Proceedings of the

4th Symposium of the Hellenic Society for Archaeometry

National Hellenic Research Foundation, Athens 28-31 May 2003

Edited by

Yorgos Facorellis Nikos Zacharias

Kiki Polikreti

BAR International Series 1746 2008

This title published by Archaeopress Publishers of British Archaeological Reports Gordon House 276 Banbury Road Oxford OX2 7ED England bar@archaeopress.com www.archaeopress.com BAR S1746 Proceedings of the 4th Symposium of the Hellenic Society for Archaeometry. National Hellenic Research Foundation, Athens, 28-31 May 2003 © the individual authors 2008 ISBN 978 1 4073 0188 4 Printed in England by Synergie Basingstoke All BAR titles are available from: Hadrian Books Ltd 122 Banbury Road Oxford OX2 7BP England bar@hadrianbooks.co.uk The current BAR catalogue with details of all titles in print, prices and means of payment is available free from Hadrian Books or may be downloaded from www.archaeopress.com

65

The ReconsTRucTion of PRehisToRic shoRelines in Dokos islanD, aegean sea, using RemoTe sensing Techniques1

G. Papatheodorou, M. Geraga and G. FerentinosLaboratory of Marine Geology and Physical Oceanography, Department of Geology, University of Patras,

George.Papatheodorou@upatras.gr

Abstract: The evolution of the coastline configuration around Dokos Island over the last 18000yrs BP is herewith presented in detail, based on the mapping of palaeoshorelines features, using marine remote sensing techniques.

The formation age of the identified palaeoshorelines based on the global sea-level change curves shows that they coincide with the occurrence of global climatic changes.

The shoreline configuration shows that Dokos Island was connected to the mainland from the 18000yrs BP to at least 9600yrs BP. During that time Dokos was a low height headland exposed to winds and waves thus making it inhospitable to the mariners of that time.

There are indicators that changes to the shoreline configuration at 6000yrs BP and 4500yrs BP may be associated with the establishment of the Neolithic settlement on the island and, may have been a contributing factor in the sinking of the ship, the wreck of which has been found on the seafloor.

Περιληψη: Το Εργαστήριο Θαλάσσιας Γεωλογίας και Φυσικής Ωκεανογραφίας (Ε.ΘΑ.ΓΕ.Φ.Ω) Τμήματος Γεωλογίας Παν/μίου Πατρών προσκλήθηκε το 1992 από το Ινστιτούτο Εναλίων Αρχαιολογικών Ερευνών (ΙΕΝΑΕ) να αναλάβει τη θαλάσσια γεωφυσική έρευνα στη βόρεια υφαλοκρηπίδα της νήσου Δοκού με τη χρήση συστημάτων θαλάσσιας τηλεπισκόπησης (τομογράφο υποδομής πυθμένα 3.5kHz και ηχοβολιστή πλευρικής σάρωσης). Στη θέση αυτή αναπαύεται αρχαίο ναυάγιο περίπου 5000 ετών, το οποίο είχε μελετηθεί με ιδιαίτερη λεπτομέρεια από το ΙΕΝΑΕ. Σκοπός της γεωφυσικής έρευνας ήταν ο εντοπισμός των παλαιοακτών και η ανάπλαση της παράκτιας παλαιογεωγραφίας της περιοχής τα τελευταία 18000 χρόνια και ιδιαιτέρως τη χρονική περίοδο που συνέβη το ναυάγιο.

Κατά τη διάρκεια των ερευνών εντοπίστηκε πληθώρα καταβυθισμένων αναβαθμών που αποδόθηκε στη δημιουργία προσωρινών παλαιοακτών. Βάσει της καμπύλης της παγκόσμιας ανύψωσης της θάλασσας κατά Fairbanks και της επιφανειακής κατανομής των βαθών εμφάνισης των αναβαθμών κατέστη δυνατή η αποτύπωση των παλαιοακτών της νήσου του Δοκού κατά τη διάρκεια της Παλαιολιθικής, Μεσολιθικής και Νεολιθικής περιόδου. Ο κόλπος Σκιντού υπολογίζεται ότι διαμορφώθηκε στην αρχή της Νεολιθικής περιόδου και ακολούθως περίπου στα 6000yrs BP ένας κολπίσκος σχηματίστηκε στην βόρεια ακτή του Σκιντού στη θέση όπου εντοπίστηκε το αρχαίο ναυάγιο. Η συνεχής άνοδος της θάλασσας φαίνεται ότι κατέκλυσε αυτόν τον κολπίσκο περίπου στα 4000yrs BP που ίσως χρησίμευε ως φυσικό καταφύγιο στους θαλασσοπόρους και πιθανώς αυτό το γεγονός να σχετίζεται με την βύθιση του πλοίου.

Introduction

The change in climate over the last 18000yrs BP caused significant changes to sea level and thus to coastal palaeogeography (Fairbanks 1989). At 18000yrs BP, during the last glacial maximum the sea level was 120m below the present level, exposing large areas of land. The melting of the ice sheets which followed caused a rise in sea level and the submersion of the coastal low lands. The rise was rapid but pulsating. Short term cold events (stadials) have caused still-stands which have resulted in the formation of a series of palaeoshorelines. Their imprints on the coastal zone depend mainly on the sediment supply. In littoral environments with adequate sediment supply the sea level stands are imprinted as changes in coastal trangressive deposits, whilst in environments with limited sediment supply the still stands are imprinted as geomorphologic features, usually scarps and ridges (van Andel & Lianos 1984, Lobo et al. 2001, Karisiddaiah et al. 2002).

During prehistoric times coastal environments had hosted human settlements and thus the identification and the mapping of the coastal paleogeography is of great importance to the archeological studies (Kraft et al. 1982). Over the last decades the use of remote sensing techniques for the reconstruction of the ancient coastal environments has become a common practice because these techniques permit the high accuracy identification and mapping of submerged palaeoshorelines which are either on the seafloor surface or are buried under loose post-glacial sediments (van Andel & Shacleton 1982, van Andel & Lianos 1984, Wiedicke et al. 1999).

The purpose of this survey is twofold: firstly to reconstruct the geomorphological condition in the embayment where the Dokos wreck was found (Papathanasopoulos et al. 1989-1992) and secondly to reconstruct the Late Paleolithic, Mesolithic and Neolithic shorelines around Dokos island (Fig. 1).

Dokos Island lies on the shelf of the Argolida peninsula. At 18000yrs BP Dokos and the nearby islands (Spetses and Hydra) were connected to the mainland forming

1 This paper is dedicated to N. Tsouhlos, former president of H.I.M.A., who passed away. His name will certainly remain as a pioneer of underwater archaeology in Greece.

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a “semicontinent” (van Andel & Shackleton 1982, Perissoratis & Conispoliatis 2003). The transgression of the sea, that followed, flooded the lowlands and thus the present day islands were shaped. This occurred at ~9000yrs BP (van Andel & Shackleton 1982).

Methodology

The marine remote sensing survey around Dokos island was carried out using a 3.5kHz Geopulse sub-bottom profiler and an EG &G side scan sonar.

The sub-bottom profiler system emits medium to high frequency acoustic pulse in the form of acoustic conical beams. The acoustic pulses, which penetrate under the seabed are reflected back by the underlying layers and are recorded on a continuously running chart, thus providing a geological profile (tomography) of the sub-bottom beneath the path over which the system is towed. The side scan sonar system emits acoustic pulses which scan the seafloor. The reflected acoustic pulses from the seafloor are graphically recorded on a running chart thus providing a plan view seafloor acoustic image.

A Magelan GPS system with an accuracy of about 30m was used for the navigation and the positioning.

The ship tracks were plotted in the hydrographic chart of the area (Chart) and a detailed bathymetric map was prepared using the depth data from the sub-bottom profiles and the bathymetric information of the chart (Fig. 2).

Data presentation

The study of the acoustic profiles based on the definitions of Damuth (1975), has shown that, the sea-bottom in the records is characterized by four different echo types each one corresponding to different seabed material (Fig.3).

Echo Type I: is characterized by a very prolonged echo with no sub-bottom reflections. Locally the prolonged echo exhibits low relief diffraction hyperbolae. Echo Type I extends from the present day shoreline to a depth of about 20 to 30m (Fig.3). The acoustic echo corresponds to hard rock seafloor which generally has a smooth surface. The rocky seafloor continues onshore and outcrops on the island. The rocky outcrops on the island were identified as Cretaceous limestones.

Echo Type II: is characterized by a continuous sharp bottom echo with one prolonged sub-bottom reflector. Echo Type II extends from the 20m isobath to the 100m isobath (Fig.3). This echo type corresponds to a surficial homogenous non-layered stratum probably consisting of sandy silt. This stratum overlies the aforementioned Cretaceous limestone and its thickness increases from 0.5 to 3m seawards. The homogeneus character indicates that the deposition of the sediments probably took place under

Figure 1. General map of the studied area. The grey area indicates the area where the marine remote-sensing survey was carried out. The arrow indicates the position of the wreck in Skindou embayment.

Figure 2. Bathymetric map of the studied area based on bathymetry data collecting during the survey. The index map presents the ship tracks.

Figure 3. Spatial distribution of the Echo Types (I-IV) identified in the studied area. In the left side of the Figure representative 3.5kHz records of Echo Types (I-IV) are shown.

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high wave energy regime inside the nearshore zone, whilst the small thickness of the stratum indicates a slow rate of deposition probably caused by the rapid transgression of the sea.

Echo Type III: is characterized by regular hyperbolae with varying vertex elevations and no sub-bottom reflectors. ET III appears within the areal extent of ET II and between the depth waters of 60 to 90m (Fig.3). Echo Type III corresponds to area whereas the hard rock seafloor appears in steep slopes.

Echo Type IV: is characterized by a continuous sharp bottom echo with up to 15m of conformable sharp continuous reflectors. This echo type borders Echo Type II and extends beyond the 100m isobath (Fig.3). This echo type corresponds to a layered sedimentary sequence which overlies the limestone bedrock. This layered sequence thickens seawards attaining a maximum thickness of about 15m. The layered character of this sequence suggests that the sediments were deposited continuously and slowly in a low energy environment beyond a nearshore zone.

The study of the seismic records suggests that the most

prominent feature in all the records is the limestone bedrock. This limestone bedrock can be traced from the shoreline to a water depth more than 110m. At water depths less than 20 to 30m the limestone bedrock outcrops on the seafloor. Beyond the 20 to 30m water depth the limestone is covered by sediments and occurs at sub-bottom depths from a few cm to 15m increasing seawards. The above suggests that the limestone bedrock in the area under investigation lies at its seaward ends about 125m below the present day sea level. The morphology of the limestone surface exhibited in the records indicates a “basal trangressive” surface. This basal trangressive surface has also been identified around the coastline of the Argolida peninsula by Van Andel & Lianos (1984).

Detailed examination of the profiles on the limestone bedrock surface reveals numerous small scarps which appear as sharp breaks in the overall slope gradient of the limestone surface (Fig. 4). These scarps on the limestone bedrocks appear to have been sculptured by the erosional power of the waves when the sea level was at a stand –still for a short period of time during the sea transgression (Fig. 5). It can therefore be regarded as evidence of palaeoshoreline.

The side scan sonar survey has shown that these palaeoshorelines on the seafloor are continuous for long distances along the coastline. Similar scarps which have also been considered as palaeoshorelines markers have been found along the coastline of the Argolid peninsula (Van Andel & Lianos 1984). If we assume that the sea level at the time of their formation corresponded to the bases of the scarps, the position of these past sea levels can be determined to within a 2 to 3m accuracy.

To examine the evolution of the past glacial sea level rise, a percentage occurrence diagram of the identified scarps

Figure 4. Selected seismic profiles from the studied area. The arrows indicate the geomorphologic features which correspond to surficial or buried traces of submerged palaeoshorelines (scarps).

Figure 5. (A) 3.5kHz profile showing a well-shaped scarp, buried under loose post-glacial sediments and (B) Simplified drawing showing the formation of the scarp.

G. Papatheodorou, M. Geraga and G. Ferentinos

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versus the water depth in which they were detected, was drawn (Fig. 6). The study of the diagram shows that the scarps are not randomly distributed but rather gathered in clusters which correspond to selective water depths. The water depth in which the scarps are clustered are at 112m, 98m, 61-62m, 51m, 45-48m, 35-38m, 31-33m, 20-24m and 10-11m. The above suggests that the transgression of the sea around Dokos island was not continuous during the Late Glacial-Holocene period but was interrupted for short time intervals. If we assume that eustasy was the only parameter controlling the above sea level changes then their age of formation can be determined using the sea-level change curve. Table I presents the age of the above mentioned palaeoshorelines according to the curve constructed by Fairbanks (1989) (Fig.7).

Discussion

The study of the palaeoshorelines around Dokos island reveals that the water depths they have formed correlates well with the water depth of the palaeoshorelines detected around the Argolida peninsula by van Andel & Lianos

(1984). Furthermore, the age of the palaeoshorelines based on the same sea level change curve (Fairbanks 1989) agrees well with the age of the palaeoshorelines around Dokos island (Table I).

A good agreement also exists between the water depth of the present study shorelines for the 18000yrs BP, 10000yrs BP and 6000yrs BP and the water depth of the same age palaeoshorelines around the Argolida peninsula, as estimated by Lambeck (1996) who took into consideration the contribution of the isostatic effect caused by the ice melting.

Figure 6. Histogram of submerged shore features (scarps) observed in the seismic records of the studied area, plotted against depth below present sea level.

Figure 7. Diagram showing the depths of the Dokos paleoshorelines plotted on the sea level change curve, by Fairbanks (1989).

N. Dokos(Present Study)

Argolid(Van Andel and Lianos, 1984)3

Depth of palaeoshorelinesBelow present sea level (m)

Fairbanks, 1989Depth of palaeoshoreline(m)

Fairbanks, 1989Age(ka BP)

Argolid shore clusters Age(ka BP)

118-115 Q 16-17112 15.198 12.7 97 O 12.7

75-74 M 11.561-62 10.4 62-65 L 10.551 9.6 52 K 9.645-48 9.5 45-48 J 9.535-38 9.0 37-39 H 9.031-33 8.6 27-28 F 8.420-24 7.6-8.0 18-16 D 7.510-11 6.0 10-11 C 6.0

Table 1

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Finally, the very last portion of the rise which formed the 10-11m palaeoshoreline formed around 6000yrs BP is in agreement with the Neolithic artifacts which are dated at between 7610 to 6200yrs in a water depth of 11m in the southern Argolida shelf (Gifford 1983).

The formation age of these palaeoshorelines matches well with the age of stadials (cold short-term events) prevailing during that period in the high latitudes by the Northern Hemisphere (Bond et al. 1992, Bond and Lotti 1995, Bond et al. 1997) and in Mediterranean areas (Matthews & Aylon 1997, Rohling et al. 1998, Geraga et al. 2000, Karkanas 2001). A detailed comparison of the age of the formation of the palaeoshorelines and the occurrence of the paleoclimatic instabilities shows the following:

The palaeoshoreline at 112m can be well correlated with the occurrence of the Heinrich 1 event between 13000 to 16000yrs BP (Table 2) whilst the palaeoshoreline at 61-62m with the occurrence of Younger Dryas event at 10000-11000yrs BP (Table 2). The palaeoshoreline at 98m formed at about 12700yrs BP does not correlate with any known climatic change, therefore it can be suggested that the palaeoshoreline has probably been formed by a local tectonic event. The palaeoshorelines at 51m and 45-48m are located in the most inclined part of the curve which indicates a very fast rate of sea level rise for a short period. These two palaeoshorelines seem to be associated with the 1st Holocene stadial at about 9600yrs BP. The presence of two palaeoshorelines with a height difference of about 4 to 5m corresponding to a time span of less than 2 to 3 hundred years may indicate that one of the two palaeoshorelines was probably caused by a tectonic event.

The palaeoshorelines at 35-38m and 31-33m were formed during the sapropel S1a layer between 9500 and 9000yrs BP during a period of warm and humid climate. The formation of these two shorelines in such a short time span during which no abrupt climate change was observed,

indicate that one of the palaeoshorelines was also caused by a tectonic event.

The palaeoshorelines at 20-24m and 10-11m coincide with the 2nd and 3rd Holocene stadials at about 7600-8000yrs BP and 6000yrs BP, respectively. The age and water depth of the latter palaeoshoreline also agrees well with the Neolithic artifacts dated between 7610 and 6200years and found submerged under a water depth of 11m (Gifford 1983).

After 6000yrs, according to archaeological data, the sea level rose at about 4000yrs BP and reached 5 to 7m below present-day sea level rise (Van Andel & Lianos, 1984).

Based on the above presented distribution of the palaeoshorelines and the archaeological records for the prehistoric period as deducted by detailed studies in the Franchthi cave located in the Argolida (Perles 1987a & b) an estimation of the areal extent of the lowlands can be made for the surrounding area. The sea level during the Upper Paleolithic at about 18000yrs BP was at about -120m and rose to –(61-62)m at about 10400yrs BP which coincides with the end of the Upper Paleolithic. During this time span the mean rising rate was about 4.4m/ka. During the Mesolithic from 10000yrs BP to 8000yrs BP the sea level rose another 30m with a mean rising rate of 15m/ka. The transition from Mesolithic to Neolithic coincide with the formation of the palaeoshoreline at -24m whilst during Late Neolithic the palaeoshoreline was at –(10-11)m.

The study of the palaeogeographic maps (Fig. 8, Fig. 9) show how different the coastal configuration was between the Upper Paleolithic, Mesolithic and Neolithic Ages. The most striking feature in the Upper Paleolithic was the extensive lowlands which in the Neolithic period were severely reduced. Dokos island was connected with the Argolida peninsula as were the two other islands Hydra and Spetses. All these three islands at that time formed isolated hills.

N. Dokos(present study) Stadials obtained at high latitudes of the

Northern Hemisphere and the Mediterranean regionDepth of palaeoshorelines (m)

Age(ka BP)(Fairbanks, 1989)

112 15.1 Heinrich 198 12.7 Tectonic event?61-62 10.4 Younger Dryas51 9.6 1st Holocene stadial45-48 9.5 Tectonic event ?35-38 9.0 Sapropel S1a 31-33 8.6 Tectonic event?20-24 7.6-8.0 2nd Holocene stadial

(interruption of the S1 sapropel)10-11 6.0 3rd Holocene stadial

(final end of the S1 sapropel)

Table 2

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The data indicates that in the Upper Paleolithic a vast area around the island was probably occupied by coastal plains. These lowlands might have been biologically productive and may have had large herds of animals. At that time Dokos island as well as the islands of Spetses and Hydra were connected to the mainland forming low height headlands. Dokos was disconnected from the mainland between 8600 and 9000yrs BP when the sea level was at about –33 to m below present sea level. At that time most of the low-land was covered by the sea. The impact of such land loss may be illustrated in the case of the nearby Franchthi cave. The human occupation of the cave became more intense and continuous after 10000yrs and lasted until Final Neolithic. This might have been caused due to the shortage of food resources as the lowlands were covered by the sea.

The study of the shorelines around Dokos Island shows that from 15100yrs BP to 9500yrs BP there was no indentations along the coastline and that the coastline was exposed to winds and waves making the island in-hospitable to mariners of that time. At about the beginning of the Neolithic, when the sea level rose to –(20-24)m below present, an embayment formed in the northern coastline of the island “the Skindou embayment” (Fig. 9). The coastal configuration of the Skindou embayment shows that it was exposed to the westerly winds with a fetch of about 10km, thus making the embayment unsafe for the seafarers for protecting their small crafts.

At about 6000yrs BP the rise of the sea level to 10-11m below present sea level changed the configuration of the shoreline in the Skindou embayment forming a small cove (Fig.9, Fig.10) which was protected in all weathers. This cove would have made an ideal shelter for the mariners carrying goods and moving to and fro in the area. This probably led to the establishment of the Neolithic settlement found on the island. At about 4000yrs BP the sea level rose to about 7m below present, causing the submergence of the small cove, making the former cove area no longer suitable for sheltering as the coastline was now straighter and exposed to the westerly winds. This change probably contributed to the sinking of the boat whose wreck was found on the seabed.

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