Middle Jurassic - Early Cretaceous integrated biostratigraphy (ammonites, calcareous nannofossils and calpionellids) of the Contrada Diesi section (South-Western Sicily, Italy).

Abstract

Facies and biostratigraphic analyses of the Contrada Diesi succession, cropping out along the northern slope of Mt. Magaggiaro (Sciacca, SW Sicily), provided new data on the Middle Jurassic-Early Cretaceous pelagic sedimentation in the Saccense domain. The richness in ammonites allowed the identification of Bathonian-Kimmeridgian Biozones and Subzones, while the Tithonian-Valanginian interval was defined mainly by calpionellids and calcareous nannofossils. Facies and microbiofacies analyses of the Jurassic-Cretaceous pelagic sediments of the area, together with ammonite, calpionellid and calcareous nannofossil integrated biostratigraphy, were very effective tools for comparison of biostratigraphic events. Many gaps in sedimentation were recognized, the most important spanning the middle and late Berriasian and part of
the early Berriasian. The Contrada Diesi succession provides new lithobiostratigraphic data on the Saccense Domain. It suggests a high degree of internal variability tied to the irregular paleotopography of the carbonate
platform substrate (Inici Fm.), derived from Early Jurassic tectonics.
Gaps in sedimentation in the Contrada Diesi sections indicate that the environment of the Saccense Domain was characterized by a variable rate of sedimentation and energy changes.

Full text

356 Rivista Italiana di Paleontologia e Stratigrafia volume 110 no. 1 ???? 2004
1 Dipartimento di Scienze Geologiche - Università di Catania, Corso Italia 55, 95129 Catania, Italy. E-mail: marinom@unict.it
2 Dipartimento di Scienze della Terra - Università degli Studi di Perugia, Piazza Università, 06100 Perugia, Italy.
E-mail: abaldanz@unipg.it - gparisi@unipg.it
3 Dipartimento di Geologia e Geodesia, Università di Palermo - Corso Tukory 131, 90134 Palermo, Italy. E-mail: mgup@unipa.it
4 Dipartimento di Scienze della Terra, Università degli Studi di Roma “La Sapienza” - Piazzale Aldo Moro 5, 00165 Roma, Italy.
E-mail: nino.mariotti@uniroma1.it; fabio.petti@uniroma1.it
5 Dipartimento di Scienze della Terra - Università “G. D’Annunzio” di Chieti, Via dei Vestini 30, 66013 Chieti Scalo (CH), Italy.
pp. 357-3723 pls.
MIDDLE JURASSIC - EARLY CRETACEOUS INTEGRATED BIOSTRATIGRAPHY
(AMMONITES, CALCAREOUS NANNOFOSSILS AND CALPIONELLIDS)
OF THE CONTRADA DIESI SECTION (SOUTH-WESTERN SICILY, ITALY)
MARIA CONCETTA MARINO1, GLORIA ANDREINI2, ANGELA BALDANZA2, CAROLINA
D’ARPA3, NINO MARIOTTI4, GIOVANNI PALLINI5, GUIDO PARISI2 & FABIO MASSIMO PETTI4
Received December 7, 2002; accepted October 1st , 2003
Keywords: ammonites, calcareous nannofossils, calpionellids,
biochronology, Middle-Late Jurassic-Early Cretaceous, Sicily, Italy
Abstract. Facies and biostratigraphic analyses of the Contrada
Diesi succession, cropping out along the northern slope of Mt. Magag-
giaro (Sciacca, SW Sicily), provided new data on the Middle Jurassic-Early
Cretaceous pelagic sedimentation in the Saccense domain. The richness
in ammonites allowed the identification of Bathonian-Kimmeridgian Bio-
zones and Subzones, while the Tithonian-Valanginian interval was defined
mainly by calpionellids and calcareous nannofossils. Facies and micro-
biofacies analyses of the Jurassic-Cretaceous pelagic sediments of the
area, together with ammonite, calpionellid and calcareous nannofossil
integrated biostratigraphy, were very effective tools for comparison of
biostratigraphic events. Many gaps in sedimentation were recognized,
the most important spanning the middle and late Berriasian and part of
the early Berriasian. The Contrada Diesi succession provides new litho-
biostratigraphic data on the Saccense Domain. It suggests a high degree
of internal variability tied to the irregular paleotopography of the car-
bonate platform substrate (Inici Fm.), derived from Early Jurassic tec-
tonics. Gaps in sedimentation in the Contrada Diesi sections indicate
that the environment of the Saccense Domain was characterized by a
variable rate of sedimentation and energy changes.
Riassunto. L’analisi biostratigrafica e delle litofacies della succes-
sione Contrada Diesi, affiorante sul versante settentrionale di Monte
Magaggiaro (Sciacca, Sicilia sud-occidentale), ha fornito nuovi dati ri-
guardanti l’evoluzione sedimentaria “pelagica” nel Dominio Saccense
dal Giurassico medio al Cretaceo inferiore. La ricchezza di ammoniti ha
permesso di riconoscere biozone e subzone dell’intervallo Bathoniano-
Kimmeridgiano, mentre l’intervallo Titonico-Valanginiano è stato ben
definito principalmente mediante nannofossili calcarei e calpionellidi. La
biostratigrafia integrata ad ammoniti, calpionellidi e nannofossili calcarei
ha fornito una buona opportunità di comparazione tra differenti eventi
sia litostratigrafici che biostratigrafici. Sono state individuate numerose
lacune di sedimentazione, fra cui la più imponente è quella comprenden-
te il Berriasiano medio e superiore e parte dell’inferiore. All’interno del
Dominio Saccense si delinea così un elevato grado di variabilità interna
legato, con ogni probabilità, alla paleotopografia irregolare del substra-
to carbonatico (Fm. Inici) ereditata dalle fasi distensive del Giurassico
inferiore. La ripetuta presenza di lacune consente inoltre di avanzare
l’ipotesi che l’ambiente deposizionale sia stato caratterizzato da tassi di
sedimentazione variabili e da improvvisi cambi energetici.
Introduction
The results of stratigraphic analyses carried out on a
Jurassic-Cretaceous succession of the Saccense Domain are
here presented. The succession is well exposed in the quarry
at Contrada Diesi, near Sciacca (South-Western Sicily), on
the northern slope of Mt. Magaggiaro (Fig. 1). Lithostrati-
graphic, biostratigraphic and facies-microbiofacies analyses
highlighted several aspects of the sedimentary evolution of
the Saccense pelagic succession during the Jurassic-Early
Cretaceous interval. The sediments examined consist of dif-
ferent lithologies belonging to the Inici Fm., Buccheri Fm.
and Lattimusa Fm. (Di Stefano et al. 2002). The time inter-
val ranges from the Bathonian to the late Valanginian. The
richness of different fossil groups (ammonites, calcareous
nannofossils and calpionellids) offered the opportunity to
compare and calibrate different biozonations, improving the
knowledge of Jurassic and Cretaceous biochronology.

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Geological setting
The area investigated is at Mt. Magaggiaro (Sciacca,
SW Sicily) and it is part of the external portion of the
south-verging side of the Apennine-Maghrebian moun-
tain chain, a thrust system derived from slight deforma-
tion of Meso-Cenozoic units covered by syntectonic ter-
rigenous deposits (Catalano et al. 1995a, 1995b, 2000).
Structural and stratigraphic analyses in the Sciacca area
were carried out by Mascle (1970, 1974, 1979), Di Ste-
fano & Vitale (1994), and Vitale (1990, 1995). Di Stefano
& Vitale (1993) mapped the Western Sicanian Mts., com-
piling a detailed lithostratigraphic scheme which shows
high degree of variability among different successions
throughout the area.
The area studied belongs to the Saccense Domain
(Catalano & D’Argenio 1978, 1982; Mascle 1970), which
represents the outer and less deformed domain and is in-
terpreted as a Triassic carbonate platform evolving to a
pelagic carbonate platform (PCP of Santantonio 1993,
1994). In recent papers (Catalano et al. 1995a, 1995b),
due to new structural data (more internal position of the
basinal units – Imerese and Sicanian – with respect to the
carbonate platform units – Panormide, Trapanese and Sac-
cense) this paleogeographic reconstruction was changed.
In this new scheme the Saccense Domain, together with
the Panormide and Trapanese Domains, represents the
remains of an extended carbonate platform, with irreg-
ular morphology, passing to a basinal area (Imerese and
Sicanian Domain). According to this palinspastic resto-
ration, the area of Mt. Magaggiaro belongs to the Hyb-
lean-Pelagian Domain, a morphostructural high with com-
plex morphology and neritic-pelagic, locally condensed,
sedimentation that took place above continental crust of
“normal” thickness.
The Jurassic-Lower Cretaceous litostratigraphic
succession of the Saccense Domain has been the object
of accurate studies (Catalano & D’Argenio 1990; Cata-
lano et al. 1995a, 1995b; Catalano et al. 2000; Di Ste-
fano et al. 1996; Vitale 1990; Di Stefano & Vitale 1993).
The lowermost part of the succession consists of several
thousand metres of platform limestone and dolostone of
Late Triassic age, formally named Sciacca Fm. and syn-
onymous with the Gela Fm. of the Hyblean Plateau. It
is overlain by 200-300 m of shallow water carbonates of
Early Jurassic age (Inici Fm.) (Schmidt di Frieberg 1965;
Ronchi et al. 2000). This unit is followed upwards by the
Buccheri Fm. (or “Rosso Ammonitico”), consisting of
different condensed pelagites with abundant ammonites,
which spans the Early Jurassic-early Tithonian interval.
The Buccheri Fm. is replaced by the “Calcari a Calpi-
onelle”, better known as Lattimusa Fm. or Chiaramonte
Fm., equivalent to the Apenninic Maiolica Fm. The Lat-
timusa Fm. is referred to the latest Jurassic to Early Cre-
taceous time interval.
Lithostratigraphy and microfacies analysis
Section I
Section I crops out along an artificial exposure of
an active quarry (Fig. 2). It may be subdivided into six in-
formal lithostratigraphic units: (bottom to top) Bioclastic
platform limestone (Inici Fm.), Bositra limestone, Calcis-
iltitic limestone, Stromatolitic calcarenitic limestone, Peb-
bly calcarenite, Grey-reddish nodular marly limestone/
Calcari a Calpionelle (Fig. 3).
Bioclastic platform limestone (Sinemurian p.p.)
- This unit is made of thick-bedded bioclastic limestone
showing fenestral lamination, with peloids, intraforma-
tional lithoclasts, oncolites and algae. The microfossil as-
semblage is represented by Siphovalvulina sp., Textular-
ia sp., Lituosepta sp., Ammobaculites sp., Trocholina sp.,
Glomospira sp., associated with Cayeuxia sp., gastropods,
bivalves, and echinoderm fragments. The end of the car-
bonate platform sedimentation is regionally known to be
Fig. 1 - Geological map of the Monte Magaggiaro area and location
of the studied sections. 1) Limestone and dolostone of per-
itidal platform environment (Late Triassic/lower part of Early
Jurassic); 2) Condensed pelagic deposits (Pliensbachian-Ti-
thonian); 3) Calpionellid limestone (Lattimusa Fm. Auctt.,
Tithonian-Albian); (4) Scaglia Fm. (Cenomanian-Eocene); 5)
Marly limestone with intercalated nummulitic biocalcarenites
(middle-Late Oligocene); 6) Grey and pink limestone and
dolostone with Lepidocyclina (Aquitanian); 7) Glauconitic
sandstones (Burdigalian-Langhian); 8) Deltaic and turbiditic
deposits (late Tortonian-Messinian); 9) Amphistegina calcaren-
ites (Pliocene); 10) Calcarenites and marls (Early Pleistocene);
11) fault; 12) thrust; 13) location of the studied sections
M. C. Marino, G. Andreini, A. Baldanza, C. D’arpa, N. Mariotti, G. Pallini, G. Parisi & F. M. Petti

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Sinemurian in age (Di Stefano et al. 2002). The uppermost
portion of the unit is cut across by mono- and polyphase
neptunian dykes of different age ranging from latest Early
Jurassic to Late Jurassic. Carbonate platform sediments
are overlain paraconformably with a sharp contact by pe-
lagites corresponding to a stratigraphic hiatus ranging
from the Sinemurian p.p. to the late Bajocian.
Bositra limestone (lower Bathonian–middle Ox-
fordian p.p.) - The pelagic succession starts with a mas-
sive, ochre to reddish biogenic calcisiltite to calcarenite;
sheet-cracks sub-parallel to bedding occur locally. The
unit consists of packstone, more rarely wackestone, with
abundant thin-shelled bivalves (sensu Conti & Monari
1992), often chaotically arranged. Peloids and intrafor-
mational lithoclasts are also present. The representative
microfossils in this portion are foraminifers (rare small
Protoglobigerinids, Textulariids, Valvulinids, Spirillinids),
Stomiosphaera sp., ostracods and rare radiolarians, while
echinoderm fragments are common throughout. Globo-
chaete sp. is ubiquitous. Upward, the occurrence of ellip-
soidal wackestone intraclasts, several centimetres across,
indicates a facies change. Thin-shelled bivalves are rarer
than in underlying levels, while the frequency of echino-
derm fragments increases; Globochaete sp. and large Pro-
toglobigerinids are common in finer-grained portions.
A discontinuity surface at 6.75 m is marked local-
ly by a black LLH (after Logan et al. 1964) stromatolite.
This discontinuity is a distinctive horizon that can be fol-
lowed along the entire front of the quarry.
Calcisiltitic limestone (middle Oxfordian p.p.-
upper Oxfordian p.p.) - Above the discontinuity, a level
rich in ammonites lying parallel to the bedding is present.
It can be followed laterally, across the entire section and
it makes a useful marker level. The calcisiltitic limestone,
2.5 m thick, consists mainly of wackestone with Protoglo-
bigerinids and radiolarians. Many ammonites bear stro-
matolitic caps and some have domes on both sides. This
unit records the disappearance of thin-shelled bivalves,
coincident with a bloom of Protoglobigerinids. The up-
permost 2 m of the interval are made of reddish calcis-
iltitic limestone, impregnated with ferruginous minerals.
Upward, the colour shades into light brown.
Stromatolitic calcarenitic limestone (Kim-
meridgian-lowerTithonian p.p.) - This unit is about 3
m thick, massive, with stromatolites occurring both as
isolated domes and as LLH continuous structures. Weath-
ering enhances cryptalgal lamination, as well as randomly
oriented skeletal remains such as belemnites and echi-
noids. Ammonites, as well as small clasts and brachio-
pods, are frequently capped by stromatolitic domes. The
Fig. 2 - Panoramic view and shematic drawing of the lithostratigraphic units. Contrada Diesi Quarry, Section I. For the lithostratigraphic units
see Fig. 3.
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texture is a laminated packstone with abundant echino-
derm fragments. Protoglobigerinids are less frequent in
levels dominated by echinoderms. At the top of this unit,
coarse calcarenites (often grainstone) contain rounded
intraclasts. Microfossils include Globochaete sp., Spirilli-
na sp., Stomiosphaera sp., Involutina sp., Lenticulina sp.,
Turrispirillina sp., Ophthalmidiids, Lagenids, and Pro-
toglobigerinids. Echinoderm debris and Lamellapthychus
fragments also occur. The first occurrence of Saccocoma
sp. is recorded at about 9.75 m of the total thickness of
the section.
Pebbly calcarenite (lower Tithonian p.p.) – Up-
ward, the section continues for a thickness of nearly 2
m with alternating conglomeratic and sand-sized crinoi-
dal levels (also with belemnites, echinoid spines, bivalves
and Saccocoma sp.). Discontinuous stromatolitic levels
are present as well. The first occurrence of Cadosinids is
recorded at the top of this unit.
Grey-reddish nodular marly limestone/Calcari a
Calpionelle (lowerTithonian p.p.-lower Berriasian) -
This unit consists of grey-reddish nodular and marly lime-
stone in thin beds. The nodular limestone is a packstone
with crinoidal debris, internal moulds of ammonites and
apthychi. Nodules are made of mudstone/wackestone,
often with stylolithic contact. Microfossils include fo-
raminifers, mainly Lenticulina sp. and Spirillina sp., ra-
diolarians, Cadosinids and Saccocoma sp. Unfortunately,
ammonites are represented only by stratigraphically not
diagnostic Phylloceratids and Lytoceratids. Because of a
little tectonic disturbance, the upper part of this unit was
analysed some metres further, along the road outside the
quarry. The last occurrence of Saccocoma, together with
the first occurrence of Calpionellids, is recorded at this
site. The interval is named conventionally Calcari a Cal-
pionelle for the inception of calpionellids.
Section II
Section II is exposed in a small natural trench just
outside the quarry (Fig. 4). In the small natural trench,
near Section I, a small outcrop, about 26 m thick, of Up-
per Jurassic p.p./Lower Cretaceous p.p. sediments, corre-
sponding to the top of Section I, is visible. Section II dif-
fers slightly from Section I because the Stromatolitic in-
terval is here replaced by a calcarenitic/calcisiltitic level.
This section could be subdivided into three infor-
mal lithostratigraphic units (bottom to top): Calcarenitic/
calcisiltitic limestone, Nodular marly limestone, Calcari
a Calpionelle (Fig. 5, 6).
Fig. 3 - Chrono-lithostratigraphy and main bioevents of the Con-
trada Diesi Quarry, Section I.
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Calcarenitic/calcisiltitic limestone (upper Kim-
meridgian-lower Tithonian p.p.) - This unit is repre-
sented by a light brown calcarenitic/calcisiltitic lime-
stone rich in thin-shelled bivalves, and by wackestone
and packstone with abundant Saccocoma and echinoid
fragments. From 3.5 m, Saccocoma increases and Pro-
toglobigerinids decrease. Protoglobigerinids disappear
at the top of the unit.
Nodular marly limestone (lower Tithonian p.p.-
upper Tithonian p.p.) - Grey-yellowish nodular marly
limestone with thin cherty levels are ascribed to this unit.
The texture is a wackestone and subordinate packstone
with Saccocoma, radiolarians and echinoid fragments.
In this unit Saccocoma decreases, while Cadosinids in-
crease.
Calcari a Calpionelle (upper Tithonian p.p.- up-
per Valanginian) - This unit is characterized at the base
by a white nodular limestone of limited thickness, which
is replaced by a thin, white well-bedded limestone. As a
whole, this interval includes wackestone and mudstone
with abundant Calpionellids, foraminifers (Textulariids
and Valvulinids), rare radiolarians, echinoid fragments and
some ammonites. Saccocoma disappears at the base of this
unit in the uppermost Tithonian; the last (rare) Saccocoma
occur together with the first Calpionellids.
Biostratigraphy
Ammonites
Section I - Ammonite-rich deposits in this sec-
tion provided new biostratigraphic data on the Bathoni-
an-Kimmeridgian interval. Bed by bed sampling yielded
more than 300 specimens. Selected ammonite species are
illustrated in Pl. 1, and the range of species observed is
reported in Fig. 3 and 7. Biostratigraphic data are referred
to the zonal schemes proposed by Meléndez & Fontana
(1993), Cariou & Hantzpergue (1997) and Meléndez et
al. (1997), including some more recent modifications by
Matyja & Wierzbowski (1997).
The first metre of the pelagic succession displays an
ammonite assemblage composed of Morphoceras sp. ind.,
Morphoceras cf. macrescens (Buckman), comparable to the
specimens illustrated by Mangold (1970b) (pl. 5, figs. 11,
12, 13), Parkinsonia sp., Parkinsonia (Gonolkites) con-
vergens (Buckman), Cadomites (C.) sp., Cadomites (Ca-
domites) daubenyi (Gemmellaro), Cadomites (Polyplec-
tites) sp., Strigoceras sp., Procerites sp. and Oppelia undat-
iruga Gemmellaro; the latter is similar to the form illus-
trated by Wendt 1964 (pl. XVIII, fig. 2) under the name
Oppelia (Oxycerites) aspidoides and is synonymous with
the specimen described by Gemmellaro, 1877 and 1882
(p. 137, pl. XVIII, fig. 8). All the forms mentioned above
may be related to the lower Bathonian Z. zig-zag Zone.
From 1.00 to 1.30 m the disappearance of Parkinsonii-
dae and of the genus Morphoceras is noteworthy; Procer-
ites sp. ind., Cadomites sp. ind., Cadomites (Cadomites)
daubenyi (Gemmellaro) (Pl. 1, figs.10-13) are still present,
together with Procerites (Procerites) cf. tmetolobus Buck-
man, Procerites (Procerites) postpollubrum Buckman and a
specimen of Bullatimorphites sp. However, the absence of
other diagnostic taxa precludes the referral of this inter-
val to the lower Bathonian P. aurigerus Zone. The interval
between 1.30 and 1.80 m is poorly fossiliferous, yielding
only two specimens of Cadomites (Cadomites) orbignyi
(de Grossouvre) (Pl. 1, fig. 12) and a single specimen of
Hecticoceras (Prohecticoceras) cf. ochraceum Elmi which
mark the beginning of the middle Bathonian P. progracilis
Zone (C. orbignyi Subzone). Oppeliidae are also present.
From 2.20 to 3.20 m no significant ammonite was found.
The upper Bathonian H. retrocostatum Zone was recog-
nized in the interval between 3.20 and 4.00 m, based on
an ammonite assemblage characterized by some diagnos-
tic taxa , i.e. Homoeplanulites (Homoeplanulites) bugesi-
acus (Dominjon) (close to the specimens illustrated by
Mangold 1970a, pl. II, figs. 2-9, H. blanazense Subzone),
Bullatimorphites hannoveranus (Roemer) (Pl. 1, fig. 11)
(similar to the specimen illustrated by Géczy & Galácz
(1998), pl. III, figs.1-2, B. hannoveranus Subzone) and
Choffatia (Choffatia) densidecorata Galàcz (Galàcz, 1980,
pl. XXXV). No ammonites related to the T. subcontrac-
tus, M. morrisi and C. bremeri Zones (middle Bathonian)
and C. discus Zone (uppermost Bathonian) were found.
From 4.65 to 5.30 m, a rich assemblage of Hecticoceras
Fig. 4 - Panoramic view and shematic drawing of the lithostratigraphic units. Contrada Diesi, Section II. For the lithostratigraphic units see
Fig. 5.
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(Hecticoceras) posterius Zeiss (Pl. 1, fig. 8), resembling the
specimens illustrated by Elmi (1967) (pl. 12, figs. 4, 6, 7,
8, 9), Holcophylloceras zignodianum (d’Orbigny), Calli-
phylloceras disputabile (Zittel), Reineckeia sp. ind., Choffa-
tia sp. ind., indicate the lower Callovian M. gracilis Zone.
There are no ammonite records indicating the B. bullatus
Zone (lowermost Callovian). Between 5.30 and 5.86 m,
the occurrence of Choffatia sp., Reineckeia nodosa Till (Pl.
1, fig. 9) and Reineckeia cf. nodosa Till (Pl. 1, fig. 14) was
detected; the latter, described and illustrated by Jeannet
(1951), are related to the R. anceps Zone. At about 6.20
m, the occurrence of a truncated specimen of Passendor-
feria (Macroconch), close to the group czenstochowiensis
(Siemiradzki), suggests the upper part of the P. clarom-
ontanus Zone. Two specimens of Prososphinctes, close to
the form described Prososphinctes sp. nov. A by Bourseau
(1977) were found between 6.25 and 6.30 m. Two speci-
mens, of Neocampylites delmontanus (Oppel) and of Tara-
melliceras obumbrans Hölder respectively, come from the
same level. According to Bourseau (1977), these species
may represent the lower P. plicatilis Zone, i.e. C. vertebrale
Subzone. Upwards, at 6.50 m, a specimen of Perisphinc-
tes sp. was recovered. This specimen could represent the
macroconch of Perisphinctes montfalconensis de Loriol,
also typical of the C. vertebrale Subzone. Passendorferia
(Macroconch Passendorferia) aff. tenuis (Enay) (Pl. 1, fig.
5) also occurs in this level. At 6.75 m, the succession is
marked by a sharp discontinuity surface, where a truncate
specimen of Tornquistes sp., showing intermediate features
between Pachytornquistes (Tornquistes) kobyi de Loriol and
Pachytornquistes (Tornquistes) oxfordiense (Tornquist), was
found. This surface probably represents the P. plicatilis-G.
transversarium Zone boundary. The ammonite record indi-
cates the existence of a biostratigraphic gap comprising at
least the P. antecedens and P. parandieri Subzones.
The G. transversarium Zone is well represented in
the overlying interval, between 6.75 and 7.25 m. The P.
luciaeformis Subzone is characterized, between 6.75 m and
7.10 m, by an ammonite assemblage comprising Passend-
orferia (Macroconch Passendorferia) ziegleri (Brochwicz-
Lewinski), found just five centimetres above the discon-
tinuity surface, Sequeirosia (microconch Gemmellarites)
trichoplocus (Gemmellaro), a specimen of Gregoryceras
transversarium (Quenstedt), and several Euaspidoceras
species. The L. schilli and P. rotoides Subzones could be
recognized between 7.17 and 7.25 m, in a mixed fossil as-
semblage. The specimens recorded, representative of this
stratigraphic interval, are: a juvenile specimen of Passen-
dorferia (Macroconch) erycensis Melendez (Pl. 1, fig. 7),
Fig. 5 - Chrono-lithostratigraphy and main bioevents of the Con-
trada Diesi, Section II.
Fig. 6 - Contrada Diesi Section II: distribution chart of the studied
fossils.
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Gregoryceras aff. G. fouquei (Kilian) and Sequeirosia (Mac-
roconch Sequeirosia) aff. trichoplocus (Gemmellaro). The
P. bifurcatus Zone can be recognized at 7.30 m. It is char-
acterized by the occurrence of Sequeirosia (Macroconch
Sequeirosia) sp. (Pl. 1, figs. 2,3), in some way comparable
to the specimen illustrated as P. (Arisphinctes) ex gr. tenuis
Enay by Brochwicz-Lewinski (1973) and several speci-
mens of Gregoryceras fouquei (Kilian) (Pl. 1, fig. 6).
The interval between 8.10 and 8.60 m yielded a few
specimens of Aspidoceras atavum (Oppel) (Pl. 1, fig. 4) and
Clambites schwabi (Oppel). This association may be typi-
cal of the E. bimammatum Zone, even though no typical
representative of the genus Epipeltoceras was found. The I.
planula Zone was recognized between 8.80 and 9.0 m. The
lower part of this Zone is characterized by a specimen of
Orthosphinctes cf. laufenensis (Siemiradzki) in association
with several specimens of Aspidoceras sp. and Physodoceras
sp. We have defined the Oxfordian-Kimmeridgian bound-
ary at the base of the I. planula Zone according to Matyja
& Wierzbowski (1997). The base of the S. platynota Zone
can be identified at about 9 m, where a specimen of Be-
nacoceras sp. (Pl. 1, fig.1) was recovered. The interval be-
tween 10 to 11.00 m yielded Nebrodites cafisii (Gemmel-
laro) (P. herbichi Zone) and several specimens of Taramel-
liceras sp. and Sowerbyceras loryi (Munier-Chalmas).
In the upper part of this section ammonites are very
rare. Some specimens of early Berriasian ammonites, i.e.
Spiticeras spitiense (Blanford) were found in the nodular
facies at about 19.30 m.
Section II - In this section the ammonites are
scanty, represented by common Phylloceratids and rare
diagnostic specimens (Fig. 6, Pl. 2). At the base of the
section the presence of Pseudowaagenia haynaldi (Her-
bich, in Neumayr), Taramelliceras gr. compsum (Oppel)
and Aspidoceras gr. acanthicum (Oppel) indicates a late
Kimmeridgian age. At 8.15 and 8.50 m, Corongoceras spp.
are present, defining the base of the upper Tithonian. At
14.50 m Tithopeltoceras paraskabensis (Fallot & Termier)
(Pl. 2, fig. 6) indicates the F. boissieri Subzone, of the low-
ermost Berriasian. Toward the top of the section, at 25
and 25.25 m, common specimens of Olcostephanus spp.
(Pl. 2, fig. 2) suggest a late Valanginian age. Lower Cre-
taceous belemnites like Duvalia lata de Blainville occur
in the same level.
Calcareous nannofossils
Section I - Seventy samples were examined for cal-
careous nannofossils using standard techniques for smear
slides preparation. Smear slides were observed under a
light polarizing microscope, at 1000x magnification. The
nannofossil zonation schemes utilized are those of Mat-
tioli & Erba (1999) for the Aalenian-Bathonian interval,
and Bralower et al. (1989) and Bown (1998) for the Ox-
fordian-Valanginian time span. The first eleven metres of
Section I are very poor in nannofossils, because the li-
thology is unfavourable to their preservation. Along the
section, ammonites are very frequent while the calcar-
eous nannofossil assemblages are poor, because of the
large amount of biodetritical supply, scarcity of micritic
sediments and additional impoverishment by diagenesis.
Watznaueria barnesae (Black) first appears at 2.00 m. The
FO of W. barnesae is reported by Mattioli & Erba (1999)
as typical for the early Bathonian. The ammonite fauna
found below this event is indeed Bathonian in age (Fig.
3). The upper portion of the section represents the op-
posite situation: the calcareous nannofossils content is
very high and the assemblages show high species diversity,
while the ammonite fauna is rare. Several calcareous nan-
nofossil events were identified during the Kimmeridgian,
Tithonian and Berriasian. The FO of Conusphaera mexi-
cana minor Bown & Cooper is found at 11.30 m in the
upper part of the Kimmeridgian, followed by C. mexica-
na mexicana Trejo and Polycostella beckmannii Thierstein
first appearences at the base of the Tithonian. The first
small specimens of the genus Nannoconus are found just
below the simultaneous occurrences of Nannoconus com-
pressus Bralower & Thierstein and Hexalithus noeliae Loe-
blich & Tappan at 14.00 m. The FO of Umbria granulosa
Bralower & Thierstein, marker for the upper Tithonian,
is found at 18.00 m. The lower Berriasian is identified
by the FO events of Nannoconus steinmannii Kamptner
subsp. minor Deres & Archéritéguy and Cruciellipsis cu-
villierii (Manivit) at 19.00 m. The last event is the FO of
N. steinmannii Kamptner subsp. steinmannii Kamptner
found at 20.20 m. These events identify the NJ20 Zone,
with both Subzone NJ20a and NJ20b, equivalent to Zone
NJK and NK1 of Bralower et al. (1989).
Section II (Fig. 5, 6) - Forty-five samples were ex-
amined, but only 30 samples were productive, with me-
dium to poor calcareous nannofossil assemblages. The
sterile samples are enriched by very fine quartz sand.
The first representative sample, at 3.50 m, contains
Watznaueria manivitae Buckry, Cyclagelosphaera deflan-
drei (Manivit), Conusphaera mexicana mexicana Trejo and
the first small specimens of Nannoconus sp. The presence
of Conusphaera mexicana mexicana and of Nannoconus
sp. characterizes the lower Tithonian.
Conusphaera mexicana mexicana increases rapidly
until 6.0 m, where P. beckmannii Thierstein is found, fol-
lowed by the first occurrence of Nannoconus compressus
which indicates the upper part of the lower Tithonian.
Up to 10 m, the assemblages are always dominated by
species of the genus Watznaueria; this is a typical conse-
quence of dissolution processes resulting in assemblages
impoverished by diagenesis. The presence of more mas-
sive and dissolution resistent taxa such as Conusphaera,
Polycostella and Nannoconus in the assemblage confirms
this interpretation.
Starting at 14.50 m, the calcareous nannofossil as-
semblage is characterized by abundant Nannoconus stein-
mannii steinmannii, Cruciellipsis cuvillieri, Watznaueria
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barnesae, C. margerelii, C. wiedmannii, Zeugrabdothus
cooperii Bown and very rare Conusphaera mexicana mex-
icana. This assemblage is typical of the lower Berriasian.
At 15.50 m from the base of the section, the assemblage
is characterized by the presence of common Retecapsa sur-
irella (Deflandre & Fert), Retecapsa angustiforata Black,
Nannoconus steinmannii steinmannii, Cruciellipsis cuvil-
lieri, Watznaueria barnesae, W. manivitae, C. margerelii
Nöel C. wiedmannii Reale & Monechi and Zeugrabdothus
cooperii. The Calcicalathina oblongata (Worsley), marker
of the lower Valanginian, first occurs at 16.00 m, while
Conusphaera mexicana mexicana disappears. The lower
Valanginian assemblages are very rich. C. oblongata be-
comes common and Assipetra infracretacea (Thierstein)
and Diazomatholitus lehmanii Noël are also present. At
24.00 m, Eiffellithus windii Applegate & Bergen, impor-
tant marker for the lower Valanginian, first occurs, while
Zeugrabdothus diplogrammus (Deflandre), indicating the
uppermost lower Valanginian, first occurs at 24.50 m.
Calpionellids
Some studies on the region of Sicily were taken
into consideration mainly to correlate the sequence of
events (De Wever et al. 1986; Catalano & Liguori 1971;
Cecca et al. 2001; Caracuel et al. 2002). Different bios-
tratigraphic zonations (Remane 1985; Grün & Blau 1997;
Remane 1998) were utilized for the identification of the
calpionellid zones and subzones.
Fig. 7 - Contrada Diesi Quarry, Section I: Ammonite distribution chart.
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Section I (Fig. 3) - The calpionellid assemblages are
very poor and the state of preservation is moderate. The
first occurrence of calpionellids is at 18.00 m and is rep-
resented by common and diversified species of Crassicol-
laria. Just above, Remaniella sp. occurs in concomitance
with the last occurrence of Saccocoma. At 19.00 m the
bloom of Calpionella alpina Lorenz, isometric specimens,
is found. This event is used to identify the Tithonian/
Berriasian boundary (Remane 1998; Oloriz et al. 1995;
Caracuel et al. 2002). Just above, the FO of Remaniel-
la duranddelgai (Pop), confirms the early Berriasian age
(Grün & Blau 1997).
Section II - Section II of Contrada Diesi shows
well preserved, diversified and abundant calpionellid as-
semblages that allow the identification of several zones
and subzones (Figs. 5, 6 and Pl. 3).
The first occurrence of calpionellids is found at
8.50 m from the base of the section and it is represent-
ed by small Tintinnopsella remanei (Colom), Calpionel-
la alpina Lorenz and Crassicollaria spp. This assemblage
identifies the Crassicollaria Zone (A Zone of Remane
1998 and Remanei Subzone of Grün & Blau 1997),
which mark the base of the upper Tithonian. From 8.90
m, the assemblage becomes more abundant and diversi-
fied with the appearance of Crassicollaria brevis Remane
(Pl. 3, fig. 3), Crassicollaria massutiniana (Colom) (Pl.
3, fig. 4), Crassicollaria intermedia (Durand-Delga) (Pl.
3, fig. 1), Crassicollaria parvula Remane (Pl. 3, fig. 2); in
this assemblage also C. alpina, Tintinnopsella carpathica
(Murgeanu & Filipescu) (Pl. 3, fig. 15) and transition-
al forms of C. alpina/Calpionella elliptica (Pl. 3, fig. 8)
(Calpionella sp. in Catalano & Liguori 1971, Pl. 2, figs.
11,12 and C alpina homeomorph of C. elliptica in Re-
mane 1985, fig. 6 and in Cecca et al. 2001) are present.
This assemblage is referable to the Crassicollaria Zone
(Intermedia Subzone). At 9.50 m, the genus Remaniella,
that marks the Catalanoi Subzone (Grün & Blau 1997),
first occurs. The finding of all three subzones of the
Crassicollaria Zone records the presence of the entire
upper Tithonian.
The Tithonian/Berriasian boundary was recognized
on the basis of the C. alpina isometric bloom (Pl. 3, fig. 9)
(explosive extention of a smaller and spherical variety of
C. alpina in Remane 1986). This event shows clearly the
decrease of the Crassicollaria genus, which is represent-
ed only by Cr. parvula (Cecca et al. 2001). The first oc-
currence of Remaniella cf. duranddelgai (Pop) (Pl. 3, fig.
7) is coeval with this bloom. On the whole, this change
inside the assemblage identifies the base of the B Zone
(Remane 1998), that corresponds to the base of the Cal-
pionella Zone (Grün & Blau 1997). Just above, Lorenziella
dacica (Filipescu & Dragastan) occurs. The assemblage
does not change until 15.50 m, where the FO of Calpi-
onellites darderi (Colom) (Pl. 3, figs. 16) marks the base
of the Valanginian (Calpionellites Zone). Ct. darderi is re-
corded together with Praecalpionellites dadayi (Knauer)
(Pl. 3, fig. 13), Calpionellopsis oblonga (Cadisch) (Pl. 3,
fig. 10) and Praecalpionellites murgeanui (Pop). At 23.50
m, Calpionellites major (Trejo), marker of the Major Sub-
zone, first occurs, indicating the upper part of the ear-
ly Valanginian. Calpionellid assemblages referable to the
middle and upper Berriasian age were not found.
Discussion and conclusion
An interpretation of the Saccense Domain sedimen-
tary evolution during the early Bathonian- late Valangin-
ian time interval was made possible by the new litho- and
biostratigraphic data collected at Mt. Magaggiaro. In ad-
dition, the comparison of bioevents related to different
fossil groups was useful to critically assess the calibrated
biostratigraphic schemes already existing.
One of the most striking features of this succes-
sion is the paraconformity between the bioclastic plat-
form limestone (Inici Fm., Sinemurian p.p.) and the over-
lying pelagic deposits, i.e. the Bositra limestone (lower
Bathonian-middle Oxfordian). This pelagic unit is fol-
lowed by a calcisiltitic limestone (middle-upper Oxford-
ian), through a sharp discontinuity surface marked by a
thin, black stromatolitic crust. The sedimentation then
evolves, through a stromatolitic level and a pebbly cal-
carenite (Kimmeridgian-Tithonian), into a nodular mar-
ly limestone (Tithonian). The nodular marly limestone
is gradually replaced by a whitish, thinly-bedded lime-
stone, the Calcari a Calpionelle of late Tithonian to late
Valanginian age.
In the lower part of the succession the biostrati-
graphic analysis was facilitated by the presence of rich
ammonite assemblages. Ammonite distribution produced
new biostratigraphic elements indicating several biozones
of the Bathonian-late Valanginian time interval. Callovian
ammonites (M. gracilis Zone, R. anceps Zone) are rela-
tively rare, while Bathonian (Z. zigzag Zone, P. progracilis
Zone, H. retrocostatum Zone), Oxfordian (P. claromon-
tanus Zone, P. plicatilis Zone, G. transversarium Zone, P.
bifurcatus Zone, E. bimammatum Zone), and early Kim-
meridgian (I. planula Zone, S. platynota Zone, P. herbichi
Zone) ammonites are well represented. The occurrence
of Corongoceras spp. indicates the base of the upper Ti-
thonian, while Tithopeltoceras paraskabensis (Fallot &
Termier) and Spiticeras spitiense (Blanford) indicate the
lower Berriasian. Furthermore, common specimens of
Olcostephanus spp. at the top of the succession suggest
a late Valanginian age.
Biofacies analysis pointed out the occurrence of
the following significant events:
- the abundance of thin-shelled bivalves character-
izes the Bathonian-Callovian interval and their disappear-
ance at the base of the middle Oxfordian is coincident
with a sharp discontinuity surface;
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- Protoglobigerinids from the Bathonian to the
lower Kimmeridgian are replaced by Saccocoma sp.; the
first occurrence of Saccocoma is recorded in the S. platyno-
ta Zone (lower Kimmeridgian), and its last appearance is
recorded in the latest Tithonian;
- the bloom of isometric C. alpina marks the
Tithonian/Berriasian boundary, which is here included
between the FO of U. granulosa of the uppermost up-
per Tithonian and the occurrence of S. spitiense, which
indicates the base of the lowerBerriasian;
- the base of the Valanginian is marked by the first
occurrence of Ct. darderi. It was found just above the oc-
currence of Tithopeltoceras paraskabensis, early Berriasian
in age;
- just above the FO of Ct. darderi (base of the Va-
langinian), the FO of C. oblongata and LO of C. mexi-
cana mexicana occur;
- upper Valanginian ammonites and belemnites
(Olcostephanus spp. and Duvalia lata) are found togeth-
er with Tirnovella gr. alpillensis and FO of Ct. major, E.
windii and Z. diplogrammus.
These data show that the middle-upper part of the
lower Berriasian and the middle-upper Berriasian are not
recorded, indicating the presence of sedimentary gaps.
It is confirmed that the nodular marly limestone facies
persists until the lower Berriasian, as it often happens in
other high structural areas in Sicily and in other Tethy-
an areas.
The different and sudden facies changes, with am-
monites capped by stromatolitic domes, found at different
stratigraphic levels, the occurrences of many discontinuity
surfaces and the reduced thickness of the sequence, sug-
gest an environment characterized by reduced but still ac-
tive sedimentary supply, low sedimentation rate and abrupt
and quite important energy changes.
All these sedimentary features suggest a very com-
plex scenario for the depositional environment of the
pelagic sediments cropping out in the Mt. Magaggiaro
succession. Nevertheless, the existence of gaps could be
related to submarine non-deposition or erosion. The pres-
ence of pelagic sediments, together with rich biogenic
and bioclastic supply, suggest that the environment of
the Mt. Magaggiaro area was a pelagic carbonate platform
that followed the drowning of the carbonate platform..
The major deepening happened during the Valanginian.
The sediments recorded in the Saccense domain display
a high degree of facies variability, probably due to the ir-
regular pre-existing, perhaps tectonically controlled, pal-
aeomorphology.
Acknowledgments. We thank J. Cope (Cardiff), P. Di Stefano
(Palermo) and U. Nicosia (Roma) for assistance in the field. We are
grateful to A. Galácz (Budapest) and J. Remane (Neuchâtel) for their
comments and suggestions. This work was supported by the Italian Min-
istry of University and Research and by the University of Perugia and
Rome (grants to G. Parisi and U. Nicosia, COFIN1999 and 2001).
During the printing of this paper unfortunately Giovanni Pal-
lini, coauthor besides remarkable scientist and darling friend, died. All
the Authors should like to mention him and dedicate this paper to his
memory.
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PLATE 1
Ammonites of Contrada Diesi Quarry, Section I: Fig.1) Benacoceras sp.; Figg. 2 and 3) Sequeirosia sp.; Fig. 4) Aspidoceras atavum (Oppel); Fig.
5) Passendorferia aff. tenuis (Eany); Fig. 6) Gregoryceras fouquei (Kilian); Fig. 7) Passendorferia erycensis (Melendez); Fig. 8) Hecticoceras posterius
Zeiss; Fig. 9) Reineckeia nodosa Till; Figg. 10 and 13) Cadomites (Cadomites) daubenyi (Gemmellaro); Fig. 11) Bullatimorphites (Bullatimorphites)
hannoveranus (Roemer); Fig. 12) Cadomites (Cadomites) orbignyi (De Grossouvre); Fig. 14) Reineckeia cf. nodosa Till.
PLATE 2
Ammonites of Contrada Diesi, Section I and II: Fig. 1) Taramelliceras sp.; Fig. 2) Olcostephanus sp.; Fig. 3) Spiticeras spitiense (Blanford); Fig. 4)
Torquatisphinctes gr. laxus Oloriz; Fig. 5) Taramelliceras pugile pugiloides (Canavari); Fig. 6) Tithopeltoceras paraskabensis (Fallot & Termier); Fig.
7) Micracathoceras micracanthum (Oppel). Scale bar = 2 cm.
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PLATE 3
Calpionellids of Contrada Diesi, Section II: Fig. 1) Crassicollaria intermedia (Durand-Delga), sample A9.50; Fig. 2) Crassicollaria parvula Re-
mane, sample A9.50; Fig. 3) Crassicollaria brevis Remane, sample A9.50; Fig. 4) Crassicollaria massutiniana (Colom), sample A8.90; Fig. 5) Re-
maniella ferasini (Catalano), sample A8.90; Fig. 6) Remaniella catalanoi Pop, sample L9; Fig. 7) Remaniella cf. duranddelgai Pop, sample A11.30;
Fig. 8) Calpionella alpina transitional form to Calpionella elliptica, sample A11.30; Fig. 9) Calpionella alpina Lorenz isometric form, sample L9;
Fig. 10) Calpionellopsis oblonga (Cadish), sample L6; Fig. 11) Tintinnopsella longa (Colom), oblique section, sample A12.50; Fig. 12) Praecalpi-
onellites filipescui (Pop), sample L6A; Fig. 13) Praecalpionellites dadayi (Knauer), L5A; Fig. 14) Tintinnopsella longa (Colom), sample L2; Fig. 15)
Tintinnopsella carpathica (Murgeanu & Filipescu), sample L9; Fig. 16) Calpionellites darderi (Colom), sample L5; Fig.17) Calpionellites cf. major
(Trejo), sample L3A. Scale bar= 50 µm.
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