Mesozoic tectono-sedimentary evolution of Rocca Busambra in western Sicily

Page 1

Facies (2009) 55:115–135

DOI 10.1007/s10347-008-0156-2

ORIGINAL ARTICLE

Mesozoic tectono-sedimentary evolution of Rocca Busambra in western Sicily

Luca Basilone

Received: 10 January 2008 / Accepted: 26 June 2008 / Published online: 25 July 2008© Springer-Verlag 2008

Abstract The Rocca Busambra ridge in western Sicily isa shallow to pelagic Meso-Cenozoic carbonate structuralunit of the Sicilian Chain with a variety of tectono-sedi-mentary features. Palaeofaults, unconformities (buttressunconformity, onlap, downlap), a network of neptuniandykes with several inWlling generations, several large hia-tuses, diVerent facies and lateral facies changes, and ero-sional submarine and subaerial surfaces are observed.Detailed Weldwork and structural analyses have indicatedthe occurrence of fault planes with diVerent orientations.These data, combined with facies studies and physical-stra-tigraphy analyses, allow for the distinction of diVerentdepositional regions. A lateral change from an open-marinecarbonate platform with a stepped fault margin (located inthe westernmost sector) to a deeper basinal depositionalsetting in the east, in the context of an upper slope scal-loped margin and base-of-slope systems with talus breccias,is envisaged here. Extensional to transtensional tectonicpulses punctuated the sedimentary evolution during EarlyToarcian, Late Jurassic, Early Cretaceous, Late Cretaceous,and Early Miocene times. The collected data show thatmost fault planes have preserved their original orientationsthroughout the reactivation processes. The reconstructedMeso-Cenozoic tectono-sedimentary evolution is closelyrelated to the late syn-rift and post-rift tectonic evolution ofthe Tethyan continental margin.

Keywords Synsedimentary tectonics · Buttress unconformity · Pelagic carbonate platform and plateau facies associations · Structural setting · Western Sicily

Introduction

Carbonate rocks deposited along rifted continental marginsdisplay a wide variety of sedimentary facies and geometri-cal relationships. The submarine topographical highscapped by a thin condensed pelagic sequence, resultingfrom the Early Jurassic break-up of the original carbonateplatforms (Jenkyns 1970a), were deWned as “Pelagic Car-bonate Platforms” (Catalano et al. 1977; Catalano andD’Argenio 1978). This concept has been further developedby Santantonio (1993, 1994), who Wrst proposed deposi-tional facies and tectonic models. Alternatively, the termplateau is preferred by some authors (among them Jenkyns1971, 1980) to deWne a drowned platform that accumulatespelagic deposits.

Tectonic control of the pelagic sedimentation is largelyconsistent with the well-known syn-rift and initial post-riftphases that aVected the Tethyan continental margins duringthe Jurassic period, which is well documented by the clas-sic papers of Wendt (1969, 1971), Jenkyns (1970a, 1971),Bernoulli and Jenkyns (1974), Castellarin et al. (1978),Catalano and D’Argenio (1978, 1982a, b), Eberli (1988),and Alvarez (1990). Most of these authors based their ideason surveys of Triassic and Jurassic rocks of the SouthernAlps, Apennines, and western Sicily.

The Jurassic–Cretaceous pelagic carbonate platformrock successions, pertaining to the Trapanese domain (Cat-alano and D’Argenio 1978, 1982a), which are widely out-cropping in central-western Sicily (Fig. 1a), have beenstudied by (Wendt (1963, 1965, 1969, 1971), Jenkyns

L. Basilone (&)Dipartimento di Geologia e Geodesia, Palermo University, via ArchiraW 20-22, 90123 Palermo, Italye-mail: [email protected]

123

Page 2

116 Facies (2009) 55:115–135

(1970b, 1971), Di Stefano and Mindszenty (2000), Di Stef-ano et al. (2002a, b), Martire et al. (2000, 2002), Martireand Bertok (2002), and Santantonio (2002).

Most of these authors suggested Jurassic evolution of theperitidal carbonate platform to a basin-swell system con-nected by escarpments.

The Rocca Busambra is part of the Meso-Cenozoic shal-low marine and pelagic carbonate platform system and per-tains to the Trapanese palaeogeographic domain (Fig. 1a).Condensed sedimentation and great facies variability of theJurassic–Cretaceous deposits are the most signiWcant fea-tures of this area (Christ 1958, 1960; Tamajo 1960; Wendt1963, 1965, 1969; Catalano and D’Argenio 1982a; Ceccaand Pochettino 2000; Martire et al. 1998 in Agate et al.1998a; Basilone 2007).

Some tectono-sedimentary features of the Jurassic–Cre-taceous succession have been previously illustrated by vari-ous authors in the westernmost sector (Piano Pilato region)of the Rocca Busambra ridge (Wendt 1971; Giunta andLiguori 1975; Mascle 1973, 1979; Gullo and Vitale 1986;Longhitano et al. 1995; Martire et al. 2002; Martire andBertok 2002; Bertok and Martire 2004).

Wendt (1971) Wrst recognized some synsedimentary tec-tonic features (e.g., neptunian dykes and normal palaeo-faults) in the westernmost side of Rocca Busambra (RoccaArgenteria and Pizzo Nicolosi) and assigned them to pre-Early Toarcian time.

Bertok and Martire (2004) brieXy summarized the his-tory of changes in the palaeotopography and the palaeotec-tonic signiWcance of the Jurassic pelagites deposited on thetop and the Xanks of the pelagic carbonate platform. Mar-tire et al. (2002) invoked normal faults and gravitationalsliding (sensu Winterer et al. 1991 and Winterer and Sarti1994) to explain the angular unconformity between RossoAmmonitico and peritidal limestones.

Di Stefano et al. (2002a, b) described, in the adjacentMonte Kumeta ridge, (located 20 km to the northwest,

Fig. 1a) vertical and lateral relationships of the recognizedlithofacies and Wrst suggested a “platform escarpment” sys-tem where the pelagic lithofacies deposited on a steppedsurface, displaced by repeatedly reactivated basinward-dip-ping normal faults.

Main aim

Of the several Mesozoic pelagic carbonate platform succes-sions in western Sicily, the Rocca Busambra section is oneof the best representatives of Mesozoic continental marginsedimentation and tectonics. Despite the complex structuralsetting of the Rocca Busambra ridge (Mascle 1979; Catalanoet al. 1998, 2004), its Meso-Cenozoic succession appearsmost suitable to depict major tectono-sedimentary events.

The main aim of the present paper is to illustrate, withthe use of a detailed geological map, stratigraphic and tec-tonic features of the Triassic–Miocene carbonate succes-sion along the entire Rocca Busambra ridge and to relatefacies geometry to tectonic features that were active duringthe Meso-Cenozoic.

Geological framework

The Sicily Chain, part of the Maghrebian–Apennine system(Fig. 1b), resulted from the piling-up of tectonic unitsderived from the deformation of some original palaeogeo-graphic domains that developed during the Meso-Cenozoicinterval in the Sicilian sector of the African continentalmargin. Their tectonic emplacement took place during theMiocene–Early Pleistocene time interval. It is commonlyassumed that there was a S–SE thrust propagation (Cata-lano and D’Argenio 1978; Catalano et al. 2000) accompa-nied by clockwise rotations (Channel et al. 1990; Oldowet al. 1990) and strike-slip (or transpressive) movements(Ghisetti and Vezzani 1984; Oldow et al. 1990).

Fig. 1 a Distribution of the Jurassic–Cretaceous Trapanese pelagic carbonate platform rock successions in central-western Sicily. b Tectonic map of the central Mediterranean (modiWed from Catalano et al. 2000). 1 Corsica-Sardinia; 2 Calabro-Kabilian Arc, “internal” Flysch sequences, ophiolites; 3 Mag-hrebian–Sicilian-South Apen-nine Chain and deformed foreland; 4 undeformed foreland (Tunisia, Hyblaean Plateau, Apulia); 5 Areas with extension; 6 Plio-Quaternary volcanism

5 19°41°

34

1 2 3 4 5 6

0 100 km

Algeria

n

basin

Ionianbasin

HybleanPlatform

South

ern

Apennines

Malta

escarp

ment

Tunisia

Tyrrhenianbasin

Tectonic map of theCentral Mediterranean area

PelagianBlock

Sardo

-Bale

aric

basin

ApuliaPlatform

Rocca Busambra

Sicily

R. Busambra

M. Kumeta

N

Palermo

Maranfusa

Galiello

Corleone

Tyrrhenian sea10 km

a

b

123

Page 3

Facies (2009) 55:115–135 117

The chain sector of the study area (Fig. 2a), locatedimmediately north-east of the town of Corleone (central-western Sicily), is characterized by: (a) imbricated slices ofa pelagic carbonate platform (Trapanese tectonic units); (b)a wedge of basinal carbonate thrust sheets (Sicanian units)and (c) the Numidian Flysch nappe. In this tectonic frame,the Rocca Busambra tectonic unit extends about 15 kmwith an E–W-trending large antiform that is slightly rotatedto the NW–SE on its eastern side (Pizzo Marabito). Thestructure is bounded by two E–W major reverse faults, withcommon right-handed strike-slip movements, and appearsto have been pushed up to the surface (Fig. 2b). It tectoni-cally overlies the basinal Sicanian tectonic units (the MountBarracù unit and its subsurface continuation, Agate et al.1998b; Catalano et al. 2000).

Areas of study

In this paper, we deal with the entire Rocca Busambraridge, whose tectonic and sedimentary features have beendeeply investigated. Detailed Weldwork supported by large-scale mapping and facies analysis highlighted widespreadhigh facies variability among the Jurassic–Miocene depos-its and mapped the occurrence of synsedimentary faulting(Fig. 3a).

In order to investigate the lateral facies variations overthe entire exposed sequence, several sections were mea-sured along the Rocca Busambra carbonate ridge and,where possible, sampling was undertaken bed by bed. Thepresent study is based on 12 stratigraphic and 8 tectonicsections (Figs. 4, 5).

The lateral discontinuity of the stratal units requires veryhigh precision in the recognition of geometrical relation-ships. Physical-stratigraphic analyses were applied alongseveral measured and sampled sections. Sedimentological

analyses were used to deWne the microfacies. Lithofacieswere calibrated by biostratigraphic data, mostly based ondetailed Jurassic ammonite biozonation (Gemmellaro1872–1882; Gugenberg 1936; Wendt 1963, 1969), calpio-nellid biozonation (Alleman et al. 1971), and Cretaceous–Miocene calcareous plankton biostratigraphy (Caron 1985;Iaccarino 1985; Perch-Nielsen 1985; Fornaciari et al. 1996;Foresi et al. 2002; Sprovieri et al. 1996, 2002).

Fig. 3 a Structural map of the Rocca Busambra ridge, displaying diVerent trending faults and their age. b Inserted map with the location of thefour regions distinguished

R. ArgenteriaPizzo Nicolosi

Late Jurassic faults

Early Toarcian neptunian dykes

Late Cretaceous faultsEarly Miocene faults

Late Cenozoic faults

Sicanian tectonic unit

Rocca Busambra tectonic unit

Rocca Busambra

C.zo Meriggio

Rocca RamusaPiano Pilato region

Pirrello region

Rocca Busambra-peak region

0 2km

Piano della Tramontana

ba

Pizzo Marabito

0 1 km

Pizzo Marabito region

Fig. 2 a Structural map of the studied region. b NNE–SSW geoseis-mic section, showing the relationships between the Trapanese, the Sic-anian, and the Numidian Flysch tectonic units (modiWed from Agateet al. 1998a)

Rocca Busambra

high angle reverse faults

strike-slipfaults

normalfaults

geological section thrusts folds

0 2 kmalluvial deposits

Terravecchia Fm.

Castellana Sicula Fm.

SICILIDI UNITS

NUMIDIAN FLYSCH UNITS

ROCCA BUSAMBRA TRAPANESE UNIT

SICANIAN UNITS

L i n e a m

e n t o B u s a mb r a

Zuccarone

P. Marabito

FICUZZA

b

a

0 m

500

1000

-500

-1000

NNW

500

1000

Rocca Busambra - Piano PilatoZuccaroneSSE

500 m

123

Page 4

118 Facies (2009) 55:115–135

Four regions (Fig. 3b) have been diVerentiated along theRocca Busambra ridge, which are characterized by com-mon lithofacies associations (Table 1).

Most of the main tectono-stratigraphic characteristics,such as stratal discontinuities at the scale of a few to a fewhundred metres, abrupt contacts, angular stratigraphic rela-tionships, hiatuses and gaps, condensed sequences, hard-ground crusts, in situ breccias, dissolution surfaces, andresedimented clastic carbonates, occur in the diVerentregions of Rocca Busambra. Neptunian dykes and normalfaults of the investigated regions display diVerent tectonicorientations (Fig. 3a).

In the present paper, we have largely used the terminol-ogy of Santantonio (1993, 1994) to describe the facies asso-ciation recognized in the study area (Table 2).

Dataset

Lithostratigraphy of Rocca Busambra

The many lithostratigraphic units outcropping at the RoccaBusambra ridge are illustrated from the more ancient unit(Fig. 4):

1. Dolomitized Upper Triassic sponge-bearing reeflimestones (a in sections 10–12 of Fig. 4), 30 m thick,

cropping out in the easternmost sector of the RoccaBusambra (Pizzo Marabito region). The rock (whosefacies association has not been previously described) isa boundstone with rim cement Wlling the space inbetween the biotic elements (Fig. 6a, b). It becomes aclast-supported breccia (a� in section 12 of Fig. 4) insome places, the large subangular fragments of whichderive from erosion without reworking processes (insitu breccias). The intergranular space is Wlled with asand-sized matrix consisting of reddish radiolarianmudstone, crinoidal packstones, and eroded bedrock.Calcareous sponges (Follicatena irregularis, Panor-mida sp., Cheilosporites tirolensis) associated with rarecorals and calcareous algae occur as primary frame-building organisms. The Norian-Rhaetian age is con-Wrmed by several biostratigraphic studies carried outon similar rocks outcropping in the Palermo Mountains(Abate et al. 1977; Senowbari-Daryan 1980; Senow-bari-Daryan et al. 1982; Di Stefano and Senowbari-Daryan 1985) and the Monte Genuardo (Di Stefanoet al. 1990). A lateral transition to the peritidal lime-stones of the Late Triassic Sciacca Formation isinferred from seismic stratigraphic data (Agate et al.1998a; Catalano et al. 1998, 2000) and outcrop strati-graphic evidence from adjacent regions (Di Stefanoet al. 1990). Several open neptunian dykes cut theseUpper Triassic carbonates.

Fig. 4 a Measured stratigraphic sections along the Rocca Busambra ridge. b Location of the study stratigraphic sections (1–12) and the recon-structed tectonic proWles (I-VIII)

2m

Upper Triassic reef dolostones (RLS)

Lower Liassic peritidal limestones (Inici Formation, INI)

Crinoidal limestones (CDR)

Bositra limestones (BCH1)

Saccocoma limestones (BCH3)

Calpionellid limestones (Lattimusa. LAT)

Lower Cretaceous marly limestones(Hybla Formation, HYB)

Upper Cretaceous-Eocene pelagic limestones (AMM)

Glauconitic grainstone (CCR)

Langhian marls (CIP)

Campanian-Lower Maastrichtianmegabreccias (AMM1)

1 2 3 4 5 6 7 8 9 10 11 12

Fe-Mn crusts (hd)

neptunian dykes

pseudonodular texturescrinoidal fragments

Fe-Mn nodules

ammonoids

erosional surfaces

palaeokarst cavities

SYMBOLS:

PIANO PILATO REGION

W E

b

b bb

b

b

a

a

a

ll

b’

b

d

d

e

e

ec

f

g

gg

g

h

h

h

k

k

j

jj

k ii

Ros

soA

mm

oniti

co

f’

a’

f’’

dea’’

f’’’

i

ii

i i

i’

PIRRELLO REGION BUSAMBRA-PEAK REGION PIZZO MARABITO REGION

Am

erill

o F

m

13m

>40m

1-12: stratigraphic sectionsI - VIII: tectonic profiles

1 2 * * *

* * *

*

* *

* *

* 3

57 986

12

11

4

2 km 10

IIIV VI

VII

VIII

IV

III

aa′

bb′

c

d

e

f-′-″

g

h

i-′

j

k

l

a

bb

a

123

Page 5

Facies (2009) 55:115–135 119

Locally, scattered resedimented oolitic grainstone (a� insection 10 of Fig. 4) onlaps erosional surface carved in thedolomitized reef limestones (Fig. 6a).

2. White peritidal limestones (Inici Formation) outcropthroughout the central and western Rocca Busambraregions (b in sections 1–9 of Fig. 4). They consist ofalgae- and mollusc-bearing wackestone and ooliticpackstone/grainstone organized in shallowing upwardcycles, up to 400 m thick. Benthic foraminifera, echino-derms, rare crinoids, calcareous algae (Cayeuxia sp.,Thaumatoporella parvovesiculifera (Raineri), Paleo-dasycladus mediterranus Pia), gastropods, pelecypods,brachiopods, and ammonites are the main fossil compo-nents. The age of these beds is constrained to the Het-tangian-Sinemurian time by algae and rich ammonitefauna (Arkell 1956; Gemmellaro 1878; Gugenberg

1936). The tops of the white peritidal limestones appearto be penetrated and dissected by dense networks ofneptunian dykes. These networks consist of subvertical,oblique and, sometimes, bed-parallel fractures withpolyphase Wlling by Jurassic, Cretaceous, and Miocenesediments. The peritidal limestones are covered by red-dish-matrix-supported in situ-breccia (b9 in section 1 ofFig. 4). The latter, 80–100 cm in thickness, consists oflight pink–grey to white, dm-sized fragments of peritidal(laminar stromatolites) and shallow subtidal algalwackestone. Blackish Fe–Mn crusts (hardground) cap-ping the top of the white peritidal limestones (Fig. 6c)outcrop only in the Piano Pilato region (c in Fig. 4);these crusts are absent in other regions. The encrustedhorizon is a 15-cm-thick single bed with a tabular shapeand Xat-lying to undulate laminae (Fig. 6d).

Fig. 5 NNE–SSW tectonic proWles, showing the depositional setting of the diVerent regions along the Rocca Busambra ridge. For localities, seeFig. 4b

123

Page 6

120 Facies (2009) 55:115–135

A regional unconformity marks the top of the Inici Forma-tion, which is overlain by pelagic ammonitic and Bositralimestones or crinoidal limestones.

3. Crinoidal limestones (d in sections 3, 4, and 8 ofFig. 4), which consist of red to white massive grain-stone/packstone, 50–80 cm thick, at places encrustedby Fe–Mn layers; its top surface is also capped byblackish Fe–Mn crusts (Fig. 6c), which, in turn, arecrossed by thin Wssures Wlled with dark-colored Fe–Mnoxides. At Pizzo Marabito, red crinoidal grainstone (din section 10 of Fig. 4) has been preserved in narrowgullies. Crinoid ossicles and plates (Pentacrinus sp.),benthic foraminifera, and micritized grains are abun-dant. These deposits which sporadically crop out onlyin the Piano Pilato region as Wllings of neptuniandykes, have been dated as Toarcian by Wendt (1963,1971) on the basis of their ammonite content.

4. The “Rosso Ammonitico” beds, grouped in the Bucc-heri Formation (Patacca et al. 1979), consist of:

(a)Bositra limestones (e in Fig. 4, BCH1 in Fig. 6c): red-dish brown to grey wackestone/packstone (Fig. 6e)with ammonites, radiolarians, fragment of thin-shelled pelagic bivalves (Bositra buchi), few frag-ments of thick-shelled molluscs, often Mn-coated(Fig. 6f), and local laminitic stromatolites, a fewmetres thick. They mostly outcrop in the Piano Pilatoregion. This lithofacies is easily recognized by thedark dm-sized nodules that are encrusted by ferro-manganese oxides (Wendt 1963; Jenkyns 1970c,1971) and by the interlayered cm-sized dark Fe–Mncrusts (Fig. 6g). These deposits were dated as Batho-nian–Early Kimmeridgian on the basis of the wide-spread ammonite association (Wendt 1965; Wendt1969; Cecca and Pochettino 2000).

(b)Saccocoma limestones (f in Fig. 4, BCH3): red togrey pelagic crinoids- and Aptychus-bearing grain-stone/packstone (Fig. 6h, i), a few metres thick. Theyoutcrop in the Piano Pilato, Pirrello and Pizzo Marab-T

able

1D

etai

ls o

f th

e fa

cies

ass

ocia

tions

rec

ogni

zed

alon

g th

e R

occa

Bus

ambr

a ri

dge

Fac

ies

asso

ciat

ions

Tex

ture

and

lith

olog

yT

hick

ness

Foss

il co

nten

tsG

eom

etri

esL

ower

bou

ndar

yS

ubst

rate

type

Con

dens

ed

pela

gic

Fos

silif

erou

s re

ddis

h lim

e w

acke

ston

e,

pink

and

whi

te n

odul

ar m

arly

lmst

, w

hite

mud

ston

e/w

acke

ston

e

0.5–

5m

Am

mon

ites,

bra

chio

pods

, pel

agic

biv

alve

s (B

osit

ra s

p.),

rad

iola

rian

s,

(mos

tly

Dog

ger)

, pel

agic

cri

noid

s (m

ostl

y M

alm

) ca

lpio

nell

ids

(Tith

onia

n)

Mas

sive

, ta

bula

rO

nlap

, pa

raco

nfor

mity

Low

er L

iass

ic p

eriti

dal

lmst

cap

ped

by F

e–M

n cr

usts

Rew

orke

d pe

lagi

c P

ink

and

redd

ish

pack

ston

e–gr

ains

tone

, gr

ey a

mm

onite

Xoa

tsto

ne,

whi

te p

elag

ic r

ewor

ked X

oats

tone

10–3

0m

Rew

orke

d bi

ocla

sts

of p

elag

ic c

rino

ids,

ben

thic

fo

ram

inif

era,

am

mon

ites,

bel

emni

tes

(mos

tly

Mal

m)

and

calc

areo

us p

lank

ton

(Lat

e C

reta

ceou

s-E

ocen

e an

d E

arly

Mio

cene

)

Len

ticu

lar,

dr

apin

gB

uttr

ess

unco

nfor

miti

es,

dow

nlap

Low

er L

iass

ic p

eriti

dal

lmst

, Upp

er T

rias

sic

reef

lmst

with

ero

ded

and/

or f

ault

ed b

eds

Res

edim

ente

dP

elag

ic m

atri

x su

ppor

ted

brec

cias

an

d m

egab

recc

ias

5–50

mA

mm

onite

s, b

rach

iopo

ds, b

elem

nite

s,

pela

gic

crin

oids

, cal

care

ous

plan

kton

(L

ate

Cre

tace

ous

and

Mio

cene

)

Pin

ch-o

ut,

talu

sO

nlap

, but

tres

s un

conf

orm

ities

, do

wnl

ap w

ith e

rosi

on

Low

er L

iass

ic p

eriti

dal

lmst

and

con

dens

ed

pela

gic

faci

es a

ssoc

iatio

n

Pel

agic

Whi

te li

me

mud

ston

e, n

odul

ar m

arly

lmst

, gra

y m

udst

one

and

mar

ls>

50m

Am

mon

ites,

cal

pion

ellid

s, r

adio

lari

ans,

ca

lcar

eous

pla

nkto

nInW

llin

g an

d ag

grad

ing

But

tres

s un

conf

orm

ities

, m

arin

e on

lap

Jura

ssic

dep

osit

s, e

rode

d L

ower

Lia

ssic

per

itida

l lm

st a

nd U

pper

T

rias

sic

reef

lmst

Table 2 Comparison of the diVerent terminology used to describefacies associations (facies ass.) in the Jurassic–Cretaceous pelagiccarbonate platform successions by multiple authors

Santantonio 1993, 1994 Martire et al. 2002 This paper

Condensed pelagic facies ass.

Normal succession

Condensed pelagic facies ass.

Composite pelagic facies ass.

Anomalous succession

Reworked pelagic facies ass.

Normal and resedimented pelagic facies ass.

Resedimented facies ass.

Basinal pelagic facies ass.

123

Page 7

Facies (2009) 55:115–135 121

ito regions. These deposits contain abundant pelagiccrinoid ossicles (Saccocoma sp.), echinoids frag-ments, brachiopods, belemnites, benthic foraminifera(Protopeneroplis striata Weynschenk), Globochaetesp., Aptychus sp., radiolarians, and ammonites. Basedupon these occurrences, these deposits are dated tothe Late Kimmeridgian–Early Tithonian time interval(Wendt 1969)

This unit consists of two main lithofacies. The Wrst is a nod-ular to pseudonodular condensed thin-bedded wackestone–packstone, with Fe–Mn crusts (widely outcropping at PianoPilato) and pink radiolarian- and ammonite-bearing mud-

stone alternated with reddish–pink crinoidal grainstone topackstone, with Fe–Mn oxide-impregnated Aptychus frag-ments (Pizzo Marabito region). The second one is a thick-bedded, tabular and massive reworked grainstone–pack-stone, outcropping along the entire ridge. This lithofacies atthe Pirrello region displays: graded and parallel laminatedmassive crinoidal coarse grainstone (5 m thick) with inter-nally encrusted microcavities and sedimentary dykes Wlledby Xat-lying and cross-laminated white to pink mudstone(f� in section 6 of Fig. 4) and grey massive Xoatstone that is2 m thick with large (dm-sized) reworked ammonites (f� insection 6 of Fig. 4). At the Pizzo Marabito region it appearsas a belemnite-bearing reddish reworked Xoatstone inter-

Fig. 6 Pizzo Marabito region. a Dolomitized Upper Triassic sponge-bearing boundstone (A) followed upwards by oolitic grainstone (B). The boundary between the two lithofacies is an erosional surface. b The same facies as above showing cement (X) Wlling the space in between sponge elements. c Jurassic con-densed succession at Piano Pil-ato. INI Lower Liassic peritidal limestones, CDR Toarcian cri-noidal limestones, BCH1 Bositra limestones, hd Fe-Mn crusts from the Piano Pilato region with pinnacles morphology at the top of the peritidal lime-stones. d Bulbous and laminated Fe–Mn crust; intraformational microbreccias are dispersed, indicating in situ erosional pro-cesses. e Wackestone with amm-onites, radiolarians, Aptychus, and thin-shelled fragments of the Bositra limestones. Piano Pilato region. f The same facies as above with Fe–Mn crusts and Mn-coated bioclasts. g Fe–Mn nodules and dark crusts (white arrows) of the Bositra lime-stones. Piano Pilato region. h Pseudonodular lithofacies of the Upper Jurassic Saccocoma lime-stones. Piano Pilato region. i Up-per Jurassic reworked facies with Saccocoma sp., Aptychus, echinoid fragments, benthic foraminifera. Piano Pilato region

123

Page 8

122 Facies (2009) 55:115–135

layered with pseudonodular pink calcareous marls (f�� insection 12 of Fig. 4).

5. Pink to white thin bedded cherty limestones (Latti-musa, g in sections 4 and 10–12 of Fig. 4). They out-crop in the Pizzo Marabito (1–15 m thick) and PianoPilato regions (few metres). At Pizzo Marabito thethin-bedded cherty nodular mudstone–wackestone arelaterally replaced by layered intraformational pebblymudstone and resedimented bioclastic breccias. Thesamples contain calcareous nannoplankton (Nannoc-onus steinmanni), radiolarians, belemnites, ammonitesand calpionellids of the Calpionella, Calpionellopsis,and Calpionellites biozones (Alleman et al. 1971).Based upon these contents, the limestones were datedto Late Tithonian–Early Valanginian time.

6. Marly calcareous and calcilutites with intercalations ofintraformational bioclastic (Aptychus and mollusc frag-ments) Xoatstone (Hybla Formation, h in sections 10–12 of Fig. 4). They outcrop in the Pizzo Marabitoregion (up to 50 m thick). Based upon the presence ofnannofossils (Lithraphidites spp., Nannoconus cfr.steinmannii, Micrantholithus obtusus) and planktonicforaminifera (Globigerinelloides algerianus (Cush-man and Ten Dam), G. ferreolensis (Moullade), Hed-bergella spp., Ticinella spp.), these deposits areassigned to the Aptian–Albian time interval.

7. White and red pelagic limestones (Amerillo Formation,i in Fig. 4). These limestones (1–50 m thick) consist ofplanktonic foraminifera-bearing wackestone (Fig. 7a,b). The presence of planktonic foraminifera (Rotali-pora appenninica White, Globotruncana ventricosa(White), G. gr. linneiana, Turborotalia cerroazulensis(Toumarkine and Bolli), Globigerinatheka sp.) and cal-careous nannofossils (Quadrum gothicum, Micror-habdulus decoratus DeXandre, Prediscosphaera sp.,Ericsonia formosa (Haq), Reticulofenestra sp., Coccol-ithus pelagicus Wallich, Discoaster cf. bisectus) sug-gests that the limestones encompass the Cenomanian–Lower Maastrichtian and the Middle–Late Eocene timeintervals. No Palaeocene deposits have been detected.The pelagic deposits outcrop widely along the entireridge.

8. Calcareous megabreccias, embedded into AmerilloFormation pelagic limestones, outcrop in the Pirrelloand Rocca Busambra peak regions (j in sections 8–9 ofFig. 4). The megabreccia is a rudstone–Xoatstone(Fig. 7c, d) that consists of subrounded cobbles andboulders, which derive from the break-up of the UpperTriassic–Jurassic peritidal and pelagic deposits. Thefossil content found in the matrix of the megabreccia islargely composed of plankton foraminifera (Globo-truncana ventricosa, G. gr. linneiana) and calcareous

nannoplankton (Quadrum gothicum, Microrhabdulusdecoratus, Prediscosphaera sp.) pointing out a Campa-nian–Lower Maastrichtian age (see also Catalano andD’Argenio 1982a; Gullo and Vitale 1986).

9. Glauconitic globigerinid-bearing yellow-green packe-stone/grainstone (k in sections 1, 2, and 5 of Figs. 4 and7e). The lithofacies (not described previously), whichare 5–30 m thick, pertain to the Calcareniti di Corleoneformation and unconformably overlie older Mesozoicdeposits (Fig. 7f). The fossil content, largely plank-tonic foraminifera (Globigerinoides spp., Praeorbulinasp.), comprised of the Globigerinoides trilobus andPraeorbulina glomerosa s.l. biozones (Iaccarino 1985),suggests that the deposits originated in the Burdiga-lian–Early Langhian age. These lithofacies outcrop inthe Pirrello and Piano Pilato regions where they Wll thepreviously formed neptunian dykes.

10. Brown and dark clayey marls with glauconite (l insections 4 and 5 of Fig. 4, not described before) out-crop in the Piano Pilato and Pirrello regions (15–20 mthick). The occurrence of nannofossils with Sphenoli-thus heteromorphus (DeXandre), Helicosphaera wal-bersdorfensis (Muller), H. waltrans (Theodoridis), andCalcidiscus premacintyrei (Theodoridis) from theMNN5a biozone indicates a Middle–Late Langhianage (Fornaciari et al. 1996; Sprovieri et al. 1996,2002).

Facies associations

The identiWed Jurassic–Miocene units of the lithostrati-graphic succession can be grouped into four facies associa-tions (Table 1). They are well localized into four regionsalong the Rocca Busambra ridge, and are related to speciWctectono-sedimentary settings (Table 3).

The “condensed pelagic” facies association consists ofa Jurassic succession which is a few metres thick and isrich in pelagic fauna. The “condensed pelagic” faciesassociation crops out widely in the Piano Pilato region,where it overlies the blackish laminated Fe–Mn crusthorizon that caps the Lower Liassic peritidal limestones;it shows, from bottom to top (Fig. 8): (a) laterally discon-tinuous reddish crinoidal limestones that onlap the under-lying beds (CDR); (b) thick-massive Dogger Bositralimestones (BCH1), which lies, often with onlap geome-try, above the encrusted white peritidal limestones and thecrinoidal limestones (INI); (c) Saccocoma limestones(BCH3) with an uneven tabular setting and a thinly bed-ded and nodular to pseudonodular texture (Fig. 6h) thatparaconformably overlies the Bositra limestones (Fig. 8).The facies association, also, occurs at Pizzo Marabitoregion, where the Dogger Bositra limestones (e insection 10 of Fig. 4) onlaps and abuts, in buttress uncon-

123

Page 9

Facies (2009) 55:115–135 123

formity (sensu Davis and Reynolds 1996), the faultedUpper Triassic reef limestones.

The “reworked pelagic” facies association is repre-sented by a Jurassic–Miocene pelagic succession, which is5–30 m thick and is characterized by coarse textures andinternal erosional surfaces (Fig. 9). The Upper Jurassicgraded and parallel laminated massive crinoidal coarsegrainstones are unconformably overlain by Upper Creta-

ceous light brown and white intraformational Xoatstoneand pebbly mudstone (i� in section 7 of Fig. 4 and AMMain Fig. 9) and, locally, Lower Miocene glauconitic grain-stone (CCR in Fig. 9). As shown in Fig. 9, this facies asso-ciation unconformably overlies, in buttress unconformity,the faulted platform subhorizontal beds and downlaps,with common erosion, the “condensed pelagic” faciesassociation. The fossil content consists of abundant

Fig. 7 a Wackestone with globotruncanids and intraclasts; Upper Cretaceous pelagic lime-stones (Amerillo formation). Piano Pilato region. b Pelagic limestones of the Amerillo formation with Middle–Late Eocene planktonic foraminifera assemblage. Pirrello region. c Upper Cretaceous carbonate megabreccias with white angular elements of Lower Liassic peri-tidal limestones (INI) welded in the pink Upper Cretaceous pe-lagic limestones. Rocca Busam-bra-peak region. d Rudstone–Xoatstone with Lower Liassic peritidal limestones (pl) and pelagic Rosso Ammonitico (ra) elements welded in the Upper Cretaceous globotruncanids wa-ckestone. Rocca Busambra-peak region. e Lower Miocene “re-worked pelagic” facies that con-sists of globigerinid packstone–grainstone with glauconite (g). Piano Pilato region. f Paracon-formity stratigraphic contact between Lower Miocene glauco-nitic wackestone (CCR) and in situ breccia lithofacies of the Lower Liassic peritidal lime-stones; glauconitic deposit sills are present. Rocca Argenteria, Piano Pilato region

Table 3 Morphologic details of the tectono-stratigraphic sys-tems recognized along the Rocca Busambra ridge

Tectono-sedimentarysystems

Morphology Facies association Timing

Stepped margins Stepped slope Condensed pelagic, reworked pelagic

Late Jurassic

Horst and graben Swell and basin Condensed pelagic pelagic and resedimented

Late Cretaceous

Scalloped margins Eroded and concave surface Reworked pelagic Late Cretaceous

Base of slope Faulted basinal margin Resedimented Late Cretaceous

Depositional slope Gently sea bottom dips Pelagic Late Jurassic

123

Page 10

124 Facies (2009) 55:115–135

pelagic crinoids, fragments of belemnites, ammonites, gas-tropods, and benthic and planktonic foraminifera. Thefacies association outcrops at the Piano Pilato, Pirrello,and Pizzo Marabito regions.

The “resedimented” facies association consists of brec-cias and/or megabreccias (Fig. 7c, d) interlayered into theUpper Jurassic, Upper Cretaceous, Middle–Upper Eocene,and Lower Miocene pelagic deposits of the Piano Pilato,Pirrello, and Rocca Busambra peak regions. The whiteangular clasts are mostly derived from fragmentation of theLower Liassic white peritidal limestones.

The “pelagic” facies association consists of white to greycherty mudstone–wackestone, marls, and calcilutites withrich calcareous plankton content. This Jurassic–Cretaceousfacies association unconformably overlies the Upper Trias-sic–Lower Jurassic carbonate platform substrate or onlapsthe “reworked pelagic” facies association.

Regional examples

Piano Pilato region

The region of Piano Pilato, located at the westernmost sideof Rocca Busambra (Fig. 3b), and uphill continuing into theminor reliefs of Rocca del Drago, Rocca Argenteria, andPizzo Nicolosi, is characterized by a Jurassic “condensedpelagic” facies association, unconformably followed by theUpper Cretaceous “pelagic” and by the Lower Miocene“reworked pelagic” facies associations. The successionrests unconformably above the subhorizontal beds of theLower Liassic peritidal limestones.

In this region Martire et al. (in Agate et al. 1998a, Mar-tire and Bertok 2002 and Martire et al. 2002) illustrated twodiVerent kinds of successions in some Weld stops (Santanto-nio 2002). “Normal” Inici Formation-Rosso Ammoniticosuccession, where the two lithostratigraphic units are super-posed in paraconformity (through a thick Fe–Mn oxidecrust), and “anomalous” succession, where an angularunconformity is between the Inici Formation and overlyingpelagic Upper Jurassic Rosso Ammonitico or Upper Creta-ceous–Paleogene Scaglia sediments (see Table 2 for com-parison).

Several, south dipping, largely subvertical (60–80°steep) WNW–ESE-oriented palaeofaults (with some metresof downthrow) cut the Liassic carbonate platform deposits(tectonic proWles I–IV in Figs. 5 and 10). These features areeither fault planes (Fig. 11) or morphotectonic scarps thatare sealed by Middle to Upper Jurassic “reworked pelagic”and “resedimented” facies associations that lie with a but-tress unconformity against the hanging-wall scarp of thefault plane (tectonic proWles II and III in Figs. 5 and 11).

The western side of Piano Pilato (Pizzo Nicolosi) showsseveral WNW–ESE faults (Fig. 3a) that cut the Jurassicsubstrate, giving rise to a horst and graben setting; the mor-photectonic depressions (Fig. 12a, b) incised in the LowerLiassic peritidal limestones are Wlled by a 40-m-thick pack-age of Upper Cretaceous “pelagic” facies association. Thedepressions are bound by subvertical and antithetic faultplanes that originate the Pizzo Nicolosi and Rocca Ramusagraben structures (Figs. 12 and 13 and tectonic proWle II inFig. 5). Their downthrow increases as it moves northward.The Upper Cretaceous “pelagic” facies association directlyonlaps the Jurassic Xoor of the depressions (Fig. 13a), cropsout, in buttress unconformity, against the subvertical walls(Figs. 12c and 13b) and drapes the horst structures withboth onlap and downlap relationships (Fig. 13c).

Several interpretations have been suggested for the“Pizzo Nicolosi canyon” (Giunta and Liguori 1975). It isconsidered to be a tectonic structure bounded by normalMesozoic faults by Wendt (1971). On the basis of theobserved geometries Gullo and Vitale (1986) and Catalano

Fig. 8 Schematic stratigraphic section reconstructed in the Piano Pil-ato region. INI Lower Liassic peritidal limestones, CDR crinoidallimestones. The Jurassic “condensed pelagic” facies association con-sists of BCH1 Bositra limestones, BCH3 Saccocoma limestones, and hdferromanganese crusts. The “reworked pelagic” and “resedimented”facies associations consist of BCH3 and breccias (br); they abut, in but-tress unconformity, the faulted INI beds and downlap the Jurassic“condensed pelagic” facies and the INI

Fig. 9 Schematic stratigraphic section (not to scale) reconstructed inthe Pirrello region, showing the stratigraphic relationships between the“reworked pelagic” facies associations and the platform-carbonatesubstrate. INI lower Liassic peritidal limestones, BCH1 Bositra lime-stones (“condensed pelagic” facies); “reworked pelagic” facies associ-ation consists of BCH3 Saccocoma limestones, AMMa reworkedpelagic limestones (Amerillo formation), CCR globigerinid grainstone

123

Page 11

Facies (2009) 55:115–135 125

and D’Argenio (1990), suggest that it is a half-graben struc-ture. Longhitano et al. (1995), who explained the festoongeometry of the pelagic inWlling sediments, state that it is anegative Xower due to left-hand strike-slip movements.Lastly, it is described as a graben structure due to UpperCretaceous transtensional faulting by Martire and Mon-tagnino 2002.

These interpretations remain unproven conjectures sincecollection of Weld mesoscopic data in this area is very diY-cult.

At the southern scarp of Piano Pilato, a half-grabenstructure bounded by an E–W and WNW–ESE fault planeoutcrops (Fig. 3a). The faults cut the subhorizontal beds ofLower Liassic peritidal limestones and are sealed by LowerMiocene glauconitic “reworked pelagic” facies association(tectonic proWles III, IV, and V in Fig. 5); basal breccias,with angular to subrounded lithoclasts of Lower Liassicperitidal limestones embedded into Lower Miocene yellow-ish glauconitic packstone, are present. On the southern sideof the half-graben, the Lower Miocene glauconitic“reworked pelagic” facies unconformably covers the Juras-sic “condensed pelagic” facies association and is conform-ably followed by the Langhian marls that display maximumthickness (tectonic proWle III in Fig. 5). At Rocca Argente-ria, the Lower Miocene glauconitic deposits paraconform-ably cover the Dogger Bositra limestones and the LowerLiassic white peritidal limestones (Fig. 7f). The former Wlls

up a tectonic network of dykes and sills that cut into thewhite peritidal limestones at the same site.

Pirrello region

This region, located in the central part of the ridge(Fig. 3b), is characterized by deeply eroded elongated chan-nels with a subcircular cross-section of 2–3 km2 (tectonicproWles V and VI in Figs. 5 and 14) corresponding to a con-cave-upward erosional surface that is carved into the top ofthe Lower Liassic peritidal limestones. The erosional sur-faces are draped by the Jurassic and/or Upper Cretaceous,Middle Eocene, and Lower Miocene “reworked pelagic”and “resedimented” facies associations (sections 5–7 inFig. 4). The top of the Lower Liassic peritidal limestones iscrosscut by neptunian dykes and cm-thick anastomosingveins Wlled with reddish or dark iron-manganese-rich car-bonate mudstone. Large karst dissolution cavities Wlled bylaminated siltstone and closed by coarse blocky calcite arepresent at the top of the subhorizontal beds.

In the Pirrello region, Wssures, fault planes, and morpho-structural scarps have diVerent orientations (Figs. 3a and14):

(a) large (mappable) neptunian dykes with the same orien-tation (Fig. 14a, b, d) are mostly Wlled by reddish Lias-sic crinoidal limestones and Dogger Bositra limestones.

Fig. 10 a Panoramic view of the southern slope of Piano Pil-ato, showing stepped faults and palaeoscarps; INI lower Liassic peritidal limestones; J Jurassic deposits. b Geological map of the area

123

Page 12

126 Facies (2009) 55:115–135

(b) WNW–ESE palaeofaults dissect the Jurassic “con-densed pelagic” facies association and its carbonatesubstrate, which results in a stepped morphology.These faults are draped with Saccocoma limestones.

(c) ENE–WSW fault planes dissect, with small displace-ment, the Lower Liassic peritidal limestones in theuphill region and are sealed by a Jurassic and UpperCretaceous “reworked pelagic” facies association(Fig. 14a, d).

(d) NNE–SSW south-easterly dipping trending faultsbound the elongated channels and are unconformablydraped by the Upper Cretaceous–Eocene “pelagic” and“reworked pelagic” facies (Fig. 14a, b, d). In certainplaces, these faults intersect the previously (Jurassic)formed WNW–ESE lineaments (Fig. 3a).

(e) E–W palaeofaults cut the Lower Liassic peritidal lime-stones and are sealed by the strongly inclined LowerMiocene glauconitic “resedimented” and “reworkingpelagic” facies associations that abut, in buttressunconformity, the subhorizontal white peritidal lime-

stones beds along a south dipping fault scarp with afew tens of metres of downthrow (tectonic proWle V inFigs. 5 and 14a, c).

Rocca Busambra peak region

Located to the east of Pirrello (Fig. 3b), this region has aprominent thick “resedimented” facies association that con-sists of massive Upper Cretaceous carbonate megabreccias.These deposits commonly overlie the Jurassic “condensedpelagic” facies association. In certain places, tabular and/orlenticular-shaped carbonate megabreccias (j section 9 ofFig. 4) abruptly onlap the Lower Liassic peritidal lime-stones and Wll up shallow channelled gullies (peak of RoccaBusambra, Fig. 15).

The measured tectonic orientations show evidence of:

(a) Subvertical ENE–WSW faults (with a few to severalmetres of downthrow) dissect the Lower Liassic whiteperitidal limestones (Fig. 15b) or the whole Jurassic“condensed pelagic” facies association (in the south-ernmost sector, tectonic proWle VII in Fig. 5). Conse-quently, the carbonate megabreccia wedge seals, as abuttress unconformity, the hanging wall block of thefault planes and downlaps, with erosion, the older(Jurassic–Cretaceous) deposits on the footwall block(tectonic proWle VII in Figs. 5 and 16).

(b) ENE–WSW oriented faults (reactivated?) dissect, inturn, the carbonate megabreccias outcropping at thepeak of Rocca Busambra and are sealed by Middle–Upper Eocene pelagic limestones (Fig. 15b). The latterdrape the megabreccia, onlap the Lower Liassic whiteperitidal limestones, and abut, in buttress unconfor-mity, the older ENE–WSW fault planes (tectonic pro-Wle VII in Figs. 5 and 15).

Pizzo Marabito region

In the Pizzo Marabito region, located along the easternmostside of the ridge (Fig. 3b), the succession deeply diVersfrom those that were previously described. An Upper Trias-sic reef carbonate substrate is overlain by Upper Jurassic“reworked pelagic” and uppermost Jurassic–Lower Creta-ceous “pelagic” facies associations (sections 10–12 inFig. 4).

Palaeotectonic features are represented by (a) Wssures,neptunian dykes, and in situ breccias in the Upper Triassicreef limestones and (b) ENE–WSW trending pre-UpperJurassic subvertical fault planes (Fig. 3a). These planesgenerated a stepped morphology and tilted the bedding(tectonic proWle VIII in Figs. 5 and 17). Consequently, theUpper Jurassic “reworked pelagic” facies association,which progressively onlaps the reef Triassic substrate,

Fig. 11 Field evidence (above) and sketch (below) of the fault planethat dissected the Lower Liassic peritidal limestones (1) and DoggerBositra limestones (2) in the Piano Pilato region. The Malm Saccoco-ma limestones (3) lie with a buttress unconformity against the hanging-wall scarp of the fault plane and in downlap on the subhorizontal Bos-itra limestones of the footwall block

123

Page 13

Facies (2009) 55:115–135 127

abuts the fault planes in buttress unconformity. The planesare, in turn, sealed (Fig. 17) by uppermost Jurassic–LowerCretaceous “pelagic” facies association. These depositsdrape the tilted fault blocks of Triassic reef limestonesoften with downlap geometries (tectonic proWle VIII inFigs. 5 and 17).

Discussion

Tectono-stratigraphic settings

Based on the presented data, the following tectono-strati-graphic settings (Table 3 and Fig. 18) were recognized.

Stepped fault margin systems

This tectono-stratigraphic setting is easily recognizable inthe Piano Pilato region. Several WNW–ESE-oriented fault

planes with small displacements (tectonic proWles III andIV in Figs. 5 and 10) produced a stepped margin morpho-structural setting (Fig. 18a).

The interpretation is supported by: (a) stratigraphic but-tress unconformities occurring between the faulted peritidallimestones and the younger deposits, (b) subangular brec-cias at the fault scarps, originated from the breaking up ofthe faulted peritidal limestones, (c) subvertical fault planes,most of which show a homogeneous orientation (WNW–ESE), (d) the lack of isolated blocks of peritidal limestonesand Jurassic megabreccias accumulation, features linked togravitational sliding and slip processes (Winterer and Sarti1994).

The faults, formed as fractures of the top of the LowerLiassic peritidal limestones, were later reactivated duringthe tectonic pulses of the Kimmeridgian, the latest Jurassic,and Late Cretaceous ages. The faults maintained the sameorientation during the Mesozoic, while they slightly rotatedduring Early Miocene tectonic events.

Fig. 12 a Graben structures at Pizzo Nicolosi. The Upper Cre-taceous pelagic limestones (AMM, colored in green) abut, in buttress unconformity, the sub-horizontal Lower Liassic peritid-al limestones beds (INI) and the Bositra limestones (BCH1) along WNW–ESE faults, thus forming depressions with rela-tive downthrow of more that 50 m (Rocca Ramusa and Pizzo Nicolosi grabens) and draping the horst erosional margins. b Filling of the Pizzo Nicolosi gra-ben (eastern-side) and c view of the angular contact in buttress unconformity between the sub-vertical Upper Cretaceous pelag-ic beds and the faulted Lower Liassic platform beds; fault plane is colored in red

Fig. 13 a, b Close-up of the Rocca Ramusa graben Wlled by the Upper Cretaceous pelagic limestones (AMM, in green) that onlap the peritidal limestones on the Xoor of the graben and abut, in buttress unconformity, the subhorizontal beds of INI in the southern Xank of the structure; fault plane is the area colored in red. c Angular relationships be-tween AMM and INI along the horst

123

Page 14

128 Facies (2009) 55:115–135

The Jurassic to Cretaceous “condensed pelagic” and“reworked pelagic” facies associations are the most com-mon lithologies. These sequences are accompanied bysome long-lasting hiatuses, dated as Early Dogger andEarly Cretaceous by Christ (1958) and Wendt (1963) orPalaeocene (this paper), which strongly supports the idea ofa depositional setting related to the original physiographicalhigh that later evolved into a stepped margin morphostruc-tural setting.

Martire and Bertok (2002) recognized and describedsome high- and low-angle surfaces at Piano Pilato, relatingto the latest Jurassic normal faults. In contrast Bertok andMartire (2004) explained these surfaces and the Lower–Middle Jurassic succession displacement as being formedby gravitational slides caused by tectonic instability. Theyrelated this setting to a main master fault located in thesouthern side of the Piano Pilato region and now buriedbelow the Tertiary deposits. This pattern may mark thetransition from the Trapanese pelagic platform domain tothe deep-water Sicanian domain.

However Weld data do not support this reconstruction.As is well evidenced by geological sections (Catalano et al.1998, 2000; Fig. 2b, this paper), the Rocca Busambra unit

shows northward and southward carbonate-platform con-tinuations. The adjacent Sicanian basinal deposits are incor-porated in a repeated thrust sheet wedge that regionallyoverthrusts the Trapanese domain (Rocca Busambra tec-tonic unit).

The “stepped margins” model is well documented inother peritidal platforms and pelagic platform domains(Bourrouilh 1981; Hurst and Surlyk 1984; Cecca et al.1990; Santantonio 1993, 1994; the “pelagic escarpment” ofDi Stefano et al. 2002a, b).

Horst and graben structures

Antithetic fault planes with rather large downthrows char-acterize the Pizzo Nicolosi area by forming two WNE–ESEparallel graben structures (Figs. 10, 11). The fault planes,cross-cutting the Jurassic morphostructures, likely repre-sent the reactivation of older faults. The graben-like struc-tures are Wlled by Upper Cretaceous pelagic sediments,while the horst accumulate only thin veneers of the “con-densed pelagic” facies association. Along the sides of thehorst structures, the small troughs, resulting from horst ero-sion (e.g., scalloped margins, see later), are Wlled with both

Fig. 14 a The Pirrello region is characterized by scalloped mar-gin features, showing uncon-formable relationships between the inWlling Upper Cretaceous pelagic limestones (colored in light green) and the faulted Low-er Liassic platform beds [see de-tail in (b)]. Panoramic picture, showing neptunian dykes (in white), E–W and ENE–WSW palaeofault trends (colored in red), and buttress unconformity between the faulted Lower Lias-sic platform beds and the Upper Cretaceous pelagic limestones (in green), see picture in (c). Fault planes are in red. d Geo-logical map of the area. INI low-er Liassic peritidal limestones, BCH1 Bositra limestones, BCH3 Saccocoma limestones, AMM1 Upper Cretaceous carbonate megabreccias, AMM Upper Cre-taceous–Eocene pelagic lime-stones, CCR Lower Miocene glauconitic grainstone (colored in yellow in the panoramic and detailed photos); CIP Langhian marls, d detritus, N neptunian bedding normal dykes, 1 synse-dimentary faults, 2 post-deposi-tional faults

123

Page 15

Facies (2009) 55:115–135 129

Jurassic “reworked pelagic” and Cretaceous “pelagic”facies associations (Fig. 12a).

Such a tectonic setting is well known as it occurred inboth ancient and modern syn-rift systems. Good examplesof this setting are reported for the Jurassic intraplatform

basins of Hungary (Galàcz et al. 1985; Galàcz 1988), theSouthern Alps (Jadoul et al. 2005), the Lower LiassicStreppenosa intraplatform basin of the Hyblean region (Pat-acca et al. 1979; Catalano and D’Argenio 1982a, b), and theintraplatform basin of the Trapanese domain in westernSicily (Marineo basin, Catalano and D’Argenio 1982b; Cat-alano et al. 2000; Di Stefano et al. 2002a).

Tilted fault-block systems

This setting is recognized along the southern scarp of thePiano Pilato and Pirrello regions, where E–W-trendingtilted blocks of the Lower Liassic peritidal limestonesextending for few kilometres are overlain by Lower Mio-cene globigerinid glauconitic grainstone and Langhianmarls. They abut, in buttress unconformity, the faultedLower Liassic beds of the hanging wall blocks and lie inonlap or downlap on the eroded Jurassic beds (peritidallimestones and Saccocoma limestones) of the footwallblocks.

Along this area basin asymmetry is clearly shown by thevariation of the thickness of the Lower Miocene glauconitic

Fig. 15 a View of the Rocca Busambra-peak where Upper Creta-ceous–Eocene pelagic limestones (AMM) onlap Lower Liassic plat-form deposits (INI). b Close-up of (a) showing faulted massive UpperCretaceous megabreccias (AMM1 and colored in light green) and up-ward thin Upper Cretaceous–Eocene pelagic beds that onlap and abut,in buttress unconformity, the faulted Lower Liassic peritidal lime-stones (fault planes colored in red)

Fig. 16 a View of the southern side of the Rocca Busambra-peakwhere Campanian-Lower Maastrichtian megabreccias (in green,AMM1) cover, in buttress unconformity, the faulted Lower Liassic plat-form deposits (INI, the fault plane is colored in light red) and, in down-lap, the Bositra limestones (dark red, BCH1) of the footwall tiltedblock. b Detailed geological map of the area. INI Lower Liassic peri-tidal limestones, BCH1 Bositra limestones, AMM Upper Cretaceous–Eocene pelagic limestones, AMM1 Upper Cretaceous megabreccias, ddetritus, e eluvium

Fig. 17 Onlap and buttress unconformity relationships between Up-per Jurassic Saccocoma limestones (BCH3), calpionellid limestones(LAT), and Upper Triassic reef limestones (RLS) at Pizzo Marabito;palaeofaults are colored in dark grey

Fig. 18 Models of the tectono-stratigraphic relationships of RoccaBusambra; a stepped fault margin system, b scalloped margin system,c base-of-slope system and tilted-fault blocks, and d depositional slopesystem

a) b)

c)d)

123

Page 16

130 Facies (2009) 55:115–135

grainstone and Langhian marls. This suggests that areas ofgreater subsidence can be considered as half-graben struc-tures.

Similar syn-sedimentary structures are recognized anddescribed by Eberli (1987) in the Northern CalcareousAlps, by Bertotti et al. (1993), Marchegiani et al. (1999),and Bernoulli et al. (1994) in the Southern Apennines, andin other areas by Wilson et al. (2000) and Bosence et al.(1998) among others.

Scalloped margin systems

This setting is recognized only for places where huge por-tions of Lower Liassic peritidal limestones appear to havebeen eroded (Fig. 18b). Spectacular features can be recog-nized in the Pirrello region, where a “hollow” morphologyoccurs. Erosional processes were active in Jurassic timesalong the sides of the faulted blocks. Along these marginalareas, one can envisage a sloping morphology at siteswhere sediment by-passing was active during the Meso-zoic.

The depressions are Wlled by Jurassic–Cretaceous“reworked pelagic” and pelagic facies associations whosesedimentological characters indicated an outer shelf orupper slope high-energy depositional environment adjacentto the minor sloping sectors of the pelagic platform whereJurassic “condensed pelagic” facies association developed(e.g., horst setting).

This tectono-stratigraphic setting can be compared witherosional margins described by Mullins and Hine (1989)from the Bahamas, by Santantonio (1994) from the Apen-nines, and by Bosellini (1998) from the Calcareous Alps,where similar processes were active.

The described features recall the concave-upward sur-faces that were related to detachment of “scoop-shapedblocks” along surWcial listric faults (Winterer and Sarti1994).

In the study area, listric faults have not been evidenced,but downslope mass wasting by sliding processes is welldocumented according to the occurrence of megabrecciabodies (e.g., Rocca Busambra peak region).

Base-of-slope talus systems

This setting (Fig. 18c) is well represented by the RoccaBusambra peak region (Figs. 15 and 16), where the thickmegabreccia bodies rest, with talus geometry, on thefaulted block of the Lower Liassic peritidal limestones. Therecognized faults appear to have been activated during theLate Cretaceous time interval (age of the carbonate megab-reccias).

Such a tectono-stratigraphic setting is well documentedin ancient and modern carbonate platform margins (Mullins

et al. 1986; Bernoulli et al. 1990; Spence and Tucker 1997;Bosellini et al. 1993; Bosellini 1998; among others).

Depositional slope

This setting (Fig. 18d) is recognized at Pizzo Marabito,where a pelagic succession rests on a dissected stepped reefcarbonate margin (Fig. 17). The occurrence of “reworkedpelagic” and “pelagic” facies associations (Lattimusa andHybla Formation) corresponds with a progressive drowningand deepening of the Upper Triassic reef substrate throughthe Mesozoic. The presence of detrital and slumping levelsin the Jurassic–Cretaceous “pelagic” facies association sug-gests that the Pizzo Marabito region was an unstable low-angle slope depositional setting.

When compared with the evolution of the nearby RoccaBusambra regions, the Jurassic–Cretaceous Pizzo Marabitosuccession appears to be settled in a “deeper” water deposi-tional environment.

Comparable examples of such sedimentary systems havebeen described in the Umbria–Marche Apennines (Farin-acci 1967; Baldanza et al. 1982; Cecca et al. 1990; Santan-tonio 1993, 1994; Marchegiani et al. 1999).

Tectono-sedimentary evolution

The collected data illustrate the Meso-Cenozoic tectono-sedimentary evolution of the Rocca Busambra very well.This evolution was dominated by tectonic pulses, partlycoeval with the history of the African continental margin(cf. Bernoulli and Jenkyns 1974; Catalano and D’Argenio1978). The evolution of the Rocca Busambra area can besummarized in the following steps (Table 4):

1. A Bahamian-type carbonate platform that developedduring Late Triassic–Early Liassic times on the conti-nental margin became a site of Jurassic pelagic sedi-mentation. Growth of the platform stopped at the endof the Sinemurian. The depositional unconformity atthe top of the Triassic–Liassic shallow-water depositsof the Peri-Mediterranean region (including westernSicily) indicated the break-up and dispersal of the car-bonate platforms. This event is related to the tectonicprocesses that generated the Tethyan Jurassic rifting(Bernoulli and Jenkyns 1974; Elmi 1977; Catalano andD’Argenio 1982b; Argiryadis et al. 1980; Bertotti et al.1993). In the Rocca Busambra ridge, this tectonic eventis documented by fractures and sedimentary dykes thataVected the top of the Liassic carbonate platform(widely known in western Sicily).

2. “Condensed pelagic” facies association of the RoccaBusambra area was deposited during the Middle Juras-sic post-rift transgressive event of Tethyan margin

123

Page 17

Facies (2009) 55:115–135 131

Tab

le4

Tim

ing

of te

cton

ic e

vent

s re

cogn

ized

alo

ng th

e R

occa

Bus

ambr

a ri

dge

Tim

ing

Faul

ts o

rien

tati

onR

egio

ns o

f ou

tcro

pO

utcr

op f

eatu

res

Tec

tono

-sed

imen

tary

set

tings

Reg

iona

l tec

toni

c ev

ents

Ear

ly T

oarc

ian

WN

W–E

SEE

ntir

e R

occa

Bus

ambr

a ri

dge

Nep

tuni

an d

ykes

Wll

ed

wit

h cr

inoi

dal l

mst

Bre

ak-u

p of

the

Low

er

Lia

ssic

per

itid

al lm

stE

xten

sion

al s

yn-r

ift

Kim

mer

idgi

an

WN

W–E

SEP

iano

Pila

to, P

irre

llo,

and

Pizz

o M

arab

ito r

egio

nsB

uttr

ess

unco

nfor

mit

y of

Sac

coco

ma

lmst

St

eppe

d fa

ult m

argi

nsE

xten

sion

al p

ost-

rift

, te

cton

ic s

ubsi

denc

e

Ear

lies

t Cre

tace

ous

WN

W–E

SEP

iano

Pila

to r

egio

nB

uttr

ess

unco

nfor

mity

of

cal

pion

elli

d lm

st, r

esed

imen

tsL

ocal

ste

pped

fau

lt m

argi

ns

and

slop

e in

stab

ility

Ear

ly C

reta

ceou

s P

izzo

Mar

abit

o re

gion

Str

ong

thic

knes

s of

Upp

er

Jura

ssic

-Low

er C

reta

ceou

s“p

elag

ic”

faci

es a

ssoc

iatio

n

Tilt

ed f

ault

bloc

ks, b

asin

asy

mm

etry

Lat

e C

reta

ceou

sW

NW

–ESE

N

NE

–SSW

Pia

no P

ilato

and

Pir

rello

reg

ions

But

tres

s un

conf

orm

ity

of U

pper

Cre

tace

ous

lmst

Sc

allo

ped

mar

gins

, hor

st

and

grab

en s

yste

ms

Lat

est C

reta

ceou

sW

SW

–EN

ER

occa

Bus

ambr

a-pe

ak r

egio

nM

egab

recc

ia p

rodu

ctio

n an

d bu

ttres

s un

conf

orm

itySc

allo

ped

mar

gin,

tilt

ed f

ault

bloc

ks,

talu

s br

ecci

a ba

se o

f-sl

ope

and

basi

n as

ymm

etry

Upl

ift,

cata

stro

phic

eve

nts

Mid

dle

Eoc

ene

WS

W–E

NE

N–S

Roc

ca B

usam

bra-

peak

an

d Pi

rrel

lo r

egio

nsM

egab

recc

ia f

ault

ed a

nd s

eale

dby

Eoc

ene

“res

edim

ente

d”

and

“pel

agic

” fa

cies

ass

ocia

tions

By-

pass

mar

gins

, tilt

ed f

ault

bloc

ks

Ear

ly M

ioce

neW

NW

–ESE

W–E

Pia

no P

ilato

and

Pir

rello

reg

ions

But

tres

s un

conf

orm

ity

of g

lauc

oniti

c sa

ndst

ones

an

d L

angh

ian

mar

ls

Tilt

ed-f

ault

bloc

ks, r

eact

ivat

ed f

ault

s

123

Page 18

132 Facies (2009) 55:115–135

(Jacquin and De Graciansky 1998) and are thereforecharacterized by frequent iron-manganese crusts andimpregnations. During this time the entire RoccaBusambra ridge, as well as some Trapanese structuresoutcropping in western Sicily, were characterized by aphysiography of morphostructural highs.

3. Faults and palaeoscarps that formed in response to thepre-Kimmeridgian tectonic pulses on the RoccaBusambra and neighboring areas (e.g., Mount Kumeta,Di Stefano et al. 2002a, b) are interpreted as originatinga “stepped fault margin” setting.

4. During the latest Jurassic to Early Cretaceous times,some of the pelagic platform areas maintained theirroles as structural highs (e.g., Piano Pilato, Pirrello,and Rocca Busambra peak regions) Xanked by mar-ginal areas that rapidly subsided to basins at depthswhere pelagic deposits onlapped the Jurassic “steppedmargins” made up of older rocks (e.g., Pizzo Marabitoregion).

5. During the Late Cretaceous, the Jurassic rock pile wasdismembered by faulting that reactivated previous faultplanes, or generated new and diverse trending linea-ments. Consequently, local intraplatform basins devel-oped and were Wlled by pelagic carbonates (e.g., horstand graben system). The uplifting of the faulted car-bonate blocks was accompanied by discharge of largeamounts of detritus at the foot of the fault scarp, form-ing thick “resedimented” facies association sequences(e.g., base-of-slope system). In western Sicily, wide-spread shallow-water carbonate-derived megabrecciasinterlayered in the Upper Cretaceous pelagic platformand basin successions have been linked to Late Creta-ceous tectonics (Catalano et al. 1991).

6. After the Late Cretaceous, the central and westernregions of Rocca Busambra maintained their role asstructural highs, while the subsiding adjacent regionswere Wlled by widespread pelagic deposits.

7. During the Late Eocene time another tectonic pulse isrevealed by the carbonate breccias found at the easternsector of the Pirrello region tilted fault-blocks system.

8. In the earliest Miocene, a new tectonic event over-printed the Meso-Cenozoic rocks of the Rocca Busam-bra. It produced a tilted fault-block system wellpreserved in the southern scarp of the Piano Pilato andPirrello regions.

Conclusions

Geological mapping, stratigraphy, sedimentology, andstructural data collected in Mesozoic pelagic carbonate sys-tems of Rocca Busambra (Western Sicily) permitted theidentiWcation of: (a) distinct patterns of vertical and lateral

facies changes in Meso-Cenozoic carbonate rocks groupedinto four major facies associations; (b) distinct angular geo-metric relationships (buttress unconformity, onlap, down-lap) between several rock bodies; (c) clear orientationtrends of the Mesozoic tectonic features, such as faultplanes and neptunian dykes; and (d) distinct timing of theidentiWed tectonic events.

Along the Rocca Busambra ridge, an articulate pelagiccarbonate platform margin can be recognized on the basisof the above-described depositional settings. From NW toSE, a palaeogeographic setting can be assumed to passfrom a structural high with horst and graben and steppedmargins systems to depositional slope areas, throughoutupper slope scalloped margins and base-of-slope environ-ments.

The tectonic features and the depositional settings in theRocca Busambra area suggest an original pelagic carbon-ate-platform system. Syn-sedimentary tectonics likelyplayed an important role in the development of this system.The tectonics is related to the syn- and post-rift phases ofthe Sicilian part of the Tethyan continental margin. Sedi-mentary evolution was driven by the tectonics that createdthe major unconformity geometry of the sediments from theEarly Liassic, Kimmeridgian, Late Cretaceous, and EarlyMiocene.

Acknowledgements The research was supported by grants “PRIN”2006 and Miur (ex 60%) 2005 (resp. Prof. R. Catalano). The author isgrateful to ProV. F. Jadoul, G. Mariotti, L. Montanari, A. Mindszenty,and L. Martire for their useful suggestions on an early draft of themanuscript. Special thanks are due to ProV. J. Wendt and H. Jenkynsfor their useful comments to the manuscript. Prof. E. Di Stefano andDr. S. Bonomo helped with the calcareous plankton data.

References

Abate B, Catalano R, D’Argenio B, Di Stefano P, Riccobono R (1977)Relationships of algae with depositional environments and faunalassemblages of the Panormide Carbonate Platform, Upper Trias-sic, Northwestern Sicily. In: Flügel E (ed) Fossil algae, recentresults and development. Springer, New York, pp 301–313

Agate M, Basilone L, Catalano R, Franchino A, Merlini S, Sulli A(1998a) Ipotesi sulla condizione strutturale della Rocca Busam-bra. In: Guida alle escursioni, vol. 1, La Sicilia occidentale, 79°Congresso della Società Geologica Italiana, Palermo, pp 71–78

Agate M, Basilone L, Catalano R, Franchino A, Merlini S, Sulli A(1998b) Monte Barracù—Deformazione interna delle UnitàSicane nell’area tra Corleone e Monte Colomba. In: Guida alleescursioni, vol. 1, La Sicilia occidentale, 79° Congresso dellaSocietà Geologica Italiana, Palermo, pp 79–88

Alleman F, Catalano R, Farès F, Remane J (1971) Standard calpionel-lid zonation (Upper Tithonian–Valanginian) of the western Med-iterranean province. Proc II Plankt Conference, Roma 1970, pp1337–1340

Alvarez W (1990) Pattern of extensional faulting in pelagic carbonatesof the Umbria–Marche Apennines of central Italy. Geology18:407–410. doi:10.1130/0091-7613(1990)018<0407:POEFIP>2.3.CO;2

123

Page 19

Facies (2009) 55:115–135 133

Argiryadis I, De Graciansky PC, Marcoux J, Ricou LE (1980) Theopening of the Mesozoic Tethys between Eurasia and Arabia-Af-rica. In: Geologie des chaines alpines issues de la Tethys. MemBur Rech Geol Min 115:199–214

Arkell WJ (1956) Jurassic geology of the world. Oliver & Boyd, Edin-burgh

Baldanza A, Colacicchi R, Parisi G (1982) Controllo tettonico sulla de-posizione dei livelli detritici nella Scaglia cretacico-paleogenica(Umbria orientale). Rend Soc Geol Ital 5:11–14

Basilone L (2007) Mesozoic tectono-sedimentary evolution of theRocca Busambra (western Sicily). FIST–Geoitalia 2007, SestoForum Italiano di Scienze della Terra, 12–14 Settembre 2007,Rimini. Epitome 2:403

Bernoulli D, Jenkyns HC (1974) Alpine, Mediterranean and CentralAtlantic Mesozoic facies in relation to the early evolution of theTethys. Modern and ancient geosynclinal sedimentation. In: DottRH, Shaver RH (eds). SEPM Spec Publ 19: 129–160

Bernoulli D, Bertotti G, Froitzheim N (1990) Mesozoic faults andassociated sediments in the Australpine-South Alpine passivecontinental margin. Mem Soc Geol Ital 45:25–38

Bernoulli D, Eberli GP, Pignatti JS, Sanders D, Vecsei A (1994) Se-quence stratigraphy of Montagna della Maiella. Fifth Symposiumon Ecology and Palaeoecology of Benthic Communities, 28–30Settembre 1992, Rome, Weld trip guide book, pp 85–109

Bertok C, Martire L (2004) Analisi di pelagiti su un margine di plateausottomarino: rilevanza a Wni strutturali e paleogeograWci. L’esem-pio di Rocca Busambra (Sicilia occidentale). Atti II Conv Geo-Sed, 22–28 Settembre 2004, Roma

Bertotti G, Picotti V, Bernoulli D, Castellarin A (1993) From rifting todrifting: tectonic evolution of the South-Alpine upper crust fromthe Triassic to the Early Cretaceous. Sediment Geol 86:53–76.doi:10.1016/0037-0738(93)90133-P

Bosellini A (1998) Scalloped versus faulted carbonate platform mar-gins and the origin of basinal megabreccias. Mem Soc Geol Ital53:63–74

Bosellini A, Neri C, Luciani V (1993) Platform margin collapses andsequence stratigraphy organization of carbonate slopes: Creta-ceous–Eocene Gargano Promontory, southern Italy. Terra Nova5:282–297. doi:10.1111/j.1365-3121.1993.tb00259.x

Bosence D, Cross N, Hardy S (1998) Architecture and depositional se-quences of Tertiary fault-block carbonate platforms: an analysisfrom outcrop (Miocene, Gulf of Suez) and computer modelling.Mar Pet Geol 15:203–221. doi:10.1016/S0264-8172(98)00016-6

Bourrouilh R (1981) “Orthoceratitico Rosso” et “ Goniatitico Rosso”:faciès marqueurs de la naissance et de l’évolution de paléomargesau Paléozoïque. In: Farinacci A, Elmi S (eds) Ammonitico RossoSymposium Proceedings, Rome, pp 39–55

Caron M (1985) Cretaceous planktonic foraminifera. In: Bolli HM,Saunders JB, Perch-Nielsen K (eds) Plankton Stratigraphy 1,Cambridge University Press, pp 17–86

Castellarin A, Colacicchi R, Praturlon A (1978) Fasi distensive, tras-correnze e sovrascorrimenti lungo la linea Ancona-Lazio, dal Liasmedio al Pliocene. Geol Rom 17:161–189

Catalano R, D’Argenio B (1978) An essay of palinspastic restorationacross western Sicily. Geol Rom 17:145–159

Catalano R, D’Argenio B (1982a) Schema geologico della Sicilia. In:Catalano R, D’Argenio B (eds) Guida alla Geologia della Siciliaoccidentale. Soc Geol Ital, Guide geologiche regionali, pp 9–41

Catalano R, D’Argenio B (1982b) Infraliassic strike-slip tectonics inSicily and Southern Apennines. Rend Soc Geol Ital 5:5–10

Catalano R, D’Argenio B (1990) Hammering a seismic section. Fieldtrip in Western Sicily, Guide Book. May 17–19, 1990, Diparti-mento di Geologia e Geodesia Univ. di Palermo, pp 19–22

Catalano R, Channell JET, D’Argenio B, Napoleone G (1977) Meso-zoic palaeogeography of the southern Apennines and Sicily. MemSoc Geol Ital 15:95–118

Catalano R, Milia A, Vitale PF (1991) Inversion tectonics in the Sicil-ian–Maghrebian Alpidic chain. Terra abstract EUG VI 3(1):232

Catalano R, Franchino A, Merlini S, Sulli A, Agate M, Basilone L(1998) Materiali per la comprensione dell’Assetto Profondo dellaSicilia Centro-Occidentale. In: Catalano R, Lo Cicero G (eds)Guida alle escursioni, La Sicilia occidentale, vol. I. 79° Con-gresso della Società Geologica Italiana, Palermo, pp 175–185

Catalano R, Franchino A, Merlini S, Sulli A (2000) Central westernSicily structural setting interpreted from seismic proWles. MemSoc Geol Ital 55:5–16

Catalano R, Sulli A, Agate M, Avellone G, Basilone L (2004) Thecrust in Western and Central Eastern Sicily. Field Trip GuideBook P45, 32° International Geological Congress, Firenze

Cecca F, Pochettino M (2000) The Early Kimmeridgian genus Metas-treblites Oloriz, 1978 (Ammonoidea, Oppeliidae) from RoccaDrago (western Sicily, Italy). Homeomorphy and iterative evolu-tion within the subfamily Streblitinae. Geobios 33:97–104.doi:10.1016/S0016-6995(00)80152-7

Cecca F, Cresta S, Pallini G, Santantonio M (1990) Il Giurassico diMonte Nerone (Appennino Marchigiano, Italia centrale): biostra-tigraWa, litostratigraWa ed evoluzione paleogeograWca. In: PalliniG, Cecca F, Cresta S, Santantonio M (eds) Atti del II ConvegnoInternazionale “Fossili, Evoluzione, Ambiente”, pp 63–139

Channel JET, Oldow J, Catalano R, D’Argenio B (1990) Paleomagnet-ically determined rotations in the Western Sicilian fold and thrustbelt. Tectonics 9:641–660. doi:10.1029/TC009i004p00641

Christ HA (1958) Eine Ammoniten-Mischfauna des Oberen Jura vonWest-Sizilien. Eclogae Geol Helv 51:394–401

Christ HA (1960) Beitäge zur Stratigraphie und Paläontologie desMalm von Westsizilien. Schweiz Palaeont Abh 77:1–141

Davis GH, Reynolds SJ (1996) Structural geology. John Wiley & Sons,New York. Di Stefano P, Senowbari-Daryan B (1985) UpperTriassic dasycladales (Green algae) from the Palermo mountains(Sicily, Italy). Geol Rom 24:189–218

Di Stefano P, Mindszenty A (2000) Fe-Mn encrusted “Kamenitza” andassociated features in the Jurassic of Monte Kumeta (Sicily): sub-aerial and/or submarine dissolution? Sediment Geol 132:37–68.doi:10.1016/S0037-0738(99)00128-1

Di Stefano P, Gullo M, Senowbari-Daryan B (1990) The upper Trias-sic reef of Monte Genuardo (Southwestern Sicily). Boll Soc GeolItal 109:103–114

Di Stefano P, Galacz A, Mallarino G, Mindszenty A, Vöros A (2002a)Birth and early evolution of a Jurassic escarpment: MonteKumeta, Western Sicily. Facies 46:273–298. doi:10.1007/BF02668084

Di Stefano P, Galacz A, Mallarino G, Mindszenty A, Vöros A (2002b)Stop 14 birth and early evolution of a Jurassic submarine escarp-ment at Monte Kumeta. In: Santantonio M (ed) 6° Internationalsymposium on the Jurassic system. General Field Trip Guide-book, Palermo, pp 102–110

Eberli G (1987) Carbonate turbidite sequences deposited in rift basinof the Jurassic Tethys ocean as recorded in the Allgäu Formationof the Austroalpine Nappes of Graubünden (Switzerland). Eclo-gae Geol Helv 81:175–214

Eberli G (1988) The evolution of the southern continental margin ofthe Jurassic Tethys ocean (eastern Alps, Switzerland). Sedimen-tology 34:363–388. doi:10.1111/j.1365-3091.1987.tb00576.x

Elmi S (1977) Polarité tectono-sédimentaire pendant l’eVritement desmarges septentrionales du Bati Africain au cours du Mésozoique(Maghreb). Ann Soc Geol Nord 97:315–323

Farinacci A (1967) La serie Giurassico-Neocomiana di Monte Lacero-ne (Sabina). Nuove vedute sull’interpretazione paleogeograWcadelle aree di facies umbro-marchigiana. Geol Rom 6:421–480

Foresi LM, Bonomo S, Caruso A, Di Stefano E, Salvatorini G, Sprov-ieri R (2002) Calcareous plankton biostratigraphy (foraminiferaand nannofossils) of the uppermost Langhian-lower Serravallian

123

Page 20

134 Facies (2009) 55:115–135

Ras-Il Pellegrin section (Malta). In: Iaccarino S (ed) Integratedstratigraphy and palaeoceanography of the Mediterranean MiddleMiocene. Riv Ital Paleont Strat 108:195–210

Fornaciari E, Di Stefano A, Rio D, Negri A (1996) Middle Miocenequantitative calcareous nannofossil biostratigraphy in the Medi-terranean region. Micropaleontology 42:37–63. doi:10.2307/1485982

Galàcz A (1988) Tectonical control sedimentation in the Jurassic of theBakony Mountains (Transdanubian Central Range, Hungary):palaeogeographic implications. Acta Geol Hung 31:313–328

Galàcz A, Horvàth F, Vöros A (1985) Sedimentary and tectonic evolu-tion of the Bakony Mountains (Transdanubian Central Range,Hungary): palaeogeographic implications. Acta Geol Hung28:85–100

Gemmellaro GG (1872–1882) Sopra alcune faune giuresi e liassichedella Sicilia. Atti Accad Lincei 12:451–472

Gemmellaro GG (1878) Sui fossili del calcare cristallino delle Monta-gne del Casale e di Bellolampo nella Provincia di Palermo. Paler-mo, pp1872–1882

Ghisetti F, Vezzani L (1984) Thin-skinned deformations of the West-ern Sicily thrust belt and relationships with crustal shortening:Mesostructural data on the Mt. Kumeta-Alcantara fault zone andrelated structures. Boll Soc Geol Ital 103:129–157

Giunta G, Liguori V (1975) Considerazioni sul signiWcato ambientalee sul ruolo paleotettonico della Rocca Busambra (Sicilia). BollSoc Nat Napoli 84:45–49

Gugenberg O (1936) I cefalopodi del Lias Inferiore della Montagna delCasale in provincia di Palermo (Sicilia). Palaeontogr Ital 37:135–213

Gullo M, Vitale FP (1986) The “Megabreccia event” in the Upper Cre-taceous-Eocene “Scaglia” of Western Sicily. Rend Soc Geol Ital9:195–202

Hurst JM, Surlyk F (1984) Tectonic control of Silurian carbonate-shelfmargin morphology and facies, North Greenland. AAPG Bull97:305–323

Iaccarino S (1985) Mediterranean Miocene and Pliocene planktonicforaminifera. In: Bolli H M, Saunders JB, Perch-Nielsen K (eds)Plankton Stratigraphy 1, Cambridge University Press, pp 283–314

Jacquin T, De Graciansky PC (1998) Major transgressive/regressivecycles: The stratigraphic signature of European basin develop-ment. In: De Graciansky PC, Hardenbol J, Jacquin T, Vail PR(eds) Mesozoic and Cenozoic sequence stratigraphy of Europeanbasins. SEPM Spec Publ 60:15–30

Jadoul F, Galli MT, Calabrese L, Gnaccolini M (2005) Stratigraphy ofRhaetian to lower Sinemurian carbonate platforms in westernLombardy (southern Alps, Italy): palaeogeographic implications.Riv Ital Paleontol Stratigr 111:285–303

Jenkyns HC (1970a) Growth and disintegration of a carbonate plat-form. Neues Jb Geol Paläont Mh 6:325–344

Jenkyns HC (1970b) The Jurassic of Western Sicily. In: Geology andHistory of Sicily. Petr Expl Soc Libya, pp 245–254

Jenkyns HC (1970c) Fossil manganese nodules from the west SicilianJurassic. Eclogae Geol Helv 63:741–774

Jenkyns HC (1971) The genesis of condensed sequences in the Teth-yan Jurassic. Lethaia 4:327–352. doi:10.1111/j.1502-3931.1971.tb01928.x

Jenkyns HC (1980) Tethys: past and present. Proc Geol Assoc 91:107–118

Longhitano S, Montanari L, Punturo R (1995) Tematiche genetiche suiWloni nettuniani della Rocca Busambra (Sicilia occidentale). BollAcc Gioenia Sci Nat 28:113–145

Marchegiani L, Bertotti G, Cello G, Deiana G, Mazzoli S, Tondi E(1999) Pre-orogenic tectonics in the Umbria-Marche sector of theAfro-Adriatic continental margin. Tectonophysics 315:123–143.doi:10.1016/S0040-1951(99)00277-2

Martire L, Bertok C (2002) Stop 9 Rocca Busambra: the Jurassic mar-gin of a platform and its Cretaceous evolution. In: Santantonio M(ed) 6th international symposium on the Jurassic system. GeneralField Trip Guidebook, Palermo, pp 189–195

Martire L, Montagnino D (2002) Stop 10 Rocca Argenteria: a complexnetwork of Jurassic to Miocene neptunian dykes. In: SantantonioM (ed) 6th international symposium on the Jurassic system. Gen-eral Field Trip Guidebook, Palermo, pp 87–91

Martire L, Pavia G, Pochettino M, Cecca F (1998) StratigraWa dellasuccessione in facies trapanese. In: Agate M, Basilone L, Cata-lano R, Franchino A, Merlini S, Sulli A (1998) Ipotesi sulla con-dizione strutturale della Rocca Busambra. Guida alle escursioni,vol. 1, La Sicilia occidentale, 79° Congresso della Società Geo-logica Italiana, Palermo, pp 74–76

Martire L, Pavia G, Pochettino M, Cecca F (2000) The middle-upperJurassic of Montagna Grande: age, facies and depositional geom-etries. Mem Soc Geol Ital 55:219–225

Martire L, Bertok C, Pavia G, Sarti C (2002) Stop 11 Rocca Drago:Mesozoic pelagic sedimentation over the faulted margin of a pe-lagic platform. In: Santantonio M (ed) 6th international sympo-sium on the Jurassic system. General Field Trip Guidebook,Palermo, pp 91–96

Mascle G (1973) Geologie sur la structure de Rocca Busambra (Sicileoccidentale): mise en èvidence d’une tectonique antècènomani-enne. C R Acad Sci Paris 276:265–267

Mascle G (1979) Etude geologique des Monts Sicani. Riv Ital Paleon-tol Stratigr Mem 16:431

Mullins HT, Hine AC (1989) Scalloped bank margins: beginning of theend for carbonate platforms? Geology 17:30–33. doi:10.1130/0091-7613(1989)017<0030:SBMBOT>2.3.CO;2

Mullins HT, Gardulski AF, Hine AC (1986) Catastrophic collapse ofthe west Florida carbonate platform margin. Geology 14:167–170. doi:10.1130/0091-7613(1986)14<167:CCOTWF>2.0.CO;2

Oldow JS, Channel JET, Catalano R, D’Argenio B (1990) Contempo-raneous thrusting and large-scale rotations in the Western Sicilianfold and thrust belt. Tectonics 9:661–681. doi:10.1029/TC009i004p00661

Patacca E, Scandone P, Giunta G, Liguori V (1979) Mesozoic paleo-tectonic evolution of the Ragusa zone (Southeastern Sicily). GeolRom 18:331–369

Perch-Nielsen K (1985) Cenozoic calcareous nannofossils. In: BolliHM, Sanders JB, Perch-Nielsen K (eds) Plankton stratigraphy.Cambridge University Press, pp 427–554

Santantonio M (1993) Facies associations and evolution of pelagic car-bonate platform/basin systems: examples from the Italian Juras-sic. Sedimentology 40:1039–1067. doi:10.1111/j.1365-3091.1993.tb01379.x

Santantonio M (1994) Pelagic carbonate platforms in the geologicrecord: their classiWcation, and sedimentary and paleotectonicevolution. AAPG Bull 78:122–141

Santantonio M (2002) 6th International Symposium on the JurassicSystem. General Field Trip Guidebook, Palermo, Italy, pp 219

Senowbari-Daryan B (1980) Neue Kalkschwämme (Sphinctozoen) ausobertriadischen RiVkalken von Sizilien. Mitt Ges Geol Bergbau-stud Österr 26:179–203

Senowbari-Daryan B, Schäfer P, Abate B (1982) Upper Triassic reefsand reef biota in Sicily. Facies 6:165–184. doi:10.1007/BF02536684

Spence GH, Tucker ME (1997) Genesis of limestone megabrecciasand their signiWcance in carbonate sequence stratigraphy models:a review. Sediment Geol 112:163–193. doi:10.1016/S0037-0738(97)00036-5

Sprovieri R, Di Stefano E, Sprovieri M (1996) High resolution chro-nology for Late Miocene Mediterranean stratigraphic events. RivItal Paleont Strat 102:77–104

123

Page 21

Facies (2009) 55:115–135 135

Sprovieri R, Bonomo S, Caruso A, Di Stefano A, Di Stefano E, ForesiML et al (2002) An integrated calcareous plankton biostrati-graphic scheme and biochronology for the Mediterranean middleMiocene. Riv Ital Paleont Strat 108:337–353

Tamajo E (1960) Microfacies mesozoiche della Montagna della Bu-sambra. Riv Min Sic 63:131–151

Wendt J (1963) Stratigraphisch-paläontologische Untersuchungen imDogger Westsiziliens. Boll Soc Geol Paleontol Ital 2:57–145

Wendt J (1965) Synsedimentäire Bruchtektonik im Jura Westsiziliens.N Jb Geol Paläontol Mh 5:286–311

Wendt J (1969) Die stratigraphisch-paläogeographische Entwicklungdes Jura in Westsizilien. Geol Rundsch 58:735–755. doi:10.1007/BF01820731

Wendt J (1971) Genese and Fauna submariner sedimentäarer Spaltenfüll-ungen im mediterranen Jura. Palaeontographica A136:122–192

Wilson MEJ, Bosence D, Limbong A (2000) Tertiary syntectonic car-bonate platform development in Indonesia. Sedimentology47:395–419. doi:10.1046/j.1365-3091.2000.00299.x

Winterer EL, Sarti M (1994) Neptunian dykes and associated featuresin southern Spain: mechanisms of formation and tectonic implica-tion. Sedimentology 41:1109–1132. doi:10.1111/j.1365-3091.1994.tb01444.x

Winterer EL, Metzler CV, Sarti M (1991) Neptunian dykes and asso-ciated breccias (Southern Alps, Italy and Switzerland): role ofgravity sliding in open and closed systems. Sedimentology38:381–404. doi:10.1111/j.1365-3091.1991.tb00358.x

123