sicilian jurassic physiography and geologic realms

Rilista It:rli:rna di Paleontologi;r e Str;rtigrafi;r
volunre I l0
no.
I
YY' '"
--
April 2001
SICILIAN JURASSIC PHYSIOGRAPHY AND GEOLOGIC REALMS (ITALY)
BENEDETTO ABATE', GIOVANNA LO CICERO & LORIS MONTANARI'
Rcc-cit'cd Ocrober -i0, 2002: dcceptcd
Ke1'
-t
or d s :
S ici
ll
J u
rls
si
c, pll;reo geo graph
Not'enber 1, 200.)
Arnnronitico" l.s); -rrdiolariti ed argilliti.
Nel Lias infcriore e mecìio i due domini erano suddivisibili nel
cluc rrsscgnebili ;rl "Rosso
r'.
Abstr"ttt. Tuo tc'ctono-sr'dinrent;rn' dorurins, uhich wcrc clc-
lntl perhaps origin,rllv to Plleozoic clcposits, ch:rracterize the fornrer.
The l;ìtter belongs to the Europe rrn "C.rlabrian Arc", ri'here the Jurlssic
tr.rnsgressivelr' r'ests ()n ;1 continental substr;rte (i.c. thc crvstallinc V;r-
Maghrcbidc secondo pi;rtt;rforme c b,rcini interdigiteti ereditati del Tri;rs
e nel Pcloriteno secondo piattrforme e rrmpe ciirbonrtiche circondanti
b.rcini pr,rlr.rbìlrncntc ronrboc:rsnrici.
Ol'unque, trirÍìne rilre eccezioni, le pìattlfornre subirono il noto
anneg;uìrento giurassico, con tendcnziale ;rnticipo ll Donrertano superiorc nel Pcloriteno e uno piir nlrrcìto e diffuso;rl To;rrciano nel Maghrebiclc. Solo in quest'ultinro furono rrttivi vulcani sottorn.rrini tuc-
risc;rn b;rscnrcnt),
diogi
fornrccl during tlre Ncogene ,rnd cvolved into t\'o liìr{c structur.rl scctors, ch,rr;rcteriz-c the Sicilian Jurlssic: thc Maghrebidcs rrnd Pclorit;rni. Afric;r nr;rrgin scrlinrcnts, p;rssinI clos'nrvrrcl to Tr-i.rssic succcssìorts
These donrlins
lre chrrlctcrizcd bv four
shlllou pl,rtfornr-dcrivcd limcstoncs; conde nse cl se,rn.tount-n pe recl
lirrrcstoncs; nodullr linrestones uith ;rnrnronitcsl rlccp radiol;rrites ;rncl
shalcs. These iacics;rre illusrratcd in,r dozen oî str.rrigr,rphic logs.
The droii'ning oi nrost Tr-iassic-l.iassic c;ìl'bonrte pl;rtfornrs
or rrn'ìps and the
dccpc'nirrg
of
irclj;rcc'nt brsirrs c,rmc
with infcrred
Jur;rssic strike-slipr tectonics, connccted to the rclrrtivc ntovenrc-nt of
Alrica (Gondrvanian p;rrt) r's. Europe (l-iìurxsiiìn p;rrt); the slnrc strikeslip tectonics mav hllc c;ìused scrttercd inrr;rpl;rtc r'olclnrc sc;.rÌl()unts
found in Meghrebitle s.
During the Jurassic the M;rghrebide rcalnr \\,irs chirrîctcrizcd bv
the intcrfingering of besins lnd c,rrbonate platforms. During the Earh' and Middle l-i;rssic, c;rrbonate plrtforn-rs ancl rlnrps s,ere donrin;rnt.
Since T<rlrcìrrn cither raciiol,rrites irr sonre b;rsins or Anrnronite-belring
calcareous n.ruds developed *'ith intcrvening basaltic florvs, :rnd u'erc
;rcconrplnied by conderrscd pelagic clrbonates on thc cnsi;rlic seanrour.rttvpe highs.
The Peloritani realnr displar.s sinrilar ch;rr;rcteristics, but l'ith
later trrnsgression on the basenrent, sever;rl strikc-slip basins lncl without lnt,r'olclnocs.
Il Ciurassico sìcililno si riscontrl in
clue donrìni strutdal Miocene seconclo due catene or,r
s,ild.rte: il Maghrebide e il Pelorit;rno (Ììig. 1). Il prinro ò form:rto ch scdinrcnti rrlrini di nrargine gondu'ani;rno-,rfricano, in continuità dcposizionllc llnreno del Trils; ìl secondo c\ iornrato da sedinrenti di nrrrrgine
laurlsilno-europc'o trrsgressivi, sul brrslnrento r';rrisico e l.r sul sottile
copcrturî contincntllc trilssico-in[r,rlirssicrr, sokr nel I-irs infcriore.
I sedimenti giur:rssici di anrbedue iclomini sono cspressi dl t1u:rttro tipologie litologiche e in una doz-zina di lor: stntìgla[ici emblenr;rtici:
-c;rlcari neritici di pitrttafornra e di r;rrp;r clrbonltica; -c.rlcari rossi di sedinrenurz-ione pelagica condens;rtr.rì -c;rlc;rri nodul;rri los;rti (questi ultirli
Rittssunto.
turlli dciorm;rtisi plicltivamente
u
rass
ici.
scclinrent.rrv f;rcies:
Introduction
A palaeoueographic restoration of two Jurassic
crustxl sectors, each other frontal to the boundaries of
the suggested oceanic domain of the Alpine-Tethys with
the southern Neotethys one (cf. Stampfli et al. 2002), is
here offered. The southern crustal sector is supposed to
belong to Gondwana, from which the Maghrebide Chain
originated. The northern sector is instead attributed to
Laurasia, from which the materials of one or more nricrocontinents derived. The latter, eventually assembled in the
Miocene, is here considered to form the Calabrian Arc,
whose Sicilian part is the Peloritani region. This region is
here rrssumed as an exotic "terrane" (Fig. 1).
For the two Sicilian sectors, characterized by a fold
-and - thrust style, a palinspastic reconstruction is proposed, not strictly takine into account their present position (as sussested by Castany 1.956; Zappaterrc 1994,
amons the others), but considering, on the whole, the
amount of shortening occurred. The sedimentary characters of them have been individuated on the basis of the
research on the Sicilian Jurassic carried out since mid XIX
century: namely the palaeontological and geological studies of G.G. Gemmellaro (Mid XIX century); Di Stefano
G. (18S7); DiStefano & Cortese (1891); Fucini (1921);
Dipartim. Geologir e Geociesir Università di Prrlernro, r: Archirlfi 22, l-9012.3; Tcl.+390916230311. E-nrail: bino(r unipe.it, locicero(a unipa.it.
CP 93 PP TT, vir Roma, 90100 P;rlernro. Tcl. + 39-3+2851659. E-nrril: lorisnron(r hotmeil.it
B. Abatt', G. L,t Cict'r,,
t6
PELORITANI
X L. ,1Ínrttannrt
I;ig.
I
- Structur.tl .chcrrrc of Sicilyl
Us = Ustica Island, Eol :
Eoli;rn Islands, Eg
Ishnds, Et = lltna.
' --'-.')"
=
Egadi
MAGHREBIDES
Maugeri-Patané (1924, 1932); Schmidt-Friedbers et al.
(1960); Ogniben (1960); Wendt (1963,1971).
From the Sixtic's of the last centurv nricropaleor.rtological contributions - initially bv oil industry:rnd Governmental Institutions - and facies an,rlyses (Rigo 8t B:rrbieri 1959; Barbicri 1964; Montanari 1965, 1966) have
been taken into consideration.
Jurassic framework
Our stratigraphic an,rlysis on Iurassic sedinrents
allows to individuate four deposits arssemblaees, correspondinr to sedimentary environments (Fig. 2): neritic
limestones; Cephalopoda-bearinq red condensed pelagites; nodular white to reddish Ammonite-bearing limestones ("Rosso Amnronitico" or R.A. ruct.); argillites
and radiolarites.
Betrveen the neritic limestones and the others, allodapic sediments may be found. Further paleoenvironmental inforn.ration came from neptunian dykes (Vendt 1965)
and fronr coeval hardgrounds (Jenkins 1970;Jenkins et al.
2002). All these lithofacies characterize several sedimen-
tary "facies-domains" (Fig. 3). The first lithofacies pertains to carbonate platforms or r:Ìmps, which started to
srorv since the Late Triassic; their age extends from Early
to Middle Liassic and sometimes up to Late Jurassic.
The depositional sites changed their characteristics in time. Till the Middle Liassic the platforms were
elevated compared to the adjacent hemipelagic basins.
Since the Late Pliensbachian (spinatum Zone) rn the Pe-
loritani domain and since the Early Toarcian falciferum
Zone) in the Maghrebian domain, almost all of them
drowned, becoming sites for pelagic red Ammonitebe:rring condensed limestones. The basins, which were
adj;'rcent to the platforms, are characterized by either
Irig.
2 - Iìour mlin Jurassic lithofacics
:rssociations.
Note pletforms
,rnd selnrount-tYpe structures
sith
condensed Middle Lias-
sic "Rosso Anrmonitico" s.l.
(R.A.) crossecì by neptuntan
dvkes. Black lines for inferred
bottortt currents; s.c.d.: s.rtur;rtion compensation depth.
S
M
G
H
ic i lian J wra
ss
i
c p hy
si
ograp by
17
Fig.
D
E
3 - Schematic stratigraphic columns of the Jurassic facies
domains. PP-TU = Prepanormide-Tunisian; PA : Panormide; IM = Imerese; VR
= Vicarese; SC = Sicanian,
TP-SA = Trapanese-Saccense;
NV = Novrra Sicula; AL :
Alì; TA = Taormina; GA =
Galati; LG = Longi.
NV
RITA
TA
AL
:]-.1ì.
I[--]
rt
GA
I
-.,,:,.',.
Ir-r""-=
-l
rt___l
|;Ir-=,1
Fe
aq Po-
t ^ ",!
'1
I
LG
nodular holopelagic limestones or hemipelagic radiolarites and argillites.
This paleoenvironmental mosaic was included
in different paleogeographic frames by some Authors
(Scandone et al. 1977; Catalano & D'Argenio 1.978;
1982; Montanart 1.989,2000; Abate er al. 1993, 1997,
2002;Yai 1992)
The sedimentological difference between the
Maghrebian and the Peloritanian domains decreased in
the Late Jurassic times (Calpionella-bearins limestones
in drowned zones) even though exceptions may be found
in the Panormide domain (Ellipsactinia-bearing deposits)
and in Peloritani ("Novara succession" wirh Clypeina jurassica-bearing carbonates). Since the Late Triassic large
amounts of allodapic and intrabasinal breccias deposited
in the basins. In many Maghrebian sectors (Fig. 3) pillow-lavas also occurred, suggesting an incipient rift, later aborted.
Structures and paleophysiographic analysis
It
is necessary to distinguish autochthonous and
allochthonous Jurassic rocks, either in deformed or undeformed sites. The structural position needs to be verified, to discriminate whether the rocks are true tectonic
Klippen or if are resedimented exotic materials. For instance, Jurassic neritic rocks from Vicari, Roccapalumba,
Pietrecadute in 'ùlestern Sicily are remains of a Nappe
overthrusting the Sicanian thrusts. Instead, in the Sicanian
sequence, the megabreccia-swarms with Liassic white neritic limestones embedded in the white Cretaceous "Scaglia" (e.g. Adranone, near Sciacca and in the same Sica-
mi';::,'::í,!,,"*""
Za
:ilii,iiiì1 i;#ilii1it,,,,"
/,.rir).,lr,yk r,:{l//i['sù
I
LoiltinLiltnl ìt
f --;'l
b a_ s-l rrl,rrrrir
A
rtltntil
srbftili,k'ro/.n,itts
nian basin) are resedimented. Same resedimentation of
Jurassic rocks in siliciclastic Miocene flysch occurs by
Case Tita near Mistretta.
In the Peioritani, near Rocca Novara and Forza
d'Agrò, Tithonian white clasts were resedimented as a
breccia-like in the Oligocene varicoloured marls; many
blocks of condensed Rosso Ammonitico are included in
the "Scaglia" as well as in Miocene siliciclastic turbidites,
suggesting a repeated mass slide.
Here we deal with the Jurassic domains, from the
"internal" to "external" ones, according to the modern
structural organisation of the deformed rock assemblages in a "cylindristic" framework of south-verging overthrusts, with a moderate transversal strike-slip tectonics.
Maghrebides
a) Prepanormide (PP)-Aegusean Tunisian (TU
eg.) ('Aegusean" from the ancient Greek generic Aegusae for Egadi islands). The name is an informal compromise. "Prepanormide" was born as a nomen nudum
(Catalano & D'Argenio 1982) suggesting another pale-
odomain between an internal realm (probably the "oceanic" Sicilide of Ogniben 1960) and an external Maghrebian-Trapanese realm.
Its stratigraphy was later considered analogous to
that of the Tunisian realm (Catalano 1,987). One of
us
(Montanari 1989) suggested therefore to change "Prepanormide" into "Tunisian", because of:
- the new opinions and data about the belonging
of such domain to North-Africa, as Fabiani Ec Trevisan
(1940) and Ruggieri (1973) had already suggested;
- stratigraphic differences from the "true" Panormide:
lJ. Abatc. G.
18
L,' Cict'ro 3; L. .llotttnttari
- the unclear use of the ternr "Panornride", l.hich
may induce confusion about its structural position. .rgc
ilnd stratisraphy. AGIP staff (Antonelli et al. 1988) used
this nerv nomencl;lture reearding " Tunisi,rn".
Montanari (2000) divided "Tunisian" in tu'o p:rrts:
the Aegusean (Egadi Isls. and Adventure Bank), ,rnd thc
Pelagian (the southernmost Me dite rraneirrr z-onc), ou,ing
to sonlc differences in stratigrlphic evolution (;rt lc:rst
since the till now knorvn Malrrr). The Aesuseirn lacks of
Jurassic volcanoes, which are instead present in its C:rrnian and Upper Cretaceous successions. Iirorr Lrrte Triassic to Early Liassic this donr:rin not changccl its calc,rrcous-dolon.ritic rocks, rvhile durins the l:rtcst Dorle ri;rn it
passed to a new cycle with radiolaritic t:narlv C.r/t.tL).u'iL1bearins lir.nestones (Falcone Mb. in Abate ct al. 1999) ancl
prosecLrtes in sinrilar conditior.rs for the entire Jur:rssic.
Instead, the Pelagian during the Malnr (decpest
layers reached by con-rnrercial drills) orvns dolorritiz-ed
limestones.
b) Panormide. This donririn shou,s ,r n.rrrxinrur.r.r cxtent of neritic conditions sincc the Carniln (Serrorvb;rrvDarian & Abate 1986). Its drowning took plirce fronr thc
Toarcian to Middle Mirlm (production of condensed rcddish limestone), then it returned to neritic conditiorrs,
shedding r.naterial into the adjacent basin,rl lrrerese do-
nrain, fror.r.r the Late Triassic (Fanusi Fnr.) to thc CretirceoLls :rt least (Crisanti Fnr.). Also this dom;rir.r lircks
subnrrrrine eruptions durin g Jr"rrassic.
c) Vicarese (Montanari 2000). This donrrin
hirs
some affinities with the Trirpanese rnd Prnormide ones.
Its nrirtcrials arc for.rnd at tast, near the Mistretttr's ncigh-
borhood (bv Casc Tita). In thc Middlc Jurassic it is charaterizecl by neritic lir.rrestoncs wirh Protopeneroplis stridtd
(C'rflisch & Crescenti 1969) ;rnd by r,olc,inic tuffs irr the
Birjocirn (Fabiani E: Ruiz 1933).Its Triirssic crrboniltc material g,rve origin to n.regirbrcccias :rs irt its nr:rrgin during
Eirrlv l-i,rssic (M. Ge'nuardo succession) ,rnd ,rs, during the
Uppcr Cretaceous, into thc irdjircent ori{Ìin,rl Sic:rni basin:rl donrlin, rvhcre the pcllgic Jurassic clrbon:rte rcsedinrenrs irre ah.r.rosr lrrckine (Di Stefano et ,rl. 1996; 2AA4.
d) Trapanese. It is ,r rvell knowrr donrain, rich in
Jurirssic :'rr.nnronites. To thc south, it extends into "Saccensc" prosecution, encircling henripelagic In.rerese and
Sicrrniar.r enrblvrncnts. Its l-orvcr and Micldle Li;rssic plirt-
fornr-c:rrbon:rtic sedinrent (lnici Fm.) follorved Triirssic
conclitions. In thc Toarrcian it dro$'ned ,rnd was occupied
both by condensed pelauic Rosso Ar.unronitico linrestones
on scanlount-tt'pe highs (M. Grande, Inici, M:rrrrnfusa,
Kurret:r, Busanrbr;r Mts e.g.) and adj,rcent nodular lisht
/{lt
V,
/
, tt I
.,t
f ,{ .\
,n1
-t
lìie.
.l
Ctlncepttt;rlphvsiolraphicnloclclforrhcMaghrcbidc
inht'rited frorr the L;rte I-irrssic:
MirrcttiÌìlo Isl. zonct IlVl : Inrcrcsc b.rsin; SC : Sic.rni.rn b.rsin; \rR = Vicrrese highl TP = Trrrp.rncse; SA
=Streppctltlslrrestrictetlb.rsin;PI,.TUeg.=Preplrntlrtlritle.lcguse.lnTunis;i1niTUpg:pel.tgi.tn
volc;rnocsi strikc-slip lìlovcrìlcnts lrc indicrrtccl Lrv h;rl i-.rrrorvs.
:
Sirccensr subdonr.rin: ST
Sici
lian
Ammonite-bearing sediments. Submarine volcanic
J urass
n-rate-
rials are here present in Jurassic tin.re.
e) Imerese and Sicanian hemipela*ic radiolaritic
basìns formed embayments within the Prepanonnide-Tunisian and Trapanese domains. Probably, the Imerese and
Sicanian basins were crossed by the Vicarese high, to meet
towards the Apenninic Lasonesro basin. The Imerese received allodapic n-raterials from the Panormide platform
durine the Late tiassic- Paleogene interval; the Sicanian
one received similar material from the Vicarese durins
the Early Liassic and in the Late Cretaceous times. The
Imerese has more expanded radiolarites than the Sicanian one. Submarine volcanic rocks are present in both the
don.rains during Late Triassic and Jurassic times.
ic phy s i ograp by
19
rin.rmins the basins of Early Jurassic age drowned since
Late Don-rerian, leaving scattered seamount-type structures with condensed Rosso Ammonitico. In the basins
coeval cherty limestones deposited (Carcione et al. 2003).
Only in the "Novara" succession a sporadic episode of Upper Malm neritic Clypeina-bearing shallow water sediment
occurred. In any case, Peloritani lack of Jurassic volcanism.
Sicilides
The separation of Peloritani from Maghrebides is
controversial.
It is supposed from literature that during Late
Jurassic an oceanic trench separated Maghrebides from
Peloritani, where varicoloured marls and shales ('Argille
Sicilidi" auct.) developed.
The Sicilide domain (Ogniben 1960) shows deep
f) The Hyblaean domain corresponds to the present lightly-deforn.red Foreland in the SE corner of the
Island. Only oil wells have reached the Jurassic. Some
pelagic sediments with a significant shale component. The
most ancient deposits have been identified at the JurassicCretaceous boundary and consist of red shales with small
normal pelagic sediments alternate seamount-type condensed ammonitic limestones. Fron-r the cornmercial point
of view, the greatest interest is in black-shales (Streppenosa Fm.), whose age extends fron.r Late Triassic to Early
Liassic (Frixia et al.2000 and ref. herein). VolcanicJurassic materials occur in this domain.
layers of Calpionella-bearing white micrite, foliowed by
reddish and greenish shales with breccia lenses including
Tintinnides and then "varicoloured marls" reaching the
Early Langhian (Caire 1970; Lentini et al. 1987). The compositional affinity to the Apenninic "argille a palombini"
is noteworthy, but in SicilyJurassic basalts and ophiolithes
from this internal domain lack, or are unknown.
Peloritani
A thin continental or paralic infraliasic deposits
('Arenaria di Longi" or "Verrucano" Auct.) occurred on
the Variscan basement. The n.rost interesting outcrops with
good stratigraphic columns are found in the Taormina,
Galati and Longi neighborhood. Here carbonate ramps
PAN
";ilh
e
Fig.
5 - Conceptual
Discussion and conclusions
Fig. 3 shows that two different depositional events
occurred in the Jurassic.
B
L
Eo
SR
a
phvsìographic r.nodel for the Maghrebian realm ìn the Middle Jurassic. Several platforn.rs drowned and sor.ne parts became
se;lmount-tvpe structures with condensed pelauic Rosso Anrnronìtico Iimestones. FA : Mt. Falcone zone irt Marettimo; TJ = ppnlt
Troja basìn rt Marettimo; MG : Mt. Gello; MP = Mt. Pellegrino; MD : Madonìe Mts.; GI : Mt. Grande and Mt. Inici area; K{J :
Mt. Kumeta; BS : Roccir Busanrbra; MIr : M:rranfuse; NI = Nilde well zone; SA : Sciacca; SR : Syracuse; RG : Ragusa. Half-arron,s for strike-slip nlovenlcnts. During the Miocene the Trlpanese approached the Saccense zone becî".. ^f " ,1.". 'h"".r
B. Abatc, G. Lo Cicero
2A
Fig.
k
L. Montanarì
phvsiographic rrrodel for thc Errlv Liassic in the Pcloritrni's .rrcr: LG : I-oniìi brsin; GA, SMA, FZ, SÌ TA, GD, SA =
G;rlari, S. Marco d'Alunzio, Frazzrnò, S. Pietro, T,rornrin.r, Galkrcloro, S. Andrea carbonate platforms or rrìmps; AL: Alì gvpsiferous
and carbonlric shclf; F-M : Fondache'lli-M:rnclrlzzi-Mlnd;rnici zone; ASP = Asprorronte zonc; NV = Rocca Novara zone. (modif.
frtrnr C.rrcione cr.rl. lOOl).
6 - Conccpturl
- In Maghrebides, until the Middle
Lias, the Triwith the presence of carbonate
scale, and deep volcanism suggest a moderate structural
platforms, ramps and relative sediments. Few enrersions
occurred (one of these took place in the Panorr.nide, at
Mt. Gallo, with bauxites occupying the Early Lias-Early
Malm interval (Di Stefano 2002)).
- In the Peloritani, both the transgression over the
basement and its continental-Triassic cover occurred later
(Lower Liassic). The correspondence between these two
zones concerning Lower Liassic sedinrentation was later
reversed during two different times: at first the drowning
took place by the Peloritan sector during Late Dornerian, then during the Toarcian in the Maghrebian one. The
Updated general models for the Gondwana-Laurasia boundary during the Jurassic, which includes the two
Sicilian realms (Stampfli & Mosar 1999; Stampfli et al.
20A4, as well as of some Authors (Muttoni et al. 2000)
ones for the Gondwana sector, show widespread strikeslip tectonics. This latter one, foreseen by Catalano &
assic structure persisted
latter occurred when the mainly carbonate sedin-rentation ;rlternated with the radiolaritic-areillitic one. The
few affinities between the two depositional areas are in
the sporadic neritic occurrence at the top of the Jurassic
(E llip sactin ia-bearin s lin.restones in the Pan orrnide, C/7peina-bearrng lin.restones in the Novarese) and in the radiolarites both by the In.rerese, Sicanian (Maghrebides) and
by the Alì (Peloritani) sequence. This resembles parental
relationships with the Sicilide rift, which was interposed
between Peloritani and Machrebides in the Jurassic-Cretaceous times.
Sin.rultaneous distinct phvsiographic siturrtions
with different depositional typology, even to a small
dynamics.
D'Argenio (1982), may fustify the contemporaneous
presence of adjacent structural ups and downs (pushups and rhombocasn-rs), even if of reduced dinrensions.
On the base of these considerations and data, and
on the base of the mutual position of domains which
were deformed during Miocene (..g. by Catalano et al.
2000 for the Maghrebides; Lentini et al. 2000; Carcione
et al. 2003 for Peloritani) we can suggest four conceptual physiographic models, for the Early Liassic (time
of carbonate platforms) or the Middle Jurassic (time of
their drowning)
.
As for M:rghrebides, excluding the Jurassic Sicilide,
the first time mav indicate platforms and half-encircled
basins (Fig. 4), u'here the Hyblaean euxinic basin of the
Streppenosa Fn-r. suggests a potential indipendence of
Maghrebides from Apulia.
At the second time (Fig. 5) the development of
transcurrent structures owing to strike-siip tectonics
Sici
Fie.
li an J u rass ic pby
si
2l
ogr.lph)t
7 - Mìddle & Late M;rlnr phvsiographv in the Peloritani rre;r. Grev for sc,rrlount-tl/pc structures l'ith condenscd Rosso Anrmonitico. SIC
: Sicilide trench; other svmbols lnd letters see prer,ious figures. (nrodif. froÌl Ciircione et al.2OO3). Dr,rring thc Miocene northern and
\\/estern sectors irpprorìched the southern Ones bcc,rusc of scl'er:ll thrusts.
may show both transpressive seanlount-like highs with
condensed carbonate pelagic sedin.rentation and transtensive basins, these last ones with both pelagìc normal
An.rn.ronitico Rosso, deeper radiolarites, and submersed
volcanoes.
As for Peloritani, the Liassic occurrences susgest
rimn.ring carbonate platforms (Fig. 6), whereas in the
Middle Jurassic these drowned and produced condensed
pelagic carbonates (Fig. Z).
Acknoo-ledgenents, The authors thank the revie*'ers B.
l)'Argenio, G. Stampfli ;rnd M. Gretani :rs tell irs the iournal editorial
st,rtf for constructive conrments. Financial support is based on MIUR
contribution (ex 60'l. G. Lo Cicero).
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