www.geologicacarpathica.com
G
G
G
G
GEOL
EOL
EOL
EOL
EOLOGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPATHICA
THICA
THICA
THICA
THICA
, OCTOBER 2015, 66, 5, 393—407 doi: 10.1515/geoca-2015-0033
On the peritidal cycles and their diagenetic evolution in the
Lower Jurassic carbonates of the Calcare Massiccio
Formation (Central Apennines)
MARCO BRANDANO
1,2
, LAURA CORDA
1
, LAURA TOMASSETTI
1
and DAVIDE TESTA
1
1
Department of Earth Sciences, Sapienza University of Rome, P. Aldo Moro 5, I-00185, Italy;
laura.corda@uniroma1.it; laura.tomassetti@uniroma1.it; davidetesta.86@gmail.com
2
Institute of Environmental Geology and Geoengineering (IGAG) CNR, Via Salaria km 29, I-00016, Italy; marco.brandano@uniroma1.it
(Manuscript received March 4, 2015; accepted in revised form June 23, 2015)
Abstract: This paper shows the environmental changes and high-frequency cyclicity recorded by Lower Jurassic shal-
low-water carbonates known as the Calcare Massiccio Formation which crop out in the central Apennines of Italy.
Three types of sedimentary cycle bounded by subaerial erosion have been recognized: Type I consists of a shallowing
upward cycle with oncoidal floatstones to rudstones passing gradationally up into peloidal packstone alternating with
cryptoalgal laminites and often bounded by desiccation cracks and pisolitic-peloidal wackestones indicating a period of
subaerial exposure. Type II shows a symmetrical trend in terms of facies arrangement with peloidal packstones and
cryptoalgal laminites present both at the base and in the upper portion of the cycle, separated by oncoidal floatstones to
rudstones. Type III displays a shallowing upward trend with an initial erosion surface overlain by oncoidal floatstones
to rudstones that, in turn, are capped by pisolitic-peloidal wackestones and desiccation sheet cracks. Sheet cracks at the
top of cycles formed during the initial phase of subaerial exposure were successively enlarged by dissolution during
prolonged subaerial exposure. The following sea-level fall produced dissolution cavities in subtidal facies, while the
successive sea-level rise resulted in the precipitation of marine cements in dissolution cavities. Spectral analysis re-
vealed six peaks, five of which are consistent with orbital cycles. While a tectonic control cannot be disregarded, the
main signal recorded by the sedimentary succession points toward a main control related to orbital forcing. High
frequency sea-level fluctuations also controlled diagenetic processes.
Key words: cyclostratigraphy, diagenesis, Calcare Massiccio, Apennines, Jurassic.
Introduction
One goal of the sedimentologist is to decipher signals re-
corded in the sedimentary record. The carbonate sedimentol-
ogist has to understand how and where carbonate sediments
have been created in response to intrinsic and extrinsic
mechanisms forced by tectonic, eustatic, oceanographic and
climatic processes, and ecological changes (Lukasik & Simo
2008; Strasser & Vedrine 2009; D’Argenio et al. 2011).
Modern carbonate platforms provide a means to examine
how many depositional processes occur and demonstrate the
complexity of facies associations (Wright & Burgess 2005;
Strasser & Vedrine 2009). When dealing with carbonate plat-
forms in the geological past, detecting facies associations and
the origin of stacked cycles becomes more difficult. In particu-
lar, a long debated problem in stratigraphy is whether to relate
the formation of peritidal carbonate cycles to autocyclic pro-
cesses (Hardie 1986; Pratt et al. 1992) or to allocyclic processes
(both Milankovitch and tectonic models). Autocyclic pro-
cesses include progradation of shorelines and lateral migration
of tidal channels, tidal inlets and bars (Ginsburg 1991). These
processes are inherent to the shallowest environments of the
platform (Strasser 1994). Cyclical perturbation of the Earth’s
orbit induces changes in the insolation and consequently sea
level, climatic, oceanographic, sedimentary, and biological
changes that are potentially recorded in the sedimentary ar-
chives through geological time (Strasser 1994; Strasser et al.
2006). In the case of proved Milankovitch cyclicity, the dura-
tion of the smaller-scale depositional sequences lies within the
Milankovitch frequency band, then a very narrow time frame-
work of 20, 41 and 100 to 400 ka can be established (Strasser
et al. 1999, 2006; D’Argenio et al. 2011). Twenty-one ka
cyclicity is produced by the precession of the equinoxes,
41 ka cyclicity is related to the obliquity of the Earth’s axis,
and the 100—400 ka cyclicity is produced by variation in the
eccentricity of the ellipse of the Earth’s orbit of ~ 100 (short
eccentricity) and ~ 400 ka (long eccentricity) periods.
On the basis of stacking patterns and time-series analysis
of western Mediterranean Lower Jurassic shallow-water car-
bonates, Crevello (1991) recognized a Milankovitch-type
cyclicity. However, tectonic subsidence changes can also
produce sedimentary cycles. Burgess (2001) showed that
shoreline and island progradation, controlled by subsidence
and sediment transport rate, are also plausible mechanisms
to create variable thickness, shallowing-upward peritidal
parasequences and should be considered in interpretations of
such strata. Based on datasets from different Lower Jurassic
peritidal cycles from western Tethyan platforms, Bosence et
al. (2009) argued strongly for an overriding tectonic control
on cycle formation.
394
BRANDANO, CORDA, TOMASSETTI and TESTA
G
G
G
G
GEOL
EOL
EOL
EOL
EOLOGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPATHICA
THICA
THICA
THICA
THICA, 2015, 66, 5, 393—407
This paper illustrates the high frequency cyclicity of the
Lower Jurassic shallow-water carbonates known as the
Calcare Massiccio Formation. The Calcare Massiccio For-
mation belongs to the Tethyan Liassic carbonate platform
domain that developed in the large epicontinental sea that
covered shelf areas of present-day North Africa and Western
Europe as well as the Apennines and the Pelagonian plat-
form of present-day Greece (Bosence et al. 2009). In the
Apennines, the Calcare Massiccio Formation is character-
ized by lateral variation in depositional environments and
in thickness, probably related to an articulated physiography
of the Triassic to Lower Jurassic carbonate platform
(Centamore et al. 1971). For this reason, it has been subdi-
vided into a number of lithostratigraphic sub-units. The ar-
ticulated physiography was attributed to the beginning of
tectonic extension, which created two different domains: a
persistent carbonate platform (Latium-Abruzzi domain) and a
deep-water domain (Umbria-Sabina Basin) with intrabasinal
structural highs. On the structural highs, the Calcare
Massiccio Formation is characterized by peritidal cyclical
sedimentation and is usually overlain by pelagic sea-mount
deposits represented by condensed pelagic cephalopod-rich
carbonates of the upper Pliensbachian—Tithonian Bugarone
unit (reduced sequences) that are no more than a few tens of
metres thick (Centamore et al. 1971; Pialli 1971; Colacicchi
et al. 1975). Deposition in the structural depressions was
characterized by the relatively deep, subtidal Calcare
Massiccio Formation that does not show evidence for cycli-
cal sedimentation (Santantonio 1993).
Notwithstanding the great extent of the Tethyan Liassic car-
bonate platform, few works have analysed the origin of the
sedimentary cyclicity following a cyclostratigraphic approach
(Bigozzi 1990; Bosence et al. 2000, 2009). This approach
uses astronomical cycles of known periodicities to date and
interpret the sedimentary record (Strasser et al. 2006).
This paper presents an analysis of environmental and dia-
genetic changes recorded in the Calcare Massiccio Forma-
tion deposited on structural highs. Based on detailed logging
and facies analysis of a well exposed section, sedimentary
cycles are defined according to cyclostratigraphic concepts.
This paper aims to distinguish the controlling factors pro-
ducing the cyclicity of the Calcare Massiccio Formation, and
to evaluate the role of autocyclic vs. allocyclic processes.
Geological setting
The studied area is located near S. Angelo Romano vil-
lage, in the Cornicolani Mountains (Fig. 1b). These moun-
tains belong to the Apennine chain and represent a structural
high within the Sabina Basin that developed from the
Pliensbachian to Tithonian.
The Apennines are an asymmetric fold and thrust belt de-
veloped on top of an eastward-retreating westward dipping
continental slab attached to the Adriatic plate (Doglioni
1991; Carminati & Doglioni 2005; Carminati et al. 2010,
2013). The Neogene to Quaternary evolution of the North-
ern-Central Apennines is characterized by east-north-eastward
migration of deformation fronts of the related foredeeps
coupled with extensional tectonics in the hinterland leading
to the opening of progressively younger backarc basins
(Gueguen et al. 1998).
The central Apennines fold-and-thrust belt consists of a
Meso-Cenozoic succession deposited on the Adria passive
margin (Fig. 1a). Deposition began with continental to ma-
rine clastic sediments followed first by Upper Triassic dolo-
mitic and/or evaporitic deposits (Burano Formation) and
then by Lower Jurassic peritidal carbonates represented by
the Calcare Massiccio Formation, which ranges in thickness
from three to seven hundred meters (Pialli 1971). The
Calcare Massiccio Formation is generally dated Late
Hettangian—Early Pliensbachian (Ibex Biozone). Deposition
of peritidal carbonate sediments persisted from Late
Hettangian to Sinemurian when a rifting phase led to plat-
form fragmentation and drowning. The resulting complex ar-
chitecture was characterized by spatial and temporal
variations in subsidence rates (Carminati et al. 2013), pro-
duced by extensional tectonic processes, which created a
persistent carbonate platform (Latium-Abruzzi carbonate
platform), a deep-water domain (Umbria-Marche and Sabina
pelagic basin) and intrabasinal morpho-structural highs
(Centamore et al. 1971; Damiani et al. 1992; Santantonio
1993; Galluzzo & Santantonio 2002; Cosentino et al. 2004).
From the Sinemurian onward, the Latium-Abruzzi carbon-
ate platform persisted as a monotonous repetition of subtidal
and peritidal cycles, interrupted by short periods of
emersion, which were associated with bauxite development.
After the fragmentation and drowning of the Hettangian-
Sinemurian platform, the Umbria-Marche and Sabina do-
main developed into a wide pelagic basin with scattered
fault-bounded structural highs (pelagic carbonate platforms
sensu Santantonio 1993) characterized by normal and con-
densed pelagic deposits, respectively. The structural-high
blocks, within the Umbria-Marche and Sabina domain were
characterized by high subsidence rates occurring during the
deposition of the Calcare Massiccio Formation (Carminati et
al. 2013). With the activation of late Hettangian—Sinemurian
extensional tectonics, subsidence rates drastically increased
in the sectors which would later host thick pelagic successions
(the definitive drowning of the Calcare Massiccio platform
occurred in the Early Sinemurian). At the structural highs,
the shallow-water deposition of the Calcare Massiccio Forma-
tion persisted until the Sinemurian—Early Pliensbachian and
was followed by condensed pelagic deposits (Santantonio
1993; Passeri & Venturi 2005).
Analysis of sedimentary cycles in the Calcare Massiccio
Formation was first undertaken by Colacicchi et al. (1975).
These authors recognized sequences of facies evolving gradu-
ally from subtidal to supratidal environments arranged into
predominantly shallowing upward cycles. The authors also re-
ported the occurrence of cycles, which do not follow this
Waltherian model, but document the superposition of
supratidal facies directly on subtidal facies. The same cycles
were also recognized by Bigozzi (1990) who showed an orga-
nized stacking pattern consisting of megacycles each compris-
ing five individual cycles and interpreted as the product of
high-frequency sea-level changes probably produced by varia-
tion of orbital parameters. Successively, Bosence et al. (2009)
395
LOWER JURASSIC PERIDITAL CYCLES, CALCARE MASSICCIO Fm (CENTRAL APENNINES)
G
G
G
G
GEOL
EOL
EOL
EOL
EOLOGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPATHICA
THICA
THICA
THICA
THICA, 2015, 65, 5, 393—407
presented the analysis of different Lower Jurassic succes-
sions along the Tethys margin including the Apennines suc-
cession in Umbria. These authors recognized five sedimentary
cycles, two of them present in the Umbrian Apennines suc-
cession (
α and γ). According to Bosence et al. (2009), α cycles
are asymmetrical, shallowing-upward cycles that evolve up-
ward from open-marine to subaerial or restricted marine to in-
tertidal facies associations. Cycle boundaries are marked by
erosional surfaces overlain by evidence of marine flooding.
The
γ cycles show a symmetrical arrangement of facies with a
transgressive phase, an interval of maximum marine flooding,
followed by a regressive phase capped by an erosional sur-
face. In these cycles, the intertidal and subaerial facies asso-
ciations are well developed and the top of the cycle is charac-
terized by calcretes with tepees. According to Bosence et al.
(2009), both
α and γ cycles may be generated by allocyclic
and autocyclic mechanisms. The other three cycle types char-
acterizing the Liassic platform outside the Apenninic domain
are: the deepening upward
β cycles bounded by an erosional
surface; the asymmetrical
δ cycles composed of subtidal sedi-
mentary facies with a subaerial diagenetic overprint affecting
its upper surface; the
ε cycles, which are characterized by
subtidal facies with a deepening upward trend. According to
Bosence et al. (2009), these cycles can be generated only by
allocyclic controls. The common character of these cycles is
the scarcity of intertidal facies, dominance of subtidal facies
Fig. 1. Geological situation, from general to detail. a – schematic geological map of Central Apennines, b – geological map of Cornicolani
Mountains and location of studied section (modified from Billi et al. 2007).
396
BRANDANO, CORDA, TOMASSETTI and TESTA
G
G
G
G
GEOL
EOL
EOL
EOL
EOLOGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPATHICA
THICA
THICA
THICA
THICA, 2015, 66, 5, 393—407
and a deepening upward trend indicative of relatively more
open marine environments.
The investigated stratigraphic section comes from the
end of the upper portion of the Calcare Massiccio Forma-
tion cropping out in the Cornicolani Mountains. Many sedi-
mentological works on the Calcare Massiccio demonstrate
a cyclically monotonous alternation of few lithofacies
forming
α and γ cycles (sensu Bosence et al. 2009), al-
though the formation displays a remarkable thickness of
up to 700 m (Pialli 1971; Colacicchi et al. 1975; Bigozzi
1990; Barattolo & Bigozzi 1996; Passeri & Venturi 2005;
Bosence et al. 2009). In this work, we present a high-reso-
lution analysis of a very well exposed road cutting (26 m
exposed thickness) located in the structural high of the
Cornicolani Mountains at the end of the upper portion of
the Calcare Massiccio Formation, around 40 m before the
drowning succession. Notwithstanding the limited thick-
ness, this section displays facies associations typical of the
peritidal cycles characterizing the Calcare Massiccio and
can be considered representative of the recorded cyclicity.
Material and methods
An outcrop in an abandoned quarry and a well-exposed
stratigraphic section along the road to S. Angelo Romano
village provide a good opportunity to study the facies as-
sociations of Calcare Massiccio Formation (Fig. 1). Tex-
tural and compositional data were observed in the field at
centimeter scale, providing a virtually continuous sedi-
mentological data set recording the stratigraphic evolution
of the investigated interval. For the sedimentary cycle
identification we followed the methodology of Bosence et
al. (2009). We used the term sedimentary cycle to identify
commonly repeated meter-scale lithofacies successions.
These cycles comprise bundles of beds of different thick-
ness separated by erosional surfaces. Each erosional sur-
face is overlain by relatively open marine facies (e.g.
subtidal facies) evolving upward to shallower more re-
stricted facies (from intertidal to supratidal facies). The
cycle boundary is placed at the most prominent erosional
surface or at a non-Waltherian facies shift at the accommo-
dation minima, for example, at the subtidal facies directly
overlying a subaerial exposure surface, or intertidal facies.
In order to better characterize the sedimentary facies and
the composition of the investigated carbonates, 82 samples
were collected along the measured section (Fig. 2). A se-
lected set of 70 thin sections was studied and classified
according to the nomenclature of Dunham (1962) and
Embry & Klovan (1971) for carbonate rocks and their
compositional and diagenetic characteristics recorded.
Ten selected thin sections were polished and examined
under cathodoluminescence (CL) microscopy at the Earth
Science Department “Ardito Desio” of the University of
Milan. Twenty selected thin sections, were polished and
Fig. 2. Measured section from the Calcare Massiccio Formation and
thickness recurrences of the main facies associations.
Twenty oxygen and carbon stable isotope analyses were
carried out on 15 samples obtained with a hand-operated
microdrill, using 0.5 mm Ø tungsten drill bits. All of the dif-
ferent recognized cements were sampled. Analyses were per-
carbon-coated and subjected to electron microprobe analysis
to determine the concentration of Mg, Sr, Mn, Fe and Ba
(CAMECA instrument – Istituto di Geologia Ambientale e
Geoingegneria-CNR, University of Roma “La Sapienza”).
397
LOWER JURASSIC PERIDITAL CYCLES, CALCARE MASSICCIO Fm (CENTRAL APENNINES)
G
G
G
G
GEOL
EOL
EOL
EOL
EOLOGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPATHICA
THICA
THICA
THICA
THICA, 2015, 65, 5, 393—407
formed using a Finnigan MAT 252 mass spectrometer at the
isotope geochemistry laboratory of the Istituto di Geologia
Ambientale e Geoingegneria-CNR. The results were cali-
brated using NBS carbonate standard and are reported on the
PeeDee belemnite (PDB) scale. The analytical precision for
the isotope data is ± 0.1 ‰
.
based on replicate standards.
87
Sr/
86
Sr dating was carried on the micrite of pure lime-
mudstones. It was microdrilled after examination under
cathodoluminescence with the luminescent portion being
discarded. Isotopic analyses were performed at IGAG-CNR
(Dipartimento di Scienze della Terra, University of Rome
“La Sapienza”) using a Finnigan MAT 262RPQ multi-
collector mass spectrometer. All samples were loaded on a
double Re filament as nitrate and analysed in static mode.
Measured Sr isotope ratios were normalized for mass fractio-
nation to
87
Sr/
86
Sr = 0.1194. NBS987 yielded a
86
Sr/
87
Sr value
of 0.710235 + /—10. The averaged analytical error (2
σ) of
86
Sr/
87
Sr was ± 0.000011 (n = 16). The
86
Sr/
87
Sr values of the
samples were converted to numerical ages using Version 4B:
08/04 of the Look-Up Table of Howarth & McArthur (1997).
An observational time series was generated from the mea-
sured stratigraphic section. A numerical value (1—3) was as-
signed to each facies association recognized (Fig. 2). A spot
sampling method was used to generate continuous-signal
records (Weedon 2003). The classical method of searching
for cyclicity in time series uses spectral analysis. This
method looks at time series in terms of their frequency com-
position (Schwarzacher 1993). Time-series analysis of the
investigated section was performed by using thickness recur-
rences of the main facies associations (Fig. 2). The sampling
interval to perform the time series analysis was 1 cm, which
was chosen based on the facies-thickness data for the investi-
gated section. To mathematically study the signal frequency,
Fourier analysis was performed with the Macintosh-based
software Analyseries 1.1 (Paillard et al. 1996). The maxi-
mum entropy approach and the Blackman-Tuckey power
spectrum estimator were used (Blackman & Tuckey 1958).
Results
In the studied section, three lithofacies associations (LF-A,
-B, and -C) were identified based on texture, main constitu-
ents, fabrics and early diagenetic features. These are inter-
preted as representing the three main sedimentary environ-
ments of the inner platform environment represented by the
Calcare Massiccio Formation (Table 1). According to the
studies on modern and ancient peritidal carbonate systems
(Pratt et al. 1992; Strasser & Vedrine 2009), the sedimento-
logical interpretation leads to a facies model representing the
spatial distribution of the products of different sedimentary
processes occurring in the different environments of the
Calcare Massiccio platform.
The investigated section comprises the last interval of the
Calcare Massiccio Formation in the Cornicolani Mountains,
where outcrops occur of about a hundred meters of peritidal
carbonates covered by beds of the drowing succession
(Cosentino et al. 2004).
The isotopic age obtained from strontium isotope analysis
of micrites from the base of the section (Fig. 2) approximates
194.30 Ma confirming a Sinemurian age for the upper part of
the formation. Lastly 19 sedimentary cycles have been rec-
ognized, with thickness ranging between 0.5 and 3 m, with
average of 1.36 m.
Lithofacies associations
LF-A packstones to grainstones with ooids, oncoidal float-
stones to rudstones
This facies association is characterized by two sublitho-
facies: packstones to grainstones (LF-A1) and oncoidal
floatstone to rudstone (LF-A2). LF-A1 comprises abundant
ooids, peloids (fecal pellets, algal peloids, microbial peloids)
and aggregate grains such as lumps. The ooids show a large
micritized nucleus and a very thin cortex characteristic of su-
perficial ooids (sensu Carozzi 1957). Typical skeletal grains
are small benthic foraminifera (valvulinids, textulariids and
lituolids), ostracods, mollusc fragments and cortoids, small
ammonites, Cayeuxia, thaumatoporellids, and porostromata
cyanobacteria (Fig. 3a). LF-A2 is dominated by oncoids of
various shape and size (up to 2 cm). Two types of oncoids are
identified: Type 1 and Type 2 (sensu Védrine et al. 2007).
Type 1 oncoids are up to 0.5 mm in diameter and show spheri-
cal to elliptical shape with smooth contours. The cortex is
micritic, homogeneous and lacks associated microencrusting
Lithofacies associations Sub-lithofacies
Components
Environment
LF-A packstones to
grainstones with ooids,
oncoidal floatstones to
rudstones
Packstones to
grainstones (LF-A1)
Peloids, superficial ooids, lumps and subordinate small benthic
foraminifera, ostracods, mollusc fragments, cortoids, Cayeuxia,
thaumatoporellids, porostromata cyanobacteria
Shallow subtidal environment
under moderately to high
energy conditions
characterizing lagoonal
channels or shoals
Floatstones to
rudstones (LF-A2)
Type 1 and type 2 oncoids, matrix comprising peloids and
skeletal fragments
LF-B peloidal
wackestones to
packstones alternating
with cryptalgal
bindstone
Peloidal wackestones
to packstones (LF-B1)
Peloids, small benthic foraminifera lituolids and textulariids,
small ostracods, serpulids, gastropod fragments and Cayeuxia
Intertidal and supratidal
environment
Bindstones (LF-B2)
Planar algal laminae and trapped mud, type 3 oncoids with
Bacinella irregularis, Lithocodium aggregatum, Cayeuxia,
subordinate type 2 oncoids
LF-C pisolitic-peloidal
wackestones with
extensive sheet-cracks
Pisoids and peloids
Supratidal environment
Table 1: Lithofacies associations of the Calcare Massiccio Formation and their interpreted environmental setting.
398
BRANDANO, CORDA, TOMASSETTI and TESTA
G
G
G
G
GEOL
EOL
EOL
EOL
EOLOGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPATHICA
THICA
THICA
THICA
THICA, 2015, 66, 5, 393—407
fauna. Laminations are micritic but rarely visible. Nuclei are
lithoclastic and comprise small ooids and/or aggregate grains.
Type 2 oncoids have diameters of between a few millimeters
and 2 cm and elliptical to elongated shapes with smooth con-
tours. The cortex is micritic with laminae easily recognizable.
Laminae are micritic but irregular and locally truncated, show-
ing different growth phases. Couplets of micritic and sparry
laminae are present and accentuate the laminar structure of the
Type 2 oncoids. Both lithoclastic (peloids, ooids) and bio-
clastic (echinoid fragments, Cayeuxia) nuclei occur (Fig. 4a).
Occasionally, small ooids are incorporated into the cortex.
Some serpulids and small articulated ostracods also occur
within the matrix.
The matrix of the oncoidal floatstones to rudstones con-
sists of fine-grained peloids or skeletal fragments. When the
matrix is lacking, oncoids are usually surrounded by a thin
rim of isopachous fibrous cement and later drusy mosaic ce-
ment. Dissolution cavities are diffuse and infilled by drusy
mosaic cement (Fig. 5a).
Interpretation:
This facies association was deposited in a shallow subtidal
environment under moderate to high energy conditions char-
acterizing lagoonal channels or shoals (Colacicchi et al.
1975; Barattolo & Bigozzi 1996; Pomoni-Papaioannou &
Kostopoulou 2008) as demonstrated by the textural charac-
Fig. 3. Field photographs of the recognized lithofacies associations. a – LF-A packstone to grainstone with ooids, oncoidal floatstone to
rudstone that forms decimetric thick beds; b – LF-B peloidal wackestone to packstone with birdeyes and laminated bindstone; c – LF-C
pisolitic-peloidal wackestone alternating with extensive sheet-cracks; d – detail of sheet cracks overlaid by oncoidal rudstone; e – photo-
micrograph of sheet cracks with isopachous radiaxal fibrous cement (rf) followed by blocky cement (b).
Fig. 4. Photomicrographs of the lithofacies associations. a – LF-A, oncoidal rudstone, dominated by Type 2 oncoids; b – LF-B, cryptal-
gal bindstone consisting of micritic laminae (black arrows) produced by microbial mat, fine grained laminated peloidal packstone to grain-
stone passing into peloidal wackestone and fenestral cavities (white arrow); c – LF-C, laminated crust, composed of radiaxial fibrous
cement and thin micritic laminae. Note the articulated ostracod concentration (black arrow); d – type 2 oncoids with Cayeuxia nuclei, and
isopachous fibrous cement around the oncoids; e – dissolution cavity with a fibrous cement rim and drusy mosaic cement in the central
portion; f – detail of the crust of fibrous cement consisting of two or more growth zones of cloudy fibrous crystals a few millimeters in
size (black arrow), growing perpendicularly to the substrate; g – detail of drusy mosaic cement; h – this drusy cement under cathodolu-
minescence is alternating bright and non-luminescent.
!
399
LOWER JURASSIC PERIDITAL CYCLES, CALCARE MASSICCIO Fm (CENTRAL APENNINES)
G
G
G
G
GEOL
EOL
EOL
EOL
EOLOGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPATHICA
THICA
THICA
THICA
THICA, 2015, 65, 5, 393—407
400
BRANDANO, CORDA, TOMASSETTI and TESTA
G
G
G
G
GEOL
EOL
EOL
EOL
EOLOGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPATHICA
THICA
THICA
THICA
THICA, 2015, 66, 5, 393—407
teristics. Shallow water, high energy conditions are also sup-
ported by the presence of oncoids that were able to overturn
and roll (cf. Védrine et al. 2007) as demonstrated by their
sub-spherical to elliptical shape.
LF-B peloidal wackestones to packstones alternating with
cryptalgal bindstone
This facies association comprises two sublithofacies: (i) pel-
oidal wackestones to packstones (LF-B1) alternating with
(ii) cryptalgal bindstone with birdseyes and fenestral fabrics
(LF-B2) (Figs. 3b and 4b). Geopetal structures and irregu-
larly shaped peloidal-micritic intraclasts, derived from un-
derlying lithologies, were also recognized.
Fenestrae are usually filled with drusy calcite; in some cases
large irregular stromatactoid voids filled with fine-grained
sediment are also recognizable. Peloids are up to 500 µm in
diameter and equal-sized and they are associated with small
benthic foraminifera lituolids and textulariids, small ostra-
cods, serpulids, gastropod fragments and Cayeuxia. Gastro-
pods and ostracods are often recrystallized and articulated
ostracods may be preserved in the center of cavities filled with
radial fibrous calcite.
Bindstones (LF-B2) are composed of stromatolitic layers,
planar algal laminae and trapped mud (Fig. 4b). Couplets of
micritic and clotted peloidal layers occur. This facies associa-
tion is characterized by Type 3 oncoids (sensu Védrine et al.
2007). These oncoids are between 0.5 mm and 3 cm in dia-
meter and show a sub-elliptical to lobate shape with wavy and
Fig. 5. a – dissolution cavity with fibrous cements, black arrows show leached grains, solution enlarged pores; b – isolated euhedral pla-
nar crystals of dolomite within the fine grained matrix interval of LF-B and LF-C facies associations.
Fig. 6. Sketch illustrating the diagenetic imprint after the deposition
of the sedimentary cycle of Calcare Massiccio. a – sheet cracks
formed during initial subaerial exposure are successively enlarged by
dissolution during prolonged subaerial exposure; b – the sea-level
fall results in the enlargement of the meteoric zone and the lowering
of the mixing zone producing dissolution cavities; c – sea-level rise
produced the space for the accumulation of the overlying sedimentary
cycle and precipitation of marine cement in the dissolution cavities.
!
401
LOWER JURASSIC PERIDITAL CYCLES, CALCARE MASSICCIO Fm (CENTRAL APENNINES)
G
G
G
G
GEOL
EOL
EOL
EOL
EOLOGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPATHICA
THICA
THICA
THICA
THICA, 2015, 65, 5, 393—407
irregular contours. The cortex comprises an alternation of or-
ganism-bearing and subordinate micritic laminae. Micritic
laminae are rarely continuous. The organism-bearing laminae
are predominant and comprise the microencrusting organisms
Bacinella irregularis (Radoičić, 1959) and Lithocodium
aggregatum (Elliott, 1956). Bacinella and Lithocodium are
commonly assumed to be cyanobacterial organisms character-
ized by an irregular microbial meshwork, alveoli and
interspaces filled with microsparry calcite (Schmid &
Leinfelder 1996; Duprax & Strasser 1999). Oncoid nuclei are
mainly bioclastic, made of echinoid or Cayeuxia fragments
and gastropods, but also include small peloids or aggregate
grains. Occasionally, small Type 2 oncoids with a Bacinella—
Lithocodium envelope occur.
Micritic layers in this facies may show partial dolomitiza-
tion with dolomite forming clear euhedral rhombs (Fig. 5b).
Interpretation:
This facies association is interpreted as the deposits of in-
tertidal and supratidal environments. A characteristic feature
of peritidal carbonates are millimeter-scale microbial lami-
nated sediments commonly associated with fenestral and
birdseye fabrics (Tucker & Wright 1990). Their preservation
is most common in the upper intertidal zone as they are fre-
quently disrupted by bioturbation in subtidal and lower inter-
tidal environments.
Type 3 oncoids indicate relatively low-energy conditions
characterized by Bacinella—Lithocodium. In fact, these micro-
encrusters dominate in low to very low energy settings
where the microbial meshwork had time to grow (cf. Védrine
et al. 2007).
LF-C pisolitic-peloidal wackestones with extensive sheet-
cracks
This facies association consists of barren mudstones to
wackestones, which are locally dolomitized. The only fauna
preserved are articulated ostracods (Fig. 4c). These deposits
are characterized by the presence of sheet-cracks and laminoid-
irregular fenestrae. The sheet-cracks can be laterally con-
tinuous on a decimeter to meter scale and are lined by an
isopachous rim followed by coarse blocky calcite (Fig. 3c,d,e).
Sheet-cracks consist of radiaxial fibrous calcitic cement with a
horizontal or undulating trend (Figs. 3d and 4c). The cracks
are up to 3 cm thick and occur individually or in stacked sets.
The sheet-cracks may be superimposed on the facies of
LF-A and LF-B. They are often associated with pisolitic
wackestones. Pisoids are centimeter-sized grains (up to 3 cm)
Cement
Mn (ppm)
Fe (ppm)
Sr (ppm)
Ba (ppm)
Mg (ppm)
δ
18
O ‰
δ
13
C ‰
Isopachous
fibrous
224 70
693 331 3023
–0.9
2.08
418 241 481 188 2927
–0.80
2.03
255 404 549
0 3074
–1.3
1.7
224
0
211
376
2244
464 0 33 232 2960
0 310 515
0 2432
85 0
515 277
2089
464 0 67 420 2698
Drusy
mosaic
224 326 0
0 2206
–1.32
1.17
0 0 0 0
2273
–1.87
1.11
139 0
169 0
1197
–1
1.01
0 139 279
0 2764
673 295.4 0
0 2106
Blocky
0
0
177
0
2404
–3.97
0.34
263 0
33.8 0
2529
–3.45
1.01
0 0 0 0
1400
–3.8
0.8
0 0 0 0
1616
Radiaxial
fibrous
464 0 67 420 2692
–2.21
2.25
0 178 0 1200 1357
–1.15
2.5
309 101 0 653 1993
–0.35
3.42
0 264 0 850 2495
–0.53
3.02
54 0
254 770
2931
–1.74
2.75
170 124 346 609 1000
–1.2
1.6
0
139
169
806
1411
–1.15
0.3
0 178 0 797 1009
–1.02
1
278 363 0 698 2479
–0.80
1.6
0 101 0 609 2395
–1.02
2.8
Dolomite
0 0 0 0
43600
0 0 0 0
110340
0 0 0 0
80000
0 0 0 0
103430
0 0 0 0
94000
0 0 0 0
125780
0 0 0 0
116000
0 0 0 0
108750
0 0 0 0
60050
Table 2: Summary of the geochemical and isotopic data of the recognized cements.
402
BRANDANO, CORDA, TOMASSETTI and TESTA
G
G
G
G
GEOL
EOL
EOL
EOL
EOLOGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPATHICA
THICA
THICA
THICA
THICA, 2015, 66, 5, 393—407
with a concentric laminated structure. Nuclei are mainly
small peloids and aggregate grains. Laminae are made of an
alternation of thin micritic laminae and calcitic microspar.
Some pisoids are fractured and fragmented. Peloidal bands
with oxidized iron staining and some root-related structures
also occur.
Some laminae are heavily disrupted by bioerosion traces.
Interpretation:
This facies association is interpreted as deposits from a
supratidal environment. The interpretation is based on the
abundance of laminar sheet cracks and features related to
subaerial diagenesis, such as vadose pisolites, diffuse red-
dish iron oxides testifying extended periods of exposure, and
partial dolomitization.
Diagenetic features
Four main types of calcitic cement were recognized in the
analysed rocks: 1) isopachous fibrous cement on oncoids
and bioclasts; 2) drusy mosaic cement infilling intergranular
pores and dissolution cavities; 3) crusts of radiaxial fibrous
cement constituting the sheet cracks; 4) blocky cement oc-
cluding large pores between the crusts of sheet cracks. The
diagenetic feature includes also the presence of dolomite that
occurs as matrix-dolomite.
The isopachous fibrous cement consists of closely packed
crystals (10
×70 µm) and occurs in interparticle and vuggy
pores (sensu Choquette & Pray 1970), and in dissolution
cavities (Figs. 4d, 5a). This cement is non-luminescent under
cathodoluminescence (CL), is non ferroan-to slighty ferroan,
with moderate Sr, Mn and Mg concentrations. Stable isotope
values of this cement are around —0.90 ‰ for
δ
18
O, and be-
tween + 2.80 ‰ and + 1.70 ‰ for
δ
13
C.
The drusy mosaic cement developed mainly in interpar-
ticle and vuggy pores, and subordinately in intraparticle
pores. It is characterized by a mosaic of polygonal, anhedral
crystals ranging in size between 50 µm and 250 µm
(Fig. 4e). Under CL, it comprises alternating bright and non-
luminescent bands (Fig. 4g,h), with moderate Fe, Mn and Sr
concentrations (Table 1). Stable isotope values are around
—1.00 ‰ for
δ
18
O and + 1.00 ‰ for
δ
13
C.
The crusts of radiaxial fibrous cement consist of two or
more growth zones of cloudy fibrous crystals 3—4 mm in
length, growing orthogonal to the substrate and showing
undulose extinction (Fig. 4f). This cement does not exhibit
luminescence under CL. It is non-ferroan and Mg concentra-
tions vary between 1300 and 2900 ppm. This cement is char-
acterized by a Ba content of up to 1200 ppm. Stable isotope
values range between —0.35 ‰ and —2.20 ‰ for
δ
18
O and
+ 0.30 ‰ and + 3.40 ‰ for
δ
13
C.
The blocky cement is found in large pores between crusts
of radiaxial fibrous cement in the sheet cracks. This cement
is characterized by subhedral to anhedral crystals ranging
from 0.2 to 1 mm in size. This cement is not luminescent un-
der CL and is non-ferroan with moderate Mg concentrations
(between 2100 and 2400 ppm). Stable isotope values range
from —3.45 ‰ to —4.00 ‰ for
δ
18
O and from + 0.34 ‰ to
+ 1.10 ‰ for
δ
13
C (Table 2).
Dolomite is represented by isolated euhedral planar crystals
or scattered patches within the fine grained matrix interval of
LF-B and LF-C facies associations (Fig. 5b). Crystals are me-
dium in size ranging between 50 and 120 µm. Dolomite oc-
curs within micritic layers 1—2 cm thick bounded by stylolites.
The analysis of major and trace elements indicate that dolo-
mite is characterized by an excess of Ca, while trace elements
are absent or present in very low concentrations (Table 2).
Interpretation:
The diagenetic features suggest that sheet cracks were
formed during the initial phase of subaerial exposure
(Fig. 6a—c), with cavities becoming infilled by sediments, and
were successively enlarged by dissolution during prolonged
subaerial exposure. The pisolitic wackestone facies, associ-
ated with the sheet cracks, are interpreted as a caliche product
(cf. Assereto & Kendal 1977; Mutti 1994). A further sea-level
fall resulted in the enlargement of the meteoric zone and the
lowering of the transition zone between the meteoric and ma-
rine water (the mixing zone). Aggressive meteoric and mixing
zone water then produced dissolution cavities in subtidal LF-A
facies (Fig. 6b). The following sea-level rise resulted in the pre-
cipitation of marine cements in dissolution cavities (Fig. 6c), in-
cluding crusts of radiaxial fibrous cement in the sheet cracks.
This cement is not luminescent, suggesting it precipitated in
oxygenating conditions and it is characterized by isotopic val-
ues consistent with Jurassic marine waters (Prokoph et al.
2008). The high concentration of Ba suggests the presence of
decaying organic matter probably related to the presence of
microbial mats (Table 2). Barite precipitates inorganically
directly from seawater in microenvironments containing de-
caying organic matter and other biogenic remains (Bishop
1988; Dehairs et al. 1990; Ganeshram & Francois 2002).
After the deposition of subtidal LF-A, isopachous fibrous
cement precipitated on oncoids and bioclasts. This cement is
not luminescent and has a geochemical character and isotopic
composition indicating precipitation from marine waters
(Table 2, Fig. 7a—d). The drusy mosaic cement infilling the
dissolution cavities and interparticle pores is alternating bright
and non-luminescent under cathodoluminescence (Fig. 4h). It
is non-ferroan, and has moderate Mn and Sr concentrations.
These characteristics indicate precipitation in fluctuating oxy-
genated to suboxygenated conditions typical of the deeper part
of the marine phreatic zone (Lohmann 1988; James & Coquette
1990). The blocky cement filling larger cavities, especially
within sheet cracks, has an isotopic composition and lumines-
cence consistent with precipitation under meteoric conditions.
Dolomite was only locally developed and occurs in asso-
ciation with muddy textures, stylolites and pressure solution
seams. There is no evidence of former evaporites, therefore it
is interpreted as a product of burial diagenesis. Burial dolo-
mites are widely documented in the Lower Jurassic carbon-
ates of the southern and northern Apennines (Ronchi et al.
2003; Iannace et al. 2011).
Sedimentary cycles
In this work, the term sedimentary cycle is used to identify
commonly repeated meter-scale succession of facies associa-
403
LOWER JURASSIC PERIDITAL CYCLES, CALCARE MASSICCIO Fm (CENTRAL APENNINES)
G
G
G
G
GEOL
EOL
EOL
EOL
EOLOGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPATHICA
THICA
THICA
THICA
THICA, 2015, 65, 5, 393—407
Fig. 7. Scatter diagrams of element compositions for the recognized cements. a – Mg vs. Ba, b – Sr vs. Ba, c – Mg vs. Sr, d – carbon
and oxygen isotopic composition.
tion (cf. Strasser et al. 1999; Bosence et al. 2009). The cycles
occur as bundles of the recognized facies associations and
are bounded by a discontinuity surface. This surface is over-
laid by subtidal facies of the following cycle. As observed by
Bosence et al. (2000), the cycle tops are not immediately rec-
ognizable as they do not weather out on natural rock surfaces
and their occurrence only becomes apparent from detailed
bed-by-bed logging. Once confidently identified, the cycle
tops may be followed for many hundreds of meters in the
open quarry and road cut.
On the basis of the facies association stacking pattern,
three types of sedimentary cycle were recognized: classic
shallowing-upward cycles (Type I), symmetrical cycles
(Type II), and shallowing upward cycles with non-
Waltherian facies shifts (Type III) (Fig. 2).
Type I consists of a sedimentary cycle produced by a re-
peated meter-scale shallowing upward succession (Fig. 8A).
The cycles are 0.5 to 2.5 m thick and either become finer or
coarsen upward. They start with an erosion surface overlain
by oncoidal floatstones to rudstones (LF-A). The basal ero-
sional surface shows an irregular morphology, evidence of
subaerial exposure, and a sharp contact with the overlying
LF-A facies that may contain reworked lithoclasts and
intraclasts from the underlying LF-C facies. The oncoidal
floatstone to rudstone passes gradationally up into peloidal
packstone alternating with cryptoalgal laminites (LF-B).
Some cycles may show lenticular oncoidal beds, up to 30 cm
thick laterally passing into peloidal packstone of LF-B. This
cycle is bounded by LF-C facies that are connected with a
period of subaerial exposure (Fig. 2). Rarely, the cycle is
capped by LF-B.
Type II is 3 m thick and shows a symmetrical trend in
terms of facies arrangement with peloidal packstone and
cryptoalgal laminites present both at the base and in the up-
per portion of the cycle, separated by oncoidal floatstones to
rudstones. Sheet-cracks associated with pisolitic-peloidal
wackestones (LF-C) characterize the top of the cycle.
Type III cycles are between 0.5 and 1 m thick (Fig. 8b).
These cycles show non-Waltherian facies shifts. An initial
erosion surface is overlain by oncoidal floatstones to
rudstones with skeletal fragments (LF-A), capped by desic-
cation cracks and pisolitic-peloidal wackestones (LF-C). In
404
BRANDANO, CORDA, TOMASSETTI and TESTA
G
G
G
G
GEOL
EOL
EOL
EOL
EOLOGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPATHICA
THICA
THICA
THICA
THICA, 2015, 66, 5, 393—407
Fig. 8. a – meter-scale shallowing upward sedimentary cycle type I showing the vertical evolution from the subtidal oncoidal floatstones
to rudstones facies (LF-A) to the supratidal peloidal packstone alternating with cryptoalgal laminites facies (LF-B) passing upward to the
pisolitic-peloidal wackestone facies associated with sheet-cracks (LF-C). The base and the top of the cycle are characterized by an erosional
surface. Dashed lines indicate the base and top of the cycle; b – Type III sedimentary cycle displaying basal erosion surface overlain by
oncoidal floatstones to rudstones (LF-A), capped by desiccation cracks and pisolitic-peloidal wackestones (LF-C) delimited by another ero-
sional surface corresponding to the top cycle.
this cycle the meteoric overprint is enhanced and penetrates
deeply into the underlying oncoidal facies, which show dis-
solution features suggesting prolonged exposure.
Spectral analysis
Six main peaks have been identified in the power spectra
of the investigated sections (Fig. 9): peak 1 at a frequency of
0.330995 (3.12 m), peak 2 at 0.380177 (1.8 m), peak 3 at
0.307043 (1.35 m), peak 4 at 0.158386 (0.97 m), peak 5 at
0.090113 (0.83 m) and peak 6 at 0.088033 (0.61 m). To in-
terpret the origin of the observed high-order cyclicity, cal-
culated ratios between peak frequencies were compared with
estimated ratios for Jurassic cycles reported by Berger et al.
Table 3: Comparison between a) the values estimated by Berger et al. (1989)
and b) the peak-frequency ratios calculated in this work.
(1989) (Table 3a). We followed the methodology of
D’argenio et al. (1997, 1999) to estimate the cycle
duration. This was calculated by comparing the
relative ratio sets for the cycle expressed in meters
(Table 3b), with the relative ratio sets of orbital pa-
rameters (Table 3a). The two ratio sets show a very
good linear correlation (r > 0.98), suggesting that
the Calcare Massiccio cycles of the investigated
section had a hierarchical organization controlled
by Earth’s orbital perturbation.
The most prominent peaks (1.8 m and 1.35 m)
are consistent with obliquity cycles, the 3.12 m
peak approximates to a short eccentricity cycle
(period of 95 ka), and the small peaks (0.83 m and
0.61 m) approximate to the two precession cycles
(21.5 ka and 18 ka, respectively). Peak 4 (0.97 m)
is not consistent with orbital cycles.
Discussion
Type I cycles correspond to the classic peritidal cycle char-
acterized by a shallowing upward evolution and match the
α cycle of Bosence et al. (2009). This cycle is the most com-
mon in the investigated section and it represents the product of
regression and infilling of accommodation space. Lithofacies
changes in peritidal carbonates may be caused by relative sea-
level changes, but also by sediment supply, increased wave
erosion or development of bedforms reducing tidal exchange
(Tucker & Wright 1990). Consequently, Type I cycles may re-
sult both from autocyclic and allocyclic processes.
Type II cycles show a symmetrical facies arrangement with
an intertidal facies association at the base and top separated by
404220
95000
47000
37000
21500
18000
a
404220 1
4.254947 8.600426 10.92486 18.80093 22.45667
95000
0.235021 1 2.021277 2.567568 4.418605 5.277778
47000
0.116273 0.494737 1
1.27027
2.186047 2.611111
37000
0.091534 0.389474 0.787234 1
1.72093
2.055555
21500
0.053188 0.226315 0.457446 0.581081 1
1.194444
18000
0.04453
0.189473 0.382978 0.486486 0.837209 1
b
3.12
1.80
1.35
0.97
0.83
0.61
3.12 1 1.733333 2.311111 3.216495 3.759036 5.114754
1.80 0.576923 1 1.333333 1.85567
2.168675 2.95082
1.35 0.432692 0.75
1
1.391753 1.626506 2.213115
0.97 0.310897 0.538889 0.718519 1
1.168675 1.590164
0.83 0.266026 0.461111 0.614815 0.85567
1
1.360656
0.61 0.195513 0.338888 0.451852 0.628866 0.73494
1
405
LOWER JURASSIC PERIDITAL CYCLES, CALCARE MASSICCIO Fm (CENTRAL APENNINES)
G
G
G
G
GEOL
EOL
EOL
EOL
EOLOGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPATHICA
THICA
THICA
THICA
THICA, 2015, 65, 5, 393—407
a subtidal facies association. This cycle corre-
sponds to the
γ cycle of Bosence et al. (2009) and
records a gradual transgressive phase followed by
regression. This cycle could also result from either
autocyclic or allocyclic processes.
The facies arrangement of Type III cycles
shows subtidal facies directly overlain by supra-
tidal facies. Consequently, this cycle records a
marked sea-level fall resulting in subaerial expo-
sure of subtidal facies. In this case, the cycle
forms as a result of relative sea-level fall that
may be caused by allocyclic processes such as
eustasy or tectonic uplift.
Spectral analysis is considered an objective
method for the detection of regular cyclicity in
data recording oscillating parameters (Weedon
1989). In this case the sedimentary record is rep-
resented by a repetitive meter-scale succession of
facies associations. In this study, spectral analy-
sis suggests that the observed cyclic pattern of
the Calcare Massiccio was controlled predomi-
paleoseismites were documented, which would have provided
evidence for an active tectonic control during deposition.
Based on spectral analysis results, we conclude that the
signal recorded in the studied succession points toward an
orbital forcing control on deposition of the Calcare Massicio
Formation.
High frequency sea-level fluctuations also controlled dia-
genetic processes in the Calcare Massiccio. Sea-level varia-
tions, by inducing changes in the water table, play a key role
in exposing the peritidal cycles to the marine, mixed marine/
meteoric and vadose meteoric zones (Fig. 6a,b,c). As a con-
sequence, they are responsible for the cyclical dissolution in
the vadose and mixing zone and the following precipitation
of cements (cf. Mutti 1994).
Conclusion
The present paper illustrates an integrated workflow for
the characterization of the Calcare Massiccio shallow-water
carbonates coupling facies analysis, cyclostratigraphy and
petrography.
The study highlights that the Calcare Massiccio, which de-
veloped on the structural high within the Sabina basin do-
main, is organized into meter-scale shallowing upward
cycles bounded by subaerial exposure surfaces. The most
frequent cycles show vertical evolution from a subtidal fa-
cies association (oncoid dominated) to a supratidal facies as-
sociation with well-developed sheet cracks.
Spectral analysis reveals prominent peaks consistent with
obliquity cycles and short eccentricity cycles, while small
peaks approximate to the two procession cycles. Nevertheless,
one of the recorded peaks is not consistent with any orbital
cyclicity.
We conclude that, in the Calcare Massiccio, a tectonic
control on sedimentary cycle development cannot be disre-
garded, but the signal recorded by the sedimentary succes-
sion points toward a significant control by orbital forcing.
Fig. 9. Blackman-Tukey power spectrum estimation from the investigated sec-
tion of Calcare Massiccio. The power spectrum indicates how much of the sig-
nal is at the recognized frequencies. The peaks show the periodicities (p = 1/f,
f = frequency) recognized in the studied section.
nantly by orbital forcing. The vertical staking pattern of sedi-
mentary cycles indicates a cyclical variation in cycle thick-
ness along the section (Fig. 2). Elementary cycles are related
to either the Earth’s precession or obliquity signal (or a com-
bination of both). The elementary cycles are hierarchically
organized into bundles (seven groups of 1—4 elementary
cycles) and the bundles into superbundles (two groups of 4
bundles), which correspond to short ( ~ 100 ka) and long
( ~ 400 ka) eccentricity signals, respectively. Consequently,
the investigated portion of the Calcare Massiccio shows an
accumulation rate of 1 m/30 ka, which is in agreement with
the values recorded for the Tethyan Liassic carbonate plat-
forms (see fig. 2 from Bosence et al. 2009).
The vertical variation of elementary cycle thickness sug-
gests that the orbital cycles are superimposed on long-term
transgressive—regressive facies trends. A transgressive facies
trend is singled out on the basis of an upward increase in
thickness of elementary cycles, while a regressive trend is
marked by a decrease of elementary cycle thickness and an
increase in restricted lagoonal deposits (LF-C and LF-B).
The carbonate cycle of the Lower Jurassic shallow-water
platform in the High Atlas of Morocco has similarly been in-
terpreted as been related to sea-level changes driven by or-
bital forcing (Crevello 1990, 1991).
However, the influence of autocyclic controls cannot be
totally excluded because the investigated facies were depos-
ited in a sedimentary environment, the tidal flat, where
autocyclic processes are documented. Furthermore, auto-
cyclic strata may be stacked as apparently allocyclic strata
(Burgess 2006). The spectral analysis records one periodicity
not consistent with orbital parameters, which may have been
produced by autocyclic processes (Fig. 9).
Bosence et al. (2009) suggested a pulsed tectonic control for
the creation and filling of accommodation space of some of
the Calcare Massiccio peritidal cycles. However, fault activity
is unlikely to be the major control on cycle repetition on ex-
tensive carbonate platforms (Tucker & Wright 1990). In this
study, and in general in the Calcare Massiccio Formation, no
406
BRANDANO, CORDA, TOMASSETTI and TESTA
G
G
G
G
GEOL
EOL
EOL
EOL
EOLOGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPATHICA
THICA
THICA
THICA
THICA, 2015, 66, 5, 393—407
The diagenetic characteristics of Calcare Massiccio are
linked to high frequency sea-level fluctuations, which pro-
duced dissolution during sea-level fall and cement precipita-
tion during following sea-level rise as illustrated by marine
cements precipitated inside sheet cracks developed on top of
the cycles.
Acknowledgments: Financial support from MIUR (PRIN
2010-11 Research Grant 20107ESMX9_001 and Sapienza
Ateneo Project 2014) are gratefully acknowledged. Criticism
and comments by František Vaček and an anonymous re-
viewer greatly improved the manuscript. Comments by Editor
Jindřich Hladil are much appreciated. The authors would like
to thank Flavio Jadoul for the cathodoluminescence analysis.
Discussions in the field with Alessandro Lanfranchi were very
useful. Mariano Parente is thanked for assistance with the
Strontium Stratigraphy. Useful discussions with Dan Bosence,
Fotini Pomoni-Papaioannou, Sabrina Amodio and Julien
Michel are much appreciated. Marcello Serracino is thanked
for the assistance with EDS-WDS analyses. We thank James
Hodson (RPS Energy) for comments and English review.
References
Assereto R.L.A.M. & Kendall St.C. 1977: Nature, origin and classi-
fication of peritidal tepee structures and related breccias. Sedi-
mentology 24, 153—210.
Barattolo F. & Bigozzi A. 1996: Dasycladaleans and depositional en-
vironments of the Upper Triassic—Liassic carbonate platform of
the Gran Sasso (Central Apennines, Italy). Facies 35, 163—208.
Berger A.F., Loutre M.F. & Dehant V. 1989: Influence of the chang-
ing lunar orbit on the astronomical frequencies of the Pre-Qua-
ternary insolation patterns. Paleoceanography 4, 555—564.
Bigozzi A. 1990: Cyclic stratigraphy of the Upper Triassic—Lower
Liassic sequence of Corno Grande (Central Apennines). Mém.
Soc. Geol. Ital. 45, 709—721.
Billi A., Valle A., Brilli M., Faccenna C. & Funiciello R. 2007:
Fracture-controlled fluid circulation and dissolutional weather-
ing in sinkhole-prone carbonate rocks from central Italy. J.
Struct. Geol. 29, 385-395.
Bishop J.K.B. 1988: The barite—opal—organic carbon association in
oceanic particulate matter. Nature 331, 341—343.
Blackman R.B. & Tuckey S.W. 1958: The measurement of power
spectra. Dover Publications, New York, 1—190.
Bosence D.W.J., Wood J., Rose E.P.F. & Qing H. 2000: Low and
high frequency sea-level changes control peritidal carbonate cy-
cles, facies and dolomitization in the Rock of Gibraltar (Early
Jurassic, Iberian Peninsula). J. Geol. Soc. London 157, 61—74.
Bosence D., Procter E., Aurell M., Kahla A.B., Marcelle B.F.,
Casaglia F., Cirilli S., Mehdie M., Nieto L., Rey J., Scherreiks
R., Soussi M. & Waltham D. 2009: A dominant tectonic signal
in high-frequency, peritidal carbonate cycles? A regional anal-
ysis of liassic platforms from western Tethys. J. Sed. Res. 79,
389—415.
Burgess P.M. 2001: Modelling carbonate sequence development
without relative sealevel oscillations. Geology 29, 1127—1130.
Burgess P.M. 2006: The signal and the noise: forward modelling of
allocyclic and autocyclic processes influencing peritidal car-
bonate stacking patterns. J. Sed. Res. 76, 962—977.
Carminati E. & Doglioni C. 2005: Mediterranean tectonics. In: Selley
R., Cocks R. & Plimer I. (Eds): Encyclopedia of Geology.
Elsevier, 135—146.
Carminati E., Lustrino M., Cuffaro M. & Doglioni C. 2010: Tecton-
ics, magmatism and geodynamics of Italy: What we know and
what we imagine. J. Virtual Explorer 36, 9, 1—64.
Carminati E., Corda L., Mariotti G., Scifoni A. & Trippetta F. 2013:
Mesozoic syn- and postrifting evolution of the Central Apen-
nines, Italy: The role of Triassic evaporates. J. Geology 121, 4,
327—354.
Carozzi A.V. 1957: Contribution a l’étude des propriétés
géométriques des oolithes. L’exemple du Grand Lac Salé,
Utah, USA. Bull. Inst. Natl. Genevois 58, 3—52.
Centamore E., Chiocchini G., Deiana A., Micarelli U. & Pieruccini
M. 1971: Contribution to the knowledge of the Jurassic of the
Umbria-Marche Apeninnes. [Contributo alla conoscenza del
Giurassico dell’Appennino umbro-marchigiano.] Studi Geol.
Camerti 1, 7—89 (in Italian).
Choquette P.W. & Pray L.C. 1970: Geologic nomenclature and
classification of porosity in sedimentary carbonates. AAPG
Bull. 54, 207—250.
Colacicchi R., Passeri L. & Pialli G. 1975: Evidences of tidal envi-
ronment deposition in the Calcare Massiccio Formation (Central
Apennines-Lower Lias). In: Ginsburg R. (Ed.): Tidal deposits, a
casebook of recent examples and fossil counterparts. Section IV.
Springer-Verlag, Berlin, 345—353.
Cosentino D., Cipollari P. & Pasquali V. 2004: The Jurassic pelagic
carbonate platform of the Cornicolani Mts. (Latium, central Italy).
In: Pasquarè G. & Venturini C. (Eds.): Mapping geology of Italy.
APAT-SELCA, IGC, Florence, 177—184.
Crevello P. 1990: Stratigraphic evolution of Lower Jurassic carbon-
ate platforms: record of rift tectonics and eustasy, central and
eastern High Atlas, Morocco. Ph.D. Dissertation, Colorado
School of Mines, Golden, Colorado, 1—456.
Crevello P. 1991: High frequency carbonate cycles and stacking pat-
terns: interplay of orbital forcing and subsidence on Lower Ju-
rassic rift platforms, High Atlas, Morocco. In: Franseen E.K.,
Watney W.L., Kendall C.G.St.C. & Ross W. (Eds.): Sedimen-
tary modelling: computer simulations and methods for improved
parameter definition. Kansas Geol. Surv., Bull. 223, 207—230.
D’Argenio B., Ferreri V. & Amodio S. 2011: Eustatic cycles and
tectonics in the Cretaceous shallow Tethys, Central-Southern
Apennines. Ital. J. Geosci. 130, 119—127.
D’Argenio B., Ferreri V., Amodio S. & Pelosi N. 1997: Hierarchy
of high-frequency orbital cycles in Cretaceous carbonate plat-
form strata. Sed. Geol. 113, 169—193.
D’Argenio B., Ferreri V., Raspini A., Amodio S. & Buonocunto
F.P. 1999: Cyclostratigraphy of a carbonate platform as a tool
for high-precision correlation. Tectonophysics 315, 357—384.
Damiani A.V., Chiocchini M. Colacicchi R., Mariotti G., Parotto M.,
Passeri L. & Praturlon A. 1992: Lithostratigraphic elements for
a summary of the Meso-Cenozoic carbonate facies of the Central
Apeninnes. [Elementi litostratigrafici per una sintesi delle facies
carbonatiche meso-cenozoiche dell’Appennino centrale.] In:
Tozzi M., Cavinato G.P. & Parotto M. (Eds.): Preliminary stud-
ies on the acquisition data for the CROP11 Civitavecchia-Vasto
profile. [Studi preliminari all’acquisizione dati del profilo
CROP 11 Civitavecchia—Vasto.] Studi Geol. Camerti, vol. spec.
1991/2, 187—213 (in Italian).
Dehairs F., Goeyens L., Stroobants N., Bernard P., Goyet C., Pois-
son A. & Chesselet R. 1990: On the suspended barite and the
oxygen minimum in the Southern Ocean. Global Biogeochemi-
cal Cycles 4, 85—102.
Doglioni C. 1991: A proposal of kinematic modelling for W-dip-
ping subductions – possible applications to the Tyrrhenian—
Apennines system. Terra Nova 3, 423—434.
Dunham R.J. 1962: Classification of carbonate rocks according to
depositional texture. In: Ham W.E. (Ed.): Classification of car-
bonate rocks. Amer. Assoc. Petrol. Geol. Mem. 1, 108—121.
407
LOWER JURASSIC PERIDITAL CYCLES, CALCARE MASSICCIO Fm (CENTRAL APENNINES)
G
G
G
G
GEOL
EOL
EOL
EOL
EOLOGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPATHICA
THICA
THICA
THICA
THICA, 2015, 65, 5, 393—407
Dupraz C. & Strasser A. 1999: Microbialites and micro-encrusters
in shallow coral bioherms (Middle to Late Oxfordian, Swiss
Jura Mountains). Facies 40, 101—130.
Elliott G.F. 1956: Further records of fossil calcareous algae from
the Middle East. Micropaleontology 2, 327—334.
Embry A.F. & Klovan J.E. 1971: A Late Devonian reef tract on
northeastern Banks Island, Norhwest Territories. Canad.
Petrol. Geol. Bull. 19, 730—781.
Galluzzo F. & Santantonio M. 2002: The Sabina Plateau: a new ele-
ment in the Mesozoic palaeogeography of Central Apennines.
Boll. Soc. Geol. Ital. 1, 561—588.
Ganeshram R. & Francois R. 2002: New insights into the mechanism
of barite formation in seawater and implications for paleo-
productivity reconstruction. EOS Trans. Amer. Geophys. Union
83, Ocean Science Meeting Supplement, Abstract OS21L-11.
Ginsburg R.N. 1971: Landward movement of carbonate mud – new
model for regressive cycles in carbonates. Amer. Assoc. Petrol.
Geol. Bull. 55, 340.
Gueguen E., Doglioni C. & Fernandez M. 1998: On the post-25 Ma
geodynamic evolution of the Western Mediterranean. Tectono-
physics 298, 259—269.
Hardie L.A. 1986: Stratigraphic models for carbonate tidal flat dep-
osition. In: Hardie L.A. & Shinn E.A. (Eds.): Carbonate depo-
sitional environments, modern and ancient. Part 3. Tidal flats.
Colorado School of Mines, Quarterly 81, 59—73.
Iannace A., Capuano M. & Galluccio L. 2011: “Dolomites and dolo-
mites” in Mesozoic platform carbonates of the Southern Apen-
nines: geometric distribution, petrography and geochemistry.
Palaeogeogr. Palaeoclimatol. Palaeoecol. 310, 324—339.
James N.P. & Coquette P. 1990: Limestones – the meteoric diage-
netic environment. In: McIlreath I.A. & Morrow D.A. (Eds.):
Diagenesis. Geoscience Canada Reprint Series 4, 35—73.
Lohmann K.C. 1988: Geochemical patterns of meteoric diagenetic
systems and their application to studies of paleokarst. In:
James N.P. & Choquette P.W. (Eds.): Paleokarst. Springer—
Verlag, New York, 58—80.
Lukasik J. & Simo J.A. (Toni) 2008: Controls on development of
Phanerozoic carbonate platforms and reefs – introduction and
synthesis. In: Lukasik J. & Simo J.A. (Toni) (Eds): Controls
on carbonate platform and reef development. SEPM Spec. Publ.
89, 5—12.
Mutti M. 1994: Association of tepees and paleokarst in the Ladinian
Calcare Rosso (Southern Alps, Italy). Sedimentology 41, 621—641.
Paillard D., Labeyrie L. & Yiou P. 1996: Macintosh program per-
forms time-series analysis. EOS Trans. Amer. Geophys. Union
77, 379.
Passeri L. & Venturi F. 2005: Timing and causes of drowning of the
Calcare Massiccio platform in Northern Apennines. Boll. Soc.
Geol. Ital. 124, 1, 247—258.
Pialli G. 1971: Co-tidal flat facies in the Calcare Massiccio of the
Umbria-Marche Apeninnes. [Facies di piana cotidale nel Cal-
care Massiccio dell’Appennino Umbro-Marchigiano.] Boll.
Soc. Geol. Ital. 90, 481—507 (in Italian).
Pomoni-Papaioannou F. & Kostopoulou V. 2008: Microfacies and
cycle stacking pattern in Liassic peritidal carbonate platform
strata, Gavrovo-Tripolitza platform, Peloponnesus, Greece.
Facies 54, 417—431.
Pratt B.R., James N.P. & Cowan C.A. 1992: Peritidal carbonates.
In: Walker R.G. & James N.P. (Eds.): Facies models: Re-
sponse to sea level change. Geol. Assoc. Canada, 303—322.
Prokoph A., Shields G.A. & Veizer J. 2008: Compilation and time-
series analysis of a marine carbonate
δ
18
O,
δ
13
C,
87
Sr/
86
Sr and
δ
34
S database through Earth history. Earth Sci. Rev. 87, 113—133.
Radoičić R. 1959: Some problematic microfossils from the Dinarian
Cretaceous. Bull. Serv. Géol. Géophys. RP Serbie 17, 87—92.
Ronchi P., Casaglia F. & Ceriani A. 2003: The multiphase dolomiti-
zation of the Liassic Calcare Massiccio and Corniola succes-
sion (Montagna dei Fiori, Northern Apennines, Italy). Boll. Soc.
Geol. Ital. 122, 157—172.
Santantonio M. 1993: Facies associations and evolution of pelagic
carbonate platform/basin systems: examples from the Italian
Jurassic. Sedimentology 40, 1039—1067.
Schmid D.U. & Leinfelder R.R. 1996: The Jurassic Lithocodium
aggregatum—Troglotella incrustans foraminiferal consortium.
Palaeontology 39, 21—52.
Schwarzacher W. 1993: Cyclostratigraphy and the Milankovitch
Theory. Developments in Sedimentology 52, Elsevier, Amster-
dam, 1—225.
Strasser A. 1994: Milankovitch cyclicity and high-resolution se-
quence stratigraphy in lagoonal-peritidal carbonates (Upper
Tithonian—Lower Berriasian, French Jura Mountains). In: De
Boer P.L. & Smith D.G. (Eds): Orbital forcing and cyclic se-
quences. IAS Spec. Publ. 19, John Wiley & Sons, 285—301.
Strasser A. & Védrine S. 2009: Controls on facies mosaics of car-
bonate platforms: a case study from the Oxfordian of the Swiss
Jura. In: Swart P.K., Eberli G.P. & McKenzie J.A. (Eds.): Per-
spectives in carbonate geology. IAS Spec. Publ. 41, Wiley—
Blackwell, 199—213.
Strasser A., Hilgen F.J. & Heckel P.H. 2006: Cyclostratigraphy –
Concepts, definitions, and applications. Newslett. Stratigr. 42,
75—114.
Strasser A., Pittet B., Hillgärtner H. & Pasquier J.B. 1999: Deposi-
tional sequences in shallow carbonate-dominated sedimentary
systems: Concepts for a high-resolution analysis. Sed. Geol.
128, 201—221.
Tucker M.E. & Wright V.P. 1990: Carbonate sedimentology. Black-
well Scientific Publications, Oxford, 1—482.
Védrine S., Strasser A. & Hug W. 2007: Oncoid growth and distri-
bution controlled by sea-level fluctuations and climate (Late
Oxfordian, Swiss Jura Mountains). Facies 53, 535—552.
Weedon G. 1989: The detection and illustration of regular sedimen-
tary cycles using Walsh power sectra and filtering, with sam-
ples from the Lias of Switzerland. J. Geol. Soc. 146, 133—144.
Weedon G. 2003: Time-series analysis and cyclostratigraphy. Exam-
ining stratigraphic record of environmental cycles. Cambridge
University Press, New York, 1—259.
Wright V.P. & Burgess P.M. 2005: The carbonate factory continuum,
facies mosaics and microfacies: an appraisal of some of the
key concepts underpinning carbonate sedimentology. Facies
51, 17—23.