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Late Palaeozoic lithostratigraphy of the Andean Precordillera revisited (San Juan Province, Argentina).

1. Introduction

This work is focused on some neopalaeozoic lithostratigraphic units of the central sector of the Argentinean Precordillera. Although the Del Raton, El Planchon and Del Salto stratigraphic units have been studied for many years (Heim, 1952; Guerstein et al., 1965; Quartino et al., 1971; Mancenido, 1973; Venturini, 1980; Sessarego, 1983; De Rosa, 1983; Selles Martinez, 1985; Archangelsky, 1987, 1996; Sessarego and Cesari, 1989; Etchichury et al., 1990; Barredo and Stipanicic, 2002), there is a dearth of reliable data about the accumulation of their materials. Nevertheless, significant advances have been made in the structure of the area (Astini et al., 1996; Alonso et al., 2005a, b; 2008) and in the definition of the ages of these formations and their stratigraphic equivalents (Limarino and Cesari, 1992; Barredo et al., 2012; Colombo et al., 2012; Limarino et al., 2012). However, certain misconceptions have been attributed to implausible data obtained from fossil remains identified as Devonian (Kerllenevich, 1967; 1969), data which have consequently never been cited in recent studies of the area. These inaccuracies have given rise to significant problems concerning the stratigraphic location of the El Planchon Formation and related units (Amenabar and di Pasquo, 2008).

The present work seeks to provide some answers to the problems arising from the stratigraphy of the upper Palaeozoic rocks that crop out in the proximity of km 114 of the Ruta Nacional 20 (National 20 highway) in the Argentine Precordillera (San Juan Province, Figs. 1, 2). The literature of the area has been revised and some misconceptions concerning the main lithostratigraphic units, the depositional interpretations and also some chronostratigraphic attributions have been cleared up. We present a schematic geological cartography of the study area. Some detailed stratigraphic sections of the main lithostratigraphic units have been studied together with the data provided by primary sedimentary structures, enabling us to interpret their sedimentology. A number of the formerly established lithostratigraphic units have also been revisited, resulting in the reorganisation of some lithostratigraphic units. At the same time, the unconformities which play a significant role in the regional correlation have also been differentiated (Fig. 3).

2. Lithostratigraphic units

The main stratigraphic units are usually limited by unconformities in the study area. There are a few exceptions such as the case of the basal limit of the El Planchon Formation, which overlies the Del Raton Formation with a normal stratigraphic contact as a result of sedimentation. The lithology and stratigraphic relationships of each of the Late Paleozoic deposited units outcropping in the region as well as their depositional palaeoenvironments are described below.

2.1. Del Raton Formation (Guerstein et al., 1965)

Carboniferous conglomerates resting on Devonian rocks (Fig. 4) by means of an angular unconformity (D1) crop out in two areas. The best known outcrops containing plant remains correspond to the exposures along the left bank of the Quebrada Del Salto creek near its confluence with the San Juan River. Another group of Carboniferous conglomerates is present in the northern margin of the San Juan River where the sequence is partially covered by Quaternary sediments. Two members are identified given the significant lithological differences exhibited by the Del Raton Formation from base to top. The unit rests on the Devonian sedimentary succession with an angular unconformity (D1). Two units may be distinguished:

Lower Member: This is a conglomeratic unit with an approximately lenticular geometry and an erosive base that is evidenced by a pavement of disorganised and polymodal (30-50 cm) granitic clasts. Two sections (A and B) with a total thickness of 85-100 m can be differentiated. The lower section section (A) consists of metric-thick stacked beds of massive matrix-supported conglomerates which in some cases grade to massive pebbly mudstones (Fig. 5A) locally deformed (Fig. 5b). The clasts, which are subrounded to rounded and vary in size from 3 to 5 cm, are predominantly composed of granite (70%) and metamorphic rocks (20%) whereas the rest are greywackes and carbonates (10%). Several discontinuous horizons with very coarse clasts (30-40 cm) are interfingered with shales bearing plant remains (coal). Some conglomeratic and shale levels with out-sized clasts are interpreted as dropstones. There are some sandstone levels displaying undulated cross-bedding. The upper section (B) is composed of cross-bedded conglomerates (up to 1.5 m thick) that sporadically show intercalations of coarse- and medium-grained sandstones. Small grooves were identified at the base of some conglomerate beds, indicating NNW-SSE palaeocurrents.

Several conglomeratic horizons display small scale cross-laminations. Some levels of conglomeratic sandstones present thin coarsening upward sequences locally (Fig. 5C). Section B, which shows a thickening upwards trend, culminates in metric cross-stratified conglomeratic levels. A smooth erosive surface (D2) is present at the summit.

Interpretation: The texture of the deposits suggests massive flows with some reworked clasts (second generation). The synsedimentary deformation indicates that the accumulation processes developed in areas with steep slopes with basement instability. Section A represents the subaqueous transport of gravelly massive flows with preservation of organic matter (coal). The undulate cross-bedding strongly suggests that some conglomeratic levels were reworked by wave action. In section B, the coarsening upwards sandy bodies (traction carpets) were probably generated by the dilution of very dense turbulent flows (hyperpicnic). The upper conglomerates would correspond to the progradation of gravelly bars in a shallow and small deltaic setting (Fig. 5D). In this context, the thin lamination of the shales is probably attributed to the flocculation of mud-rich flows within a water body with varying salinity. Thus, the accumulation in a fjord environment (Boulton et al., 2001; Evans, 2003; Iverson and Iverson, 2001; Powell, 2003) cannot be ruled out because of the presence of dropstones, synsedimentary large-scale deformation and hyperpicnic flow deposits, According to Amenabar and Di Pasquo (2008), these materials accumulated during the Lower Carboniferous.

Upper Member: The Upper Member rests on a smooth erosive surface (D2), and mainly corresponds to orthoconglomerates (Fig. 6) and coarse-grained sandstones (up to 700 m thick). The stratigraphic significance of the surface that separates the Lower and Upper Members of the Del Raton Formation should be evaluated in the future from a regional perspective in order to ascertain whether this surface is associated with significant changes in the palaeogeography of the basin. Conglomerate clasts are dominated by sandstones (65%, chiefly greywackes), granites and rhyolites (30%) and scarce quartz and metamorphic rocks (5%). The relatively high proportion of rhyolitic and granitic clasts gives a reddish colour to the coarse-grained beds. The sandstone intercalations have a grain-size ranging from coarse to very coarse. The sandy matrix is poorly sorted whereas the clasts are very rounded and clearly aligned. A number of dispersed clasts (3-5 cm) are present locally. Conglomeratic unitary sequences, which have thicknesses of about of 3-4 m, display plane beds enhanced by clast lineations (Fig. 5E). Some levels show a large number of clasts of pink granite (40%) locally. The sandy materials are interfingered with poorly sorted and disorganised conglomeratic levels which display some imbricated clasts locally, indicating E-W oriented currents. Poorly sorted conglomeratic levels evidenced by planar clast alignments consist of coarse red granites and rhyolites (40-50 cm) locally. Some conglomeratic levels show clast lineations which indicate SE-NW oriented currents. The uppermost thick sandstone levels display cross-stratification generated by hydraulic dunes, indicating palaeocurrents from the W and WNW. The top of the conglomeratic section, with a thickness of about 125-130 m is characterised by levels showing different types of middle and small scale cross bedding (Fig. 5F). Several bodies are lenticular whereas others with a stratiform morphology are interfingered with shales and sandstones with undulated lamination (wavy).

Interpretation: The Upper member of the Del Raton Formation accumulated in an alluvial depositional system that was predominantly characterised by gravels carried by upper flow regime currents. Flows transported sandy materials by means of bars and hydraulic dunes in the upper part of some conglomerate sections. The alluvial system finally evolved into a fan delta in a coastal setting as evidenced by different mouth bar sequences. The clastic accumulation is the sedimentary response to the erosion of the Protoprecordillera generated during the Chanic orogeny (Heredia et al., 2012).

The age of the unit is provided by the chronostratigraphic vertical distribution of some organic remnants found in the Lower Member (Sessarego and Cesari, 1989; Amenabar and Di Pasquo, 2008) whereas the Upper Member displays a conspicuous absence of fossils. The study of a large clast of granite (Fig. 14, site 1), which belongs to the basal pavement of the Lower Member, yields an absolute chronology (Gallastegui et al., this volume) of 348 [+ or -] 2 Ma (U-Pb zircon data). Thus, the granite was generated during the Lower Missippian near the Tournaisian-Visean limit, whereas the sedimentary accumulation of this granitic clast in the Del Raton Formation was more recent, Visean or younger. Moreover, pollen and spores found in section A of the Lower Member provide ample evidence that the conglomerates were deposited during the Lower Visean (Azcuy et al., 1981; Amenabar and di Pasquo, 2008).

2.2._El Planchon Formation (Quartino et al., 1971)

This unit is about 1300-1400 m thick and is made up of alternating shales and sandstones that crop out along the Quebrada Del Salto, with synsedimentary deformations in the whole section, increasing towards the top (Fig. 7E). Sandy materials with a fine to medium grain-size are well sorted, displaying several cross-laminations and basal marks that indicate NW-SE palaeocurrents. Polygenic and polymodal conglomerates change laterally to more muddy materials towards the S and E (Figs. 7C, 7D). Shale and sandstone layers are distorted by some dropstones locally (Fig. 8). The upper part of the unit is strongly reddening below a marked angular unconformity (D3).

Interpretation: The shales and sandstones are arranged in decimetric Bouma-type sequences, Tc-e and Tb-e. They suggest that these materials were deposited by turbidity flows in a deep and relatively narrow N-S oriented marine basin. The interfingered coarse-grained levels (Fig. 9) display facies of poorly sorted, matrix supported and disorganised conglomerates, suggesting that these materials were transported and deposited by different mass flow (debris flow) episodes. These rocks are interfingered with the shales that graded laterally into conglomerates that were deposited coevally in a marine environment. The presence of some striated clasts and deformations produced by dropstones indicates that the deposition occurred in a glacial setting. The conglomerates filled the N-S aligned palaeovalley with contributions mainly from the N and the E. A number of turbiditic episodes in a deep water context led to several synsedimentary slumps due to the high detrital input on unstable slopes. The strongly reddening of the top of the unit probably corresponds to an episode of intense chemical alteration because of prolonged subaerial exposure.

2.3. Del Salto Formation (Quartino et al., 1971)

Yellowish cross-stratified sandstones (Sessarego, 1983) overlying an angular unconformity (D3) accumulated during the early Permian (Mancenido, 1973; Taboada, 2006a, b). A thick sandstone level characterised by several middle-scale cross-stratifications displays some intercalations (Fig. 10) of shales and sandstones with different types of cross-stratification and cross-lamination (hydraulic dunes and ripples respectively). The fossil (brachiopoda) associations (Mancenido, 1973; Mancenido and Sabattini, 1974; Mancenido et al., 1976a, b) distributed in the shales are Aselian (Taboada, personal communication) i.e. Cisuralian (Lower Permian). Some coarsening and thickening upwards sequences are present towards the upper part of the unit. The base of the upper third of this section consists of cross-stratified sandstones (dipping towards the S and SE) which evolved into planar beds. The tops of some sequences are characterised by large-scale trough cross bedding. The unit is about 550-600 m thick. The whole section is arranged into more than seven megasequences that are clearly differentiated in the outcrop. These display green and grey mudrocks at the base. Towards the top, they grade into thick sandstone levels with different types of medium-scale cross bedding and large cross-stratification. In the upper part only large cross-stratified sets were identified locally. A very small number of sequences with coarsening-upwards arrangements are present at the top of the unit (Fig. 11).

Interpretation: Sandy levels, generated by coastal bars with their tops reworked by waves, controlled restricted areas where large populations of brachiopods developed. At large scale, the sandy materials are arranged in a number of coarsening-upward macrosequences. These sequences start with levels of shaly materials, and are interpreted as having been deposited in an offshore environment that onlapped sandy shoreface levels and culminated in aeolian dunes locally. Some large cross-bedded planar layers probably corresponded to a foreshore, indicating that the open sea was to the S and SE. Thus, after an initial sea-level rise, resulting in an offshore environment, a shallowing event gave rise to shoreface sandy accumulations. This system tract, which underwent significant variations in the sea-level, was repeated at least seven times in this area.

The Del Salto Formation ends in an erosive unconformity which supports the overlying unit.

2.4. Quebrada del Alumbre Formation (new unit)

This is a new definition of the older non-formal lithostratigraphic unit known as Conglomerados "chocolate" (Heim 1952) or Conglomerados Morados (Mancenido, 1973) by the authors working in the area. The new denomination is derived from neighbouring Quebrada del Alumbre located in the area where the unit crops out (Fig. 12).

The Formation is made up of purple polygenic and polymodal conglomerates with a poorly-sorted sandy matrix supported fabric displaying a variable crude cross-stratification. The clasts, which are usually subrounded, consist of volcanic rocks (80%), reddish sandstone, greywackes and quartz. Some of them are of the second generation. The Formation overlies the Del Salto Formation with an erosive unconformity (D4). It has a regional lenticular geometry with a thickness of around 60-75 m to the north, and attains a maximum thickness of about 100-125 m to the south (Figs. 12A, 12B).

Interpretation: The matrix-supported fabric suggests that the conglomerates were initially deposited by debris-flow episodes in a sub-aerial context as evidenced by the red colouring. In several cases, some cross-stratifications indicate that the sediment was transported by a variety of bars in a braided context. The facies arrangement and the scarce palaeocurrents to the W and SW suggest that these materials resulted from the progradation of an alluvial fan that prograded from the N and NE to the S and SW (Fig. 13). The study of a thin andesitic level (Fig. 14, site 2) yields an absolute chronology between 289 [+ or -] 4 Ma and 293 [+ or -] 5 Ma (U-Pb zircon data). Thus, the unit accumulated near the limit between the Lower Artinskian and the Upper Sakmarian, Cisuralian, Permian.

2.5 Escombrera Formation (new unit)

The basal part is mainly composed of yellow-grey sandstones in metric and decimetric units which display some volcanic clasts reworked from the underlying Quebrada del Alumbre unit. The new denomination is derived from neighbouring "Escombrera" (mine-waste deposit) generated by the activity of the former aluminium sulphide mine owned by the IMSA Company in the area where the unit crops out. The sandstones are arranged at large scale in more than four megasequences with a total thickness of about 320-350 m. These sequences usually start with a green-grey shaly section. Towards the upper part of each sequence is an intercalation of some thin sandstone levels and shales which characterise a heterolitic section. Some thick sandstone levels with medium-scale cross bedding are present at the top. In the upper part of the unit is a white-coloured level which displays a large number of feldspar grains in the sandstones. In some cases, large sets of cross-bedding are present at the top of the minor units. Towards the upper part of the unit are several levels of sandstones that are intercalated with shales and are distinguished by medium-scale cross bedding and small-scale cross-laminations locally (Fig. 14).

Interpretation: The upper member was probably deposited in transitional, coastal and continental environments. The shales corresponded to the deepest accumulations and accumulated in an offshore-dominated environment. This environment was controlled by a significant rise in sea-level. By contrast, the sandstones which display many primary sedimentary structures (megaripples, bars and sub aquatic dunes) accumulated in a non-confined hydraulic setting in a relatively shallow coastal environment (Fig. 15). Thus, the accumulation probably developed in a shoreface setting that gave rise to some aeolian dunes at the top.

All the sandy materials deposited during the Permian were characterised by extreme dryness. Thus, the assumption that the rise and fall in sea-level was directly controlled by climatic variations can be ruled out. By contrast, the regionally significant base-level oscillations controlled by extensional tectonic activity could be possible. This activity played a major role in the Triassic (Barredo and Stipanicic, 2002) with minor activity in the area during the middle Permian.

2.6 Quebrada de la Arena Formation (new unit)

This reddish Formation is made up of shales, sandstones and conglomerates. Two members may be distinguished as a result of the variable amount of these materials. The new denomination is derived from neighbouring Quebrada de la Arena located in the area where the unit crops out (Fig. 16).

Lower Member: This unit, which is about 180-200 m thick and comprises intercalated beds of sandstones and mudstones, overlies the Escombrera Formation with a smooth unconformity (D6). The member is made up of more than four sandstone-dominated megasequences separated by intercalated levels of mudstones. The thick sandstone levels usually show different types of cross-bedding such as megarriples, hydraulic dunes, bars and other minor structures. The central part of each megasequence is characterised by metric trough cross-bedding which laterally show significant changes in size. Associated with the main thick sandstone levels are climbing ripple-type cross laminations locally. Many small intercalacions of mudrocks are displayed towards the summit of the unit. A thin cineritc level (Fig. 14, site 3), intercalated in the basal levels of the unit gives information of an absolute chronology between 238 [+ or -] 1.5 Ma and 240 [+ or -] 3.5 Ma. Thus, the unit accumulated during the middle Triassic near the limit between the Anisian and Ladinian.

Interpretation'. The vertical and lateral arrangement of the small units together with the distribution of sedimentary primary structures and the variety of through cross-bedding suggests that the unit was deposited by sand-dominated braided rivers. The mudstone-dominated major intercalations seem to have been produced by the occasional abandonment of the sedimentary activity of the environment. The whole unit graded into a shallowing upwards depositional environment that gave rise to some ponded areas or small lagoons. Several rooting systems and Lycopsidae stems have been found in one of the fine-grained sections interpreted as coastal lagoons. They are presented as mould-cast forms and the dispersed foliage was not found in the same beds. The stems of the Lycopsidae seem to have had small diameters (c.a. 30 mm), retaining (without much detail) the characteristic external rhombic leaf cushions. The associated rhizomes have larger diameters, reaching 60 mm. Lycopsidae were typical of wetland vegetation during the late Paleozoic-Triassic. The evidence therefore suggests that the fossil beds resulted from short flooding events of the muddy-dominated areas where the Lycopsidae flourished before the inflow of the clastics in which the stems were buried. A rapid change from wetness to dry conditions is assumed.

Middle Member: This unit, which is about 220-250 m thick, is made up of sandstones intercalated with mudstones. Muddy materials with few intercalations of sandstones are present in the lower part. Some sandstone levels grade into conglomerates towards the top in the middle part. This unit shows different types of cross-stratification magnified by clast alignments locally. The sections are metric and incorporate abundant mud clasts locally. The basal surface of some sandstone levels displays mud crack casts (Fig. 12C). The sandstones show a planar stratification that is locally crude. Medium-scale trough cross-stratifications are present towards the middle part. The upper section displays some large diagonal structures and lineations. The shales are interfingered with thin sandstone levels with different types of cross-lamination. They are mainly composed of clays and siliceous silts and display variable amounts of water-reworked ash deposits.

Interpretation: Some waterways initially carried large amounts of muddy materials deposited in a playa-lake setting (continental mudflats). Thereafter, the sedimentary context underwent some changes, enabling the confined courses to carry large amounts of sandy-dominated bed-load materials towards the playa-lake. Following the loss of confinement of these channels, the area was affected by several events of water discharge. A number of high-energy episodes are evidenced by sedimentary structures such as parting lineations and large-scale and low-angle cross bedding. Planar cross-stratifications suggest that some sandstone levels were deposited by sheet flood episodes locally. Subsequently, the main channels graded into meandering courses as evidenced by some diagonally-dominated large-scale cross bedding probably because of lateral accretion in point bars. The interfingered heterolitic levels could be due to several crevasse-splay episodes (Fig. 12D).

Upper Member: This unit, which is composed of conglomerates and sandstones, varies from 300 to 350 m in thickness. The conglomerates display several medium-scale and high-angle cross-stratifications, some of which show concave-up scars in the lower part. The main cross-bedding is evidenced by clast lineations. The clasts are made up of graywackes, sandstones and well rounded pink quartz. Some of them are from former reworked conglomerates. Poorly-sorted sandy shales intercalated with conglomerates are present. The upper part of the unit is characterised by coarse-grained levels which display massive-dominated facies evidenced by the predominance of matrix-supported conglomerates (Fig. 15).

Interpretation: The medium-scale cross bedding suggests that the coarse-grained materials in the lower part were transported by hydraulic flows in a braided environment where the gravel load gradually increased upwards. Subsequently, when the mass flow-dominated levels became predominant, the accumulation was produced by a number of debris flow episodes. The main coarsening and thickening upwards sequence indicates that the gradual progradation of an alluvial system was caused by erosional processes related to the new extensional ranges (Figs. 17, 18) to the east of the study area.

A marked angular unconformity (D7) separates this stratigraphic unit from the overlying Rincon Blanco Group (Lopez-Gamundi 1994). However, in the vicinity of the study area the Upper Permian (Choiyoi Group and equivalents) is clearly extensional and unconformably covers the Gondwanan structures (Heredia et al., 2012). The last angular unconformity (D8) probably developed within the Rincon Blanco Group as a result of an extensional tectonic reactivation coeval with the Triassic sedimentary accumulation.

3. Sedimentary evolution

During the early Carboniferous (late Tournasian-Visean), a small fjord developed on a sharp angular unconformity (D1) on the Devonian basement. After its sedimentary infilling, another smooth unconformity (D2) developed before the generation of an alluvial fan system (Del Raton Formation) which evolved into a coastal fan delta probably at the beginning of the Chanic orogeny. A marked rise in relative sea-level led to the development of the El Planchon Formation in a deep-sea fan setting. This Formation represents the end of the synorogenic Chanic sedimentation. The rapid sea level rise was probably due to an event of regional deglaciation. The Lower Carboniferous rocks were then deformed and exposed to subaerial alteration as evidenced by the rubefaction (Fig. 19) of the mudrocks located below the main angular unconformity (D3). The subaerial exposure was probably much longer since no new deposits accumulated until the Permian. Thus, during most of Carboniferous, this area was part of a basement high (horst) known as the Protoprecordillera, a remnant of the Chanic cordillera, which was located between the Rio Blanco and Paganzo extensional basins (Heredia et al., 2012).

During the basal Permian, an expansive coastal system (Del Salto Formation) accumulated on a sharp angular unconformity (D3), the open-sea being located to the south. This Permian Formation developed as a sedimentary response (Fig. 3) to the erosion of the Gondwanan orogenic ranges and was deposited in the same retroarc foreland basin located in the Frontal Cordillera at this latitude (Busquets et al., 2005). The Protoprecordillera disappeared at the start of the Permian owing to the flexural subsidence associated with the origin of the Gondwanan foreland basin (Heredia et al., 2012).

The Andean cycle, which was characterised by an extensional tectonic setting, started in the middle Permian. In this context, a transverse alluvial fan system (Quebrada del Alumbre Formation) was deposited over another unconformity (D4). These coarse-grained rocks were transported from new ranges located to the west (Fig. 20). Subsequently, a new expansive coastal system (Escombrera Formation) was deposited over a smooth unconformity (D5). This unit seems to be the last Palaeozoic sedimentary accumulation.

A sand-dominated (Fig. 21) braided watershed (Quebrada de la Arena Formation) accumulated on a smooth unconformity (D6) and gradually evolved into a mud-dominated playa lake. Subsequently, a sheet-flood dominated sand accumulation (Lower Member), which was replaced (Fig. 22) by a meandering system (Middle Member), developed. Thereafter, this system progressively changed to another braided sedimentary environment overlain by conglomeratic and progradational alluvial fans from the east (Upper member). This unit was the first Triassic accumulation in the study area.

The Rincon Blanco Group ("sensu lato") accumulated over an angular unconformity (D7). It displays another angular unconformity locally (D8) that was generated by the reactivation of the Andean extensional activity during the Triassic (Stipanicic, 1972, 2002; Ramos et al., 1986; Spalletti, 1999; Ramos, 2004; Mancuso et al., 2010).


The authors are indebted to V. Ramos, T. Lawton and S.N. Cesari whose comments have considerably improved the earlier versions of the manuscript. This study was funded by the Spanish Proyecto de Investigacion CGL2009-13706-C03-03 BTE of MINCINN and by the Grup de Qualitat, 2009-SGR1198. Secretaria de Universitats i Recerca. Departament d'Economia i Coneixement. Generalitat de Catalunya.


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F. Colombo (1) *, C.O. Limarino (2), L.A. Spalletti (3), P. Busquets (1), R. Cardo (4), I. Mendez-Bedia (5), N. Heredia (6)

(1) Dept. Estratigrafia, Paleontologia y Geociencias Marinas. Facultad de Geologia, Universidad de Barcelona, C/ Marti-i-Franques s/n. E-08028 Barcelona, Spain.

(2) Dept. Geologia. Facultad de Ciencias Exactas y Naturales. Universidad de Buenos Aires. Ciudad Universitaria. Pabellon II, 1428 Buenos Aires, Argentina.

(3) Centro de Investigaciones Geologicas CIG-CONICET. Universidad Nacional de La Plata. Calle 1, no. 644, 1900 La Plata, Argentina.

(4) Universidad Nacional de San Juan. Servicio Geologico Minero Argentino (SEGEMAR), Sargento Cabral, 685 Oeste. 5400 San Juan, Argentina.

(5) Dept. de Geologia. Facultad de Geologia. Universidad de Oviedo. C/Jesus Arias de Velasco s/n. E-33005 Oviedo, Spain.

(6) Instituto Geologico y Minero de Espana (IGME), Matematico Pedrayes, 25, E-33005 Oviedo, Spain.

e-mail addresses: (F.C., Corresponding author); (P.B.); (C.O.L.); (L.A.S); (R.C.); (I.M.-B.); (N.H.)

Received: 17 March 2014 / Accepted: 25 May 2014 / Available online: 25 June 2014
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Title Annotation:articulo en ingles
Author:Colombo, F.; Limarino, C.O.; Spalletti, L.A.; Busquets, P.; Cardo, R.; Mendez-Bedia, I.; Heredia, N.
Publication:Journal of Iberian Geology
Date:Jul 1, 2014
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