Two-phase orogenic convergence in the external and internal SW Alps

Two-phase orogenic convergence in the external and internal SW Alps

Ford, Mary


The NW-SE-trending sector of the SW Alps includes the Dora Maira massif where Tertiary eclogites record ultrahigh pressures and rapid exhumation. Along a NE-SW crustal cross-section (Italy-France) compiled pressure-temperature-time data in internal zones are correlated with Tertiary stratigraphy in external zones to reconstruct orogen evolution, revealing a coherent two-phase convergence history. During the first, subduction-accretion phase (Eocene, 55-34 Ma) rapid north-south plate convergence caused the subduction and exhumation of high-pressure and ultrahigh-pressure (UHP) rocks in a steady-state subduction channel. This coincided with the north to NNW migration of an underfilled flexural basin across the European foreland. Nappe stacking within the subduction channel did not create significant relief, implying that primarily subduction forces generated this flexural basin. From 34 Ma onward, the second, collisional phase was characterized by slower NW-SE plate convergence. The internal units of the SW Alps underwent considerable anticlockwise rotation as they became involved in a NW-SE-oriented sinistral transpression zone between the European and Adriatic plates. To the north of the orogen the North Alpine Foreland Basin became overfilled as a result of high sediment supply from increasing orogen relief. In contrast, in SE France active flexure of the European plate appears to have ceased and sedimentation became limited to small thrust-sheet-top basins created by continuing gentle NE-SW shortening. Internal units were exhumed slowly from depths of c. 20 km, principally by erosion. In the SW Alps, the transition between these two phases was marked by the rapid subduction and exhumation of the Dora Maira UHP unit. Assuming lithostatic pressure, this unit would have been exhumed from 100 km depth, requiring a rate that exceeds that generated by plate convergence. Therefore, either exhumation was accelerated by additional stresses (locally generated by transpression, slab breakoff or high density contrasts) or, more controversially, the ultrahigh pressure occurred at a considerably shallower depth as a result of local overpressure.

The western Alpine orogen (Fig. 1) was caused by the convergence of the Adriatic microplate and the southward subducting European plate over a period of more than 60 Ma from the Late Cretaceous to the Miocene. Whereas many crustal cross-sections and their restorations have been constructed using the deep seismic profiles of the central and western Alps, few models have been proposed for the SW Alps (the NW-SE-striking arm of the western Alpine arc) where no deep seismic line has yet been shot. This sector includes the Dora Maira massif, where Tertiary eclogites record the highest pressures and most rapid exhumation in the Alps. In addition, the external zones in SE France record a distinct history from that of the central Alps. By integrating our own work with published data, a NE-SW crustal cross-section of the SW Alps has been constructed. We correlate pressure-temperature-time (P-T-t) histories across internal zones with the deformation and foreland basin evolution in external zones. As reconstructions involve considerable rotation and shear, both palaeogeographical maps and cross-sections are used. The trajectories of the internal high-pressure (HP) and ultrahigh-pressure (UHP) units are reconstructed in space and time.

Two phases of exhumation are recognized. It is shown that the subduction and exhumation of HP internal Alpine units are compatible with plate convergence models except for the Dora Maira UHP unit. Reconstruction of the trajectory of this unit during plate convergence demonstrates that forces other than those generated by plate convergence are required if lithostatic pressure gradients are assumed.

Deep structure of the SW Alps

The profile crosses the SW Alps from Savigliano on the Po plain of NW Italy to Digne in SE France (Fig. 2). No deep seismic profile crosses this part of the Alps. Deep structure is therefore constrained only by surface geology and published seismic tomographic models (Solarino et al. 1997; Waldhauser et al. 1998, 2002; Paul et al. 2001; Lippitsch et al. 2003). These data constrain the depth of the European Moho and the top and base of the east-dipping Ivrea body. The Ivrea body is a largely buried feature that is defined geophysically as having high density, high magnetic susceptibility and high seismic velocity. It can be traced at depth around the inner curve of the western Alpine arc, where it is estimated to be 10-30 km thick and dipping steeply east (Fig. 1). The roof of its southern termination lies 10km directly below the southern end of the Dora Maira massif.

The depth of the Adriatic Moho in the study area is poorly defined because the strong signature of the Ivrea body prohibits good tomographic resolution (Waldhauser et al. 1998). Ultramafic rocks of lower crustal and upper mantle origin crop out just south of the Insubric Line in the central Alps and are correlated with the Ivrea geophysical body. The Ivrea body is interpreted as part of the Adriatic upper mantle and is shown on our profile as an east-dipping wedge of mantle below the Dora Maira dome. To preserve coherence with crustal models proposed along the ECORS line to the north (e.g. Tardy et al. 1999; Schmid & Kissling 2000), the Ivrea body is shown to overlie the subducted European crust (Fig. 2). The contact between the internal Alpine units and the Adriatic crust below the Tertiary Po basin is shown as a SW-dipping thrust overlain by thick Oligocene-Neogene sediments of the Solinaro Basin (Cassano et al. 1986; Mosca 2006).

Surface structure of the SW Alps

Internal zone

The internal zone of the SW Alps comprises several tectonic units that, on our transect, stratigraphically belong to three palaeogeographical domains. These domains represent the proximal European passive margin (Briançonnais and Sub-Briançonnais domains) passing eastward through the distal European passive margin into the Ligurian ocean realm (Piemont-Liguria domain) (Stampfli et al. 2002). The Austroalpine domain (southern Adriatic plate margin) is not observed in this part of the Alps. Tectonostratigraphic units are defined within these palaeogeographical domains as having a common first-order tectonic and stratigraphic character.

The structure and kinematics of the internal zones in this region are not well constrained, with major differences in data and interpretation between researchers. Four deformation phases are generally recognized, one synchronous with, and three post-dating the HP and UHP metamorphism. Transport directions are towards either the east to NE or the west to SW. A more detailed analysis is considered unfeasaible at present and the reader is referred to Agard et al. (2001a) for a detailed review of published data and their discrepancies.

The Piemont-Liguria domain is dominated by the Schistes Lustrés (Upper Triassic to Upper Cretaceous), a sequence of monotonous calcschists intercalated on a kilometre to centrimetre scale with marbles, metabasites and ophiolitic slices. The Monviso unit is a 5-6 km thick, west-dipping stack of ophiolitic slices. The tectonostratigraphic units of the Piemont-Liguria domain underwent a polyphase deformation and locally record Alpine eclogitic conditions, overprinted by later more pervasive blueschist and greenschist events (e.g. Schwartz et al. 2000a).

In the Briançonnais domain, Triassic to Eocene carbonate and clastic sediments overlie a pre-Mesozoic basement of metasediments and gneisses. The Acceglio unit (Fig. 1) records early Alpine eclogite conditions overprinted by blueschist then greenschist conditions (Lefèvre & Michard 1976; Michard 1977; Schwartz et al. 2000b).

The Dora Maira massif is an elliptical dome-shaped tectonic window of probable Briançonnais rocks appearing from below Piemont-Liguria units (Fig. 1). UHP assemblages are found in a unit 4 km by 10 km and 1 km thick (UHP unit) forming around 3% of the surface area of the SE Dora Maira massif (Chopin 1984; Henry et al. 1993). Palaeogeographically, the Dora Maira massif is variably interpreted as either basement on the eastern limit of the Briançonnais domain (European margin; see Debelmas & Lemoine (1970) and Chopin et al. (1991) for discussion) or as part of the Adriatic margin (Stampfli et al. 2002) or an independent crustal block (Platt 1986). Along its eastern boundary the Dora Maira is unconformably overlain by onlapping Oligocene and Neogene deposits of the Savigliano basin, implying subsidence of up to 5 km since the Oligocene (Mosca 2006).

Based on deep structural models along the ECORS line further north, we speculate that the area between the Dora Maira dome and the Ivrea body is occupied by principally backfolded Briançonnais nappes (Fig. 2).

The internally derived Embrunais-Ubaye nappes include lower tectonic slices of Sub-Briançonnais Triassic-Upper Eocene sediments interleaved with the Autapie nappe of Helminthoid Flysch (Kerckhove 1969) and the upper and largest Parpaillon nappe consisting almost entirely of Helminthoid Flysch. This thick sequence of Upper Cretaceous turbidites is believed to originate from above the internal units. The whole lower Embrunais-Ubaye edifice was emplaced onto the foreland in the early Oligocene, and it was folded there with its substrate (Kerckhove 1969). Emplacement direction is as yet poorly constrained (Merle & Brun 1984; Fry 1989).

Recent workers have documented a composite kinematic history on the contact between external and internal zones (Sue & Tricart 1999; Ceriani et al. 2001; Tricart et al. 2001), which is referred to here by the non-generic name of Basal Penninic Fault following Ceriani el al. (2001). Late Miocene and younger extensional and strike-slip faults cut across the internal and external zones (Tricart et al. 2004).

External zone

The external fold and thrust belt of SE France comprises the Digne thrust system trending NW-SE and curving southward into the east-west-trending Castellane arc. Our cross-section cuts across the southern Digne thrust system and the northern end of the Argentera basement massif. A Triassic to Cretaceous, mainly carbonate passive margin sequence, up to 4 km thick, overlies Variscan crystalline basement. Remnants of the Eocene-Oligocene foreland basin are preserved as outliers. Sequential section balancing across the area indicates that 21 -26 km of basement-involved SW-SSW-directed shortening was accommodated during and after foreland basin development (Ritz 1991; Lickorish & Ford 1998). Active structures (folds and faults) controlled the late Priabonian-early Oligocene Grès d’Annot depocentres (Joseph & Lomas 2004). Mio-Pliocene exhumation of the Argentera crystalline basement massif (Bigot-Cormier et al. 2000, 2004) accounts for 10km of SW shortening and can be linked with final emplacement further west of the Digne thrust sheet over the Mio-Pliocene deposits of the Valensole basin (Fig. 1).

Pressure-temperature-time evolution of the SW metamorphic domain

Since the first report of coesite (Chopin 1984), the western Alps have become the focus of many studies on the exhumation of HP and UHP rocks during plate convergence (e.g. Platt 1986, 1993; Ballèvre et al. 1990; Philippot 1990; Chopin et al. 1991; Michard et al. 1993; Agard et al. 2001a; Wheeler et al. 2001; Reddy et al. 2003). The petrological and geochronological data obtained for the main tectonostratigraphic units on the transect (Acceglio, Schistes Lustrés, Monviso and Dora Maira UHP unit) have been given in Figure 3. Data from the Schistes Lustrés are taken from a wider area extending north to the Chenaillet Massif (Fig. 1). The paucity of geochronological data for the Briançonnais unit precluded the reconstruction of its T-t and P-t history. The retrograde P-T paths (Fig. 3a) are based on metamorphic petrology studies referenced in the figure captions. As much as possible, the P-T paths of the various subunits have been reported. The T-t diagrams (Fig. 3b) have been reconstructed from the published data, either by considering the temperature range given by authors (e.g. titanite formation, Rubatto & Hermann 2001; phengite formation, Agard et al. 2001b) or by assuming approximate closure or retention temperatures chosen to satisfy as much as possible the interpretation of authors (c. 350 °C for Ar in white micas, 300 °C in biotite, 500 °C for Rb-Sr in white micas, 250 °C for fission tracks in zircons and 100 °C for fission tracks in apatite). The P-t paths (Fig. 3c) have been constructed by combining the P-T and the T-t diagrams (Fig. 3a and b), except if the age could be directly related to pressure (e.g. pressure estimated from the Si^sup 4+^ content for phengite recrystallization by Agard et al. (2001b) or from the jadeite content of symplectites by Rubatto & Hermann (2001)). These data allow us to propose a two-phase exhumation history for the internal zones of the SE Alps: a period of subduction and rapid exhumation within the subduction channel during the Eocene, followed by a period of slower exhumation from Early Oligocene onward.

Eocene (55-34 Ma): subduction and rapid exhumation

Petrological studies indicate that peak pressure and temperature conditions were not homogeneous inside each tectonostratigraphic unit. Nevertheless, several workers (e.g. Schwartz et al. 2000a; Agard et al. 2001a) have pointed out that there is a general tendancy for peak pressure and temperature to increase from west (300-500 °C, 12-21 kbar in the Schistes Lustrés) to east (700-750 °C, 30 kbar in Dora Maira). Assuming a lithostatic pressure gradient, units were subducted to depths varying between 20km and 100km (Fig. 3) but these estimates would be reduced if there were local overpressure conditions (Petrini & Podladchikov 2000).

Although abrupt increases in metamorphic grade may occur across major tectonic contacts (Ballèvre et al. 1990; Philippot 1990), similar increases can occur from one subunit to another within individual tectonostratigraphic units, for example in the Monviso unit (Schwartz et al. 2000a; Agard et al. 2001a). Furthermore, this compilation shows the following features.

(1) Ages of peak pressure conditions in the Schistes Lustrés and Monviso units (Piemont-Liguria domain) lie within the period 55-45 Ma. Peak pressure in the Schistes Lustrés may be slighty older (55 Ma) than that in the Monviso unit (45-50 Ma).

(2) Although the highest pressure and temperature conditions in the Piemont-Liguria units are recorded by the most easterly Monviso slice (Lago Superiore), the range of pressure and temperature conditions recorded within the Monviso unit overlaps largely with that in the Schistes Lustrés so that the P-T gradient is not simply continuous from Schistes Lustrés to Monviso. Instead, these two units appear to have been buried along the same regional thermal gradient (c. 8 °C km^sup -1^ assuming lithostatic pressure, Agard et al. 2001a). This temperature gradient is geologically significant over the 55-45 Ma period provided that the thermal structure of the subduction channel remained constant over the whole subduction history, and that there were few lateral thermal heterogeneities across the subduction channel. The Schistes Lustrés and Monviso units seem to have sampled, at different times, different parts of a subduction complex characterized by a nearly steady-state thermal structure. This steady-state thermal structure can be generalized for the western Alps as underlined by Fry & Barnicoat (1987), who recognized that all HP Alpine rocks define a common metamorphic gradient of c. 8 °C km^sup -1^ whatever their age. There must have been differential burial, as all units did not experience the same peak pressure conditions (maximum in the Dora Maira UHP unit, no burial of the Helminthoid Flysch).

(3) The age of maximum pressure of the Dora Maira UHP unit (35 ± 3 Ma) is much younger than that of the Schistes Lustrés and Monviso units. However, maximum pressures and temperatures also define a gradient of c. 8 °C km^sup -1,^ which may indicate that the thermal structure of the subduction channel remained unchanged up to 35 Ma.

(4) The exhumation paths are all characterized by a continuous cooling, as evidenced by the T-t diagrams. Temperatures dropped from their peak to c. 300-350 °C (closure temperature for Ar in micas) in less than 10 Ma, which converts to cooling rates of 20-40 °C Ma^sup -1^.

(5) P-t paths during the Eocene are characterized by steep slopes, and therefore rapid exhumation. The Schistes Lustrés unit was exhumed first, and the Dora Maira UHP unit last, at minimum rates of 1-10 mm a^sup -1 ^assuming a lithostatic pressure gradient. Ar-Ar ages obtained on detrital white micas from Oligocene sediments of the Piemont basin that sample the metamorphic western Alps (Carrapa et al. 2003) define two peaks, c. 45 Ma and c. 38 Ma, and may represent the exhumation of the Piemont-Liguria units first (Schistes Lustrés, Monviso) followed by the Dora Maira UHP unit.

It should be emphasized that in the western Alps, the Dora Maira UHP unit appears to be an end-member in the P-T-t paths. The peak metamorphic conditions are the highest, the age of metamorphism is the youngest, and the exhumation is the most rapid. It represents the latest tectonic unit that we now see that benefited from the near steady-state dynamics of the subduction channel. We do not yet know if the history of the Dora Maira UHP unit can be extrapolated to the whole Dora Maira unit.

Oligocene to present day (34-0 Ma): a period of slow exhumation

The period 34-30 Ma (early Oligocene) saw the end of rapid exhumation in the SW Alps. From this time onward, zircon and apatite fission-track data (Schwartz 2002) record cooling at a mean rate of c. 10 °C Ma^sup -1^, and a slow exhumation (

The T-t data also indicate that the Monviso unit passed through the 250 °C and 100 °C isotherms somewhat later than the Schistes Lustrés. Although it is the youngest HP unit, the Dora Maira UHP unit apparently reached the 250 °C isotherm first at 30 Ma.

Foreland basin evolution

Across the external Alpine chains of SE France, just under 2 km of Palaeogene to Neogene synorogenic sediments are preserved in a series of isolated outliers. These sediments record a diachronous marine transgression that migrated toward the WNW-NW during the mid- to late Eocene (for review see Ford et al. 1999; Ford & Lickorish 2004; Joseph & Lomas 2004). Shallow marine carbonates (Calcaires Nummulitiques) are over-lain by foraminiferal marls (Marnes à Globigérines) recording a diachronous deepening of the sediment-starved basin. Sediment supply increased during the latest Priabonian and early Rupelian as clastic turbidites (Grès d’Annot) were supplied from the exhuming Sardinia-Corsica block to the south and later by the Maures-Esterels massif (Joseph & Lomas 2004). These turbidites were deposited in SE-NW-oriented synclinal sub-basins (Elliott et al. 1985; Du Fornel et al. 2004). The area was overthrust by the Embrunais-Ubaye nappes (Kerckhove 1969) toward the end of the Rupelian (around 30 Ma). Sedimentation (mainly fluvial-alluvial, up to 600m) was then limited to small structurally controlled basins (e.g. Barrême, Dévoluy, Fig. 1) to the west of the Embrunais-Ubaye nappes (Evans & Elliott 1999). From the Burdigalian to the Pliocene more than 2000 m of marine and continental clastic sediments were deposited in the Valensole Basin to the west of the frontal Digne Thrust.

The Tertiary basin history of SE France is correlated with that of the North Alpine Foreland Basin to reconstruct the evolution of the foreland basin around the western Alpine arc (Fig. 4). The map in Figure 4, updated from Ford & Lickorish (2004) using data from Varrone & Clari (2003) and Kempf & Pfiffner (2004), shows the progressive migration of the outer limit of the foreland basin. SW-NE shortening has been restored in SE France and north-south to WNW-ESE shortening has been restored in the central Alps. A major change in basin dynamics can be detected during the Rupelian.

Eocene (55-34 Ma): broad underfilled flexural basin

During the Eocene the northern limit of the underfilled marine basin (Fig. 4) migrated toward the N-NW across the European plate. A general rate of 9-10mm a^sup -1^ was estimated by Ford & Lickorish (2004) for the Eocene, and Kempf & Pfiffner (2004) provided a more detailed analysis in the Central Swiss Alps suggesting an initial slow rate (1-2 mm a^sup -1^) in the Palaeocene and early Eocene followed by a more rapid migration (20 mm a^sup -1^). The pre-Lutetian Alpine foreland basin did not reach the SW external Alps; however, a transgressive Nummulitic series of early Eocene to Ypresian age is preserved in the Solaro basin in northern Corsica (Waters 1990). Therefore, based on sparse data from the central Alps and Corsica, the Early Eocene foreland basin is speculatively represented as a north- to NW-migrating basin around the subduction-accretion orogen. Around 37-34 Ma the orientation of the transgressive coastline of the foreland basin changed from SSE-NNW to ESE-WNW (Kempf & Pfiffner 2004). From Lutetian to Priabonian time (45-34 Ma) the westward closure and migration of the foreland basin was recorded across SE France and can be traced into the central Alps. The deepening-upward stratigraphy of the Nummulitic series (Eocene-Rupelian) is remarkably consistent around the Alpine arc (Sinclair 1997) and can be modelled as a migrating flexural basin (Ford et al. 1999). Low sediment supply is interpreted to indicate low relief in the orogen. Flexure of the European plate was therefore not generated by a topographic load but more probably by the negative buoyancy of the subducting plate. Turbidites were supplied to the basin from the late Priabonian onward, indicating increasing relief to the south. These sediments gradually filled the basin to the end of the Rupelian (Joseph & Lomas 2004).

Oligocene-present day (34-0 Ma): end of flexural basin in SE France, overfilled flexural basin to the north of the Alps

After the emplacement of the Embrunais-Ubaye nappes at the end of the Rupelian, no further regional accommodation space was created in SE France (west of the Alps) by lithospheric flexure. Instead, sediment locally accumulated in small tectonically controlled basins (e.g. Barrême).

North of the Alps, however, subsidence and sediment supply increased considerably in the North Alpine Foreland Basin (4 km thickness; Fig. 4). This overfilled basin continued to migrate northward at the same rate until the early Miocene (Aquitanian), when it slowed considerably. This basin closed off to the west at Chambéry (C in Fig. 4). A high sediment supply indicates high orogen relief (Schlunegger et al. 1997).

Palaeogeographical reconstructions of the western Alpine orogen

The western Alpine arc developed as a result of the collision of the Adriatic plate with the European plate. Palaeomagnetic data (Dewey et al. 1989; Rosenbaum el al. 2002b) as well as stretching lineations in metamorphic rocks (Choukroune et al. 1986; Schmid & Kissling 2000) indicate a change in plate motion direction during the Tertiary from north-south to NW-SE. This change has been dated at 20 Ma by Rosenbaum & Lister (2005) and at 38 Ma by Dewey et al. (1989). The motion of the Adriatic plate on our palaeogeographical maps is in accordance with the second hypothesis. Following Schmid & Kissling (2000) we restore the Insubric Line as the northern margin of the rigid Adriatic plate. Palaeomagnetic data from the Brianconnais domain of the SW Alps indicate that significant late Tertiary anticlockwise rotation affected internal tectonic units with respect to stable Europe (Thomas et al. 1999; Collombet et al. 2002). In contrast, late anticlockwise rotations in the external zones are localized and relatively minor (Aubourg & Chabert-Pelline 1999) and are not considered here. To incorporate these rotational components, internal and external geometries are represented in both cross-section and map view (Figs 5 and 6). Construction of palaeogeographical maps (Fig. 5) involved integration of the data presented above with published plate reconstructions and tectonic models of principally Schmid et al. (1996, 1997), Stampfli & Marchant (1997), Collombet et al. (2002) and Schmid & Kissling (2000). The Dora Maira unit is shown as a star on cross-sections and maps. The cross-sections in Figure 6 are not restorations of the present-day cross-section (Fig. 2) but instead are intended principally to show the trajectories of internal units through time. Based on Collombet et al. (2002), we estimate that the internal zones on our cross-section have rotated through 90° since the early Eocene. Therefore the first three cross-sections (Ypresian, Priabonian and Rupelian) are oriented NW-SE whereas the last (Burdigalian) is oriented NE-SW. Although horizontal distances and depths are respected in the cross-sections and correspond to those on the maps, the geometries of internal nappes is largely speculative as there is little control on present-day deep structure in this area.

Eocene (55-34 Ma)

The Ypresian palaeogeographical map (Fig. 5a) shows the Adriatic plate moving northward with respect to a fixed Europe. The European ocean-continent transition was subducting obliquely below the Adriatic plate. The curved subduction zone passed into a poorly constrained north-south sinistral transform plate boundary to the SW. The subduction complex comprised an accretionary prism, probably of Helminthoid Flysch, overlying the subduction channel. To the north and west the flexural basin was migrating rapidly across the European foreland. The Dora Maira UHP unit was positioned at the southern limit of the European passive margin (Figs 5a and 6a). This model contrasts markedly with that of Stampfli & Marchand (1997) in which the Dora Maira formed part of the Adriatic microplate margin.

The Ypresian cross-section (Fig. 6a), oriented NW-SE, cuts through the transpressive margin on the NW side of the Adriatic plate. Although no evidence of an orogenic lid is preserved today, an early minor Adriatic lid above the subduction channel is drawn to limit the size of the subduction prism. The contact between the Adriatic plate and the subduction channel is shown as a synthetic normal fault (as in the models of Chemenda et al. 1996). Slices of Adriatic (Austroalpine) material may have been detached and subducted (but not exhumed to surface) in a similar way to that recorded by the metamorphic evolution of the Sesia and Dent Blanche units (Fig. 1) situated just to the north of our cross-section.

During the Eocene, significant convergence is required to subduct all the internal units to HP conditions assuming a lithostatic pressure gradient. Between 50 Ma and 35 Ma (Figs 5a,b and 6a,b), 195 km of north-south convergence is estimated to have occurred in the central and western Alps (Schmid et al. 1996), giving a north-south plate convergence rate of 13 mm a^sup -1^. A component of NW-SE convergence of 138 km is therefore estimated along our section line. During the Ypresian, slices of Schistes Lustrés and ophiolites were already subducted to HP conditions (Fig. 3). As the edge of the European passive margin (Dora Maira UHP unit) was just entering the subduction channel, it is reasonable to estimate that it was subducted down to 100km depth (assuming lithostatic pressure gradients) in 15Ma (50-35 Ma) in a subduction channel dipping at 36° toward the SE and with a SE-directed subduction component of 11 mm a^sup -1^, which is compatible with the north-south plate convergence rate of Schmid et al. (1996).

The cross-section for the Priabonian (Fig. 6b) shows the Dora Maira unit at maximum depth whereas the Schistes Lustrés and ophiolitic units were already exhumed to relatively shallow levels in the subduction channel (

The shape and migration of the early foreland basin reflects the northward migration of the Adriatic plate (Fig. 5a). The flexural basin reached SE France in the Lutetian and continued to migrate northward. During the Bartonian and Priabonian, the migration direction changed to NW (Fig. 5b). Further out in the foreland the West European rift system became active in the Priabonian (Séranne 1999).

Oligocene-present day (34-0 Ma)

At around 35 Ma the motion vector of the Adriatic microplate with respect to Europe changed from northward to northwestward (305°; Schmid et al. 1996). The SW-NE-striking subduction channel on the western side of Adria thus became a zone of frontal subduction. Plate convergence slowed considerably in the early Oligocene to 5 mm a^sup -1^ (Schmid et al. 1996). We show a reconstruction at 30 Ma to illustrate the ‘Dora Maira problem’ (Fig. 5c). By this time P-T-t data indicate that the Dora Maira UHP unit had been exhumed to within 10-20 km of the surface (assuming lithostatic pressure). To achieve this, the unit must have moved horizontally 124 km and vertically 90 km within the adopted subduction channel geometry between 35 and 30 Ma. However, NW-directed plate convergence for this period is estimated to have been only 25 km using the rate of 5 mm a^sup -1^. Therefore, forces other than plate convergence forces must be evoked to exhume this unit. Figure 6c shows the nappe stack in the late Rupelian, just before emplacement of the Ivrea mantle wedge (Adriatic mantle lithosphere) The cross-section illustrates that between 35 and 30 Ma, the Dora Maira UHP unit was effectively ‘injected’ into the already exhumed nappe stack near the top of the subduction channel. Based on a similar evolution further north, we propose that the whole nappe stack was backthrust onto the Adriatic crust to create the observed thrust contact. This contact was then sealed by Oligocene deposits and underwent continuous subsidence during the Neogene. From the Oligocene to the present slow and continuous erosion of the HP and UHP units of the internal Alps also supplied sediment with a uniform ^sup 40^Ar/^sup 39^Ar signature to the Tertiary Piement basin in NW Italy (Barbieri et al. 2003; Carrapa et al. 2003). Therefore the structure of the western internal nappes changed very little after this time.

Between 30 Ma and 15 Ma, around 68 km of NW convergence occurred in the western and central Alps at a rate of 4.5 mm a^sup -1^ (Schmid et al. 1996). At the same time, the Adriatic plate rotated 20° anticlockwise around an axis close to Turin (Schmid & Kissling 2000; see Collombet et al. 2002, for discussion). The Ivrea body is generally located at depth at the front of the Adriatic plate during this late collisional phase (Fig. 5d; e.g. Stampfli & Marchand 1997). During anticlockwise rotation and NW convergence the Ivrea body was wedged below the internal zones of the SW Alps (Fig. 6d). However, no change in the slow exhumation of internal units can be correlated with this deep crustal wedging. Whereas the Insubric Line records dextral displacements during the Oligocene and Miocene (Schmid et al. 1989), the contact between the Adriatic crust and internal Alpine units west of Turin was sealed from Oligocene time onward. It is proposed therefore that the 68 km NW convergence was accommodated by sinistral transpression within the internal units between the Dora Maira and the western boundary of the internal zone (shaded areas in Fig. 5c and d).


Exhumation processes in the SW Alps

Exhumation processes during the Eocene were due to subduction channel dynamics, which are now well described in numerical, analogue and conceptual models (e.g. Platt 1986, 1993; Fry & Barnicoat 1987; Henry et al. 1993; Chemenda et al. 1996; Burov et al. 2001; Ernst 2001; Gerya et al. 2002). Vertical exhumation rates for the Schistes Lustrés and Monviso ophiolitic unit are estimated at around 1-5 mm a^sup -1^ (Fig. 3), which is compatible with (slower than) the estimated vertical component of the subduction rate (8 mm a^sup -1^ assuming a convergence rate of 11 mm a^sup -1^ and a subduction angle of 36°). Rapid exhumation involved complex stacking of tectonic units within the subduction channel with both normal and inverse tectonic contacts. Because maximum P-T conditions vary within a single tectonic unit (e.g. within the Monviso unit or the Schistes Lustrés), and P-T conditions overlap between tectonic units, the size of tectonic slices in the subduction channel was not that of the whole unit but rather that of the smaller subunits observed today (e.g. Monviso is made up of several slices). The Dora Maira UHP unit was the last to be exhumed and at a rate of at least 10 mm a^sup -1^ (Fig. 3), which is higher than the vertical component of 4 mm a^sup -1^ assuming a subduction rate of 5 mm a^sup -1^. This special case is discussed further below.

Subduction was accompanied by the creation of little or no relief, as is recorded by the underfilled foreland basin. Erosion was therefore not a major exhumation agent during this stage. The absence of a significant topographic load also implies that flexure of the European plate was generated by subduction forces. This may be the case for flexural basins in other orogens that formed early in the collision process.

During the early Oligocene there was a major change in P-T-t paths. The observed decrease in the P-T path slope for each unit (Fig. 3a) is that expected during the exhumation because of the vertical thermal structure of the crust with the gradient increasing upward toward the Earth’s surface. But it may also reflect an increase of the thermal gradient through time. The P-1 diagram (Fig. 3c) presents a change in slope at around 30 Ma corresponding to a sharp decrease in the vertical component of the exhumation rate. This can be interpreted to mean that either the rock trajectories in the subduction channel had a constant velocity but became more horizontal toward the surface or that the orientation of the trajectories remained constant but their velocity decreased through time, or both (Duchêne et al. 1997b). It is important to note that only the second scenario would indicate a major change in orogen dynamics at around 30 Ma, which corresponds to changes in the plate movement vector proposed by Schmid & Kissling (2000).

From the Oligocene onward, erosion was probably the principal exhumation process, as present-day erosion rates from the main rivers more or less match required exhumation rates (Milliman & Meade 1983). Sediments eroded from the SW Alps began to accumulate in the Po basin from Oligocene times onward (Barbieri et al. 2003; Carrapa et al. 2003). This contrasts with the subduction phase, when erosion rates were very low but exhumation rates were 10 times higher. Major relief was created and frontal flexure of the overfilled North Alpine Foreland Basin was generated by subduction, and sedimentary and topographic loads. In contrast to the central Alps, the external zone of the SW Alps did not accommodate significant shortening during this period nor is there a record of active lithospheric flexure. So in the SW Alps, no major tectonic processes need be invoked for post early Oligocene exhumation.

Exhumation of the Dora Maira UHP unit: a special case?

The transition from subduction to collision is marked by the rapid subduction and exhumation of the Dora Maira UHP unit. Exhumation of this unit effectively ceased in the late Oligocene as the eastern margin began to subside and was progressively onlapped by Po Basin sediments. The subduction of Dora Maira at c. 35 Ma is in accordance with the reconstruction of plate convergence if we consider it as a distal part of the European margin. However, its exhumation cannot be explained by steady-state subduction channel dynamics because not only exhumation rates but also lateral displacement rates are much higher than those generated by plate convergence. This inconsistency can in part be resolved if the UHP in Dora Maira is considered as due to tectonic overpressure. At present, UHP is proven only in a tectonic slice of 40 km^sup 2^ by 1 km thick. It is reasonable to envisage that a local overpressure could develop within such a small volume (Petrini & Podladchikov 2000). Assuming overpressure developed at a maximum depth of 50 km at 35 Ma, the displacement rate during the exhumation is estimated at 16 mm a^sup -1^, which is in accordance with the estimated convergence rates of Dewey et al. (1989) at c. 35-30 Ma. This model could explain why calculated eclogitic P-T conditions are lower in the other Dora Maira subunits. However, the timing of the maximum subduction of these subunits is not constrained. Alternatively, additional mechanisms may have been active during the exhumation to enhance lateral and vertical movements. Slab breakoff could explain the accelerated vertical movement, but not the lateral component. A higher buoyancy for Dora Maira continental rocks compared with other parts of the subduction complex could lead to its movement as an isolated slice relative to surrounding material. Finally, as shown by the palaeogeographical reconstructions (Fig. 5), the Dora Maira UHP unit approached the transpressive western limit of the Adriatic plate at c. 35 Ma. The incorporation of the UHP unit into the transpressive zone may have laterally constricted the subduction channel and thus accelerated extrusion of its constituent material.

Regional significance of Eocene-Oligocene transition

In the central Alps, a major change in orogen dynamics occurred in the early Oligocene (34-30 Ma) with emplacement of the Bergell granodiorite, initiation of dextral slip and backthrusting of internal units along the Insubric Line. In the Oligocene, emplacement of the external (Helvetic-Dauphinois) units accommodated over 100 km of NW-WNW-directed shortening associated with thickening of the orogenic wedge and creation of substantial relief. Frontal flexure of the European plate continued to migrate northwestward as recorded by the overfilled North Alpine Foreland Basin.

This major change in Alpine dynamics at the beginning of the Oligocene has been variably attributed to clogging of the subduction system by stacking of tectonic units or by arrival of normal thickness crust into the subduction zone (e.g. Stockmal et al. 1986; Schmid et al. 1989; Stampfli et al. 2002) possibly followed by slab breakoff (von Blanckenburg & Davies 1995; Sinclair 1997). Across the whole Mediterranean region, the early Oligocène was marked by the reorganization of plate movements (Stampfli et al. 2002) and it has been suggested that blockage of the Alpine subduction was followed by the creation of a new NNW-dipping subduction zone further south (Rosenbaum et al. 2002a).


A major change in Alpine dynamics at the beginning of the Oligocene has been recognized in foreland and internal zone evolution of the SW Alps.

Eocene subduction-accretion phase (50-34 Ma)

While the Adriatic plate moved northward with respect to a fixed Europe at a rate of 13 mm a^sup -1^, the European ocean-continent transition in SW Alps was subducting obliquely below the Adriatic plate. The sedimentary record and the P-T-t path of metamorphic rocks indicate low relief and rapid exhumation of metamorphic rocks derived from oceanic crust and overlying sediments. Exhumation of HP and UHP rocks is not controlled by erosion at this stage but is best explained by steady-state subduction channel dynamics.

Oligocene to present-day collision phase (34-0 Ma)

The motion of the Adriatic microplate with respect to Europe changed from north-directed to NW-directed (Schmid et al. 1996). The internal SW Alps became accordingly a zone of sinistral transpression pinched between the Adriatic and European plates. Plate convergence slowed considerably to 5 mm a^sup -1^. This period corresponds to high orogen relief and high erosion rates, as indicated by stratigraphy in the North Alpine Foreland Basin. Erosion can account for the slow exhumation rates observed in the internal zone at this stage.

The transition between these two phases is marked by the subduction and exhumation of the UHP unit of Dora Maira. If the maximum subduction depth of this unit was 100 km (which assumes purely lithostatic pressure), the required vertical and horizontal exhumation rates exceed those generated by plate motion. This discrepancy may be resolved by evoking additional stresses, which may have been generated by increasing lateral constriction within the transpressive plate boundary, slab breakoff or high density constrasts within the subduction channel, or any combination of these. Alternatively, Dora Maira was never subducted to 100 km but the ultrahigh pressure was generated by significant local overpressure.

Fieldwork was funded by the ‘Federation de Recherche EST’ of Nancy. We thank P. Henry, S. Schmid and Edi Kissling for lively and fruitful discussions on the deep structure of the western Alps. We thank N. Fry and an anonymous reviewer for challenging reviews. This paper is CRPG Publication 1798.


AGARD, P., JOLIVET, L. & GOFFÉ, B. 2001a. Tectonometamorphic evolution of the Schistes Lustrés complex: implications for the exhumation of HP and UHP rocks in the western Alps. Bulletin de la Société Géologique Je France, 172, 617-636.

AGARD, P., VIDAL, O. & GOFFÉ, B. 2001b. Interlayer and Si content of phengite in HP-LT carpholite-bearing metapelites. Journal of Metamorphic Geology, 19, 477-493.

AUBOURG, C. & CHABERT-PELLINE, C. 1999. Neogene remagnetization of normal polarity in the Late Jurassic black shales from the Subalpine chains (French Alps): evidence for late anticlockwise rotations. Tectonophysics, 308, 473-486.

BALLÈVRE, M., LAGABRIELLE, Y. & MERLE, O. 1990. Tertiary ductile normal faulting as a consequence of tithospheric stacking in the western Alps. In: ROURE, F., HEITZMANN, P. & POLINO, R. (eds) Deep Structure of the Alps. Mémoires de la Societé Géologique de France, 156, 227-236.

BARBIERI, C., CARRAPA, B., DI GIULIO, A., WIJBRANS, J. & MURRELL, G.R. 2003. Provenance of Oligocene syn-orogenic sediments of the Ligurian Alps (NW Italy): inferences on belt age and cooling history. International Journal of Earth Sciences, 92, 758-778.

BIGOT-CORMIER, F., POUPEAU, G. & SOSSON, M. 2000. Denudations différentielles du massif cristallin externe alpin de l’Argentera (Sud-est de la France) rélévées par thermochronologie traces de fission (apatites, zircons). Comptes Rendus de l’Académie des Sciences, Sciences de la Terre et des Planètes, 330, 363-370.

BIGOT-CORMIER, F., SAGE, F. & SOSSON, M. ET AL. 2004. Déformations pliocènes de la marge nord-Ligure (France); les conséquences d’un chevauchement crustal sud-alpin. Bulletin de la Société Géologique de France, 175, 197-211.

BUROV, E., JOLIVET, L., LE POURHIET, L. & POLIAKOV, A. 2001. A thermomechanical model of exhumation of HP and UHP metamorphic rocks in alpine mountain belts. Tectonophysics, 342, 113-136.

CARRAPA, B., WIJBRANS, J. & BERTOTTI, G. 2003. Episodic exhumation in the Western Alps. Geology, 31, 601-604.

CASSANO, E., ANELLI, L., FICHERA, R. & CAPPELLI, V. 1986. Pianura Padana: Interpretazione Integrata di Dali Geofisici e Geologici. (Po River Plain; Integrated Interpretation of Geophysical and Geological Data J. AGIP, Rome.

CERIANI, S., FUGENSCHUH, B. & SCHMID, S.M. 2001. Multi-stage thrusting at the ‘Penninic Front’ in the Western Alps between Mont Blanc and the Pelvoux Massif. International Journal of Earth Sciences, 90, 685-702.

CHEMENDA, A.I., MATTAUER, M. & BOKUN, A.N. 1996. Continental subduction and a mechanism for exhumation of high-pressure metamorphic rocks: a new modelling and field data. Earth and Planetary Science Letters, 143, 173-182.

CHOPIN, C. 1984. Coesite and pure pyrope in high-grade blueschists of the Western Alps: a first record and some consequences. Contributions to Mineralogy and Petrology, 86, 107-118.

CHOPIN, C., HENRY, C. & MICHARD, A. 1991. Geology and petrology of the coesite-bearing terrain, Dora Maira massif, Western Alps. European Journal of Mineralogy, 3, 263-291.

CHOUKROUNE, P., BALLEVRE, M., COBBOLD, P.R., GAUTIER, Y., MERLE, O. & VUICHARD, J.-P. 1986. Deformation and motion in the western Alpine Arc. Tectonics, 5, 215-226.

CLIFF, R.A., BARNICOAT, A.C. & INGER, S. 1998. Early Tertiary eclogite facies metamorphism in the Monviso Ophiolite. Journal of Metamorphic Geology, 16, 447-455.

COLLOMBET, M., THOMAS, J.C., CHAUVIN, A., TRICART, P., BOUILLIN, J.-P. & GRATIER, J.-P. 2002. Counterclockwise rotation of the western Alps since the Oligocene: new insights from paleomagnetic data. Tectonics, 21, 14.1-14.15.

DEBELMAS, J. & LEMOINE, M. 1970. The western Alps; palaeogeography and structure. Earth-Science Reviews, 6, 221-256.

DEWEY, J.F., HELMAN, M.L., TURCO, E., HUTTON, D.W.H. & KNOTT, S.D. 1989. Kinematics of the western Mediterranean. In: COWARD, M.P., DIETRICH, D. & PARK, R.G. (eds) Alpine Tectonics. Geological Society, London, Special Publications, 45, 265-284.

DUCHÊNE, S., BLICHERT-TOFT, J., LUAIS, B., LARDEAUX, J.M., TÉLOUK, P. & ALBARÈDE, F. 1997a. The Lu-Hf dating of Alpine eclogites. Nature, 387, 586-589.

DUCHÊNE, S., LARDEAUX, J.M. & ALBARÈDE. F. 1997b. Exhumation of eclogites: insights from depth-time path analysis. Tectonophysics, 280, 125-140.

DU FORNEL, E., JOSEPH, P. & DESAUBLIAUX, G. ET AL. 2004. The southern Grès d’Annot outcrops (French Alps): an attempt at regional correlation. In: JOSEPH, P. & LOMAS, S.A. (eds) Deep-water Sedimentation in the Alpine Foreland Basin of SE France: New Perspectives on the Grès d ‘Annot and Related Systems. Geological Society, London, Special Publications, 221, 137-160.

ELLIOTT, T., APPS, G., DAVIES, H., EVANS, M., GHIBAUDO, G. & GRAHAM, R.H. 1985. A structural and sedimentological traverse through the Tertiary foreland basin of the external Alps of South-East France. In: ALLEN, P., HOMEWOOD, P. & WILLIAMS, G. (eds) International Symposium on Foreland Basins. International Association of Sedimentologists, Excursion guide book, Fribourg, 39-73.

ERNST, W.G. 2001. Subduction, ultrahigh-pressure metamorphism, and regurgitation of buoyant crustal slices-implications for arcs and continental growth. Physics of the Earth and Planetary Interiors, 127, 253-275.

EVANS, M.J. & ELLIOTT, T. 1999. Evolution of a thrust sheet-top basin: the Tertiary Barrême basin, Alpes-de-Haute-Provence, France. Geological Society of America Bulletin, 111, 1617-1643.

FORD, M. & LICKORISH, H. 2004. Foreland basin evolution around the western Alpine Arc. In: JOSEPH, P. & LOMAS, S.A. (eds) Deep-water Sedimentation in the Alpine Basin of SE France: New Perspectives on the Ores d’Annot and Related Systems. Geological Society, London, Special Publications, 221, 39-63.

FORD, M., LICKORISH, W.H. & KUSZNIR, N.J. 1999. Tertiary foreland sedimentation in the southern Subalpine chains, SE France: a geodynamic analysis. Basin Research, 11, 315-336.

FRY, N. 1989. Southwestward thrusting and tectonics of the western Alps. In: COWARD, M.P., DIETRIC-H, D. & PARK, R.G. (eds) Alpine Tectonics. Geological Society, London, Special Publications, 45, 83-109.

FRY, N. & BARNICOAT, A.C. 1987. The tectonic implications of high-pressure metamorphism in the western Alps. Journal of the Geological Society, London, 144, 653-659.

GEBAUER, D., SCHERTL, H.P., BRIX, M. & SCHREYER, W. 1997. 35 Ma old ultrahigh-pressure metamorphism and evidence for very rapid exhumation in the Dora Maira Massif, Western Alps. Lithos, 41, 5-24.

GERYA, T.V., STOCKHERT, B. & PERCHUK, A.L. 2002. Exhumation of high-pressure metamorphic rocks in a subduction channel: a numerical simulation. Tectonics, 21, 6-1-6-19.

GRADSTEIN, F.M. 2004. A new geological time scale with special reference to Precambrian and Neogene. Episodes, 27, 2.

HENRY, C., MICHARD, A. & CHOPIN, C. 1993. Geometry and structural evolution of ultra-high-pressure and high-pressure rocks from the Dora Maira massif, Western Alps, Italy. Journal of Structural Geology, 15, 965-981.

JOSEPH, P. & LOMAS, S.A. 2004. Deep-water sedimentation in the Alpine Foreland Basin of SE France: new perspectives on the Grès d’Annot and related systems-an introduction. In: JOSEPH, P. & LOMAS, S.A. (eds) Deep-water Sedimentation in the Alpine Foreland Basin of SE France: New Perspectives on the Grès d’Annot and Related Systems. Geological Society, London, Special Publications, 221, 1-16.

KEMPF, O. & PFIFFNER, O.A. 2004. Early Tertiary evolution of the North Alpine Foreland Basin of the Swiss Alps and adjoining areas. Basin Research, 16, 549-568.

KERCKHOVE, C. 1969. La ‘zone du Flysch’ dans les nappes de l’Embrunais-Ubaye (Alpes occidentales). Géologie Alpine, 45, 5-204.

LEFÈVRE, R. & MICHARD, A. 1976. Les nappes Briançonnaises internes et ultra-briançonnaises de la bande d’Acceglio (Alpes franco-italiennes). Une étude structurale dans la faciès des schistes bleues à jadéite. Sciences Géologiques Bulletin, Strasbourg, 29, 183-222.

LICKORISH, W.H. & FORD, M. 1998. Evolution of the Digne thrust system, southern Subalpine chains: kinematics and timing of deformation. In: MASCLE, A., PUIGDEFÀBREGAS, C., LUTERBACHER, H.P. & FERNANDEZ, M. (eds) Cenazoic Foreland Basins of Western Europe. Geological Society, London, Special Publications, 134, 189-211.

LIPPITSCH, R., KISSLING, E. & ANSORGE, J. 2003. Upper mantle structure beneath the alpine orogen from high resolution teleseismic tomography. Journal of Geophysical Research, 108(B8), 2376.

MERLE, O. & BRUN, J.P. 1984. The curved translation path of the Parpaillon Nappe (French Alps). Journal of Structural Geology, 6, 711-719.

MESSIGA, B., KIENAST, R., REBAY, G., RICCARDI, P. & TRIBUZIO, R. 1999. Cr-rich magnesiochloritoid eclogites from the Monviso ophiolites (Western Alps, Italy). Journal of Metamorphic Geology, 17, 287-299.

MICHARD, A. 1977. Charriages et métamorphisme haute pression dans les Alpes cottiennes méridionales: à propos des schistes à jadéite de la bande d’Acceglio. Bulletin de la Société Géologique de France (7), XIX, 883-892.

MICHARD, A., CHOPIN, C. & HENRY, C. 1993. Compression versus extension in the exhumation of the Dora Maira coesite-bearing unit, western Alps, Italy. Teclonophysics, 221, 173-193.

MILLIMAN. J.D. & MEADE. R.H. 1983. World-wide delivery of river sediments to the oceans. Journal of Geology, 91. 1-21.

MONIÉ, P. & CHOPIN. C. 1991. ^sup 40^Ar/^sup 39^Ar dating in coesite-bearing and associated units in the Dora Maira massif, western Alps. European Journal of Mineralogy, 3, 239-262.

MONIÉ, P. & PHILIPPOT, P. 1989. Mise en évidence de l’âge éocène moyen du métamorphisme du haute-pression dans la nappe ophiolitique du Montviso (Alpes Occidentales) par la méthode ^sup 39^Ar-^sup 40^Ar. Comptes Rendus de l’Académie des Sciences, Série II, 309, 245-251.

MOSCA, P. 2006. Neogene basin evolution in the western Po plain (NW Italy): insights from seismic interpretation, subsidence analysis and low temperature (U-Th)/He thermochronology. PhD thesis, Vrije Universiteit of Amsterdam.

PAUL, A., CATTANEO, M., THOUVENOT, F., SPALLAROSSA, D., BETHOUX, N. & FRECHET, J. 2001. A three-dimensional crustal velocity model of the southwestern Alps from local earthquake tomography. Journal of Geophysical Research, B, 106, 19367-19389.

PETRINI, K. & PODLACHIKOV, Y. 2000. Lithospheric pressure-depth relationship in compressive regions of thickened crust. Journal of Metamorphic Geology, 18, 67-77.

PHILIPPOT, P. 1990. Opposite vergence of nappes and crustal extension in the French-Italian western Alps. Tectonics, 9, 1143-1163.

PLATT, J.P. 1986. Dynamics of orogenic wedges and the uplift of high pressure metamorphic rocks. Geological Society of America Bulletin, 97, 1037-1053.

PLATT, J.P. 1993. Exhumation of high-pressure rocks: a review of concepts and processes. Terra Nova, 5, 119-133.

REDDY, S.M., WHEELER, J. & BUTLER, R.W.H. ET AL. 2003. Kinematic reworking and exhumation within the convergent Alpine Orogen. Tectonophysics, 365, 77-102.

RITZ, F. 1991. Evolution du champ de contraintes dans les Alpes du Sud depuis la fin de l’Oligocène. Implications sismotectoniques. PhD thesis, Université de Montpellier II.

ROSENBAUM, G. & LISTER, G.S. 2005. The western Alps from Jurassic to Oligocene: spatio-temporal constraints and evolutionary reconstructions. Earth-Science Reviews, 69, 281-306.

ROSENBAUM, G., LISTER, G.S. & DUBOZ, C. 2002a. Reconstruction of the tectonic evolution of the western Mediterranean since the Oligocene. Journal of the Virtual Explorer, 8, 107-126.

ROSENBAUM, G., LISTER, G.S. & DUBOZ, C. 2002b. Relative motions of Africa, Iberia and Europe during Alpine orogeny. Tectonophysics, 359, 117-129.

RUBATTO, D. & HERMANN, J. 2001. Exhumation as fast as subduction? Geology, 29, 3-6.

RUBATTO, D.S. & HERMANN, J. 2003. Zircon formation during fluid circulation in ecolgites (Monviso, Western Alps): implications for Zr and Hf budjet in subduction zones. Geochemica et Cosmochimica Acta, 47, 2173-2187.

SCHLUNEGGER, F., JORDAN, T.E. & KLAPER, E.M. 1997. Controls of erosional denudation in the orogen on foreland basin evolution: the Oligocene central Swiss Molasse Basin as an example. Tectonics, 16, 823-840.

SCHMID, S.M. & KISSLING, E. 2000. The arc of the western Alps in the light of geophysical data on deep crustal structure. Tectonics, 19, 62-85.

SCHMID, S.M., AEBLI, H.R., HELLER, F. & ZINGG, A. 1989. The role of the Periadriatic Line in the tectonic evolution of the Alps. In: COWARD, M.C., DIETRICH, D. & PARK, R.G. (eds) Alpine Tectonics. Geological Society, London, Special Publications, 45, 153-162.

SCHMID, S.M., PFIFFNER, O.A., FROITZHEIM, N., SCHÖNBORN, G. & KISSLING, E. 1996. Geophysical-geological transect and tectonic evolution of the Swiss-Italian Alps. Tectonics, 15, 1036-1064.

SCHMID, S.M., PFIFFNER, O.A., SCHÖNBORN, G., FROITZHEIM, N. & KISSLING, E. 1997. Integrated cross-section and tectonic evolution of the Alps along the Eastern Traverse. In: PFIFFNER, O.A., LEHNER, P., HEITZMANN, P., MUELLER, S. & STECK, A. (eds) Deep Structure of the Swiss Alps: Results of NRP20. Birkhäuser, Basel, 289-304.

SCHWARTZ, S. 2002. La zone piémontaise des Alpes Occidentales: un paléo-complexe de subduction. Arguments métamorphiques, géochronologiques et structuraux. PhD thesis, Université Claude Bernard Lyon I.

SCHWARTZ, S., LARDEAUX, J.M., GUILLOT, S. & TRICART, P. 2000a. Diversité du métamorphisme éclogitique dans le massif ophiolitique du Monviso (Alpes occidentales, Italie). Geodinamica Acta, 13, 169-188.

SCHWARTZ, S., LARDEAUX, J.M. & TRICART, P. 2000b. La zone d’Acceglio (Alpes Cottiennes): un nouvel example de croûte continentale éclogitisée dans les Alpes occidentales. Comptes Rendus de l’Académie des Sciences, Sciences de la Terre et des Planètes, 330, 859-866.

SÉRANNE, M. 1999. The Gulf of Lion continental margin (NW Mediterranean) revisited by IBS: an overview. In: DURAND, B., JOLIVET, L., HORVÁTH, F. & SÉRANNE, M. (eds) The Mediterranean Basins: Tertiary Extension within the Alpine Orogen. Geological Society, London, Special Publications, 156, 15-36.

SINCLAIR, H.D. 1997. Tectono-stratigraphic model for underfilled peripheral foreland basins: an Alpine perspective. Geological Society of America Bulletin, 109, 324-346.

SOLARINO, S., KISSLING, E., CATTANEO, M. & EVA, C. 1997. Local earthquake tomography of the southern part of the Ivrea body, North-Western Italy. Eclogae Geologicae Helvetiae, 90, 357-364.

STAMPFLI, G.M. & MARCHANT, R.H. 1997. Geodynamic evolution of the Tethyan margins of the western Alps. In: PFIFFNER, O.A., LEHNER, P., HEITZMANN, P., MUELLER, S. & STECK, A. (eds) Deep Structure of the Swiss Alps: Results of NRP20. Birkhäuser, Basel, 223-239.

STAMPFLI, G.M., BOREL, G.D., MARCHANT, R. & MOSAR, J. 2002. Western Alps geological constraints on western Tethyan reconstructions. Journal of the Virtual Explorer, 8, 77-106.

STOCKMAL, G., BEAUMONT, C. & BOUTILIER, R. 1986. Geodynamic models of convergent margin tectonics: transition from rifted margin to overthrust belt and consequences for foreland basin development. AAPG Bulletin, 70, 181-190.

SUE, C. & TRICART, P. 1999. Late alpine brittle extension above the Frontal Pennine Thrust near Briançon, western Alps. Eclogae Geologicue Helvetiae, 92, 171-181.

TARDY, M., BETHOUX, N., LARDEAUX, J.M., PAUL, A. & THE ALPS WORKING GROUP, 1999. The Géofrance 3D project in the western Alps: a synthesis. Colloque Géofrance 3D (Lyon): résultats et perspectives. Documents BRGM, 293, 52-63.

THOMAS, J.C., CLAUDEL, M.E., COLLOMBET, M., TRICART, P., CHAUVIN, A. & DUMONT, T. 1999. First paleomagnetic data from the sedimentary cover of the French Penninic Alps: evidence for Tertiary counterclockwise rotations in the Western Alps. Earth and Planetary Science Letters, 171, 561-574.

TILTON, G.R., SCHREYER, W. & SCHERTL, H.P. 1991. Pb-Rb-Nd isotopic behaviour of deeply subducted crustal rocks from the Dora Maira Massif, Western Alps, Italy: what is the age of the ultrahigh-pressure metamorphism? Contributions to Mineralogy and Petrology, 108, 22-33.

TRICART, P., SCHWARTZ, S., SUE, C., POUPEAU, G. & LARDEAUX, J.M. 2001. La dénudation tectonique de la zone ultradauphinoise et l’invérsion du front briançonnais au sud-est du Pelvoux (Alpes occidentales): une dynamique miocène à actuelle. Bulletin de la Société Géologique de France, 172, 49-58.

TRICART, P., SCHWARTZ, S., SUE, C. & LARDEAUX, J.M. 2004. Evidence of synextension tilting and doming during final exhumation from analysis of multistage faults (Queyras Schistes Lustrés, Western Alps). Journal of Structural Geology, 26, 1633-1645.

VARRONE, D. & CLARI, P. 2003. Evolution stratigraphique et paleo-environnementale de la Formation à Microcodium et des Calcaires à Nummulites dans les Alpes Maritimes franco-italiennes. Geobios, 36, 775-786.

VON BLANCKENBURG, F. & DAVIES, J.H. 1995. Slab breakoff: a model for syncollisional magmatism and tectonics in the Alps. Tectonics, 14, 120-131.

WALDHAUSER, F., KISSLING, E., ANSORGE, J. & MUELLER, S. 1998. Three-dimensional interface modelling with two-dimensional seismic data; the Alpine crust-mantle boundary. Geophysical Journal International, 135, 264-278.

WALDHAUSER, F., LIPPITSCH, R., KISSLING, E. & ANSORGE, J. 2002. High-resolution teleseismic tomography of upper-mantle structure using an a priori three-dimensional crustal model. Geophysical Journal International, 150, 403-114.

WATERS, C.N. 1990. The Cenozoic tectonic evolution of Alpine Corsica. Journal of the Geological Society, London, 147, 811-824.

WHEELER, J., REDDY, S.M. & CLIFF, R.A. 2001. Kinematic linkage between internal zone extension and shortening in more external units in the NW Alps. Journal of the Geological Society, London, 158, 439-443.

Received 8 March 2005; revised typescript accepted 10 January 2006.

Scientific editing by Tim Needham


1 Centre de Recherches Pétrographiques et Géochimiques, CNRS-UPR 2300, 15, rue Notre Dame des Pauvres, BP 20, 54501 Vandoeuvre lès Nancy Cedex, France (e-mail:

2 Present address: Université de Savoie, Centre Interdisciplinaire Scientifique de la Montagne (CISM), Laboratoire Environnements, Dynamiques et Territoires de la Montagne (EDYTEM), CNRS-UMR 5204, Domaine Scientifique, F 73376 Le Bourget du Lac Cedex, France

3 Université Henri Poincaré Nancy 1, CNRS-UMR 7566, Géologie et Gestion des Ressources Minérales et Energétiques, BP 239, 54506 Vandoeuvre-lès-Nancy Cedex, France

Copyright Geological Society Publishing House Sep 2006

Provided by ProQuest Information and Learning Company. All rights Reserved