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Origin and Distribution of Clay Mineralsin the Alexandroupolis Gulf, Aegean Sea, Greece

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Origin and Distribution of Clay Mineralsin the Alexandroupolis Gulf, Aegean Sea, Greece Estuarine, Coastal and Shelf Science (2000) 00, 000–000 doi:10.1006/ecss.1999.0620, available online at http://www.idealibrary.com on Origin and Distribution of Clay Mineralsin the Alexandroupolis Gulf, Aegean Sea, Greece K. Pehlivanogloua, A. Tsirambidesb and G. Trontsiosb aDepartment of Oceanography, Hydrographic Service, Hellenic Navy, T.G.N. 1040, Holargos, Athens, Greece; e-mail: [email protected]. bDepartment of Geology, Aristotle University of Thessaloniki, 540 06 Thessaloniki, Greece Received 29 March 1999 and accepted in revised form 18 December 1999 The mechanisms of clay mineral distribution in Alexandroupolis Gulf are studied. The annual solid supply of the Evros River, flowing into the Gulf, amounts to at least 1 000 000 m3. The surficial bottom sediments are commonly fine-grained and are distributed along zones almost parallel to the coastline. In the central part of the Gulf clay-silt size sediments predominate. The main clay minerals in the size fractions (2–1, 1–0·25 and <0·25 m) are illite, smectite, kaolinite and in small amounts interstratified illite/smectite. Quartz, feldspars, amphiboles and chlorite occur in traces in the coarser fraction (2–1 m) of some samples. All the above minerals are the weathering products of the Evros River drainage basin, as well as of the Neogene and Quaternary unconsolidated sediments of the coast. The hydrodynamic regime and physical grain size are the main mechanisms, which control the distribution of the clay minerals in the Gulf. The low content of kaolinite in all samples and the presence in traces of chlorite and amphiboles in some coarse clay fractions may be due to the unfavourable climatic and physicochemical conditions, as well as to the rapid transport and deposition of freshly weathered material. 2000 Academic Press Keywords: clay mineral distribution; river solid supply; Alexandroupolis Gulf; Aegean Sea Introduction (1976) and Biscaye and Eittreim (1977) showed that suspended particulate material in the Atlantic ocean The general scarcity of clay sized sediments in shallow ranges from 5 to 300 gkg 1 mainly depending on water, due to winnowing through the action of waves, regional characteristics. Chamley et al. (1977) ob- tides and currents, contrasts with the huge accumula- served an increase of relative abundance of smectite tions of argillaceous deposits in the rest of the oceans. and palygorskite from 1000 to 3000 m water depth in Where they do occur, source mixing during transpor- sediments off NW Africa, which is attributed to a late tation, flocculation and differential settling processes deposition of these fine and low-flocculable minerals. appear to be the main mechanisms for their distribu- Preferential clay settling was also proposed for the tion (Griffin et al., 1968; Chamley, 1989). Gibbs Ganges sediments, where increased amounts of smec- (1977) reports that the most probable explanation for tite in hemipelagites are reported offshore from the the clay mineral variations off the mouth of the coastline (Bouquillon & Chamley, 1986). Amazon River is a physical size segregation. Addition- Preferential settling of smectite and expandable ally, Chamley (1989) suggests that the aggregation of mixed minerals represents a common phenomenon in clay particles by marine organic matter appears to be a the western Mediterranean Sea. Chamley (1971), widespread phenomenon, mainly responsible for the Monaco (1971) and Roux and Vernier (1977) report rapid sinking of land-derived materials. Clay is mainly a frequent increase of expandable minerals at in- incorporated in fecal pellets and other mucous matter creased distance from the shore of the Gulf of Lion. In within the surface water masses where high planktonic the Adriatic Sea, mechanical sorting and flocculation productivity develops seasonally. account for the distribution of clay suites derived from Gorbunova (1962) observed a decrease in kaolinite the Po and other rivers (Veniale et al., 1972; Tomadin abundance with increasing distance from the Indian & Borghini, 1987). coast because of changes in conditions of marine In this study the mechanisms responsible for the transportation. The occurrence of grain sorting was distribution of the clay minerals in the Alexandroupo- suggested later by many researchers. Brewer et al. lis Gulf are investigated. 0272–7714/00/000000+00 $35.00/0 2000 Academic Press 2 K. Pehlivanoglou et al. 40° 55' N 0 n.m. 3 n.m. 6 n.m. 9 n.m. 12 n.m. 15 n.m. Makri Alexandroupolis 40° 50' Evros River ° 40 45' 20 50 30 30 40° 40' 40° 36' 25° 30' 25° 35' 25° 40' 25° 45' 25° 50' 25° 55' 26° 00' 25° 05' E F 1. Bathymetry of the Gulf of Alexandroupolis (depths in m). Geographic setting of the study area Oceanography Seasonal measurements of oceanographic parameters Hydrography (salinity, density etc.) during maximum discharge The Gulf of Alexandroupolis covers an area of periods have shown that water of low salinity, 26–34 350 km2 and constitutes the NE part of the Thrace (using the Practical Salinity Scale) and low density Sea (Figure 1). The Evros River flows into the eastern (1·0019 g cm3)diffuses at shallow depth (up to 5 m) part of the Gulf through a lobate type delta, which has into the sea, in a SE direction (Hydrographic Service, an area of 188 km2. The total drainage basin of the 1984). This water, with slightly changed parameters, Evros is 52 500 km2, extending from Bulgaria through can be traced up to 30 km from the river mouth. Turkey to Greece. The length of the main branches of Towards the bottom, the salinity and density gradu- the Evros is 410 km (Psilovikos & Hahamidou, 1987). ally increases, thus confirming that the initial surface The wide range of estimates on sediment discharge of layer gradually sinks and is mixed with the ambient the Evros River in the Greek literature is very confus- sea water with increasing distance from the river ing. Psilovikos et al. (1993) estimated the sediment mouth. discharge of the Strymon River (about 200 km west of From current measurements during the minimum Evros), which has a drainage basin of 11 000 km2,at discharge periods (July), at distances of about 10 km 1 000 000 m3 annually. They used geomorphological from the river mouth, a distinct retrogressive motion data of the whole drainage basin, examined about of the seawater is noticed with NW to SE direction. It 1000 samples taken close to the main bed during shows changeable range of 10–30 km, average velocity floods for a period of 2 years and compared old of 17 cm s1 and maximum velocity of 40 cm s1, and new maps of the morphology of the area. Thus, with a WNW to ESE direction. In contrast, current taking these data into account, the annual sediment measurements during March and under the action of discharge of the Evros River should well exceed south winds, showed motion of the seawater towards 1 000 000 m3. Aksu et al. (1995), using a mathemati- west, parallel to the northern coastline (Hydrographic cal formula, suggest an average annual sediment Service, 1984). yield of approximately 107 tonnes. In addition, a According to the data of the National Meteoro- number of small creeks flow into the N and NW part logical Service of Greece (Alexandroupolis Airport of the Gulf. Station) the broader area presents average annual Origin and distribution of clay minerals 3 Legend Fluvial deposits (sands, pebbles etc) Greece Conglomerates, sandstones, schists, mudstones, marbles, andesites Volcanic rocks interstratified with sedimentary rocks Schists, limestones, dolomites, marbles Pliocene-pleistocene deposits Turkey Crystalline rocks and migmatites (leptites, gneis, schists) Granites and diorites Flysch Ultrabasic rocks Pyroclastic rocks Igneous rocks F 2. Petrographic sketch map of the Evros river drainage basin (Pehlivanoglou, 1995). rainfall of 576 mm and the predominating winds metamorphic rocks (Figure 2). Plutonic intrusions, as have mainly NE (25%), N (13%) and SW (10%) well as volcanic rocks of rhyo-dacitic composition, directions. Calm period is 32%. outcrop in small areas of the basin. During early Tertiary time the meta-alpine basin of Thrace was formed and filled with molassic sediments that lie Bathymetry unconformably on the rocks of the greater region The bathymetry of the Gulf was studied from the (Mountrakis, 1985). Calc-alkaline volcanism of bathymetric diagrams of the Hydrographic Service of Eocene-Oligocene age produced extensive deposits of the years 1966, 1967 and 1978 with scale 1:5000, as volcaniclastic tuffs interbedded with a variety of other well as from the bathymetric charts of the area with sediments (Arikas, 1979). Finally, a transgressive se- scale 1:50 000 and 1:75 000. The relief of the Gulf quence of Miocene coastal sediments was deposited bottom as well as of the surrounding area is smooth on the Oligocene sediments (Papadopoulos, 1980; with very low gradient. Thus the Gulf bottom seems Solakius and Tsapralis, 1987). The meta-alpine sedi- almost flat (Figure 1). The sea depth, even at large ments (conglomerates, sandstones, marls, marly lime- distances from the coast, is low and does not exceed stones etc.) were rapidly deposited during periods of 35 m. The bottom gradient is less than 1% except in high seasonal rainfall. As a result, physical and chemi- the SE and NW edges of the Gulf where the relief is cal weathering processes and reworking of these sedi- more intense (1–2% dip). After the isobath of 30 m, ments was of limited influence (Trontsios, 1991). The an elongate undersea platform exists at an average large discharge of sediments from the land, into the depth of 35 m with SE–NW direction. coastal basin, while initially was periodically sub- merged and later crossed by the Evros River, resulted in the formation of 3000 m thick sediment beds in Geology front of the river mouth and 1500 m thick in the The drainage basin of the Evros River is part of the western part of the Gulf (Lalechos, 1986).
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