Evolution of the central Catalan margin of the Valencia trough (western Mediterranean

Tectonophysics 315 (1999) 209–233www.elsevier.com/locate/tecto

Oligocene to Middle Miocene evolution of the centralCatalan margin (northwestern Mediterranean)

Eduard Roca a,*, Maura Sans a, Luis Cabrera b, Mariano Marzo ba Departament de Geodinamica i Geofısica, Facultat de Geologia, Universitat de Barcelona, 08028 Barcelona, Spain

b Departament d’Estratigrafia i Paleontologia, Facultat de Geologia, Universitat de Barcelona, 08028 Barcelona, Spain

Abstract

The Catalan margin belongs to the northern sector of the margin that separates the extremely thinned continentalcrust of the Valencia trough from the undeformed or thickened crust of the Iberian microplate.

The integration of the available onshore and offshore data (mapping, stratigraphic sections, seismic profiles andwell data) enables the present structure of the central Catalan margin to be identified as a major northwest-directed,thick-skinned thrust sheet compartmentalised in a system of NE–SW oriented horsts and grabens. The geometry anddepositional features of the Tertiary successions denote that this structure resulted from two successive evolutionaryepisodes. The first episode was compressional and gave rise to the emplacement of the Catalan major thrust sheet;the second was extensional, linked to the opening of the Valencia trough.

The compressional ( pre-extensional ) episode is recorded by Lower to lower Upper Oligocene deposits sedimentedin a piggyback basin that developed in the present-day offshore. The pre-rift signature of these sedimentary successionsis clear (they show constant thickness, are cut by all the normal faults, etc.) and their facies distribution indicates amostly southwestward spreading of the sediments.

The extensional episode includes the syn-rift and post-rift stages. The syn-rift stage resulted in the present horst-and-graben structure of the Catalan margin and it is recorded by the uppermost Oligocene–lower Burdigalian (LowerMiocene) sediments restricted to the graben troughs. The post-rift stage started in the late Langhian and has continueduntil the present. It is characterised by the attenuation of the tectonic activity, the sediment spreading over the horsts(most of them were completely overlapped during this stage) and no sediment thickness changes near the faults. Theupper Burdigalian and lower Langhian sequences record that the transition between the syn-rift and post-rift stageswas not sharp. These units show intermediate features since they concealed some minor faults and overlapped horsts,but were still affected by most of the major normal faults.

The onshore and offshore tectono-sedimentary and palaeogeographic evolution show that: (1) the northwesternMediterranean basin existed during the early to middle Oligocene as an extensional basin in the Gulf of Lions and asa contractional piggyback basin in the northeastern Valencia trough; (2) the extension started in the early Oligocenein southern France and migrated progressively southwestward, affecting the northeast Valencia trough during thelatest Oligocene–Aquitanian. © 1999 Elsevier Science B.V. All rights reserved.

Keywords: Catalan coastal ranges; inversion tectonics; Neogene; Oligocene; palaeogeography; west Mediterranean

* Corresponding author. Tel.: +34-93-4035911; fax: +34-93-4021340.E-mail address: [email protected] (E. Roca)

0040-1951/99/$ - see front matter © 1999 Elsevier Science B.V. All rights reserved.PII: S0040-1951 ( 99 ) 00289-9

210 E. Roca et al. / Tectonophysics 315 (1999) 209–233

1. Introduction In order to define the age and tectonic featuresof the earliest extensional stages in the Catalanmargin more accurately, the set of the availableUnderstanding and characterising the transition

from contractional to extensional situations is offshore data (mainly seismic profiles and welldata) was analysed. Subsequently, these data werealways a difficult task because: (1) contraction and

extension may be active simultaneously in the compared with the already known onshore data(i.e. Bartrina et al., 1992; Cabrera and Calvet,mountain chains, and hence there is not necessarily

a clear ‘time break’ between the two; and (2) the 1996). The tie of the well data by correlation ofseismic profiles and the analysis of the geometryearliest extensional structures often develop over

areas uplifted during the previous contractional of sedimentary packages and their relationshipwith the tectonic structures allowed us to developtectonic evolution. Effectively, in areas uplifted by

compression, erosive processes are dominant and a model for the evolution of the entire region inwhich the offshore and onshore basins arethe potential energy generated by crustal thicken-

ing may cause early extension in the highest parts integrated.The results of this study, together with dataof the contractional chains (Dewey, 1988). As a

consequence, the earliest normal faults usually from the Provencal margin and the rest of theValencia trough, provide a better understandingform in abrupt topographic areas (i.e. steep slopes,

cliffs, peaks) where the erosion is sufficiently of the geodynamic change that occurred in thewestern Mediterranean between the Oligocene andintense to prevent or hamper the development of

syn-rift basins in which sediments could be Early Miocene. A set of spatial and temporalconditions, which should be taken into account intrapped. This results in a poor preservation of the

sediments deposited synchronously to the earliest any future evolution model proposed for the west-ern Mediterranean, is presented.extensional stages. Moreover, if the early exten-

sional successions are not uplifted by later tectonicmovements, they will not crop out and will remaincovered by younger sedimentary successions. 2. Regional setting

In the western Mediterranean, for example, thetiming, location and tectonic features of the earliest The northwestern Mediterranean (Fig. 1)

includes a system of Oligocene–Early Miocenerifting, related to the formation of the northwest-ern Mediterranean basins, are still rather extensional basins ( Valencia trough, Provencal and

Ligurian basins) that records the early evolution-unknown. Most authors (i.e. Roca and Desegaulx,1992; Gorini et al., 1994, Mauffret et al., 1995; ary stages of the western Mediterranean. The

origin of this system is related to the southwest-Seranne et al., 1995; Roca, 1996) agree that theextension began in the Provencal basin and in the wards Oligocene–Early Miocene propagation of

the Western European rift system and theValencia trough during the Oligocene by the tec-tonic inversion of previous contractional faults. Burdigalian oceanic accretion associated with the

southeastward drift of the Corsica–Sardinia blockHowever, a detailed analysis of the studies carriedout in the northwestern margin of these basins (Auzende et al., 1973; Burrus, 1984; Rehault et al.,

1984). The northwestern Mediterranean is charac-shows no general agreement as to the age of theextension. Even in the Catalan margin of the terised by a very thin lithosphere, which includes

a thin continental crust and, in the case of theValencia trough, where some oil wells cut a con-tinuous, probably Late Eocene–Early Oligocene Provencal and Ligurian basins, also an oceanic

crust. The southeastern boundary of this basinto Present sedimentary succession, the onset ofextension has been a subject of debate, with pro- system is formed by the Balearic Promontory and

the Corsica–Sardinia block, which both have dis-posed ages ranging from Late Eocene to EarlyMiocene (Garcıa-Sineriz et al., 1979; Clavell and tinctive structural features. The Corsica–Sardinia

block bounds the northern part of this systemBerastegui, 1991; Bartrina et al., 1992; Maillardet al., 1992; Martınez del Olmo, 1996). (Provencal and Ligurian basins) by steep north-

211E. Roca et al. / Tectonophysics 315 (1999) 209–233

Fig. 1. Simplified geological map of the western Mediterranean. The hatched box indicates the study area. CCR: Catalan CoastalRanges; C.F.: Catalan fault.

west-dipping normal faults, which were active 2.1. Catalan marginduring basin formation (Vially and Tremolieres,

The Catalan margin belongs to the northern1996). In contrast, the boundary formed by thesector of the margin that separates the extremelyBalearic Promontory is integrated by a thrust-and-thin continental crust of the Valencia trough (8–fold belt which developed mainly after the exten-10 km) from the undeformed or thickened crust ofsional formation of the Valencia trough (Sabatthe Iberian microplate (32–40 km). In this marginet al., 1997). Unlike the southeast margin of thethe crust thins towards the SE (32 to 22 km insystem, the structure of its northwestern boundary20 km; Gallart et al., 1990; Vidal et al., 1997) andis similar along its entire length and shows typicaldisplays a well-developed horst-and-graben struc-continental margin features, dominated by NE–ture, which was acquired during the LateSW oriented horsts and grabens. This marginOligocene–Early Miocene opening of the Valenciarecords the Oligocene–Early Miocene opening oftrough. This extensional structure is superimposedthe basins and is cut by the Catalan transfer faulton diverse contractional fold-and-thrust belts(Fig. 1), which divides the margin in two sectors:(Pyrenees and Catalan Coastal Ranges) thatthe Gulf of Lions, which corresponds to the NWdeformed the Catalan margin during theboundary of the Provencal and Ligurian basins,

and the Catalan–Valencian domain, which consti- Palaeogene collision between Iberia and Eurasia.In terms of the observed geometric and kine-tutes the NW margin of the Valencia trough.


Fig. 2. Sketch of the northeastern Iberian Peninsula and surrounding offshore areas in which the main Cainozoic structures andbasins are reported. The Catalan margin (framed by the thick dotted line) extends from the Pyrenees to the Ebro delta and it ischaracterised by the ENE–WSW- to NNE–SSW-oriented structures. The thick line labelled A–A∞ indicates the location of cross-section in Fig. 3. From NE to SE: Rb, Roses basin; SFb, Sant Feliu basin; Cb, Campins basin; GMh, Garraf–Montnegre horst; PR,Prelitoral Range; VPb, Valles-Penedes basin; Bb, Barcelona basin; Ba, Barcelona; ECb, El Camp basin; Tt, Tarragona trough.

matic features of the extensional and contractional NW–SE normal faults, which cut these thrustsheets, have been active since the Middle Miocenestructures, the Catalan margin can be divided into

a northern and a southern sector (Fig. 2). (Tassone et al., 1996) and are related to an impor-tant alkaline volcanism (Saula et al., 1996).The northern sector shows a complex Cainozoic

structure with superposition of the eastern end of The southern sector extends for about 200 kmand, in it, the Neogene extension splits the ENE–the Palaeogene South-Pyrenean thrust belt and the

NW–SE-trending normal fault system, which sepa- WSW Palaeogene intraplate chain of the CatalanCoastal Ranges into a horst-and-graben systemrates the northwestern margins of the Valencia

trough and the Provencal basins. The South- with the same orientation. The Palaeogene struc-ture of this sector consists mainly of a major ENE–Pyrenean thrust belt is characterised by the imbri-

cation of E–W- to NW–SE-oriented thrust sheets, WSW-oriented thick-skinned thrust sheet, whichhad a limited strike-slip motion and deformedwhich affected the Hercynian basement, the

Mesozoic cover and the latest Cretaceous to the previous minor thrusts and fault-related folds. Thismajor thrust sheet, involving the Hercynian base-Early Oligocene successions of the northeastern

Ebro basin (Pujades et al., 1989). The Neogene ment, bounded the Ebro basin to the SE and


uplifted the Catalan Coastal Ranges more than normal faults: the Valles-Penedes and Barcelonafaults (Figs. 2 and 3). Both faults are more than1900 m in relation to the neighbouring marginal

zones of the Ebro basin (Lopez-Blanco et al., 100 km long and dip to the SE. The verticaldisplacement, calculated with the base of the2000). From the Late Oligocene, the tectonic inver-

sion of the main Palaeogene faults split the area Cainozoic as a reference, reaches 4 km in theValles-Penedes fault and 6 km in the Barcelonain a set of ENE–WSW blocks mainly tilted to the

NW (Bartrina et al., 1992; Roca and Guimera, fault. The displacement increases to a minimumof 8.5 km in the Barcelona fault, if it is calculated1992). In the most depressed part of these blocks,

the El Camp, Tarragona, Barcelona, Sant Feliu from the top of the Hercynian basement, since oil-well data show that, in contrast to the footwall-and Valles-Penedes basins developed and were

infilled by more than 4000 m of sediments ranging block where it is absent, the Mesozoic cover is2.5 km thick in the hanging-wall-block. Listricin age from Oligocene to Present (Bartrina et al.,

1992; Martınez del Olmo, 1996; Alvarez de Buergo geometry for both faults can be inferred from theseismic profiles. The trace of the Barcelona faultand Melendez Hevia, 1996).

According to this regional arrangement, the is marked by a set of strong reflectors that flattenat depth whereas its hanging wall has a roll-overstudy area comprises the northern and central

parts of the southern sector of the Catalan margin, geometry (Fig. 4). In the Valles-Penedes fault,some of the few available seismic profiles (Bartrinawhere Cainozoic ENE–WSW contractional and

extensional structures were superimposed. et al., 1992) show a roll-over geometry in itshanging wall, also suggesting a listric fault geome-try. From the geometric analysis of these roll-overstructures, the detachment depth of both faults3. Structure of the central Catalan marginhas been located in the lower/upper crust boundary(13–15 km; Roca and Guimera, 1992).The upper crustal structure of the study area

consists of three differently deformed domains(Prelitoral range and the Ebro basin; the Valles- 3.1. Prelitoral range and Ebro basinPenedes half-graben and Garraf–Montnegre horst;and the Barcelona and Sant Feliu half-grabens) Northwest of the Valles-Penedes master fault,

the upper crust is characterised by the presence ofseparated by two major ENE–WSW-oriented

Fig. 3. General cross-section across the central Catalan margin. The offshore part corresponds to the depth conversion of the 75141interpreted seismic line. PR: Prelitoral Range. See Fig. 2 for location.


Palaeogene structures only. The Hercynian base- suggest that the Valles-Penedes normal faultresulted from the tectonic inversion of the base-ment, the Triassic cover and the Ebro basin-fill

(Palaeocene–Late Eocene in age) are gently tilted ment thrust.to the NW, except close to the Valles-Penedes faultwhere they are strongly deformed by northwest- 3.2. Valles-Penedes half-graben and Garraf–

Montnegre horst structureverging contractional structures along a 5–10 kmwide stripe. These structures accommodate about8 km of NW–SE shortening (Lopez-Blanco et al., Between the Valles-Penedes and Barcelona

faults, the Cainozoic upper crustal structure is2000) and record the emplacement of a majorthick-skinned thrust, which includes the Catalan simpler. It consists of Hercynian basement overlain

by a Mesozoic cover, which are tilted northwest-Coastal Ranges. The coeval syntectonic Ebro basininfill deposits record the activity of this contractio- ward to form a major depocentre close to the

Valles-Penedes fault and a parallel system of highsnal structure from Palaeocene until a period laterthan Late Eocene (Lopez-Blanco et al., 2000). to the SE (the so-called Garraf–Montnegre horst).

This structure is cut by hectometric ENE–WSWThe verging of the minor structures and thefold geometry of the pre-Tertiary rocks indicate normal faults that split the area into minor horsts

and grabens (Fig. 3).that this thrust sheet was emplaced towards thenorthwest. However, the presence in the hanging These minor grabens and the above-mentioned

depocentre (the so-called Valles-Penedes half-wall of this thrust of synchronous ENE–WSWsubvertical faults with sinistral strike-slip motion graben) are infilled mainly by Early Miocene–

Pliocene deposits (Cabrera and Calvet, 1996).(Anadon et al., 1985) denotes that, at depth, thisthrust moved northwards. Taking this into account These deposits are cut by the normal faults and

the strata are generally tilted to the NW, exceptand the N–S regional shortening direction resultingfrom the Iberian–Eurasian convergence (Guimera close to the Valles-Penedes fault where they consti-

tute a tight syncline. Therefore, taking into accountand Alvaro, 1990), we interpret that thePalaeogene structure of the Catalan Coastal that all the preserved structures affect the Neogene

deposits, the present upper crustal structureRanges records the emplacement of a major base-ment thrust above an oblique ramp. The detach- between the Valles-Penedes and Barcelona faults

appears to be a result of the Neogene stage ofment level of this basement thrust has been locatedat a depth of 12 km southwest of the study area, extension.

The available chronostratigraphical data of thewhere the Palaeogene structure of the CatalanCoastal Ranges is better preserved from both outcropping sequences (early Burdigalian to

Pliocene; Crusafont et al., 1955; Agustı et al.,erosion and Neogene extension (Gomez-Exposito,1997). The coincidence of this value with that 1985) only allows the dating of the middle and

upper part of the syntectonic sediments recognisedcalculated for the adjoining Valles-Penedes masterfault (12–15 km) denotes that both faults have the in the seismic lines. Therefore, in this sector, the

initiation of extension has not been dated.same detachment level. This fact, together withthe surface data that show that the extensional Nevertheless, the structure and sedimentology of

the deposits infilling the Valles-Penedes half-grabenValles-Penedes fault and the out-of-sequencePalaeogene thrusts join at depth (Fontbote, 1954), indicate that most extensional faulting ended

Fig. 4. (a) Part of unmigrated 75141 seismic line (Shell ) with the location of the Calella C-1 (CALC1) and Barcelona C-1 (BARC-1)wells. In both wells, there are indicated the diverse units that they cut according the interpretation done in this work. (b) Geologicalcross-section through the Barcelona half-graben constructed from 73141 and 75141 seismic profiles (Shell ). Thick lines represent thefaults and arrows onlaps and truncations observed in the Cainozoic sediments. The differentiated Cainozoic units are: PQ, Plio-Quaternary; M4, Tortonian–Messinian; M3, Langhian–Serravallian; M2, Burdigalian; M1, Aquitanian; O1, O2, O3, O4, O5, Oligoceneand also maybe Late Eocene. The pre-Cainozoic basement is represented by a pattern of small lines chaotically oriented. (c) Transversesedimentary model of the Barcelona half-graben based on the above-shown seismic profile and cross-section.


during the late Burdigalian (Early Miocene) and Blanco et al., 2000) show that the Valles-Penedeshalf-graben and the Garraf–Montnegre horst werethat only the Valles-Penedes fault was active until

the Tortonian (Bartrina et al., 1992; Garces an uplifted sector in which only minor local foldsand vertical strike-slip to reverse faults developedet al., 1997).

The absence of readily recognisable sediments during the Palaeogene (Fontbote, 1954).and structures older than Early Miocene results ina rather imprecise knowledge of the Palaeogene 3.3. Barcelona–Sant Feliu half-grabensstructure, which is essentially based on datarecorded in the surrounding areas. Sedimento- These half-grabens, which occur southeast of

the Barcelona fault, are aligned along its strikelogical studies of the Ebro basin deposits (Lopez-

Fig. 5. Isochrone map of the pre-Cainozoic basement of the offshore Catalan margin showing the main recognised structures (faults,highs and half-grabens). This map has been constructed from the interpretation of more than 400 seismic profiles shot between 1972and 1987 by Auxini, Shell, Eniepsa, Georex, Total, Western, California Oil and Chevron Oil and from their correlation with the 18wells drilled in the area. A–A∞, B–B∞ and C–C∞ indicate the location of the seismic lines respectively shown in Figs. 4, 6 and 8.


Fig. 6. (a) Part of unmigrated S81-92 seismic line (Chevron Oil ) with the location of the Rosas 3-2 (R3-2), Rosas 3-1 (R3-1) andthe projected Rosas 2-1 (R2-1) wells. In the three wells, there are indicated the diverse units that they cut according to the interpretationdone in this work. (b) Geological cross-section through the Sant Feliu half-graben constructed from the S81-92 seismic profile(Chevron Oil ). Same legend as Fig. 4 except for the Oligocene sediments, which here have been represented in a unique dark greycolour labelled with the letter O. (c) Transverse sedimentary model of the Sant Feliu half-graben based on the above-shown seismicprofile and cross-section. Same legend as Fig. 4.


Fig. 7. Synthetic stratigraphic sections of the Barcelona, Sant Feliu and Valles-Penedes basin infilling series showing the differentiatedunits and the main lithostratigraphic features. Only major unconformities are depicted.


and bounded to the SE by ENE–WSW highs 4.1. Lower ensemble (Late Eocene?–LateOligocene in age)(Fig. 5). In both half-grabens, the pre-Cainozoic

rocks are generally tilted towards the northwest,This includes units O1, O2, O3 and O4, whichexcept near the Barcelona fault where they are

are restricted to the troughs, and are cut by thetilted in an opposite direction, forming a synclinenormal faults. They show no significant thicknessparallel to the fault (Figs. 4 and 6). In the struc-changes related to faults, and lie parallel to thetural highs, the pre-Cainozoic rocks define antop of the pre-Cainozoic rocks, even in areas whereanticline of 15–30 km wavelength, which is com-this is folded.partmentalised by normal faults that dip mainly

The lower ensemble is latest Eocene (?)–northwestward.Oligocene in age on the basis of regional criteriaThis basement structure is covered by a thickand the study of non-marine charophyte assem-(1000–8000 m) sequence of Late Eocene (?) toblages (Roca et al., 1999). It consists of alluvialPresent sequences that are also partially affectedand lacustrine successions with some interfingeringby this deformation. However, the geometry, agemarine units in the eastern part of the Sant Feliuand stratigraphy of these Cainozoic sediments andbasin and in the southwestern part of the Barcelonatheir geometric relationship with the pre-Cainozoicbasin. In the latter, O1 to O4 units are wellstructure has not been analysed thoroughly tocharacterised and significant changes from coarse-date. This is surprising if we take into accountgrained proximal alluvial deposits to finer-grainedthat, amongst the three defined blocks of thedistal alluvial and marine successions occur fromCatalan margin, that of the offshore is the onlythe NE to the SW, where lacustrine to marine,one to show a sedimentary cover that embracessulphate and chloride evaporites were deposited.

the Palaeogene and the Neogene and, therefore:(Fig. 8).

(1) is coeval with the development of contractionalas well as extensional processes in the Catalanmargin; (2) covers the time span (Late Eocene to 4.2. Middle ensemble (Late Oligocene–Aquitanian)the early Burdigalian), which is scarcely recordedin the onshore successions. The only depositional This ensemble incorporates units O5 and M1,record belonging to the previously mentioned time which are restricted to the deepest parts of thespan that has been recognised onshore occurs in a troughs. They are cut by most of the faults, overlievery small Early Oligocene non-marine basin (the unconformably the top of the pre-Cainozoic rocksso-called Campins basin) in the ENE corner of the and show sharp and frequent thickness changes.Valles-Penedes half-graben (Anadon, 1986). In the Barcelona and Sant Feliu half-grabens these

units do not describe the underlying syncline andshow a noticeable thickening towards the synclineaxis through divergent sets of beds, which displayfrequent angular unconformities (Figs. 4 and 6).

4. Structure and stratigraphy of the offshore The age of the middle ensemble is only wellsediments constrained in the M1 unit, which contains

Aquitanian marine fossils (Roca et al., 1999). TheTen stratigraphic units, which are in part bound latest Oligocene age of unit O5 has been deduced

by major unconformities and show significant from the age of its overlying and underlying units.depositional and geometrical differences, are Units O5 and M1 are mainly alluvial and showdefined in the offshore central and northern areas rapid facies changes from NW to the SE (i.e.of the Catalan margin (Roca et al., 1999). These compare Figs. 4 and 8). For unit M1, the alluvialunits, according to their geometric relationships assemblages shift from proximal to distal and towith the structure of the pre-Cainozoic rocks, can marine shelf deposits in only a few kilometres

away from the fault.be grouped in three ensembles (Fig. 7).

Fig. 8. (a) Part of unmigrated 73212 seismic line (Shell ) with the location of the Barcelona B-1 (BARC-1) and the projected Barcelona C-1 (BARC-1) wells. In both wells, there are indicated the diverse units that they cut according to the interpretation done in thiswork. (b) Geological cross-section along the Barcelona half-graben constructed from the 73162, 73212 (Shell ) and S87-22 (Chevron Oil ) seismic profiles. Same legend as Fig. 4. (c) Longitudinal sedimentary model of the Barcelona half-graben based on the above-shown seismic profile and cross-section.

pp. 220–223E. Roca et al. / Tectonophysics 315 (1999) 209–233


4.3. Upper ensemble (Burdigalian–Present day) covered the faults developed offshore and spreadover the structural highs), it still shows typicalfeatures of the syn-rift deposits near the BarcelonaThe upper ensemble includes the M2, M3, M4fault as: (1) it presents minor thickness increasesand PQ units. These units are subhorizontal ortowards the fault through divergent sets of bedsgently tilted to the SE and spread over the troughand (2) it is cut, together with units M3 and M4,margins overlapping all the pre-Cainozoic highsby this major fault.(Figs. 4, 6 and 8). Only the lowermost part of unit

M2 is affected by faults and has some significantthickness changes related to them. The overlyingsequences show no fault-related thickness changes 5. Evolution of the central Catalan marginand appear to cover most of the faults identifiedin the seismic profiles. The offshore tectono-sedimentary evolution,

Unlike the two lower ensembles, the age of the together with available onshore data, allows us toM2, M3, M4 and PQ units is well constrained by define and date the main tectonic events thatplanktonic foraminifera. Unit M2 has been dated happened in the Catalan margin from the Lateas Burdigalian, M3 as Langhian–Serravallian, M4 Eocene to the present. Thus, three major stagesas Tortonian and PQ as Plio-Quaternary (Roca can be distinguished in the post-Eocene evolutionet al., 1999). From a sedimentological point of of the Catalan margin (Figs. 10 and 11).view, the upper ensemble embraces a large varietyof facies. In the Burdigalian and Langhian, trans- 5.1. Late Eocene–early Late Oligocenegressive–regressive episodes are recognised. Thisresulted in the formation of early fan-deltas and The Oligocene units O1–O4 of the Barcelonashelf complexes in the offshore sedimentary basin and the lower and middle parts of thetroughs and coralgal platforms on their surround- Oligocene successions of the Sant Feliu basin wereing highs. The spreading of marine environments deposited during this period. On the basis of theirtowards the present onshore zones resulted in the geometry and their relationship with the faults,exhaustion of the non-marine deposits in the off- these units represent the pre-rift period and wereshore zones and the shifting of the fan-delta, shelf sedimented before the development of horsts andand coralgal depositional frameworks towards the grabens. Taking this and other regional featuresonshore zones. Late Langhian to Present deposi- into account, we can infer that the Oligocenetional evolution was characterised by an increasing successions preserved in the Barcelona and Santrestriction of carbonate sedimentation and by the Feliu half-grabens record the existence of a pre-development of shelf–talus progradational systems rift basin (Fig. 10). This basin was bound towards(units M3, M4 and PQ), the evolution of which the northwest by a set of relieves located along thewere temporarily truncated during the late currently emerged area of the Catalan CoastalMessinian regression. Ranges. The existence of these relieves is well

recorded in the Barcelona basin thanks to the4.4. Structural meaning of the depositional record occurrence of Palaeozoic clasts in the Oligocene

successions. Nevertheless, the arrangement andsedimentological features of the units O1–O4 alsoAll the above-mentioned features (summarised

in Fig. 9) suggest that the lower (O1–O4), middle suggest the existence of other relieves to the north-east in the Malgrat structural high, since these(O5–M1) and upper ensembles were deposited

respectively during the pre-, syn- and post-rift units onlap the basement in this direction, theystack in a retrogradational sequence and thestages. Nevertheless, the boundary syn-rift–post-

rift is more transitional than previously interpreted coarser facies increase towards the northeast(Fig. 8). These facies and the composition of thefrom the depositional record (Bartrina et al., 1992)

and does not correspond to a sharp and marked clast (mainly Mesozoic carbonates) indicate theexistence of alluvial fans that spread from NE toboundary like a regional unconformity. Although

in its broad outline, unit M2 is post-rift (since it SW of the present Barcelona basin. In the Sant


Fig. 9. Summary chart with the main tectono-sedimentary features of the diverse units that integrate the Catalan margin sedi-mentary infill.

Feliu basin, the facies arrangement and the mainly 1986). This suggests that the early and early–lateOligocene (Rupelian, early Chattian) offshoregranitic contribution recorded in the Oligocene

terrigenous deposits denote that the basin opened relief and sedimentation were also developed in acontractional setting. The partial restoration oftowards the southeast and that the Palaeozoic of

the Les Gavarres and Montseny was submitted to the regional cross-section (Fig. 11) and the palaeo-geographic map that corresponds to the period oferosion (Fig. 10). The presence of Oligocene

marine sediments in the eastern end of this basin, O4 sedimentation (Fig. 10) show that the sedi-mentation of the lowermost four Oligocene unitsand of marine evaporites in the southwestern part

of the Barcelona basin, corroborate that both appears to be synchronous with the thrusting ofthe Catalan Coastal Ranges over the Ebro basin.sectors were connected with the western Tethys

during the Late Palaeogene. This thrusting could be related to the major north-directed buried thrust that, detached at a depth ofThe tectonic setting in which this basin and the

surrounding highs developed is not well character- 12 km (see Section 3.1), uplifted the presentlyemerged Catalan Coastal Ranges. The geometryised, but in the emerged part of the Catalan

Coastal Ranges the early Oligocene belongs to the of the hanging wall suggests that this major thrustconsisted of a south-dipping ramp linked with acontractional episode during which folds and

thrusts developed (Anadon et al., 1985; Anadon, flat southwards. This geometry would explain both


Fig. 10A.


Fig. 10. Palaeogeographic maps of the central Catalan margin showing the main evolutionary features of the area during the Oligoceneand Miocene. The four maps attempt to show significant stages of the pre-rift (upper Oligocene map), syn-rift (Aquitanian–earlyBurdigalian map), the syn-rift–post-rift ( late Burdigalian–early Langhian map) and the post-rift (Tortonian map) evolution of the area.

the lack of vertical uplift of the offshore areas, back basin that occupied the northeastern part ofthe Valencia trough (Fig. 11).and the horizontal position of the Mesozoic strata

in the uplifted Catalan Coastal Ranges andbeneath the offshore Oligocene basin. As a conse- 5.2. Late Oligocene–early Burdigalianquence, the Late Eocene to middle Oligocene off-shore successions in the Catalan margin could be During this period, sedimentation of the units

O5, M1 and the lower part of M2 took place. Ininterpreted as having been deposited in a piggy-


Fig. 11. Schematic partial restorations of a synthetic regional cross-section through the central Catalan margin. Note that the threepartial restoration correlate in time with the first three evolutionary stages represented in the maps of Fig. 10. Same environmentallegend as Fig. 10.


contrast to the previous contractional stage, there Miocene (M1) units are restricted to the troughsand display: (1) a syncline geometry with sharpwas a strong extensional tectonic activity and the

main structural features were acquired from the thickening towards the bounding faults, tilting ina NW–SE direction; (2) internal angular unconfor-compartmentalisation of the contractional build-

ing in a system of horsts and grabens bounded by mities and onlaps that developed mainly in adirection perpendicular to the faults. Moreover,ENE–WSW normal faults. The main normal faults

are the Valles-Penedes and Barcelona faults. These denoting a significant change in the tectonic evolu-tion of the area, in the Barcelona half-graben, thefaults have a listric geometry, dip to the southeast

and form the northwestern boundary of the Valles- best recorded transport direction of the sedimentschanges from predominantly NE–SW to NW–SE,Penedes and Barcelona half-grabens respectively.

The age in which the normal motion of these faults as indicated by the predominance of onlaps andfacies changes in this new direction.began is only well constrained in the Barcelona

fault, where the older syn-rift related sediments In addition to its syn-rift character, the offshoreas well as onshore uppermost Oligocene andhave been dated as late Oligocene. In the Valles-

Penedes fault, the uncertainty in age of the oldest Aquitanian to lower Burdigalian successions reveala complex palaeogeography. The Catalan marginsediments filling the Valles-Penedes graben only

allows one to place the beginning of the extensional appears to have been split by a system of NE–SWbasins, which were separated by structural highsmotion of the fault between the middle Oligocene

and the Burdigalian (age of the younger pre-rift submitted to erosion. The basins were closed orconnected by narrow corridors with the marineand older syn-rift well-dated sediments). This

implies that the initiation of the normal motion of environment of the Valencia trough (Fig. 10). Inthis scenario, the Sant Feliu and Valles-Penedesthe Valles-Penedes fault might be coeval or youn-

ger than in the Barcelona fault. half-grabens were probably closed basins in whichthe main source areas of the terrigenous sedimentsThe location and geometry of these two major

faults in relation to the previous contractional were located towards the north and northwest, asis reflected by the mostly Palaeozoic compositionstructure indicate that they developed from the

tectonic inversion of the major thick-skinned thrust of the clasts (mainly granitic in the Sant Feliu half-graben but also slaty in the Valles-Penedes half-that uplifted the Catalan Coastal Ranges. Besides

the presence at the surface of minor Miocene graben). The closed drainage system of these twobasins is suggested by the presence of lacustrinenormal faults that link at depth with previous

Palaeogene thrusts, the analysis of the geometry evaporitic sediments in the southern parts of thebasin that spread over the retrogradational alluvialof the major faults shows that: (1) the late

Oligocene–Miocene normal faults only developed fan system that infill the rest of the basins. Incontrast, the Barcelona half-graben appears toin the hanging wall of the major Eocene–middle

Oligocene thrust; and (2) the detachment level of have been connected with the sea, with alluvialfans that developed in its northwestern and north-this major thrust coincides with that of the Valles-

Penedes and Barcelona normal faults. Hence, we ern margins. The marine influence is shown by thepresence of transitional deposits in the southernsuggest that the Valles-Penedes fault coincides at

depth with the frontal ramp of the major thrust parts of the basin where, according to the locationof the surrounding basement highs, the connectionthat uplifted the Catalan Coastal Ranges during

the Palaeogene, and that the Barcelona fault with a terrigenous marine shelf seems moreprobable.formed on the backlimb of the anticline developed

above this ramp (Fig. 11).The presence of extensional tectonic activity 5.3. Late Burdigalian–Quaternary

during the late Oligocene–early Burdigalian is wellrecorded in the infill of the Valles-Penedes, During this stage, extensional tectonics had not

completely ceased, but it attenuated so that onlyBarcelona and Sant Feliu half-grabens. Here,the uppermost Oligocene (O5) and lowermost the Valles-Penedes and Barcelona major faults


were active. In these faults, extensional faulting maps that show the basin configuration at thetransition from compression to extension in thedecreased during the Middle and Late Miocene

and virtually ceased during the Pliocene. This northwestern Mediterranean (Fig. 12). These mapsoutline three tectonic features referring to the timedevelopment is well recorded in the sedimentary

successions of this age outcropping onshore and during which the northwestern Mediterranean basinformed and which had not been shown or definedin the offshore Miocene M3, M4 and the Plio-

Quaternary PQ units. These successions onlap and with precision in previous studies.First, the northwestern Mediterranean basincover most of the structural highs and are only

deformed in their lower parts (M3 and M4) by (precursory of the present western Mediterranean)did not belong to a simple extensional basin duringthe major faults (Figs. 4, 6 and 8). Also denoting

this almost total attenuation of the tectonic activ- its initial stages. Although the Gulf of Lions data(Seranne et al., 1995; Benedicto, 1996) indicateity, the younger successions of this evolutionary

stage (M3, M4 and PQ) show a smoothening of that it was an extensional basin during the middleto upper Oligocene, this study shows that, towardsthe basin floor and a great sedimentological homo-

geneity (marine terrigenous sediments deposited in the northeastern Valencia trough, this basin existedat the same time as a contractional piggybacka transitional and shallow nearshore environment

that grades offshore to a shelf–slope prograda- basin. The geometry and size of this piggybackbasin is not well constrained. It developed betweentional system).

This stage is still related to the rifting event, the Late Eocene–Oligocene thrust belts of theCatalan Coastal Ranges and the Balearic islands,but it records a period in which (1) most of the

faults became inactive and, (2) the offshore basins and, did not expand over the central and south-western parts of the Valencia trough according tosubside due to the thermal relaxation of the

thinned crust (Bartrina et al., 1992; Watts and available offshore data.Second, the timing in which the CainozoicTorne, 1992). Therefore, it can be considered that

this stage includes the post-rift evolution of the extensional tectonics began in the basin. Accordingto the available data, the extension started in theCatalan margin.

In this tectonic setting, the persistence of fault early Oligocene in southern France and migratedprogressively to the southwest, affecting the north-activity along the Barcelona and Valles-Penedes

faults (outer marginal major faults of the exten- east Valencia trough during the latest Oligocene–Aquitanian.sional fault system of the Valencia trough) has

been related to the opposing lithospheric vertical Third, the map reveals that, along most of thenorthwestern margin of the basin, the extensionmovements between the subsiding Valencia trough

basin and its rising shoulders (Bartrina et al., resulted from the tectonic inversion of thePalaeogene NE–SW thrusts that emerged in the1992). These movements could explain the dis-

placement of 1–2 km along the Valles-Penedes and Catalan Coastal Ranges and Provencal arc.All these features suggest that the northwesternBarcelona faults during the Middle and Late

Miocene, and, therefore, the syn-rift features of Mediterranean basin mainly developed inside a beltof northwest- to north-directed thrusts of Eocene–the unit M2 close to these faults.Oligocene age that was totally or partially occupiedby piggyback basins. The presence of marine depos-its in these piggyback basins indicates that they6. Implications in the evolution of the northwestern

Mediterranean Basin were connected to the southeast with the Tethysand that these areas were not largely thickened.Therefore, the extensional northwesternThe results of this study, together with available

data of the other sectors of the northwestern Mediterranean basin formed over a crust in themain, slightly thickened by contractional processesMediterranean (i.e. Gorini et al., 1991, Seranne

et al., 1995; Mauffret and Gorini, 1996; Roca, and where sedimentary basins already existed form-ing part of the northwestern margin of the Tethys.1996), allowed us to construct two palinspastic


The data also corroborate the propagation ofthe extension or collapse of this older (Eocene–Oligocene) thrust belt from the northeast duringthe early Oligocene to the southwest until itaffected the southwest Valencia trough during theBurdigalian.

7. Conclusions

The integration of data from the northwesternMediterranean with available onshore and offshoreinformation for the Catalan margin enables us toestablish the following.

(1) The structure of the central Catalan marginis the result of the emplacement (during Eocene–middle Oligocene time) of a major northwesterlydirected thrust sheet. This contractional structurewas inverted and compartmentalised during thelatest Oligocene–Aquitanian in a system of NE–SW oriented horsts and grabens.

(2) The relation between the Tertiary sedi-mentary record and the pre-Cainozoic structuresindicates: (a) an initial, pre-extensional episode,probably related to the late stages of the Pyreneancompression, and (b) a subsequent extensionalepisode, linked to the opening of the Valenciatrough and which includes syn-rift and post-riftstages.

(3) The development of a NE–SW-orientedpiggyback basin in the present offshore character-ises the last stages of the pre-extensional episodeand is well recorded by Lower to lower UpperOligocene, continental to marine successions. Thisbasin was bound to the northwest (present locationof the coastline) by a contractional topographicrelief resulting from the motion of a major thrustsheet above a footwall ramp. The pre-rift signature

Fig. 12. Palinspastic maps of the northwestern Mediterraneanshowing two consecutive stages of the formation and earlydevelopment of the northwestern Mediterranean basin. Datafrom: Carmignani et al. (1995), Benedicto (1996), Roca (1996),Vially and Tremolieres (1996). In these reconstructions, therelative position of continental blocks is based on Burrus(1984). The location of the inferred subduction zone is approxi-mate [modified from Rehault (1981) and Rehault et al. (1984)].Co., Corsica; Sa., Sardinia; Ca., Calabria; Ka., Kabylies.


of the basin infill is clear and its depositional also provided by the Research Group ofGeodynamics and Basin Analysis (SGRarrangement shows that the spread of the sedi-

ments was mainly southwestward. 1997-00073) of the Comissionat per Universitats iRecerca of the Generalitat de Catalunya. The(4) The syn-rift episode took place from the

end of the Oligocene until the early Burdigalian authors wish to thank Roy H. Gabrielsen and ananonymous reviewer for their critical comments(Early Miocene) and gave rise to the present horst-

and-graben structure of the Catalan margin. The and helpful suggestions.sedimentation was restricted to the grabens andthe sediment transport direction changed from onethat was longitudinal (NE–SW ) to one that was Referencestransverse (NW–SE). The syn-rift character of theuppermost Oligocene–lower Burdigalian is shown Agustı, J., Cabrera, L., Moya, S., 1985. Sinopsis estratigrafica

del Neogeno de la fosa del Valles-Penedes. Paleontol.by the onlaps in a NW–SE direction, as well as byEvol. 18, 57–81.their thickness variations towards the normal

Alvarez de Buergo, E., Melendez Hevia, F., 1996. Caracterısti-faults.cas generales de las subcuencas del margen peninsular medit-

(5) The post-rift stage started in the late erraneo (‘‘Rift’’ del Surco de Valencia). Acta Geol. Hisp. 29Burdigalian and has continued until Present. The (1994), 67–79.

Anadon, P., 1986. Las facies lacustres del Oligoceno de Cam-attenuation of the tectonic activity, the sedimentpins (Valles oriental, provincia de Barcelona), Sedimenta-spreading over most of the horsts (which becamecion Continental de Espana. Cuad. Geol. Iberica 10,completely covered) and the constant sediment271–294.

thickness with no changes near the faults character- Anadon, P., Cabrera, L., Guimera, J., Santanach, P., 1985.ise this episode. However, although they concealed Paleogene strike-slip deformation and sedimentation along

the southeastern margin of the Ebro Basin. In: Biddle, K.,some faults, the upper Burdigalian and lowerChristie-Blick, N. (Eds.), Strike-Slip Deformation, BasinLanghian sequences are still affected by normalFormation and Sedimentation. Spec. Publ. Soc. Econ.faults. This indicates that the syn-rift–post-riftPaleont. Mineral. 37, 303–318.

change was transitional. Auzende, J.M., Bonnin, J., Olivet, J.L., 1973. The origin of the(6) The northwestern Mediterranean basin Western Mediterranean basin. J. Geol. Soc. London 129,

607–620.existed during the early to early late Oligocene asBartrina, M.T., Cabrera, L., Jurado, M.J., Guimera, J., Roca,an extensional basin in the Gulf of Lions and as

E., 1992. Evolution of the central margin of the Valenciaa contractional piggyback basin in the northeast-trough (western Mediterranean). Tectonophysics 203,

ern Valencia trough. Also, the extension started in 219–247.the Early Oligocene in southern France and shifted Benedicto, A., 1996. Modeles tectono-sedimentaires de bassins

en extension et style structural de la marge passive du Golfeprogressively to the southwest, affecting the north-du Lion (partie nord), Sudest France. Ph.D. Thesis, Uni-east Valencia trough during the latest Oligocene–versite Montpellier II, France.Aquitanian. This demonstrates that the extension

Burrus, J., 1984. Contribution to a geodynamic synthesis of thein the western Mediterranean not only shifted Provencal basin (north-western Mediterranean). Mar. Geol.from the northwest to southeast but also that 55, 247–269.

Cabrera, L., Calvet, F., 1996. E8 onshore Neogene record inlongitudinal, from northeast to southwest, shiftsNE Spain: Valles-Penedes and El Camp half-grabens (NWoccurred.Mediterranean). In: Friend, P., Dabrio, C.J. (Eds.), TertiaryBasins of Spain: the Stratigraphic Record of CrustalKinematics. Cambridge University Press, Cambridge, UK,

Acknowledgements pp. 97–105.Carmignani, L., Decandia, A., Disperati, L., Fantozzi, L., Laz-

zarotto, A., Liotta, D., Oggiano, G., 1995. RelationshipsThis work was carried out in the framework ofbetween the Tertiary structural evolution of the Sardinia–a research project funded by the Elf-Aquitaine andCorsica–Provencal Domain and the Northern Apennines.

the DGICYT PB97-0882-C03-01 and -03 projects. Terra Nova 7, 128–137.We wish to thank Repsol and Shell for their Clavell, E., Berastegui, X., 1991. Petroleum geology of the Gulf

of Valencia. In: Spencer, A.M. (Ed.), Generation, Accumu-generous release of data. Financial support was


lation and Production of Europe’s Hydrocarbons. Oxford Mauffret, A., Pascal, G., Maillard, A., Gorini, C., 1995. Tecton-ics and deep structure of the north-western MediterraneanUniversity Press, Oxford, UK, pp. 355–368.Basin. Mar. Petrol. Geol. 12, 645–666.Crusafont, M., Villalta, J.F., Truyols, J., 1955. El Burdigaliense

Pujades, J., Casas, J.M., Munoz, J.A., Sabat, F., 1989. Thrustcontinental de la cuenca del Valles-Penedes. Mem. Com.tectonics and Paleogene syntectonic sedimentation in theInst. Geol. Dip. Prov. Barcelona 12, 1–260.Emporda area, southeastern Pyrenees. Geodinam. Acta 3,Dewey, J.F., 1988. Extensional collapse of orogens. Tectonics195–216.7, 1123–1139.

Rehault, J.P., 1981. Evolution tectonique et sedimentaire duFontbote, J.M., 1954. Las relaciones tectonicas de la depresionBassin Ligure (Mediterranee occidental ). Ph.D. Thesis,del Valles-Penedes con la Cordillera Prelitoral Catalana yUniversite Paris VI France.con la Depresion del Ebro. Tomo Homenaje Prof. E. Her-

Rehault, J.P., Boilot, G., Mauffret, A., 1984. The western Medi-nandez-Pacheco. R. Soc. Espanola Hist. Nat., 281–310.terranean basin geological evolution. Mar. Geol. 55,Gallart, J., Rojas, H., Diaz, J., Danobeitia, J.J., 1990. Features447–477.of deep crustal structure and the onshore–offshore transition

Roca, E., 1996. La evolucion geodinamica de la Cuenca Catala-of the Iberian flank of the Valencia trough (Western Medi-no–Balear y areas adyacentes desde el Mesozoico hasta laterranean). J. Geodyn. 12, 233–252.actualidad. Acta Geol. Hisp. 29 (1994), 3–25.Garces, M., Cabrera, L., Agustı, J., Pares, J.M., 1997. Old

Roca, E., Desegaulx, P., 1992. Analysis of the geological evolu-World first appearance datum of ‘‘Hipparion’’ horses: Latetion and vertical movements in the Valencia Trough area,Miocene large-mammal dispersal and global events. Geol-western Mediterranean. Mar. Petrol. Geol. 9, 167–185.ogy 25, 19–22.

Roca, E., Guimera, J., 1992. The Neogene structure of the east-Garcıa-Sineriz, B., Querol, R., Castillo, F., Arribas, J.R., 1979.ern Iberian margin: structural constraints on the crustal evo-A new hydrocarbon province in the western Mediterranean.lution of the Valencia trough ( Western Mediterranean).Final Proc. 10th World Petrol. Congr. (PD4), Bucharest,Tectonophysics 203, 203–218.Rumania, 191–197.

Roca, E., Sans, M., Cabrera, L., 1999. Modelo tectonosedi-Gomez-Exposito, M., 1997. Estil de plegament i deformaciomentario del sector central y septentrional del Margen Cata-alpina de la serra de Miramar i l’acabament NE de les Mun-lan sumergido (cubetas de Barcelona, Sant Feliu, Begur ytanyes de Prades. Thesis, University of Barcelona, Spain.Riumors-Roses). Libro Homenaje a Jose Ramirez del Pozo.Gorini, C., Viallard, P., Deramond, J., 1991. Modele d’inver-

Sabat, F., Roca, E., Munoz, J.A., Verges, J., Santanach, P.,sion negative: la tectonique extensive post-nappe du fosseMasana, E., Sans, M., Estevez, A., Santisteban, C., 1997.de Narbonne–Sigean (Corbieres, sud de la France). C. R.Role of extension and compression in the evolution of the

Acad. Sci. Paris Ser. II 312, 1013–1019.eastern margin of Iberia: the ESCI–Valencia trough seismic

Gorini, C., Mauffret, A., Guennoc, P., Le Marrec, A., 1994.profile. Rev. Soc. Geol. Espana 8 (1995), 431–448.

Structure of the Gulf of Lions (northwestern MediterraneanSaula, E., Picart, J., Mato, E., Llenas, M., Losantos, M., Beras-

Sea): a review. In: Mascle, A. (Ed.), Hydrocarbon and tegui, X., Agustı, J., 1996. Evolucion geodinamica de la fosaPetroleum Geology of France. Special Publ. E.A.G.P. 4, del Emporda y las Sierras Transversales. Acta Geol. Hisp. 29223–243. (1994), 55–75.

Guimera, J., Alvaro, M., 1990. Structure et evolution de la Seranne, M., Benedicto, A., Labaume, P., Truffert, C., Pascal,compression alpine dans la Chaıne iberique et la Chaıne G., 1995. Structural style and evolution of the Gulf of Lioncotiere catalane (Espagne). Bull. Soc. Geol. Fr. 8 (6), Oligo-Miocene rifting: role of the Pyrenean orogeny. Mar.339–349. Petrol. Geol. 12, 809–820.

Lopez-Blanco, M., Marzo, M., Burbank, D.W., Verges, J., Tassone, A., Roca, E., Munoz, J.A., Cabrera, L., Canals, M.,Roca, E., Anadon, P., Pina, J., 2000. Tectonic and climatic 1996. Evolucion del sector septentrional del margen conti-controls on the development of large, foreland fan deltas: nental catalan durante el Cenozoico. Acta Geol. Hisp. 29Montserrat and Sant Llorenc del Munt systems (Middle (1994), 3–37.Eocene, Ebro basin, NE Spain). Sediment. Geol. in press. Vially, R., Tremolieres, P., 1996. Geodynamics of the Gulf of

Maillard, A., Mauffret, A., Watts, A.B., Torne, M., Pascal, G., Lions: implications for petroleum exploration. In: Ziegler,Buhl, P., Pinet, B., 1992. Tertiary sedimentary history and P.A., Horvath, F. (Eds.), Peri-Tethys Memoir 2: Structurestructure of the Valencia trough (western Mediterranean). and Prospects of Alpine Basins and Forelands. Mem. Mus.Tectonophysics 203, 57–75. Natn. Hist. Nat. 170, 129–158.

Martınez del Olmo, W., 1996. E3 Depositional sequences in the Vidal, N., Gallart, J., Danobeitia, J., 1997. Contribution of theGulf of Valencia Tertiary basin. In: Friend, P., Dabrio, C.J. ESCI–Valencia trough wide-angle data to a crustal transect(Eds.), Tertiary Basins of Spain: the Stratigraphic Record in the NE Iberian margin. Rev. Soc. Geol. Espana 8of Crustal Kinematics. Cambridge University Press, Cam- (1995), 417–429.bridge, UK, pp. 55–67. Watts, A.B., Torne, M., 1992. Subsidence history, crustal struc-

Mauffret, A., Gorini, C., 1996. Structural style and geodynamic ture, and thermal evolution of the Valencia trough. A youngevolution of the Camargue and Western Provencal basin, extensional basin in western Mediterranean. J. Geophys.

Res. 97, 20 021–20 041.southeastern France. Tectonics 15, 365–375.

Evolution of the central Catalan margin of the Valencia trough (western Mediterranean

Documents

Transcript of Evolution of the central Catalan margin of the Valencia trough (western Mediterranean