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Mediterranean Marine Science Vol. 2, 2001 Coastline changes in relation to longshore sediment transport and human impact, along the shoreline of Kato Achaia (NW Peloponnese, Greece) POULOS S. Department of Geology, Division of Geography- Climatology, University of Athens, Panepistimioupoli, Zografou 157 84, Athens CHRONIS G. Hellenic Centre for Marine Research, Institute of Oceanography, P.O. Box 712, P.C. 19013, Anavyssos, Attiki https://doi.org/10.12681/mms.271 Copyright © 2001 To cite this article: POULOS, S., & CHRONIS, G. (2001). Coastline changes in relation to longshore sediment transport and human impact, along the shoreline of Kato Achaia (NW Peloponnese, Greece). Mediterranean Marine Science, 2(1), 5-14. doi:https://doi.org/10.12681/mms.271 http://epublishing.ekt.gr | e-Publisher: EKT | Downloaded at 07/10/2021 01:47:25 | Mediterranean Marine Science Vol. 2/1, 2001, 5-13 Coastline changes in relation to longshore sediment transport and human impact, along the shoreline of Kato Achaia (NW Peloponnese, Greece) S.E. POULOS1 and G.TH. CHRONIS2 1 Department of Geology, Division of Geography-Climatology, University of Athens, Panepistimioupoli, Zografou 157 84, Athens, Greece 2 National Centre for Marine Research, Institute of Oceanography, Aghios Kosmas, Helliniko 166 04, Athens, Greece. Manuscript received: 16 March 1999; accepted in revised form: 29 March 2000 Abstract Coastal configuration depends upon the equilibrium between available sediment budget and prevail- ing nearshore wave and current conditions. Human activities often disturb this natural equilibrium by altering the sources of beach material and littoral drift pattern. In the coastal zone of the NW Peloponnese, an essentially tideless environment, the oblique approach of wind-induced waves implies an overall longshore drift from east to west. On an annual basis, the potential longshore sediment transport rates in the different sections of the study area (Kato Achaia) is estimated to vary between 0.02 10-3 m3/s and 5x103 m3/s and to fluctuate seasonally. The construction of a port and the extraction of aggregates from the R. Peiros have significantly changed the pattern of sediment transport, inducing dramatic changes in coastline configuration; thus, the part of the coastline west of the port has retreated as much as 70 m, eliminating a tourist beach, while the entrance to the port has silted up, inhibiting navigation. Coastal engineering measures, such as modification of port-breakwaters and construction of groins have made an only minimal contribution to beach recovery. Hence, coastal management plans should con- sider this dynamic equilibrium and protect the natural coastal system from arbitrary human activities. Keywords: Coastal zone, Sediment transport, Shoreline erosion, Human impact, Greece. Introduction A shoreline is a dynamic system with sed- by the existing (locally) wind-induced wave iment moving continually, being deposited climate. Furthermore, the oblique approach here and eroded there, as the shoreline of the waves generates longshore currents attempts to establish an equilibrium with that transport sand parallel to the shore, if it respect to available sediment budget and is not intercepted and moved offshore by rip prevailing nearshore marine processes. In currents. Hence, the natural evolution of the microtidal environment of Greek waters, coastline configuration depends primarily shoreline morphodynamics are dominated upon the offshore wave conditions, the asso- Medit. Mar. Sci., 2/1, 2001, 5-13 5 http://epublishing.ekt.gr | e-Publisher: EKT | Downloaded at 07/10/2021 01:47:25 | ciated longshore current activity, coastline The present study concerns the coastal morphometry, sedimentary material of the area of Kato Achaia (NW Peloponnese, sea-bed and the overall sediment budget of Greece) where human activities such as any coastal cell under consideration abstraction of aggregates from the lower (CARTER, 1988). reaches of the R. Peiros and the construc- Many studies, concerning the coastal tion of a small port have caused extended zone of the Mediterranean Sea, have shown changes in the coastline. The subsequent that until the beginning of the 20th century measures undertaken against changes (i.e. the general trend has been one of growth groins) have produced further alterations to (LEWIN et al., 1995); this has been excep- the configuration of the coastline. For the tionally pronounced in the case of coastlines near river mouths. In contrast, over the last purpose of this investigation longshore sed- few decades human activities (e.g. construc- iment transport rates are estimated, on a tion of dams) have caused a dramatic reduc- seasonal basis, and related to human- tion in sediment supply from the rivers, induced coastline changes over the last 20 while coastal structures often disturb the years, as indicated by aerial photographs. natural equilibrium between the sources of beach material and the littoral drift pattern, The Study Area frequently resulting in a general coastal ret- reat. For example, erosion has been report- The coastal cell, under investigation, is ed not only in the case of the deltaic coasts that part of the southern coast of the Gulf of of major Mediterranean rivers such as that Patras (NW Peloponnese) extending from of the R. Nile (Egypt) (FANOS, 1995), the R. the mouth of the small R. Peiros, in the east, Ebro (Spain) (MARINO, 1992), the R. Axios (Greece) (POULOS et al., 1996), but also to the region of the coastal cliff (named along other parts of the Mediterranean “Liritzi cliffs”), in the west (Fig. 1). The shoreline in Spain (MARQUES & JULIA, Gulf of Patras is a Plio-Quaternary graben 1986), Tunis (PASKOF, 1992) and Italy (PIPER et al., 1990) with maximum water (BAVESTELLO et al., 1995; COLANTONI et al., depth of 130 m. To the west, it opens into 1997). the Ionian Sea and to the east, it is linked Fig. 1: The study area (I: Raxi Liritzi; II: White Castle Hotel; III: promontory; IV: river mouth). 6 Medit. Mar. Sci., 2/1, 2001, 5-13 http://epublishing.ekt.gr | e-Publisher: EKT | Downloaded at 07/10/2021 01:47:25 | with the Gulf of Corinth via the narrow (<2 to play the dominant role in littoral sedi- km) and shallow (∼ 62 m) Rion strait. ment transport. The coastal cell consists of recent Wind data (of hourly measurements for marine and fluvial deposits of, mostly, fine- the period 1965-1985) comes from the grained and loose sediments. The nearby Araxos airport, located some 30 km WNW inland zone is formed by Plio-pleistocene of the study area. Wind climate is charac- lagoonal deposits (i.e. Liritzi cliffs; after terised by long calm periods varying from DOUTSOS et al., 1988) and Holocene alluvial 34% (March) up to 41.3% (July) and maxi- formations represented by sandy, silty and mum values of wind speed rarely exceeding conglomerate formations (Fig. 1). In partic- 20 m/s. On a seasonal basis (Fig. 2), the ular, the backshore area is characterised by wind climate during winter and autumn is the presence of sandy formations whice similar, characterised by the dominance of locally exceed 400 m in width and reach ele- NE and E winds. In spring, the winds are vations of up to 10 m. Seaward the littoral more evenly distributed, although the NE zone deepens gently (1.5o-4o) reaching component is the principal one for winds water depths of 10 and 20 m at distances of ≥4B. Summer winds are generally weaker 1.2 and 2 km, respectively. Bed material of (<4B) and blow mostly from westerly direc- the nearshore zone consists mostly of sandy tions (SW, W, NW). deposits with mean grain-diameter between 0.1 and 0.5 mm (THALASSINOS, 1988). Methodology The coastal area under investigation, at its eastern limit, receives water and sedi- In the absence of wave records, wave ment fluxes from the small River Peiros; it characteristics required for the calculation drains a mountainous area of 437.5 km2 with of the rate of wave-induced longshore sedi- elevations exceeding 1000 m. A gross esti- ment transport have been estimated using mate of water and suspended sediment dis- wind data. Thus, the significant wave height 3 3 charge of 9.7 m /s and 120x10 tonnes/yr, (Hs) and the peak period (Tm) of the wave respectively, have been attributed to the R. spectrum, are calculated for the dominant Peiros (after POULOS & CHRONIS, 1997). fetch directions (NW, N, NE and E), using The study area, as part of the Gulf of deep-water (d/L<0.25; d: water depth and Patras, is characterised only by minimal L: wave length in deep waters), wave fore- tidal ranges (<10 cm; after TSIMPLIS, 1994). casting equations for the fetch-limited case Thus, the locally wind-induced waves and (CERC, 1984): associated longshore currents are expected Fig. 2: Schematic presentation of seasonal distribution of wind velocity and direction. Medit. Mar. Sci., 2/1, 2001, 5-13 7 http://epublishing.ekt.gr | e-Publisher: EKT | Downloaded at 07/10/2021 01:47:25 | to their compass orientation (see Fig. 1); (1) this satisfies also the restrictions for the use of equation 4. All the units are exposed to (2) NW, N, NE and E winds with the exception of the units B and D that are not exposed to where, W is wind stress (m/s) related to the winds from the east. The fetch lengths measured wind speed (U) through the equa- for the different directions and the corre- tion W=0.71 U1.23, F is the fetch in m, while sponding angles between the wave crests the prediction of both Hs and Tm is based and the shoreline of the units (A-D) are upon the assumption that wind blows over summarised in Table 1. the sea surface for a sufficient time for the For the calculation of the longshore generated waves to obtain their maximum transport rate (Ql), for each of the four units height under the given fetch limited condi- (A-D), the winds blowing from different directions are grouped into four categories, tions.