurate age of 302 ± 2 Ma. Considering that the morphological features and high Th/U ratios (>0.1; e.g. Hoskin & Schaltegger, Reference Hoskin and Schaltegger2003) of the zircon crystals are consistent with its magmatic origin, the result obtained (≈302 Ma) can be considered as the emplacement age of the Posets pluton. The emplacement age of most synkinematic plutons (syn-D2) from the central Pyreneees falls into a broad timespan constrained between 298 and 310 Ma: for example: 301 ± 9 Ma for the Eaux-Chaudes massif (Guerrot, Reference Guerrot, Ternet, Majesté-Menjoulas, Canérot, Baudin, Cocherie, Guerrot and Rossi2001; Ternet et al. Reference Ternet, Majesté-Menjoulas, Canérot, Baudin, Cocherie, Guerrot and Rossi2004); 301 ± 9 Ma (Guerrot, Reference Guerrot, Majesté-Menjoulas, Debon and Barrère1998) and 306 ± 2 Ma (Denèle et al. Reference Denèle, Laumonier, Paquette, Olivier, Gleizes, Barbey, Schulmann, Martínez Catalán, Lardeaux, Janousek and Oggiano2014) in the Eastern Cauterets pluton; 298 ± 2 Ma (NG Evans, unpub. PhD thesis, Univ. Leeds, 1993) and 303 ± 4 Ma (Pereira et al. Reference Pereira, Castro, Chichorro, Fernández, Díaz-Alvarado, Martí and Rodríguez2014) in the Maladeta massif; 309 ± 4 Ma (Gleizes et al. Reference Gleizes, Crevon, Asrat and Barbey2006) for the Bordères–Louron pluton; and 300 ± 2 Ma (Esteban et al. Reference Esteban, Aranguren, Cuevas, Hilario, Tubía, Larionov and Sergeev2015) for the Lys pluton. The new age, 302 ± 2 Ma, we have obtained for the emplacement of the Posets pluton fits into the time range specified for the emplacement of the above-mentioned syn-D2 granite plutons of the central Pyrenees (298 to 310 Ma).
A few Pyrenean granite plutons have yielded much younger ages: 267.1 ± 1.1 Ma in the Aya pluton (Denèle et al. Reference Denèle, Paquette, Olivier and Barbey2012) and 279.6 ± 3 Ma in the Vielha granodiorite (Pereira et al., Reference Pereira, Castro, Chichorro, Fernández, Díaz-Alvarado, Martí and Rodríguez2014), for example. These ages nearly overlap with those of the Permian volcanism recognized more than 60 km to the west, in the Midi d’Ossau and Anayet volcanic edifices (278–272 Ma; Briqueu & Innocent, Reference Briqueu and Innocent1993) or in subvolcanic dykes from the Sallent area (259 ± 3.2 Ma; Rodríguez-Méndez et al. Reference Rodríguez-Méndez, Cuevas, Esteban, Tubía, Sergeev, Larionov, Llana-Fúnez, Marcos and Bastida2014). Owing to this time convergence, it has been suggested that the Aya pluton would mark the transition from the late Variscan transpression to dextral transtensional conditions that first promoted the opening of Stephanian–Permian basins and subsequently led to the formation of the Bay of Biscay rift during the Mesozoic extension (Dènele et al. Reference Denèle, Paquette, Olivier and Barbey2012). In contrast, according to Pereira et al. (Reference Pereira, Castro, Chichorro, Fernández, Díaz-Alvarado, Martí and Rodríguez2014), the magmatism of the Variscan Pyrenean would be the expression of the subduction of the Palaeotethys Ocean in a long time interval, from c. 304 Ma to c. 266 Ma. Nevertheless, certain regional issues would question the geological meaning of the youngest ages of the Pyrenean granites. For instance, according to Pesquera and Pons (Reference Pesquera and Pons1990) and Olivier et al. (Reference Olivier, Améglio, Richen and Vadeboin1999) the Aya Pluton was synkinematically emplaced during the main D2 tectonic phase that is unconformably sealed by Stephanian deposits (Campos, Reference Campos1979). If true, these facts would require an emplacement older than 290 Ma for the Aya pluton and the age of 267.1 ± 1.1 Ma (Denèle et al. Reference Denèle, Paquette, Olivier and Barbey2012) could reflect the younging effect of the Alpine Aritxulegi fault that completely traverses the pluton. Regarding the Vielha granodiorite the sample is very close to the southern contact of the pluton (Pereira et al. Reference Pereira, Castro, Chichorro, Fernández, Díaz-Alvarado, Martí and Rodríguez2014; Fig. 2), which could have been reactivated as a shear zone during the Alpine orogeny (Leblanc et al. Reference Leblanc, Gleizes, Lespinasse, Olivier and Bouchez1994). Consequently, further geochronological work focused on the possible overprinting effect of the Alpine orogeny would be desirable to test these interpretations.
6. Conclusions
(1) U–Pb SHRIMP and LA-ICP-MS analysis of zircon crystals from a diorite of the Posets pluton yields an age ∼302 Ma for its emplacement in the Variscan upper crust, now the Axial Zone of the Pyrenees, in shallow depth conditions.
(2) The obtained age fits into the wide timespan (310 to 298 Ma) established from other synkinematic plutons of the central Pyrenees.
(3) The emplacement and development of the metamorphic aureole must be considered as short-lived events along the long-lasting D2 deformational process that led to S2 formation in a dextral transpressional field.
Supplementary material
To view supplementary material for this article, please visit https://doi.org/10.1017/S0016756821000686
Acknowledgements
This work was supported by grants EHUA13/03 and GIU20/017 from the University of the Basque Country (UPV/EHU) and CGL2017-82976 from the Ministerio de Economía, Industria y Competitividad / Agencia Estatal de Investigación / Fondo Europeo de Desarrollo Regional, European Union. E. Druguet, Y. Denèle, an anonymous reviewer and the editor Olivier Lacombe are thanked for reviews and discussions that improved the final manuscript.
Declaration of Interest
There are no potential conflicts of interest.
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