3D Structural and Thermal Modeling in the Po Valley Basin, Northern Italy

Turrini, C.; Ryan, P. J.; Bosica, Barbara; Shiner, Peter; Lacombe, Olivier; Roure, F.

doi:10.3997/2214-4609.201413095

Cited by 1 publication

(3 citation statements)

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“…Following the May 2012 Emilia earthquake, the analysis of the new seismological data, modeling of surface deformations, and seismotectonic interpretation of the existing subsurface data set have indisputably documented the activation of seismogenic thrusts within the Meso‐Cenozoic sedimentary covers while leaving open the scientific debate regarding a possible activation of faults involving the basement (among many other, Argnani et al, ; Bonini et al, ; Bonini et al, ; Carannante et al, ; Govoni et al, ; Lavecchia et al, ; Tizzani et al, ; Turrini et al, , , and references therein).…”

Section: Discussionmentioning

confidence: 99%

“…The Po Basin represents the foredeep, nowadays filled by Plio‐Pleistocene turbidite and deltaic sequences of both the Southern Alps and the Northern Apennines (e.g., Bertello et al, ; Boccaletti et al, ; Carminati, Doglioni, & Scrocca, ; Castellarin et al, ; Doglioni, ; Fantoni & Franciosi, , ; Ghielmi et al, , ; Pieri & Groppi, ; Turrini et al, , , ). It is a fast‐subsiding basin, with foredeep sediments syntectonically deposited both in isolated piggyback basins and in the prism foreland, well described by the geometry of the base of the Plio‐Pleistocene foredeep deposits shown in Figure (Consiglio Nazionale delle Ricerche, ).…”

Section: Geological Settingmentioning

confidence: 99%

“…Three different arcs have been recognized along the thrust front: the Monferrato, the Cremona, and the Ferrara arcs (see Consiglio Nazionale delle Ricerche, ). The accretionary prism front is seismically active (Albano et al, ; Benedetti et al, ; Boccaletti, Corti, & Martelli, ; Bonini et al, ; DISS Working Group, ; Govoni et al, ; Lavecchia et al, ; Michetti et al, ; Toscani et al, ; Turrini et al, ; Vannoli et al, , and references therein). Before the M L 5.9, 20 May 2012 Emilia earthquake, the area was characterized by low strain rate, which potentially indicates a greater likelihood for more numerous and larger earthquakes (Cuffaro et al, ; Doglioni et al, , ; Riguzzi et al, ).…”

Section: Introductionmentioning

confidence: 99%

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Structural and Stratigraphic Control on Salient and Recess Development Along a Thrust Belt Front: The Northern Apennines (Po Plain, Italy)

Livani

Scrocca

Arecco³

et al. 2018

JGR Solid Earth

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The external part of the Northern Apennines accretionary wedge in northern Italy is buried beneath its fast subsiding and asymmetric foreland basin in the Po Plain. It is characterized by a diffused noncylindrical geometry resulting in salients and recesses in the study area, namely, the Cremona salient, the Parma recess, and the Ferrara salient. The interpretation of borehole and seismic reflection data suggests that the thrust belt is characterized by thin‐skinned tectonic style. Two main décollement levels have been identified: a basal décollement located in the Upper Carnian units (San Giovanni Bianco Clay and Raibl Group) and a shallow décollement located in the late Eocene‐Oligocene formations (Gallare Marls). The décollement surfaces dip SSW toward the hinterland of the accretionary prism, parallel to the steep (>10°) regional monocline. The geometry of the seismically active Northern Apennines system of salients and recesses is essentially controlled by the interplay of two factors: (i) the lateral facies variations of the stratigraphic units hosting and controlling the location and depth of the décollement levels and (ii) the slope of the basal décollement. Salients occur where, due to the inherited variable stratigraphy of the Mesozoic‐Cenozoic Tethyan passive margin, the shaly formations hosting the two décollements are well developed allowing larger forward propagation of the thrust wedge. Recesses are instead associated to erosional‐nondepositional areas. Moreover, salients are more pronounced where the flexural behavior of the Adriatic subducting slab has generated a steeper geometry of the foreland monocline and consequently of the basal décollement.

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