LONG-TERM EVENT STRATIGRAPHY OF THE APULIA PLATFORM MARGIN (UPPER JURASSIC TO
EOCENE, GARGANO, SOUTHERN ITALY)
ALFONSO BOSELLINI, MICHELE MORSILLI, AND CLAUDIO NERI
Dipartimento di Scienze Geologiche e Paleontologiche, Università di Ferrara, Corso Ercole I8 d’Este 32, 44100 Ferrara, Italy
e-mail: [email protected]
ABSTRACT: The Upper Jurassic to Eocene Apulia Platform margin
and the eastward transition to the adjacent basinal deposits are well
exposed in the Gargano Promontory (southern Italy), a carbonate
block that is part of the slightly deformed foreland of the southern
Apennine thrust belt. The long-term stratigraphy of this margin and
slope transect is punctuated by five major dynamic phenomena that
subdivide the succession into six second-order sequences. These events
include (1) a Valanginian drowning unconformity, (2) an early Aptian–
Albian drowning and demise of the platform, (3) late Albian–Cenomanian platform-margin failures, (4) a Santonian–Campanian retreat
of the platform margin, and (5) Eocene uplift and platform-margin
collapse. The first event is documented worldwide and is probably eustatic in origin. The second is concomitant with some oceanic anoxic
events (OAE). The last three processes are probably related to foreland
reaction to subduction and collision in the Dinarides and Hellenides
thrust belts. The ultimate cause of the Albian–Cenomanian failures is
more problematic. A worldwide eustatic regression is documented at
this time, but regional geology seems to favor tectonic uplift.
INTRODUCTION
Since the first appearance of the famous Exxon cycle chart (Vail et al.
1977; Haq et al. 1987), many geologists have accepted as a dogma these
eustatic ‘‘curves’’ and have tried to fit their own regional or local data to
them. On the other hand, there are so many Exxon sequence-boundary
events from which to choose (Miall 1992), in many cases spacing closer
than any biostratigraphic resolution, that it is easy and tempting to find an
‘‘ad hoc’’ boundary.
A different approach could be to elaborate local detailed stratigraphies
and construct local relative sea-level curves for many regions of the world
and then to compare the various charts. Only for those sequence boundaries
dated accurately and precisely and occurring synchronously over large areas of the globe, some kind of eustasy could be invoked for the dominant
operating mechanism.
In this report we present the long-term event stratigraphy of a transect
of the Apulia Platform margin and slope exposed in the Gargano Promontory of southern Italy (Fig. 1). The Apulia Platform was a relatively small
carbonate bank, isolated in the middle of the western Tethys ocean, which
flourished throughout the Jurassic and the Cretaceous. The importance of
documenting the evolution of the Apulia Platform comes from its isolation.
Because the rhythm of growth and decline in the life span of platform
systems is influenced by regional environmental and tectonic conditions
(Föllmi et al. 1994), it is clear that an isolated carbonate bank can easily
register variations in large-scale oceanographic conditions, without any
contamination from hinterland processes: the Apulia carbonate platform
had a position beyond the reach of terrigenous sediments, and it was isolated and ‘‘clean’’. However, the Apulia Platform was presumably influenced by such major geologic phenomena as eustatic sea-level rises, oceanic anoxic events, and intraplate response to distant subduction or collision
processes.
In this report we present for the first time the entire evolution of the
platform, from the Late Jurassic to the Middle Eocene, focusing on its
margin and slope. In fact, along the margin and slope of a carbonate platform, flooding or lowstand events, tectonic episodes, demise of the system,
JOURNAL OF SEDIMENTARY RESEARCH, VOL. 69, NO. 6, NOVEMBER, 1999, P. 1241–1252
Copyright q 1999, SEPM (Society for Sedimentary Geology) 1073-130X/99/069-1241/$03.00
etc. are all amplified and quite often physically visible; in contrast, in the
platform interior or in the deep basin floor such events are in most cases
barely recorded and the sedimentary succession might appear monotonous.
Finally, we document that classic sequence stratigraphic successions may
be the result of episodic failure of a carbonate platform margin or of regional tectonic events.
GEOLOGIC SETTING AND STRATIGRAPHIC FRAMEWORK
The Apulia carbonate platform was a major paleogeographic element of
the southern margin of the Mesozoic Tethys Ocean (Fig. 2). It is one of
the so-called peri-Adriatic platforms, which are comparable to the Bahama
banks in their carbonate facies, shape, size, and subsidence rate and also
in the internal architecture (D’Argenio 1976; Eberli 1991; Eberli et al.
1993).
The Apulia Platform, which is part of the stable and relatively undeformed foreland of the Apennine thrust belt, is bounded on both sides by
basinal deposits; westward the margin is buried under the Apennine thrust
sheets, to the east the adjacent paleogeographic domains are the vast Ionian
Basin to the south and the Umbria–Marche Basin to the north (Fig. 2). To
the west, the Apulia Platform plunges downfaulted underneath the terrigenous sediments of the Apennine foredeep; to the southeast, the Jurassic–
Early Cretaceous margin lies 20–30 km offshore from the present Apulia
coastline (De Dominicis and Mazzoldi 1989; De Alteriis and Aiello 1993).
The Gargano Promontory and the Maiella Mountain, which now is part
of the external Apennine thrust belt (Eberli et al. 1993), are the only areas
where the transition from platform facies to basin facies are exposed on
land (Fig. 2). In the Gargano area this transition has been investigated
extensively in the last decade (Luperto Sinni and Masse 1987; Masse and
Luperto Sinni 1989; Bosellini and Ferioli 1988; Bosellini et al. 1993a,
1993b, 1994; Bosellini and Morsilli 1997; Morsilli and Bosellini 1997;
among others). As a matter of fact, since the mid 1960s AGIP geologists
and the Italian Geological Survey (Pavan and Pirini 1966; Martinis and
Pavan 1967; Cremonini et al. 1971) recognized that the western part of the
promontory is part of the shallow-water Apulia Platform, whereas the eastern part is characterized by slope and basinal deposits (Fig. 3).
The backbone of the Gargano Promontory consists of a thick pile (3000–
3500 m) of Jurassic and Cretaceous shallow-water carbonates. A small
outcrop of Upper Triassic evaporite (Anidriti di Burano) and black limestone is present on the northern seashore (Punta delle Pietre Nere) (Fig. 1).
These rocks have also been encountered in wells Gargano–1 (G.1–Conoco)
and Foresta Umbra–1 (F.U.–Agip) (Fig. 1). The outcropping succession
comprises Upper Jurassic to Eocene carbonate rocks representing platformto-basin settings (Martinis and Pavan 1967; Masse and Luperto Sinni 1989;
Bosellini et al. 1993b). Minor scattered outcrops of Miocene sediments,
unconformably overlying the Cretaceous and Jurassic platform, are present
in many parts of the promontory, mainly along the lowland border zones
(Cagnano Varano, Sannicandro, Apricena, Manfredonia), and also one site
inland near S. Giovanni Rotondo (Fig. 1) (Cremonini et al. 1971).
On the basis of physical stratigraphic relationships and of the presence
of evident bounding surfaces, the Jurassic–Eocene succession can be subdivided into six major packages of sediments, which can be classified as
second-order depositional sequences (Fig. 4).
The lower three sequences (Callovian to Albian) are represented by the
1242
A. BOSELLINI ET AL.
FIG. 1.—Location map of the Gargano
Promontory with main roads. F.U. 5 Foresta
Umbra well (Agip); G.1 5 Gargano 1 well
(Conoco)
entire spectrum of sediments from platform to slope and basin, and the
younger ones (Cenomanian to Lutetian) largely by slope and basin deposits.
Probably the most typical and significant feature of the Gargano slope
and basin setting is the presence of huge megabreccia bodies, which, in
terms of sequence stratigraphic terminology, can be interpreted as typical
lowstand wedges (Sarg 1988).
ARCHITECTURE AND SEQUENCE STRATIGRAPHY OF THE PLATFORM
MARGIN
In this section, a long-term event stratigraphy—as representing long-term
dynamic phenomena including changes in climate, tectonics, and global sea
level—and a sequence stratigraphic organization of the platform margin are
presented. Geometries and types of unconformities (especially on the slope)
and associated lithologies will be discussed.
During the last twenty years, the sequence stratigraphic approach has
been used largely to subdivide sedimentary successions. However, a lively
debate concerning primary causes, physical scale (thickness above all), and
time duration of depositional sequences still exists (Posamentier et al. 1988;
Christie-Blick 1991; Schlager 1991, 1993, 1998; Bosellini et al. 1993b;
Christie-Blick and Driscoll 1995). As is well known, the original definition
of depositional sequences (Mitchum et al. 1977, p. 53) and their bounding
surfaces does not imply any specific genetic mechanism or a time or physical scale. The same can be said for the original definition of systems tracts
(Brown and Fischer 1977).
However, in spite of the original definitions of depositional sequences
and systems tracts, many authors (Vail et al. 1977; Haq et al. 1987; Posamentier et al. 1988; Van Wagoner et al. 1988, Jacquin et al. 1991; among
others) gave to these stratigraphic units a specific genetic significance and
a precise time duration—for example, the depositional sequences are thirdorder cycles (2–3 Myr), and systems tracts are confined within them. Vail
et al. (1991) maintain that the depositional sequences and the associated
systems tracts are generated by short-term relative sea-level fluctuations.
This interpretation is a possible one but, as shown by Schlager (1992),
Bosellini (1993), and Bosellini et al. (1993b), other mechanisms, including
ecological demise and tectonic collapse, can operate as well in carbonate
systems.
Various terms (megasequence, supersequence, composite sequence) have
been used to designate depositional sequences involving a longer time span
(Hubbard 1988; Vail et al. 1991; Mitchum and Van Wagoner 1991; Bosellini 1992). However, the distinction between different orders is largely
arbitrary and often determined by goals and tools of the research (local vs.
regional, seismic profile vs. outcrop analysis, etc.) (Christie-Blick 1991).
According to our personal experience (e.g., Bosellini 1992), depositional
sequences and systems tracts show a self-similarity at different scales
(Greenlee and Moore 1988; Mitchum and Van Wagoner 1991).
In conclusion, if we admit that depositional sequences, particularly in
carbonate successions, can result not only from relative sea-level fluctuations but also from other mechanisms (carbonate system demise, tectonic
collapse) and that their definition is independent of time, then the definition
of their constituent systems tracts must also follow the same logic. In this
report we use the term depositional sequence for unconformity-bounded
stratigraphic units that are different in time scale with respect to the typical
third-order sequences. However, they present the same internal organization, and systems tracts can be easily identified.
Monte Sacro Sequence
FIG. 2.—Restored distribution of platforms and basins in central–southern Italy
during the Jurassic–Cretaceous (from Zappaterra 1990; modified).
The lowermost sequence cropping out in the Gargano has been designated the Monte Sacro Sequence (Morsilli and Bosellini 1997), and its age
EVENT STRATIGRAPHY OF THE APULIA PLATFORM MARGIN
1243
FIG. 3.—Late Jurassic–Early Cretaceous facies
distribution in the Gargano Promontory. 1) inner
platform (Sannicandro Formation); 2) internal
margin (Monte Spigno Formation); 3) external
margin (Monte Sacro Limestone); 4) slope and
basinal deposits (Casa Varfone Formation and
Maiolica); 5) fault of regional importance
(Mattinata Fault). The right-lateral displacement
of the platform margin is due to Neogene strikeslip movements along the Mattinata fault (after
Morsilli and Bosellini 1997).
is Callovian–Valanginian p.p. (the lower boundary is not exposed). The
outcropping part of the sequence (only the upper part, the Tithonian–Berriasian interval) shows an aggradational–progradational trend, interpreted
as the highstand systems tract. The sequence is composed of five lithostratigraphic units (formations with several facies associations) (Fig. 4). From
the inner platform to the basin, they include the following.
(1) Sannicandro Formation. This unit crops out only in the western and
central sector of the Gargano (Fig. 3) and consists of a thick succession of
meter-scale (1–5 m) peritidal parasequences representing lagoonal to su-
pratidal environments. Common lithofacies include mudstone–wackestone
rich in dasycladacean algae, ostracods, gastropods (Nerinea sp.), and peloidal and oolitic packstone–grainstone. Birdseye structures, fenestral fabric, and stromatolite layers associated with flat-pebble breccia are common
at the cycle tops.
(2) Monte Spigno Formation. This unit crops out in the central area of
the Gargano promontory (Fig. 3) and consists mainly of oolitic and oncolitic grainstones. Sedimentary structures include current and wave ripples
and low-angle planar lamination (dune scale). Meniscus cements and key-
FIG. 4.—Chronostratigraphic chart showing formations, second-order sequences, and ‘‘systems tracts’’ of the Gargano Promontory. 1) Inner platform facies; 2) margin
facies; 3) slope and base-of-slope facies; 4) basin facies; 5) megabreccia; 6) hiatuses; 7) bauxites. Time scale after Gradstein et al. (1995).
1244
A. BOSELLINI ET AL.
jacent onlapping succession (Maiolica 2) is Valanginian p.p.–Hauterivian.
No evidence of impregnation of authigenic minerals, like phosphate, glauconite, and Fe–Mn crusts, commonly found associated with drowning surfaces in other areas of the Tethyan domain (Föllmi et al. 1994), has been
observed on the Monte Sacro unconformity surface. The lack of mineralization could be related to the isolation of the Apulia Platform with respect
to continental influx.
Mattinata 1 Sequence
FIG. 5.—White basinal limestones (Maiolica) with thin chert layers. Several slump
features are clearly visible (road cut east of Mattinata).
stone vugs are common features in thin section. This facies suggests a
shallow-water high-energy setting, such as oolitic shoals with local zones
of emersion (small islands with beaches).
(3) Monte Sacro Limestone. This formation occurs in a narrow and arcuate belt from Monte d’Elio to Mattinata (Fig. 3) and consists of massive
wackestone rich in Ellipsactinia, Sphaeractinia, and stromatoporoids.
Boundstone rich in Tubiphytes, corals, and stromatactis are present in some
areas (M. d’Elio). This facies association is interpreted to represent a spectrum of environments from reef front to external margin (Morsilli and Bosellini 1997). The landward boundary with the Monte Spigno Formation is
gradual with a zone of skeletal sands and scattered branching coral colonies
(reef flat).
(4) Casa Varfone Formation. This consists of thick-bedded skeletal rudstone, stromatoporoid breccias, and graded grainstones interfingering with
cherty lime mudstones. Clasts are mainly fragments of Ellipsactinia,
Sphaeractinia, stromatoporoids, and corals. The geometric relationships observable in the field support the interpretation that this facies association
is a proximal to distal, clinostratified slope succession (dip between 10–
158 and 25–288). It is the product of different types of gravity flows, from
hyperconcentrated flows to high-density turbidity currents (sensu Mutti
1992). Upslope it passes into the Monte Sacro Limestone.
(5) Maiolica 1. This is the well known formation of the Mediterranean
basinal sediments of Late Jurassic–Early Cretaceous age. It consists of
white, thin-bedded, micritic limestone with cherts, rich in calpionellids and
Nannoconus, and rich in slump features (intraformational folds, truncation
surfaces) (Fig. 5).
Upper Sequence Boundary.—Near the town of Mattinata and between
Foresta Umbra and Coppa dei Tre Confini, the inclined surface (20–288)
of the platform slope is onlapped by a thick succession of white, thinbedded micritic limestones (Maiolica 2). The physical stratigraphic relationships, directly observable in the field (fig. 5 in Bosellini and Morsilli
1997), are clearly unconformable and suggest the existence of a drowning
unconformity (sensu Schlager 1989). Moreover, the horizontal to subhorizontal onlap pattern of the Lower Cretaceous basinal sediments indicates
that the platform margin had substantial vertical relief above the basin floor
at the time of drowning. The age of the platform and of its coeval flank
and basinal deposits (Monte Sacro Limestone, Casa Varfone Formation,
Maiolica 1) is Late Jurassic–Valanginian p.p., whereas the age of the ad-
This sequence, which spans in age from Valanginian p.p. to early Aptian,
is represented mainly by inner-platform facies and slope-to-basin sediments
(Fig. 4). Margin-bioconstructed facies (rudists and stromatoporoids) occur
only at Monte degli Angeli. The progradational trend (highstand systems
tract) of the sequence is documented by the superposition of the Mattinata
1 Formation (slope facies) over the Maiolica 2 (basin facies). A brief description of these different units follows.
(1) San Giovanni Rotondo Limestone. This is a thick succession (500–
600 m) of shallow-water limestone that can be subdivided into three members (see Claps et al. 1996 for a more detailed description). Member 1
consists of a monotonous and acyclic subtidal unit and represents (probably) the transgressive systems tract of the sequence. Member 2 is represented by a thick cyclic unit characterized by quasi-periodic alternation of
‘‘loferitic’’ beds and centimeter-thick layers of green shales, deposited in
a tidal-flat setting. Member 3 displays a variety of facies including subtidal
high-energy thin-bedded calcarenites at the base of parasequences and domal stromatolites in the upper peritidal units. Members 2 and 3 represent the
middle and late highstand systems tract, respectively.
(2) Monte degli Angeli 1 Limestone. This represents the bioconstructed
margin of the platform and consists of skeletal sand and stromatoporoid
boundstone and rudstone with scattered coral fragments. It is present only
at the Monte degli Angeli (lower part), to the west of Monte S. Angelo
(Fig. 6).
(3) Mattinata 1 Formation. This is a slope and base-of-slope carbonate
succession, rich in gravity-displaced deposits (calciturbidites, breccias), interbedded with cherty micritic limestone, commonly slumped (Luciani and
Cobianchi 1994; Cobianchi et al. 1997). The type section is exposed near
the town of Monte S. Angelo, along the road to Val Carbonara and S.
Giovanni Rotondo (Fig. 6).
(4) Maiolica 2. Same facies of the Maiolica 1 described above.
Upper Sequence Boundary.—There is a rather abrupt change in lithology in slope and basinal settings: both the Maiolica 2 and Mattinata 1
Formation are overlain by a marly and shaly succession, the so-called Scisti
a Fucoidi Formation (Cobianchi et al. 1997), early Aptian–late Albian in
age (see a more detailed description in the following sequence). At Coppa
di Pila, south of Cagnano Varano, the transgressive systems tract of the
following sequence (Mattinata 2 Sequence) is exposed on the platform
margin. A few meters of lower Aptian pelagic limestone disconformably
onlap and overlie rudist mounds associated with oolitic grainstone of Berriasian age. These pelagics are in turn overlain by bioclastic rudstone rich
in orbitolinids and large rudist fragments. From the standpoint of physical
stratigraphy, the sequence boundary is clearly a drowning event: the platform and its bioclastic apron (Mattinata Formation) is abruptly backstepped
some 5–10 km, suggesting that shallow deposition was terminated in a
short time.
Mattinata 2 Sequence
This sequence spans from early Aptian to late Albian and is represented
largely by slope and basin deposits. Equivalent shallow-water deposits are
rare and are present only at Monte degli Angeli and Coppa di Pila and in
the area between Rignano and Manfredonia. The sequence, characterized
EVENT STRATIGRAPHY OF THE APULIA PLATFORM MARGIN
1245
FIG. 6.—Geologic profile (from photograph) between Monte degli Angeli and the town of Monte S. Angelo, The paleoslope, its connection with the platform margins
(Monte degli Angeli), and the thin wedge of Aptian black mudstone (Scisti a Fucoidi), subdividing the two Mattinata sequences are clearly visible. No tectonic tilting.
in the upper part by its strong progradational trend (Fig. 6), is represented
by the following formations.
(1) Masseria Quadrone Limestone. According to Merla et al. (1969), an
inner-platform succession of Albian–Cenomanian? age crops out in the
southern part of Gargano. This succession consists of thick beds of mudstone–wackestone with peloidal packstone–grainstone intercalations. Recently, Luperto Sinni (1996b), described a thin succession (about 30 m) of
mudstone–packstone with late Albian orbitolinids in the same area; the top
consists of a Sellialveolina vialli–bearing limestone, early Cenomanian in
age.
(2) Monte degli Angeli 2 Limestone. This is the late Aptian to middle–
late Albian tract of the Lower Cretaceous margin of the Apulia Platform.
It is grafted onto the underlying Hauterivian–early Aptian platform margin,
but, in places, there may be 1–2 m of pelagic limestone (transgressive
systems tract). The Monte degli Angeli Limestone is rich in sponges, chaetetids, corals, and rudists and represents the bioconstructed margin of this
sequence. The age of the outcropping part of this formation is limited to
the late Aptian, whereas the Albian part is documented only in platformderived breccia occurring in the Mattinata 2 Formation.
(3) Scisti a Fucoidi Formation. This lithological unit, rich in marls and
black shales deposited by episodic anoxic events (Cobianchi et al. 1997),
has a maximum thickness of 120 m and overlies both the Maiolica 2 and
Mattinata 1 formations. It clearly represents a rather abrupt change in the
basin sedimentation and is associated with a standstill in the platform evolution. The Scisti a Fucoidi wedges out against the platform slope (Fig. 6)
and is absent on the platform top, where a few meters of pelagic limestone
or an unconformity surface are present.
(4) Mattinata 2 Formation. This is the same slope and base-of-slope
succession as the Mattinata 1 Formation, previously described, from which
it is separated by a wedge of pelagic limestone with thin beds of black
shale (Scisti a Fucoidi Formation) (Fig. 4). The Aptian–Albian Mattinata
Formation, rich in graded breccias and calciturbidites, represents the highstand systems tract of the sequence. Upslope, it is physically correlatable
with the shallow-water platform of Monte degli Angeli (Fig. 6).
Upper Sequence Boundary.—This is a major erosional unconformity
of regional extent. On the platform it corresponds to well known karst and
bauxite horizons developed over the entire peri-Adriatic region (Crescenti
and Vighi 1964; Accarie et al. 1988; D’Argenio and Mindszenty 1991;
Carannante et al. 1992; Mindszenty et al. 1995). In the slope and base-ofslope settings, the Mattinata and Scisti a Fucoidi formations are unconformably overlain by a huge megabreccia; the boundary is clearly erosional
(Fig. 7).
Monte S. Angelo 1 Sequence
FIG. 7.—The deeply erosional contact between the Monte S. Angelo Megabreccia
and the underlying Scisti a Fucoidi formation (Superstrada road cut, near Ischitella).
This sequence (late Albian–Santonian) (Bosellini et al. 1993b; Neri and
Luciani 1994) consists mainly of slope (Monte S. Angelo Megabreccia and
Monte Acuto 1 Formation) and basinal, fully pelagic sediments (Scaglia 1)
(Fig. 4). The shallow-water tract of the sequence is represented by a small
outcrop in the western and southern part of the promontory. The sequence
consists of the following formations.
(1) Casa Lauriola Limestone. This formation consists of shallow-water,
subtidal to peritidal carbonates, and crops out in two zones, near S. Giovanni Rotondo and near Apricena. It unconformably overlies the mid-Cretaceous bauxite horizon (Merla et al. 1969). In the S. Giovanni Rotondo
area it consists of mudstone–wackestone with thin intercalations of green
marls of late Turonian?–Coniacian p.p. age (Luperto Sinni 1996b), whereas
in the Apricena area the outcropping succession consists of meter-thick
mudstone–wackestone beds with scattered bouquets or clusters of rudists
1246
A. BOSELLINI ET AL.
(radiolitids) and intercalated stromatolite layers, planar or LLH (laterally
linked hemispheroids, sensu Logan et al. 1964) (late Turonian–Senonian).
(2) Monte S. Angelo Megabreccia. This represents the base of the sequence (lowstand systems tract) in the slope and base-of-slope settings. In
the type area, it consists mainly of megabreccia lenses with boulders and
clasts derived from the Lower Cretaceous carbonate platform margin. In
the Ischitella–Vico area (northern Gargano), graded breccias and calciturbidites are intercalated with pelagic limestones. The thickness can be as
much as 200 m. This unit, late Albian–Cenomanian in age (Neri and Luciani 1994), represents the slope and base-of-slope accumulation derived
from large platform-margin failures.
(3) Monte Acuto 1 Formation. This is a succession deposited in slope
and base-of-slope settings (Neri 1993; Neri and Luciani 1994). It consists
of white, chalky and cherty lime mudstones, alternating with coarse bioclastic calciturbidites, breccias, and megabreccias; clasts are both of platform and slope–basin derivation. The entire M. Acuto Formation (1 and 2)
has been divided into five units (Neri 1993): (a) a basal condensed pelagic
interval (Unit 1), which may be interpreted as the transgressive systems
tract; (b) two bodies of calciturbidites (Units 2 and 4) (highstand systems
tract), separated by a Scaglia tongue (Unit 3), some 50 m thick, (Santonian–
early Campanian in age), and (c) a pelagic interval on top of the succession
(Unit 5). Facies associations of Units 2 and 4 are representative of a system
of laterally coalescing depositional lobes (Neri 1993). Only Units 1 and 2
constitute the Monte Acuto 1 Formation.
(4) Scaglia 1. This is the basinal counterpart of the sequence and consists of thin-bedded, chalky and cherty white lime mudstones.
Upper Sequence Boundary.—Even if there is no control from the platform section, we consider the Scaglia tongue (Unit 3) as a possible transgressive systems tract of a younger depositional sequence of Santonian–
early Danian age (Fig. 4). Moreover, this sequence boundary has also been
recognized in offshore seismic profiles, with a marine onlap that probably
reflects a partial drowning of the Apulia Platform (De Alteriis and Aiello
1993).
Monte S. Angelo 2 Sequence
This sequence comprises only slope and basin facies. Two formations
are present.
(1) Monte Acuto 2 Formation. This corresponds to units 3, 4, and 5 as
defined by Neri (1993). Unit 3, the Scaglia tongue previously described,
consists of pelagic sediments with some breccia and turbidite layers, which
seem to be more common upslope. Unit 4 is a thick calciturbidite body,
like unit 2. The last unit is represented by pelagic sediments with some
thin bioclastic turbidite of Danian age (M. trinidanensis zone) (Bosellini et
al. 1993b).
(2) Scaglia 2. Lithologically, this succession is the same as Scaglia 1
and crops out extensively along the northeastern part of the Gargano.
Upper Sequence Boundary.—The Monte Acuto 2 and Scaglia 2 formations are overlain by the Grottone Megabreccia or by laterally equivalent
calciturbidites of the Peschici Formation (Bosellini et al. 1993a, 1993b) of
Middle Eocene age. The contact is everywhere unconformable and deeply
erosional.
Monte Saraceno Sequence
The youngest depositional sequence of the Gargano succession is 250–
300 m thick and entirely Middle Eocene (Lutetian) in age (Bosellini et al.
1993a, 1993b) (Fig. 4). The Monte Saraceno Sequence is separated from
the underlying Upper Cretaceous and Paleocene substratum (Monte Acuto
Formation and Scaglia) by a pronounced unconformity, and is represented
almost entirely by slope and base-of-slope deposits. It is the result of the
margin collapse of an Early Eocene carbonate platform and of its Cretaceous–Paleocene ‘‘basement’’, followed by the installation and prograda-
FIG. 8.—The marine onlap of the Peschici Formation (Lutetian) over the deeply
eroded Scaglia (left) of late Turonian–early Coniacian age (Vieste sea-cliff).
tion of a nummulite platform over the adjacent basinal deposits. It consists
of the following formations.
(1) Grottone Megabreccia. The basal lowstand systems tract is a 50–60
m thick megabreccia consisting of several channelized bodies separated by
amalgamation surfaces. The Grottone Megabreccia records a series of catastrophic debris-flow episodes resulting from the dismantling of a Cretaceous and Early Eocene platform (lowstand systems tract).
(2) Peschici Formation. This is a thick succession (350 m) of graded
breccias and calciturbidites alternating with pelagic marlstone onlapping
(marine onlap) a huge scar on the underlying Scaglia (Fig. 8), deeply eroded into the late Turonian–early Campanian strata (Bosellini et al. 1993b).
This large hiatus has also been recognized offshore (De Alteriis and Aiello
1993).
(3) Punta Rossa Limestone. This is the Eocene basinal (proximal) facies,
consisting of chalky, whitish and thin-bedded lime mudstone. There are
several 20–30 m thick calciturbidites within the succession, which appears
to be characterized by frequent truncation surfaces and discordances (slump
scars).
(4) Monte Saraceno Limestone. This is the uppermost unit of the sequence and is represented by clinostratified, coarse calcarenites and rudstones, consisting entirely of Nummulites and Dyscociclinidae. In places,
floatstones rich in branching corals, gastropods, and bivalves occur. This
unit can be interpreted as a proximal slope with small patch reefs growing
on the deeper margin and is probably related to a forced regression (lowstand shelf edge); in fact, no progradation of the system is observed, as it
should be in case of depositional regression.
PROCESSES AND EVENTS CONTROLLING MARGIN ARCHITECTURE:
DISCUSSION
In this section, the various geological processes and events (Fig. 9) that
punctuated and gave rise to the sequence stratigraphic architecture of the
platform margin will be analyzed and discussed.
The Valanginian Drowning Unconformity
Physical relationships and age determination of the sedimentary succession clearly document that the Apulia Platform, moderately prograding during the Late Jurassic–Valanginian p.p. interval, was stopped in its evolution
in the early Valanginian and then onlapped by basinal sediments (Maiolica
2) (Bosellini and Morsilli 1997). According to all available paleontological
data (Chiocchini 1987; Barattolo and Pugliese 1987; De Castro 1987; Parente, personal communication), the age of the uppermost part of the shallow-water carbonate platform in Apulia and southern Apennines is Berriasian–earliest Valanginian, whereas the Gargano onlapping basinal succession is early Valanginan at the toe of the slope (Calpionellites Zone) and
EVENT STRATIGRAPHY OF THE APULIA PLATFORM MARGIN
1247
FIG. 9.—The various events that controlled the
sequence stratigraphic architecture of the Apulia
Platform margin along the Gargano transect.
O.A.E. column after Jenkyns (1991).
progressively younger upward (latest Valanginian–early Hauterivian; subzone NC4a of Bralower 1987). We can therefore infer a hiatus from a
minimum of less than 1 Myr at the slope toe to a maximum of 6 Myr
toward the top of the platform.
The Late Jurassic was a time of rapid subsidence and widespread platform growth on the margins of the central North Atlantic and of the Ligurian Ocean (western Tethys). However, these carbonate platforms were
drowned and their growth suddenly interrupted during the Valanginian.
This phenomenon and the associated drowning unconformities are well
known in a large part of world, from the Caribbean to eastern Arabia. The
Valanginian drowning is documented (see references in Bosellini and Morsilli 1997) in: (1) the western continental margin of the Atlantic Ocean
(Scotian Shelf, Baltimore Canyon, Caribbean); (2) the eastern continental
margin of the Atlantic Ocean (Iberia, Morocco); (3) the western peri-Alpine
domain, i.e., the northern and western continental margin of the Ligurian
Ocean and the margin of Iberia (southern France, Helvetic Alps, Estremadura, eastern Prebetic and Betic areas); and (4) the margins of the Adria
Plate (Apulia Platform). Recently, additional data have been presented by
Stoll and Schrag (1996). According to these authors, strontium-isotope data
from the deep ocean (Blake–Bahama Basin, off the eastern coast of United
States) from an interval spanning 7 million years in the Berriasian–Valanginian would imply that global sea level fluctuated about 50 meters over
time scales of 200,000 to 500,000 years.
Interpretation of widespread episodic synchroneity in carbonate platform
ecologic behavior is controversial (Föllmi et al. 1994). Besides eustasy,
proposed mechanisms include widespread eutrophism (Hallock and Schlager 1986), globally increased tectonic movements (Eberli 1991), large-scale
oceanic anoxia (Vogt 1989; Schlager and Philip 1990; Jenkyns 1991;
among others), and pulses in ocean-crust formation (Mullins et al. 1991).
As documented in other carbonate platform during the same time (Schlager 1991, 1998; Erlich et al. 1993; Föllmi et al. 1994), the Valanginian
relative sea-level rise was associated with an environmental crisis that reduced the potential growth of the previously healthy platform. However,
the Apulia carbonate platform had a position beyond the reach of terrigenous sediments; it was isolated and ‘‘clean’’, at least during Valanginian
time. In conclusion, the worldwide Valanginian drowning unconformities
and sea-level fluctuations suggest some kind of eustatic mechanism (glacio-
eustatic, geoidal eustasy, pulses in ocean-crust formation, etc.), which can
also be invoked for the onlap geometry and associated drowning unconformity observed in the Gargano.
The Aptian–Albian Anoxia
The Apulia Platform and the adjacent slope suddenly became inactivate
during the early Aptian (Figs 4, 6). This event coincides with a relatively
abrupt change in open marine sedimentation: the pelagic (and cherty) coccolith-rich, white lime mudstones of the Maiolica 2 Formation are overlain
by marly and shaly sediments, the so-called Scisti a Fucoidi Formation.
This pelagic unit is widespread along the southern continental margin of
the Tethys ocean and is characterized by a well developed cyclicity expressed by limestone–marlstone couplets and by redox rhythms (Erba 1992;
Tornaghi et al. 1989; among others). In the Gargano, the Scisti a Fucoidi
Formation has a thickness of 100–120 m and consists mainly of marls and
marly limestone. Two organic-carbon-rich black shales are scattered within
the Albian tract of this unit (Cobianchi et al. 1997; Cobianchi et al. 1999).
Because the base of the Scisti a Fucoidi Formation is early Aptian, there
seems to be no hiatus in the slope-to-basin setting. The hiatus shown in
Figure 4 on the platform top is inferred and not really detectable on a
biostratigraphic basis.
The onset of deposition of the Scisti a Fucoidi Formation, so rich in
marls and with episodic organic-carbon-rich black shales, was clearly not
related to the sedimentary dynamics of the Apulia Platform. Aptian–Albian
units equivalent to the Gargano Scisti a Fucoidi are well known from the
southern Alps to the Apennines (the Umbria–Marche basin is the type
locality) (Arthur and Fischer 1977; Cresta et al. 1989; Bersezio 1992), and
Greece (Skourtsis-Coroneou et al. 1995) and Cretaceous anoxia events occurred on a global scale, related to worldwide oceanographic and climatic
conditions (Schlanger and Jenkyns 1976; Jenkyns 1980, 1991; Arthur et
al. 1990; Bralower et al. 1994). During the Cretaceous five anoxic events
took place in the ocean (Jenkyns 1991). Oceanic Anoxic Event 1 (O.A.E.
1), subdivided into OAE 1A, 1B, and 1C, occurred during the late Barremian interval and continued through the Albian, O.A.E. 2 during the Cenomanian–Turonian transition and O.A.E. 3 during the Coniacian–Santonian
interval (Arthur and Schlanger 1979; Jenkyns 1980, 1991; Bralower et al.
1248
A. BOSELLINI ET AL.
FIG. 10.—The amphitheater-like contact
between the Monte S. Angelo Megabreccia and
the adjacent Lower Cretaceous platform
carbonates. 1) Monte Spigno Formation; 2)
Monte Sacro Formation; 3) Monte degli Angeli
Formation; 4) Mattinata Formation; 5) Scisti a
Fucoidi Formation; 6) Monte S. Angelo
Megabreccia; 7) Monte Acuto Formation; 8)
Monte Saraceno Sequence; 9) Quaternary
deposits; 10) erosional unconformities; 11)
paraconformable sequence boundary; 12) faults.
1994). Large amounts of organic carbon were deposited and preserved in
the marine sediments as the result of the development of poorly oxygenated
waters and the expansion of the oxygen-minimum zones.
As suggested by Jenkyns (1991), a particularly thick column of deoxygenated water developed in the Umbria–Marche–Ionian deep-water basin
and was carried onto the adjacent carbonate platforms during the various
Cretaceous transgressions. This water lapped onto the Apulia Platform and
fostered regional deposition of carbon-rich facies (Scisti a Fucoidi Formation). Causal mechanisms of changes in atmospheric CO2 concentrations
and greenhouse intensity, globally increased carbon transfer rates into the
sedimentary reservoirs, global positive d13C excursion, rise in nutrient input into the oceans etc., and concomitant sea-level rise are extensively
discussed by Föllmi et al. (1994) and Drzewiecki and Simo (1997). However, exact relationships between rising sea level and anoxia, and the source
of oxygen-depleted waters, remain problematic (Jenkyns 1991). It is not
our intention to solve this problem here: we present only data and it is
reasonable to infer that the early Aptian drowning and retreat of the Apulia
Platform might be associated with the deposition of the Scisti a Fucoidi
Formation. Because this unit appears to be the result of specific worldwide
oceanographic and climatic conditions, we suggest a causal link between
the platform standstill and the Aptian–Albian poorly oxygenated marine
waters.
The Late Albian–Cenomanian Collapses
According to our field observations (Bosellini et al. 1993a, 1993b), the
Monte S. Angelo Megabreccia is the result of major collapses of the platform margin that occurred in the late Albian–Cenomanian interval during
a time span of about 6 Myr (Neri and Luciani 1994). At least three superimposed megabreccia bodies can be distinguished in the northern Gargano
area, whereas to the south there is a single amalgamated megabreccia unit.
As visible in plan view (Fig. 10), the geometry of the contact between
the megabreccia and the adjacent Lower Cretaceous platform carbonates is
an amphitheater-like feature, and this rules out the presence of a paleofault
as suggested by previous authors. But this is not the only indentation observed along the edge of the Apulia carbonate platform; there are several
other scalloped features (Bosellini et al. 1993b, fig. 13). For example, a
large scallop that incises the almost rectilinear Apulia Platform margin, has
recently been identified by Bosellini and Morsilli (1994). This reentrant,
which grossly corresponds to the present-day Lake of Varano (Fig. 11), is
in part sutured by Cretaceous breccias and megabreccias and by a thick
Miocene succession. Supported by detailed geologic mapping and by several stratigraphic data, Bosellini and Morsilli (1994) believe that the depression that accommodates the Lake of Varano originally was a submarine
slide scar of Cretaceous age resulting from a large-scale platform collapse.
It is well known (Crescenti and Vighi 1964; D’Argenio and Mindszenty
1991, 1992; Mindszenty et al. 1995) that pronounced exposures of the
shallow-water platforms occurred over the entire southern Apennines and
Apulia during the mid-Cretaceous. Accarie et al. (1988) document a Cenomanian unconformity in the Maiella Mountain, some 150 km northwest
of Gargano, with karst cavities penetrating into the Lower Cretaceous substratum for about 50 meters; hiatuses associated with the bauxite horizons
are included within the late Albian–early Cenomanian interval. In the
Matese mountains, Ruberti (1993) documents two gaps, the lower one extending from the middle Albian to the Cenomanian p.p., the upper one
corresponding to the lower–middle Turonian. Hiatuses extending from the
Albian p.p. to the early Cenomanian are also reported by Carannante et al.
(1992) from various platform sections in the Campania region.
Recently, Mindszenty et al. (1995) reviewed the general problem of the
mid-Cretaceous emergences of the southern Apennine carbonate platforms
and of the associated bauxite and paleokarst horizons and unconformities.
Their conclusion is that the ‘‘rather monotonous story’’ of the Cretaceous
carbonate platforms is interrupted by two major regional unconformities,
one of them Albian–Cenomanian, the other Turonian. According to Crescenti and Vighi (1964), the age of the Gargano bauxites is Turonian, whereas the Gargano collapses and megabreccias are late Albian to Cenomanian
(Neri and Luciani 1994). Therefore, they are coeval with the older bauxite
and paleokarst horizons. However, quite recently, it has been shown
(Grötsch et al. 1993; Fernández-Mendiola and Garcı́a-Mondéjar 1997) that
a late Albian phase of global karstification is present in many carbonate
platforms of the world (Slovenia, Mid-Pacific guyots, Venezuela, BascoCantabrian basin, etc.). It should be ultimately related to a short-term regressive–transgressive cycle with an amplitude of more than 100 m.
General stratigraphy and geology demonstrate that the Gargano collapse
events were coeval with a general emergence of the southern Apennines
and Apulia and of many carbonate platforms around the world (Grötsch et
al. 1993). Therefore, it is tempting to consider a relative sea-level lowstand
as the triggering mechanism. The generalized mid-Cretaceous emersions of
the southern Apennines and Apulia carbonate platforms have been interpreted by many authors (D’Argenio et al. 1987; D’Argenio and Mindszenty
1991, 1992; Bosellini 1989; Eberli 1991; Mindszenty et al. 1995) as the
EVENT STRATIGRAPHY OF THE APULIA PLATFORM MARGIN
1249
FIG. 12.—The pelagic interval (‘‘transgressive systems tract’’) overlying the Monte S. Angelo Megabreccia and abruptly overlain by gravity-displaced debrites
(‘‘highstand system tract’’). The erosional contact represents the downlap surface of
the prograding depositional system of the Monte Acuto Formation (Monte S. Angelo–Manfredonia road).
be related to seismic shocks associated with the incipient uplift of Apulia,
which culminated with its generalized emersion in Cenomanian and Turonian times.
In conclusion, the result of this story is that the classic sequence stratigraphic organization of a slope-to-basin succession can simply derive from
platform dismantling. In fact, margin failure interrupts carbonate production by bioconstructors or by sedimentary processes (oolite and skeletal
sands). After megabreccia accumulation (‘‘lowstand systems tract’’) and
before the margin is recolonized, there necessarily follows a period of starvation along the entire slope and base-of-slope tract: pelagic, thin-bedded
sediment accumulates on the ‘‘lowstand’’ megabreccia, simulating the
transgressive systems tract and the associated condensed section (Fig. 12).
Finally, once margin deposition resumes, sediment export starts and the
entire system begins to prograde again (‘‘highstand systems tract’’).
Santonian–Campanian Retreat of the Platform Margin
FIG. 11.—The Varano Lake (A) is a morphological feature inherited from a large
scallop (B) of the Cretaceous Apulia Platform edge (modified from Bosellini and
Morsilli, 1994). 1) Monte Spigno Formation; 2) Monte Sacro Formation; 3) slope
and basin deposits; 4) depositional platform edge; 5) erosional margin.
foreland reaction to distant plate collision (lithospheric bulge). We are also
in favor of a tectonic origin for the Gargano megabreccias for several
reasons, including: (a) no major karst or bauxite horizon seems to be present in the platform interior during the late Albian to Cenomanian; (b) it is
well known that the Albian–Cenomanian emergence resulted in a karstbauxite surface, and this dissolution process is not expected to generate
sediment export to the basin; on the contrary, the adjacent basin should be
in starved conditions (see Bosellini 1993); (c) the megabreccia boulders do
not show any sign of previous exposure and karstification (vadose cements,
red color, terra rossa, etc.); and (d) the Cenomanian–Turonian time is a
period of enhanced sea-level rise and platform drowning all over the world
(Haq et al. 1987; Schlager and Philip 1990).
We believe that the triggering mechanism of the Gargano collapses might
The ‘‘highstand’’ deposits (coarse bioclastic calciturbidites forming progradational lobe cycles) of the Monte S. Angelo 1 Sequence of the southern
Gargano area are overlain quite abruptly by pelagic cherty limestone (Scaglia 2, Fig. 4). This is a wedge-shaped unit with a maximum thickness of
50–60 m, thinning upslope and inserted as a ‘‘Scaglia 2 tongue’’ within
the Monte Acuto Formation. On the basis respectively of planktonic foraminifers and nannoplankton, this pelagic unit has been referred to the Santonian–early Campanian by Neri and Luciani (1994) and to the late Santonian by Laviano and Marino (1996). There seems to be no hiatus between
the sequences Monte S. Angelo 1 and 2 in the basin setting. Upslope,
however, erosional hiatuses responsible for the omission of the whole G.
elevata zone (about 3 Myr) locally occur.
The pelagics are characterized upslope by 1–5-m-thick platform-derived
megabreccias, commonly deeply channelized, by isolated platform olistoliths up to 4–5 m in size, by massive breccia and paraconglomerates derived
from cannibalization of slope-to-basin deposits (pelagic lime mudstone,
chert, and calciturbidites), and by slumpings and slump scars, resulting in
significant hiatuses, recognizable biostratigraphically (Neri and Luciani
1994).
The ‘‘Scaglia tongue’’ marks the base of the Monte S. Angelo 2 Sequence and is overlain by a succession of coarse calciturbidites, about 150
m thick, the base of which can be referred to the early Campanian p.p. It
testifies to a retreat of the margin and a strong reduction in platform productivity, although the presence of bioclastic turbidites within the unit indicates that the carbonate factory did not stop entirely. Because impressive
1250
A. BOSELLINI ET AL.
gravity processes affected the slope and the platform margin, we tend to
believe that a simple rise in sea level cannot completely account for them.
A significant landward retreat of the margin of the Apulia platform during early Campanian times is also recorded in the Fasano–Ostuni area,
some 200 km to the southeast (Murge, Fig. 1) (Luperto Sinni and Borgomano 1989; Pieri and Laviano 1989; Guarnieri et al. 1990; Luperto Sinni
1996a; Luperto Sinni and Reina 1996a, 1996b) and in the Adriatic offshore
(De Alteriis and Aiello 1993). The pre-Campanian platform margin is located a few tens of kilometers offshore, whereas the Campanian margin is
documented about 5–10 km inland of the present-day coastline.
It is not clear what kind of mechanism controlled such a transgression:
tectonics or eustasy. According to Simo et al. (1993), a prominent sequence
boundary (seaward shift of the coastal onlap followed by fast transgression)
is recorded at the Santonian–Campanian transition in carbonate successions
in a number of very different paleogeographic settings, such as the Caribbean, Western Europe, Adria, and North Africa, thus suggesting a primary
eustatic control. However, the frequent occurrence in the discussed stratigraphic interval, both in Gargano and Murge areas, of megabreccia lenses,
olistolith swarms, and significant gravity-displaced slope-to-basin deposits
suggests that downfaulting and local tectonically induced collapses may
have been important mechanisms in the platform retreat. Further data are
required, especially from Murge, to solve the problem, but it seems reasonable that the intraplate stress controlling the Albian–Cenomanian collapses was still at work during Santonian–Campanian time.
The Middle Eocene Collapse
The last depositional sequence of the Gargano succession is the Monte
Saraceno Sequence. It is separated from the underlying Upper Cretaceous
and Paleocene substratum (Scaglia and Monte Acuto Formations) by a
pronounced unconformity associated with a major erosional hiatus (Fig. 4).
The age of Eocene catastrophic event is bracketed between the Morozovella
trinidadensis zone (Danian; age of the youngest sample of the underlying
sequence) and the Morozovella lehneri zone (middle Lutetian; age of upper
pelagic chalk). The presence of nummulites of probable Lutetian age in the
matrix of the basal megabreccia confines its age to the initial Lutetian or
the top of the Ypresian, a time (between 49 and 45.5 Myr) of a major
lowstand event, according to Haq et al. (1987). We must admit, however,
that the timing of the Grottone Megabreccia is based on the presence of
very poorly preserved nummulites. Moreover, the biostratigraphic dating
by this fossil group certainly does not allow resolution at the 0.5–1 Myr
range. The extent of the associated hiatus may vary from 12–15 to more
than 40 Myr in the eastern Gargano (see Fig. 4), where the Peschici Formation, dated as mid-Lutetian, disconformably overlies the Scaglia Formation, the uppermost part of which is Coniacian in age (Marginotruncana
sigali zone) (Bosellini et al. 1993b).
The Eocene was a time of general uplift and subaerial exposure of Apulia
and present-day southern Adriatic Sea. A major unconformity at the top of
Cretaceous carbonates is documented by outcrops, well data, and seismic
data (De Dominicis and Mazzoldi 1989; Colantoni et al. 1990; De Alteriis
and Aiello 1993; Argnani et al. 1993). It is worth noting that this unconformity is present in all offshore wells of the Adriatic, suggesting that the
uplift was associated with the foreland bulge of the west-verging Dinarides–Hellenides thrust belts (Gambini and Tozzi 1996).
Once again, a classic sequence stratigraphic succession—the Monte Saraceno Sequence—is the result of a ‘‘tectonic’’ relative sea-level fluctuation.
CONCLUSIONS
The long-term event stratigraphy of the Apulia Platform margin and
slope along the Gargano transect is punctuated by five major events. These
events subdivide the succession into six second-order sequences and constitute the framework of its stratigraphic architecture.
(1) Valanginian drowning unconformity. Physically visible as an onlap
of basinal sediments onto the Jurassic–Berriasian platform slope, this abrupt
sea-level rise is documented worldwide, from the deep ocean to the Atlantic
continental margins, Iberia, Alps, etc. It is reasonable to infer that some
kind of eustatic mechanism (glacio-eustatic, geoidal eustasy, pulse in ocean
crust formation, etc.) is responsible for the onlap geometry and the associated drowning unconformity observed in the Gargano.
(2) Early Aptian–Albian drowning and demise of the platform. This
event is coeval with the onset of deposition of the Scisti a Fucoidi Formation in the basin. This unit, rich in organic deposits and black shales,
records several global Cretaceous anoxia events. We suggest (cf. Jenkyns
1991) that a particularly thick column of deoxygenated water lapped onto
the Apulia Platform and fostered regional deposition of carbon-rich facies.
As a result, the carbonate platform factory was temporarily turned off,
giving way to a substantial drowning and retreat of the platform system.
(3) Late Albian–Cenomanian collapse. The slope and base-of-slope settings of the Gargano are characterized by huge megabreccia bodies and
other gravity-displaced deposits. According to detailed field work, these
megabreccias are the result of major collapses of the platform margin and
are coeval with a general emergence of the southern Apennines and Apulia
and of many carbonate platforms of the world (Grötsch et al. 1993; Fernández-Mendiola and Garcı́a-Mondéjar 1997). Because no data indicative
of a previous exposure have been found in the megabreccia elements, however, it is suggested that the triggering mechanism of the Gargano collapses
could be related to seismic shocks associated with the incipient uplift of
Apulia, which culminated in its generalized emersion in Cenomanian and
Turonian times. This uplift was the result of foreland reaction to distant
plate collision (Mindszenty et al. 1995).
(4) Santonian–Campanian retreat of the platform margin. This is the
less well documented event. A 50–60-m-thick pelagic tongue inserted into
the bioclastic calciturbidite and breccia slope succession testifies to a retreat
of the margin and a strong reduction in platform productivity. A significant
landward retreat of the Apulia Platform margin, both in the Adriatic offshore and in southern Apulia, is also documented.
(5) Eocene uplift and platform-margin collapse. A major erosional unconformity separates the Middle Eocene (Lutetian) bioclastic turbidites
from the underlying Upper Cretaceous or Paleocene pelagics. The Eocene
was a time of general uplift and subaerial exposure of Apulia and the
present-day southern Adriatic Sea, most probably related to the foreland
arching of the west-verging Dinarides-Hellenides thrust belts.
We hope that our data on the Gargano stratigraphy will be regarded as
a further contribution to construct a global stratigraphic template for Cretaceous chronostratigraphic correlation.
ACKNOWLEDGMENTS
The authors gratefully acknowledge reviewers Karl Föllmi, Robert W. Scott, and
Helmut Weissert for very helpful and constructive comments. The careful editorial
work by John B. Southard is very much appreciated. Financial support was provided
by grants from the Italian Consiglio Nazionale delle Ricerche (CNR Grants 94.00
170, 95.00 349, 96.00 273).
REFERENCES
ACCARIE, H., BEAUDOIN, B., CUSSEY, R., JOSEPH, P., AND TRIBOULET, S., 1988, Dynamique sédimentaire et structurale au passage plate-forme/basin, les faciés carbonates Cretacés du Massif
de la Maiella (Abruzzes, Italie): Società Geologica Italiana, Memorie, v. 36 (1986), p. 217–
231.
ARGNANI, A., FAVALI, P., FRUGONI, F., GASPERINI, M., LIGI, M., MARANI, M., MATTIETTI, G., AND
MELE, G., 1993, Foreland deformational pattern in the Southern Adriatic Sea: Annali di
Geofisica, v. 36, p. 229–247.
ARTHUR, M.A., AND FISCHER, A.G., 1977, Upper Cretaceous–Paleocene magnetic stratigraphy
at Gubbio, Italy. 1. Lithostratigraphy and sedimentology: Geological Society of America,
Bulletin, v. 88, p. 321–479.
ARTHUR, M.A., AND SCHLANGER S.O., 1979, Cretaceous ‘‘Oceanic Anoxic Events’’ as casual
factors in development of reef-reservoired giant oil fields: American Association of Petroleum Geologists, Bulletin, v. 63, p. 870–885.
EVENT STRATIGRAPHY OF THE APULIA PLATFORM MARGIN
ARTHUR, M.A., JENKINS, H.C., BRUMSACK, H.J., AND SCHLANGER, S.O., 1990, Stratigraphy, geochemistry, and paleoceanography of organic carbon-rich Cretaceous sequences, in Ginsburg,
R.N., and Beaudoin, B. eds., Cretaceous resources, events and rhythms: Dordrecht, The
Netherlands Kluwer Academic Publishers, v. 304, p. 75–119.
BARATTOLO, F., AND PUGLIESE, A., 1987, Il Mesozoico dell’Isola di Capri: Quaderni Accademia
Pontaniana, n. 8, p. 1–37.
BERSEZIO, R., 1992, La successione aptiano–albiana del Bacino Lombardo: Giornale di Geologia, v. 54, p. 125–146.
BOSELLINI, A., 1992, The continental margins of Somalia. Structural evolution and sequence
stratigraphy, in Watkins, J.S., Zhiqiang, F., and McMillen, K.J., eds., Geology and Geophysics of Continental margins: American Association of Petroleum Geologists, Memoir 56,
p. 185–205.
BOSELLINI, A., 1993, Sequence stratigraphy in carbonate successions: some Italian examples:
Offshore Technology Conference, Houston, Texas, 3–6 May, p. 249–255.
BOSELLINI, A., 1989, Dynamics of Tethyan carbonate platforms, in Crevello, P.D., Wilson, J.L.,
Sarg, J.F., and Read, J.F., eds., Controls on Carbonate Platform and Basin Development:
SEPM, Special Publication 44, p. 1–13.
BOSELLINI, A., AND FERIOLI, G.L., 1988, Sequenze deposizionali e discordanze nel Gargano
meridionale: Società Geologica Italiana, 748 Congresso, Sorrento, Irtaly, Atti, v. A, p. 49–
54.
BOSELLINI, A., AND MORSILLI, M., 1994, Il Lago di Varano (Gargano, Puglia settentrionale): una
nicchia di distacco da frana sottomarina cretacea: Università di Ferrara, Annali (N.S.), Sezione Scienze della Terra, v. 5, p. 39–52.
BOSELLINI, A., AND MORSILLI, M., 1997, A Lower Cretaceous drowning unconformity on the
eastern flank of the Apulia Platform (Gargano Promontory, southern Italy): Cretaceous Research, v. 18, p. 51–61.
BOSELLINI, A., NERI, C., AND LUCIANI, V., 1993a, Guida ai carbonati cretaceo–eocenici di scarpata
e bacino del Gargano (Italia meridionale): Università di Ferrara, Annali, Sezione Scienze
della Terra, supplemento, v. 4, p. 1–77.
BOSELLINI, A., NERI, C., AND LUCIANI, V., 1993b, Platform margin collapses and sequence stratigraphic organization of carbonate slopes: Cretaceous–Eocene, Gargano Promontory, southern Italy: Terra Nova, v. 5, p. 282–297.
BOSELLINI, A., NERI, C., AND LUCIANI, V., 1994, Platform margin collapses and sequence stratigraphy of slopes carbonates (Cretaceous–Eocene, Gargano Promontory, southern Italy):
International Association of Sedimentologists, 15th Regional Meeting, April 1994, Ischia,
Italy, Excursion A7, p. 125–161.
BRALOWER, T.J., 1987, Valanginian to Aptian calcareous nannofossil stratigraphy and correlation with the upper M-sequence Magnetic Anomalies: Marine Micropaleontology, v. 11, p.
293–310.
BRALOWER, T.J., ARTHUR, M.A., LECKIE, R.M., SLITER, W.V., ALLARD, D.J., AND SCHLANGER, S.
O., 1994, Timing and paleoceanography of oceanic dysoxia/anoxia in the late Barremian to
early Aptian (Early Cretaceous): Palaios, v. 9, p. 335–370.
BROWN, L.F., AND FISCHER, W.L., 1977, Seismic-stratigraphy interpretation of depositional systems: examples from Brazil rift and pull-apart basins, in Payton, C.E., ed., Seismic Stratigraphy, Applications to Hydrocarbon Exploration, American Association of Petroleum Geologists, Memoir 26, p. 213–248.
CARANNANTE, G., D’ARGENIO, B., DELLO IACOVO, B., FERRERI, V., MINDSZENTY, A., AND SIMONE,
L., 1992, Studi sul carsismo cretacico dell’Appennino Campano: Società Geologica Italiana,
Memorie, v. 41 (1988), p. 733–759.
CHIOCCHINI, M., 1987, Il Giurassico in facies di margine della piattaforma carbonatica
nell’Appennino centro-meridionale: breve sintesi dei dati paleontologici e stratigrafici: Società Paleontologica Italiana, Bollettino, v. 26, p. 303–308.
CHRISTIE-BLICK, N., 1991, Onlap, offlap, and the origin of unconformity-bounded depositional
sequences: Marine Geology, v. 97, p. 35–56.
CHRISTIE-BLICK, N., AND DRISCOLL, N.W., 1995, Sequence stratigraphy: Annual Review of Earth
and Planetary Sciences, v. 23, p. 451–478.
CLAPS, M., PARENTE, M., NERI, C., AND BOSELLINI, A., 1996, Facies and cycles of the S. Giovanni
Rotondo Limestones (Lower Cretaceous, Gargano Promontory, Southern Italy): the Borgo
Celano Section: Università di Ferrara, Annali, Sezione Scienze della Terra, supplemento, v.
7, p. 1–35.
COBIANCHI, M., LUCIANI, V., AND BOSELLINI, A., 1997, Early Cretaceous nannofossils and planktonic foraminifera from northern Gargano (Apulia, southern Italy): Cretaceous Research, v.
18, p. 249–293.
COBIANCHI, M., LUCIANI, V., AND MENEGATTI, A., 1999, The Selli level of the Gargano Promontory, Apulia, southern Italy: foraminiferal and calcareous nannofossil data: Cretaceous
Research, v. 20, p. 255–269.
COLANTONI, P., TRAMONTANA, M., AND TEDESCHI, R., 1990, Contributo alla conoscenza
dell’avampaese apulo: struttura del Golfo di Manfredonia: Giornale di Geologia, v. 52, p.
145–162.
CREMONINI, G., ELMI, C., AND SELLI, R., 1971, Note illustrative della carta geologica d’Italia,
Foglio 156 ‘‘S. Marco in Lamis’’: Servizio Geologico d’Italia, Roma, 66 p.
CRESCENTI, U., AND VIGHI, L., 1964, Caratteristiche, genesi e stratigrafia dei depositi bauxitici
cretacici del Gargano e delle Murge; cenni sulle argille con pisoliti bauxitiche del Salento:
Società Geologica Italiana, Bollettino, v. 83, p. 285–337.
CRESTA, S., MONECHI, S., AND PARISI, G., 1989, Stratigrafia del Mesozoico e Cenozoico nell’area
Umbro–Marchigiana, Itinerari geologici sull’Appennino Umbro–Marchigiano (Italia): Memorie descrittive della Carta Geologica d’Italia, Ministero dell’Ambiente, Servizio Geologico d’Italia, Roma, v. 39, p. 185.
D’ARGENIO, B., 1976, Le piattaforme carbonatiche periadriatiche. Una rassegna di problemi nel
quadro geodinamico mesozoico dell’area mediterranea: Società Geologica Italiana, Memorie,
v. 13 (1974), p. 137–159.
D’ARGENIO, B., AND MINDSZENTY, A., 1991, Karst bauxites at regional unconformities and geo-
1251
tectonic correlation in the Cretaceous of the Mediterranean: Società Geologica Italiana, Bollettino, v. 110, P. 85–92.
D’ARGENIO, B., AND MINDSZENTY, A., 1992, Tectonic and climatic control on paleokarst and
bauxites: Giornale di Geologia, v. 54, p. 207–218.
D’ARGENIO, B., MINDSZENTY, A., BARDOSSY, G. Y., JUHASZ, E., AND BONI, M., 1987, Bauxites of
southern Italy revisited: Società Geologica Italiana, Rendiconti, v. 9 (1986), p. 263–268.
DE ALTERIIS, G., AND AIELLO, G., 1993, Stratigraphy and tectonics offshore of Puglia (Italy,
southern Adriatic Sea): Marine Geology, v. 113, p. 239–253.
DE CASTRO, P., 1987, Le facies di piattaforma carbonatica del Giurassico italiano: diffusione
areale e lineamenti biostratigrafici: Società Paleontologica Italiana, Bollettino, v. 26, p. 309–
325.
DE DOMINICIS, A., AND MAZZOLDI, G., 1989, Interpretazione geologico-strutturale del margine
orientale della Piattaforma Apula: Società Geologica Italiana, Memorie, v. 38 (1987), p.
163–176.
DRZEWIECKI, P.A., AND SIMO, J.A., 1997,. Carbonate platform drowning and oceanic anoxic
events on a mid-Cretaceous carbonate platform, south-central Pyrenees, Spain: Journal of
Sedimentary Research, v. 67, p. 698–714.
EBERLI, G.P., 1991, Growth and demise of isolated carbonate platforms: Bahamian controversies, in Muller, D.W, McKenzie, J.A., and Weissert, H., eds., Controversies in Modern
Geology: London, Academic Press, p. 231–248.
EBERLI, G.P., BERNOULLI, D., SANDERS, D., AND VECSEI, A., 1993, From aggradation to progradation: the Maiella Platform, Abruzzi, Italy, in Simo, T., Scott, R.W., and Masse, J.P., eds.,
Cretaceous Carbonate Platforms: American Association of Petroleum Geologists, Memoir
56, p. 213–232.
ERBA, E., 1992, Calcareous nannofossil distribution in pelagic rhythmic sediments (Aptian–
Albian, Piobbico core, central Italy): Rivista Italiana di Paleontologia e Stratigrafia, v. 97,
p. 445–484.
ERLICH, R.N., LONGO, A.P., JR., AND HYARE, S., 1993, Response of carbonate platform margins
to drowning: evidence of environmental collapse, in Loucks, R.G., and Sarg, J.F., eds.,
Carbonate Sequence Stratigraphy: American Association of Petroleum Geologists, Memoir
57, p. 241–265.
FERNÁNDEZ-MENDIOLA, P.A., AND GARCı́A-MONDÉJAR, J., 1997, Isolated carbonate platform of
Caniego, Spain: a test of the latest Albian worldwide sea-level changes: Geological Society
of America, Bulletin, v. 109, p. 176–194.
FÖLLMI, K.B., WEISSERT, H., BISPING, M., AND FUNK, H., 1994, Phosphogenesis, carbon-isotope
stratigraphy, and carbonate-platform evolution along the Lower Cretaceous northern Tethyan
margin: Geological Society of America, Bulletin, v. 106, p. 729–746.
GAMBINI, R., AND TOZZI, M., 1996, Tertiary evolution of the southern Adria microplate: Terra
Nova, v. 8, p. 593–602.
GRADSTEIN, F. M., AGTERBERG, F.P., OGG, J.G., HARDENBOL, J., VAN VEEN, P., THIERRY, J., AND
HUANG, Z., 1995, A Triassic, Jurassic and Cretaceous time scale, in Berggren, W.A., Kent,
D.V., Aubry, M.P., and Hardenbol, J., eds., Geochronology, Time Scales and Global Stratigraphic Correlation: SEPM, Special Publication 54, p. 95–126.
GREENLEE, S.M., AND MOORE, T.C., 1988, Recognition and interpretation of depositional sequences and calculation of sea-level changes from stratigraphic data: offshore New Jersey
and Alabama Tertiary, in Wilgus, C.K., Hastings, B.S., Kendall, C.G.St.C., Posamentier,
H.W., Ross, C.A., and Van Wagoner, J.C., eds., Sea Level Changes: An Integrated Approach: SEPM, Special Publication 42, p. 329–353.
GRÖTSCH, J., SCHRÖDER, R., NOÈ, S., AND FLÜGEL, E., 1993, Carbonate platforms as recorders of
high-amplitude eustatic sea-level fluctuations: the late Albian appenninica-event: Basin Research, v. 5, p. 197–212.
GUARNIERI, G., LAVIANO, A., AND PIERI, P., 1990, Second International Conference on Rudists,
Rome and Bari, 1/7/1990, Guide book, 49 p.
HALLOCK, P., AND SCHLAGER, W., 1986, Nutrient excess and the demise of coral reefs and
carbonate platforms: Palaios, v. 1, p. 389–398.
HAQ, B.U., HARDENBOL, J., AND VAIL, P.R., 1987, The chronology of fluctuating sea levels since
the Triassic: Science, v. 235, p. 1156–1167.
HUBBARD, R.J., 1988, Age and significance of sequence boundaries on Jurassic and early Cretaceous rifted continental margins: American Association of Petroleum Geologists, Bulletin,
v. 72, p. 49–72.
JACQUIN, T., ARNAUD-VANNEAU, A., ARNAUD, H., RAVENNE, C., AND VAIL, P.R., 1991, Systems
tracts and depositional sequences in a carbonate setting: a study of continuous outcrops from
platform to basin at the scale of seismic lines: Marine and Petroleum Geology, v. 8, p. 122–
139.
JENKYNS, H.C., 1980, Cretaceous anoxic events: from continents to oceans: Geological Society
of London, Journal, v. 137, p. 171–188.
JENKYNS, H.C., 1991, Impact of Cretaceous Sea Level Rise and Anoxic Events on the Mesozoic
Carbonate Platform of Yugoslavia: American Association of Petroleum Geologists, Bulletin,
v. 75, p. 1007–1017.
LAVIANO, A., AND MARINO, M., 1996, Biostratigraphy and paleoecology of Upper Cretaceous
carbonate successions in the Gargano Promontory: Società Geologica Italiana, Memorie, v.
51, p. 685–701.
LOGAN, B.V., REZAK, R., AND GINSBURG R.N., 1964, Classification and environmental significance of algal stromatolites: Journal of Geology, v. 72, p. 68–83.
LUCIANI, V., AND COBIANCHI, M., 1994, Type section of the Mattinata Formation (Lower Cretaceous, Gargano Promontory, southern Italy): new biostratigraphic data (calcareous nannofossils and planktonic foraminifers): Memorie di Scienze Geologiche, v. 46, p. 283–301.
LUPERTO SINNI, E., 1996a, Sintesi delle conoscenze biostratigrafiche del Cretaceo del Gargano
e delle Murge: Società Geologica Italiana, Memorie, v. 51, p. 995–1018.
LUPERTO SINNI, E., 1996b, Schema stratigrafico del Cretacico del Gargano basato su risultati di
recenti ricerche: Società Geologica Italiana, Memorie, v. 51, p. 1019–1036.
LUPERTO SINNI, E., AND BORGOMANO, J., 1989, Le Crétacé supérieur des Murges sud-orientales
1252
A. BOSELLINI ET AL.
(Italie méridionale): stratigraphie et évolution des paléoenvironnements: Rivista Italiana di
Paleontologia e Stratigrafia, v. 95, p. 95–136.
LUPERTO SINNI, E., AND MASSE, J.P., 1987, Données nouvelles sur la stratigraphie et la micropaléontologie des séries carbonatées de talus et de bassin du Crétacé inférieur du Gargano
(Italie méridionale): Rivista Italiana di Paleontologia e Stratigrafia, v. 93, p. 347–378.
LUPERTO SINNI, E., AND REINA, A., 1996a, Gli hiatus del Cretaceo delle Murge: confronto con
dati offshore: Società Geologica Italiana, Memorie, v. 51, p. 719–727.
LUPERTO SINNI, E., AND REINA, A., 1996b, Nuovi dati stratigrafici sulla discontinuità mesocretacea delle Murge (Puglia, Italia meridionale): Società Geologica Italiana, Memorie, v. 51,
p. 1179–1188.
MARTINIS, B., AND PAVAN, G., 1967, Note illustrative della carta geologica d’Italia, Foglio 157
‘‘Monte S. Angelo’’: Servizio Geologico d’Italia, Roma, 56 p.
MASSE, J.P., AND LUPERTO SINNI, E., 1989, A platform to basin transitional model: the lower
cretaceus carbonates of the Gargano Massif: Società Geologica Italiana, Memorie, v. 40
(1987), p. 99–108.
MERLA, G., ERCOLI, A., AND TORRE, D., 1969, Note illustrative della carta geologica d’Italia,
Foglio 164 ‘‘Foggia’’: Servizio Geologico d’Italia, Roma, 22 p.
MIALL, A.W., 1992, Exxon global cycle chart: an event for every occasion?: Geology, v. 20,
p. 787–790.
MINDSZENTY, A., D’ARGENIO, B., AND AIELLO, G., 1995, Lithospheric bulges recorded by regional
unconformities. The case of Mesozoic–Tertiary Apulia: Tectonophysics, v. 252, p. 137–161.
MITCHUM, R.M., AND VAN WAGONER, J.C., 1991, High-frequency sequences and their stacking
patterns: sequence-stratigraphic evidence of high-frequency eustatic cycles, in Biddle, K.T.,
and Schlager, W., eds., The Record of Sea-Level Fluctuations: Sedimentary Geology, v. 70,
p. 131–160.
MITCHUM, R.M., JR., VAIL, P.R., AND THOMPSON, S., 1977, Seismic stratigraphy and global
changes of sea-level, part 2: the depositional sequences as a basic unit for stratigraphic
analysis, in Payton, C.E., ed., Seismic Stratigraphy, Applications to Hydrocarbon Exploration: American Association of Petroleum Geologists, Memoir 26, p. 53–62.
MORSILLI, M., AND BOSELLINI, A., 1997, Carbonate facies zonation of the Upper Jurassic–Lower
Cretaceous Apulia Platform margin (Gargano Promontory, southern Italy): Rivista Italiana
di Paleontologia e Stratigrafia, v. 103, p. 193–206.
MULLINS, H.T., DOLAN, J., BREEN, N., ANDERSEN, B., GAYLORD, M., PETRUCCINONE, J.L., WELLNER,
R.W., MELILLO, A.J., AND JURGENS, A.D., 1991, Retreat of carbonate platforms: response to
tectonic processes: Geology, v. 19, p. 1089–1092.
MUTTI, E., 1992, Turbidite sandstones: Agip (Agenzia Generale Italiana Petroli), San Donato
Milanese, 275 p.
NERI, C., 1993, Stratigraphy and sedimentology of the Monte Acuto Formation (Upper Cretaceous–Lower Paleocene, Gargano Promontory, Southern Italy): Università di Ferrara, Annali (N.S.), Sezione Scienze della Terra, v. 4, p. 13–44.
NERI, C., AND LUCIANI, V., 1994, The Monte S. Angelo Sequence (Late Cretaceous–Paleocene,
Gargano Promontory, southern Italy): physical stratigraphy and biostratigraphy: Giornale di
Geologia, v. 56, p. 149–165.
PAVAN, G., AND PIRINI, C., 1966, Stratigrafia del Foglio 157 ‘‘Monte S. Angelo’’: Servizio
Geologico Italiano, Bollettino, v. 86 (1965), p. 123–189.
PIERI, P., AND LAVIANO, A., 1989, Tettonica e sedimentazione nei depositi senoniani delle Murge
sud-orientali (Ostuni): Società Geologica Italiana, Bollettino, v. 108, p. 351–356.
POSAMENTIER, H.W., JERVEY, M.T., AND VAIL, P.R., 1988, Eustatic controls on clastic deposition:
I—conceptual framework, in Wilgus, C.K., Hastings, B.S., Kendall C.G.St.C., Posamentier,
H.W., Ross, C.A., and Van Wagoner J.C., eds., Sea Level Changes: An Integrated Approach:
SEPM, Special Publication 42, p. 109–124.
RUBERTI, D., 1993, Le lacune stratigrafiche nel Cretacico del Matese centro-settentrionale: Società Geologica Italiana, Bollettino, v. 111 (1992), p. 283–289.
SARG, J.F., 1988, Carbonate sequence stratigraphy, in Wilgus, C.K., Hastings, B.S., Kendall,
C.G.St.C., Posamentier, H.W., Ross, C.A., and Van Wagoner, J.C., eds., Sea Level Changes:
An Integrated Approach: SEPM, Special Publication 42, p. 155–181.
SCHLAGER, W., 1989, Drowning unconformities on carbonate platforms, in Crevello, P.D., Wilson, J.L., Sarg, J.F., and Read, J.F., eds., Controls on Carbonate Platform and Basin Development: SEPM, Special Publication 44, p. 15–25.
SCHLAGER, W., 1991, Depositional bias and environmental change—important factors in sequence stratigraphy, in Biddle, K.T., and Schlager, W., eds., The Record of Sea-Level
Fluctuations: Sedimentary Geology, v. 70, p. 109–130.
SCHLAGER, W., 1992, Sedimentology and sequence stratigraphy of reefs and carbonate platform:
American Association of Petroleum Geologists, Short Course 34, 71 p.
SCHLAGER, W., 1993, Accommodation and supply—a dual control on stratigraphic sequences:
Sedimentary Geology, v. 86, p. 111–136.
SCHLAGER, W., 1998, Exposure, drowning and sequence boundaries on carbonate platforms, in
Camoin, G.I., and Davies, P.J., eds., Reefs and Carbonate Platforms in the Pacific and Indian
Oceans: International Association of Sedimentologists, Special Publication 25, p. 3–21.
SCHLANGER, S.O., AND JENKINS, H.C., 1976, Cretaceous oceanic anoxic sediments: causes and
consequences: Geologie en Mijnbouw, v. 55, p. 179–184.
SCHLAGER, W., AND PHILIP, J., 1990, Cretaceous carbonate platforms, in Ginsburg, R.N., and
Beaudoin, B., eds., Cretaceous resources, events and rhythms: Dordrecht, The Netherlands,
Kluwer Academic Publishers, v. 304, p. 173–195.
SIMO, J.A., SCOTT, R.W., AND MASSE, J.P., 1993, Cretaceous Carbonate Platforms: an overview,
in Simo, J.A., Scott, R.W., and Masse, J.P., eds., Cretaceous Carbonate Platforms: American
Association of Petroleum Geologists, Memoir 56, p. 1–14.
SKOURTSIS-CORONEOU, V., SOLAKIUS, N., AND CONSTANTINIDIS, I., 1995, Cretaceous stratigraphy of
the Ionian zone, Hellenides, western Greece: Cretaceous Research, v. 16, p. 539–558.
STOLL, H.M., AND SCHRAG, D.P., 1996, Evidence for glacial control of rapid sea level changes
in the Early Cretaceous: Science, v. 272, p. 1771–1774.
TORNAGHI, M.E., PREMOLI SILVA, I., AND RIPEPE, M., 1989, Lithostratigraphy and planktonic
foraminiferal biostratigraphy of the Aptian Albian ‘‘Scisti a Fucoidi’’ in the Piobbico core,
Marche, Italy: background for cyclostratigraphy: Rivista Italiana di Paleontologia e Stratigrafia, v. 95, p. 223–264.
VAIL, P.R., MITCHUM, R.M., JR., TODD, R.G., WIDMIER, J.M., THOMPSON, S., SANGREE, J.B., BUBB,
J.N., AND HATLELID, W.G., 1977, Seismic stratigraphy and global changes of sea level, in
Clayton, C.E., ed., Seismic Stratigraphy, Applications to Hydrocarbon Exploration: American Association of Petroleum Geologists, Memoir 26, p. 49–212.
VAIL, P.R., AUDEMARD, F., BOWMAN, S.C., EISNER, P.N., AND PEREZ CRUZ, G., 1991, The stratigraphic signature of tectonics and sedimentation: an overview, in Einsele, G., Ricken, W.,
and Seilacher, A., eds., Cycles and Events in Stratigraphy: Berlin, Springer-Verlag, p. 617–
659.
VAN WAGONER, J.C., POSAMENTIER, H.W., MITCHUM, R.M., VAIL, P.R., SARG, J.F., LOUTIT, T.S.,
AND HARDENBOL, J., 1988, An overview of the fundamentals of sequence stratigraphy and
key definitions, in Wilgus, C.K., Hastings, B.S., Kendall, C.G.St.C., Posamentier, H.W.,
Ross, C.A., and Van Wagoner, J.C., eds., Sea Level Changes: An Integrated Approach:
SEPM, Special Publication 42, p. 39–45.
VOGT, P.R., 1989, Volcanogenic upwelling of anoxic, nutrient rich water: A possible factor in
carbonate bank/reef demise and benthic faunal extinctions?: Geological Society of America,
Bulletin, v. 101, p. 1225–1245.
ZAPPATERRA, E., 1990, Carbonate paleogeographic sequence of the Periadriatic region: Società
Geologica Italiana, Bollettino, v. 109, p. 5–20.
Received 1 June 1998; accepted 9 February 1999.