Structural setting along the CROP-04 deep seismic

Boll.Soc.Geol.It. (Ital.J.Geosci.), Spec. Issue No. 7 (2007), pp. 283-296, 9 figs., CROP-04 (ed. by A. Mazzotti, E. Patacca and P. Scandone)
Structural setting along the CROP-04 deep seismic profile
(Southern Apennines - Italy)
D. SCROCCA (*), S. SCIAMANNA (**), E. DI LUZIO (*), M. TOZZI (*), C. NICOLAI (***) & R. GAMBINI (****)
ABSTRACT
RIASSUNTO
An updated review of the Southern Apennines structural architecture, a proven petroleum province in Italy, is presented taking
into consideration the new stratigraphic and structural constraints
provided both by almost forty years of petroleum exploration and by
the recently reprocessed CROP-04 deep seismic reflection profile. A
regional geological cross-section, drawn nearly parallel to the CROP04 seismic line, is described and discussed to point out the main features of the Southern Apennines. Moreover, a second shorter crosssection (named M. Foi cross-section), very well constrained by good
quality seismic and well data, is used to describe the allochthonous
units structural setting in detail, with special attention to the tectonic evolution of the Lagonegro units.
The Southern Apennines (SA) are a Neogene and Quaternary
thrust belt located in the hanging wall of a W-directed, E-retreating,
subduction of the Apulo-Adriatic lithosphere. From a structural point
of view, the SA are made up of a huge duplex system consisting of
two main units: the allochthonous nappes and the Apulian platform.
The allochthonous units, derived from the deformation of both peritidal carbonate platforms and pelagic basin successions and from the
stratigraphically overlying foredeep deposits, are completely detached
from their original substratum and transported onto the carbonates
of the Apulian platform. Beneath the mountain chain the Apulian carbonates are deformed to form a buried antiformal stack.
Some outstanding problems concern both the structural setting
of the deeper part of the SA thrust belt (e.g. the degree of involvement of the crystalline basement in the Apulian antiformal stack)
and of the allochthonous nappes.
CROP-04 and well data suggest the possibility that Lagonegro
and Apulian Platform carbonate units could extend at depth westward below the Apenninic platform units. Moreover, some geological and geophysical evidences suggest that shortening within the
Apulian carbonate platform units might be significantly greater than
previously assumed in several recent structural interpretations. The
increased shortening hypothesis may have relevant implications for
a better understanding of the petroleum system evolution.
The complex antiformal stack-type structure of the Lagonegro
units, revealed by well data and characterised by the tectonic repetition of the couple «Scisti Silicei» plus «Calcari con Selce», could be
reproduced with a relatively simple series of ramp-flat thrusts propagating through the Lagonegro succession. Based on both the regional
and the M. Foi cross-sections, a likely original width of about 125 km
has been estimated for the Lagonegro basinal domain: 90 km are now
deformed in antiformal-stack type structures in the axial zone of the
Campania-Lucania arc while other 35 km might be buried, in our
interpretation, below the Apennine units. The resulting total internal
shortening for the Lagonegro domain is about 60%.
Assetto strutturale lungo il profilo sismico crostale CROP-04
(Appennino meridionale - Italia).
KEY WORDS: Structural setting, seismic profiles, fold and
thrust belt, Southern Apennines.
(*) Istituto di Geologia Ambientale e Geoingegneria - C.N.R., c/o
Dip. di Scienze della Terra, Università degli Studi di Roma «La Sapienza», P.le A. Moro, 5 - 00185 Roma. E-mail: [email protected] Tel.: 06.4991.4922.
(**) Repsol-YPF, Esmevalda 255, Buenos Aires C1035ABE,
Argentina.
(***) Shell UK & P, Aberdeen, United Kingdom.
(****) OMV Aktiengesellschaft, EP-Exp-RG1 Gerasdorferstraße
151, A-1210 Wien, Austria.
In questo lavoro viene presentata una revisione della struttura
dell’Appennino meridionale sviluppata sulla base di nuovi vincoli stratigrafici e strutturali resi disponibili da oltre quaranta anni di esplorazione petrolifera e dal recente riprocessamento del profilo sismico crostale
CROP-04. Una sezione geologica regionale, tracciata circa parallelamente al profilo CROP-04, viene presentata e discussa per mettere in evidenza le principali caratteristiche dell’Appennino meridionale. Inoltre, una
seconda sezione geologica, costruita nell’area interessata dal pozzo
M. Foi 1 e fortemente vincolata da dati sismici e di pozzo, consente una
efficace descrizione della struttura delle unità alloctone con particolare
attenzione all’assetto ed all’evoluzione tettonica delle unità lagonegresi.
L’Appennino meridionale è un orogene sviluppato nel corso del
Neogene e del Quaternario a tetto di una zona di subduzione immergente verso ovest ed in arretramento flessurale verso est. Dal punto di
vista strutturale, l’Appennino meridionale è interpretabile come un sistema a duplex composto da due grandi unità: le unità alloctone e la
piattaforma Apula. Le unità alloctone derivano dalla deformazione di
successioni deposte in bacini pelagici e in area di piattaforma carbonatica e dai sovrastanti depositi di avanfossa; tali unità, completamente
scollate dal loro originario basamento, sono tettonicamente sovrapposte
ai carbonati apuli; questi ultimi si seguono relativamente indeformati
nel substrato dell’avanfossa bradanica sino al di sotto della catena dove
assumono un assetto caratterizzato da scaglie tettoniche embricate.
Alcuni dei principali problemi aperti riguardo alla geologia
dell’Appennino meridionale sono rappresentati dal possibile assetto
strutturale della porzione più profonda del cuneo orogenico (ad es.
dal grado di coinvolgimento del basamento) e dell’evoluzione tettonica delle unità alloctone.
L’interpretazione del profilo CROP-04 e dati di pozzo suggeriscono che le unità lagonegresi e la piattaforma apula possano estendersi in profondità al di sotto della piattaforma appennica nel settore tirrenico della catena. Inoltre, diverse evidenze geologiche e
geofisiche suggeriscono entità di raccorciamento per le unità apule
significativamente maggiori di quanto generalmente supposto in diverse recenti ricostruzioni strutturali dell’Appennino meridionale.
Tale ipotesi può avere importanti implicazioni per una migliore
comprensione dei processi di generazione e migrazione degli idrocarburi all’interno della piattaforma Apula.
Il complesso assetto strutturale delle unità lagonegresi, messo in
evidenza dai dati di sottosuolo e caratterizzato dalla ripetizione tettonica della coppia «Scisti Silicei» e «Calcari con Selce», può essere
riprodotto con la propagazione attraverso la successione sedimentaria lagonegrese di sovrascorrimenti con una geometria a ramp-flat
relativamente semplice. Sulla base delle nostre ricostruzioni strutturali, l’oroginario bacino lagonegrese doveva avere un’ampiezza di
circa 125 km: 90 km sono ora deformati in strutture tipo antiformalstack nella zona assiale dell’Appennino campano-lucano mentre altri
35 km potrebbero essere sepolti al di sotto delle unità appenniniche.
Il raccorciamento complessivo delle unità lagonegresi può essere
stimato in circa il 60%.
TERMINI CHIAVE: Assetto strutturale, profili sismici, catena
a pieghe e sovrascorrimenti, Appennino meridionale.
INTRODUCTION
Over the last few decades the Southern Apennines
(SA) have been the object of an intensive hydrocarbon
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D. SCROCCA ET ALII
Fig. 1 - Simplified geological map of the Southern Apennines (modifed after PATACCA et alii, 1992a).
– Schema geologico semplificato dell’Appennino meridionale (da PATACCA et alii, 1992a, modificato).
exploration that led to the discovery of the significant Val
d’Agri oil fields. This exploration activity has produced a
wealth of new data that has allowed an increasing understanding of the geological structure and evolution of this
part of the Apennines (MAZZOLI et alii, 2000; MENARDI
NOGUERA & REA, 2000; SCIAMANNA et alii, 2004; PATACCA
& SCANDONE, 2001; SCROCCA et alii, 2005). However, several outstanding questions still remain regarding both the
structural setting of the allochthonous nappes and of the
deeper part of the SA thrust belt.
The recent reprocessing of the CROP-04 deep seismic
reflection profile (MAZZOTTI et alii, 2000; SCROCCA et alii,
2003), that traverses the whole Southern Apennines (SA)
from the Tyrrhenian to the Adriatic Sea, has provided further constraints to develop an updated interpretation of
the SA structural setting.
Aim of this paper is to describe and discuss a regional
geological cross-section, drawn nearly parallel to the
CROP-04 seismic line (fig.1), in order to point out the
main features of the SA and the structural architecture of
the Campania-Lucania segment.
A first version of this line was developed, few years
ago, during a regional study of the SA promoted by Enterprise Oil Italiana S.p.A. The geological interpretation at
depth of this cross-section was based on the available
commercial seismic lines and was properly tied, on one
hand, to the field data collected during dedicated geological surveys led along the section line and, on the other
hand, to the well data available in the whole area (fig. 2).
This first version has been significantly improved taking
into consideration the new structural constraints highlighted by the reprocessing of the CROP-04, to produce
the regional cross-section presented in this paper.
Moreover, particular attention has been paid to the
structural setting of the Lagonegro Units. Based on a second, shorter, cross-section built in the M. Foi 1 well area
(very well constrained by good quality well and seismic
data), a detailed forward model of the tectonic evolution
of the Lagonegro units has been carried out.
REGIONAL GEOLOGICAL BACKGROUND
The SA are a roughly NW-SE trending segment of the
Apennine thrust belt, that developed in Neogene and Quaternary times, in the hanging wall of a west-directed eastretreating subduction zone (DOGLIONI et alii, 1996). The
SA thrust belt, characterised by low structural and topographic elevation, is bordered to the east by a foredeep
lying all along its Adriatic side, filled up by Pliocene-Pleistocene sediments (CASNEDI et alii, 1981; BALDUZZI et alii,
1982a; 1982b; BIGI et alii, 1992), and to the west by a
back-arc basin, the Tyrrhenian Sea (KASTENS et alii, 1988,
and references therein) developed starting from Tortonian times (fig. 1).
The progressive propagation of the compressional
deformation towards the foreland is clearly documented
by the development and evolution of a series of eastward-
STRUCTURAL SETTING ALONG THE
CROP-04 DEEP SEISMIC PROFILE
285
Fig. 2 - Subsurface data-base
(wells and selected seismic
lines) used to constrain the
structural interpretations.
– Dati di sottosuolo (pozzi e
linee sismiche) utilizzate per
vincolare le ricostruzioni strutturali.
migrating foredeep basins, developed in response to the
eastward roll-back of the Apulian lithosphere, and by the
occurrence of several piggy-back basins which developed
on top of the advancing allochthonous units (PATACCA &
SCANDONE, 1989; 2001).
Starting from Late Tortonian time, the development
of low angle «in-sequence» and «out-of-sequence» thrusts
within the thrust belt has been contemporaneous with the
extensional faulting processes along the Tyrrhenian side,
that are responsible for the thinning of the belt itself. The
progressive eastward migration of the extensional
processes in the Tyrrhenian side, as well of the thrust belt
compressive fronts and of the foreland flexure (and consequent shift of the foredeep basins) can be related to the
same geodynamic process: the roll-back of the subducting
Apulo-Adriatic lithosphere (MALINVERNO & RYAN, 1986;
PATACCA et alii, 1990; DOGLIONI, 1991).
Except for the uppermost nappes of the tectonic pile,
which represent remnants of the Neotethyan oceanic
domain (Liguride-Sicilide complexes), all the other units
nowadays exposed in the SA are derived from the western
Mesozoic passive margin of the Adriatic plate (CHANNELL
et alii, 1979).
Recent geodynamic reconstruction of the western
Mediterranean show that, after a stage of oceanic subduction, the complete closure of the Neotethyan domain was
achieved in the SA, apart from the Calabrian arc where
oceanic lithosphere is still subducting (CATALANO et alii,
2001). Continuing convergence led to the overthrusting of
the Liguride-Sicilide units onto the Adriatic margin characterised by normally thick or thinned continental lithosphere, and to the deformation of the continental margin
itself. The latter occurred, from Miocene times onward,
through a series of thrusting events (PATACCA et alii,
1990).
From a structural point of view, the SA are made up
of a huge duplex system consisting of two main units: the
allochthonous nappes and the Apulian Platform. The
allochthonous units, derived from the deformation of
both peritidal carbonate platforms and pelagic basin successions and from the stratigraphically overlying foredeep
deposits, are completely detached from their original substratum and transported onto the carbonates of the Apulian platform.
Due to the very complex geological setting of the
Apennines, several and often conflicting paleogeographi-
286
D. SCROCCA ET ALII
cal models have been proposed for the SA by different
Authors. Some of these differences are due to the widespread occurrence, both in outcrops and in wells, of lithologically monotonous basinal sequences, sometimes characterised by the absence of diagnostic fossils that have
prevented reliable chronological attributions. These
sequences have been assigned by different researchers to
diverse tectonic units. A typical example is represented by
the «Argille Varicolori» (Varicoloured shale) outcropping
in the axial segment of the Campania-Lucania arc (e.g. SW
of Potenza) that have been assigned by some researchers
to the Sicilide Units (PATACCA et alii, 1992a) while are considered by other researcher the detached upper portion of
the Lagonegro sequence (PESCATORE et alii, 1988).
The proposed paleogeographical models are characterised by different numbers of carbonate platforms and
pelagic domains (D’ARGENIO et alii, 1975; MOSTARDINI &
MERLINI, 1986; CASERO et alii, 1988; SGROSSO, 1988; PATACCA et alii, 1992a; MARSELLA et alii, 1995; MENARDI
NOGUERA & REA, 2000). It is beyond the aims of this
paper to discuss in detail on the differences between
them. We adopted a conservative paleogeographic model
that, at least in the Lucania sector crossed by our geological sections, seems to fit the available stratigraphical and
structural constraints.
The main units of the adopted paleogeographic framework are described below from the uppermost to the lowermost in the thrust pile, corresponding to a west to east
transect of the original paleogeography.
INTERNAL NAPPES
In this group have been placed units derived from
internal domains and that were deposited on oceanic to
transitional crust. This group of nappes is made up by the
following:
– Liguride units, Lower Cretaceous to Lower Miocene
sequences with incorporated ophiolitic suites; it comprises both the metamorphic Frido Unit and the unmetamorphosed Cilento Unit (OGNIBEN, 1969; KNOTT, 1987;
BONARDI et alii, 1988; MONACO & TORTORICI. 1995). The
Frido Melange has been interpreted as a part of an accertionary prism built up during the Cretaceous subduction
of the Tethys oceanic lithosphere (KNOTT, 1987; 1994).
– Sicilide units, Upper Cretaceous-Lower Miocene
succession of basinal deposit (OGNIBEN, 1969); in our
reconstruction, the provenance of the Sicilide units from
a basinal domain located west of the Western Platform
can be inferred from their geometric position, since the
Sicilide Unit systematically overlies the Alburno-Cervati
carbonates from the Cilento area to the high Agri valley.
An external original position (i.e. east of the Apennine
Carbonate Platform, see below) has been prososed in
other studies (MOSTARDINI & MERLINI, 1986; CASERO et
alii, 1988; PESCATORE et alii, 1988); a discussion on this
topic can be found in MENARDI NOGUERA & REA (2000).
APENNINE CARBONATE PLATFORM
The thrust units belonging to this domain (also
known as Western or Campano-Lucana Platform), form
the SA backbone. This domain consists of a thick pile (up
to 5000 m) of Upper Triassic-Lower Miocene shallowwater carbonates (SARTONI & CRESCENTI, 1961; SELLI,
1957, 1962) overlain by condensed hemipelagic and siliciclastic deposits marking respectively its flexural sinking
and the onset of foredeep environments (PATACCA et alii,
1990).
In the area crossed by CROP-04 profile, this paleogeographic domain include tidal-flat with protected
shelf-lagoon facies (Alburno-Cervati unit), platform-edge
(M. Marzano) and slope facies (Monti della Maddalena).
All the thrust sheets derived from this domain are
detached from their Paleozoic substratum at an intra-Triassic decollement.
LAGONEGRO-SANNIO AND MOLISE BASINAL UNITS
These units derive from sedimentary successions
deposited in relatively deep basinal domains. While the
Middle Triassic-Early Cretaceous portion (Lagonegro) of
this basinal domain is not controversial, the nature and
characteristics of the Upper Cretaceous/Tertiary section
are still highly debated.
The typical Lagonegro stratigraphic succession is
made up of the following four formations: «Monte Facito» (Middle Triassic), «Calcari con Selce» (Upper Triassic), «Scisti Silicei» (Jurassic), and «Galestri» (Lower Cretaceous). For a detailed description of the Lagonegro
formations see, among many others, SCANDONE (1967,
1972), WOOD (1981), and MICONNET (1988).
In the historical geological literature, the Lagonegro
sequence has been divided into four different facies
(SCANDONE, 1967). At a regional scale, the structural setting of the Lagonegro units has been defined in terms of
two superimposed nappes (SCANDONE, 1972): the uppermost nappe is named Lagonegro type II, and displays
more proximal depositional characteristics, while the
lower nappe is termed Lagonegro type I, and shows more
distal facies. This structural setting has been confirmed
by some more recent works (e.g.: CARBONE et alii, 1991)
while some other studies (e.g.: MAZZOLI et alii, 2001) have
questioned the aforementioned rigid matching between
thrust units and sedimentary facies. In this paper we will
refer to Lagonegro type I and II as synonyms of distal and
proximal facies respectively in order to maintain consistency with the existing literature.
The primary geometry of the Lagonegro basin has
been drastically modified in Miocene/Pliocene times by
thrusting, breaching and out-of-sequence processes that
produced complex imbricates and antiformal stacks, as
will be discussed later.
Regarding the palinspastic reconstruction of the
Lagonegro domains in the Campania-Lucania arc, there
is large agreement about the original position of the
Lagonegro basin between the Apennine and Apulian Platforms (altough an internal provenance of the Lagonegro
units has been proposed by MARSELLA et alii, 1995).
According to the available data, in our tectonic reconstruction, the Sannio Unit (PATACCA et alii, 1992a) is
likely to represent the Upper Cretaceous-Lower Miocene
portion of the Lagonegro units detached from its TriassicLower Cretaceous part and transported farther east (CARBONE et alii, 1988; CARBONE & LENTINI, 1990).
Also the Molise units (Tufillo-Serrapalazzo and Daunia
units) were completely detached from their original substratum. The Lower Messinian age of the Molise foredeep
deposits (PATACCA et alii 1992b) clearly documents an original external position for the Molise units (i.e. located east
STRUCTURAL SETTING ALONG THE
of the western carbonate platform and likely to the northeastern margin of the Lagonegro-molise basin).
APULIAN CARBONATE PLATFORM
This carbonate platform is made up of 5000 to 7000
m thick Mesozoic-Miocene shallow-water carbonates conformably lying on Permian volcanoclastic deposits penetrated by the Puglia 1 well (RICCHETTI et alii, 1988; MAZZOLI et alii, 2000) and stratigraphically overlain by upper
Messinian and Pliocene terrigenous deposits (PATACCA &
SCANDONE, 2001).
This sedimentary succession outcrops in Apulia
(Gargano and Salento regions) and represents the preorogenic cover of the foreland area, from the Adriatic to
the Ionian Seas (RICCHETTI et alii, 1988); it can be followed westward, by means of seismic and well data,
below the Plio-Pleistocene foredeep deposits (ROURE et
alii, 1991; MAZZOLI et alii, 2000). The tectonic units
derived from Apulian Carbonate Platform have been recognized in the subsurface structure of the SA, where they
form the buried Apulian belt (MOSTARDINI & MERLINI,
1986; CASERO et alii, 1988; MAZZOLI et alii, 2000;
MENARDI NOGUERA & REA, 2000). This buried belt consists of several imbricate units accreted from the internal
portions of the Apulian Platform, to form a major duplex
structure showing an antiformal stack geometry. The sole
thrust of this duplex separates the Apulian belt from the
undeformed or weakly deformed part of the Apulian
platform (outcropping in the Apulia-Salento foreland),
whereas the roof thrust represents the boundary to the
overlying Apenninic belt (including previously defined
units).
Finally, on top of the already deformed thrust belt
several thrust-sheet-top deposits can be recognised (PATACCA et alii, 1990; PATACCA & SCANDONE, 2001). These
deposits are very important because they provide dating
of the main deformation phases and allow kinematic
reconstruction of the SA thrust belt evolution.
REGIONAL CROSS-SECTION
The geometric relationships between the units
described in the previous chapter are shown in the
regional geological cross-section.
The first draft of this cross-section was developed
during a SA regional study sponsored by Enterprise Oil
Italiana (EOI) SpA. Dedicated field surveys were carried
out along the section line to define the main structural
features. The reconstruction of the geometrical setting at
depth has been initially driven by the interpretation of the
commercial seismic lines and well logs available from the
EOI database (fig. 2). The reconstruction of the deeper
part has been further refined and constrained by the
interpretation of the CROP-04 profile.
The cross section (fig. 3) will be described starting
from its north-eastern edge, located in the SA foredeep
basin, and moving towards the Tyrrhenian side.
NORTH-EASTERN SECTOR
The north-eastern end of the cross-section is located
within the Plio-Pleistocene clays and sands of the
CROP-04 DEEP SEISMIC PROFILE
287
Bradanic Trough (BALDUZZI et alii, 1982a; 1982b; PA& SCANDONE, 2001).
Below these deposits, well and seismic data clearly
show the flexural geometry of the Apulian Platform (fig.
4), being the top Apulian horizon (TAP) easily identifiable (SELLA et alii, 1988; NICOLAI & GAMBINI, this volume). Another deeper strong reflector, generally subparallel to the TAP, can be picked in several areas; a
reliable interpretation for this deep seismic event reflector is suggested by the stratigraphic data obtained from
some deep wells. The Puglia 1 well, below 6112 m of
shallow water carbonates and evaporites, penetrated an
unconformity underlain by about 1000 m of lower Triassic-upper Permian clastic deposits (RICCHETTI et alii,
1988; MAZZOLI et alii, 2000). The significant acoustic
impedance contrast between the upper Triassic
dolomites and the lower Triassic-upper Permian clastic
deposits can explain the strong and deep seismic event,
recognised both below the foredeep (ROURE et alii,
1991) and in some sector of the SA thrust belt (MAZZOLI
et alii, 2000), that can be interpreted as a bottom Apulian horizon.
Below the foredeep, on the CROP-04 profile, a thickness of about 2.4 s TWT can be estimated for the Apulion
units corresponding to about 7000-7400 m (depending on
the average interval velocity used for depth convertion).
This thickness can be considered a representative value in
the study area, although with some variation often due to
the variable thickness of the Cretaceous section.
In our cross-section, a simplified stratigraphy for the
Apulian Carbonate Platform has been represented with
an average thickness of about 7400 m for the Upper Triassic-Miocene carbonates (fig. 3).
Considering the lack of data, a constant tickness of
1500 m has been assumed for the Permo-Triassic clastic
deposits penetrated by the Puglia 1 well altough these
deposits represent a syn-rift sequence, by definition characterised by variable thickness. Consequently, the top of
the supposed crystalline basement has been reconstructed
by interpolating TAP and Moho attitude (SCARASCIA et
alii, 1994).
The Plio-Pleistocene clays and sands of the Bradanic
Trough are partly deformed by the outer embricate thrust
involving the Tufillo-Serrapalazzo and Daunia units
(Molisan allochton).
The Serra Palazzo Unit, widespread along the eastern
margin of the Apennines, entirely consists of Tertiary
basinal deposits representing the detached upper portion
of a basinal sequence, originally deposited in the northeastern sector of the Lagonegro-Molise basinal domain.
In the subsurface, the Serra Palazzo and Daunia Units are
usually the lowest Apenninic thrust sheets above the
Lower Pliocene Clays which disconformably overlie the
Apulia carbonates (fig. 4).
Moving westward large outcrops of the Lagonegro
units occur in the S. Fele area (fig. 5). The Lagonegro
sequence is overlaid by the Sannio units, that in our interpretation represent the detached upper portion of the
Lagonegro sequence, which in turn is unconformably
covered by the Pliocene sediments of the Ofanto cycle.
The main surface structural features of the Lagonegro
Units are represented by brachianticlines separated by
brachisynclines (with average length of major axes
around 1-2 km). Based on seismic and well data (e.g. S.
Fele 1 and M. Foi 1 wells), it can be inferred that such
TACCA
Fig. 3 - Regional geological cross-section (location in figs. 1 and 2).
– Sezione geologica regionale (ubicazione in figg. 1 e 2).
288
D. SCROCCA ET ALII
STRUCTURAL SETTING ALONG THE
CROP-04 DEEP SEISMIC PROFILE
289
Fig. 4 - Detail of the central part of the CROP-04 seismic profile (CDP interval: 1486-2546, see location in fig. 2). The main structural features
of the allochthonous units can be recognised. Top Apulian horizon has been traced integrating well data and the interpretation of commercial
seismic lines.
– Dettaglio del settore centrale del profilo sismico CROP-04 (intervallo di CDP: 1486-2546, ubicazione in fig. 2). Sono riconoscibili le principali
caratteristiche strutturali delle unità alloctone. L’orizzonte relativo al top Apula è stato tracciato sulla base dell’interpretazione di linee sismiche
commerciali e di dati di pozzo.
basinal units are actually involved in a complex antiformal stack-type structure and affected by further thrusts
(not older than Upper Pliocene). Although these thrusts
seem to have out-of-sequence features at the shallower
levels (with decapitation of earlier anticlines in the
Lagonegro antiformal stack, as suggested by the available
S. Fele 1 stratigraphy), they turn out to be breaching
thrust at depth, responsible for the building up of the
Apulian thrust units. A detailed analysis of the Lagonegro
Units structural setting and tectonic evolution will be
developed in the following chapter, using a better constrained geological section built in the M. Foi 1 well area.
Below the allochthonous units, several wells (e.g. S.
G. Magno 1 well) have drilled Apulian carbonate units
belonging to the buried Apulian antiformal stack (PATACCA et alii, this volume). Seismic data show only the top
of this antiformal stack (PATACCA & SCANDONE, 2001;
NICOLAI & GAMBINI, this volume), while the geometrical
setting of the footwall units of the main thrust affecting
the Apulian carbonates is generally poorly defined (fig. 4).
As a consequence, one of the outstanding problems in any
reconstruction of the SA structural setting is the real
shortening within the buried Apulian belt and the possible involvement of the Apulian crystalline basement in
the compressional deformation.
In our section we have chosen a conservative approach
adopting a minimum displacement at TAP level of about
25 km suggested by the structural modelling of seismic and
well evidences, leaving a blank area below the modelled
antiformal stack (fig. 3).
WESTERN SECTOR
The south-western segment of the geological crosssection is characterised by large outcrops of carbonate
units of the Apennine platform.
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D. SCROCCA ET ALII
Fig. 5 - Structural relationships between Sicilide Units, Apennine
Platform (Maddalena Unit) and Lagonegro Units.
– Rapporti strutturali tra le unità sicilidi, la piattaforma appenninica
(unità dei Monti della Maddalena) e unità lagonegresi.
a thrust which caused a tectonic thickening of the
Apennine platform. In the footwall of this thrust lies the
SW-plunging Alburno-Cervati homocline. This interpretation accounts for the anomalous thickness of the
Apennine platform detected in the CROP-04 seismic
section in the M. Faito-M. Chianello area (about 9000
m). It should be noted that on the CROP-04, a thickness
of about 1.8 s TWT (and possibly up to 2 s) can be estimated for the Apennine Platform below M. Alburno.
This evidence, assuming an interval average velocity of
5500-6000 m/s, implies a total thickness of at least 5000
m for this unit.
On the whole western side of the CROP-04 seismic
line (fig. 7), the «transparent» seismic facies of the homogeneous carbonate sequence of both the Alburni and
Monte Marzano units overlie a well stratified seismic
facies, about 1 s. TWT thick, with a very distinctive character. Based on well data (e.g. Contursi 1 well), this stratified seismic facies can be correlated to the Lagonegro
basinal sequence. Below the Lagonegro units, deep exploration wells (e.g. S. G. Magno 1 well) penetrate the Apulian carbonates. In our seismic interpretation, the stratified seismic facies attributed to the Lagonegro Units and
the top Apulian horizon can be seen to deepen westward
below the Apennine carbonate units. This interpretation
is supported by the strong seismic event at about 8 s TWT
in the SW sector of the CROP-04 line (fig. 7), that could
be interpreted as a near bottom Apulian carbonates
reflector.
LAGONEGRO UNITS: TECTONIC EVOLUTION
Fig. 6 - Tectonic contact (marked by a N120 left-lateral strike-slip
slip fault) between the Alburni Massif (Apennine Platform) and the
Sicilide Units.
– Contatto tettonico (caratterizzato da un sistema di faglie trascorrenti
sinistre orientato N120) tra il massiccio carbonatico degli Alburni e le
unità sicilidi.
The Alburno-Cervati structure, exhibits a constant
SW dip and is bounded on each edge by WNW-ESE subvertical, strike-slip, fault systems (fig. 6) which were
active in the Upper Pliocene (ASCIONE et alii, 1992;
BERARDI et alii, 1996).
East of the Alburni, NW-SE normal faults offset the
Monte Marzano transitional facies, which is considered
to be the eastern margin of the Apennine carbonate platform. Some of these faults are active and reflect the present day extensional tectonic field responsible for the
Irpinian earthquake (1980). This earthquake has been
related to a main seismogenetic structure, NW-SE trending and dipping about 60° to NE (PINGUE et alii, 1988).
At the south-western edge of our geological cross-section, the M. Faito-M. Chianello NE-plunging homocline is
shown. It represents the southernmost segment of the
Monte Soprano-Monte Sottano ridge, consisting of carbonates Lower Cretaceous to Upper Tortonian in age.
This homocline is overthrust by the Sicilide units.
The M. Faito-M. Chianello homocline is considered
the forelimb of a wide anticline, whose western limb is
cut by a normal fault, developed in the hanging-wall of
Enterprise Oil Italian SpA drilled the Monte Foi well
through the Lagonegro units to reach the Apulian carbonate units at depth. As it was important to understand the
nature of the allochthonous Lagonegro units, both for the
well prognosis and during drilling operation, much effort
was devoted to build up a consistent model of the
Lagonegro tectonic setting. An initial interpretation was
developed utilising the available surface and subsurface
information in the study area. Detailed field mapping,
updated revisions of wells stratigraphy, well log correlation, and seismic interpretation based on a good quality
dense seismic grid, were used to constrain the structural
interpretation. This interpretation has been subsequently
improved taking into consideration the M. Foi 1 well
results. A detailed description of the M. Foi 1 well stratigraphy can be found in PATACCA et alii (this volume).
The wealth of reliable geological and geophysical
information has resulted in a complicated structural
interpretation for the M. Foi cross-section (fig. 8). The
Lagonegro II units are involved in a complex antiformal
stack-type structure consisting of the tectonic repetition
of the couple «Scisti Silicei» plus «Calcari con Selce».
Sometimes the «Galestri» formation is preserved within
this tectonic repetition. In the M. Foi 1 well, no upper
Cretaceous-Tertiary units were encountered in this
antiformal stack structure and the Lagonegro II units are
thrust over the Lagonegro I succession.
Despite the complexity of the M. Foi Cross-section,
this final interpretation has been demonstrated to be
structurally and kinematically viable and admissible
through a forward modelling performed by means of
GEOSECTM software. The forward modelling was carried
STRUCTURAL SETTING ALONG THE
CROP-04 DEEP SEISMIC PROFILE
291
Fig. 7 - Detail of the western part of the CROP-04 seismic profile (CDP interval: 6-1166, see location in fig. 2). On the eastern edge of the
seismic data the presence of the Lagonegro units and of the top Apulian is proved by well data. In our interpretation both Lagonegro units
and the Apulian platform could extend westward below the Apennine carbonate units.
– Dettaglio del settore occidentale del profilo sismico CROP-04 (intervallo di CDP: 6-1166, ubicazione in fig. 2). Nel margine orientale della sezione
sismica la presenza delle unità lagonegresi e della piattaforma apula è dimostrata da perforazioni profonde. Nella nostra interpretazione sia le
unità lagonegresi che la piattaforma potrebbe estendersi verso ovest al di sotto delle unità appenniniche.
out to reproduce a slightly simplified version of the interpreted structural setting (see figure 8 for a comparison
between actual and modelled structural setting) and to
analyse the first order structural features of the Lagonegro units; for this reason simplistic ramp-flat geometries
have been assumed. A detailed reconstruction of the complex polyphase deformation experienced by the Lagonegro units (e.g. MAZZOLI, 1992) is beyond the aim of this
study and is not allowed by the resolution of seismic and
well data.
Furthermore, the following assumptions were adopted,
for the sake of simplicity, to develop the forward modelling:
– geological formations have constant thickness;
– no Tufillo-Serrapalazzo unit is modelled;
– assumed vertical shear deformation algorithm (volume is conserved during deformation but line lengths
may change slightly).
Based on this forward modelling (fig. 9), the following step by step deformation history can be highlighted.
1) The detachment of the Upper Cretaceous-Tertiary
cover of the Lagonegro basinal sequence must be a
regional and early tectonic process, probably related to
the activation of a very efficient intra-Cretaceous detachment (likely the Varicoloured shale formation).
2) The tectonic repetitions of the couple «Scisti Silicei»
plus «Calcari con Selce» within the Lagonegro II units
were an early event linked to the propagation of secondary
detachments, located at the base of the «Calcari con Selce»
and propagating upward with short ramps up to shallower
flats at the base of the «Galestri» formation. This process
implies that somewhere on the back of the model (below
the Apennine units in the geological cross-section) about
13 km of «Monte Facito» remain without its original Jurassic-Lower Cretaceous cover. Ramp segment splaying from
the same thrusts at the base of the «Galestri» formation, or
breaching thrust ramps propagating from lower detachments, caused the stacking of the tectonic repetition «Scisti
Silicei» plus «Calcari con Selce» on top of the «Galestri».
3) Regional tectonic doubling of the Lagonegro (Type
II on top of Type I) occurs by means of a footwall/hang-
Fig. 8 - Comparison between the interpreted structural setting in the M. Foi 1 well area and the modelled section.
– Confronto tra l’assetto strutturale ricostruito nella zona del pozzo M. Foi 1 e la sezione riprodotta con il forward modelling.
292
D. SCROCCA ET ALII
CROP-04 DEEP SEISMIC PROFILE
Fig. 9 - Forward modelling of the possible structural evolution of the Lagonegro units in the M. Foi 1 well area (see text for details).
– Forward modelling della possibile evoluzione strutturale delle unità lagonegresi nell’area del pozzo M. Foi 1 (spiegazione nel testo).
STRUCTURAL SETTING ALONG THE
293
294
D. SCROCCA ET ALII
ingwall flat thrust geometry at any time after (or during)
the early Lagonegro II deformation.
4) Lagonegro units (I and II) are already deformed
prior overthrusting the Apulian Platform.
5) The final configuration of the Lagonegro antiformal stack is due to the late propagation of at least one
main thrust, that shows out-of-sequence features at the
shallower levels but turn out to be a breaching thrust at
depth, responsible for the piling up of the buried Apulian
thrust units.
The initial length of the Lagonegro II domain in our
model is of only 50 km because this was the minimum
length necessary to reproduce the Lagonegro II structural
setting, which was the main task of this modelling exercise.
The regional overthrusting of the Lagonegro II over
the Lagonegro I units implies that at least another 40 km
should be added to the initial model, to consider the minimum initial length of the Lagonegro I domain that is
represented in the M.Foi cross-section. Consequently, the
minimum total width of the Lagonegro basin that should
necessarily be considered to honour the available data in
the M. Foi area is of at least 90 km. According to the
structural interpretation proposed in the regional crosssection (fig. 3), other 35 km of undifferentiated Lagonegro units, suggested by the combined interpretation of
wells data and CROP-04 seismic (fig. 7), should be buried
below the Apennine units.
The resulting total width of the Lagonegro basinal
domain, in the portion of the SA considered in this study,
increases to about 125 km; a figure similar to the one
(130 km) estimated by MENARDI NOGUERA & REA (2000).
The total displacement necessary to reproduce the
Lagonegro II structures is about 13 km (Step 2, evaluated
at top «Calcari con Selce»), implying an internal shortening of the Lagonegro II of about 26%. Moreover, the displacements necessary to reproduce the tectonic duplication Lagonegro II over Lagonegro I (at least 40 km) and
the internal shortening of the Lagonegro I units produce
a total shortening for the Lagonegro domain of about
60% (Step 3).
Finally, at least 4 km displacement should be assumed
in the forward model for the breaching thrust propagating
upward from the Apulian antiformal stack to honour the
interpreted geometry. The internal shortening within the
Apulian is likely to be significantly higher (at least 25 km
of total displacement, at top Apulian level, has been
adopted in the regional cross-section).
DISCUSSION & CONCLUSION
The available data clearly show the structural configuration of the SA thrust belt represented in our regional
cross section (fig. 3). It is characterised by the flexural
bending of the Apulian carbonate covers, that can be followed below the Plio-Pleistocene foredeep deposits, in
response to the west-directed, east-retreating, subduction
of the Apulo-Adriatic lithosphere.
Further west, the Apulian carbonates are deformed to
form an antiformal stack that is buried beneath the
allochthonous sheets. The latter, derived from the deformation of both peritidal carbonate platforms and pelagic
basin successions and from the stratigraphically overlying
foredeep deposits, are completely detached from their
original substratum.
The new information provided by the interpretation
of the CROP-04 suggest the possibility that Lagonegro
and Apulian Platform carbonate units could extend at
depth westward below the Apenninic platform units.
The tectonic evolution of the Lagonegro units has
been analysed in detail in the M. Foi 1 well area thanks to
high quality seismic and well data (fig. 8). The interpreted
structural setting has been tested by means of a forward
kinematic modelling (fig. 9). The complex antiformal
stack-type structure, characterised by the tectonic repetition of the couple «Scisti Silicei» plus «Calcari con
Selce» revealed by well data, cab be reproduced with a
relatively simple series of ramp-flat thrusts propagating
through the Lagonegro succession.
Based on both the regional and the M. Foi cross-sections, a likely original width of about 125 km has been
estimated for the Lagonegro basinal domain: 90 km are
now deformed in antiformal-stack type structures in the
axial zone of the Campania-Lucania arc while other 35
km might be buried, in our interpretation, below the
Apennine units. The resulting total internal shortening for
the Lagonegro domain is of about 60%.
One of the outstanding uncertainties in any reconstruction of the SA structural setting is the actual shortening within the buried Apulian belt and by the degree of
involvement of the crystalline basement in the Apulian
antiformal stack. Although seismic data show the general
features of the Apulian antiformal stack units (PATACCA
& SCANDONE, 2001; NICOLAI & GAMBINI, this volume),
the amount of displacements along the main thrust is
still a matter of debate because of poor seismic resolution in the thrusts’ footwall, where lithological contrast
disappear. In our section, we have chosen a conservative
approach representing a minimum displacement suggested by the structural modelling of seismic and well
evidences (at least 25 km of total displacement at top
Apulian level).
Other geological and geophysical constraints might
suggest larger displacements than assumed in several
recent structural interpretations (MAZZOLI et alii, 2000;
MENARDI NOGUERA & REA, 2000), implying higher
shortening within the buried Apulian belt and little or
no crystalline basement involvement in the SA (SCROCCA
et alii, 2005), as is also suggested by a comparative
analysis of the geological signatures (morphology and
structure) of thrust belts world-wide (DOGLIONI et alii,
1996; 1999).
For instance, shortening within the buried Apulian
belt higher than 25 km could be inferred by comparing
the total displacement at TAP level vs. timing and magnitude of the allochthonous nappes advance (PATACCA &
SCANDONE, 2001). Moreover, maturity and thermal modelling performed in the Val d’Agri area (SCIAMANNA et alii,
2004), SE of the area considered in this study, indicate
that the reduced shortening hypothesis within the Apulian antiformal stack is inconsistent with the observed
different maturity trends.
ACKNOWLEDGEMENTS
Many thanks to P. Scandone, E. Patacca and C. Doglioni for
fruitful discussions. V. Zucconi is acknowledged for contribution to
the seismic interpretation of the allochthonous units. Comments by
S. Merlini greatly improved the manuscript.
STRUCTURAL SETTING ALONG THE
REFERENCES
ASCIONE A., CINQUE A. & TOZZI M. (1992) - La Valle del Tanagro
(Campania): una depressione strutturale ad evoluzione complessa.
Studi Geol. Camerti, Vol. Spec. (1992), 209-219.
BALDUZZI A., CASNEDI R., CRESCENTI U. & TONNA M. (1982a) - Il
Plio-Pleistocene del sottosuolo del Bacino pugliese (Avanfossa
appenninica). Geol. Romana, 21, 1-28.
BALDUZZI A., CASNEDI R., CRESCENTI U., MOSTARDINI F. & TONNA
M. (1982b) - Il Plio-Pleistocene del sottosuolo del Bacino lucano
(Avanfossa appenninica). Geol. Romana, 21, 89-111.
BERARDI F., DE ROSA G. & TOZZI M. (1996) - Vincoli strutturali di
auperficie per una ricostruzione geometrica e cinematica del Massiccio dei Monti Alburni (Appennino Meridionale). Mem. Soc.
Geol. It., 51, 13-21.
BIGI G., COSENTINO D., PAROTTO M., SARTORI R. & SCANDONE P.
(1992) - Structural Model of Italy. Scale 1:500.000. P.F. Geodinamica, 114. C.N.R.
BONARDI G., AMORE F.O., CIAMPO G., DE CAPOA P., MICONNET P. &
PERRONE V. (1988) - Il Complesso Liguride auct.: stato delle conoscenze e problemi aperti sulla sua evoluzione pre-appenninica ed i
suoi rapporti con l’Arco Calabro. Mem. Soc. Geol. It., 41, 17-35.
CARBONE S., CATALANO S., LENTINI F. & MONACO C. (1988) - Le
unità stratigrafico-strutturali dell’Alta Val d’Agri (Appennino Lucano) nel quadro dell’evoluzione del sistema catena-avanfossa.
Mem. Soc. Geol. It., 41, 331-341.
CARBONE S. & LENTINI F. (1990) - Migrazione neogenica del sistema
catena-avampaese nell’Appennino meridionale: problematiche paleogeografiche e strutturali. Riv. Ital. Paleont. Stratigr., 96, 271296.
CARBONE S., CATALANO S., LAZZARI S., LENTINI F. & MONACO C.
(1991) - Presentazione della carta geologica del Bacino del Fiume
Agri (Basilicata). Mem. Soc. Geol. It., 47, 129-143.
CASERO P., ROURE F., ENDIGNOUX L., MORETTI I., MULLER C., SAGE
L. & VIALLY R. (1988) - Neogene geodynamic evolution of the
Southern Apennines. Mem. Soc. Geol. It., 41, 109-120.
CASNEDI R., CRESCENTI U., D’AMATO C., MOSTARDINI F. & ROSSI U.
(1981) - Il Plio-Pleistocene del sottosuolo molisano. Geol. Romana, 20, 1-42.
CATALANO R., DOGLIONI C. & MERLINI S. (2001) - On the Mesozoic
Ionian basin. Geophys. J. Int., 144, 49-64.
CHANNELL J.E.T., D’ARGENIO B. & HORVATH F. (1979) - Adria, the
African promontory, in Mesozoic Mediterranean paleogeography.
Earth Science Rev., 15, 213-292.
D’ARGENIO B., PESCATORE T. & SCANDONE, P. (1975) - Structural
pattern of the Campania-Lucania Apennines. In: Structural Model of Italy, CNR, Quaderni Ricerca Scientifica, 90, 313-327.
DOGLIONI C. (1991) - A proposal of kinematic modelling for W-dipping
subductions. Possible applications to the Tyrrhenian-Apennines
system. Terra Nova, 3, 423-434.
DOGLIONI C., HARABAGLIA P., MARTINELLI G., MONGELLI F. & ZITO
G. (1996) - A geodynamic model of the Southern Apennines accretionary prism. Terra Nova, 8, 540-547.
DOGLIONI C., HARABAGLIA P., MERLINI S., MONGELLI F., PECCERILLO A. & PIROMALLO C. (1999) - Orogens and slabs vs. their direction of subduction. Earth Science Rev., 45, 167-208.
KASTENS K., MASCLE J. & ODP LEG 107 SCIENTIFIC PARTY (1988) ODP Leg 107 in the Tyrrhenian Sea: insigths into passive margin
and back-arc basin evolution. Geol. Soc. Am. Bull., 100, 11401156.
KNOTT S.D. (1987) - The Liguride complex of southern Italy – a Cretaceous to Paleogene accretionary wedge. Tectonophysics, 142,
217-226.
KNOTT S.D. (1994) - Structure, kinematics and metamorphism of the
Liguride complex, southern Apennines, Italy. J. Struct. Geol., 16,
1107-1120.
MALINVERNO A. & RYAN B. F. (1986) - Extension in the Tyrrhenian
Sea and shortening in the Apennines as result of arc migration
driven by sinking of the lithosphere. Tectonics, 5, 227-245.
MARSELLA E., BALLY A.W., CIPPITELLI G., D’ARGENIO B. & PAPPONE
G. (1995) - Tectonic history of the Lagonegro domain and
Southern Apennine thrust belt evolution. Tectonophysics, 252,
307-330.
CROP-04 DEEP SEISMIC PROFILE
295
MAZZOLI S. (1992) - Structural analysis of the Mesozoic Lagonegro
Units in SW Lucania (Southern Italian Apennine). Studi Geol.
Camerti, 7, 117-146.
MAZZOLI S., CORRADO S., DE DONATIS M., SCROCCA D., BUTLER R.,
DI BUCCI D., NASO G., NICOLAI C. & ZUCCONI V. (2000) - Time
and space variability of «thin-skinned» and «thick-skinned» thrust
tectonics in the Apennines (Italy). Rend. Fis. Acc. Lincei, 11, 5-39.
MAZZOLI S., BARKHAM S., CELLO G., GAMBINI R., MATTIONI L., SHINER P. & TONDI E. (2001) - Reconstruction of continental margin
architecture deformed by the contraction of the Lagonegro Basin,
Southern Apennines, Italy. J. Geol. Soc., 158, 309-319.
MAZZOTTI A., STUCCHI E., FRADELIZIO G., ZANZI L. & SCANDONE P.
(2000) - Seismic exploration in complex terrains; a processing experience in the Southern Apennines. Geophysics, 65, 1402-1417.
MENARDI NOGUERA A. & REA G. (2000) - Deep structure of the Campanian-Lucanian Arc (Southern Apennine, Italy). Tectonophysics, 324 (4), 239-265.
MICONNET P. (1988) - Evolution mesozoique du secteur de Lagonegro.
Mem. Soc. Geol. It., 41, 321-330.
MONACO C. & TORTORICI L. (1995) - Tectonic role of ophiolite-bearing
terranes in the devolopment of the Southern Apennines orogenic
belt. Terra Nova, 7, 153-160.
MOSTARDINI F. & MERLINI S. (1986) - L’Appennino centro-meridionale. Sezioni geologiche e proposta di modello strutturale. Mem.
Soc. Geol. It., 35, 177-202.
NICOLAI C. & GAMBINI R. (this volume) - Structural architecture of
the Adria platform-and-basin system.
OGNIBEN L. (1969) - Schema introduttivo alla geologia del confine calabro-lucano. Mem. Soc. Geol. It., 8, 453-763.
PATACCA E. & SCANDONE P. (1989) - Post-Tortonian mountain building in the Apennines. The role of the passive sinking of a relic
lithospheric slab. In A. Boriani, M. Bonafede, G.B. Piccardo and
G.B. Vai (Eds.), «The lithosphere in Italy. Advances in Earth
Science Research». Atti dei Convegni Lincei, 80, 157-176, Italian
National Committee for the International Lithosphere Program.
PATACCA E., SARTORI R. & SCANDONE P. (1990) - Tyrrhenian basin
and Appeninic Arcs: kinematic relations since late Tortonian times.
Mem. Soc. Geol. It., 45, 425-451.
PATACCA E., SCANDONE P., BELLATALLA M., PERILLI N. & SANTINI U.
(1992a) - The Numidian-sand event in the southern Apennines.
Mem. Sc. Geol., 18, 297-337.
PATACCA E., SCANDONE P., BELLATALLA M., PERILLI N. & SANTINI U.
(1992b) - La zona di giunzione tra l’arco appenninico settentrionale e l’arco appenninico meridionale nell’Abruzzo e nel Molise.
In: M. Tozzi, G.P. Cavinato and M. Parotto (Eds.), «Studi preliminari all’acquisizione dati del profilo CROP 11 CivitavecchiaVasto». Studi Geol. Camerti, vol. spec. 1991-2, 417-441.
PATACCA E. & SCANDONE P. (2001) - Late thrust propagation and sedimentary response in the thrust-belt-foredeep system of the
Southern Apennines (Pliocene-Pleistocene). In: Vai G.B. & Martini I.P. (Eds.): «Anatomy of an Orogen: the Apennines and the
adjacent Mediterranean Basins». Kluwer Academic Publishers:
401-440.
PATACCA E., CASCELLA A. & MEROLA D. (this volume) - Stratigraphy
of selected wells along the CROP-04 transect.
PESCATORE T., RENDA P. & TRAMUTOLI M. (1988) - Rapporti tra le
unità lagonegresi e le unità sicilidi nella media Valle del Basento,
Lucania (Appennino meridionale). Mem. Soc. Geol. It., 41, 353361.
PINGUE F., DE NATALE G., BONASIA V., CAGNETTI V., DEL PEZZO E.,
MARTINI M., SCARPA R. & ZOLLO A. (1988) - Il terremoto IrpinoLucano del 23 Novembre 1980. Mem. Soc. Geol. It., 41, 1163-1169.
RICCHETTI G., CIARANFI N., LUPERTO SINNI E., MONGELLI F. & PIERI P. (1988) - Geodinamica ed evoluzione sedimentaria e tettonica
dell’avampaese apulo. Mem. Soc. Geol. It., 41, 57-82.
ROURE F., CASERO P. & VIALLY R. (1991) - Growth processes and melange formation in the southern Apennines accretionary wedge.
Earth Planet. Sc. Let., 102, 395-412.
SARTONI S. & CRESCENTI U. (1961) - Ricerche biostratigrafiche nel
Mesozoico dell’Appennino meridionale. G. Geol., 29, 161-302.
SCANDONE P. (1967) - Studi di geologia lucana: la serie calcareo-silicomarnosa e i suoi rapporti con l’Appennino Calcareo. Boll. Soc.
Natur. Napoli, 76, 301-469.
296
D. SCROCCA ET ALII
SCANDONE P. (1972) - Studi di geologia lucana: la carta dei terreni della
serie calcareo-silico-marnosa e note illustrative. Boll. Soc. Natur.
Napoli, 81, 225-300.
SCARASCIA S., LOZEJ A. & CASSINIS R. (1994) - Crustal structures of
the Ligurian, Tyrrhenian and Ionian seas and adjacent onshore
areas interpreted from wide-angle seismic profiles. Boll. Geofis.
Teor. Appl., 36, 5-19.
SCROCCA D., DOGLIONI C., INNOCENTI F., MANETTI P., MAZZOTTI A.,
BERTELLI L., BURBI L. & D’OFFIZI S. (Eds.) (2003) - CROP
Ateas: Seismic reflection profiles of the Italian crost. Mem. Descr.
Carta Geol. It., 66, 194 pp.
SCROCCA D., CARMINATI E. & DOGLIONI C. (2005) - Deep structure of
the southern Apennines, Italy: thin-skinned or thick-skinned? tectonics, 24, TC 3005, doi: 10.1029/2004 TC 001634.
SCIAMANNA S., SASSI W., GAMBINI R., RUDKIEWICS S.L., MOSCA F.
& NICOLAI C. (2004) - Predicting hydrocarbon generation and
expulsion in the southern Apennines thrust belt by 2-D integra-
ted structural and geochemical modeling: Part I - structural
and thermal evolution. In Swenne R., Roure F. and Granath
S.W. (Eds.), «Deformation, fluid flow, and reservoir appraisal
in foreland fold and thrust belt». AAPG Hedberg Series, 1,
51-67.
SELLA M., TURCI C. & RIVA A. (1988) - Sintesi geopetrolifera della Fossa Bradanica. Mem. Soc. Geol. It., 41, 87-108.
SELLI R. (1957) - Sulla trasgressione del Miocene nell’Italia meridionale.
G. Geol., 26, 1-54.
SELLI R. (1962) - Il Paleogene nel quadro della geologia dell’Italia meridionale. Mem. Soc. Geol. It., 3, 733-789.
SGROSSO I. (1988) - Nuovi elementi per un più articolato modello paleogeografico nell’Appennino centro-meridionale. Mem. Soc. Geol. It.,
41, 225-242.
WOOD A.W. (1981) - Extensional tectonics and birth of the Lagonegro
Basin (Southern Italian Apennines). Neues Jahrb. Geol. Palaeont.
Abh., 161, 93-131.
Received 13 October 2002; revised version accepted 12 March 2004; last proofs received 5 September 2006.

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