Tectonophysics, 142 (1987) 217-226

Elsevier Science Publishers B.V., Amsterdam - Printed in The Netherlands

217

The Liguride Complex of Southern Italy -a Cretaceous to Paleogene accretionary wedge

STEVEN D. KNOTT

Department of Earth Sciences, University of Oxford, Parks Road, Oxford OXI 3PR (Great Britain)

(Received March 25, 1986; revised version accepted January 1, 1987)

Abstract

Knott, SD., 1987. The Liguride Complex of Southern Italy-a Cretaceous to Paleogene accretionary wedge.

Tectonophysics, 142: 217-226.

The ophiolite-bearing allochthonous flysch (Liguride Complex) of the Southern Apennines, Italy, has traditionally

been divided into two tectonic units: the metamorphic Frido Unit and the unmetamorphosed Cilento Unit. The two

units have hitherto been considered to derive from two distinct paleogeographic domains; however, the identification of

Cilento Unit sediments within Frido Unit successions implies that the sediments of both units were coeval deposits

within the same sedimentary basin. Cilento Unit sediments also occur as the sedimentary cover of kilometre-scale

oceanic slices within the Liguride Complex indicating deposition on oceanic basement and not continental basement as

was previously considered. Thrust transport directions and sediment provenance indicate that during Late Jurassic time

this ocean basin lay to the east of the Calabrian terrain and to the west of Apulia, Calabria and Apulia representing the

European and African margins of Neotethys respectively. Northwestwards subduction of oceanic crust beneath the

Calabrian terrain from Late Cretaceous time onwards produced an accretionary wedge which was later emplaced onto

the Apulian margin during the Burdigalian collision of Calabria and Apulia. The Liguride Complex represents the

abducted remains of this accretionary wedge.

This interpretation contains three important implications for pre-Tertiary plate tectonic reconstructions of the

western Mediterranean region, these are:

(1) The Calabrian continental terrain formed part of the Iberian Plate on the north margin of Neotethys, this may

have implications for the former location and continuation of the North Pyrenean Fault.

(2) The existence of a continuation of the “Eo-Alpine” belt through Calabria and the Kabylies is placed in doubt

thus requiring only one, constant polarity (NW-dipping) subduction direction to explain the structures now seen in

these regions.

(3) The existence of a transform fault between the Europe-vergent structures of Corsica and the Africa-vergent

structures of Calabria. This transform must have been active from at least Late Cretaceous time in a position now

occupied by the Tyrrhenian Sea.

Introduction

The Calabrian Arc (Fig. l), Southern Italy, can

be divided into three major tectonic elements. The

lowest element consists of thrust sheets of

carbonate sediments, originally deposited upon

the continental margin of Apulia, and now for-

ming the Apennine mountain chain (Scandone,

1979). Tectonically overlying this element is an

ophiolite-bearing allochthonous flysch which, in

the Southern Apennines, is known as the Liguride

Complex (Ogniben, 1969). The upper-most

tectonic element consists of thrust slices of con-

tinental basement with or without a Mesozoic

sedimentary cover.

This sequence of tectonic elements is consid-

ered to be a remnant of the “Eo-Alpine” chain of

European vergence which was later thrust east-

0040-1951/87/$03.50 0 1987 Elsevier Science Publishers B.V.

STROVILLARI

Fig. I. Geologic map of Southern Italy and Sicily.

wards onto the Apennine domain in Late Tertiary time (Alvarez, 1976; Amodio-Morelli et al., 1976). In the most recent synthesis of Calabrian geology (Bonardi et al., 1982) the Liguride Complex was divided into the Frido Unit and the Cilento Unit each unit being derived from a different sedimen- tary basin, the former was situated upon Tethyan oceanic crust on which sedimentation commenced in Early Cretaceous time, the latter was situated upon the Apulian continental margin with deposi- tion commencing in Early Paleogene time.

The aim of this paper is to show that the Liguride Complex, including the Frido Unit and the Cilento Unit, represents the remains of a single ocean basin which originally lay between the Calabrian and Apulian terrains, was deformed by subduction-accretion processes and was finally emplaced onto the Apulian margin during the Neogene. The structure of the paper shall be to review the previous work on the Liguride Com- plex, present new structural and sedimentological data and finally to discuss the implications of this data and their interpretation to plate tectonic re- constructions of the western Mediterranean re- gion.

Liguride Complex

The Liguride Complex has been divided by Amodio-Morelli et al. (1976) into three tectonic units, the Frido Unit, the Cilento Unit and an

ophiolite unit (Fig. 2).

Frido Unit

The Frido Unit includes the Frido Formation of Vezzani (1969) and is roughly equivalent to the “ flysch ar~lloso-filladi~o” of Ippolito and Lucini (1957) the “flysch fillonitico” of Cotecchia (1958) the “ flysch a quartzites” of Caire et al (1960) and also the “argillitico-quartzoso-calcareo” flysch of Selli (1962). This unit is composed of weakly foliated shale, slate, talc-schist and quartz-arenite. In the Southern Apennines the Frido Unit is associated with kilometre-scale masses of con- tinental and oceanic crust. Figure 2 shows the extent of Frido Unit outcrops within the Southern Apennines. The age of the Frido Formation according to Vezzani (1969) is Neocomian to Ap- tian. However, Scandone (in Amodio-Morelli et al., 1976) identified Globotruncana sp. in Frido

Fig. 2. Geologic map of the Southern Apennines including the

region involved in this study. M-Timpa delle Murge,

P -Timpa Pietrasasso, T-Monte Tumbarino.

219

Formation shales from the Cilento area (Fig. 1)

suggesting a Late Cretaceous age.

Vezzani (1969) and Ogniben (1969) state that

the Frido Formation in the Southern Apennines

lies stratigraphically below the Crete Nere Forma-

tion (the oldest formation of the Cilento Unit).

Amodio-Morelli et al. (1976), however, state that

the two are separated tectonically by fragments of

an ophiolite unit and the Polia-Copanello base-

ment unit, and are therefore not in stratigraphic

contact. In the Calabrian Coastal Chain to the

west (Fig. 1) the Frido Unit is situated tectonically

beneath the ophiolitic Malvito, Diamante-Ter-

ranova and Gimigliano Units, and above Apen-

nine carbonate rocks of the Verbicaro and San

Donato Units (Amodio-Morelli et al., 1976).

The metamorphism of the Frido Unit within

the Southern Apennines is considered to be very

low, on the border between greenschist facies

metamorphism and diagenesis (Amodio-Morelli et

al., 1976). However, Lanzafame et al. (1979)

recognise high pressure/low temperature lawso-

nite-albite to incipient glaucophane schist facies

assemblages within this part of the Frido Forma-

tion. The latter authors and De Roever (1972)

distinguish true glaucophane schist facies assemb-

lages within outcrops of the Frido Unit in the

Calabrian Coastal Chain.

Cilento Unit

According to Amodio-Morelli et al. (1976) the

Cilento Unit belongs to a group of allochthonous

units of uncertain paleogeographic position and

lies tectonically above the Frido Unit.

The Cilento Unit comprises three sedimentary

formations. The oldest, the Crete Nere Formation

consists of black shale, quartz-arenite, calcarenite

and calcilutite, of Aptian to Albian age (Vezzani,

1968). The overlying Saraceno Formation consists

of calcarenite and calcilutite with occasional

volcaniclastic sediments of Middle to Late Eocene

age (De Blasio et al., 1978). Unconformably

overlying both these formations is the Albidona

Formation which comprises conglomerate and

quartz-arenite of Late Oligocene to Burdigalian

age (Zuppetta et al., 1984) and contains two

laterally continuous calcilutite beds occasionally

reaching 50 m in thickness. The conglomerates of

the Albidona Formation contain boulders which

have been derived from the Calabrian continental

terrain (Zuppetta et al., op. cit.).

“Ophiolites”

Various interpretations of the relationships be-

tween the tectonic units mentioned above and the

ophiolitic rocks have been suggested within the

literature. Dietrich and Scandone (1972) and

Amodio-Morelli et al. (1976) both consider that

the ophiolites belong to a tectonic unit distinct

from the Frido Formation, and that the latter is

the sedimentary cover to an oceanic basement not

yet recognised. Bousquet (1973) assigned the

ophiolite sedimentary cover to the “Timpa delle

Murge Formation” and stated that it is this for-

mation and not the Frido Formation which lies

stratigraphically beneath the Crete Nere Forma-

tion (cf. Vezzani, 1968), suggesting that the Cilento

Unit was deposited on the ophiolitic sequence.

Lanzafame et al. (1978) recognised a stratigraphic

continuity between the ophiolite sedimentary cover

and the overlying Crete Nere Formation and they

further suggested that this sedimentary cover lay

within a basin with an ophiolitic basement. In a

subsequent paper (Spadea et al. 1980) however,

the same authors stated that the relationship be-

tween the ophiolites and the sediments of the

Cilento Unit was still debated. (The “ophiolites”

of the Southern Apennines and Calabria are all

incomplete and dismembered and should really be

classed as disrupted oceanic slices following the

recommendation of the ophiolite Penrose Con-

ference (Conference Participants, 1972).

Present study

The present study was carried out within an

area situated in the region of Basilicata, Italy at

the northern extremity of the Calabrian Arc (Fig.

2).

Oceanic slices

Kilometre-scale oceanic slices crop out to the

east of Monte Pollino at Timpa delle Murge,

220

Timpa Pietrasasso and Monte Tumbarino (Fig. 2).

At each of these localities serpentinite (c. 15 m

thick), gabbro (c. 20 m), basalt dykes (rare), pillow

lavas (40 m) and sedimentary cover (10 m of

pelagic limestone and ribbon radiolarite) are ex-

posed. Detailed mapping around the base of Timpa

delle Murge and Timpa Pietrasasso (Fig. 3) was

carried out to determine the nature of the contact

between the slices and the underlying material.

At Timpa delle Murge a southward-dipping

shear zone (c. 200 m wide) lies beneath the slice,

separating it from underlying pelitic schists of

Early Cretaceous age. Within the shear zone a

number of diverse hthologies display moderate to

intense ductile deformation. The upper part of the

shear zone contains tectonised serpentinite derived

from the oceanic slice above. Beneath the

serpentinite sheet is a tectonic slice of granite

surrounded by a foliated granite envelope. Defor-

mation gradually increases away from the unde-

formed granite core with undeformed granite

augen becoming smaller and more diffuse until

eventually minor shear zones within the foliated

granite become so pervasive that the lithology is

entirely mylonitic displaying no original igneous

texture in thin-section. Beneath the granite and

serpentinite sheet lie pelitic schists and deformed

calcarenite and quartz-arenite. Well-bedded sedi-

CR ET E N E A E F 0 R hi A T I 0 N

m BASALT h GAEERO

m SHEAR ZONE

a APENNINIC IJNfT

- QEOLOGICAL BOUNDARY

- FAULT

- THRUST N tt-_

0.*.-O TRAVERSE 500m f

NORTH SOUTH

TIMPA OELLE MURGE

A S

Fig. 3. Geologic map and cross-section of the Timpa delle Murge and Timpa Pietrasasso oceanic slices.

221

ments belonging to the Crete Nere Formation occur below and outside the shear zone, and these appear to be the less deformed equivalents of the schists and metasediments found within the shear zone.

At Timpa Pietrasasso (Fig. 3) a similar south- ward-dipping shear zone occurs below an oceanic slice comprising ribbon radiolarite, basalt, gabbro and a serpentinite thrust sheet containing frag- ments of granite, amphibolite, talc-schist and basalt. The serpentinite sheet is superposed tecton- ically above calcarenite of Late Cretaceous age belonging to the Crete Nere Formation which contain abundant calcite veins. Immediately to the north of the serpentinite sheet the strike of adjac- ent Crete Nere Formation bedding becomes paral- lel to the shear zone margin. Figure 3 shows a schematic section displaying the geometry of these imbricate oceanic slices.

Fig. 4. Geologic map of the San Severino Lucano area showing

the extent of Cilento Unit sediments (i.e. Crete Nere and

Saraceno Formations) previously considered to belong to the

Frido Formation (Frido Unit).

Sedimentary cover

At Timpa delle Murge a traverse (Fig. 3) was carried out to determine the relationship between the sedimentary cover of the oceanic slice and the surrounding sediments. The traverse commenced at the conformable stratigraphic contact between the Crete Nere and Saraceno Formations and terminated at the base of the sedimentary cover exposed on top of Timpa delle Murge. The sedi- ments throughout the entire traverse were found to be in stratigraphic continuity from the basal contact of the Saraceno Formation, down succes- sion through the Crete Nere Formation to the pelagic limestone and ribbon radiolarite deposited above the pillow lavas. The sedimentary cover at Timpa delle Murge is lithologically identical to exposures already attributed to the Crete Nere Formation (e.g., Crete Nere Formation at Serra Scorzillo located on the border between Calabria and Basilicata, Foglio 221 I NO Terranova di Pollino). This suggests that the entire succession above the pillow lavas up to the base of the Saraceno Formation, should be assigned to the Crete Nere Formation.

Significance of the Frido Formation and the Frido

Unit

A re-evaluation of the Frido Formation type- area (Fig. 4) showed that all members of this formation were in fact moderately or intensely deformed rocks of the Crete Nere Formation or Saraceno Formation. The less deformed portions were lithologically and petrographically similar to Crete Nere Formation and Saraceno Formation sediments found within the eastern part of the area (i.e. Cilento Unit). Figure 5 shows the similar- ity between the sedimentary petrography of the Frido Formation (Frido Unit) and the Crete Nere and Saraceno Formations (Cilento Unit). Within the “calcareo-scistoso” member of the “Frido

Formation” it was possible to recognise Saraceno Formation lithic arenites, the base of the beds containing the characteristic schist, limestone and quartz clasts commonly found in Saraceno Forma- tion sediments in the eastern part of the area (see Fig. 32; Vezzani, 1968a). The identification of

222

IRF Q mQn

MRF ’ F L

C

0 FRIDO FORMATION QUARTZ-ARENITE 0 FRIDO FORMATION LITH-ARENITE l CRETE NERE FORMATION QUARTZ-ARENITE l SARACENO FORMATION LITH-ARENITE

Fig. 5. Petrography of the Frido Formation (Frido Unit) and the Crete Nere and Saraceno Formations (Cilento Unit). IRF-igneous

rock fragments; SRF-sedimentary rock fragments: MRF-metamorphic rock fragments; Q-total quartz; F-total feldspars; L

-total lithic fragments; m&r-non-undulose monocrystalhne quartz; mQu--undulose monocrystalline quartz; C-stable lithic

fragments.

~u~~u~if~s from the detrital clasts of these iithic arenites by the present author and P. Scandone (pers. commun., 1985) indicates an Eocene age which makes them correlatable with the Saraceno Formation. The type-area also contains numerous major and minor isoclinal folds and thrusts (Fig. 6). The type-area was re-mapped replacing the Frido Formation with the Saraceno and Crete Nere Formations where applicable (Fig. 4).

A

SSE

Fig. 6. Schematic cross-sections of fold and thrust structures

near San Severino Lucano, see Fig. 4 for locations.

St~ctura~ data

Structural analysis of the Liguride Complex shows a polyphase history involving internal de- formation within thrust sheets at deeper structural levels with an early pressure-solution cleavage de- formed by later thrusts and recumbent isoclines

r

Fig. 7. Thrust transport directions within the Liguride Com-

plex derived from stretching lineations, shear bands and thrust

plane mineral fibre lineations coupled with fold vergence, the

area shown is roughly the same as that in Fig. 2.

223

which are themselves folded by minor upright

folds. At higher structural levels kilometre-scale

recumbent folds are affected by later minor thrusts

and upright folds, and pressure-solution is less

intense but dilation veins filled with calcite are

common. Serpentinite often occurs along the basal

decollement to large thrust sheets of both oceanic

and continental basement. Kinematic data derived

from extension lineations, shear bands, and minor

thrust geometries combined with fold vergence

indicate thrust transport towards present-day

northeast. These data are summarised in Fig. 7.

Discussion

The equivalence of the sedimentary successions

of the Frido Unit and the Cilento Unit and their

deposition upon oceanic crust is supported by the

following lines of evidence:

(1) Similarities in lithology, petrology and

facies.

(2) Equivalence in age range, i.e. Late Jurassic

to Eocene (based on the identification of Late

Cretaceous and Eocene faunas in Frido Forma-

tion localities).

(3) Stratigraphic continuity from condensed

pelagic cover sequences belonging to oceanic slices

passing upwards to younger levels of the Crete

Nere Formation (Middle Eocene; M. Russo, pers.

commun., 1985).

Evidence for a subduction related origin for the

Liguride Complex include:

(1) A detached northwestward-dipping litho-

spheric slab beneath the Tyrrhenian Sea (Caputo

et al., 1972).

(2) A talk-alkaline volcanic arc in Sardinia

(Cohen, 1980).

(3) HP/LT metamorphic assemblages in Cala-

bria (De Roever, 1972).

The oceanic slices within the Liguride Complex

represent fragments of oceanic crust and upper

mantle accreted to the inner slope of a trench.

Similar features have been recognised in the

accreted terrains of the Tonga and Mariana arcs

(Evans and Hawkins, 1979). The condensed pelagic

sequences of Late Jurassic age deposited above the

pillow lavas probably represent sedimentation

upon seamounts which stood proud of the ocean

floor and were accreted to the inner slope. The

abundance of serpentinite along thrust contacts

and as individual thrust sheets suggests that sub-

duction may have initiated along an oceanic frac-

ture zone where large volumes of mantle material

would be involved in the first imbricate slices. The

terrigenous detritus deposited on the pillow lavas

at Timpa delle Murge and the tectonic inclusions

of continental basement at the base of the oceanic

slices suggest that the site of subduction initiation

was near the southeast margin of the Calabrian

continental terrain (Knott and Turco, in press).

The presence of HP/LT mineral assemblages in

parts of the “Frido Unit” is probably due to

underplating of material during subduction.

Zuppeta et al. (1984) have shown that sedi-

ments of the Albidona Formation were derived

from the Longobucco Unit (Fig. l), i.e. Calabrian

continental terrain. Provenance studies by the pre-

sent author show a clear correlation between the

detrital evolution of the Liguride Complex, from

Eocene time onwards, and the progressive denuda-

tion of the Calabrian terrain (Longobucco Unit)

(Fig. 8). Are&es at the base of the Saraceno

Formation contain detrital clasts of mainly

carbonate material which were probably derived

from either Apulian carbonates or the predomi-

nantly carbonate-rich cover sediments of the

Longobucco Unit. Towards the upper part of the

Saraceno Formation abundant detritral clasts of

lithic rock fragments occur suggesting provenance

from the pelitic and granitic basement of the

emergent Calabrian terrain. Conglomerates from

the overlying Albidona formation contain boulders

which are readily identifiable as elements of the

Calabrian continental terrain.

It follows from the discussion above that the

Calabrian continental terrain lay on the northern

(European) margin of Neotethys in Late Creta-

ceous time. This is in contrast to the interpreta-

tions of Alvarez (1976) and Amodio-Morelli et al.

(1976) who both placed Calabria on the southern

margin at this time. This would suggest that the

so-called “Alpine” units from the rest of the

Calabria-Peloritani arc will contain structures in-

dicating transport directions towards Africa/Apu-

lia. Dietrich (in press) has in fact shown, from

microstructural evidence, that the upper-most units

224

LONGOBUCCO UNIT Early Cretaceous

l”OOm

CARBONATE TURBIDITES

SHELF CARBONATES LlaS

CONTINENTAL ARENITES PELlTtC SCHIST

GRANITE BASEMENT

>A T

CA CALCARENITE LA’- LlTHlC ARENITE I SRF S PREDOMINATE) LA2-LlTHiC ARENlTE ( IRF’S PREDOMINATE1 C -CONGLOMERATE WliH BOULDERS OF 10NGOB”CCO WIT AND SARACENO FORMATION

LA’ T c

QA

1 1

LIGURIOE COMPLEX

Fig. 8. Petrographic evolution of the Liguride Complex showing the derivation of litho-types from the progressive denudation of the

Calabrian continental terrain (~ngobucco Unit).

of the “Alpine” nappes in north Calabria were

transported from west to east. However, more

detailed work is required around the Calabrian arc

and within the Kabylies to determine the age of

such structures and the nature of the tectonic

contacts (?thrust/back-thrust or extensional fault)

before a comparison can be drawn with the struc-

tures described in this paper.

Bouillin (1984) also proposed that the Calabrian

continental terrain originally lay on the northern

margin of Neotethys based, essentially, on a com-

parison between the structure of Calabria and the

Maghrebides with very little new data. The data

presented here provides more conclusive evidence

for the former position of the Calabrian terrain

and contains important implications for pre-Ter-

tiary plate tectonic reconstructions of the western

Mediterranean region as follows.

Firstly the Calabrian continental terrain would

have formed the eastern promontory of the Iberian

Plate (Fig. 9) and may therefore have experienced

Pyrenean deformation. This may help constrain

the former location and continuation of the North

Pyrenean Fault (NPF). Secondly the European

vergence in Calabria and the Kabylies proposed

by Alvarez (1976) and Amodio-Morelli et al. (1976)

implies the existence of an early southward dip-

ping subduction zone. This would then be fol-

lowed by subduction with opposite polarity giving

rise to the structures of African vergence. How-

ever, if the evidence for the European vergence is

rejected or at least considered to be due to back-

thrusting, as is suggested here, then the structures

in Calabria and the Maghrebides can be explained

by subduction with a single polarity (i.e. north-

1

Fig. 9. Early Cretaceous plate tectonic configuration of the

western Medit~rr~ean with the Calabrian continental terrain

forming the eastern promontory of the Iberian Plate.

NPF-North Pyrenean Fault, stippled-oceanic crust (after

Knott and Turco, in press. and Dewey et al., 1973).

225

westward) commencing in approximately Late

Cretaceous time. Finally the opposed vergence of

structures in Corsica (towards Europe) and

Calabria (towards Africa) requires the existence of

a transform fault between the two regions active

from at least Late Cretaceous time in a position

now occupied by the Tyrrhenian Sea (cf. Bouillin

1984 who places a transform zone along the length

of the Apennines).

Conclusions

It is proposed that the sediments of both the

Frido Formation and the Frido Unit are in fact

deformed and metamorphosed Crete Nere Forma-

tion and Saraceno Formation sediments. This im-

plies that prior to ?Late Cretaceous subduction

the sediments of both the Frido Unit and the

Cilento Unit were lateral equivalents within the

same sedimentary basin lying for the most part

upon an oceanic basement. Thrust transport direc-

tions towards present-day northeast (i.e. towards

Apulia) and sediment provenance from Calabria

indicate that this ocean basin originally lay be-

tween the Calabrian and Apulian terrains. This

Late Cretaceous paleogeography is in agreement

with Ogniben (1969) and Boullin (1984) with the

Calabrian terrain on the European (i.e. NW)

margin of the Neotethys ocean (Fig. 10).

The structures described above are related to

subduction-accretion during Late Cretaceous to

Early Oligocene time prior to the Burdigalian con-

tinent-continent collision of Calabria and Apulia.

The subsequent deformation history involving em-

placement of the Liguride Complex onto the

Apulian margin, the formation of the Apennine

LATE EOCENE I

Fig. 10. Schematic cross-section of the Late Eocene configura-

tion of the Liguride Complex, Calabrian terrain and Apulia.

European margin of the Neotethys is on the left; stipple-oce-

anic crust; crosses-continental crust.

mountain chain and the opening of the Tyr-

rhenian Sea has greatly disrupted the original

large-scale geometries of the accretionary wedge.

The interpretation presented here places in

doubt the validity of the Frido Formation type-

section proposed by Vezzani (1969). Furthermore

the usefulness of the terms “Frido Unit” and

“Cilento Unit” is brought into question. It is

suggested that the latter two terms be abandoned

and the stratigraphy of the Liguride Complex be

revised.

On a more regional scale this interpretation

places three main constraints on the pre-Tertiary

plate tectonic evolution of the western Mediter-

ranean (see also Knott and Turco, in press), they

are:

(1) Calabria formed part of the Iberian Plate

and may show Pyrenean deformation and thus

help constrain the former location of the NPF.

(2) Only one polarity of subduction (i.e. north-

westward-dipping) from Late Cretaceous time on-

wards is required to explain the structures in

Calabria and the Kabylies.

(3) A transform fault occurred between the

Europe-vergent structures of Corsica and the

Africa-vergent structures of Calabria. The trans-

form was active from at least Late Cretaceous

time and was located in a position now occupied

by the Tyrrhenian Sea.

Acknowledgements

I would like to thank Professor E. Turco for

providing stimulating discussion on the implica-

tions of this work on western Mediterranean geol-

ogy. I thank Drs. J.P. Platt and W.S. McKerrow

for their criticism of an early draft of the

manuscript. A N.E.R.C. Studentship Award is

gratefully acknowledged.

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