THE IBERIAN VARISCAN OROGEN - the analysis of continental crust features, the ... of relief. The Variscan orogeny ... The importance of the Iberian Variscan orogen lies in its

  • Published on

  • View

  • Download


THE IBERIAN VARISCAN OROGENC H A P T E R 1Martnez Cataln, J.R.Aller, J.Alonso, J.L. Bastida, F.Aerial view of the tectonic repetition of limestone beds in the Lncara Formation, Primajas duplex structure of the Esla thrust (photo by J.L. Alonso)M a r t n e z C a t a l n , J . R . A l l e r, J - A l o n s o , J . L . a n d B a s t i d a , F.14Rocks of Upper Proterozoic to Carboniferous age - forming the Variscan or Hercynian orogen - crop out widely in the western part of the Iberian Peninsula, in what is called the Iberian or Hesperian Massif. These deformed rocks, often metamorphosed and intruded by different types of granitoids, were witness to the great mountain range formed in the late Paleozoic, basically in the Late Devonian and Carboniferous (between 370 and 290 million years ago), by the convergence and collision of two major continents: Laurasia and Gondwana.The Iberian Massif constitutes a geological framework of global interest. It is unique due to the continuity of its exposures and because it displays excellent records allowing the analysis of continental crust features, the tectonic, metamorphic and magmatic evolution of orogens, and therefore provides enormously relevant data about the lithospheric dynamics during the latest Precambrian and the Paleozoic.The Variscan orogen forms the basement of the Iberian Peninsula and of most of western and central Europe. A crustal basement is the result of an orog-eny, that is, the consequence of a deep remobilization of the continental crust caused by the convergence of plates, and is associated to uplift and the creation of relief. The Variscan orogeny is the name given to the whole set of geological processes which deeply modified the continental crust of western Europe and the north and northwest of Africa during the Late Paleozoic (Devonian-Permian). In its long period of activity (approximately 80 million years), this orogeny shortened and intensely deformed those sediments deposited previously along vast continental margins, remobilized the prior basement on which they laid, generated a new crust by partial melting of the former, added fragments of oceanic crust and mantle, eroded and re-sedimented part of the newly formed crust, and deformed the majority of the new sediments.The importance of the Iberian Variscan orogen lies in its location close to three big orogenic belts: Caledonian, Variscan and Appalachian. Given the diversity and quality of the outcrops, it is one of the key geologi-cal frameworks recording the latest Precambrian and Paleozoic evolution of the planet, the deformation and generation of structures at different levels of the continental crust, the thermal history and the genera-tion of granitoids, all within the context of an active continental margin (latest Precambrian) and a conti-nental collision (Variscan Orogen).What crops out in the Iberian Peninsula from that basement (Iberian Massif) is part of a much longer orogenic belt, extending to the north and east through Central Europe into Poland, where it is shifted by a tectonic line known as Thornqvist Fault, and continu-ing towards south Asia.On the opposite side, the belt extends along north and northwest Africa parallel to the Atlantic margin. However, the Atlantic did not exist when the belt was formed at the end of the Paleozoic. In its place, what presently is North America (then part of Laurentia) went around the Variscan orogen and a wide belt developed along its eastern margin: the Appalachians.Figure 1 shows a paleogeographic reconstruction of the continental masses at the end of the Paleozoic. It is noticeable how Iberia, the west of France and the south of Great Britain used to occupy a key posi-tion within the Variscan belt, at the junction of the three most important Paleozoic orogenic belts: the Appalachians to the southwest, the Caledonides to the northwest, and the Variscan to the northeast. Besides, Iberia shares with west France a marked and striking bend or curvature known as the Ibero-Armorican Arch (Ribeiro et al., 1995).The former reconstruction allows to infer the ultimate cause of the orogeny, since a set of continental crustal blocks are nearby but separated by orogenic belts. It is thus clear that convergence caused the orogenic pro-cesses, and continental collision was the final result. We are talking about the convergence of three large tectonic plates: Laurentia (North America), Baltica (Scandinavia, northern belt of Europe and Russia), and Gondwana (Africa, South America, Antarctica, India and Australia). The final result was the creation, by the amalgamation of many continental masses, of a supercontinent, in this case the last Pangea generated by the continuing geodynamics of our planet.Being such an old orogenic belt (its main development finished 290 million years ago), it is to be expected that the continental crust generated is already totally balanced (thermally and isostatically), and the orogenic reliefs should have completely disappeared. However, Figure 1. Scheme showing the position of the Iberian Peninsula in relation to the Appalachians and the Caledonian and Variscan belts. Modified from Neuman and Max (1989).15THE IBERIAN VARISCAN OROGENthe subsequent history of the Iberian Peninsula origi-nated new reliefs, and that is what makes the Iberian Variscan orogen even more interesting.As a matter of fact, the Iberian Peninsula did not even exist at the end of the Paleozoic, but was a later result of the separation of the African and Eurasian plates. The Iberian crustal block ended up with Eurasia in the first fragmentation (Middle Jurassic), but was later iso-lated in the Early Cretaceous with the opening of the Bay of Biscay and the Pyrenean line, remaining at the mercy of both plates dynamics from then onwards, which began their convergence in the Paleocene and mid Eocene. This convergence, which is still active, deeply remobilized the Variscan basement in the Betic Range, and with less intensity in the Pyrenees, Iberian Range, Demanda Range, and several other modern mountain ranges. Some of these mountain ranges are aligned from east-northeast to west-soutwest (Cantabrian Range, Ancares, Montes de Len, Central System and the Portuguese extension through Serra da Estrela, Sierra Morena and many other minor reliefs) reflecting the north-south convergence of the African and Eurasian plates, and resulting in excellent exposures of the Variscan basement.For a better presentation of the most outstand-ing features of the Variscan orogen in the Iberian Peninsula, the different areas of the Massif will be described according to the scheme proposed by Julivert et al. (1972) (Figure 2). The five zones parallel and concentric to the Ibero-Armorican Arch are: Cantabrian Zone, West Asturian-Leonese Zone, Central Iberian Zone, Ossa-Morena Zone and South Portuguese Zone.The Galicia-Trs-os-Montes Zone of Farias et al. (1987) has also been added, although it is not a belt of the orogen but an allochthonous crustal block thrusted over the Central Iberian Zone.Figure 3 shows two schematic sections through the Iberian Massif, representative of the northwest (Prez Estan et al., 1991) and of the southwest (Simancas et al., 2002) of the Iberian Massif. It can be noticed that we are dealing with a belt with double centrifuge vergence.In the Iberian Massif there are several structures, which due to their geological interest together with the good exposure, have been chosen as Geosites: The Esla River Thrust in the Cantabrian Zone, the Mondoedo Thrust in the West Asturian-Leonese Zone, Sierra del Caurel in the Central Iberian Zone, and the Cabo Ortegal Complex in the Galicia-tras-os-Montes Zone (Figure 4).Figure 2. Zonation of the Iberian Massif according to the subdivision proposed by Julivert et al. (1972). The red lines mark the position of the sections in figure 3.The Cantabrian Zone represents the Iberian Massif foreland: an area of Paleozoic pre-orogenic sediments with relatively small thickness. These are Cambrian to Devonian shallow sea deposits, and display a wedging towards the external part as well as some stratigraphic discontinuities. This wedging is in part a result of crustal uplift followed by erosion in the late Devonian, and shows the change from a passive margin to Variscan collision. This erosion was followed by basin deepening in the earliest Carboniferous, followed by synorogenic sedimentation.The Cantabrian Zone is the most continental part of the Paleozoic basin and a magnificent example of foreland thrust belt. In addition, it displays an extremely tight tectonic bend representing the core of the Iberian-Armorican Arch.Thin-skinned tectonics, the deformation style of the outer crust, features in the Cantabrian Zone a sequen-tial development of thrusts and associated folds, con-temporaneous with the classic clastic wedges along the front of major thrusts. It is also characterized by M a r t n e z C a t a l n , J . R . A l l e r, J - A l o n s o , J . L . a n d B a s t i d a , F.16Figure 3, above. Two schematic geological sections across the Iberian Massif.a) According to Prez-Estan et al. (1991).b) According to Simancas et al. (2002).The location of the section is marked in figure 2.Figure 4, left. Geosites described in the text: 1) Esla River Thrust. 2) Sierra del Caurel. 3) Mondoedo Thrust. 4) Cabo Ortegal Complex.Figure 5, below. Esla River Thrust section showing the main allochthonous units and duplexes, according to Alonso (1985).deposits filling in piggy-back basins located over the thrusted slabs (Marcos and Pulgar, 1982; Rodrguez Fernndez et al., 2002). The tectonic structure is fur-ther complicated by the arcuate bending of the belt, which seems to be partially contemporaneous with thin-skinned tectonics, according to structural data (Prez-Estan et al., 1988).As a consequence of Cenozoic Alpine uplift, the Cantabrian Mountain Range displays magnificent landscapes with outstanding calcareous massifs, some of which are protected areas such as Montaa de Covadonga (Picos de Europa) National Park, and the natural parks of Somiedo and San Emiliano Valley.Several sites with panoramic outlooks allow to see large structures such as the Esla Thrust (Figures 5, 6, 7 and 8), the front of the Ponga Thrust, and that of the Picos de Europa Thrust, together with associ-ated smaller structures such as duplexes, frontal imbri-cations and ramps (Alonso, 1987; lvarez-Marrn and Prez-Estan, 1988).The Esla Thrust, in the province of Len, has been selected as a Geosite due to its magnificent outcrops of sedimentary formations of early Cambrian to early Carboniferous age, piled in a series of allochthonous structures (Figure 5). Inside this thrust, the frontal and internal areas of several minor thrust slabs and associ-ated sheets can be studied, as well as the geometrical relationships that the different thrust sheets and faults show amongst themselves and with the bedding (Figures 6 and 7).There are wonderful examples of thrust overstep geometries, of drape folds and associated fault propa-gation, and of frontal imbrications and duplexes, such as those at Primajas, Pardaminos and Pico Jano. The accumulated minimum shortening of all thrusts cropping out in this region is considered to be slightly above 92 km. Typical in this zone are the fault rocks developed under low temperature conditions and limited to a 1 to 2 meter thick band at the base of the Esla Thrust, which concentrates the deformation associated to the displacement, which is calculated to be around 19 km (Alonso, 1985, 1987).Synorogenic deposits are also very interesting, abundant and well preserved, with ages between Westphalian and Stephanian B (Figure 8). Their pres-ence allows to date the emplacement of thrusts, as well as the folds associated to the thrust and the reactiva-tion of bedding as a flexure-folding surface. Five main unconformities have been identified in the synorogenic sediments, although not all of them are discrete and some change laterally to progressive unconformities. The first two are related to the emplacement of the thrusts, whereas the remaining three are related to thrust reactivation and to the re-compression of folds associated to them (Alonso, 1985).THE IBERIAN VARISCAN OROGEN 17Figure 6. Esla River Thrust in the Valdor tectonic window. The colored line shows the thrust plane. On top of it: limestones of the Lncara Fm, slates of the Oville Fm and quartzites of the Barrios Fm (Cambrian-Ordovician). Below, Upper Devonian limestones of the Portilla Fm and a thin succession of Lower Carboniferous. To the left, the layout of the Aguasalio syncline is observed.Figure 7. Esla River Thrust north of Valdor. The thrust (upper colored line) superimposes with perfect parallelism Cambrian and Devonian layers. Within the relative autochtonous, a thrust partially repeats the calcareous succession of the Portilla Fm (lower colored line).The West Asturian-Leonese Zone is a very impor-tant unit because of its tectonic significance in relation to middle crust deformation problems and the dynam-ics of orogenic wedges, as well as for the study of the origin of granitoids and their relation to the orogeny. With regard to structural features, this zone forms a slate belt, not only because that is precisely the most frequent lithology, but also because it displays a wide belt with vertical folds and steeply-inclined axial-plane cleavage which curves in depth becoming asymptoti-cally parallel to a slightly-tilted mid-crustal detachment, and which may go across the whole crust.The West Asturian-Leonese Zone is divided into two domains: western and eastern. The eastern one, called Navia and Alto Sil domain (Marcos, 1973), is generally characterized by steeply-dipping folds and cleavage, as well as by the ductile deformation of greenschist facies, and includes some thrust-related repetitions. The seismic cross section ESCIN 3.3 (Figure 9) proves that the thrusts join at depth to (or are crossed by) a basal detachment which ends rooted M a r t n e z C a t a l n , J . R . A l l e r, J - A l o n s o , J . L . a n d B a s t i d a , F.18Figure 8. Syncline developed upon Stephanian conglomerates (thin colored lines) in relation to a reverse fault (thicker line) thrusting the limestones of the Alba and Barcaliente formations (Mountain Limestone). The fault is an example of flexural sliding along the stratigraphic surface during tightening of the Pea Quebrada syncline (Alonso, 1985).Figure 9. Interpretation of the seismic lines ESCIN-1 and ESCIN-3.3, placed one next to the other to show the large scale structure in this part of the Iberian Massif, as it is deduced from seismic reflection profiles. According to Prez-Estan et al. (1994) and Ayarza et al. (1998).at the Mohorovicic discontinuity much farther to the west. The western one, called Mondoedo Thrust domain, also shows steep folding and cleavage, although to the west the folds become recumbent and faulted folds, while cleavages turn subhorizontal and metamorphism increases.The coastal section between Cudillero and Viveiro estuary is extremely interesting in this area, as it offers an almost continuous structural section with spec-tacular deformation structures (Bastida, 1980; Pulgar, 1980).Uplifted areas also offer an excellent blend between geology and landscape. The Oscos region of west-ern Asturias, the Ancares Natural Park, and the gra-nitic massifs of La Tojiza and the surroundings of Viveiro, both north of Lugo province, deserve to be mentioned.The West Asturian-Leonese Zone, and the part of the Central Iberian Zone adjacent to it in Galicia, were key areas in the definition of the different types of granitoids and their interpretation (Capdevila, 1969; Capdevila et al.,1973). The oldest granitoids (Figure 10) are typically biotitic, frequently porphyritic, and include diorites, tonalites, granodiorites and monzo-granites. They are collectively called early granodior-ites, and are rocks originated deep at the base of the continental crust, with mantle contribution. Their development was followed by mid-crustal melting which generated peraluminous magmas of so-called leucogranites or two mica granites.Both the early granodiorite massifs and the leucogran-ites are syntectonic with ages between 350 and 305 Ma, broadly coinciding with Variscan deformation. The most modern group of granitoids is formed by a set of post-kinematic plutons (gabbros, tonalites, granodiorites and monzogranites). In contrast to the former, its emplacement is restricted to a short span of 295-285 Ma, a magmatic pulse suggesting a single cause which Fernndez-Surez et al. (2000) linked to the delamination of the mantle lithosphere at the end of the orogeny, and its replacement by a hotter asthe-nospheric mantle.The Mondoedo Thrust, and more specifically its basal shear zone in the coastal area of the Lugo province (Figure 11), has been selected as a Geosite. Its Cambrian slate and quartzite outcrops show the effects of tangential deformation of the second Variscan deformation phase (Bastida and Pulgar, 1978; Bastida et al., 1986; Aller and Bastida, 1993). Its interest stems from it being an exposure of the internal and deeper area of a thrust slab emplaced under ductile conditions in the beginning stages, and fragile in the last stages. Spectacular meso- and micro-structures are observed in a ductile shear zone related to crustal thrusting, with a thickness between 3 and 3.5 km. Some medium-grade metamorphic foliations, stretching lineations, and fault rocks developed under a wide temperature range, can also be studied.East-verging isoclinal folds are abundant and show a strong scattering of their hinges, very often displaying curved hinges and tight shapes belonging to sheath folds (Figures 12a, b and c). Folds are also affected by the development of a second axial-plane foliation and by a stretching lineation striking between N 100 and 110 E. Boudinage structures are also common affecting quartzites, as well as S-C structures, which are particularly abundant in Upper Proterozoic rocks at the base of Mondoedo Thrust, showing an ESE trend of displacement (Figure 12d). In addition, the basal thrust crops out at Aureoura beach (As Areouras) and, north of it, the autochtonous slab of the Mondoedo Thrust crops out in the tectonic window of Xistral (Gistral), as a train of regular folds affecting the thick homonymous quartzitic formation (Figure 12e).The Central-Iberian Zone comprises the central part of the Iberian Massif and is the widest of all the belts, around 400 km in the centre of the massif (Figure 2). The structure of the low metamorphic grade regions in the upper crustal levels is well defined at the surface by the Armorican Quartzite, which due to its resistance to weathering and erosion forms lined up reliefs bor-dering the elongated synclines in the southern part of this zone, such as Guadarranque, in Toledo, Caaveral (cropping out along Monfrage Natural Park) and San Pedro Range, in Cceres, and Herrera del Duque, THE IBERIAN VARISCAN OROGEN 19Figure 10. Granitic plutons of the Iberian Massif in relation with Variscan deformation stages (according to Lpez Plaza and Martnez Cataln, 1987).Figure 12. Structures associated to the basal shear zone of the Mondoedo Thrust: a) 2nd phase isoclinal folds showing hinge scattering. Cliff between Fazouro and Foz. b) Set of folds with folded hinges and en chelon distribution; the stretching lineation is parallel to the pencil. Cliff north of Nois. c) Cross section of a closed fold. Cliff south of Area Longa beach. d) S-C structures at the base of the Mondoedo Thrust in the SE limit of Areoura beach. The C surfaces (shear areas) dip around 30 to the east (left) and among them the S surfaces (schistosity) show sigmoidal geometry. e) Anticline on Lower Cambrian quartzites of the Mondoedo Autochton, underneath the basal thrust. Cliff southeast of Burela.M a r t n e z C a t a l n , J . R . A l l e r, J - A l o n s o , J . L . a n d B a s t i d a , F.20Figure 11. Geological cross section through the northern part of the Mondoedo Thrust in two versions. The one above shows lithostratigraphic units with folds and major faults. The one below shows regional metamorphism isogrades and main areas of ductile shear. The arrows point to the motion direction of the faults and shears (according to Martnez Cataln et al., 2003).between Badajoz and Ciudad Real. In the centre of the zone, the Tamames and Pea de Francia synclines crop out in the Batuecas Natural Park (Salamanca). In the north (Galicia) and in the Central System, the Armorican Quartzite also delineates those anticline cores with outcrops of the Ollo de Sapo Formation, a thick volcanic, subvolcanic and volcanoclastic sequence of Tremadoc-Arenig age (Parga Pondal et al., 1964; Dez Montes, 2006).The generic name of Armorican Quartzite is used, by analogy with the Armorican Massif (France), to refer to a mostly quartzitic lithostratigraphic unit deposited on a wide, stable and homogenous platform exist-ing in the Early Paleozoic. These quartzitic facies with Arenig (Lower Ordovician) trace fossils followed by a slate formation with trilobites, are not only present in the Central Iberian Zone, but also in other areas of the Iberian Massif. These facies extend from West Africa to Afghanistan, showing the enormous size of the marine platform. The platform was part of a passive continental margin, as inferred from the mostly shal-low marine sedimentary facies and its extraordinary continuity, as well as by the existence of synsedimen-tary normal faults. The Central Iberian Zone provides a magnificent field to study deformation under low to high metamorphic grade conditions. Low-grade meta-morphism is the most widely represented, particularly towards the south and southeast, in Extremadura and Toledo Mountains, where anchimetamorphic condi-tions are frequent. High-grade metamorphic rocks with extensive partial melting crop out within antifor-mal structures and a few domes, where a fast transi-tion between metamorphic grades is often observed. The transition of metamorphic zones is either thinned or incomplete, so several of these domes have been related to extensional detachments, for example in the region of Salamanca (Escuder Viruete et al., 1994; Dez Balda et al., 1995) and in Toledo (Hernndez Enrile, 1991). The natural parks of Sanabria Lake, in Zamora, and Arribes del Duero and Agueda, in Zamora and Salamanca, offer excellent exposures of the deeper structural levels of the range, similarly to Guadarrama and Gredos Ranges, where the granitic outcrops are also impressive.Differing deformation trends are evident within this zone, with a narrow northern domain with recumbent folds, a wider middle domain with vertical folds and usually not too tight (Dez Balda et al., 1990), and a very narrow southern domain with recumbent folds (Martnez Poyatos, 2002).Sierra del Caurel (Serra do Courel in Galician lan-guage), in the southern province of Lugo, has been selected as a Geosite representative of the great recumbent folds, with spectacular views of the folds affecting the Armorican Quartzite (Figures 13 and 14), formed during the first Variscan deformational phase.The geometry of the Sierra del Caurel folds, cropping out in an area 43 km long and 12 km wide, can be reconstructed thanks to the splendid outcrop condi-tions (Matte, 1968). It consists of two structures (Piornal anticline and Caurel syncline) with almost horizontal axial plane folds in the northern half. Even not being the biggest, these are the best outcrops of recumbent folds in the northern Iberian Peninsula. The anticline plunges to the south towards its roots. The overturned limb common to both folds reaches 10 km semi-wavelength in the central part, narrowing to the east and west. The hinge of the anticline is curved, varying between N100E and N160E from west to east. The most spectacular views are from the Quiroga to Seoane do Courel road (El Caurel syncline), at Alto do Castro, and from Busto and Froxn.The Ossa-Morena Zone is a key region to deter-mine the significance of the Cadomian orogeny (Neoproterozoic) and therefore to understand end-Precambrian plate dynamics and its continuation into the Paleozoic. The location of the zone, in the THE IBERIAN VARISCAN OROGEN 21Figure 13. El Caurel syncline, folding towards the Armorican Quartzite, on the eastern slope of the Ferreirio river.Figure 14, below. 2nd order anticline in the hinge zone of El Caurel syncline. The hinge is displayed by the Armorican Quartzite (coloured lined marking the top). At the summit of the relief, in the middle of the picture, the quartzite of the reverse flank of El Caurel Syncline.southern Iberian Massif (Figure 2) makes its structural evolution and its magmatism essential to understand Late Paleozoic dynamics. Places like Sierra Morena offer a good combination of geology and landscape all along the Aracena and Picos de Aroche Natural Park, and its extension to the east through Sierra Norte Natural Park.The combination of isotopic age and geochemical data in the Ossa-Morena Zone supports its evolution as an active margin followed by the scattering of the peri-Gondwanan terrains. In fact, up to now, this is the only zone in the Iberian Massif where ages of Cadomian metamorphism have been obtained. These ages span from 562 to 524 Ma (Blatrix and Burg, 1981; Dallmeyer and Quesada, 1992; Ochsner, 1993; Ordez et al., 1997) and even if the youngest ones may reflect late- to post-orogenic thermal events, the earlier ones clearly show a latest Proterozoic dynamo-thermal metamorphism.Cadomian or end-Proterozoic magmatism has been identified in the West Asturian-Leonese and Central Iberian Zones, but it is particularly well defined in the Ossa-Morena Zone. Here, the geochemistry and ages fit within a long evolution of 120 My, allowing to identify several stages (Oschner, 1993): anorogenic rift (620-590 Ma), early calcalkaline orogenic magmatism (590-540 Ma), peraluminous orogenic magmatism (530 Ma), late-orogenic calcalkaline (525-510 Ma) and alkaline (500 Ma) magmatism, and post-orogenic rift (490-470 Ma). The last synorogenic stages were con-temporaneous to the detachment and separation of the first peri-Gondwanan crustal fragments.The northeast and southwest boundaries of the Ossa-Morena Zone are important geological structures, most probably related with former plate boundaries. The Beja-Acebuches ophiolite along the southwest mar-gin represents an oceanic suture. Furthermore, there are strong differences between the granitoids of the Ossa-Morena Zone and those of the rest of the Iberian autochton. The granitic massifs are usually of limited extension (Figure 10), lack the typical big plutons of the Central Iberian Zone, and include more abundant basic rocks, which calls for a bigger mantle contribu-tion. The southern vergence of Variscan structures in the Ossa-Morena and South Portuguese Zones, and the existence of a crustal suture, suggest subduction of the oceanic lithosphere towards the north, underneath the Ossa-Morena Zone, which also explains its early magmatism. The Ossa-Morena Zone represents the complex evolution of a continental margin during the Late Paleozoic, although in this case it is not associated to a context of Cordilleran orogeny or long-lived active margin, but to the convergence and collision of two large continental masses, Gondwana and Laurasia.The South Portuguese Zone is the southernmost of the Iberian Massif and holds some of the keys of Variscan evolution. It is a thin-skinned thrust belt and, from the point of view of orogenic evolution, the zone is considered an example of the importance that transcurrent faults may have in continental deformation. The northern part of the zone is an interesting Variscan suture which crops out along southern Sierra Morena, most of it inside the Natural Park of Aracena and Picos de Aroche. In Portugal, the coastal sections of Baixo Alentejo and Algarve are worth mentioning.A set of basic rocks cropping out along the boundary between the South Portuguese and Ossa-Morena Zones is interpreted as a fragment of oceanic lithosphere (Figure 3), represented by the Beja-Acebuches unit. South of it, there is a Lower Devonian - Carboniferous basement accretion prism, the Pulo do Lobo anti-form (Munh et al.,1986; Oliveira, 1990; Quesada et al.,1994; Onzime et al., 2002). The rest of the South Portuguese Zone comprises the Iberian Pyrite Belt, one the most important volcanogenic polymetallic sulphide deposits of the planet. The Pyrite Belt volcanism, even if bimodal and dominated by intermediate and acid facies dated in the Devonian-Carboniferous bound-ary (347-355 Ma; Quesada, 1999), suggests a relation with a magmatic arc.The South Portuguese Zone displays a south-vergent thin-skinned tectonic overthrust, that is, opposed to that in the other structurally comparable belt, the Cantabrian Zone. The genetic significance of these two external zones of the Iberian Massif is different. Whereas the Cantabrian Zone is a Gondwanan over-thrust foreland belt, the South Portuguese Zone first developed as a foredeep basin, and later as an accre-tionary complex, particularly in the northern part. The subduction of oceanic lithosphere under the marginal prism ended with the arrival of continental crust, when a terrain, most likely peri-Gondwanan, forming the basement underlying the South Portuguese Zone, came under the accretionary prism and developed a thin-skinned thrust belt on top of it.The zone also features mostly sinistral transcurrent shear ing , and has been proposed to be contemporaneous with tangential deformation. The most abundant stretching lineations in the Beja-Acebuches ophiolite are subparallel to the amphibolite band (Crespo Blanc, 1991), although the first movements of the ophiolites record the convergent component (Onzime et al., 2002). This suggests that amphibolite shearing represents the transition from a ductile overthrust to a sinistral ductile tear-fault. Some structures display the kinematics of oblique convergence, but it is more common for the deformation to undergo partitioning into convergent and transcurrent components, each one creating its own structures. Both situations point to transpression (Sanderson and Marchini, 1984), a deformation regime whose geotectonic significance is that of oblique collision between the plate underneath the thrust belt of the South Portuguese Zone, and the Iberian autochthonous plate (Silva et al., 1990).The Galicia-Trs-os-Montes Zone includes the alloch-thons of Cabo Ortegal, rdenes and Malpica-Tui in M a r t n e z C a t a l n , J . R . A l l e r, J - A l o n s o , J . L . a n d B a s t i d a , F.22Galicia (Spain), and of Bragana and Morais in Trs-os-Montes (Portugal), as well as a common underlying thrust sheet which has been called the Schistose or Parautochtonous Domain (Farias et al., 1987; Ribeiro et al., 1990), although it would be more appropri-ate to call it Lower Allochthon. Due to the variety of terrains comprised by the allochthonous complexes, each with different origin and tectonometamorphic evolution, this zone is a basic reference to understand Paleozoic geodynamics. It is herein described at the end of this chapter because of the exotic character of the units, and because it does not fit the continuous and concentric trend of the rest of the zones making up the Iberian Massif (Figure 3).The units of the allochthonous complexes are grouped into basal, intermediate or ophiolitic, and upper units, according to their structural position within the thrust pile. Many of them have recrystallized under deep THE IBERIAN VARISCAN OROGEN 23Figure 15. Evolution of the peri-Gondwanan terrain preserved in the upper allochthonous units, according to Gmez Barrero et al. (2007), based upon the reconstruction of continental masses and oceans by Winchester et al. (2002). In the Silurian, the lapetus ocean almost disappeared, whereas the Rheic ocean is still very wide, although it is being subducted between Gondwana and Laurentia.conditions, and are thus representative of the lower crust, and sometimes even of the underlying mantle.The basal units represent the most external margin of Gondwana, with magmatic evidence for Ordovician rifting, and metamorphic evidence for early Variscan subduction (Gil Ibarguchi and Ortega Girons, 1985; Pin et al., 1992; Arenas et al., 1995; Rodrguez Aller, 2005). Ordovician rifting continued with the separation of a peri-Gondwanan terrain and the creation of oce-anic lithosphere beneath the Rheic Ocean between the terrain and the new border of Gondwana. Fragments of oceanic lithosphere with different isotope ages are present in the suture included in the Galicia-Trs-os-Montes Zone, mostly linked to the Rheic ocean (Daz Garca et al., 1999; Snchez Martnez et al., 2006, 2007; Arenas et al., 2007).The evolution of the upper units indicates their multi-ple orogenic character, with a first deformation during the Lower Ordovician and later recycling by Variscan collision. The associated magma chemistry and meta-morphic evolution of the upper units suggests a vol-canic arc environment in the Early Ordovician (Abati et al., 1999; Andonaegui et al., 2002; Fernndez-Surez et al., 2002). It would be an arc developed along the Gondwana margin, and its detachment would have left behind a backarc basin which in time would have evolved to generate the Rheic Ocean. Figures 15 and 16 show schematically, in a map and a section, a pos-sible evolution of the plates and terrains involved in Variscan collision, according to the interpretations by Gmez Barreiro et al. (2007) and Martnez Cataln et al. (2007), respectively.The existence of only one oceanic domain between Avalonia and Gondwana has been taken into con-sideration, although the evolution was undoubtedly complex. The opening of this domain, called Rheic, was already taking place while the convergence between Avalonia and Laurentia closed the lapetus ocean in the Early Ordovician. This convergence meant the first Taconic orogenic event, 490-480 Ma ago, and ended M a r t n e z C a t a l n , J . R . A l l e r, J - A l o n s o , J . L . a n d B a s t i d a , F.24Figure 16. Evolution of the Rheic ocean and the Variscan orogen according to Martnez Cataln et al. (2007).with the amalgamation of Avalon 480-430 Ma ago, that is, between the Middle Ordovician and Early Silurian. From the Middle Silurian on, deformation progressively started to affect the peri-Gondwanan terrains and the Gondwana margin itself. Apparently, an accretionary prism developed on the margin of Laurentia following the amalgamation of Avalonia (Figure 16). The Galicia-Trs-os-Montes Zone records the progressive incorpora-tion onto the orogenic prism of a volcanic arc repre-sented by the upper units, an imbricate pile of oceanic lithosphere of variable ages, and the partial westward subduction of the outermost margin of Gondwana, represented by the basement units (Martnez Cataln et al., 1997, 2007). The blocking of continental subduc-tion in the late Devonian marked the transition to a collisional regime. The subducted basal units were over-thrusted onto the external platform of Gondwana in the Early Carboniferous, and a sheet of sediments was wedged underneath forming the Schistose Domain. Later, intracontinental deformation gradually affected more external areas of the orogen. The fourth Geosite selected in the Iberian Massif is the Cabo de Ortegal Complex, in the province of La Corua, as it is an excellent representative of the THE IBERIAN VARISCAN OROGEN 25Figure 18. Northern end of the eclogite belt of the Cabo Ortegal Complex at Punta dos Aguillns. This is part of the allochthonous unit of La Capelada, structurally the highest of the complex. Figure 17. Geological map and cross section of the Cabo de Ortegal complex based on Vogel (1967), Marcos et al. (1984) and Arenas (1988).Figure 19. Pictures of the Cabo de Ortegal Complex: a) Recumbent fold syncline in the La Capelada Unit, with granulites of the Bacariza Fm in the core (grey) surrounded by ultrabasic rocks (yellowish). The colored line marks the contact. Southwest of San Andrs de Teixido. b) Closed shaped folds developed during the thrust which emplaced the catazonal units. Unit of Cedeira. c) Shear area at Carreiro, north of Cedeira, limited by two surfaces dipping 45. It represents the overthrust separating the Cedeira Unit to the east (right), from the Purrido Unit to the west. d) Detail of the upper limit of Carreiro shear, showing a thrust plane under which some folds can be observed. e) Punta Candelaria (o Candieira). The lighter colored rocks are amphibolites, gneisses and ultrabasic rocks of the shear area of Carreiro, while the darker rocks to the left are amphibolites of the Purrido Unit. f) Pillow-lava breccias in the ophiolitic Somozas Mlange, the structurally lower unit of the Cabo de Ortegal Complex. Southern part of the Ensenada de Espasante.exotic terrains making up the Galicia-Trs-os-Montes Zone. All the groups of allochthonous units are present in this complex (Figure 17), and one of those units has provided the oldest rocks in the Iberian Peninsula (1160 Ma; Snchez Martnez et al., 2006). In addition, this complex stands out for the quality of its exposures and its spectacular landscapes. The estuaries of Cedeira, Ortigueira and Espasante offer magnificent structural sections, combined with the cliffs on both sides of the cape (Figure 18) and with the outcrops of Sierra de la Capelada.The Cabo de Ortegal Complex includes a great expo-sure of two catazonal allochthonous units: a deeper M a r t n e z C a t a l n , J . R . A l l e r, J - A l o n s o , J . L . a n d B a s t i d a , F.26one, representative of the lower crust and the upper mantle of a continent, and/or a volcanic arc, corre-sponding to a peri-Gondwanan terrain (Galn and Marcos, 1997; Santos et al., 2002). These are the Cedeira and La Capelada units (Marcos et al., 1984, 2002), cropping out within the core of a SW-NE elongated synform with a size of 28 by 12 km. The catazonal units are part of the upper part of the allochthonous complexes, and consist of rocks which underwent high pressure and high temperature meta-morphism (Vogel, 1967; Menda Aranguren, 2000). They include granulites and eclogites structurally overlying ophiolitic units representing fragments of Paleozoic oceanic lithosphere (Figure 19), and base-ment units representative of the Gondwana margin. These ophiolites and basement units crop out in an imbricate zone, structurally emplaced at the base of the complex, and include an area of tectonic mixture known as the Somozas Mlange (Arenas, 1988). The imbricate zone continues underneath, affecting the Schistose Domain, which is here formed by a series of sheets comprising metasedimentary and metavolcanic rocks of Silurian and Ordovician age (Valverde-Vaquero et al., 2005).The whole set of the complex is key to reconstruct the evolution of the Rheic Ocean. It probably includes the largest eclogite exposure in the world, with high-pressure metamorphosed basic rocks indicative of subduction processes. Given the excellent exposure conditions of the lower crust, the processes of burial and exhumation in an orogenic cycle can be studied. The Cabo Ortegal Complex is also a good example of a deep allochthonous unit emplaced into an epi-zonal crustal domain. The structural sequence shows a spectacular development of structures at all scales, from recumbent folds, ductile shears and thrusts (Figure 19), to microfolds, boudinage, porphyroclast systems, lineations and foliations. It constitutes a natural laboratory for fabric deformation ranging from high pressure and temperature conditions to greenschist facies.Summing up, the Iberian Massif provides the keys to understand the history of the circum-Atlantic domain during the Late Proterozoic and the Paleozoic, particularly with regard to the evolution of the northern margin of Gondwana and the Rheic ocean. It also offers excellent exposures and structures to study deformation mecha-nisms in a collisional orogenic belt at different depths, particularly the large thrust at crustal and even litho-spheric scale. It also turns out to be a paramount refer-ence to understand the genesis of granitoids in orogenic collisional contexts. Its importance also lies on the fact that not many times a complete section including both forelands of an old collisional orogen is found preserved. The selected Geosites represent some of those keys but, in addition, the Iberian Massif features two particularly outstanding structural and tectonic characteristics: the transpressive orogen of the peninsular southwest, and the arcuate structure, very tight in the northwest, known as Asturian Knee and Ibero - Armorican Arch at the level of the Variscan orogenic belt.The transpressive orogen in the southwest of the Iberian Peninsula, from the Central Iberian Zone to the South Portuguese Zone, displays peculiar features in relation to the deeply transpressive nature (oblique collision) under which it formed in the Late Paleozoic (Ribeiro et al., 1990; Quesada, 1991). The reconstruc-tion of this sector is essential to understand the vast circum-Atlantic Paleozoic orogenic domain, presently scattered in three continents (Europe, Africa and America) with a triple junction among the three of them located precisely in this Iberian southern sec-tion (Figure 1).The spectacular Iberian-Armorican Arch (arcuate struc-ture) is a first-rate imbricate structure of geological units arched or bent around a sub-vertical axis located to the east and with centripetal emplacement direc-tions. The most external zones of the Iberian foreland are located in the center of the arch (Cantabrian Zone), with well-preserved Carboniferous synorogenic depos-its. To the west, a complete section of the Variscan Orogen consists of a piling of E-to-NE-vergent thrusts including (from lower-eastern to upper-western), the Cantabrian, West Asturian-Leonese, Central Iberian and Galicia-Trs-os-Montes zones. The first three represent progressively deeper units of the Paleozoic continental margin of the Iberian plate, whereas the fourth one comprises the allochthonous exotic com-plexes of Galicia-Trs-os-Montes. Towards the exterior of the arch, there are two more areas, Ossa-Morena and South Portuguese Zones, where transpressive deformation may provide some clues about the for-mation of the arch itself.The models proposed to explain the Ibero-Armorican Arch are varied. One of them is that of strict orocli-nal bending, with an initial rectilinear belt which later became bent. A popular model is that of the indenter, which suggests the presence of a rigid buttress out of Gondwana which might have caused the orogen bend during its collision with Laurentia (Matte and Ribeiro, 1975; Matte, 1986; Ribeiro et al., 1995).THE IBERIAN VARISCAN OROGEN 27R E F E R E N C E SABATI, J., DUNNING, G.R., ARENAS, R., DAZ GARCA, F., GONZLEZ CUADRA, P., MARTNEZ CATALN, .J.R. and ANDONAEGUI, P. (1999). Early Ordovician orogenic event in Galicia (NW Spain): evidence from U-Pb ages in the uppermost unit of the Ordenes Complex. Earth Planet. Sci. Lett., 165, 213-228.ANDONAEGUI, P., GONZLEZ DEL TNAGO, J., ARENAS, R., ABATI, J., MARTNEZ CATALN, J.R., PEINADO, M. and DAZ GARCA, F. (2002). Tectonic setting of the Monte Castelo gabbro (Ordenes Complex, northwestern Iberian Massif): Evidence for an arc-related terrane in the hanging wall to the Variscan suture. En: Martnez Cataln, J.R., Hatcher, R.D., Arenas, R. and Daz Garca, F. (Eds.), Variscan-Appalachian Dynamics: the Building of the Late Paleozoic Basement, Geol. Soc. Am. Spec. Paper, 364, 36-56.ALLER, J. and BASTIDA, F. (1993). Anatomy of the Mondoedo Nappe basal shear zone (NW Spain). J. Struct. Geol., 15, 1405-1419.ALONSO, J.L. (1985). Estructura y evolucin tectonoestratigrfica de la regin del Manto del Esla (Zona Cantbrica, NW de Espaa). Diputacin Provincial de Len, Inst. Fray Bernardino de Sahagn, 276 p.ALONSO, J.L. (1987). Sequences of thrust and displacement transfer in the superposed duplexes of the Esla Nappe Region (Cantabrian Zone, NW Spain). J. Struct. Geol., 9, 969-983.LVAREZ-MARRN, J. and PREZ-ESTAN, A. (1988). Thin-skinned tectonics in the Ponga Region (Cantabrian Zone, NW Spain). Geol. Rundsch., 77, 539-550.ARENAS, R. (1988). Evolucin petrolgica y geoqumica de la unidad alctona inferior del complejo metamrfico bsico-ultrabsico de Cabo Ortegal (Unidad de Moeche) and del Silrico paraautctono, Cadena Hercnica Ibrica (NW de Espaa). Corpus Geologicum Gallaeciae, 4, 543 p.ARENAS, R., RUBIO PASCUAL, F.J., DAZ GARCA, F. and MARTNEZ CATALN, J.R. (1995). High-pressure micro-inclusions and development of an inverted metamorphic gradient in the Santiago Schists (Ordenes Complex, NW Iberian Massif, Spain): evidence of subduction and syn-collisional decompression. J. metam. Geol., 13, 141-164.ARENAS, R., MARTNEZ CATALN, J.R., SNCHEZ MARTNEZ, S., DAZ GARCA, F., ABATI, J., FERNNDEZ-SUREZ, J., ANDONAEGUI, P. and GMEZ-BARREIRO, J. (2007). Paleozoic ophiolites in the Variscan suture of Galicia (northwest Spain): distribution, characteristics and meaning. En: Hatcher, R.D., Jr., Carlson, M.P., McBride, J.H. and Martnez Cataln, J.R. (Eds.), 4-D framework of continental crust. Geo.l Soc. America Mem., 200.AYARZA, P., MARTNEZ CATALN, J.R., GALLART, J., DAOBEITIA, J.J. and PULGAR, J.A. (1998). Estudio Ssmico de la Corteza Ibrica Norte 3.3: a seismic image of the Variscan crust in the hinterland of the NW Iberian Massif. Tectonics, 17, 171-186.BASTIDA, F. and PULGAR, J.A. (1978). La estructura del Manto de Mondoedo entre Burela and Tapia de Casariego (Costa Cantbrica, NW de Espaa). Trab. Geol. Univ. Oviedo, 10, 75-124.BASTIDA, F., MARTNEZ CATALN, J.R. and PULGAR, J.A. (1986). Structural, metamorphic and magmatic history of the Mondoedo nappe (Hercynian belt, NW Spain). J. Struct. Geol., 8, 415-430.BLATRIX, P. and BURG, J.P. (1981). 40Ar/39Ar dates from Sierra Morena (Southern Spain): Variscan metamorphism and Cadomian Orogeny. Neues Jahrb. Mineral. Monatsch., 10, 470-478.CAPDEVILA, R. (1969). Le mtamorphisme rgional progressif et les granites dans le segment hercynien de Galice nord oriental (NW de l'Espagne). Thesis, Universit de Montpellier. 430 p.CAPDEVILA, R., CORRETG, L.G. and FLOOR, P. (1973). Les granitodes varisques de la Meseta Ibrique. Bull. Soc. Gol. Fr., 15, 209-228.CRESPO BLANC, A. (1991). Evolucin geotectnica del contacto entre la Zona de Ossa-Morena y la Zona Surportuguesa en las sierras de Aracena and Aroche (Macizo Ibrico meridional): un contacto mayor de la Cadena Hercnica Europea. Fac. Ciencias, Granada, 328 p.DALLMEYER, R.D. and QUESADA, C. (1992). Cadomian vs. Variscan evolution of the Ossa-Morena zone (SW Iberia): field and 40Ar/39Ar mineral age constraints. Tectonophysics, 216, 339-364.DAZ GARCA, F., ARENAS, R., MARTNEZ CATALN, J.R., GONZLEZ DEL TNAGO, J. and DUNNING, G. (1999). Tectonic evolution of the Caren ophiolite (Northwest Spain): a remnant of oceanic lithosphere in the Variscan belt. J. Geology, 107, 587-605.DEZ BALDA, M.A., MARTNEZ CATALN, J.R. and AYARZA, P. (1995). Syn-collisional extensional collapse parallel to the orogenic trend in a domain of steep tectonics: the Salamanca detachment zone (Central Iberian Zone, Spain). J. Struct. Geol., 17, 163-182.DEZ BALDA, M.A., VEGAS, R. and GONZLEZ LODEIRO, F. (1990). Central-Iberian Zone. Autochthonous Sequences. Structure. En: Dallmeyer, R.D. and Martnez Garca, E. (Eds.), Pre-Mesozoic Geology of Iberia, Springer-Verlag, Berln, 172-188.DEZ MONTES, A. (2006). La Geologa del Dominio "Ollo de Sapo" en las comarcas de Sanabria and Terra do Bolo. Tesis Doctoral, Universidad de Salamanca, 496 p.ESCUDER VIRUETE, J., ARENAS, R. and MARTNEZ CATALN, J.R. (1994). Tectonothermal evolution associated with Variscan crustal extension in the Tormes Gneiss Dome (NW Salamanca, Iberian Massif, Spain). Tectonophysics, 238, 117-138.FARIAS, P., GALLASTEGUI, G., GONZLEZ-LODEIRO, F., MARQUNEZ, J., MARTN PARRA, L.M., MARTNEZ CATALN, J.R., MACI, J.G. DE PABLO and RODRGUEZ FERNNDEZ, L.R. (1987). Aportaciones al conocimiento de la litoestratigrafa and estructura de Galicia Central. Memrias da Faculdade de Cincias, Universidade do Porto, 1, 411-431.M a r t n e z C a t a l n , J . R . A l l e r, J - A l o n s o , J . L . a n d B a s t i d a , F.28THE IBERIAN VARISCAN OROGEN 29FERNNDEZ-SUREZ, J., GUTIRREZ-ALONSO, G., JENNER, G.A. and TUBRETT, M.N. (2000). New ideas on the Proterozoic-Early Paleozoic evolution of NW Iberia: insights from U-Pb detrital zircon ages. Precambrian Research, 102, 185-206.FERNNDEZ-SUREZ, J., CORFU, F., ARENAS, R., MARCOS, A., MARTNEZ CATALN, J. R., DAZ GARCA, F., ABATI, J. and FERNNDEZ, F. J. (2002). U-Pb evidence for a polyorogenic evolution of the granulitic-eclogitic units of the NW Iberian Massif: Contr. Mineral. Petrol., 143, 236-253.FRANKE, W. (1989). Tectonostratigraphic units in the Variscan belt of central Europe. En: Dallmeyer, R.D. (Ed.), Terranes in the Circum-Atlantic Paleozoic Orogens. Geol. Soc. Am. Spec. Paper, 230, 67-90.GALN, G. and MARCOS, A. (1997). Geochemical evolution of high-pressure mafic granulites from the Bacariza formation (Cabo Ortegal complex, NW Spain): an example of a heterogeneous lower crust. Geol. Rundsch., 86, 539-355.GARCA-CORTS, A., RBANO, I., LOCUTURA, J., BELLIDO, F., FERNNDEZ-GIANOTTI, J., MARTN-SERRANO, A., QUESADA, C., BARNOLAS, A. and DURN, J. J. (2000). Contextos geolgicos espaoles de relevancia internacional: establecimiento, decripcin y justificacin segn la metodologa del proyecto Global Geosites de la IUGS. Bol. Geol. Min., 111-6, 5-38. Madrid.GARCA-CORTS, A., RBANO, I., LOCUTURA, J., BELLIDO, F., FERNNDEZ-GIANOTTI, J., MARTN-SERRANO, A., QUESADA, C., BARNOLAS, A. and DURN, J. J. (2001). First Spanish contribution to the Geosites Project: list of the geological frameworks established by consensus. Episodes, 24 (2), 79-92.GIL IBARGUCHI, I. and ORTEGA GIRONS, E. (1985). Petrology, structure and geotectonic implications of glaucophane-bearing eclogites and related rocks from the Malpica-Tuy (MT) Unit, Galicia, Northwest Spain. Chemical Geol., 50, 145-162.GMEZ BARREIRO, J., MARTNEZ CATALN J.R., ARENAS, R., CASTIEIRAS, P., ABATI, J., DAZ GARCA, F. and WIJBRANS, J.R. (2007). Tectonic evolution of the upper allochthon of the rdenes Complex (northwestern Iberian Massif): structural constraints to a polyorogenic peri-Gondwanan terrane. En: Linnemann, U., Nance, R.D., Kraft, P. and Zulauf, G. (Eds.), The evolution of the Rheic Ocean: From Avalonian-Cadomian active margin to Alleghenian-Variscan collision. Geol. Soc. Am. Spec. Paper, 423, 315-332.HERNNDEZ ENRILE, J.L. (1991). Extensional tectonics of the Toledo ductile-brittle shear zone, central Iberian Massif. Tectonophysics, 191, 311-324.JULIVERT, M., FONTBOT, J.M., RIBEIRO, A. and CONDE, L. (1972). Mapa Tectnico de la Pennsula Ibrica y Baleares E. 1:1.000.000. Inst. Geol. Min. Espaa, Madrid, 113 p.LEFORT, J.P. (1989). Basement Correlation Across the North Atlantic. Springer-Verlag, Berln, 148 p.LPEZ PLAZA, M. and MARTNEZ CATALN, J.R. (1987). Sntesis estructural de los granitoides hercnicos del Macizo Hesprico. En: Bea, F., Carnicero, A,, Gonzalo, J.C., Lpez-Plaza, M. and Rodrguez Alonso, M.D. (Eds.), Geologa de los granitoides and rocas asociadas del Macizo Hesprico, Rueda, Madrid, 195-210.MARCOS, A. (1973). Las Series del Paleozoico Inferior y la estructura herciniana del occidente de Asturias (NW de Espaa). Trab. Geol., Univ. Oviedo, 6, 1-113.MARCOS, A. and PULGAR, J.A. (1982). An approach to the tectonostratigraphic evolution of the Cantabrian Foreland thrust and fold belt, Hercynian Cordillera of NW spain. Neues Jb. Geol. Palont. Abh., 163, 256-260.MARCOS, A., MARQUNEZ, J., PREZ-ESTAN, A., PULGAR, J.A. and BASTIDA, F. (1984). Nuevas aportaciones al conocimiento de la evolucin tectonometamrfica del Complejo de Cabo Ortegal (NW de Espaa). Cuad. Lab. Xeol. de Laxe, 7, 125-137.MARCOS, A., FARIAS, P., GALN, G., FERNNDEZ, F.J. and LLANA-FNEZ, S. (2002). Tectonic framework of the Cabo Ortegal Complex: A slab of lower crust exhumed in the Variscan orogen (northwestern Iberian Peninsula). En: Martnez Cataln, J.R., Hatcher, R.D., Arenas, R. and Daz Garca, F. (Eds.), Variscan-Appalachian Dynamics: the Building of the Late Paleozoic Basement, Geol. Soc. Am. Spec. Paper, 364, 125-142.MARTNEZ CATALN, J.R. (2006). El orgeno varisco ibrico. Informe final para el "Proyecto Global Geosites", IGME.MARTNEZ CATALN, J.R., AYARZA ARRIBAS, P., PULGAR, J.A., PREZ-ESTAN, A., GALLART, J., MARCOS, A., BASTIDA, F., ALVAREZ-MARRN, J., GONZLEZ LODEIRO, F., ALLER, J., DAOBEITIA, J.J., BANDA, E., CORDOBA, D. and COMAS, M.C. (1997). Results from the ESCI-N3.3 marine deep seismic profile along the Cantabrian continental margin. Rev. Soc. Geol. Espaa, 8, 341-354.MARTNEZ CATALN, J.R., ARENAS, R., DAZ GARCA, F. and ABATI, J. (1997). Variscan acretionary complex of northwest Iberia: Terrane correlation and succession of tectonothermal events. Geology, 25, 1103-1106.MARTNEZ CATALN, J.R., ARENAS, R. and DEZ BALDA, M.A. (2003). Large extensional structures developed during emplacement of a crystalline thrust sheet: the Mondoedo nappe (NW Spain). J. Struct. Geol., 25, 1815-1839.MARTNEZ CATALN, J.R., ARENAS, R., DAZ GARCA, F., GMEZ-BARREIRO, J., GONZLEZ CUADRA, P., ABATI, J., CASTIEIRAS, P., FERNNDEZ-SUREZ, J., SNCHEZ MARTNEZ, S., ANDONAEGUI, P., GNZALEZ CLAVIJO, E., DEZ MONTES, A., RUBIO PASCUAL, F.J. and VALLE AGUADO, B. (2007). Space and time in the tectonic evolution of the northwestern Iberian Massif. Implications for the comprehension of the Variscan belt. En: Hatcher, R.D., Jr., Carlson, M.P., McBride, J.H. and Martnez Cataln, J.R. (Eds.), 4-D framework of continental crust. Geological Society of America Memoir, 200.MARTNEZ POYATOS, D. (2002). Estructura del borde meridional de la Zona Centroibrica and su relacin con el contacto entre las Zonas Centroibrica y de Ossa-Morena. Lab. Xeol. Laxe, Nova Terra, 18, 295 p.MATTE, PH. (1968). La structure de la virgation hercynienne de Galice (Espagne). Revue Gol. Alp., 44, 1-128.MATTE, PH. (1986). Tectonics and plate tectonics model for the variscan belt of Europe. Tectonophysics, 126, 329-374.MATTE, P. and RIBEIRO, A. (1975). Forme et orientation de l'ellipsoide de dformation dans la virgation hercynienne de Galice. Relations avec le plissement et hypothses sur la gense de l'arc ibero-armoricain. C. R. Acad. Sci. Paris, 280, 2825-2828.MENDIA ARANGUREN, M.S. (2000). Petrologa de la Unidad Eclogtica del Complejo de Cabo Ortegal (NW de Espaa). Lab. Xeol. Laxe, Nova Terra, 16, 424 p.MUNH, J., OLIVEIRA, J.T., RIBEIRO, A., OLIVEIRA, V., QUESADA, C. and M A R T N E Z C ATA L N , J . R . - A L L E R , J - A L O N S O , J . L . - B A S T I D A , F30KERRICH, R. (1986). Beja-Acebuches Ophiolite: characterization and geodynamic significance. Bol. Soc. Geol. Portugal, 2, 1-31.NEUMAN, R.B. and MAX, M.D. (1989). Penobscottian-Grampian-Finnmarkian orogenies as indicators of terrane linkages. En: Dallmeyer, R.D. (Ed.), Terranes in the Circum-Atlantic Paleozoic Orogens. Geol. Soc. Am. Spec. Paper, 230, 31-45.OCHSNER, A. (1993). U-Pb geochronology of the Upper Proterozoic-Lower Paleozoic geodynamic evolution in the Ossa-Morena Zone (SW Iberia): constraints on the timing of the Cadomian orogeny. Ph.D. Thesis, Univ. Zurich. Diss. ETH, 10, 392, 249 p.OLIVEIRA, J.T. (1990). South Portuguese Zone. Stratigraphy and synsedimentary tectonism. En: Dallmeyer, R.D. and Martnez Garca, E. (Eds.), Pre-Mesozoic Geology of Iberia, Springer-Verlag, Berln, 334-347.ONZIME, J., CHARVET, J., FAURE, M., CHAUVET, A. and PANIS, D. (2002). Structural evolution of the southernmost segment of the West European Variscides: the South Portuguese Zone (SW Iberia). J. Struct. Geol., 24, 451-468.ORDEZ, B., GEBAUER, D. and EGULUZ, L. (1997). Late Cadomian formation of two anatectic gneiss domes in the Ossa-Morena zone: Monesterio and Mina Afortunada. XIV Reunin de Geologa del Oeste Peninsular, Villa Real, Portugal, Abstracts, 161-164.PARGA PONDAL, I., MATTE, P. and CAPDEVILA, R. (1964). Introduction la gologie de l'"Ollo de Sapo", Formation porphyroide antesilurienne du Nord Ouest de l'Espagne. Not. Com. Inst. Geol. Min. Espaa, 76, 119-153.PREZ-ESTAN, A., BASTIDA, F., ALONSO, J.L., MARQUNEZ, J., ALLER, J., ALVAREZ-MARRN, J., MARCOS, A. and PULGAR, J.A. (1988). A thin-skinned tectonics model for an arcuate fold and thrust belt: The Cantabrian Zone (Variscan Ibero-Armorican Arc). Tectonics, 7, 517-537.PREZ-ESTAN, A., MARTNEZ CATALN, J.R. and BASTIDA, F. (1991). Crustal thickening and deformation sequence in the footwall to the suture of the Variscan Belt of northwest Spain. Tectonophysics, 191, 243-253.PREZ-ESTAN, A., PULGAR, J.A., BANDA, E., ALVAREZ-MARRN, J. and ESCI-N Research Group. (1994). Crustal structure of the external Variscides in NW Spain from deep seismic reflection profiling, Tectonophysics, 232, 91-118.PIN, C., ORTEGA CUESTA, L.A., and GIL IBARGUCHI, J.I. (1992). Mantle-derived, early Paleozoic A-type metagranitoids from the NW Iberian Massif: Nd isotope and trace-element constraints. Bull. Soc. gol. France, 163, 483-494.QUESADA, C. (1991). Geological constrains on the Paleozoic tectonic evolution of tectonostratigraphic terranes in the Iberian Massif. Tectonophysics, 185, 225-245.QUESADA, C. (1999). Tectonostratigraphic evolution of the Iberian Pyryte Belt. Post-Conference Field Trip. XV Reunin de Geologa del Oeste Peninsular. International Meeting on Cadomian Orogens. J. Conf. Abstracts 4, 1032-1034.QUESADA, C., FONSECA, P.E., MUNH, J., OLIVEIRA, J.T. and RIBEIRO, A. (1994). The Beja-Acebuches ophiolite (Southern Iberia Variscan fold belt): Geological characterization and geodynamic significance. Bol. Geol. and Min., 105, 3-49.RIBEIRO, A., DIAS, R. and BRANDAO SILVA, J. (1995). Genesis of the Ibero-Armorican arc. Geodinamica Acta, 8, 173-184.RIBEIRO, A., QUESADA, C. and DALLMEYER, R.D. (1990). Geodynamic evolution of the Iberian Massif. En: Dallmeyer, R.D. and Martnez Garca, E. (Eds.), Pre-Mesozoic Geology of Iberia, Springer-Verlag, Berln, 399-409.RODRGUEZ ALLER, J. (2005). Recristalizacin y deformacin de litologas supracorticales sometidas a metamorfismo de alta presin (Complejo de Malpica-Tuy, NO del Macizo Ibrico). Lab. Xeol. Laxe, Nova Terra, 29, 572 p.RODRGUEZ FERNNDEZ, L.R., FERNNDEZ, L.P. and HEREDIA, N. (2002). Carboniferous of the Pisuerga-Carrin Unit. En: Garca-Lpez, S. and Bastida, F. (Eds.), Paleozoic conodonts from Northern Spain, Cuadernos del Museo Geominero, 1, Inst. Geol. Min. Espaa, 93-104.SNCHEZ MARTNEZ, S., JEFFRIES, T., ARENAS, R., FERNNDEZ-SUREZ, J. and GARCA-SNCHEZ, R. (2006). A pre-Rodinian ophiolite involved in the Variscan suture of Galicia (Cabo Ortegal Complex, NW Spain). J. Geol. Soc., 163, 737-740.SNCHEZ MARTNEZ, S., ARENAS, R., DAZ GARCA, F., MARTNEZ CATALN, J.R., GMEZ-BARREIRO, J. and PEARCE, J.A. (2007). Caren Ophiolite, NW Spain: Suprasubduction zone setting for the youngest Rheic Ocean floor. Geology, 35, 53-56.SANDERSON, D.J. and MARCHINI, W.R.D. (1984). Transpression. J. Struc. Geol., 6, 449-458.SANTOS, J.F., SCHRER, U., GIL IBARGUCHI, J.I. and GIRARDEAU, J. (2002). Genesis of pyroxenite-rich peridotite at Cabo Ortegal (NW Spain): geochemical and Pb-Sr-Nd isotope data. J. Petrology, 43, 17-43SCOTESE, C.R. and McKERROW, W.S. (1990). Revised World maps and introduction. En: McKerrow, W.S. and Scotese, C.R. (Eds.), Paleozoic Paleogeography and Biogeography. Geol. Soc. Mem., 12, 1-22.SILVA, J.B., OLIVEIRA, J.T. and RIBEIRO, A. (1990). South Portuguese Zone. Structural outline. En: Dallmeyer, R.D. and Martnez Garca, E. (Eds.), Pre-Mesozoic Geology of Iberia. Springer-Verlag, Berln, 348-362.SIMANCAS, F., GONZLEZ LODEIRO, F., EXPSITO RAMOS, I., AZOR, A. and MARTNEZ POYATOS, D. (2002). Opposite subduction polarities connected by transform faults in the Iberian Massif and western European Variscides. En: Martnez Cataln, J.R., Hatcher, R.D., Arenas, R. and Daz Garca, F. (Eds.), Variscan-Appalachian Dynamics: the Building of the Late Paleozoic Basement, Geol. Soc. Am. Spec. Paper, 364, 249-258.VALVERDE-VAQUERO, P., MARCOS, A., FARIAS, P. and GALLASTEGUI, G. (2005). U-Pb dating of Ordovician felsic volcanism in the Schistose Domain of the Galicia-Trs-os-Montes Zone near Cabo Ortegal (NW Spain). Geolgica Acta, 3, 27-37.VOGEL, D.E. (1967). Petrology of an eclogite -and pyrigarnite- bearing polymetamorphic rock Complex at Cabo Ortegal, NW Spain. Leidse Geol. Med., 40, 121-213.WINCHESTER, J.A., PHARAOH, T.C. and VERNIERS, J. (2002). Palaeozoic amalgamation of Central Europe: an introduction and synthesis of new results from recent geological and geophysical investigations. En: Winchester, J.A., Pharaoh, T.C. and Verniers, J. (Eds.), Palaeozoic Amalgamation of Central Europe. Geol. Soc. Spec. Publ., 201, 1-18.M a r t n e z C a t a l n , J . R . A l l e r, J - A l o n s o , J . L . a n d B a s t i d a , F.Go back to index file


View more >