Emplacement of the Lavadores granite (NW Portugal): U/Pb and AMS results

Petrology, geochemistry (Geochronology) Emplacement of the Lavadores granite (NW Portugal): U/Pb and AMS results Mise en place du granite de Lavadores (Portugal nord-occidental) : re ´sultats U/Pb et ASM Helena C.B. Martins *, Helena Sant’Ovaia, Joana Abreu, Miguel Oliveira, Fernando Noronha Geology Centre/Department of Geosciences, Environment and Spatial Planning, Faculty of Sciences, Porto University, Rua do Campo Alegre 4169-007 Porto, Portugal 1. Introduction It is well documented that the ascent and emplacement of many granites intrusions is significantly controlled by tectonic activity along faults and shear zones, in different tectonics settings (Castro, 1986; Hutton, 1988; Ingram and Hutton, 1994; Speer et al., 1994; Tikoff and Saint Blanquat, 1997). This relationship is well demonstrated by the synchronous timing and spatial association of many Variscan granites in the Variscan belt (Faure, 1995; Faure and Pons, 1991; Faure et al., 2002; Ge ´belin et al., 2006, 2007, 2009; Joly et al., 2009). C. R. Geoscience 343 (2011) 387–396 ARTICLE INFO Article history: Received 30 July 2010 Accepted after revision 31 May 2011 Presented by Jean Aubouin. Keywords: Variscan Emplacement Anisotropy of magnetic susceptibility U-Pb zircon Portugal Mots cle ´s: Varisque Mise en place Anisotropie de susceptibilite ´magne ´tique U-Pb zircon Portugal ABSTRACT Studies of Anisotropy of Magnetic Susceptibility (AMS) and U-Pb geochronology, in zircon fractions, were carried out in a magnetite type-granite, the Lavadores granite, which is an example of a late to post-orogenic Variscan granite in northern Portugal (NW Iberian Peninsula). The U-Pb zircon analyses yield an age of 298 11 Ma that is considered to be the emplacement age of this granite and thus suggesting a post-tectonic emplacement. This is also supported by the magmatic nature of the microstructures. Magnetic lineations are subvertical and magnetic foliations display a general WNW-ESE subvertical pattern consistent with a dextral kinematic. These AMS data suggest that the emplacement of the Lavadores granite was controlled by a major mechanical anisotropy formed by transtensional structures associated with the Porto-Tomar shear zone. ß2011 Acade ´mie des sciences. Published by Elsevier Masson SAS. All rights reserved. RE ´SUME ´ Une e ´tude de l’anisotropie de susceptibilite ´magne ´tique (ASM), couple ´ea `la datation U-Pb, sur fractions de zircon, a e ´te ´mene ´e dans le granite de Lavadores, un granite a `magne ´tite, qui est un bon exemple de granites Varisques, tardi a `post-oroge ´nique. Les analyses U-Pb sur zircon ont donne ´un a ˆge a `298 11 Ma interpre ´te ´comme l’a ˆge de mise en place posttectonique du granite de Lavadores. Les microstructures magmatiques confirment cette mise en place post-tectonique. Les line ´ations magne ´tiques sont verticales et les foliations magne ´tiques pre ´sentent un fort pendage avec une orientation WNW-ESE en accord avec une cine ´matique dextre. Ces donne ´es ASM sugge `rent que la mise en place du granite de Lavadores a e ´te ´contro ˆle ´e par une anisotropie me ´canique majeure qui correspond a `des structures transtensives associe ´es a `la zone de cisaillement de Porto-Tomar. ß2011 Acade ´mie des sciences. Publie ´par Elsevier Masson SAS. Tous droits re ´serve ´s. * Corresponding author. E-mail address: [email protected] (Helena C.B. Martins). Contents lists available at ScienceDirect Comptes Rendus Geoscience www.sciencedirect.com 1631-0713/$ – see front matter ß2011 Acade ´mie des sciences. Published by Elsevier Masson SAS. All rights reserved. doi:10.1016/j.crte.2011.05.002 Outstanding features of the internal zone of the Iberian Variscides, the Central Iberian Zone, are a complex shear zone network and a intensive late to post-orogenic Variscan magmatism with the most active period spanning broadly the time between c. 320 and 290 Ma (Dias et al., 1998, 2009; Ferna ´ndez-Sua ´rez et al., 2011; Martins et al., 2009). In northern Portugal, this magmatic activity has left large granitoid plutons which presented highly contrasted compositions and whose emplacement was in most cases associated to major Variscan structures, namely shear zones and strike slip faults. The Lavadores granite emplacement was controlled by one of the most important structure crossing the Variscan basement, the Porto-Tomar Shear Zone (PTSZ). The PTSZ is a north-south dextral transform fault that was active throughout much of the Devonian as well as the Variscan (Dias and Ribeiro, 1995; Ribeiro et al., 2009). Other authors propose that the PTSZ is a major fault only structured since the beginning of the Variscan orogeny (Pereira et al., 2010). The first Rb-Sr geochronological data of the Lavadores granite were obtained by Mendes (1967) in biotite and Silva (1995) in whole rock, which respectively gave an age of 346 14Ma and 314 11Ma, suggesting a syntectonic emplacement. However, the well-known limitations of the Rb-Sr isotopic system and because these ages are not in agreement with field and structural data, lead us to the development of a U-Pb zircon geochronology.The aim of this work is to better constrain the emplacement age of the Lavadores granite (northern Portugal) with a multidisciplinary approach: U-Pb geochronology data and structural characterization through a study of Anisotropy of Magnetic Susceptibility (AMS). Studies of AMS were preceded by detailed geological mapping and complemented by petrographic and microstructural observations. The AMS studies were performed in the Lavadores granite as well as in its country rocks. The main results of this study show that this granite is post-tectonic and ascent and emplaced along a non-active ductile extensional shear zone. 2. Geological setting The tectonometamorphic and magmatic features of the Western Europe Variscan belt have been explained by the collision of Laurentia-Baltica with Gondwana (Lagarde et al., 1992; Matte, 1991) and has taken place from Early Devonian to Mid-Carboniferous (390–330), followed by post-thickening extension from the MidCarboniferous to the Permian times (330–280). The innermost zone of the Iberian Variscan Belt constitutes the Central Iberian Zone (CIZ) in which three main ductile Variscan deformation phases (D 1 ,D 2 and D 3 ) were recognized (Noronha et al., 1979; Ribeiro, 1974; Ribeiro et al., 1990). The D 1 and D 2 deformation phases correspond to the collision stage of the Variscan orogeny whereas the last ductile deformation phase D 3 ,Namurian-Westphalian in age, is related to the post-thickening extension tectonic regime. This event develops open to tight vertical folds with subhorizontal axes and subvertical shear zones with sinistral or dextral wrench movements and was followed by a fragile deformation phase giving rise to a set of conjugate strike-slip faults (NNW-dextral and NNE-sinistral), pointing to a LateVariscan main compression around north-south (Arthaud et al., 1975; Ribeiro, 1974). Most of the granitoids of the CIZ are correlated with D 3 and define alignments closely related to the ductile shear zones. These granitoid magmatism, based on emplacement ages (Dias et al., 1998) has been classified as: synorogenic (syn-late and late to post-D 3 ; 320–300 Ma) and late to post-orogenic (post-D 3 ; 299–290 Ma). The granite rock selected for this study is located in the west boundary of the Central Iberian Zone, in northern Portugal. This boundary is marked by one of the most important Variscan structures the Porto-Tomar Shear Zone (Ribeiro et al., 2009). The PTSZ is a north-south subvertical strike-slip fault that is 2 to 8 km wide and extends ca. 170 km from Porto to Tomar (Fig. 1). This important crustal anisotropy controlled the emplacement of the Lavadores granite during the post-collisional stage of the Variscan orogeny.The geology of the studied area is dominated by the presence of metamorphic rocks, intruded by the Lavadores granite. The Lavadores granite outcrops at about 3 km south of Porto in a narrow band along the coastline, in Vila Nova de Gaia, and the massif extended to the south ca. 60 km cutting discordantly Precambrian metamorphic rocks (Chamine ´et al., 2003; Oliveira et al., 2010). At southeast, the Lavadores granite has a gradual contact with the Madalena granite (Fig. 1). Most outcrops of the Lavadores granite are, however, covered by sand which difficult fieldwork and sampling.The host rocks, uncharted at this map scale, comprise different lithologies, consisting in gneiss, amphibolites and folded quartz-pelitic metasediments (micaschists and quartz-micaschists). All of these metamorphic rocks present a shearing deformation, related to the last ductile Variscan deformation phase (D 3 ). The Lavadores granite has a pinkish colour and presents abundant mafic microgranular enclaves with a wide range of compositions (Silva, 2010; Silva and Neiva, 1998, 2004). This granite is porphyritic, coarse-grained biotite granodiorite-monzogranite and contains quartz + plagioclase (andesine/oligoclase) + perthitic orthoclase and microcline + biotite + zircon+ sphene + apatite + allanite amphibole. The main petrographic feature that distinguishes this granite is the presence of the accessory phase magnetite, which is uncommon in Late Variscan granites in northern Portugal (Dias et al., 2002; Martins et al., 2009; Mendes and Dias, 2004) and can be considered a magnetite-type granite (Ishihara, 1977). No clear shape preferential orientation of the main minerals was observed in the studied sites. Microstructural observations support the general lack of intracrystaline deformation in minerals, as shown by undeformed biotite and euhedral feldspar crystals, accompanied by large quartz grains. Slight imprints of solidstate deformation are observed, as represented by undulatory extinction in quartz (Fig. 2). Hence, the rock fabric is considered to have developed essentially in the magmatic state. Available geochemical, mineralogical and isotopic data are reported in several papers (Martins et al., 2003, 2004; Silva, 2010; Silva and Neiva, 1998, 2004). H.C.B. Martins et al. / C. R. Geoscience 343 (2011) 387–396 388 3. Analytical methods 3.1. Anisotropy of magnetic susceptibility The AMS studies sampling was performed in the Lavadores granite and also in country-rocks (gneiss, micaschists and amphibolites) (Fig. 4). A total of 3/4 oriented cores were collected at each of the sampling stations corresponding to 63 rock-cylinders, 25 mm in diameter and 22 mm in length, which were prepared for magnetic measurements. Measurements were performed using KLY-4S Kappabridge susceptometer Agico model (Czech Republic) of ‘‘Centro de Geologia’’ of the Porto University. For each site, the AGICO software enabled us to calculate the mean susceptibility Km, which is the mean of the eight (or more) individual arithmetic means (k1 + k2 + k3)/3. There also calculated the intensities and orientations of the three axes K1 K2 K3, which are the tensorial means of the k1 k2 k3 axes for the eight specimens, and the 95% confidence angles E12, E23 and E31 corresponding to these three axes. The magnetic fabric is defined by the magnetic lineation (parallel to the long axis of the mean ellipsoid orientation average, K1) and the magnetic foliation (plane perpendicular to the orientation of K3, the short axis). P, the magnetic anisotropy ratio, corresponds to K1/K3. To describe the shape of the AMS ellipsoid the shape parameter, T, expressed by T¼2InK2=K3ðÞ=In K1=K3ðÞ½1 (Jelinek, 1981) was computed. A Molspin pulse induction magnetizer was used to create magnetic fields at room temperature to a maximum of 1 T. The magnetization of the representative samples after each exposure was measured with a Molspin spinner magnetometer controlled by a microcomputer. The magnetization obtained in this maximum field was defined as the effective saturation Isothermal Remanent Magnetization value for each of the samples. These [(Fig._1)TD$FIG] Fig. 1. Geological sketch map of the Lavadores area and its location in northern Portugal (Central Iberian Zone). MVF: Manteigas-Vilaric¸a Fault; PVF: Penacova-Verin Fault; DBSZ: Douro-Beira Shear Zone; JPCSZ: Juzbado-Penalva do Castelo Shear Zone; PTSZ: Porto-Tomar Shear Zone; TCBSZ: TomarCordoba-Badajoz Shear Zone Fig. 1. Mappe ge ´ologique simplifie ´edelare ´gion de Lavadores et sa localisation au Nord-Ouest du Portugal (Zone Centrale Ibe ´rique). MVF : Faille de Manteigas-Vilaric¸a ; PVF : Faille de Penacova-Verin ; DBSZ : Zone de Cisaillement de Douro-Beira ; JPCSZ : Zone de Cisaillement de Juzbado-Penalva do Castelo ; PTSZ : Zone de Cisaillement de Porto-Tomar ; TCBSZ : Zone de Cisaillement de Tomar-Cordoba-Badajoz. H.C.B. Martins et al. / C. R. Geoscience 343 (2011) 387–396 389 Table 1 Anisotropy of Magnetic Susceptibility data for the sampling sites. Tableau 1 Re ´sultats des mesures d’anisotropie de susceptibilite ´magne ´tique pour les sites d’e ´chantillonnage. Sampling Sites/ Lithology Km E 6 SI P T K1 K3 Foliation E12 E23 E31 n Dec Inc Dec Inc LV1Lavadores granite 16477.50 1.116 0.292 245 69 31 18 N121; 72SW 37 11 8 12 LV2Lavadores granite 17426.67 1.206 –0.246 194 81 23 4 N144; 83 SW ***3 LV3Lavadores granite 17031.43 1.164 –0.106 200 72 12 18 N102; 72 SW 29 10 9 7 LV4Lavadores granite 10589.00 1.144 0.214 241 79 20 9 N119; 81 SW 8 16 5 9 LV5Lavadores granite 19302.86 1.192 –0.028 171 78 355 12 N085; 78 S 12 6 7 7 LV6Lavadores granite 15000.00 1.251 –0.285 248 80 21 8 N111; 82 SW ***2 Amphibolite 1348.88 1.311 –0.253 226 62 340 12 N070; 78 SE 5 20 4 7 Micaschist 3965.56 1.932 –0.060 219 58 52 31 N142; 59 SW 18 28 8 9 Gneiss 22.71 1.034 0.079 316 77 123 23 N33; 77 NE 49 73 57 7 Km: mean susceptibility in 10 6 SI; P: anisotropy degree; T: shape parameter (Jelinek, 1981); Dec, Inc: declination, inclination; E12, E23 and E31: 95% confidence angles corresponding to the three axes; n: number of specimens. *: not enough data for statistics. [(Fig._2)TD$FIG] Fig. 2. Magmatic microstructures in the Lavadores granite: undeformed biotite and feldspar and incipient undulatory extinction in quartz. All microphotographs under crossed polars. bt: biotite; Kf: K-feldspar; pl: plagioclase; all: allanite; qtz: quartz. Fig. 2. Microstructures magmatiques du granite de Lavadores : la biotite et le feldspath ne sont pas de ´forme ´s, et le quartz pre ´sente une le ´ge `re extinction onduleuse. Toutes les microphotographies ont e ´te ´prises en lumie `re polarise ´e. bt : biotite ; Kf : feldspath potassique; pl : plagioclase ; all : allanite ; qtz : quartz. H.C.B. Martins et al. / C. R. Geoscience 343 (2011) 387–396 390 [(Fig._3)TD$FIG] Fig. 3. a: frequency histogram for bulk magnetic susceptibility; b: plots of the shape (T) and anisotropy (P) parameters showing dominant prolate ellipsoids. Fig. 3. a : histogramme de fre ´quence pour la susceptibilite ´magne ´tique ; b : repre ´sentation du parame `tre de forme (T) et du parame `tre d’anisotropie (P) montrant des ellipsoı ¨des allonge ´s. [(Fig._4)TD$FIG] Fig. 4. Simplified geological map of the studied area with the sampling sites and the stereograms (Schmidt, lower hemisphere) of the magnetic fabrics. Fig. 4. Carte ge ´ologique simplifie ´e de la zone e ´tudie ´e avec les sites d’e ´chantillonnage et les ste ´re ´ogrammes (Schmidt, he ´misphe `re infe ´rieur) de fabrique magne ´tique. H.C.B. Martins et al. / C. R. Geoscience 343 (2011) 387–396 391 measurements were performed in the Earth Sciences Department of the University of Coimbra. 3.2. U–Pb dating The U–Pb isotopic analyses were carried out at CRPG, Nancy, France, using a conventional U–Pb method on multigrain zircon fractions. The zircons were recovered by crushing the sample and sieving, followed by heavy liquid and magnetic separations and finally hand picking. Four zircon fractions were selected according to their morphology, colour, and lack of inclusions, fractures and metamictisation. Some of these fractions were submitted to air-abrasion (Krogh, 1982) to eliminate the external zones of the crystal where Pb loss may have occurred. All zircon fractions were observed on a backscattered scanning electron microscopy (BSEM). Chemical preparation of U and Pb analysis includes:  HNO 3 3 N warm washing of the zircon;  HF digestion at 240 8C and HCl 3 N dissolution of the fluorides at 180 8C in a Teflon bomb (Parrish, 1987);  separation of Pb and U by elution on anionic resin of two aliquots (one with the addition of a mixed 208 Pb235 U spike) following Krogh (1973). Common Pb blanks varied from 30 and 80 pg during this study. 4. Results 4.1. Anisotropy of Magnetic Susceptibility (AMS) The results for the nine stations are summarized in Table 1. The magnetic susceptibility values fall into two major groups: K >10 10 3 SI for the Lavadores granite and K <510 3 SI for the amphibolite, metasediments and gneiss as is shown on the K histogram (Table 1 and Fig. 3a). The magnetic anisotropy, P, has values always higher than 1.10 in the amphibolite, metasediments and Lavadores granite and less than 1.10 in the gneiss. The shape parameter T is below zero in six sites, which is indicative of prolate AMS ellipsoids: in metasediments, amphibolite and four sites of the Lavadores granite. The gneiss and two sites of the Lavadores granite show oblate ellipsoids (Table 1). The plot of the T and P parameters show that the prolate shape of the AMS ellipsoid is related to the highest anisotropies (Fig. 3b). [(Fig._5)TD$FIG] Fig. 5. Isothermal Remanent Magnetization (IRM) acquisition curves for representative samples. Js: saturation magnetization; J: magnetization. Fig. 5. Courbes d’acquisition d’aimantation re ´manente isotherme pour les e ´chantillons repre ´sentatifs. Js : aimantation a `saturation ; J : aimantation. H.C.B. Martins et al. / C. R. Geoscience 343 (2011) 387–396 392 Equal-area stereographic projections of the three principal axes of magnetic susceptibility each site are presented in Fig. 4. The Lavadores granite has very homogeneous magnetic lineations with steep dip (mean dip is 798) trending to N2038. The magnetic foliations have also steep dip (mean dip is 778SW) and trend to N1138. In amphibolites and metasediments, the magnetic lineations are also subvertical. Nevertheless, in the gneiss, the magnetic lineations are poorly defined. The magnetic foliation of the metasediments have WNW-ESE trend and dip to south-west (similar to Lavadores granite). In the amphibolites, the magnetic foliation has a NE-SW trend and is subvertical. Finally the foliation in the gneiss is subvertical with WNW-ESE trend; however, the low magnetic anisotropy of this facies, creates a wide dispersion of the AMS axes which implies a bad definition of the magnetic foliation and lineation. The Isothermal Remanent Magnetization data obtained point out three distinct magnetic behaviors: in the granite the IRM data are due to the ferrimagnetic fraction; in the metasediments and amphibolites are due to both the paramagnetic and ferrimagnetic fractions; finally the gneiss values are controlled by the paramagnetic fraction (Fig. 5). 4.2. U–Pb geochronology The analytical data and calculated ages with 2 s errors from Lavadores granite are presented in Table 2. The U–Pb zircon data were carried out on four zircon fractions of one sample of the Lavadores granite. A typological study (Pupin, 1980) has allowed the identification of several zircon types (Martins et al., 2003, 2004). The zircons are very limpid, colourless or light rose color. The backscattered scanning electron microscope imaging of the long prismatic zircons revealed an inner zone, sometimes partially resorbed, surrounded by a finely magmatic zoned rims. Some of them have cores that could correspond to an earlier magmatic crystallization. The prismatic acicular Table 2 U-Pb isotopic data on zircon from the Lavadores granite, northern Portugal. The atomic ratios were corrected for initial common lead composition blanks (Stacey and Kramers, 1975) and mass fractionation using NBS 983 Standard. The U–Pb ages with 2 s errors were calculated using a version of Isoplot program (Ludwig, 2003). The decay constants used for age determinations are from Steiger and Ja ¨ger (1977). Tableau 2 Re ´sultats analytiques U-Pb des zircons provenant du granite de Lavadores, Nord-Portugal. Les rapports isotopiques ont e ´te ´corrige ´s des blancs, de la composition du plomb commun initial (Stacey et Kramer, 1975)et du fractionnement de masse (NBS 983 Standard). Les a ˆges U–Pb, les erreurs 2 s , ont e ´te ´calcule ´sa `l’aide d’une version du programme Isoplot (Ludwig, 2003). Les constantes de de ´sinte ´gration, utilise ´es pour les de ´terminations d’a ˆge sont de Steiger et Ja ¨ger (1977). Concentrations Isotopic ratios Apparent ages (Ma) Fractions (shape) Weight (mg) U Total (ppm) Pb * (ppm) 206 Pb/ 204 Pb 206 Pb * / 238 U 2 s (%) 207 Pb * / 235 U 2 s (%) 207 Pb * / 206 Pb * 2 s (%) 206 Pb * / 238 U 2 s s 207 Pb * / 235 U 2 s 207 Pb * / 206 Pb * 2 s Lav99 (Z) b (needle) 0.95 1486.7 63.1 1763.79 0.04222 0,084522 0.304251 0,239064 0.052265 0,158541 266.6 0,2 269.7 0,6 297 4 Lav99 (Z) b (short prisms) 21 1665.9 69.1 1313.71 0.041804 0,182463 0.301108 0,369571 0.05224 0,191685 264 0,5 267.3 0,9 296 4 Lav99 (Z) b (flat) 0.16 1183.9 48.7 1032.34 0.040716 0.212583 0.293165 0.410623 0.05222 0.2056772 257.3 0.5 261 0.9 295 5 Lav99 (Z) a (long prisms) 0.43 1343.9 58 1628.11 0.04306 0.120448 0.310184 0.2559 0.052245 0.13844 271.8 0.3 274.3 0.6 296 3 Pb * : radiogenic lead. a Fraction submitted to abrasion. b Fraction not submitted to abrasion. [(Fig._6)TD$FIG] Fig. 6. U-Pb Concordia diagram showing analytical data for zircon fractions from the Lavadores granite, northern Portugal. Fig. 6. Diagramme Concordia du granite de Lavadores, Nord-Portugal. H.C.B. Martins et al. / C. R. Geoscience 343 (2011) 387–396 393 and flat zircons are more homogeneous crystals devoid of cores and showing generally a faint zoning. The four zircon fractions are concordant and define a line (MSWD of concordance = 0.013, probability of fit = 0.99) intersecting the Concordia at 298 11 Ma (Fig. 6) that can be interpreted as the emplacement age of this granite. This new data do not confirm the age of 314 11 Ma obtained by Silva (1995) using the Rb/Sr method, although the error bars are large for the two of them, since the Lavadores granite shows no evidence of being syntectonic. In fact the new age and thus the post-tectonic character is in agreement with geological and tectonic settings and corresponds to the age of Variscan late-orogenic granite magmatism, post-D 3 (Dias et al., 1998, 2009; Ferreira et al., 1987; Martins et al., 2009). 5. Discussion and conclusion Granite bodies record the tectonic events that are related to their emplacement during magma cooling, through the orientation of the magmatic foliation and lineation, and trough solid-state deformation at high and low temperature that record the kinematics of deformation as crystallization progress (Be Mezeme et al., 2007; Gleizes et al., 2006; Verner et al., 2009). Based on petrographic overview and AMS data, we argued that the Lavadores granite structure indicates fabrics developed at a magmatic stage during magma crystallization. Based on the AMS measurements, the inclusion of the magnetic susceptibility values in two large groups (K >10 3 SI and K <10 4 SI) allows the characterization of the magnetic behaviour of the studied facies. According to Tarling and Hrouda (1993), in a rock presenting K>10 3 SI, its susceptibility and anisotropy are due to the ferrimagnetic fraction (magnetite); if K <10 4 SI then the paramagnetic fraction controls the magnetic susceptibility and anisotropy of the rock. Isothermal Remanent Magnetization (IRM) data pointed out two distinct magnetic behaviours: in the granites and metasediments, the IRM data are due to a ferrimagnetic fraction and in the gneiss values are controlled by the paramagnetic one (Sant’Ovaia et al., 2009). In the case of Lavadores granite, the presence of magnetite can include this granite in the series of ‘‘magnetite type granites’’ defined by (Ishihara, 1977). In the case of the gneiss, the magnetic susceptibility is mainly due to iron-bearing minerals such as the biotite. The Lavadores granite shows a high magnetic anisotropy (the average for the six sampling stations is 1.179). Even so, field and microscope observations do not show signs of low temperature solid-state deformation. Occasionally some magmatic flow is visible on the field and magmatic to high temperature solid-state deformation microstructures are present. Apparently this anisotropy is due solely to the fact that the bearer of the magnetic signal is the magnetite (which has a high susceptibility) and, though a weak alignment of magnetite grains leads to a higher anisotropy to the rock. The ‘‘subfabric’’ of magnetite prevails over any other ‘‘fabric’’ mineral, especially that of biotite or amphibole. In addition, the ‘‘subfabric’’ of magnetite is reflected generally in the constrict shape of AMS ellipsoids. The magnetic foliations presents generally high dips and most of the magnetic lineations are subvertical; it is also worth noting that prolate ellipsoids characterize the studied granite. These features might suggest the presence of a feeding zone for the Lavadores granite. In this zone, the magma ascended into a conduit, the PTSZ anisotropy, towards upper-crustal levels. The Lavadores granite emplacement was controlled by transtensional structures associated with the PTSZ, which create offsets for magma emplacement, as attested by the magnetic subvertical WNW-ESE foliation associated with subvertical magnetic lineations. This magnetic fabric pattern probably records the evolution of regional tectonics during or just after the complete crystallization of the magma because only magmatic microstructures are present rather than low temperature solid-state microstructures. In the metasediments and gneiss, the NW-SE magnetic foliations are concordant with the foliation measured in the field. In the case of metasediments the magnetic anisotropy (mean 1.932) may not be justified exclusively by the presence of magnetite. A deformation event must be taking into account as well, to explain the high magnetic anisotropy. However in the gneisses the magnetic anisotropy (mean 1.034) is an indicator of an incipient foliation and issimilarwiththe valuesfoundinsyntectonicperaluminous granites of the Central Iberian Zone (Sant’Ovaia and Noronha, 2005). The subvertical lineations found in the metasediments are parallel to the subvertical folds axes, which are observed in the field. The Rb-Sr age (314 11 Ma) previously obtained in the Lavadores granite cannot represent an emplacement age since structural studies have evidenced a late tectonic emplacement (Late Carboniferous-Permian) of the granite body rather than a syntectonic emplacement. The lack of internal structures led to a model of magma ascent and emplacement after the last Variscan folding event occurred. In addition, the country rocks are clearly deformed by this Variscan event, which predates pluton emplacement. The U-Pb zircon age 298 11 Ma obtained in the present study is consistent with field relationships and structural data and suggest a post-tectonic emplacement. This posttectonic feature of the Lavadores granite is also supported by the magmatic nature of the microstructures, which suggest that the magma did not suffer further significant deformation once crystallized. In spite of a limited number of data, we may propose that the Lavadores granite can be considered a late to postorogenic (post-D 3 -290-299) granite with an age constrained to 298 11 Ma whose emplacement was controlled by the WNW-ESE local structures linked with a dextral movement in this sector of the north-south trending PTSZ. Nevertheless, tectonic control was only moderated since no related low temperature solid-state microstructures appear. Acknowledgements This research was carried out at the Geology Center (Porto University), an R and D unit from Portuguese Foundation of Science and Technology. The authors which to thank J. Leterrier for his assistance at CRPG (Nancy, H.C.B. Martins et al. / C. R. Geoscience 343 (2011) 387–396 394 France) and to the CEMUP (Porto University) for SEM analyses. We would like to thank to an anonymous reviewer and to Aude Ge ´belin for constructive comments that helped to greatly improve the manuscript. References Arthaud, F., Matte, Ph, 1975. Les de ´crochements tardi-hercyniens du SudOuest de l’Europe. Ge ´ome ´trie et essai de reconstituition des conditions de la de ´formation. Tectonophysics 25 (1/2), 139–171. Be Mezeme, E., Faure, M., Chen, Y., Cocherie, A., Talbot, J.-Y., 2007. 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