by Ì. DERMITZAKIS**. Õ. KARAKITSIOS** & Å. LAGIOS**

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2 RESUL TS OF GRA VIMETRIC MEASUREMENTS OF ÔÇÅ LAST 7 YEARS ÉÍ CRETE (GREECE) AND THEIR CONTRIBUTION ÔÏ ÔÇÅ UNDERST ANDING OF ÔÇÅ RECENT -ACTIVE DEFOR- ÌÁ ÔÉÏÍ OF ÔÇÅ REGION* by Ì. DERMITZAKIS**. Õ. KARAKITSIOS** & Å. LAGIOS** 1. GENERAL INTRODUCTION The Mediterranean is tectoçically an especially active area and thus the geodynamic factors should always be taken seþïuslõ ßç mind. The present situation was resulted from a long geological history. The Alpic mountain ranges have been gradually formed during the last 180 million years, since the closure ofthe Tethysocean which broadened eastwards. Since the opening ofthe Atlantic, Europe and ÁfÞca have cïmñþsed two separate plates with relative movements. The most recent phase, which began 50 ÌÕ ago is characteþæed by slow rotation of ÁfÞca northwards, around an axis placed ßç the Gibraltar area. The relative convergence speed remains minor, less than one centimeter per year. This may mean that the drift is hindered by collision between the two continents. Áé present this collision is pushing Turkey towards the West, where apparently the last remains of ocean crust still exist. ÁÉÉ these movements indicate the existence ofhigh energies ßç the lithosphere. The Mediterranean, therefore, is characteþæed by a dense-pattem (ïçéõ 10% ofthe area of ß ts basins is situated at a distance more than 100 km from the coastaline). This fact caused a rapid sedimentation ßç these basis (approximately 0,3 mm/year ßç the last 5 million years). As a consequence, the crust has been buþed under a layer of sediments about 1 Ï km thick at least. Because of the weight of these sedimentary beds, the Westem Mediterranean basins subsided for at least 7 km while those of Eastem Mediterranean, 6-15 km. This movement marks a progressive migration of the bending of continental margins towards. the continent with a general tendency of the coasts Éï sink, which often neutralizes the Þsßçg tectonic movements that are produced by subduction or collision phenomena. Actually there are some zones of subduction ßç the Mediterranean. One of them is associated with the Hellenic Arc which is geocrhonologicaly situated ßç the Serravallian-Quartemary (Mc ÊÅÍÆÉÅ, 1978; MERCIER, 1981; LE PICHON & ANGELIER. * ÁðïôåëÝóìáôá âáñõôïìåôñéêþí ìåôñþóåùí ôùí ôåëåõôáßùí 7 ñüíùí óôçí ÊñÞôç (ÅëëÜäá) êáé óõìâïëþ ôïõò óôçí êáôáíüçóç ôçò ðñüóöáôçò åíåñãïý ðáñáìüñöùóçò ôçò ðåñéï Þò. ** University of Athens. Department ofgeolo~y, Panepistimiopolis, (15784) Athens. Greece.

3 ). The dßstþbutßïn of seismic activity and tomographic results allow us Éï estimate that 200 km (Mc ÊÅÍÆÉÅ, 1978; LE PICHON & ANGELIER, 1979; MERCIER, 1981) Éï 600 km (SPAKMAN et al., 1988; MEULENKAMP et al., 1988) ofthe ÁfÞcan plate have dissapeared under the arc. These tectonic movements have made the watery balance very delicate. The Mediterranean is joined with the Atlantic ocean and the Black Sea by shallow and narrow straits which are easily inf1uenced by tectonics. If, for instance, the straits of Gibraltar were closed, then, under the present conditions, the Mediterranean would dry up ßç approximately 3,000 years. This phenomenon occurred duþng the Messinian when ÅvaÑïÞtes were deposited at the bottom of the basins. The sea water's level rose again duþng the Pliocene, when the straits were opened again. Éé seems that duþng the Quaternary the straits remained open, although they were gradually becoming shallower since the Lower Pliocene. That is why the Mediterranean was inf1uenced by the eustatic movements of the ÁtÉantßc-ïcean. Ïç the other side, the Black Sea, had been connected Éï the Mediterranean Sea duþng the main interglacial ÑeÞïds (ST ANLEY & BLANPIED, 1980). According Éï data supplied by the «SEASA Ô)) satelite, extensive depression is manifested ßç the Eastern Mediterranean, around the Hellenic- Arc, ßç the area of the Ionian Trench and of ÑÉßçÕ and Strabo trenches. The inclination of the median surface level is very pronounced between this depression and the Aegean Sea. The sea-f1oorelief ref1ects the ditterences ßç density ßç the Earth's ßnteÞïr, according Éï the geological history. That is why the relief gradually becomes more pronounced from West Éï East, which is ßç accordance with the increasing relative displacement between Europe and ÁfÞca. Éé is indeed particularly pronounced near the areas where the ÉßthÏSÑheÞc convergence is active or recent. Éç general the sea-f1oor surface slopes towards ÁfÞca, while the subduction zones are characteþæed by a great depression of the level. Á contrary phenomenon can be observed ßç the area of the CaÉabÞan Arc. If we take ßçÉï consideration the intense-tectonic activity of the Mediterranean basin, we can state that the relief of its sea-f1oor surface is çïé static but changes gradually. According Éï a model proposed by RHIZO (1983) ßé has been predicted that the present relief will become even more pronounced, with an increase ßç the inclination of the geoid surface of about 5-1 Ï cm per century. í ertical displacements of Crete are closely related Éï the mechanisms of the Hellenic subduction zone. Ôï determine the dßstþbutßïn and the succesion ofvertical displacements, a thorough study of the structure of the Alpine nappe system (which provides a key Éï the evaluation of neotectonic deformation, inferred from vertical ottsets of the faults which cut the nappe pile) and the stratigraphy of Neogene (dating of the neotectonic events) is necessary. 2. GEOLOGICAL BACKGROUND The A1pine units of Crete have been studied thorough1y ßç the 1ast twenty years (AUBOUIN & DERCOURT, 1965; FYTROLAKIS, 1967, 1972, CREUTZBURG & ÑÁ- PASTAMATIOU, 1969; BoNNEAU, 1970, 1972, 1973a, b, 1984; SANNEMANN & SEI- DEL, 1976; AUBOUIN et al., 1979; BONNEAU et al., 1977; CREUTZBURG & SEIDEL, 1975; SANNEMANN & SEIDEL, 1976; CREUTZBURG & coll., 1977; ÂÏÍÍÅÁý & KARAKITSIOS, 1979; KARAKITSIOS, 1979, 1987, 1989; HALL et al., 1984; ALEXO-

4 -225- POULOS, 1990). Based ïç the literature the Alpine sequence of Crete synthetically consists by: - the parautochtonous «lda- Talea ïþ» unit, which corresponds to the metamorphic Ionian seþes ofthe Westem Greece; - the «ÔÞÑaÉß unit» known ïçlõ ßç Westem Crete, which probably corresponds to the 10wer part of the parautochtonous sequence from which it was tectonical1y detached; - the ÔÞÑïlßs nappe s.1. which consists oftwo units: the underlying «metamorphic phyl1itic nappe» and the calcareous ÔÞÑïlßs nappe s.s. ïç top of it. The tectonic contact that separates the two units corresponds to a «Rabotage basal» that aftected the base of calcareous ÔÞÑïÉßs nappe s.s., showing that the tectonic emplacement of the ÔÞÑïlßs nappe s.1. has been multiphase; - the Pindos-Ethia nappe constitutes the extension of the 010nos-Pindos seþes from mainland Greece to Crete; - the «upper tectonic nappes» that include: the «intermediate units» (Miamou, Vatos, Arvi), the Asteroussia nappe s.s. and the ophiolitic complexe ïç top. The stratigraphic data confirm the initial continuation of this system of nappe pile despite the neotectonic faulting of Crete. The neotectonic analysis, of Crete mainly concems the ÑeÞïd after the latest orogenetic movement. The big thrusts of the most extemal Cretan seþes took place after the Lower Oligocene and before the Serraval1ian- Tortonian. This has been concluded from the fact that both the flysch ofthe parautochtonous seþes has a Lower 01igocene age (ÂÉÆÏÍ et a1., 1976; BARRIER, 1989), and the first post-alpine sediments which are ßç discordance with the Alpine formations of Crete are molasses of Serraval1ian- Tortonian age (DROGER & MEULENKAMP, 1973). Consequently, the tectonic emplacement of nappe system corresponds to the interval between -35 and -13 mi11ion years. Therefore the Neotectonic evolution of Crete started 13 mi11ion years ago. The Neogene sedimentary record of Crete provides ample evidence of repeated, dramatic changes ßç the paleogeographic configuration, which were ßç most cases connected with major tectonic events. From the Middle Miocene onward the Cretan area became transformed into a mosaic of horsts and grabens (fig. 4), the difterential vertical movements varying ßç intensity both ßç space and time (cf. infra). The complex ßçterplay of tectonics and sedimentation resulted ßç a large vaþetõ of sediment types and ßç a rapid lithological changes both ßç a hïþæïçtaé and ßç a vertical sense. More than 60 formal and informal rock units have been recognized ßç the last twenty years (e.g. DERMITZAKIS, 1969-É973; FREUDENTHAL, 1969; MEULEN- ÊÁÌÑ, 1969; DE BRUIJN et a1., 1971; GRADSTEIN, É973; FORTUIN, 1977; DER- MITZAKIS & SONDAAR (1978) DERMITZAKIS et a1., 1979; DERMITZAKIS & ÑÁ- PANIKOLAOU, 1981; DE BRUIJN & ÕÁÍ DER MEULEN, 1981; ZACHARIASSE, 1983; FORTUIN & PETERS, 1984, PETERS, 1985). These rock units can be classified (MEULENKAMP et a1., 1979; fig. 1) into six groups offormations (most groups can be recognized al1 over the island): l-priná Group. Sediments attþbuted to the ÑÞça Group consist of dark limestone breccias and breccioconglomerates. As a rule the components are embedded ßç a wel1- cemented, calcareous matþ. The breccias and breccioconglomerates were deposited ßç çïç-maþçe to brackish or shal1ow-marine environments. The ÑÞça Group forms either the local base of the Neogene sequence, or it represents a lateral equivalent of part of the next-higher Tefeli Group. At some places the ÑÞça Group contains large slabs of gravity-displaced preneogene limestones.

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6 Tefeli Group. The Tefeli Group comprises all «non-consolidatero> terrigenousclastic formations overlying the Prina Group or the preneogene basement and underlying the calcareous successions ofth~ Vrysses Group. The formations incorporated ßç this group are predominantly composed of conglomerates, sands and clays reflecting deposition infresh-water, brackish and marine environments. 3- Vrysses Group. Bioclastic, often reefal algal-corallimestones which constitute ßç part the lateral equivalent of alternations of laminated and hogogeneous, shallowmarine marls. Áé some places the marls contain intercalations of gypsum. The Vrysses Group overlies the Tefeli Group, the preneogene basement or, occasionally, the Prina Group. 4-Hellenikon Group. The Hellenikon Group consists ofreddish, non-marine conglomerates, fluvio-lacustrine, relatively fine-grained successions and, occasionally, brackish and lagoonal deposits with some gypsum. The group unconformably overlies the Vrysses Group, older Neogene strata or, at some places, the preneogene basement. 5-Finikiá Group. ÁÉÉ formations consisting of open marine marls and clays which overlie the Hellenikon Group or the Vrysses Group are incorporated ßç the Finikia Group. Often the marls and clays display laminated, sometimes siliceous interbeds. Áé many places the base ofthe Finikia Group is formed by a marl breccia. 6-Ag. Gálini Group. Coarse, generally reddish, non-marine conglomerates and sands, which overlie, andare ßç part the lateral equivalent of, sediments of the Finikia Group. The Ag. Galini Group represents the highest Noegene rock unit ïç Crete. 7-Pleistocene. Íï formal subdivision was madefor the Pleistocene marine teðaces and continental deposits. The Pleistocene sediments unconformably overlie Neogene or preneogene rocks. 3. NEOTECTONICS Éç Crete, the analysis of the entire Neotectonic ÑeÞïd, shows that extentional movements (fig. 2) took place duþng Upper Miocene times ßç faulted basins (fig. 4), as shown by syn-sedimentary faulting. The main characteþstßcs of this tectonics are the large amplitude and the 10ng duration of extentional movement related to normal faulting since Miocene times. óç the contrary, the observed compressional events ßç the interval of the same ÑeÞïd, have quite difterent intensities and seem all bþef(áígåléår, 1979; GOURNELLOS & KARAKITSIOS, 1987). The average speed of difterential deformation related to the vertical motions for the entire Neotectonic ÑeÞïd (=13 Ma), as this results from the actual disposition of nappes (fig. 3), ranges between 4 to 5 cm/l00 years. According to MOURTZAS (1990) the uplift of Crete started duþng the Late Pliocene-Early Pleistocene and the uplift rate, duþng the last years had not been more than 0.63 cm/100 years that is very difterent ofthe uplift rate accepted by ANGELIER, 1979 (3.2 to 4.6 cm/l00 years) or PETERS, 1985 (6 cm/100 years). Due to the big difterence ßç between the rate values proposed by MOURTZAS (1990), ANGELIER (1979) & PETERS (1985), the latest proposals seem to be more reasonable. RadßïmetÞc dating of the Quatemary shorelines made from vaþïus investigations (THOMMERET et al., 1981; PIRAZZOLI, 1986), shows that the average speed ofsome uplifts from Tyrrhenian up to the last thousand years ranges between 5 to 6 cm/l00 vears. This soeed is aooroximatelv the same with the soeed of the difterential vertical

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13 -234- before coming up Éï final conclusions, longer time observational procedures is re- Quired. Some preliminary maximum values of subsidence or uplift may be deduced though. Éé is estimated (fig. 7) that the maximum gravity change value observed as an average ßç Crete is" ìgal (:É: 6 ìgal) corresponding Éï 6-7 cm (:É: 3 cm)/7 years (=100 cm/l00 years) ofupliftor subsidence ßç an average manner. 5. DISCUSSION ÁÍÏ CONCLUSIONS New data ïç the structure ofthe Upper Mantle undemeath the Aegean area -tomographic images of the Aegean/Eastem Mediterranean Upper Mantle ßç cross sectionby SPAKMAN et a1., indicate that the duration ofthe Hellenic subduction zone ranges from 26 to 40 ma (SPAKMAN et a1., 1988, MEULENKAMP et a1., 1988). This is considerably 10nger than earlier estimates which vary between 5 (MERCIER, 1981) and about 13 Ma (LE PICHON & ANGELIER, 1979). According to MEULEN- ÊÁÌÑ et a1. (1988) this implies that the geological processes around 12 Ma ago, such as fragmentation of Crete into several basins, are not to be attþbuted to the initiation of subduction ßç the Hellenic Trench, but they are associated with the inception of the roll-back process (south-southwestward migration of the Hellenic Trench system). Consequently, the role of compressional tectonics ßç the tectonic evolution of Crete is moreimportant than hitherto thought. The stretching of the Aegean lithosphere is ac:' commodated by along 10w angle shear zones. Along such zones (MEULENKAMP et a1., 1988) a supracrustal slab became detached and began to slide ßç southward direction. Éç the frontal part of this slab (containing the Cretan segment) compression may be generated. Folding and thrusting within the southem extreme of the supractrustal slab has caused the recent overall uplift of Crete, being stronger ßç the south, coupled to a northward tilting of large parts of the island. DuÞng ÑeÞïds without tectonic transport of the supracrustal slab, almost vertical maximal stressóé (gravity) generates almost universally ïþented extension within the supracrustal slab. If this is true vertical movements are also possible for the ÑeÞïd of the tectonic emplacementr of nappe system S.s. of Crete (between -35 and -13 Ma) and one has to distinguishe the comressional and extensional structures of this ÑeÞïd. This a new problem open for research which is beyond the aim of the present study. Summing up, the already published results of Neogene-Quatemary stratigraphy, sea-level changes (shorelines uplift) and recent gravßmetþc measurements ßç Crete show that: - the rate of difterential deformation for the entire Neotectonic ÑeÞïd (-13 Ma) is estimated to be similar to the speed of the fossilized pleistocenic shorelines; - shorelines ofthe last 1500 years, involve an acceleration ofvertical mouvement; - the upward and downward movements, recorded from a mßcrïgravßmetþc network, for the last 7 years ßç the horsts and grabens respectively, show that vertical mouvement is stil1 continuing ßç an increasing speed. This phenomenon is probably related to a particular stage ofsubduction or even, to the onset of the continental collision between ÁfÞca and Europe. ABSTRACT Én Crete, the analysis of the Neotectonic ÑeÞïd faults shows that these are asso-

14 -235- ciated with a strong extensional regime, ßn a perpendicular direction to the longer dimension of Crete (and ßn general to the Aegean arc). This extension that has been expressed with normal faults, has caused a gravitational spreading of Aegean towards the Ionian sea ßn an extremely large scale, especially ßn Crete. This phenomenon is associated with the subduction of the ÁfÞcan plate under the Aegean plate. Én the interior of this regime, compressional events have been observed. Shorelines of the last 1500 years «record» revolving upward movements ßn West Crete with maximum Þsßng approximately 10 m. This uplift involves an acceleration of vertical deformation. Én Crete, the speed of difterential vertical deformation for the entire Neotectonic ÑeÞïd (approximately 13 million years) is estimated to be similar with the speed deduced from the fossilized Pleistocenic shorelines. GravßmetÞc measurements of the last 7 years ßn Crete show that the upward and downward movements ßn the horsts and the grabens respectively, are still continuing ßn an increasing speed. This phenomenon is probably related to a particular stage of subduction or even, to the onset of the continental collision between ÁfÞca and Europe. ÐÅÑÉËÇØÇ Óôçí ÊñÞôç ç áíüëõóç ôùí ñçãìüôùí ôçò ÍåïôåêôïíéêÞò ðåñéüäïõ äåß íåé üôé áõôü óõíäýïíôáé ìå Ýíá éó õñü åöåëéáéóôéêü.êáèåóôþò, ìå äéåýèõíóç êüèåôç ðñïò ôçí ìáêñýôåñç äéüóôáóç ôçò ÊñÞôçò (êáé ãåíéêüôåñá ôïõ ôüîïõ ôïõ Áéãáßïõ). Ï åöåëéáéóìüò áõôüò ðïõ åêöñüóôçêå ìå êáíïíéêü ñþãìáôá, ðñïêüëåóå óå ìåãüëç êëßìáêá ôçí åðýêôáóç ëüãù âáñýôçôáò ôïõ Áéãáßïõ êáé éäéáßôåñá ôçò ÊñÞôçò ðñïò ôçí Éüíéá èüëáóóá. Ôï öáéíüìåíï áõôü óõíäýåôáé ìå ôçí õðïâýèéóç ôçò ÁöñéêáíéêÞò ðëüêáò êüôù áðü ôçí Áéãáßá ðëüêá. Óôï åóùôåñéêü áõôïý ôïõ êáèåóôþôïò ðáñáôçñþèçêáí óõìðéåóôéêü óõìâüíôá. Ïé áêôïãñáììýò ôùí ôåëåõôáßùí 1500 åôþí êáôáãñüöïõí ðåñéóôñïöéêýò áíïäéêýò êéíþóåéò óôçí ÄõôéêÞ ÊñÞôç ìå ìýãéóôç áíýøùóç ðåñßðïõ 10 ffi. Óôçí ÊñÞôç ç ôá- ýôçôá ôçò äéáöïñéêþ ò êáôáêüñõöçò ðáñáìüñöùóçò ãéá ôç óõíïëéêþ ÍåïôåêôïíéêÞ ðåñßïäï (êáôü ðñïóýããéóç 13 åê. Ýôç) åêôéìüôáé ùò ðáñüìïéá ìå ôçí ôá ýôçôá ðïõ óõíüãåôáé áðü ôéò áðïëéèùìýíåò ÐëåéóôïêáéíéêÝò áêôïãñáììýò. Ïé âáñõôïìåôñéêýò ìåôñþóåéò ôùí ôåëåõôáßùí 7 åôþí óôçí ÊñÞôç äåß íïõí üôé ïé áíïäéêýò êáé êáèïäéêýò êéíþóåéò óôá ôåêôïíéêü êýñáôá êáé ôéò ôåêôïíéêýò ôüöñïõò áíôéóôïß ùò, óõíå ßæïíôáé áêüìá ìå áõîáíüìåíç ôá ýôçôá. Ôï öáéíüìåíï áõôü ðéèáíþò óõíäýåôáé ìå Ýíá éäéáßôåñï óôüäéï õðïâýèéóçò Þ áêüìç, ìå ôçí Ýíáñîç ôçò çðåéñùôéêþò óýãêñïõóçò ìåôáîý ÁöñéêÞò êáé Åõñþðçò. REFERENCES ALEXOPOULOS Á. (1990). GeologicaI and hydrogeological conditions of the topographical sheet Mohos area (central-seastern Crete). Doct. thesis, õçßí. of Athens (unpublished). ANGELIER J. (1979). Neotectonique de l'arc egeen. Soc. Geol. Nord, 3,418 ñ. AUBOUIN J. & DERCOURT J ): Sur Ia geologie de I'Egee: regard sur la Crete. Bu/l. Soc. Geol. France, 7, ññ AUBOUIN J., LE PICHON., WINTERER Å. & ÂÏÍÍÅÁõ Ì. (1979): Les HelIenides dans I¼Ñtßque de la tectonique des piaques. Proc. VI Coll. Geod. Aegean Region (Athens 1977),11É, ññ BARRIER Å. (1979). Etude neotectonique des iles de Karpathos et Kassos (Dodecanese, Grece) et esquisse geoiogique de l'ile de Kassos. Th. Doct 3e cycie, õçßí. Ñ. et Ì. CuÞe, ÑaÞs, 206ñ.

15 -236- ÂÉÆÏÍ G., BONNEAU Ì., LEBOULENGER Ñ., MATESCO S. & THIEBAULT F. (1976). Sur la signification et ('extension des «massifs cþstaééßçs extemes» en PeIoponnese meþdßïçal et dans l'arc egeen. Bul/. Soc. geo/. Fránce, 7, ÕÉÉÉ, 2, ññ ÂÏÍÍÅÁõ Ì. (1970). Les lambeaux allochtones du revers señteçtþïçaé du massif de ÑsßÉïÞtß. Grete moyenne. Bul/. Soc. Geo/. Fránce. 7, ÉÉ, ññ ÂÏÍÍÅÁõ Ì. (1972'). La nappe metamorphique de É sterïussßa, Iambeau d'affinites pelagoniennes char- Þe jusque sur Ia zone de ÔÞÑïlßtÆa en Crete moyenne (Grece). C. R. Acád. Sc. Páris, Ù, 275, ññ ÂÏÍÍÅÁõ Ì. (1973a). Les differentes «seþes ophiolitireres» de Ia Crete: une mise au point. C. R. Acád. Sc. Páris, Ù, 276, ññ ÂÏÍÍÅÁõ Ì. (1973b). Sur les affinites ioniennes des «Calcaires en piaquettes» epimetamorphiques de Ia Crete, Ie chamage de la seþe de Gavrono- ÔÞÑïÉßtÆa et la structure de l'arc egeen. C. R. Acád. Sc. Páris, Ù, 277, ññ BONNEAU Ì. (1984). Cïðelatßïç ofthe HeIlenic nappes ßç the SQuth-east Aegean and their tectonic reconstruction. Geo/. Soc. London, Sp. Publ. 17, ññ ÂÏÍÍÅÁõ Ì. & KARAKITSIOS V. (1979). Les niveaux ßçfeÞeurs (ÔÞas SUÑeÞeur) de la nappe de ÔÞñïlitza en Crete moyenne (Grece) et leurs relations avec Ia nappe des phyllades. Problemes stratigraphiques, tectoniques et de metamorphisme. C. R. Acád. Sc. Páris, Ù, 288, ÑÑ CREUTZBURG Í. & PAPASTAMATIOU J. (1969). Die Åthßa-SeÞe des sudlichen Mittelkretas und ihre Ophiolitvorkommen. Sitzungsber. Heidelberger Akád. Wiss, math.-naturw.ki, 1,63 ñ. CREUTZBURG Í. & SEIDEL Å. (1975). Zum Stand der Geologie des Praneogens auf Kreta. Í. Jb. Geo/. ÑáÉáïðé., Abh., Stuttgart, 149, ñ CREUTZBURG Í. & coll. (1977). General geological map of Greece (Crete Island), 1/ e. IGMR, Athens. ÙÅ BRUIN Ç., SONDAAR Ñ.Õ. & ZACHARIASSE W.J. (1971). Mammalia and Foraminifera from the Neogene of KasteIios ÇßÉÉ (Crete), a cïðelatßïç of Continental and ÌaÞçe Biozones. Proc. Ned. Akád. Wet., Â. 74 (5), (1971), ññ ÙÅ BRUIN Ç., ÕÁÍ DER MEULEN A.J. (1981). The dßstþbutßïç ofland MammaIs ßç the Mediterranean Through the Neogene-Is there a fit with the Paleogeographic and Paleoclimatologic Reconstruction Based ïç Data from ÌaÞçe Basins? Ann. Geo/. Páys Hellen., 4, ññ DERMITZAKIS Ì. (1969). Geological Researches of the Neogene Deposits of Hierapetra Province ßç Crete. Ann. Geo/. Páys Hellen., 21, ññ DERMITZAKIS Ì. (1973a). Recent Tectonic Movements and Old-Strandlines along the Coasts of Crete. Âõll. Geo/. Soc. Greece,, É, ññ DERMITZAKIS Ì. (1973b). The Occurrence of Pleistocenic Deposits ßç SE Sitiil DßstÞct (Å. Crete). Bull. Geo/. Soc. Greece,, 2, ññ DERMITZAKIS Ì. & THEODORIDIS S.A. (1978). Plaktonic Fïramßçßfera and Clacareous Nannoplankton from the PIiocene of Koufonisi Island (Å. Crete, Greece). Ann. Geo/. Páys Hellen., 29, 2, ññ DERMITZAKIS D. & SONDAAR Ñ.Õ. (1978). The Importance offossii Mammals ßç Reconstructing Pa- Ieogeography, with SpeciaI Reference to the Pleistocene Aegean ArchipeIago. Ann. Geo/. Páys Hellen., 29, ññ DERMITZAKIS Ì. & PAPANIKOLAOU D. (1981). Paleogeography and Geodynamics of Aegean Region duþçg Neogene. VIith Int. Congress ïç Medit. Neogene, Athens Ann. Geo/. Páys Hellen., ÉÕ, DROOGER C.W. & MEULENKAMP J.E. (1973). StratßgraÑhßcïçtÞbutßïçs to geodynamics ßç th Mediteðaçeaç area: Crete as a case hßstïry. Bull. Geo/. Soc. Greece,, É, ññ FORTUIN A.R. (1977). Stratigraphy and Sedimentary History ofthe Neogene Deposits ßç the Ierapetra Region, Eastem Crete. GUA Pápers ofgeology, 1,8, 164 ñ. FORTUIN A.R. & PETERS J.H. (1984). The ÑÞma Complex ßç Eastem Crete and its relationship to possible StÞke-SÉßÑ Tectonics. J. Struct. Geo/., 6, 5, ññ FREUDENTAL Ô. (1969).,Stratigraphy ofneogene deposits ßç the Khania province, Crete, with special reference to foraminifera offamiiy Planorbulinellidae and the genus Heterostegina. Utrecht microp. Bul/., 1,208 ñ. FYTROLAKIS Í. (1967). Ïç fossii occurence ßç eastem Crete metamorphic rocks. Bul/. Geo/. Soc. Greece, 7, ññ FYTROLAKISN. (1972). Die Åßçwßrkuçg gewisser ïðïgeçeç Bewegungen und die Gipsbildung ßç Ostkreta (Prov. Sitia). Bul/. Geo/. Soc. Greece, 9, É, ññ GOURNELLOS Ô. & KARAKITSIOS V. (1987). Neotectonic observations ßç the Eagean Arc. Bull. Geo/. Soc. Greece, É, ññ

16 -237- GRADSTEIN F.M. (1973): The Neogene and Qwuaternary deposits ßç the Sitia dßstþct of eastern Crete. Ann. Geol. Páys He/len., 24, ññ HALL R., AUDLEY-CHARLES M.G. & CARTER D.J. (1984). The significance ofcrete for the evolution ofthe eastern Ìedßteðanean. Geol. Soc. London, Sp. Publ., 17, ññ KARAKITSIOS V. (1979). CïntÞbutßïn a l'etude geologique des He11enides: la region de Se11ia (Crete moyenne-occidenta1e). Th. Doct. 3e cyc1e, õçßí. Ñ. et Ì. CuÞe, ÑaÞs, 167 ñ. KARAKITSIOS v. (1987). Sur la signification de la «seþe de Trypali» dans 1a region de Sel1ia en Crete occidentale (Grece). C. R. Acád. Sc. Páris, 304,11,3, ññ KARAKITSIOS v. (1989). A1pine defïðçatßïn of ÔÞÑï1ßs seþes s..l. ßç Peloponnesus and Crete (Greece) and its dynamic interpretation. Ann. Geol. Páys He/len. 34/1, ññ LAGIOS Å. & ÇÉÑÊÉÍ R.G. (1986). High precision gravity observations ïç Crete, Greece. Tectonophysics, 126, ññ LAGIOS Å., DRAKOPOULOS J., ÇÉÑÊÉÍ R.G. & GIZELI C. (1988). Microgravimetry ßç Greece; app1ications Éï earthquake and volcanoeruption prediction. Tectonophysics. 152, ññ LE PICHON & ANGELIER J. (1979). The He11enic Arc and Trench System a key Éï the Ne9tectonic Åíï- 1õéßïç ofthe Eastern Ìedßteðanean. Tectonophysics. 60, ññ Mc ÊÅÍÆÉÅ D.P. (1978). Some remakrs ïç the deve1opment ofsedimentary basins. Eárth Plánet. Sci. Lett. MERCIER J.L. (1981). Extensional-compressiona1 tectonics associated with the Aegean arc: comñaþson with the Andrean Cordil1era of south Peru-north Bolivia. Phil. Tráns. Royál Soc. London. Á, 300, MEULENKAMP J.E. (1969). Stratigraphy of Neogene Deposits ßç the Rethymnon Province, Crete, with special Reference Éï the Phylogeny of Universal UíßgeÞna from the Mediterranean Region, Utr. Ìßcropál. Bull. 2, 168 ñ. MEULENKAMP J.E. & ZACHARIASSE W.J. (1973). Stratigraphic and Structural Framework ofthe Messinian Deposits ïç Crete. Éç: Drooger (Ed.), Messinian events ßç the Mediterannean, (Amsterdam 1973), ññ MEULENKAMP J.E., JONKERS Á. & SPAAK Ñ. (1977a). Late Miocene Éï Early Pliocene Development ofcrete. Proc. VI Co/l. Aegeán Region Athens MEULENKAMP J.E., ßç col. DERMITZAKlS Ì., GEORGIADES-DlKEOULIA Å. & JONKERS Á. (1979). Field Guide Éï the Neogene ofcrete. Ed. Dep. ofgeology and Paleontology, õçßí. of Athens, seþes Á. MEULENKAMP J.E., WORTEL M.J.R., ÕÁÍ WAMEL W.A., SPAKMAN W. and HOOGERDUYNG STRATING Å. (1988). Ïð the Hellenic subduction zone and the geodynamic evolution ofcrete since the 1ate Middle Miocene. Tectonophysics. 146, MOURTZAS Í. (1990). Quaternary tectonic movements of eastern Crete. Doct. thesis, Techn. School of Athens (unpublished). PETERS J.M. (1985). Neogene and Qwuaternary vertical tectonics ßç the south Hellenic arc and their effect ïç cïncuðent sedimentation processes. GUA Ñáñ. geol.. 1,23,247 ñ. PIRAZZOLI Ñ.Á. (1986). The Ear1y Bysantine Tectonic Paroxysm. Æ. Geomorph. Í. F., Stuttgart, 62, ññ PIRAZZOLI Ñ.Á., THOMMERET J., THOMMERET Õ., LABOREL J. & MONTAGGIONI L.F. (1982). Crustal B1ock Movements from Ho1ocene shore1ines: Crete and Antikythira (Greece). Tectonophysics, 86, ññ SANNEMANN W. & SEIDEL Å. (1976). Die ÔÞas-Schßchten íïç Ravducha/NW-Kreta. Ihre ste11ung im Kretischen Deckendau. Í. Jb. Geol. Páláont. Mh., 4, ññ STANLEY D.J. & BLANPIED C. (1980). Late Quaternary water exchange between the Eastern Mediterra-. nean and B1ack Sea. Neture 285, THOMMERET Õ., THOMMERET J., LABOREL J., MONTAGGIONI L.F. & PIRAZZOLI Ñ.Á. (1981). Late 01ocene shoreline changes and seismotectonic displacements ßç western Crete (Greece). Æ. Geomorph.N. F.. 40, ññ ZACHARIASSE J.W. (1983). Paleoenvironmental and Paleooceanographic Interpretation ofmediterranean Middle Miocene Éï Pleistocene Plaktonic Associations. Utrecht Micropál. Bu/l ÑÑ. 9 É -É 10.