Brittle deformations in the Upper Pleistocene deposits of the Crotone Peninsula, Calabria, southern Italy

Tectonophysics,

205

163 (1989) 205-217

Elsevier Science Publishers

B.V., Amsterdam

- Printed

in The Netherlands

Brittle deformations in the Upper Pleistocene deposits of the Crotone Peninsula, Calabria, southern Italy D. COSENTINO

* and F. SALVINI

3

Scienze della Terra, Universitci di Roma, Rome (Italy)

’ Dipartimento 2 Dipartimento

‘, E. GLIOZZI

Scienre delia Terra, Universitci di Napoli, Naples (Italy) Scienze della Terra, Vniversitd di Piss, Pisa (Italy)

3 Dipartimento (Received

December

1,1987;

accepted

May 8, 1988)

Abstract Cosentino,

D., Gliozzi,

Peninsula,

E. and Salvini, F., 1989. Brittle deformations

Calabria,

southern

Italy. In: N.-A.

Tectonophysics,

163: 205-217.

The structural

setting

analyses

were carried

field which affected The tectonic

the area during observed

for the dislocation

substage

Terrace,

From Crotone

the studies

The comparison for several

Upper

which affected

Italy)

is discussed

of the Crotone

and Neotectonics.

in this paper.

scale to detect the main structural by normal

ENE-WSW,

depositional substage

faults and extensional

NNE-SSW,

units (Cutro correlatable 5c and Capo

out on a mesostructural by an extensional

systems

Structural

and the stress

E-W,

Terrace,

NW-SE correlatable

with the isotopic Colonne

joints:

with the isotopic

substage

Terrace,

the regional-scale

and NNW-SSE.

They are stage 7;

5e; Le Castella-Capo

correlatable

with the isotopic

between

the average

Pleistocene

deposits

Peninsula

scale it is possible

uplift rates calculated located

to conclude

that for the last 200,000 yrs the

stress field. for the Crotone

in Sicily, Calabria

can be related

activity

terraces

suggests

and those computed

that the intense

of the Calabrian

tectonics

Arc.

bearing Strombus bubonius reveal that these deposits originated in the course of only four marine depositional events. It is possible to correlate these events to the following isotopic stages: 7 (Cutro

The Crotone Peninsula is located in southern Italy, on the Ionian side of the Calabria Province (Fig. 1). It has extensive outcrops of calcareniticsandy marine deposits, arranged into six distinct terraces (Gueremy, 1980; Gliozzi, 1988; Gliozzi and Ruggieri, 1987), which unconformably overlie Plio-Pleistocene clays.

Terrace), 5e (S. Leonardo-Campolongo-Isola Capo Rizzuto Terrace), 5c (Le Castella-Capo

di Riz-

zuto Terrace)

and

and 5a (Capo Colonne

Terrace),

thus estimate their age as Late Pleistocene. The neotectonics of the Calabria Province has been extensively studied and recently synthesized by several authors (Cello et al., 1982; Ghisetti, Tortorici and Vezzani, 1983; Boccaletti et al., 1984). The analysed data (both mesostructural

The presence of U-Th and aminoacid dating (ranging from 172,000 to 72,000 yrs B.P.) (Voltaggio and Gliozzi, 1986; Belluomini et al., 1988; Voltaggio and Gliozzi, in prep.) and a fauna 0 1989 Elsevier Science Publishers

Peninsula

and Campania

to the geodynamic

Introduction

0040-1951/89/$03.50

southern

deposits

Paleoseismicity

terraces.

was affected

the Crotone

striking

with the isotopic

carried

Pleistocene

(Editors),

the Late Pleistocene.

di Capo Rizzuto Terrace,

correlatable

Peninsula

(Calabria,

and an outcrop

of four marine

5a) in several distinct

in the Upper

and J. Adams

in the area are represented

in five main systems

S. Leonardo-Campolongo-Isola Rizzuto

Peninsula

out both on a regional

features

faults are arranged responsible

of the Crotone

MBmer

B.V.

206

not only by uplift fractures.

but also by several

faults

and

The main aim of this paper is the analy-

sis of these tectonic the structural

features

setting

in order

of the area

to provide

and

its stress

field. Furthermore, the findings are compared to the tectonic history of the two Calabrian sectors previously

mentioned.

pact of tectonics

Finally,

the principal

on the morphological

im-

setting

has

been investigated. Tectonic framework Field investigation, together with air photo examination, have shown that the Crotone Peninsula Fig. 1. Location

of the studied

area.

is affected

by several

the Plio-Pleistocene tectonic features and focal mechanisms-the latter for most recent earthquakes) indicate that Calabria and the Eastern Sicily display features of peculiar Neogene and Recent tectonic history, different from that of the Southern

Apenmnes.

That origin

faults

which

displace

clays of the “argille

both

marnose

di Cutro” Formation and the Upper Pleistocene sedimentary cover. The youth of these faults is also confirmed by the preservation, cases, of the fault scarp, notwithstanding vailing loose nature Two main fault

in

several the pre-

of the displaced sediments. systems, namely ENE-WSW

needs to be related to the complex geodynamic interaction between the opening of the Tyrrhenian

and NNE-SSW,

and subordinately

and NNW-SSE

striking

Sea and the eastward Peloritan nappes. Two main regions

nized in the area (Fig. 2). The ENE-WSW striking system is well recognizable in the southern area of the peninsula both

motion

of the

can

distinguished

Calabria, each characterized styles: in northern Calabria

be

Calabroin

by different tectonic the more recent pre-

in the Capo

arranged

fected the area during

sola di Capo

the other hand

southern

Calabria

Pleistocene); is mainly

acterized by strike-slip deformations. Considering this regional tectonic

on char-

framework,

the tectonic history of the Crotone Peninsula (studied in detail by Ciaranfi et al., 1982) seems to be more related to the northern region than to the southern one. In fact in the Crotone area Ciaranfi et al. (1982) recognize a main tensional stress field which acted chiefly to cause uplift (Middle-Late Pleistocene interval). Neither Ciaranfi et al. (1982) nor Ghisetti et al. (1983) recognize any main fault system in the Crotone Peninsula. The results of the recent field work on the Crotone Peninsula (Gliozzi, 1988) indicate that the terraced deposits have been strongly affected

and

E-W,

NW-SE

have been recog-

Le Castella

zones.

In

sector I (Fig. 2) a group of parallel faults belonging to this system defines a block-faulted area

vailing tectonic stress field is extensional (apart from some lesser compressional events which afthe Middle

Rizzuto

systems

in small graben

The occurrence

Rizzuto

and horst structures-I-

(A), and La Mazzotta

of two major

normal

faults

(B). with

opposite dip helps to define this structural setting. The first, the Varitaggi fault (a in Fig. 2) downthrows the deposits of the uppermost terrace (Cutro Terrace) to the southern area, with a displacement of 20 m. This value has been obtained by the different outcropping altitudes of an Ostreabearing key bed (Fig. 3). Field

data

have

suggested

that

this displace-

ment took place after the deposition of the Cutro Terrace sediments but before the Eutyrrhenian sea deposited the sedimentary cover of the Isola di Capo Rizzuto Terrace, that is in the time span between about 172,000 and about 123,000 yrs B.P. (Gliozzi, 1988). Such an indication is suggested by the fact that the Isola di Capo Rizzuto strip of

Cannone

to the NNE-SSW

Boscoverde-Torre

belonging

sketch map of the Crotone

striking

Fault

system,

(b) which

downthrows throws of about

10 m. Squared

deposits

*I

(r

of the Cutro

faults

c, d and e indicate

those faults

with

by step faults,

area, and the

to the ENE-WSW in the southern

belonging 2 is characterized

Terrace Sector Terrace;

area.

of the Cutro

Inferred normal faults

Normal faults

Cutro marly clays (PLIO-PL&ISTOC&NE)

Upper Pleistocene marine deposits of the Cutro Terraca (CROTONIAN)

Upper Pleistocene marine deposits of the SLeonarda-Campolongo-lsola di Capo Rizzuto Terrace (EUTYRRHENIAN)

by several parailel deposits

in more detail in Figs. 4 and 5.

marine

.,

*-?r-*-

-

in the northern

marine Terrace

Pleistocene Rizzuto Pleistocene areas are represented

area in Upper

km

(A) and horst (B) defined

2

the Upper of the Le Castella-Capo

in the eastern

the deposits

1

by a small graben

Fault ((1) which downthrows

Sector I is characterized

the Varitaggi

Peninsula.

which downthrow

system. Two main faults are evidenced:

Fig. 2. Geological

striking

07

Cap0 Zolonne

upper Pleistocene marine deposits of the Le Castella-Cap Rizzuto Terrace (NEOTYARHEhlAX)

Upper Pleistocene marine deposils 01the Cap0 Cokxme Terrace (NEO~RRUENIAN)

LEGEND

8 -l

208

Fig. 3. Osrrea-bearing high -way) nearby

key bed belonging

the Isola di Capo

to the depositional

Rizzuto calculate

village.

Using

sequence

of the Cutro

the different

the displacement

terrace is the only one portion of the S. Leonardo-Campolongo-Isola di Capo Rizzuto Terrace that lies directly against the Cutro Terrace deposits and not against the clayey slope. The case of the Varitaggi Fault is the only one in the

Terrace,

outcropping

outcropping

altitudes

value of the Varitaggi

along

the S.S. 106 (Ionian

of this key bed it was possible

to

Fault.

of the terrace in the southern area with a total throw of 20-25 m. The NNE-SSW striking system is mainly represented in the eastern part of the peninsula.

Crotone Peninsula with at least the first time of activity firmly established. However, it is not possible to exclude any other more recent movement of this tectonic feature. The second fault, namely the Boscoverde-Torre Cannone Fault (b in Fig. 2), displays a sharp morphological evidence, represented by a 6 km rectilinear fault scarp clearly visible both on the field and from the air photos. It displaces the deposits of a younger terrace (Le Castella-Capo Rizzuto Terrace, i.e. Neotyrrhenian) with a north downthrow of 15-20 m. The ENE-WSW striking system is also responsible for the dislocation of a strip of Le Castella-Capo Rizzuto Terrace nearby Le Castella village (Fig. 4). In this case a system of three parallel faults downthrow the sedimentary cover

Fig. 4. The Cozzo

S. Domenico

village, is affected

by a step-fault

which displaces Terrace.

Numbers

the deposits represent Symbols

area,

nearby

system

the Le Castella

striking

of the Le Castella-Capo the elevation as in Fig. 2.

ENE-WSW Rizzuto

above sea level (m).

209

Fig. 5. Detail of the sector 2 of Fig. 2. The step-fault the Cutro Terrace always belonging

deposits

system striking

to the same striking

system, which induce the formation level (m). Symbols

Particularly

in the sector

2 (Fig. 2) this system is

represented by step faults which in the eastern area downthrow the deposits of the uppermost

Fig. 6. Outcrop

of Upper

NNE-SSW

is represented

with throws on the order of tens of meters. The structure

Pleistocene

sequence

marine

is affected

sands, with arenaceous

by several normal

by three main faults which displaces

is complicated

of a small horst. Numbers

by the presence represent

of minor

the elevation

faults,

above sea

as in Fig. 2.

terrace (Cutro Terrace) with a total throw of about 40 m. Only three of these faults (c, d, and e in Fig. 2) show a significant displacement of about

and pebbly

intercalations,

faults with throws ranging

belonging

to the Cutro

from 1 cm up to 50 cm.

Terrace.

The

cf7

,Jg

,pj

,m

,m

I

I I

I

I I

I

O.S% 3.3% Fig. 7. Schmidt net diagrams of the mesostructural

8.7% 1

6.0%

10.7%

data collected in the Upper Pleistocene deposits of the Crotone Peninsula. a.

Stereoplot of the poles of planes of the normal faults (small circles) and of the joints (black dots). b. Pole density diagram obtained using the Kalsbeek counting net. The percentage value represents the percentage amount of data per 1% of net surface. Small letters indicate the position of the barycenters of the different pole concentrations. pole concentrations

c. Diagram showing the plane trends drawn from the

of diagram b.

the tensile axis (u3) oriented ESE-WNW and a vertical ur, is recognized as the predominant system to have been active in the northern Calabria

10 m, exceeding the thickness of the terrace marine deposits, since the underlying clays outcrop along their fault scat-p. A detail of this sector, as shown in Fig. 5, demonstrates that the general step-faulted tectonic

during the Late Pleistocene (Boccaletti et al., 1984).

style is affected by several minor faults, still belonging to the NNE-SSW striking system, which

Mesostructur~l

induce some complications small horst.

Beside the regional tectonic features discussed above, the Upper Pleistocene deposits are also affected by mesostructural elements (Fig. 6). All

and give origin to a

Such striking system, due to a stress field with

analysis

N

N

Fig. 8. Schmidt net diagrams of the normal-fault data collected in the Upper Pleistocene marine deposits of the Crotone Peninsula. For explanations see Fig. 7. In Fig. 8c a conjugate system is figured.

211

of them are of brittle into

faults,

nature

and can be divided

with displacements

centimetres

up to l-2

ranging

m, and

from few

extension

joints

often filled with calcite. Due to the loose nature

of the lithology,

whole area it was possible surement

sites,

consisting

of 15 faults

These stations the irregular

yielding

Fig. 9. Normal

to find only ten meaa total

and

of 75 elements

60 extension

are not evenly distributed distribution

yield mesostructural

joints. owing to

of fresh sections

data. Taking

fault conjugate

in the

which

into account

system belonging

the

to the ENE-WSW

easy weathering deposits,

nature

both

tectonic

elements

regarded

as sufficient

The poles (Fig.

tinguish

difficult,

striking

observed

pole

has been

symbols

to dis-

(small

circles)

to faults counting

(black dots). net the isodenses

concentrations

in a sandy

data

net (lower hemi-

different to joints

the Kalsbeek

system

Cutro 11 section (Cutro Terrace).

figure

an analysis.

on a Schmidt

referring

of the different

this

of these

of all the collected

7a) using

those

age of the

recognition

to attempt

from those pertaining Using

the

to planes

have been plotted sphere)

and the young

making

succession

have

outcropping

been

at

212

drawn (Fig. 7b) in order to obtain their barycentres. The percentage value pertinent to each area included between two isodenses represents the percentage amount of data per 1% of net surface. From this analysis it was possible to obtain the deformation trends which affected the Crotone Peninsula during the Late Pleistocene (Fig. 7~). Six prevailing striking systems have been recognized; they are (in decreasing order of density): 084”, 130”, 113O, 146O, 065” and 050’. The systems striking 130 O, 113” and 146” belong to the same fracture domain (a in Fig. 7~). The tectonic structures which are related to the systems striking 084’, 130°, 113”, 146’. 050” and 065” show almost vertical dips (Fig. 7c), while the faults related to the 138” one (b in Fig. 7c) have less dipping planes. The results obtained from the mesostructural analysis, as shown in Fig. 7c, do not provide

Fig. 10. Lower deft brmation

Pleistocene

clay quarry

net with rhomboidal

mesh.

at M. Viscovatello In this locality

enough indications about the stress field orientation. Nevertheless, field evidence proves that all the brittle deformations observed in the area on the Upper Pleistocene deposits have an extensional stress field as an originating factor. In fact, all the faults recognized both on regional and on outcrop scale display a normal deformational mechanism and the fractures are mainly represented by open joints often with calcite mineralization. Most of the mesoscale faults belong to the 084”-065” striking systems which correspond to one of the main fault systems observed on a regional scale (ENE-WSW). The extensional nature of this system is well established in the diagrams of Fig. 8, in which the poles to fault planes alone are plotted. In fact, in Fig. 8c the plotted data provide evidence as to the existence of a conjugate system with vertical ul axis. A con-’ jugate fault system belonging to the ENE-WSW

(Crotone).

Global

there is a total patterns.

view of the drainage

correspondence

between

pattern the tectonic

placed and

on a blittle the drai

213

system has been observed on a mesost~ctural scale in the Cutro 11 section (Cutro Terrace) (Fig. 9).

striking

Drainage segments analysis

The existence of relations between the structural setting of an area and its morphologic features is generally accepted (Scheidegger, 1981; Wise et al., 1985). In the Crotone Peninsula such a relation has been observed on the outcrop scale in a clay quarry. As the case in Fig. 10 illustrates, there is a total correspondence between the tectonic and the drainage patterns. In this paper we have attempted a comparison between the structural systems recognized in the area and its fluvial pattern. A positive correlation between them would strengthen and complete the information about the deformational pattern which has been obtained from the mesostructural analysis. The drainage segments have been drawn from the four I.G.M.I. topo maps (scale 1 : 25,000) which represent the study area. Only the straight segments longer than 1 cm (i.e. 250 m) have been chosen for this analysis in order to get a significative sample with respect to

Fig.

11. Computer

drainage

from I.G.M.I. tone

order

diagram

between

macro-

of the drainage

straight

segments.

to allow their comparison.

The segments

topo maps (scale 1: 25,000)

S. Leonardo

I

I

I

*

t

I

I

I

These elements,

The sizes of the asterisks

of the drawn

Cutro.

Cro-

I

I

I

I

I

I

I

._ *..___

features,

orientations.

i

recognized

very different

used in the diagram

azimuthal

sheets:

been

E I

*

and mesostructural

analysis have

di Cutro and Isola di Capo Rizzuto.

*...*I...* \**~

Drainage straight segments n= 1217

Fig. 12. Correlation

I

*

Mesostructural elements n = 7.5

distributions

of the azimuthal

N I

elements n=42

output segments.

the used scale. In this way 1217 data have been digitized and processed to obtain their azimuthal distributions. Figure 11 represents the computer output in which it is possible to recognize a non-random dist~but~on of the drainage segments. The data are arranged according to 3 main azimuthal groups (174’, 055” and 027O) together with the presence of 4 other minor groups (159 O, 081”, 141” and 005 o ).

W

Macrostructural

straight

in the Crotone

in nature,

Peninsula,

have been processed

are proportional

and the azimuthal in the same way in

to the frequencies

of the different

214

As Fig. 12 shows, taking very different quite

nature

different

macrodrainage

and

into account

of the analysed

methods

straight

data and the

used to obtain

mesostructurai segments

both the them,

the

macrost~ctural

and

the

azimuthal

features

share some azimuthal

the best correlations

for the ENE-WSW

striking

Fig. 13. Uplift average rates since b-Ravagnese, c-Nocella, d-Cap0 m--Vibo

Valentia,

system

of

and

the

the

drainage

spondences

are better

orientation

than to the frequency

and

larly in the case of the drainage

for the

o-Scalea,

p-Praia,

co~esponding straight

seg-

ments. The same figure also reveals that the corre-

Late Pleistocene to Recent of some dell’Armi, e-Lazxaro, j-Milazzo,

n-Cetraro,

systems

values

are obtained

orientations. In particular,

NW-SE one. A good agreement is recognizable also between the NNE-SSW and NNW-SSE

q-Maratea,

related

to the preferential values, straight

particusegments.

Tyrrhenian deposits of Southern Italy: a-Bovetto, g-Cap0 Tindari, h-Cap0 Peloro, l-Monte Poro, r-Amalfi,

s-C’rotone,

I-

Mare Piccolo.

215

Uplift rates and discussion

1987)

very

similar

to

those

of

the

Crotone

Peninsula. The analysis

of the tectonic

fected the Upper

Pleistocene

cropping

in the Crotone

features marine

Peninsula

which af-

deposits indicates

northern

Calabria

no average uplift rates have been

computed

the

terraces

that

Vaticano-Vibo

Valentia

area

the Tyrrhenian

of Monte

Poro and Vibo Valentia

in the last 200,000 yrs this part of the Calabria Province was subject to a tectonic history similar to that which affected

Unfortunately,

out-

(Bocca-

for

(Carobene

et al., 1986; Dumas

Nevertheless, observe

that the Tyrrhenian

henian

coast

uplift

Cetraro-Maratea

that probably

Pleistocene. No evidence

continued

of an extensional since

the Middle

of strike-slip

displacements

typical

posits of the Crotone Peninsula (strike-slip faults of undetermined age are reported by Boccaletti et al. (1984) only offshore the peninsula, bordering coast).

Moreover,

another

similarity

between the neotectonics of the Crotone area and that of northern Calabria is represented by the NNE-SSW represents

striking system which, in both sectors, one of the main extensional systems

that acted during the Late Pleistocene. The Late Pleistocene uplift which affected

deposits

northern

field work provided enough data to permit the computation of average uplift rates for the Upper Pleistocene terraces (Gliozzi and Ruggieri, 1987; Gliozzi, 1988). These values are quite high ranging from 1.8 mm/yr during the interval between the of the Cutro Terrace of the subsequent

deposits and the S. Leonardo di

Cutro-Campolongo-Isola di Capo Rizzuto Terrace ones (i.e. the Crotonian-Eutyrrhenian interval) and reaching 0.85 mm/yr since the Eutyrrhenian up to the recent times. They are comparable with the average uplift rates that occur in present active tectonic areas (cf. Matsuda et al., 1978) and with average rates computed for other Tyrrhenian deposits of the Calabria Province and eastern Sicily (Fig. 13). In particular, such localities of southern Calabria as Ravagnese, Bovetto, Nocella, Capo dell’Armi, Lazzaro and eastern Sicily as Milazzo, Capo Tindari and Capo Peloro display very high uplift rates (Hearty et al., 1986; Dumas et al.,

of

to

on the Tyrr-

Calabria

area provides

in

the

average uplift rates illustrated.

It needs Calabrian

to be noted that this portion cost is located to the north

Sangineto boundary

tectonic line which represents the between the Southern Apennines (to the

north) south).

and

the Calabrian-Peloritan

Arc

of the of the

(to the

Therefore, we believe that the recent high uplift rate in the Calabria Province represents another tectonic peculiarity of this area, which, together with the intense seismic activity (also with deep hypocenters)

along

a Benioff-like

ble with lithospheric the

Crotone area has already been stressed by Ciaranfi et al. (1982) and Ghisetti et al. (1983). The recent

deposition deposition

the

Capo

interesting

very much lower than those previously

of the tectonic style of the southern Calabria have been found, affecting the Upper Pleistocene de-

its eastern

of

the

for that

et al., 1987).

it is particularly

stress field which, in this area, flanks a continuous

letti et al., 1984), i.e. the working

in except

zone, correlata-

slab subduction

al., 1982), characterizes the complex of one of the most active sectors Mediterranean

(Gasparini

et

geodynamics of the peri-

chain.

Conclusions The present study carried Pleistocene marine deposits P,eninsula

suggests

(1) During Peninsula

the following

out on the Upper of the Crotone conclusions:

the last 200,000 yrs B.P. the Crotone

was affected

not only by uplift but also

by brittle deformations. (2) The six morphological

terraces

recognized

in the area are the results of the displacement of only four original marine depositional units, namely the Cutro Terrace, the S. Leonardo-Campolongo-Isola di Capo Rizzuto Terrace, the Le Castella-Capo Rizzuto Terrace and the Capo Colonne Terrace, which are correlatable respectively with isotopic stages 7, 5e, 5c and 5a. (3) The tectonic features which affected the area are represented by normal faults, recognizable both on regional and outcrop scale, and extension joints often with calcite mineralizations.

216

(4) The regional scale faults, arranged in five main systems striking ENE-WSW, NNE-SSW, E-W, NW-SE and NNW-SSE, show throws of the order of tens of meters. (5) Both macrostructural and mesostructural analysis indicate that in the last 200,000 yrs B.P. the area was affected by an extensional stress field. (6) The azimuthal distributions of the drainage segments correlate well with the structural data, showing that neotectonics plays an important role in the morphological evolution of this area. (7) The intense neotectonics and the high uplift rates recognizable in the area are related to the geodynamic activity of the Calabrian Arc. Acknowledgements

We thank Mr. M. Albano and Mr. M. Salvati for making the drawings. Grants from Dipartimento di Scienze della Terra, University of Naples (Dottorato di Ricerca in Geologia de1 Sedimentario) (E.G.) and from 40% M.P.I. (Prog. “Litosfera”), U~versity of Rome are also kindly acknowledged. References Belluomini, G., Gliozzi, E.. Ruggieri, G., Branca, M. and Deli&a, L., 1987. First dates on the terraces of the Crotone peninsula (Calabria, Southern Italy). Boll. Sot. Geol. Ital., 7: 249-254. Boccaletti, M., Nicolich, R. and Tortorici, L., 1984. The Calabrian Arc and the Ionian Sea in the dynamic evolution of the Central Mediterranean. Mar. Geol., 55: 219-245. Burton, A.N.. 1971. Carta geologica della Calabria alla Scala 1: 25.OCO: relazione gene&e. Cassa per il Mezzogiomo, Servizio Bonifiche. Carobene. L., Dai Pra, G. and Gewelt, M., 1986. Niveaux marins du Pleistocene moyen-superior de la tote tyrrhenienne de la Calabre (Itahe mkidionale). Datation *~%I/*~~U et tectonique rkente. 2. Geomorphol., N.F., 62 (suppl.): 141-15s. Cello, G., Guerra, I., Tortorici, L., Turco, E. and Scarpa, R., 1982. Geometry of the neotectonic stress field in Southern Italy: geological and seismological evidence. J. Struct. Geol., 4(4): 385-393. Ciaranfi, N., FrancescangeIi, R. and Rapisardi, L., 1982. Osservazioni suila neotettonica dei fogb 237 “S. Giovanni in Fiore” e 238 ““Crotone”. Co&b. Concl. R-one Carta Neotett. d’ItaL, Pubbl. Progetto Finakzato Geodin., 513: 405-425.

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