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Deep Oil Plays in Po Valley:
Deformation and Hydrocarbon Generation in a Deformed Foreland*
By
M. Bello1 and R. Fantoni1
Search and Discovery Article #10042 (2003)
*Adapted from an extended abstract of presentation at AAPG Hedberg Conference, “Deformation History, Fluid Flow Reconstruction and Reservoir Appraisal in Foreland Fold and Thrust Belts,” May 14-18, 2002, Palermo – Mondello (Sicily, Italy).
1ENI – AGIP Division, Via Emilia 1 - 20097 San Donato Milanese (Milano) Italy
Introduction
In the western Po Valley, more than 5,000 meters deep, few gas and condensate fields are present in alpine compressional structures (Malossa type). Oil fields are found in Mesozoic extensional structures (Villafortuna-Trecate type); both these petroleum systems consist of Triassic reservoir and source rocks.
Po Valley oil plays in the Mesozoic series were first investigated in the early seventies with Valle Salimbene 1 well and the Malossa gas and condensate field discovery (Vaghi et al., 1979; Errico et al., 1979; Mattavelli and Margarucci, 1992). While the Alpine compressive structures were being explored (S. Bartolomeo, Seregna and Canonica oil discoveries), in the western Po Valley, a new exploration play was defined in the Mesozoic extensional structures only gently deformed during the alpine orogeny. The discoveries in this play occurred during the eighties with the Gaggiano (Schlumberger, ed., 1987; Bongiorni, 1987) and Villafortuna-Trecate oil fields, located respectively southwest and west of Milan (Figure 1).
The Malossa field has produced 30 Mbbls of condensate and more than 5000 x 103 MSTm3 of gas (from a reservoir 5300 meters deep). The Villafortuna-Trecate field, at the end of 2000, had produced 188 Mbbls of oil and more than 2000 MSTm3 of gas (from two reservoirs, 5700 and 6300 metres deep, respectively).
This work aims to prove that these plays may be pursued in some uninvestigated structures involved in the external part of the Apennines chain.
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uMalossa & Villafortuna-Trecate plays
uMalossa & Villafortuna-Trecate plays
uMalossa & Villafortuna-Trecate plays
uMalossa & Villafortuna-Trecate plays
uMalossa & Villafortuna-Trecate plays
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Geological SettingThe Po valley subsurface framework resulted from a Mesozoic extensional tectonic phase, developed in the western Tethys realm, followed mainly by Tertiary collisional tectonic phases (Figure 1). Sedimentation started during the Lower Triassic with continental to paralic siliciclastics, followed by a Middle Triassic carbonate depositional system, articulated in platforms and intra-platform basins filled with mixed siliciclastics and carbonate sediments. The Upper Triassic-Jurassic extensional phases caused the maximum deepening and widening of the north-south-trending pelagic basins (Bertotti et al.; 1993; Sarti et al., 1993). During the alpine orogenic phases, which began at the end of the Cretaceous, the Po Valley represented the foreland of the Southern Alps (Figure 1). Since then the foreland dipped northward and was progressively involved in south-verging compressional structures. The deformation involved the Mesozoic carbonates and the overlying syntectonic Tertiary siliciclastics. During the Pliocene and Quaternary, after the last South-alpine tectonic phase, the area was involved only in the Apennines deformation, which produced the southward dip of the entire foreland (see geological sections in Pieri and Groppi, 1981; Cassano et al., 1986). Malossa and Villafortuna-Trecate PlaysFrom a structural point of view these plays are the expression of the interference between a first extentional stage, which occurred in Late Triassic-Early Jurassic, and a later compressive stage (Late Cretaceous- Miocene).
Malossa
field
is located in the central sector of the Po Plain (Figure
1). Tectonic relief (structure) related to the Mesozoic extensional
phase and passively involved with a SW-verging alpine compressive
structure represents the The New Plays in the External Part of the Northern-Apennines ChainThe Mesozoic carbonate foreland units at the northern Apennine margin of the Po Valley have not been investigated until now. The hydrocarbon potential and the exploratory risk of the area were recently revaluated. The new interpretation, based first on a detailed structural analysis, highlights the presence of wide compressional structures at the southern margin of the Po Valley foreland (Ripalta deep and Asti nord plays--Figure 1). Both structures are located below the more external structural domains of the Northern Appennines. They consist of a multi-kilometric North-verging structures involving the foreland carbonate succession. The deformation geometries are characterised by thrusting of the inner part of the belt on a parautochthonous foreland (Figure 2). They are ramp anticlines with short forelimbs, flat crestal domains and long backlimbs. The consistency of the geological interpretations was tested by balancing and restoring representative sections obtained from depth converted regional seismic profiles. The kinematic reconstruction of the geological evolution provided the deformation and the source rock burial history from the Mesozoic tectonic setting to the present-day arrangement and allowed us to perform hydrocarbon-generation modelling. The comparison between the tectonic and hydrocarbon generation history permitted us to establish that these structures are related to Messinian-Lower Pliocene tectonic events and that they precede the age of hydrocarbon generation and expulsion from the source rocks present in the drainage area. The Asti nord play (Figures 1 and 2 [section B-B’]) could have a petroleum system similar to Villafortuna-Trecate and could drain a portion of the hydrocarbons produced in the regional synclines interposed between these structures and Villafortuna-Trecate fields. The Ripalta deep play (Figures 1 and 3) is located in the central Po valley just south of Malossa field, and due to the N-S trend of the Mesozoic feature the petroleum system is expected to be similar to the Malossa system.
Selected ReferencesBertotti, G., Picotti, V., Bernoulli, D., and Castellarin, A., 1993, From rifting to drifting: tectonic evolution of the Southalpine upper crust from the Triassic to the Early Cretaceous: Sedimentary Geology, v.86, no. 1/2, p. 53-76. Bongiorni, D., 1987, La ricerca di idrocarburi negli alti strutturali mesozoici della Pianura padana: l’esempio di Gaggiano: Atti Tic. S. Terra, v. 31, p. 125-141. Cassano, E., Anelli, L., Fichera, R., and Cappelli, V., 1986, Pianura Padana. Interpretazione integrata di dati geofisici e geologici: 73° Congr. Soc. Geol. It., 29 sett-4 ott. 1986, Roma, 27. Errico, G., Groppi, G., Savelli, S., and Vaghi, G.C., 1979, Malossa Field, deep discovery in Po Valley, in Giant Oil and Gas Field of the decade 1968-1978, A.A.P.G. Mem. 30, p. 525-538. Mattavelli, L., and Novelli, L., 1987, Origin of Po Basin hydrocarbons: Memoires Societé Geologique de France, v. 151, p. 97-106. Mattavelli, L., and Margarucci, V., 1992, Malossa Field – Italy, Po Basin, p. 119-137. Novelli, L., Chiaramonte, M.A., Mattavelli, L., Pizzi, G., Sartori, L., and Scotti, P., 1987, Oil habitat in the north western Po Basin, in Doligez B. (ed.), Migration of Hydrocarbons in Sedimentary Basins, p. 27-57. Pieri, M., and Groppi, G., 1981, Subsurface geological structure of the Po Plain, Italy: Prog. Finalizzato Geodinamica C.N.R., Publ. 414. Ronchi, P., and Ricchiuto, T., 2000, Relationships between diagenesis and porosity in Norian-Hettangian carbonate platforms (Subsurface, Po Valley, Italy): EAGE Conference Malta, 1-4 October 2000, Extended Abstracts Book, v. 4. Sarti, M., Bosellini, A., and Winterer, E.L., 1993, Basin geometry and architecture of a Tethyan passive margin (Southern Alps, Italy): implications for rifting mechanisms, in J.S.Watkins et al. (eds.), Geology and Geophysics of continental margins: A.A.P.G.Mem., 53, p. 241– 258. Schlumberger, ed., 1987, Gaggiano, in Well evaluation conference, Italia 87, v. 1, p. 49-52. Vaghi, G.C., Torricelli, L., Pulga, M., Giacca, D., Chierici, G.L., and Bilgeri, D., 1979, Production in the very deep Malossa Field, Ital: 10th World Petroleum Congress, Bucarest. |
Figure
2. Geological cross sections across the Po Valley from the Southern Alps
(A”-A) and from the Northern Apennines (Monferrato arc) (B-B’).
Figure
3. Geological cross section across the Po Valley from the Southern Alps
to the Northern Apennine (Emilian arc).
