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Quaternary International 232 (2011) 132e143

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Quaternary International

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Relative sea level change in western Istria (Croatia) during the last millennium

Sanja Faivre a,*, Eric Fouache b, Matthieu Ghilardi c, Fabrizio Antonioli d, Stefano Furlani e,Vladimir Kova�ci�c f

a Faculty of Science, Department of Geography, Maruli�cev trg 19/II, 10 000 Zagreb, CroatiabUniversité Paris Ouest Nanterre la Défense, EA 375 GECKO and UMR 8591, 200 Avenue de la République, 92000 Nanterre, FrancecCEREGE, UMR 6635, CNRS. Europôle Méditerranéen de l’Arbois BP80, 13545 Aix-en-Provence CEDEX 04, Franced ENEA National Agency for New Technologies, Energy and Environment, Via Anguillarese 301, 00060 S. Maria di Galeria, Rome, ItalyeDiSGAM, Dipartimento di Scienze Geologiche, Ambientali e Marine, via Weiss 2, 34127 Trieste, ItalyfNative Museum of Pore�c, Decumanus 9, 52 440 Pore�c, Croatia

a r t i c l e i n f o

Article history:Available online 11 June 2010

* Corresponding author. Tel.: þ385 1 48 95 422; faE-mail addresses: sfaivre@geog.pmf.hr (S. Faivre

(E. Fouache), ghilardi@cerege.fr (M. Ghilardi), fabri(F. Antonioli), sfurlani@units.it (S. Furlani), vladimir.k

1040-6182/$ e see front matter � 2010 Elsevier Ltd adoi:10.1016/j.quaint.2010.05.027

a b s t r a c t

Relative sea level change occurred along the western coast of the Istrian peninsula in Croatia. Sedimentsfrom two cores located in the bay of Santa Marina and Soline Bay have been analyzed for microfaunal andsedimentological investigations. Chronostratigraphical evidence was obtained from 14C dating oflagoonal shells (gastropods). From the sedimentological and paleo-environmental analysis, 4300 years ofcontinuous deposition in a shallow marine environment was determined. At around 550 cal BP, marinesedimentation changed to continental. Consequently, the initial sedimentation rate of 0.7 mm/y changedto 2.36 mm/y after 550 cal BP. Those upper deposits of continental origin are today partly submerged.The data were further compared with a geophysical model which allows the prediction of the local sealevel curve. As the results from the cores are largely below the curve, tectonic subsidence of the area isconfirmed. Radiocarbon analysis allowed the age of the shells to be related to the age of the submergedtidal notch that occurs almost continuously some hundreds of meters south-eastwards, from the Gulf ofTrieste to the Dalmatian coast.

� 2010 Elsevier Ltd and INQUA. All rights reserved.

1. Introduction

Recent sea level rise along the Istrian shores (Fig. 1) has beensurveyed by many researchers (e.g. Gnirs, 1908; Andrija�sevi�c, 1910;Degrassi, 1955; Vrsalovi�c, 1979; Kozli�ci�c, 1986). Historians andarchaeologists have estimated the degree and rate of the last twomillennia of relative sea level change from the position of thesubmerged archaeological remains. Degrassi (1955) suggested thatthe sea level was 1.5 m lower than nowadays during Roman times,but without considering precise measurements and corrections,while Vrsalovi�c (1979) andKozli�ci�c (1986) proposed a change of 2m.Using geological and archaeological indicators, �Segota and Filip�ci�c(1991) calculated that the sea level between the XI-II century BCcould have been between 3.1 and 1.96 m below present sea level.

The presence of a submerged tidal notch along the Croatianshore, located at �0.5 and �0.6 m below the recent mean sea level,

x: þ385 1 48 95 440.), eric.G.fouache@wanadoo.frzio.antonioli@casaccia.enea.itovacic@poup.hr (V. Kova�ci�c).

nd INQUA. All rights reserved.

was first reported by Pirazzoli (1980), who suggested a submersiondue to a co-seismic event. In the area of RijekaBay, Benac (1989,1992) first noted the presence of a notch whose position variesfrom �0.5 to �1.1 m below the mean sea level. This variation isinterpreted as a consequence of the differential tectonic subsidenceof the various parts of the Bay.

Fouache et al. (2000) worked on thewesternpart of Istria, on theMt.Velebit shoreline and on the islands of Pag and Rab wherea submerged notch was found �0.5 to �0.7 m below the presentsea level. Datawere further correlatedwith archaeological markers.Those investigations show that the tidal notch in the Istria andKvarner area has a regional extent (Faivre and Fouache, 2003) andthat this area represents a relatively homogeneous unit. Thenotches in RijekaBay and Vinodol Channel weremeasured by Benacet al. (2004, 2008) andwere related to the biological mean sea level.Further research was carried out in the central and southern partsof the eastern Adriatic, working primarily on the submergedarchaeological remains which indicate a submersion of at least1.5 m in 2 ka (Fouache et al., 2005). The submerged marine notchesin the Istrian area and in the Gulf of Trieste (max depth �2.6 m)have also been studied by Antonioli et al. (2004, 2007) and Furlaniet al. (2011) as well as the archaeological markers (Fouache, 2006;

Fig. 1. Main geomophological properties; legend: A. Erosional plain; B. Mountain ridges of �Ci�carija and U�cka; C. Eocene flysch foothill; 1. structural escarpment; 2. canyon; 3.Quaternary buried valley; 4. polje with thick terra rossa deposits; 5. paleo valley; 6. spring; 7. swallow-hole 8. loess deposits.

S. Faivre et al. / Quaternary International 232 (2011) 132e143 133

Antonioli et al., 2007; Radi�c Rossi and Antonioli, 2008). New find-ings regarding notch distribution in the southern part of theCroatian coast have been indicated in Faivre et al. (2010).

The fairly continuous occurrence of a submerged tidal notchalong the Istria and Kvarner area at a depth between �0.5 and�1.1 m led the authors to drill two boreholes in order to indirectlyestimate the time of its formation. Two small, relatively shelteredbays along the shores of western Istria which have not beenaffected by significant deformation were selected. Although theobtained 14C ages represent the only dates on the submerged notchthat occurs along the Eastern Adriatic coast, and have been indi-rectly obtained, they allow better understanding of the late Holo-cene relative sea level change in western Istria.

2. Geological and geomorphological overview

Istria belongs to the NW part of the ancient Adriatic CarbonatePlatform. This platform is composed of a carbonate depositsuccession which is very thick (between 3500 and 5000 m), inplaces even more than 8000 m (Vlahovi�c et al., 2002, 2005). The

Istrian sequence consists predominantly of carbonate rocks rangingfrom Middle Jurassic (Late Dogger) to Eocene, with subordinateMiddleeUpper Eocene clastic rocks composed of flysch andcalcareous breccias (Ti�sljar et al., 1998; Veli�c et al., 1995, 2003). Atthe top, the Quaternary terra rossa and loess close the sequence.

The geomorphological peculiarities can easily be discerned fromthe local colloquial names. The Red Istria e the southern andwestern Istrian erosional plain, named after the terra rossa, the Greyor Green Istria e in its central part characterized by stronglydissectedMiddleeUpper Eocene flysch foothill, and theWhite Istriae in the eastern, north-eastern and north Istria, characterized bykarstified outcrops of “white” Cretaceous e LowereMiddle Eocenelimestones. The White Istra is represented by mountain ridges of�Ci�carija (1272 m) and U�cka (1396 m), which is, together with thecentral flysch area, particularly strongly expressed in relief (Fig. 1).

Red soil or terra rossa is the most common soil type in thewestern part of Istria, and it developed on Jurassic-Cretaceous-Paleogene carbonate rocks. In most cases, terra rossa has poly-genetic origins and was formed by mixing of insoluble residue ofcarbonate rocks with weathered and eroded loess and flysch

S. Faivre et al. / Quaternary International 232 (2011) 132e143134

sediments (Durn, 1996; Durn et al., 1999). The thickness of thesedeposits depends on its position with respect to relief. It fills cracksand dolines and forms discontinuous surface layers up to 2.5 mthick. In karst depressions, accumulations of terra rossa are alsofound in the form of pedo-sedimentary colluvial complexes whichcan be up to 14m thick. Climatic and glacioeustatic changes, as wellas tectonic movements during Quaternary have influenced recentposition of terra rossa and its mineralogical composition (Benac andDurn, 1997).

The youngest deposits, which are still actively forming, arerepresented by colluvial and alluvial sediments accumulated in theriver valleys. Three main rivers drain the Istrian peninsula: Drag-onja, Mirna and Ra�sa (Fig. 1). Their mouths existed as large anddeep estuaries up to historical time. The Dragonja and Mirna rivermouths are today completely buried due to the high sediment inputsupplied by water flow. The Ra�sa River mouth is still in a marinebay, but today it experiences rapid progradation (Benac et al., 1991;Jura�ci�c et al., 1995). The neotectonic movements as well as sea leveloscillations during the Quaternary controlled the erosion intensity.During the last marine transgression the sea penetrated far into theland allowing the flooding of the valleys. Under postglacial condi-tions or rapid sea level rise, the dominant geomorphic processshifts from erosion to deposition. Finer sediments were depositedin newly flooded bays and estuaries. Decelerating sea level rise atabout 7000 calibrated (cal) BP (Antonioli et al., 2007) createdfavourable conditions for progradation.

The Istrian Rivers originate in the flysch area, where thehydrographic network is well developed. Further downstream, theypass through karst areas, often in canyons, which do not contributesignificantly to the river-borne material (Janekovi�c et al., 1995). Thesignificant denudation of the flysch provided a great volume ofsediments which decreased the depth to the sea floor causing theshifting of the river mouth (Benac, 1992).

Unlike other karst rivers, carrying predominantly dissolvedmaterial, the Mirna River carries a substantial amount of sedi-ments classified as clayey-silts. The Mirna River has almostcompletely buried the lower part of the valley and transformedit into swamp. Today, only a small bay and a few small lagoonsremain. Some 2000 years ago, the Mirna River mouth was muchfurther inland than today. Historical data confirm the existenceof sea water at the foot of Motovun hill (Kandler, 1875; Alberi,1997). The sedimentation rate in historical time can be calcu-lated using several lines of evidence. In 1994, at the base of theMotovun hill (formerly called Montona), a log was found 9 mabove sea level and �4.5 m below the valley level of today.From 14C analyses the date the log was cut is estimated as415 � 65 BP (Rubini�c et al., 1999; Prodan, 2001; Miloti�c, 2004).This means that the river valley has risen 4.5 m in 460 years(1535e1994) and that the sedimentation rate was approximately10 mm/y.

The historian Luigi Morteani (1895) wrote, in his work on thehistory of Motovun, about degradation of oak trees due to the greatquantity of river deposits. In the year 1818, 26,000 trees weredestroyed. He stated that 0.80 m of deposit accumulated within 55years. From this data the sedimentation rate comes to 14.5 mm/year. Other historical evidence indicates similar sedimentationrates, around 10 mm/y on average, with other possible periods ofhigher sedimentation rates.

Recent geotechnical investigations (Institut graCevinarstvaHrvatske, 1998), near the Mirna River mouth, show that thebedrock is, for the most part at a depth greater than 100m, while inthe central part of the valley it increases up to 160 m. The physi-ography of the valley has radically changed in the 20th century dueto human interference to avoid flooding. After regulations, floodingand sedimentation was significantly decreased (Rogli�c, 1974).

3. Geodynamic setting

The oldest records of tectonic activity in Istria have been foundin the Upper Bathonian, phase D1 of Veli�c et al. (2003). From thattime Istria underwent different tectonic phases. The WesternIstrian Anticline formed in the Early Cretaceous, and it is one of themost important geological structures of the Istrian peninsula(Pol�sak and �Siki�c, 1973; Marin�ci�c and Mati�cec, 1991; Mati�cec, 1994),(phase D2 of Veli�c et al., 2003). The effects of the Cretaceoustectonism are still visible in the Istrian peninsula, whereas theyhave beenmostly destroyed by latter tectonic activity in other areasof the Adriatic Carbonate Platform (Mati�cec et al., 1996).

Tectonic events of the Upper Cretaceous started the disinte-gration of the former carbonate platform and marked the end oftypical productive carbonate platform sedimentation. The Eocenetransgression was a consequence of a new deformation phase(phase D3 of Veli�c et al., 2003). The intensity of these movements iswitnessed by the formation of the flysch basins, which are theconsequence of the regional compression of the area. Hence, the D3deformation phasewas the decisive factor in the tectogenesis of theDinarides.

The carbonate complex of southern Istria was not intensivelydeformed, except for mild refolding or occasional reactivation ofinherited faults. In contrast, overlying deposits were affected bysignificant compression by the overthrusted structures of �Ci�carija,characterized by SW vergence.

Neotectonic deformation (phase D4 of Veli�c et al., 2003) inthe whole Dinarides is a consequence of the regional NeSdirected compressional stress (Prelogovi�c et al., 2004). This stresswas accommodated by formation of new neotectonic structuresand partly by reactivation or rotation of previously formedstructures.

Istria is not considered a seismically active area (Herak andHerak, 2006) as seismicity is shallow and earthquakes are locatedwithin the upper crust. The most important epicentral zone liesbetween Senj, Vinodol, Rijeka and Ilirska Bistrica. The U�cka e

Trieste fault zone (Fig. 2), 1e3 km wide, is the boundary faultbetween weakly and strongly deformed parts of the Adriaticmicroplate (Prelogovi�c et al., 2003, 2004).

4. Location of the cores

In order to estimate the age of the submerged tidal notches andimprove previous results (Fouache et al., 2000, 2004; Faivre andFouache, 2003; Antonioli et al., 2007), two bays were selected fordrilling. They are located in the western part of Istrian peninsula,which has not been affected by substantial deformation in the lateQuaternary (Fig. 3). Structurally, this area is characterized by almosthorizontal to slightly inclined layers. On this carbonate erosionalplain, shallow and large depressions prevail, with numerousdolines, isolated small hums, small valleys, ponors and caves. Theplain is inclined westward and most of the waters flow in thatdirection (Fig. 1). As previously explained, the bays are situated inthe environment of increased sedimentation which occurred inIstria during the past centuries.

The cores were drilled in the inner parts of the bays, at themouth of two small seasonal streams (Fig. 3). Those bays have beenselected for drilling due to the expected lower sedimentation rates,compared to those in the Mirna River valley, with the aim to obtaingreater age ranges in smaller profiles. The first core is located closeto the Mirna River valley, in the Santa Marina Cove, formed withinthe Upper AlbianeUpper Santonian megasequence (Veli�c et al.,2003), and the second one near the Limski Channel, at the SolineBay, formed within the Bathonian-Lower Kimmeridgian mega-sequence (Veli�c et al., 2003).

Fig. 2. Earthquake epicentres in Istra and Kvarner area from 1500 to 2003. (mainshocks with magnitude > 5.0 or with intensity > VII MCS scale after Herak and Herak (2004) andHerak et al., 2005)) with main regional faults after Prelogovi�c et al., 2004).

S. Faivre et al. / Quaternary International 232 (2011) 132e143 135

The seasonal stream at the Santa Marina Bay is around 1 kmlong (Fig. 4a), while the one in the Soline Bay is 2 km long (Fig. 4b).At the mouth of the periodic stream, the Santa Marina and theSoline Bay are 58 and 160 m wide respectively.

The studied area is a micro-tidal, low energy environment. Theaverage tidal amplitude is 0.477 m (date from Rovinj mareograph).The bays have relatively sheltered positions, exposed only towestern winds which are not frequent and not strong because ofthe short fetch.

5. Materials and methods

Two 40 mm diameter vibracores (S1 and S2) up to 4.5 m depthwere drilled in July 2005 (Table 1). The boreholes were locatedwith DGPS measurements. Sedimentological analyses were carriedout at the Laboratoire de Géographie Physique de Meudon (UMR8591 e Centre National de la Recherche Scientifique, France).Grain-size analyses were conducted at 5 cm intervals. The sampleswere mixed with a dispersing agent (0.5% sodium hexameta-phosphate) and left in deionised water for 2 h to disperse the clayparticles, and then exposed to ultrasound. The grain-size distri-bution was measured using a Coulter LS 230 laser granulometerwith a range of 0.04e2000 m, in 116 fractions. The calculationmodel (software version 2.05) uses Fraunhofer and Mie theory,which works down to a grain-size of about 0.04 mm (Buurmanet al., 1996).

The chronostratigraphy of the cores was determined using fiveradiocarbon dates undertaken on in situ marine-lagoonal shells

(gastropods). These analyses were performed at the PoznanRadiocarbon Laboratory in Poland. 14C ages were subsequentlycalibrated using the Calib 5.01 Software without additional delta R,as established in Siani et al. (2000). At the light of the variability ofdelta R and the few data published for the Adriatic Sea (Siani et al.,2000) the original 14C values using the fossils living in shallowmarine water were only calibrated using the Calib 5 program(Stuiver et al., 2005).

Elevation measurements with respect to the mean sea levelwere performed through the use of optical methods (SalmoiraghiErtel automatic level), following themethod suggested by Antonioliet al. (2007). The surveying included: 1) measurement of the depthof the marker with respect to the local sea level at the time ofsurveying. Values reported in Tables 2 and 3 represent the meanvalue of multiple measures; 2) correction of surveyed measureswith respect to the tide gauge data collected at the time ofsurveying. Data are reported in Tables 1 and 2; 3) comparison ofpredicted (Antonioli et al., 2007) and observed sea level positionof the markers, which corresponds to the relative sea level changeat each considered location. The tectonic stability of an areacorresponds to data fitting the predicted sea level curve, whiledown lift or uplift is supposedwhen the elevations of themarkers isdifferent from the predicted curve. Error bars for the elevation andage values of the sea level markers have been provided in order toconsider the inaccuracy of measures. Moreover, the errors con-nected to the use of lagoon fossils as sea level markers areconsidered, because the elevation of samples could be partly due tosedimentation rates.

Fig. 3. Hypsometrical map with location of the boreholes.

S. Faivre et al. / Quaternary International 232 (2011) 132e143136

The use of these fossils, although generally affected by errorsdue to their large range of elevation habitat (2 m) and bioturbationactivity, could be considered useful in this case because thegeometry and in particular the bathymetry of the valley, influencedby the flat and few deep bedrock, was similar during the lateHolocene, decreases the error connected to this marker.

The measurements were reduced to the mean sea level applyingtidal corrections at the surveyed sites, using the data of the tidegauge of Trieste. Elevation measurements are given (Stravisi andPurga, 2005) with respect to the Italian reference plane networkof the Istituto Geografico Militare (Genova Mean Sea Level 1942;Gamboni, 1965).

6. Results

Both core profiles of Holocene sediments reveal a transitionfrom marine-lagoonal to sediments of continental origin. At SolineBay the bedrock was found at 3.9 m, whereas at Santa Marina at2.3 m below mean sea level. The lowermost unit in Santa MarinaBay is represented by 0.59 m of very dark grey stiff clays, followed

by 1.25 m of dark grey marine clays. These marine sediments arecovered by continental deposits represented by 0.72 m of red claysfollowed by 0.04 m of soil. The whole core is 2.60 m long. In SolineBay themarine deposits are represented by 2.81m of dark grey clayfollowed by 1.29 m of red clays continental deposits and 0.10 m ofsoil. The Soline core is 4.20 m long (Fig. 5).

The gastropods determine the environment of deposition: Bit-tium sp., Cerithium sp. and Rissoa ventricosa were identified(Table 2). Those shells found in the boreholes suggest shallowmarine-lagoonal conditions of low energy.

The results of the sedimentological analysis reveal the almostuniform characteristics of both cores. The modal index reflects lowvalues, around 5 mm, homogeneous all along the cores. Clays arewidely represented. There are no strong variations except in theuppermost parts of the boreholes, where some terrestrial influ-ences slightly modify the modal index (10 mm). The presence ofsome fine silts mixed with fine clays in the upper part of theterrestrial deposits can be explained by colluvial processes. Thegrain-size analysis reveals a bimodal distribution and minor fluc-tuations. Several fragments of limestone are bedded within the

Fig. 4. A) Santa Marina (core S2) and B) Soline Bay, (core S1).

Table 1Borehole ID.

Core ID Latitude Longitude Length (m) Elevation aboveMSL/DGPS (cm)

Date and time (h)

Soline Bay e S1 N 45�06059.100 E 13�37027.800 4.2 30 8.07.2005. e 11.00SantaMarina Bay e S2 N 45�17007.800 E 13�36006.100 2.6 30 7.07.2005. e 10.30

S. Faivre et al. / Quaternary International 232 (2011) 132e143 137

sediments in the lowermost part of the core and indicate theproximity of the bedrock. These deposits are typical of a shallowmarine environment. Both malacofaunal identification and grain-size analysis indicate generally a low energy environment. Theintensive red colour of the continental deposits implies theirformation by the erosion of terra rossa from the carbonatesurroundings. Colluvial processes affecting the mainland feed rivercatchments and seasonal streams.

Radiocarbon dates were performed on five marine gastropods(Tables 2 and 3), found at different depths in the two boreholes(Fig. 6). Two of them indicate a similar age at very close depths(Soline 2 and 3). The R. ventricosa (Santa Marina 4) from the core S2and the Bittium (Soline 1) from Soline Bay were found at the samedepth, but the ages are different. However, a relatively goodagreement between age and depth of the samples is apparent.Bittium used as sea level marker (Lambeck et al., 2004), also inassociation with R. ventricosa (Peres and Picard, 1964) whoseposition with respect to mean sea level, between 0 and 2 m(Gravina et al., 1989), represents a good sea level indicator.

Table 214C analyses of the marine gastropods found in cores S1 and S2.

Sample Lab code Uncorrectedaltitude

Age 14C (BP)

Soline 1 Poz 15845 �1.43 970 � 30Soline 2 Poz 15846 �4.16 4640 � 35Soline 3 Poz 15847 �4.17 4635 � 30Santa Marina 4 Poz 15849 �1.46 1395 � 30Santa Marina 5 Poz 15850 �2.59 3105 � 30

Sedimentation rates calculated from the 14C dating for themarine and continental sediments are 0.7 mm/y and 2.36 mm/yrespectively. At present, continental deposits are partly submerged.They are 0.98 m below the mean sea level at Soline Bay and 0.46 mbelow mean sea level at Santa Marina Bay.

7. Discussion

The results of the sedimentological analysis reveal a changefrom shallowmarine to deposits of continental origin. The lagoonalsediments show a continuous and regular accretion during sedi-mentation in a shallow marine, low energy environment. Sedi-mentation rate calculated from 14C dating for the marine sedimentsis 0.7 mm/y, whereas for the continental sediments it is 2.36 mm/y,but it seems to be difficult to distinguish whether the rates area consequence of a major erosion event or of a gradual deposition.Those continental deposits are today partly submerged, but as thedeposition was extremely fast their deposition entirely above sealevel is uncertain.

Cal age sigma 1 Fossil Core

528e599 Bittium S1 Soline4815e4898 Cerithium S1 Soline4803e4893 Bittium S1 Soline904e970 Rissoa ventricosa S2 Santa Marina

2830e2930 Rissoa ventricosa S2 Santa Marina

Table 3Depths and ages of marine gastropods from cores with the Antonioli et al., 2007 predicted curve for the Brijuni coastal area data and down lift rates which derive.

Sample Uncorrected altitude Corrected HFor tide �30 cm

Ø Cal age sigma 1 Predicted curvefrom Antonioliet al., (2007)

Vertical subsidencerates in mm\y errorbars between �0.05and �0.2

Soline 1 �1.43 �1.13 563,5 � 35 �0.05 �1.92Soline 2 �4.16 �3.86 4856,5 � 41 �1.57 �0.45Soline 3 �4.17 �3.87 4848 � 45 �1.66 �0.47Santa Marina 4 �1.46 �1.16 937 � 33 �0.01 �1.23Santa Marina 5 �2.59 �2.29 2880 � 50 �0.69 �0.55

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Taking into account the sedimentation rates of marine sedi-ments, it is possible to see a constant 0.20 m difference in depth forthe same age horizon between the two cores. By calculating therelative sea level for 2000 BP for both cores, the position ofthe horizon of the same age in the Soline core is 20 cm lower than inthe Santa Marina core.

Fig. 5. S1 and S2 core profiles (ages of marine gastropods are indic

In the Istria and Kvarner areas, the submerged tidal notch iswidespread. In the western part of Istria the notch depth variesfrom �0.50 m to �0.70 m. The tidal notch in the Limski Channelis �0.70 m deep (Figs. 7 and 8). As the Soline Bay core S1 isalmost at the entrance of the Limski Channel, the tidal notchcan be well correlated with the core sediments. At Verudela

ated on the right side of the cores as given in Tables 2 and 3).

Fig. 6. Marine gastropods from the cores Legend: 1. Bittium reticulatum, S1 (Soline 1); Cerithium sp., S1 (Soline 2); Bittium reticulatum, S1 (Soline 3), Rissoa ventricosa, S2 (SantaMarina 4) Rissoa ventricosa, S2 (Santa Marina 5).

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Cape (Fig. 1), for example, the notch is 0.20 m higher (�0.50 m)than in Soline Bay (Fouache et al., 2000). Therefore, the differ-ence in depth between notches (0.20 m) can be compared withthe 0.20 m difference depth of similar ages found in the twocore profiles. If the notches formed simultaneously, as assumed,then the difference in subsidence arose after the notch forma-tion. Consequently, the well-preserved notches points to greatervalues of subsidence after 550 cal BP.

As the notches could not be formed before 2000 BP because thesea was still too low, formation occurred between 1000 years and500 BP. After 500 BP, the sedimentation changed from marine tocontinental.

In order to explain the elongated shape of the notches in theKvarner area and the excellent preservation of the notch roofs,Benac et al. (2004, 2008) have suggested that there was a longer

Fig. 7. Thedepthof tidal notches in the Istria andKvarner areaLegend:1. Faultswhichdelimit tfault; 5. Notches measured by Pirazzoli (1980); 6. Notches measured by Benac et al. (2004, 20

period of quite slow relative sea level rise, prior to the rapidsubsidence. This relatively very slow rise or, possibly, even sea levelstagnation to around 500 year BP allowed the development of wellexpressed tidal notches and also the sedimentation of continentaldeposits in the cores.

On the basis of the highly accurate GPS measurements,a geodetic model of recent tectonic movements on the studied areawas established by Altiner (1999). The model encompasses 15 GPSpoints in Croatia. For themeasurement of the vertical component ofmovement, two different models were constructed: an absoluteand a relative model. For the computation of the absolute stationco-ordinates and the velocity field, 4 IGS stations (InternationalGNSS Service, formerly the International GPS Service) wereemployed in the processing (Wettzel, Matera, Graz and Zimmer-wald) fixing their co-ordinates and velocities. The results give the

he regional structural units; 2. Faultswithin structuralunits; 3. Reverse fault; 4. Strike-slip08); 7. Notches measured by Fouache et al. (2000), and Faivre and Fouache (2003).

Fig. 8. The notch at the Limski Channel �0.70 m below mean sea level (7.07.2004).

Fig. 9. Vertical velocities computed within the 1994e1996 CRODYN GPS campaignswith fixed co-ordinates of the ISG stations Wettzell, Graz, Matera and Zimmerwald(modified from Altiner, 1999).

S. Faivre et al. / Quaternary International 232 (2011) 132e143140

velocities of the stations within the CRODYN network (Croatiangeodynamic project, �Coli�c et al., 1996) relative to the fixed IGSstation on the Euroasian plate (Altiner, 1999). The velocitiesobtained by that model depend of course on the assumed motionsfor the fixed stations. The GPS measurements, in spite of the smallnumber of points and a very short period of measurement (1994/1996), give further support to this rate of subsidence. The ratesobtained are important and can be described as follows: Rovinj e6.5 mm/y, Pula e 2.3 mm/y and Malija e 2.7 mm/y, (Fig. 9) (Altiner,1999). Rovinj, which is near Limski Channel and Soline Bay, issubsiding more rapidly than Pula near Verudela Cape (the notchsubsided 20 cm less), or Malija, in the hinterland of Santa MarinaBay. Consequently, Soline Bay is also subsiding at a higher rate thanSanta Marina Bay, as observed from the cores. Thus, the relativemovement velocities (the relative values) are in accordance withthe results from the cores and the notches. The results show a goodcorrelation with the Altiner (1999) absolute model of the GPSmeasurement, while his relative model does not relate to any of theevidence within the field data.

High rates of subsidence are in accordance with these results,because if the subsidence is slow it would destroy the notch. So thesubsidence must exceed the corrosion and bio-erosion ratesvarying from 0.1 to 1 mm/y (Torunski, 1979; Furlani et al., 2009). Itmust be emphasized that there is no recent tidal notch along theIstrian shores, meaning that there is also no recent relative sea levelstabilization or that the subsidence is very young (Antonioli et al.,2007; Benac et al., 2008).

The Istria area cannot be considered seismically very active(Fig. 2; Herak and Herak, 2006). Seismicity in the region is shallow;earthquakes are located within the upper crust. Thus, after stabi-lization and notch formation, points are subsiding at different rates,

in accordance with tectonic structure and GPS measurements. Thevery low seismicity of the region suggests gradual subsidence thenepisodic, co-seismic subsidence. A regionally subsided notchshould have a regional cause, particularly in a low seismic setting.Consequently, the problem of the origin of this subsidence is stillunder debate. However, this subsidence may possibly be related tothe flexural banding of less deformed part of the Adriatic plate infront of the advancingWSWpropagating deformational front of theExternal Dinarides.

The sea level change is the sum of the eustatic, glacio-hydro-isostatic and tectonic factors. The first is global and time dependent,while the other two also vary according to location (Antonioli et al.,2007). According to the Lambeck geophysical model (Antonioliet al., 2007) the predicted sea level in the North Adriatic area,calculated for Brijuni along the coast of the Istrian peninsula, is�1.7 m at 5 ka BP, �1.2 m at 4 ka BP and �0.3 m at 2 ka BP. Thesevalues are largely above the core results, and therefore this differ-ence is again attributed to the tectonic subsidence of the area(Fig. 10).

A multi-proxy study of the Holocene sediment core from thewestern side of the central Adriatic (Oldfield et al., 2003) shows thatthe most striking episodes of deforestation and expanding humanimpact begin around 3600 BP (Late Bronze Age) and around 700 BP(Medieval). Each led to an acceleration in mass sedimentation andan increase in the proportion of terrigenous material, reflecting theresponse of surface processes to widespread forest clearance andcultivation, although climatic effects may also have been important.Sedimentation rates roughly quadrupled between 1100 and 700years ago. The core extracted from the �Cepi�c polje, in Istria, showsthe increased values of sedimentation from 4000 BP, that is, thesedimentation tripled (Balbo et al., 2006). Unfortunately, theuppermostparts of the �Cepi�c polje corewerenot analyzed.However,different historical data confirmed that the sedimentation rates areparticularly high after 700 BP. At Motovun hill the sedimentationrate between 1535 and 1994 was 10 mm/y (Rubini�c et al., 1999;Prodan, 2001; Miloti�c, 2004). In the period between 1763 and 1818at the end of LIA it reached 14.5 mm/y. These high rates can be alsorelated to the increased anthropogenic pressure on the area, prin-cipally due to intensedeforestation.High sedimentation rates in thatperiod were also obtained from analyzing the changes of the rivermouths on the old topographic maps from the years 1771, 1882 and1930 at the Mirna river mouth and particularly at the Ra�sa rivermouth (Benac et al., 2007). The strongest amount of erosion isconnected to the Istrian inland flysch area (Jurak and Fabi�c, 2000;Zorn, 2008), but as shown in this paper it is also important along

Fig. 10. Observed data for Soline (S1) and Santa Marina (S2) core analysis during the last 5 ka, compared with the predicted sea level curve for the Istrian coast given in Antonioliet al. (2007).

S. Faivre et al. / Quaternary International 232 (2011) 132e143 141

the mouths of the coastal seasonal streams. Since the second half of20th century, the sedimentation at the river mouths is attenuatedprobably due to the changes in land use, that is the increase ofvegetation cover in the river basins (Benac et al., 2007).

Increased sedimentation rates in the last centuries, around theMediterranean, were also mentioned by various authors (e.g. Vita-Finzi, 1969). From the example of the Ombrone River delta in Italy,Bellotti et al. (2004) have shown that very high sedimentation ratesoccurred between the 16th and 19th centuries. Pranzini (2001) hasdemonstrated rapid delta progradation of the Arno and Ombronerivers between the Early Middle Ages and the 18th century. Thisincreased river sediment input is explained as a consequence of thewidespread deforestation within the catchment area. The samecauses were revealed by Marchetti (2002), explaining the pro-gradation of the River Po delta, which was also shown by Stefaniand Vincenzi (2005). An extraordinary increase in progradation inSouthern Iberia (Spain), was also detected along both the Atlanticand Mediterranean shorelines ca. 500 BP, particularly after the 17thcentury (Goy et al., 1996).

According to profiles, the relative sea level 2000 BP was around1.7 to 1.9 m lower than today. However, it must be also stressed thatthe core samples yield mainly lower limits to past sea level(Antonioli et al., 2007). Consistent with the preserved shape of thesubmerged notches, the progradation of the river mouths (Mirnaand Ra�sa), and the deposits of continental origin at the top of thecores, very slow sea level rise or even sea level stabilization prior torapid subsidence is assumed.

8. Conclusions

From the sedimentological and paleo-environmental analyses,4293 years of continuous deposition in shallow marine environ-ment was determined (from 4856 to 563 cal BP). At around 550 calBP marine sedimentation changed to sediments of continentalorigin. Those continental deposits are today partly submerged. Thisterrestrial dynamic is still active today.

A relatively good agreement between age and depth of thesamples is also apparent. The fossil shells (Cerithium, Bittium and R.ventricosa) found at low depths indicate a very rapid subsidence ofthe area, younger than 1 ka cal BP. Before 550 cal BP the sedi-mentation rate was 0.7 mm/y while after 550 cal BP it increased to2.36 mm/y. Comparison between dates older than 2 ka (2880, 4856

and 4848 cal BP) with the Lambeck model used in Antonioli et al.(2007) indicates a tectonic down drop rate of about �0.51 mm/y,which is well comparable to archaeological data (Antonioli et al.,2007). The younger than 2 ka dates (937 and 563 cal BP) showmuch higher subsidence rates according to the model, around�1.58 mm/y (Table 3).

Based on the evidence, the presently submerged tidal notcheson the Istrian peninsula and Kvarner area could have been formedbetween 1000 and 1500 AD in an environment of very slow sealevel rise or almost stillstand during the Medieval Warm Period.Then circa 1500 AD, as revealed by geomorphological, geologicaland historical evidences sedimentation rates increased and a strongprogradation of river mouths occurred. The increased sedimenta-tion and the change to the continental deposition are also observedin the cores which can be dated as younger than 550 cal BP. Theconsequence of this relatively stable sea level is the formation ofroof notches which are found in Istria and Kvarner. These orders ofevents perfectly fit the morphology of the notch. This was thenfollowed by rather quick subsidence, otherwise the notch would bedestroyed. The subsidence must be also very young.

The tidal notch is widespread in this larger area (in the Gulf ofTrieste, on the Istrian peninsula, on the islands of Krk, Rab, Cres,Lo�sinj and Pag and along the coast of the VelebitMt. [Faivre andFouache, 2003; Antonioli et al., 2007]), so there were regionallysimilar properties. Thus, after 500 BP, the subsidence started atdifferent speeds in different structural units (Fig. 7). Along themajor discontinuities, as along the Bakar fault, the notch subsidedat �1.1 m, as found by Benac (1992), but along the other local faults(or in other structural parts) the depths changes from �0.5 to�0.7 m on average. Those differences in relative subsidence ratescould also be discerned from the GPSmeasurements (Fig. 9; Altiner,1999) which could not be regarded as proof, but could be consid-ered as a relative indicator of those tectonic movements observedin the distribution of the notches and their shapes.

Even if the surveyed data strongly suggest rapid co-seismicsubsidence, younger than 550 cal BP, there is no seismic evidence.Seismicity in the region is very low.Moreover, there is no recent tidalnotch, which indicates that there is no recent sea level stabilization.Subsidence of�0.60m� 0.20mon average occurred during the lastfew centuries. The new geomorphological and sedimentologicalobservations support the idea of possibly very young increasedregional tectonic subsidence occurring at different rates.

S. Faivre et al. / Quaternary International 232 (2011) 132e143142

Acknowledgments

We are especially grateful to the “Laboratoire de GéographiePhysique Pierre Birot” in Meudon which allowed us to conduct thesedimentological analyses in their laboratory. We would like tothank Antony Blundell from the Geography Department at theLiverpoolUniversity for his helpful suggestions. We are also greatlyindebted to Eduard Prelogovi�c, Professor at a ZagrebUniversity,Faculty of Mining, Geology and Petroleum Engineering, for havingallowed us to look into his own field measurement data and byfruitful discussions. Special appreciation goes to BrunoTomljanovi�c,Professor at ZagrebUniversity, Faculty of Mining, Geology andPetroleum Engineering for fruitful discussions and suggestions. Weremain indebted to SrCan �Cupi�c and Prof. Franco Stravisi for thecorrections of the mareograph data and to Stavros Frenopoulos fortopographical measurements. This research was partly supportedby the Ministry of Science, Education and Sport of Republic ofCroatia (Project 119-1191306-1305), and Italian National projectVECTOR. The authors wish to thank the two anonymous reviewersfor their constructive comments which substantially improved thesubmitted manuscript as well as Norm Catto, Editor and CarmeloMonaco, Guest Editor, for their precious editorial handling.

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