Morphological, sedimentological and tectonic features of diamante-m. Carpinoso Marine terrace flight...

EARTH SURFACE PROCESSES AND LANDFORMS, VOL. 18,225-239 (1993)

MORPHOLOGICAL, SEDIMENTOLOGICAL AND TECTONIC FEATURES OF DIAMANTE-M. CARPINOSO MARINE

TERRACE FLIGHT (TYRRHENIAN COAST OF NORTHERN CALABRIA, ITALY)

LUIGI CAROBENE

Dipartimento di Scienze della Terra, Universita degli Studi di Genova, Corso Europa 26, 16132 Genova, Italy AND

GIANLUCA FERRINI

Dipartimento di Scienze della Terra, Universita degli Studi della Calabria, 87036 Arcavacata di Rende ( C S ) , Italy

Received 10 January 1991 Revised 25 November 1991

ABSTRACT

Marine terrace flights resulting from the interaction of Quaternary glacio-eustatic fluctuations and tectonic uplift are a typical feature of the Tyrrhenian coast of Calabria in Southern Italy; in particular a tei-race flight with four orders of terraces is evident in the Diamante area. The lowest terrace levels (fourth order: Diamante-Cirella terrace) are typified by a calcarenitic deposit with Cladocora caespitosa which give a Th/U age > 300,000 years. The third order terrace has a sedimentary cover formed of a basal discontinuous level of well rounded pebbles which underlies a deeply weathered coarse-grained sand horizon. The deposit ends with a paleosol locally cut by erosional scours filled by yellowish tuff deposits. The formation of this terrace dates from the Middle Pleistocene. The second order terrace presents a sedimentary cover composed of two generations of soils and is attributed to Middle Pleistocene age. The first order terrace (M. Carpinoso terrace) presents a wave-cut platform covered by a clastic deposit of marine and continental origin; this deposit consists of superimposed depositional events separated by unconformities, bounded by two diachronous surfaces. The formation of the wave-cut platform could be related to several sea-level stands during a long-lasting slow subsidence phase of the coastal area during the Lower Pleistocene. The uplift following terrace formation displaced the first order terrace most markedly; tectonic lineations controlled the hydrographic pattern and erosion of the surfaces.

KEY WORDS Geomorphology Marine terrace Sedimentology Littoral sedimentation Neotectonics Pleistocene Italy

INTRODUCTION

Marine terrace flights resulting from the interaction of Quaternary glacio-eustatic fluctuations and tectonic uplift are a typical feature of the Tyrrhenian coast of Calabria in Southern Italy. Owing to the differential tectonic/isostatic uplift rate, which has affected the Coastal Range, the terraces vary in width and elevation: this fact, together with the erosion of the covering sediments, does not favour age determination of terraces and their correlation with the deposits outcropping in the various sectors of the coast.

The Coastal Range is a portion of the northern Calabrian Arc which, in turn, is a segment of the peri- Tyrrhenian system connecting the Apennine chain and the Sicilian-Maghreb chain. A map of the study area is shown in Figure 1. Between Diamante and Monte Carpinoso, there outcrops the ‘Diamante sequence’ (Damiani, 1970) which is made up of well bedded limestone with calcarenite levels of Lower Cretaceous- Malm age, metamorphic rocks, and a marly complex of Lower-Middle Miocene age; in particular, Monte Carpinoso is composed of Triassic dolostone.

0 197-933 7/93/030225-15$12.50 0 1993 by John Wiley & Sons, Ltd.

226 L. CAROBENE AND G. FERRINI

CIRELLA C x " ' / DI AM ANTE T , c o r v \ n

1 0 BELvEDEREMv I 0 km

Figure 1. Index map of the study area

The aim of this study was to define the type of tectonics that acted in the area and to determine its effects, based on morphologic, morphotectonic, sedimentologic and stratigraphic evidence.

TERRACE MORPHOLOGY AND DEPOSITS

The western slope of the Monte Carpinoso can be divided into two distinct portions:

1. the lower portion from 0 to 510m a.s.l., which is stepped by well developed marine terraces; and 2. the upper portion from 510 to 988 m a d . , which is a regular, rather gentle (average inclination 30") slope

Four orders of marine terraces have been recognized (Figure 2).

Fourth order: Diamante-Cirella terrace (20-25 m a d . shoreline) The lowest terrace levels, grouped in this order are clearly visible near the localities of Cirella and

Diamante (Figure 2) and are typified by a calcarenitic deposit with Cladocora caespitosa (Carobene et al., 1986; Carobene and Dai Pra, 1991a). Biocalcarenite relics are found up to 2 m a.s.1. at Cirella; a sample (LBl) has given a Th/U age >300,000 years (Carobene et al., 1986; Carobene and Dai Pra, 1991b). Cladocora- bearing biocalcarenite relics, outcropping on 'Punta di Diamante' above the bedrock limestone from sea level to 5.60 m a.s.l., have given an age > 306,000 years (sample LB69) (Carobene et al., 1986). In thin sections the

with talus breccia at its foot.

MARINE TERRACE FLIGHTS 221

Figure 2. Marine terrace distribution map: 1, first order terrace; 2, second order terrrace; 3, third order terrace; 4, fourth order terrace; 5, inner margin (with elevation); 6, outer edge; 7, terrace surface’s morphological boundary; 8, morphological step cutting the same

terrace order; 9, muddy terraced alluvial fans

Cladocora-bearing biocalcarenite is composed of limestone clasts, quartz, mica grains and rock/fossil fragments (especially Lithothamnium sp.). The elevation of the inner margin of the marine terrace indicates the ancient shoreline; at present the continental deposits (colluvium/talus) which cover the inner margin obscure the critical break in slope.

The sedimentary cover of the terrace outcropping at Diamante locally shows a massive basal fine-grained sand member, probably of aeolian origin, covered by a 4 m thick heterometric breccia (clasts up to 30 cm) with a silt/sandy matrix. Locally the breccia may be covered by a 1 m thick reddish soil horizon (colour

Along the coast between Cirella and Diamante, around 10 m a d , outcrops coarse sand with gravel horizons, probably of beach origin, which are covered by continental deposits. Gently dipping surfaces

5YR-4/6).

228 L. CAROBENE A N D G. FERRINI

(5-6"), recognizable between Diamante and Cirella (Figure I), have been considered to be alluvial fans (Figure 2). The fan deposits end with a paleosol 1-2 m in thickness, which makes them well correlatable with and genetically similar to the deposits covering the Diamante marine terrace.

Third order (80-100 m a d . shoreline) The terraced surface (Figure 2) seen on the South of T. Vaccuta (near Cirella) varies in elevation between 30

and 80 m a.s.1. Uphill, where the calcareous dolomitic bedrock outcrops (Compagnoni and Damiani, 1971), the sedimentary cover is eroded and the degraded and karstified wave-cut platform can be seen with small rounded quartz pebbles still visible on it. The terrace deposit is, on the contrary, still present in the seaward portion of the terrace itself (Figure 3) below a thick layer of a yellowish-red to brown soil (5YR-4/6) (Figure 4). To the North of T. Vaccuta can be seen a marine deposit composed of fossiliferous gravel with rounded

Figure 3. Sedimentary cover distribution map. Marine deposits: 1, mainly conglomeratic; 2, mainly sandy. Continental deposits: 3, debris flow, reworked alluvial deposits, breccias; 4, colluviurn; 5, talus breccia; 6, alluvial fan muddy deposits; 7, regolith,

8, lithostratigraphic section locations


Figure 4. Marine terrace soil distribution map: 1, reddish soil on marine deposits; 2, brownish/reddish soil on continental deposits; 3, weathered regolith

and flat pebbles, rounded blocks up to more than 50 cm in diameter with Lithodomus holes. The maximum width of the terrace is 700 m and the inclination is about 3.5".

Another terraced surface, located to the North of T. Corvino near Diamante, varies in elevation from 60 to 100 m a.s.1.; its maximum width is 450 m, with inclination of about 5". The terrace bedrock is formed of a thinly layered calcareous schist; the wave-cut platform, which is locally covered by a sedimentary deposit, is clearly visible on the outer edge of the terrace. The deposit has at its base a discontinuous horizon formed by a concentration of well rounded pebbles up to 10 cm in diameter which overlies the bedrock and underlies a deeply weathered coarse-grained sand horizon with scattered large pebbles. The deposit ends with a paleosol locally cut by erosional scours filled by yellowish tuff deposits. This sedimentary cover was formed in a coastal/shallow water environment related to the wave-cut platform. The paleosol is truncated by an erosional surface on which a continental deposit is clearly visible. The formation of this terrace dates from Middle Pleistocene (Carobene and Dai Pra, 1991a).

230 L. CAROBENE A N D G. FERRINI

Second order (190-220 m a d . shoreline) Well preserved surfaces and subhorizontal narrow stretches are evident along the ridge of the watersheds

(Figure 2), showing the existence of the second order terrace. To the north, the surfaces vary in elevation from 130 to 190ma.s.l., and from 180 to 220ma.s.l. in the south; their inclination is 5-6" seawards, and the maximum width is 600m.

The features of the surfaces are varied: to the east of Cirella the sedimentary cover has the greatest thickness at the centre of the surface, and it thins to nothing towards the margins (Figure 3). The karstified dolomitic bedrock is clearly visible along the outer edge. On the surface there is a red soil (Figure 4) enriched with small rounded quartz pebbles, and covered by a colluvial deposit landward along the surface inner margin. Southwards, on the first surface, rounded pebbles are found only near the inner margin covered by colluvium. The rest of the wave-cut platform is covered by a continental debris-flow deposit 3-4m in thickness, which includes reworked small rounded pebbles. The bedrock is schistose, and the red paleosol has not been found on this surface (Figure 4). The other surfaces have similar features: the wave-cut platform is covered by a thin layer of gravel to sand, the pebbles are rounded with average diameters of less than 3 cm to a maximum of 20 cm. The deposit is deeply weathered to a yellowish-red coloured soil that may also be indurated (colour 5YR-5/8,4/6); the soil profile is truncated. The deposit becames thinner towards the outer edge of the platform. The red soil is covered on the surface inner margin by a continental deposit made up of colluvium or talus. The deposit is formed of silt containing scattered small pebbles and it is weathered to a dark brown soil (colour 7/5YR-3/4; Figure 4). In conclusion, the sedimentary cover of this order of terraces presents two generations of soils: the older is red in colour and consists of the gravel and sand deposit of marine origin; the younger is brown in colour and consists of the silty continental cover. The second order terrace is attributed to Middle Pleistocene age (Carobene and Dai Pra, 1991a).

First order: M . Carpinoso terrace (540-5 10 rn a.s.1. shoreline) The surfaces belonging to this terrace order can be seen between the T. Vaccuta on the north (Figure 2) and

the T. Corvino on the south (Carobene and Ferrini, 1990a, b, c). The westward flowing rivers (Figure 5) have divided the original terrace into elongated surfaces. The southern portion of the terrace is well preserved from 280 to 510 m a d . with a maximum width of 3300 m; the inclination varies from 3" in the outer edge to 4" in the middle part and 6" in the inner margin. The terrace's landward limit is given by the M. Carpinoso slope (mean inclination 30") resulting from the erosion of an old cliff shaped up on a Triassic dolomite. The raised shoreline at the foot of this feature is still recognizable (up to 550 m a.s.1.) by the presence of large boulders with Lithodomus holes. The first description of the terrace is given in Damiani (1970) who observed the Lithodomus holes up to an elevation of 410 m a.s.1.

The wave-cut platform is covered by a clastic deposit whose thickness varies from 10-20m up to a maximum of 70 m, corresponding to a tectonic depression or a paleovalley. The deposit (of marine and continental origin) has been deeply weathered into an evoluted soil which is now truncated by erosion.

Lithostratigraphy. The stratigraphic section which characterized the inner margin area (Figure 6) is constituted by different superimposed depositional events showing a general regressive trend. The basal portion of the sequence is commonly represented by a ruditic horizon, lying directly on the calcareous bedrock, consisting of rounded limestone boulders displaying abundant Lithodomus holes; locally the bedrock itself is perforated by Lithodomus holes. This level has been interpreted as a rocky coast with sea cliff base deposits.

On the ruditic portion lies an alternation of conglomerates and coarse-grained to pebbly sandstone which form laterally extensive tabular sheets. The palaeocurrent pattern is indicative of a mean transport direction from the NE quadrant coherent with the actual direction of the Corvino valley; scanty bone fragments scattered in the sandy levels are present. These conglomeratic beds can be interpreted as parts of 'bar cores' (Bluck, 1974) typical of straight or low-sinuosity rivers (Steel and Thompson, 1983; Ramos and Sopena, 1983; Billi et al., 1987). The sequence ends with debris flow deposits represented by large cobbles and pebbles in an abundant sandy matrix, currently capped by a soil horizon. Locally the debris flow is absent and the paleosol is covered by talus formed of angular limestone boulders. The stratigraphic sequence is at higher elevations and away from the paleosediments' entry point of the Corvino valley: at the base, conglomerate

MARINE TERRACE FLIGHTS 23 1

Figure 5. Hydrographic pattern of the study area. Small arrows show the old drainage inferred from morphological features; Large arrows show the paleovalley cut in the first order terrace inferred from lithostratigraphic sections

and cemented gray sand with well rounded clasts are always present. Loose coarse-grained massive sand overlies the conglomerate. This sand may be rubefied and locally may directly overlie the bedrock. The sequence ends with a brown soil.

The sedimentary sequence of the medium part of the terrace (Figure 7) is characterized by a thick basal portion of coarse- to medium-grained sand with conglomeratic levels interbedded. This part consists of hummocky-stratified sand with interstratified conglomerate levels arranged in a series of superimposed, shallow, concave-upward scours. These irregularly shaped features are as much as 2 m wide and 0.4-0.5 m deep and are filled with gently inclined (less than loo) laminae. Concentrations of small pebbles are present along some of the laminae. The conglomeratic beds are thin and laterally discontinuous with pebbles aligned along low-angle cross-laminae; the laminae commonly have a gently convex-upward outline; the conglomerates are generally matrix-supported.

The low-angle crossstratified conglomerates were probably deposited within low-amplitude migrating bedforms; the presence of convex-upward surfaces suggests that they represent bars produced in an onshore


515 m 490 m

C

M

Figure 6. First order terrace. Lithostratigraphy of inner margin; 1, brown/reddish brown soil; 2, red/yellowish red soil; 3, laminated sands; 4, sloping sandy laminae; 5, erosional scour; 6, well rounded clasts with Lithodomus holes; 7, bedrock; M = marine environment;

C = continental environment. For section locations see Figure 3

wave translation zone. The crossbedded pebbly sandstone is due to a unidirectional migration of megaripples in the zone above wavebase and can be considered part of the upper-shore facies of a high-energy near-shore environment.

At the end of marine sedimentation, the facies were covered by an alternation of massive medium- to fine- grained sand and conglomerates. The conglomerates consist of well rounded pebbles (mean diameter 35 mm) in laterally extensive sheet-like bodies; the clasts are imbricated with poor sandy matrix. The medium- to fine-grained interbedded sand has a flat planar crossbedding. These sediments are the result of the migration of bars, overlain by laminar flows, in a braided or low-sinuosity river flowing in a back-shore/coastal plain environment. The sequence ends with a ruditic episode represented by debris flow deposits consisting of rounded boulders and cobbles in an abundant sandy matrix. This deposit is discontinuous and is capped by a dark red paleosol.

The continental deposits at the top of the sequence are seaward cut by a gently inclined surface marked by an alignment of calcareous boulders with Lithodomus holes (Section 4, Figure 7). The deposit consists of basal

C

M

I I

10 -

I

C

M

I /

I I

Figure 7. First order terrace. Lithostratigraphy of central portion: 1, red/yellowish red soil; 2, pebbly sands; 3, massive silty sands; 4, marine fossil fragments; 5, shallow scours; 6, clasts with Lithodornus holes; 7, bedrock; M = marine environment; C = continental

environment. For section locations see Figure 3

234 L. CAROBENE AND G. FERRINf

conglomerates with large well rounded clasts in a tightly packed gravel matrix. The conglomerate passes upwards to an extremely well sorted coarse-grained sand with conglomeratic levels interbedded. This deposit passes abruptly to a continental, 1 m thick, rubified level consisting of heterometric clasts, mainly angular, in a sandy matrix. The intersection between this erosional surface and the alluvial deposits is the shoreline of a subsequent moving transgression.

The stratigraphic situation of the terrace outer edge (Figure 8) is characterized by a variable thickness of the terrace sedimentary cover, thickening northwards. Usually the contact with the underlying metamorphic bedrock is not clearly exposed, but one section (8 in Figure 8) shows a conglomeratic horizon at the point of maximum thickness. Lower members are formed of fine-grained sand in layers 10cm thick dipping 20" seawards; this sand member is covered by alternating fine- to medium-grained, parallel to crossbedded, sand and gravel with rounded clasts. The deposit has been attributed to a delta front, its location corresponding to a paleovalley cutting the terrace (Figure 5). The delta deposit changes into a horizon of massive medium- grained sand with scattered clasts interbedded with graded coarser horizons. Locally, the sand horizon is covered by a micro-conglomerate, well sorted and varying in thickness from 30 cm to 3 m. This conglomeratic horizon is fairly continuous. Locally, massive sands have mottled colour, and include scattered fragments of Mollusca (Ostrea sp.); micropaleontological specimens gave a Lower Pleistocene age (M. L. Colalongo, personal communication, 1990) In the coarser deposit only a few remains of broken shells were found. It is fairly continuous and can be followed along the entire outer edge; sections 7 and 8 show thin beds of coarse materials following the attitude of the axis of the above-mentioned paleovalley (Figure 5). These sandy sediments are typical of an upper shoreface/beach environment; the coarser graded beds interbedded in the massive sands may have originated by deposition of a single high-energy event ('storm layers').

The sequence described above changes abruptly into a massive structureless very fine-grained sandy/silty deposit, locally enriched with coal debris and Pelecypoda remains, interpreted as back-shore/lagoonal environments. Sample LB183, collected at this stratigraphic level on the outer edge (250 m a d . ) , represents the last transgression that affected the high terrace of the M. Carpinoso; micropaleontological analysis indicated the presence of Lamellibranchi and Briozoa remains, and Ostracods. Among the Foraminifera, Cibicides lobatulus and other Cibicides sp. are abundant; also recognized were EterolepaJloridana, Elphidium crispum, Cribroelphidium semistriatum, Ammonia parkinsoniana, Brisalina sp. and Globigerinoides trilobus. The presence of Hyalinea baltica and the reworking of many specimens dates the deposit to the upper part of the Lower Pleistocene (C. Pirini, personal communication, 1990).

The sequence is truncated at the top by a continental debris flow deposit made up of large, well rounded cobbles and pebbles in an abundant sandy matrix and of coarse-grained gravel with scattered pebbles. The deposit is deeply weathered and covered with a reddish brown soil; locally, a more recent soil is present (7, 5YR-3/4; Figure 4).

Discussion. The lithostratigraphic analysis of the sedimentary cover of the terrace demonstrated the presence of different superimposed depositional events separated by unconformities (alloformation-Bosi, 1989) bounded by two diachronous surfaces, namely: a transgression surface cutting the pre-Quaternary bedrock (on the bottom); and a final regressive surface (on the top).

The lack of datable fauna makes it impossible to drawn chronological conclusions about the difference in time between these depositional units, which represent the result of terrace uplift-sea level change interactions. The formation of the wave-cut platform could be related to several sea-level stands during a long-lasting slow subsidence phase of the coastal area (Carobene and Dai Pra, 1991a). This subsidence period is well known throughout the region and is represented by clay deposits of Lower Pleistocene (Emiliano) age characterized by the presence of Hyalinea baltica, Globigerina pachyderrna, Globorotalia injata and Elphidium crispum (Ogniben, 1969).

CONCLUSION

The studies carried out on the terraces outcropping on the area between T. Vaccuta and T. Corvino have provided useful information on the morphology and genesis of the marine terraces, on the nature and erosion of sedimentary covers and on the uplift that occurred in the area during the Quaternary.

280 rn

a t-

A

w -

n I w a

9 1

260 m

c - 3 d?

I---"'

-*

1

2

3

4

5

6

7

8

9

10

11

Figure 8. First order terrace. Lithostratigraphy of outer edge: 1, brown/reddish brown soil; 2, pebbly sands; 3, massive silty sands; 4, marine fossil fragments; 5, laminated pebbly sands; 6, massive sands; 7, conglomerates/sands interbedding; 8, scour; 9, dipping (20")

sandy beds; 10, bedrock; 11, palaeontological sample. For section locations see Figure 3


Morphological features and tectonics Four orders of marine terraces have been distinguished in the area. The oldest shoreline fits with the foot of

M. Carpinoso (Figure 2); its arcuate shape suggests the presence of a narrow embayment up the present Corvino valley, and of a larger gulf northwards across the present Lao and Abatemarco river valleys (Figure 1). Because of its great areal extent the original surface of the terrace was much wider than the present one. The age of the terrace has been fixed from the fossils contained in the sedimentary cover and by correlating the terrace with the clay deposits of Calabrian age (Lower Pleistocene) (Carobene and Dai Pra, 1991a). Moulding of the terrace ended with the strong uplift which occurred at the end of Lower Pleistocene during interglacial progressively lower sea-level stands, as suggested by the alternation of marine and continental sediments in the stratigraphic sequences (Figures 6-8).

The terraces at lower elevations (orders 2-4) are narrower than the first order terrace, with mean widths of 700 m. All are wave-cut platforms covered by thin marine and continental deposits. The second order terrace is the first Middle Pleistocene terrace, probably corresponding to stages 21-17 (Carobene and Dai Pra, 1991a). The fourth order terrace has a Th/U age of >300,000 years (Carobene et al., 1986), probably corresponding to stages 11-9. The present elevation of the terraces above sea level has thus been controlled by uplift of the area in Middle and Upper Pleistocene.

Tectonics and sedimentation The terraces are generally covered by sedimentary deposits of variable thickness (Figure 3) whose basal

portion has a marine origin and the upper portion, continental. Both the facies distribution and the geometry of deposits appear to have been controlled by tectonics; the bedrock in particular is faulted, throws being in the order of tens of metres. Tectonic lineations mark the presence of an elongated subsiding area in the northern portion of the terrace which was occupied by a paleovalley, as suggested by the thickness and nature of the sediments (Figure 8). On the basis of relict morphology it has been possible to identify secondary tributary valleys of the main paleovalley (Figures 5 and 9). The deposit of the first order terrace is composed of at least three transgressive/regressive sequences that can be attributed to three separate high sea-level stands at progressively lower elevations during the time of strong uplift in the area. During regressive phases following glacio-eustatic lowering of the sea and uplift of the area, most of the transgressive deposits were eroded. The sedimentary cover of the three lower orders of terraces is thinner than that of the first order terrace, and on the wave-cut platform relicts of the transgressive marine deposit covered by a continental deposit are visible in places (Figure 3). This is formed of colluvium at the scarp foot and reworked colluvium with local debris flow deposits on the terrace surfaces.

Remodelling of terraces and tectonics After emergence, the terraces were exposed to modification by several agents, including tectonic deforma-

tion. The main agents of terrace remodelling are described below. Running water. The old hydrographic net of the highest terrace (first order) is shown by relict valleys with

a concave profile (Figures 5 and 9) coexisting with the present hydrographic net formed by very deep valleys and gorges. The hydrographic net which formed after the complete emergence of the area (Figure 5 ) has subdivided the terraces into many relict surfaces which often appear as narrow subhorizontal strips on the slopes (Figure 2). At present, the first order terrace is bounded by high erosion scarps both northwards and southwards (Figure 9). In the central part of the area, between Cirella and Diamante, eroded materials have accumulated to form a band of loose debris fans (Figure 2).

Weathering. The marine terraces of the Calabrian coast formed over a period of at least 1 Ma, during which many climatic changes occurred, as shown by the paleoclimatic curves of Quaternary (Williams et al., 1988). In general, the marine deposits overlying the wave-cut platforms are deeply weathered into well developed soils that are truncated by several metres. The continental silt deposits that commonly cover the marine deposits display soils brown or red in colour, which are also cut by erosion (Figure 4).

Wave action. The sea also played a role in remodelling terraces. In fact, each new high sea-level stand has had its own cliff that eroded the outer edge of the previous terrace (which was raised to a higher elevation


Figure 9. Morphotectonic map. Fault-induced features: 1, large fault scarp; 2, small fault scarp; 3, reversed slope; 4, saddle; 5, fluvial bend; 6, straight valley. Induced uplift features; 7, relict valley 8, gorges; 9, erosional scarp edge. 10, Contour lines; 11 , relief boundary

because of the uplifting of the area). Thus, the present terraces appear less wide than they were originally. Faulting efect . The Middle to Upper Pleistocene uplift was accompanied by three main fault and fracture

systems (Figure 10): the WNW-ESE or NE-SW trending system, the ESE-WNW trending system, and the N-S trending system. The recent activity of all the systems is demonstrated by morphotectonic evidence (Figure 8). Fault activity would have been strong initially, reducing over time: the second, third and fourth order terraces are not faulted very much.

It can thus be concluded that the sedimentological and morphological study of the raised marine terraces of the Tyrrhenian coast between Cirella, Diamante and M. Carpinoso provides valuable information on the geomorphological evolution, climatic change and tectonic activity along this sector of the Calabrian coast for most of Pleistocene.


Figure 10. Neotectonic map: 1, Quaternary faults; 2, master joints; 3, lineations

ACKNOWLEDGEMENT

The research has been supported by MURST 40% and 60% Programmes (University of Caiabria).

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Bluck, B. J. 1974. ‘Structure and directional properties of some sandur deposits in southern Iceland’, Sedimentology, 21, 533-554. Bosi, C. 1989. ‘Considerations and proposal on morpho-pedolithostratigraphic units in Quaternary studies’, I1 Quaternario, 2(1), 3-9. Carobene, L. and Dai Pra, G. 1991a. ‘Genesis, chronology and tectonics of the quaternary marine terraces of the Tyrrhenian coast of

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Carobene, L. and Ferrini, G. 1990b. ‘Morphological, sedimentological and tectonic features of Diamante-M. Carpinoso marine terrace flight (Tyrrhenian coast of Northern Calabria)’, in Sorriso Valvo, M. (Ed.), IGU-Comtag ’90, Int. Symposium on Geomorphology of Active Tectonics Area, Field Exursion Guidebook, CNR-IRPI Geodata.

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