Sonderdruck aus STUDIA TROICA Band 1 · 1991
VERLAG PHILIPP YON ZABERN · MAINZ AM RHEIN INHALT - CONTENTS
Teil A: Teil B: Troia und Troas - Aktuelle Ausgrabungen Weitere Forschungen und Rezeptionen und Umfeld
1. Troia 1. Forschungsgeschichte
Manfred Korfmann: J ustus Cobet, Emre Madran and Troia - Reinigungs- und Dokumentations Nimet Özgönül: arbeiten 1987, Ausgrabungen 1988 und 1989 From Saewulfto Schliemann. A Preliminary Bibliography of Travel Books about Troy Günter Mansfeld: and the Troad ...... 101 Pinnacle E 4/5 - Bericht über die Ausgrabung 1988 ...... 35 Donald F. Easton: Troy before Schliemann 111 Stella G. Miller: Terracotta Figurines. New Finds at Ilion, 1988-1989 ...... 39 2. Frühere Grabungen
Charles Brian Rose: Dieıer Hertel.· The Theater of Ilion 69 Schliemanns These vom Fortleben Troias in den 'Dark Ages' im Lichte neuer Forschungsergebnisse ...... 131 2. Der Naturraum Stefan Hiller: İlhan Kayan: Two Trojan Wars? On the Destructions of Holocene Geomorphic Evolution of the Troy Vlh and Yiia ...... 145 Beşik Plain and Changing Environment of Ancient Man ...... 79 Jerome Sperling: The !ast Phase of Troy VI and Mycenaean Jehuda Neumann: Expansion ...... 155 Number of Da~ s that Black Sea Bound Sailing Ships were delayed by Winds at the Entrance to the Dardanelles near Troy's Site 93 3. Troas und Agais
Dimitris Matsas: Samothrace and the Northeastern Aegean: The Minoan Connection ...... 159
Danksagung - Acknowledgements ...... 18 1
V, 182 Seiten, 102 Abb. im Text, 8 Farbtafeln
© 1991 by Philipp von Zabern, Mainz anı Rhein ISBN 3-8053-1124-9 Preis: DM 148,- HOLOCENE GEOMORPHIC EVOLUTION OF THE BEŞiK PLAIN AND CHANGING ENVIRONMENT OF ANCIENT MAN
İlhan Kayan
I. Introduction and prehistoric-historic settlements in the environs of ancient Troia. This study found a transgression Troia and its environs form one of the most of rising sea level into the lower part of the interesting prehistoric and historic areas on the Karamenderes (Scamander) and Dümrek (Simois) Aegean coast ofTurkey (Figs. 1and2). The loca valleys during the Holocene (Fig. 2). The results tion of Troia has been a serious subject of discus were based on core drilling with radiocarbon dates sion among many scholars and some of them have from shells and some organic muds. In order to studied this prehistoric-historic site for a long determine the nature and depth of the sedimentary time. Many studies and excavations have been environments and their deposits, seven drill cores, done at Troia and the site played an important role the deepest down to 75 m, were obtained along the in advancing archaeology as a science. axis of Karamenderes and Dümrek flood plains. The Beşik plain and its environs are another well Core drilling was done in cooperation with known part of the Troad. Part ofthe importance of General Directory of Mineral Research and Ex this area is based on a harbor theory (Korfmann ploration Institute of Turkey (M.T.A.). Three 1986 and Latacz 1986). Some scholars have dimensional shapes of the sedimentary units suggested that the harbor of Troia was in Beşik deposited in each environment were delineated. bay instead of the mouth of the Karamenderes The older deposits in the valleys consisted of pre (Scamander) river, which joins the Çanakkale Holocene shallow marine sediments and early Strait (Dardanelles) in the north (Fig. 2). There Holocene river deposits covered by coastal and fore, fıeld investigations have been made in this shallow marine sediments from rising sea level small coastal plain. One study by Mey (1926) during the Holocene. Then, flood plain deposits of obtained important evidence from test pits on the the Karamenderes and Dümrek rivers overlaid the plain. They indicate that the present plain was an marine sediments progressively. Yang (1982) indentation of the Aegean sea in ancient times and studied the microfauna of the sediments to inter it was possible that the people of Troia used this pret the different sedimentary environments. bay asa naturally sheltered harbor. This evidence Paleogeographic sections, based on information is stili being discussed . about sediments below the present flood plain, Studies of Troia and its environs have shown that showed the pre-Holocene marine sedimentary the geomorphic environment was different from unit, about 40 m below the present sea !eve!, had the present during the earliest known stages of been cut by rivers during the pre-Holocene regres human occupancy of the area. This has led to some sion of the sea and then covered by fluvial coarse paleogeographical research. sediments. About 10.000 years before present, the General information on the geology and geography rising sea Jevel invaded the valley. The marine of the region is available from Darkot (1938 and transgression extended about 15 km south and 1938a), Yalçınlar (1949), Erinç (1955), Inandık inland by about 7.000 B. P., when sea level was (1958) and Erol (1969, 1976, 1981 and 1983). still much lower than at present (about -20 to Bilgin (1969) and Erol (1972) have studied and -10 m). The sea level continued to rise, but ata published specifically on the geomorphology of much slower rate. The Karamenderes and its lower the area. tributaries, like the Dümrek river, filled the nar Kraft-Kayan-Erol (1980 and 1982) investigated row marine embayment with alluvium. Sea !eve! the relationship between paleogeographical changes reached its present position about 6.000 B. P. 80 İLHAN KAYAN
o 20 ı.o km
~ MOUNTAINS E:3 PLATEAU (DEEPLY DISSECTED) [;]. A LLUVIAL PLAINS, DE LTAS ,,r-' RIV E RS 1774 ELEVATIONS i N METE RS • MODERN CITY
GÖK ÇE ADA
Fig. l Geomorphological outlines of the Biga peninsula and location of the Beşik plain.
Alluvial deposition from the rivers into the marine Dümrek flood plain and Aegean Sea were con embayment increased and the Karamenderes sidered in the study of Kraft-Kayan-Erol (Fig. 2). Dümrek flood plain formed . During the earliest The cliff along this straight coastline has been known human occupancy of the area, ca. 6.000 eroded and it receded through the wave action of B. P., the physiography was completely different. a rising sea level during the Holocene, especially The present flood plain of Karamenderes-Dümrek after the sea reached almost to its present level rivers was a marine embayment. in this early ca. 6.000 B. P. Along this steep coastline, the period, Kumtepe and a later Troia 1 were estab present Beşik plai n shows a different geomor lished on the coast of this narrow marine em phological history as a coastal depositional area. bayment. Mey ( 1926) established that there was a small Geomorphological changes along the coast of the bay here extending about 2 km inland. He narrow Neogene ridge between the Karamenderes- (1926) considered paleogeographical changes HOLOCENE GEOMORPHIC EVOLUTION OF THE BEŞiK PLAIN 81
HHJ HI GH PLATEAU (200-250 m ) ÇANAl ~ BEACHES ~ RI VERS ... SPRINGS ~ VILLAGES 50 ELEVATIONS iN MET ERS e ARCHAEOLOGICAL SITE S K KU MTEPE 5 BEŞiK - SIVRITEPE Y BE$1K - VASSITEPE A ARAPLAR GORGE +N J km Fig. 2 Geomorphological outlines of the Troia area and the B eş i k plain. since prehistorical times and dug some test pits on geomorphology was first studied and mapped the plain. He found marine sediments below the (Pi. 5). Small test pits were dug in 1983 in order present colluvial surface. Based on this, Mey to understand subsurface sedimentary environ hypothesised that Beşik bay had been a calm and ments, especially on the old coastal barrier extend sheltered bay-coast during the Trojan War and the ing NW-SE in the middle of the Beşik plain physiography was convenient for Achaean ships as (Fig. 3). However, high ground water, less than a natura] harbour. 2 m below the surface, prevented deeper test pits. Prof. Dr. M. Korfmann has initiated a new era in A small gouge auger also was incapable of sampl Troad research. The first project began on the ing deeper sections, especially in sandy sediments. Beş i k plain in 1981 with an intensive survey and in 1985, a large trench was opened by a machine excavation program especially aJong the north at the foot of Beş ik-Ya ssıtepe , below the newly edge of the plain, at Beşik-Sivritepe and Beşi k discovered cemetery. Erol fo und fine beach sands Yass ıtepe. Since its inception this new Troia pro here, up to 1 m above present sea level. However, ject has considered the important effects of the they were supralittoral sediments, not enough to paleogeographic change on cuJtural change. Korf indicate that sea level was higher than currently mann invited us to join the project and undertake during the late Holocene. studies of the environment and paleogeography of These studies ali showed that a systematic drill the area. Our work started with Prof. Dr. O . Erol coring program needed to be done to make in B eş i k plain and its environs in 1983. Present satisfactory paleogeographical reconstructions of 82 İLHAN KAYAN o __,500 m .... __--_ CONTOUR LINES ~ (lnterv•l 2m, duhed 1 m) s SPRINGS DRILL S OR TEST PITS: o 1-6 O. MEY 1926 M. KORFMANN 1982, 1985, 1988 • 1-7 O. EROL 1983 • 01-74 1. KAYAN 1986, 1987, 1988 Fig. 3 Topographical map of the Beşik plain and the drill sites. the Beşik plain. Of special interest was the vertical sediments using Edelman and Riverside augers. and horizontal position of old coastlines and their These penetrated a maximum of 7 m. In addition, relation to the newly discovered cemetery. Core a thin gouge auger was used for a quick examina drilling started in 1986. Seventy cores were taken tion of shallow subsurface features such as locating in two years on the Beşik plain of about 4-5 krn2 the top surface of the marine sediments under the area (Fig. 3). A hand auger was used for most of terrestrial or eolian deposits covering them. Since the holes. it was possible to core most of the the highest parts of the Beşik plain are about 2 m HOLOCENE GEOMORPHIC EVOLUTIO"I OF THE BEŞiK PLAIN 83 ı- p R E S E N T BEŞ 1 K P LA 1 N L AT E HO LOCENE B A y ) .!!!. w E m 6 8 Dun e CoHtline AEGEAN: Be•ch 2 SEA ! 13 2 o o -2 -2 -1. _, -6 CoHtlin• positions : - 6 al Present -8 - 8 ~ 2000 Y.8.P. ~ 3500 Y.B.P. cr> 6000 Y.8.P. o 100 m 1 km Time Archaologic.ıl Se• Su-lttvel Sediment•ry env i ro nment.ıl s t r•tigr•phic units Sc•le Chronology Level Ch•ngu •nd geomorp hic processes (YBP) (m) o- --PRE SENT - -- o Aggr•d•t ion •nd progr•d•tion : 1000 - RISING 5 Reced ing s e • and l ow dune form.ıt i on behind the very fl at .ınd t ine Hndy buch 2000- ~ Str•bo's t ime - 0.5 ı S tillst.ın d 8Wıo.ıt her i ng s urface (r eddish) w ith some sherds TRISING form•t ion ( yellowis h ), ~ Homer's time O B• r r i ı>r s •ndy - gr.ıve ll y 3000- ı D vertic•l ch.ınge in t he c o.stline "T ROİAN WAR" L•te UJ T roi• VI - 2 (!) .... . <ı 4000 - Mıddle uı ... T ro i.ı ııı - ıv -v N :::.«::,":"::: ..: :, •hoc,. T ro i .ı il ::;:.~::~.. , B· ::'.h.::,~: z ... E•rly o BEŞİK - ( greyish sandy - g r .ı v e l ly ) T ro i .ı 1 (Slow) Q'. ... YASSITEPE aı 5000 - o l H 2b : Co.ı s tal s w• mp. Fine r sediments f l o ~ • l u Stillst •nd MAX IMUM EXTENS IO N OF T HE SEA r l!mıi ns o 6000- - -~ L .ıte BEŞİK-SİVR İ T EPE :I: (Kumtepe 1 A) ..... R ISI NG S h.ıllow m.ı rin e ba r f or mation 7000- - _, 8000 - o - 4 Stillst.ınd H 1 •: Sapropelic l a yer. Fi n er sedim ents in shallower co as t .ı l-L .ı goon .ıl sw.ı mp UJ l RISI NG Tr •nsgressive s hallow mari ne 9000- z sandy - gr.ıvel ly sedi m ents PRE - HOLOCE NE S M Shallow muine . Bluish-grey f ine s• nd wi th f req uent L.ıyers of c oashl flor•l r em• İ n s. 3. S h• llow muine - l•goon.ıl mud (d.ırk green-grey, silty, h.ı rd mud) L C L•goon•l co•st. Greenish -grıoy si l ty - s.ı n dy mud with flo r .ıl remains • nd shells. 2 . Terrestri.ıl-co•st.ıl mottled h>rd mud LA L.ıgoon;ı l mud. Mos t ly d.ı r k gr ey or b l ;ı ck is h, 1. Neogene bedrock p.ırtly greenish d .ı r k gre y st icky mud (mudstone, sandstone, limestone) wit h flor•l r em•ins ;ınd shells. Fig. 4 Holocene geomorphic evolution o f the Beş ik embayment and correlati on wi th the archaeolog ical cvidence . 84 İLHA N KAYAN higher than the present sea level, the hand augers Kazdağı ridge where several towns are located: penetrated about 5 m below mean sea level. This Ezine, Bayramiç, Çan, Biga (Fig. 1). This strip is vertical section contains about 6.000 years of sedi a !ine of small depressions formed by young tec ment deposited in different environments such as tonic movements. The depressions are separated shallow marine, coastal, lagoonal and terrestrial. into two sections between Bayramiç and Çan by a Until 1987 information about the sediments and volcanic belt about 500 m high. The Çan river their correlation was used to develop paleogeo flows in the NE part and the Ezine-Bayramiç basin graphical maps. In 1987, about 10 samples were of Karamenderes river is located in the SW part of taken from subsurface sedimentary units for C 14 this depression belt. The Ezine-Bayramiç part is a dating. These samples were dated by Dr. Kromer Neogene basin filled by soft, easily erodable, at the Institut für Umweltphysik der Universitiit sandy-clayey-limy sediments. Therefore, the Heidelberg. The C 14 dates correlated well with Karamenderes river and its upper tributaries have the paleogeographical reconstructions. eroded this area and formed a low river basin with In 1988, Prof. Korfmann shifted his project to the an alluvial plain. main site of Troia near Tevfikiye. Daimler-Benz The 'Salihler plateau' (Bilgin 1969) extends to presented a UNIMOG work-machine for the new the north of the Ezine-Bayramiç basin about Troia excavation to which Korfmann added a 250- 300 m high (Fig. 1). The surface of this hydraulic auger. This powerful machine became plateau, which cuts different lithological units, is known as the " Archaeomog" in Troia. Archae a low undulated erosional surface descending omog coring was tested on the Beşik plain in 1988. gradually to the NW. The Karamenderes river cuts Four holes were augered; each penetrated 11 .5 m this plateau with a deeply incised meandering to the base of the Holocene sediments (Fig. 3 drill valley in the NW Ezine-Bayramiç basin. This hole numbers 71 to 74). Thus, the new drill made 'Araplar gorge' connects the Ezine-Bayramiç it possible to describe the changing sedimentary basin to the low flood plain of Karamenderes river environments and paleogeography during the en and the Çanakkale Strait. The source of the great tire Holocene (Fig. 4). amount of alluvium in the Karamenderes flood plain is soft Neogene sediments in the Ezine Bayramiç basin controlled by slower erosion in the hard rocks of Araplar gorge. II. Setting of Beşik plain North and west of Araplar gorge the surface in the geomorphic outlines of Biga descends by a step-like slope from the Salihler peninsula plateau to a lower plateau surface on the Neogene sediments along the SE border of Çanakkale Strait Beş ik plain is a small lowland located on the west (about 60-80 m high). This plateau extends as low coast of the Biga peninsula which is the largest ridges toward the Aegean Sea. The lower valley of extension of Anatolia toward the west between the Karamenderes river and its lower tributaries are Marmara and Aegean seas (Fig. 1). The main situated on this plateau and filled by alluvium structural and geomorphological lineation through forming the flood plains. the peninsula is SW-NE. Kazd ağ ı (Kaz mountain) Neogene (Upper Miocene-Pliocene) shallow in the SE and Çanakkale strait and Gelibolu penin marine, unconsolidated sediments (mostly sand sula in the NW are the most distinct elements stone, conglomerate, marl) occur between the of this elongation. Between them, the Ezine Salihler plateau and the Çanakkale Strait. They Bayrarniç-Çan-Biga depression belt and Salihler were deposited in a shallow bay extending from the plateau ridge are alsa clearly seen as low and high Black Sea (Paratethys) toward the SW during the topographic expressions. The ridge of Kazdağ ı Sarmatian period of the Upper Miocene. There (1774 m in the NE and 500- 600 m in the SW) was a land bridge in this period between the consists ofa granitic core with a gneiss surround Anatolian and Greek peninsulas separating the ing it. Black Sea from the Mediterranean (Erol 1969). A strip of lowland extends along the NW foot of The configuration of the course of Karamenderes HOLOCENE GEOMORPH1C EVOLUTION OF THE BEŞIK PLAIN 85 river is explained by this Neogene paleogeo slopes are gentle with some small structural plat graphy. The Çanakkale trough emerged as land in forms or terraces. Troia is located at the west end the Pliocene forming a river valley collecting of the Tevfikiye ridge. Thus it has a commanding water flowing toward the north. In the Quater position overlooking both the Karamenderes plain nary, especially after the Middle Pleistocene, the in the west and the Dümrek in the north (Fig. 2). Mediterranean advanced northward graduaJly and West of Karamenderes flood plain is another the Çanakkale "valley" became the strait it is ridge of the Neogene sediments, Yeniköy ridge, today. separating the Karamenderes plain from the Lowered sea level during the glacial stages of Aegean sea. This ridge is about 1O km long, 1- 1 .5 the Pleistocene caused increased erosion of the km wide, and 40-60 m high. The layers of this easily erodable Neogene sediments. Valleys became ridge are almost horizontal or very slightly tilted deeper and wider. However, during the inter eastward. Wave erosion has formed a straight cliff glacial stages shallow marine-estuarine sedimenta !ine along the Aegean coast. East-facing slopes are tion advanced into the mouths of the deepened very gentle, irregular in shape with some flat steps river valleys. This process was repeated at least related to the underlying structure. twice. Drill core evidence and C 14 dates show The west coast of Biga peninsula lies fairly straight that there were some shallow marine-estuarine in a north-south direction. Its profile shows a steep sediments in the Karamenderes valley from the cliff about 40 -60 m high in the soft Neogene previous high sea !eve! stages (probably Ri ss sediments. Although there are no deep indenta Würm or mid-Würm). They were deeply incised tions, there are small alluvial flats along the by the rivers during the !ast glacial stage Aegean coast. Some of them are delta plains at the (Würm) when sea level dropped about 100 m mouths of small rivers located along weak struc (Kraft et al. 1980). The present flood plain of the tural lineations or in depressed zones of the Karamenderes river and its lower tributaries Neogene bedrock. However, no important river or formed during rising sea level in the Holocene. large delta plain occurs. The biggest river is the Plateau ridges about 60- 80 m high lie between the Tuzla river in the south and its coastal-delta plain Karamenderes river and its lower tributaries is more extensive than the others (Fig. 1). (Fig. 2) . These ridges formed on the Upper The west coast of the Biga peninsula has been Miocene-Pliocene shallow marine sedimentary an important area for occupation and cultural rocks. They are mostly sandy sediments inter development since prehistoric times. The locations bedded with more resistant marl or limestone of archaeological sites imply some relation to the layers and some terrestrial mudstone especiaJly small coastal embayments which were convenient toward top. The sediments are almost horizontal in harbours along this straight and steep coastline. some places, but in others are tilted or faulted. Such places are not marine indentations today, but Thus some ridges show cuesta features and some alluvial plains, having straight coastlines in the structural terraces are related to lithological same direction as the coastal cliffs. However, it differences. is clear that the small alluvial coastal plains had The flood plain of the Karamenderes river occurs been marine embayments before they filled with between the exit from Araplar gorge and the alluvium. The geomorphological and sedimento Çanakkale strait, a distance of 15 km with an logical evidence obtained from the drill cores in the average width of 4 km (Fig. 2). Two west-east alluvial fili of the Beşik plain ha ve been very useful ridges lie in the eastem section of this plain : in understanding this process. Yenikumkale ridge in the north and Tevfikiye ridge in the south. The Dümrek river with its wide flood plai n lies between them joining the III. Geomorphology of the B eş ik Karamenderes plain in the west. Both ridges plain formed on Neogene layers tilted slightly southward. Therefore the northern slopes at the Beşik plain is the first embayment along the steep ridges are steeper and straighter. South-facing coast extending southward from the Aegean mouth 86 İLHAN KAYAN of the Çanakkale strait (Fig. 2). This small plain drains to the sea through the old coastal barrier in occurs on the coastal part of a NE-SW structural the middle of the plain. Although the lagoon is dry lowland between low plateau ridges of Yeniköy during summer seasons, it cannot be used for in the north and a wider part of the same plateau agriculture because the soil is too clayey and has in the south. The plain is separated from the halomorphic-hydromorphic characteristics. Agri Karamenderes plain by a very low (below 10 m) cultural areas have been extended recently from and small threshold in the NE. Loose and fine the edges by using better agricultural tech marine sand cover with shell fragments on the nıques . threshold suggests that the sea once passed over Rain erodes soil from the adjacent plateau and this threshold. However, there is no evidence that slopes and carries it to the edge ofthe plain. Thus, sea level rose to this elevation during the Quater the area of the old lagoon is bordered by colluvial nary, especially the Holocene. foothill deposits especially in the east. But this The coastline of the Beşik plain extends NW-SE material does not reach the centre of the lagoonal and about 2 km inland, narrowing to a triangular area because there is no stream to carry it. shape (Pi. 5). No river traverses the Beşik plain. Therefore, in spite of its small area, the old Only an old cana) on the threshold in the east is lagoon has not completely infilled. The colluvial noticeable (Fig. 3). The cana) was dug so water foothill deposits are advancing slowly over the from the Pınarbaşı karstic springs in the south of lagoon. Extending the agricultural areas inward is the Karamenderes plain would flow directly to the also partly related to this geomorphic process. sea (Fig. 2). The ruin of an old water-mill at the Lagoonal sediments found by drilling through the mouth of the canal opening to the Beşik plain colluvial foothill deposits show that the lagoon is known as " Hanım Değirmeni" or "Hamam covered a larger area in earlier times. Değirmeni" in old maps. The cana) turns south The coastal part of Beşik plain is a strip of Iand and reaches the sea in the southern part of the about 500 m wide. it is separated into two sections plain. However, it is currently dry and infilled in by a longitudinal, 100-150 m wide, lagoonal most places. channel which is only active in the winter (Pi. 5). Beşik plain is bordered by plateau slopes, 40-60 This channel accommodates sea water during m high, in the north and south (Pi. 5, Korfmann storms. The area covered by water depends on 1986). Neogene bedrock interbedded with more wind direction. The bottom of the channel is only resistant limestone and marl layers and less resist about 30-40 cm above mean summer sea level. ant mudstone layers form low step features along Sediments in the channel are finer than outside it these slopes. A smooth belt of foothills occurs and sand cover does not exist. The surface is damp between the plain and the slopes. This very flat even during the dry summer season and partly feature is wider in the east. it formed along the covered by halomorphic small plants. foot of the Iow plateau slopes by deposition of The main coastal flats of the Beşik plain extending sediments from the mudstone layers ofthe plateau. on both sides of the lagoonal channel are about it can be differentiated from the deposits of the 60-80 cm above mean sea level. The steps along plain by its reddish-brown colour. the channel edges are low but clear. The surface There are two main geomorphic features on the covered by eolian sand and dust coming mostly plain. üne is the inner or old lagoonal part, the during dry summer periods with the dominant other is the outer or coastal part. A very low and northerly winds. However, there is no dune relief flat old coastal barrier occurs between them, about on this surface except one small dune ridge along 500 m inland from the present coastline (Pl. 5). the northern part of the coast. Drill cores on both The old lagoon in the east comer of the Beşik plain sides of the channel showed a sandy-dusty eolian has silted in and is only semi-active today. The bot section from the top down to the present sea level. tom of the lagoon (about 50-80 cm above sea This layer covers homogenous shallow marine level) may be covered by water in the rainy seasons sandy foreshore sediments. The upper eolian sec especially during severe storms. However, this tion is well indurated especially toward the sur condition does not persist because a small outlet face. it is evident that the sandy material consists HOLOCENE GEOMORPHIC EVOLUTION OF THE BEŞiK PLAIN 87 of coastal sand mixed with eolian dust. This Rising sea level during the Holocene first intruded material is slightly cemented by deposition from a coastal indentation forming a bay in the location capillary ground water. The reason for the lack of of the present Beşik plain. Then a barrier formed dune relief is the hard surface of this eolianite (in the rniddle of the present plain) separating a formation. lagoon from the sea. The alluvial plain developed The dominant northerly winds blow stronger in from this framework. it has been possible to some natural troughs. These winds blow the understand and date the important events in coastal sands from the beaches along the foot of the geomorphological evolution of this small cliffs in the north through the low gap between embayment. Beşik-Yas s ıtepe and the main plateau ridge and spread them along the coastal part of Beş ik plain from north to south (Figs. 2, Pi. 5). The source of these sands is the shallow marine, soft Neogene IV. Pre-Holocene geomorphology of deposits. Sandstone layers of the Neogene are the Beşik embayment reworked by waves along the straight cli ffs of Yeniköy plateau ridge and the sand accumulates There is a structural platform of Neogene bedrock in some places to form fıne beaches like the about 5-6 m below the eastern part of Beşik plain one immediately north of Beşik-Ya ss ıtepe prom (Unit number 1 in Fig. 4). The surface of this plat ontory. form was probably open to the atmosphere during Another source of the sandy-dusty cover of the the Würmian and early Holocene when sea level coastal part of Beş ik plain is fıne eolian material was Jower than at present, but it was not dissected brought by strong NE winds. The northerly winds because no major stream traversed the plain. blow stronger over the low threshold between The deepest sedimentary unit on the Neogene Karamenderes and Beşik plains picking up fıne bedrock reached by the drilling is a mottled, hard, material from the disaggregation of Neogene terrigenous mud (Unit number 2 in Fig. 4). The sediments. Strong winds coming from NE may origin of this sediment is the Neogene bedrock. bring fıne material also from the Karamenderes There are some coarse sand and gravels which plain. Therefore, instead of coastal dunes develop belong to the conglomerate layers of the Neogene. ing from the coastline landward, a flat landscape Some pieces ofwhite marl and limestone are found has developed along the Beş ik coast. in a tan-yellowish, silty-clayey, sti cky matrix . No The profile of the Beş ik coast is very flat both sedimentary structures are evident. However, along the foreshore and inland. There is nota clear there is a ·gradual change upward to the shallow beach slope. Beach sand is homogenously fı ne. marine sediments where the colour becomes Masses of dead sea plants, especially Posidonia greyish and some Jarninations are seen in the fıner oceanica, occur along the beach. sediments. This marine Jevel is about 5-6 m below An old coastal barrier divided the old inner lagoon present Jagoonal surface of the plain in the east and and the coastal part of the Beş ik plain (Pi. 5). it is graduall y rises toward north, east and south. It about 500 m inland from the present coastline. The descends toward west or SW to the open sea. barrier is not very clear as a relief feature. it is Core drilling showed that a greenish-dark grey, about 2 m above sea Ievel and very flat. Although generally clayey-silty, partly homogenous, hard the Iagoonal edge is more obvious because the mud unit overlies the mottled base unit in the Iagoon is occasionally covered by water, the eastern Beşik plain, especially in the small exten boundary of the barrier along the coastal side is sion of the Iagoonal plain near Hanımdeğirmeni obscured by eolian cover. However, the barrier (Unit number 3 in Fig. 4). Some cross-bedded can be recognized easily in the field because it is sandy sections with many thin shells occur in this covered by oak trees. On the lagoonal and coastal unit. Dr. G. Falkner determined that the most of flats only xeromorphic and halomorphic small them are Corbula gibba, Ostrea edulis and annual plants can be seen. The oak trees are on the Cerastoderma glaucum. The high population of decline, but they stili exist in small groups Corbula gibba indicates somewhat extreme condi- especially north of the barrier. 88 İLHAN KAYAN tions in a quiet, brackish to salty water, with low cross-bedded or inter-bedded sections containing oxygen. abundant shells. Light grey or greenish-grey finer The top surface of this unit is about 1 m below sediments generally show laminations. This means present sea level. It is covered by a thin sand layer that the inner part of the Beşik embayment was with abundant shells overlaid by a lagoonal mud. separated from the sea by a coarse sandy coastal This sequence implies that the lower hard mud shoal (bar). From the time the sea reached the edge (Unit number 3 in Fig. 4) alsa may be a part of of the platform the inner part has been a quiet Holocene lagoonal section. However, the shells lagoon. were C 14 dated to 24.000 years before present The oldest Holocene sedimentary unit was en ( uncalibrated HD 11899- 11471). The date must countered in the middle of the present Jagoonal flat be older than 24.000 years because sea level was (Drill hole number 54 in Fig. 3). This is a black, much lower at that time. This mud must be a very sticky-hard, silty-clayey mud on a mottled lagoonal sediment from a previous high sea stand, base (H 1 a in Fig. 4). Fine shells are abundant and such as Riss-Würm or mid-Würm. Shells of the a rich plant cover was likely at the time of forma overlying sandy layer are dated at 5. 800 years tion. A C 14 date ona sample from this mud at - B. P. (HD 11898- 11422) and some oxidation 4 m (below present sea level) gave an age of 8.000 (weathering) traces can be seen between these two years B. P. (without calibration HD 11904- units. 11915). Therefore, it may be supposed that when rising sea level reached to the Beşik embayment (to the platform about 5-6 m below the present sea V. Holocene geomorphic evolution level), this area was covered by terrigenous of the Beşik embayment sediments. The flat area then became a swamp with thick plant cover, while coarser sediments were Configuration of the pre-Holocene subsurface being deposited in the outer and deeper part. The sediments and their morphology imply that rising occurrence of homogenous fine sediments with sea level during the Holocene climbed two slopes thin-walled shells implies that sea level rise stop in Beşik embayment (Fig. 4). üne of them is the ped or slowed temporarily at that time. Shell outer slope ofthe Neogene platform from open sea from a sandy layer a little higher in the same drill toward the present line of old coastal barrier in the hole (about -3 m) gave a 6.700 years B. P. date rniddle of the plain. The other one is the inner edge (calibrated HD 11903-11496). The whole profile of the platform which is covered by pre-Holocene is sandy in the west indicating that a shallow (Riss-Würm or mid-Würm) lagoonal mud. Be ınarine bar started to form in about the same loca tween them, a small flat surface of the platform tion as the barrier in the middle of the present occurred as a different environment for shallow Beşik plain, separating an ancestral lagoon in the marine sedimentation. east. Drill core evidence shows that the outer slope is The C 14 date of 5.800 B.P. mentioned above covered by coarse coastal or shallow marine indicates rising sea level during the Holocene sediments, such as coarse sand and gravel contain reached its highest position about 6.000 years ago ing abundant large shells, mostly ostrea and car (almost the present sea level) and extended to the dium. This material occupies only the bottom east of Hanımdeğ irmeni at that time. However, 2-3 m. Then a generally fine, sandy shallow this easternmost coast was not an open sea coast, marine sedimentary unit occurs up to the present but lagoonal. sea level. Along the old barrier (the edge of the Drill cores from the old coastal barrier in the Neogene platform), coarse sediments are thicker. middle of the present Beşik plain showed that there They occur to about 1- 2 m below the present sur are at least two different sections in it. A grey, face. This is very close to the present sea level. wide and thick section forms the lower barrier. There are completely different sediments in the This consists of a very coarse sand and gravel inner part of the plain. Here finer sediments occur, deposit without sedimentary structures. Shells, mostly silt and clay with some coarse sandy, mostly ostrea and cardium, are abundant. In addi- HOLOCENE GEOMORPHIC EVOLUTION OF THE BEŞIK PLAIN 89 tion plant remains are found in the coarse sedi sent position about 2.000 years ago, with the ments. This implies an environment similar to the coastline close to the old barrier. This means that present coast where shallow marine sandy sea level started to rise again about 3.500-3.000 fo reshore plants, such as Posidonia oceanica, years ago and reached approximately its present accumulate along the beach and become covered position 2.000 years ago (Figs. 4 and 5). by sand. In the lower old barrier one of the plant samples taken from about - 3 m gave a date of VI. Paleogeographical reconstruc 5 .200 years B. P., indicating that the barrier had formed by that time. tions and changing environment of In the vertical profile of the barrier a clear color ancient man change occurs at - 2 m (Fig. 4). The upper section is yellowish-tan, while the lower section is grey. The earliest known occupation site is Beşik Both sediments are coarse sand and gravel with Sivritepe in the north of the plain (Pi. 5 and 6). it abundant (eroded) shell material. The abrupt is dated to the end of the 5th millennium B. C. as change in color indicates a subaerial barrier forma is the Kumtepe 1 A peri od (Korfmann 1985, 1986a, tion separating the lagoon in the east from the sea. 1986b and 1989). Be şik-Yass ıt epe was occupied This new barrier had two coastlines undergoing 5 .000 years ago (Korfmann 1985, 1986a, 1986b different processes. The inner, lagoonal, coast was and 1989). This period (between 6.000-5.000 quiet and fıne sediments were accumulating. Plant years ago) coincides with the t ime of first remains from about - 1 m were dated at 3.500 high sea level, as high as today. However, the years B. P. (HD 11902- 11902). Along this coastline was in a different place because sea lagoonal coast some potsherds were found in drill level had reached its maximum extension inland at cores on a fine sandy or muddy beach. in contrast, that time. The lagoon, separated from the sea by the outer, seaside, coast of the barrier was under a shoal, must have been widest in this period. Piles severe wave attack. Along this coastline earlier of cardium and ostrea shells sometimes are fo und sediments of the barrier were being reworked, in or near the ancient occupation sites. The early reducing and rounding the shell fragments. A date inhabitants consumed these abundant mussels from eroded shell fragments was 6.000 years B. P. which lived in the brackish-salty water of the old (HD 11960-11497). This shows clearly that the lagoons or estuaries (Korfmann 1986b). The material has been reworked. lagoon may also have been used as a naturally Drill core evidence, especially the change of the sheltered harbour for small ships. barrier from subaquatic to subaerial indicates a Settlements were on the higher plateau ridges small lowering of sea level, about -2 m. With the rather than along the coast of the Beş ik bay. This lowering of sea level the old barrier became wider may have been to take advantage of proximity to and higher. The period of this formation is prob Kumtepe and Troia, to ha ve a view of the entrance ably from 5.000 years B. P. to 3.500- 3.000 B. P. to the Çanakkale strait, and to be closer to fresh There is a clear concordance between this result water springs. There are several springs in the and evidence from other Aegean coasts, especially south but the northern edge was preferred fo r westem Anatolia (KeUetat 1975 and Kayan 1988). occupation. Wind direction may have been another The coastal plain to the west of the barrier is factor in the choice. Mosquitoes would be re covered by eolian material. Ali of the gouge auger moved by the north wind and the northern area data showed that the base of this cover is almost would be clear of flies. at present sea level (Figs. 4, Pl. 5). Sandy The third and second millennia B. C. are the period foreshore deposits with plant material lie below ofa small lowering of sea level . At the end of this this level. Some sea-grasses, such as Posidonia period, about in the middle of the second millen oceanica, can stili be recognized. A sample taken nium B. C., sea level was down about -2 m from about - 80 cm (drill hole number 61) gave a (Fig. 5). This led to the lagoonal area being date of 2.000 years B. P. (HD 11 906-11916) reduced and fılled by coll uvial sediments more indicating that sea !eve! was very close to its pre- quickly than before. By the end of the second 90 iLHAN KAYAN ...c 1 1 -... -~ E ::.::- t.ı o w · -UlW V> uıa.. "' ..... o::: a.. ~ > 1 ~"' w~ W<{W "' QI QI ı- CD > t- > u c ı: :ı:: -1 .... E "1:1 0::: ... c ~ :;:~ Dep th > QI -' ·- o. > ~ ... - - De pth uı QI . t.ı 1 ..... c !!' =. .."' o ~ m <{ <{ <( <{ ...... m -~ E QI z .c z .oz ti) :::J o o o o o Eo t.ı O '" O o::: o::: .... o - .... - .... _ w ::.:: o::: o::: 1- 2 m ~ 1- 1- 1- 1- • :ı::=~ ~ Ul ::: 2 NE OL I T H IC BRONZE A G E 7 6 5 4 3 2 o s.~ -1 ı. "•ı ~(/,,. ,,. -2 -3 -3 ? T 1 M E (TH OUSAND YEARS BEFORE PRESENT) Fig. 5 Sea level changes on the Beş ik coast during the !ast 6000 years. millennium the lagoon was smaller and the coastal have protected the Beşik embayment from strong barrier wider (Pl. 8). Some potsherds were found northerly winds (Pi. 8). along the Jagoonal coast of the barrier. They showed no evidence of transportation or erosion by waves. They appeared to be in situ. in the opinion VII. Conclusions of Korfmann and his colleagues th~ potsherds may belong to the end of the second millennium B. C. ln spite of its small area on a cliff coast, Beşik The "Trojan War" and its environment have long embayment has had a very slow and quiet geomor been topics for discussion. it has been suggested phic development during the Holocene. Therefore, that, if such a war took place, the Achaean camp it has been possible to understand ali the geomor may have been at the Beşik embayment instead of phic events and paleogeographical changes in this the embayment at the mouth of Karamenderes period related to human occupation. During the river (Korfmann 1986 and 1986a). During the time earliest known occupation of the area, about 6.000 of Trojan War, about l .200 B. C., sea Jevel was years ago, sea Ievel had reached its present level about 2 m below its current level (Fig. 5). The and extended inland into the embayment. People Beşik lagoon was reduced in size and the barrier settled in the north, along the top of a coastal widened (Pi. 8). It is difficult to believe that ships promontory, the Beşik-Sivritepe - Beşik-Yassı passed through a widened barrier to the lagoon. tepe ridge. However, one can imagine that small ships may There is no evidence that sea Jevel rose higher than have been dragged easily onto the flat sandy beach present in this area during the Holocene. Sedi (personal communication by Kraft). The coastline mentological investigations show that sea level was about 400 m farther inland at that time, and the descended about 2 m from 5.000 to 3.500 years Beşik-Sivritepe - Beşik-Yassıtepe ridge might before present (Fig. 5). This had an important HOLOCENE GEOMORPHIC EVOLUTlON OF THE BE Ş iK PLAIN 91 geomorphic effect on coastal barrier formation in vestigation with laboratory facilities to examine the old Beşik bay and a Jagoon was separated from systematically the paleontological and sedi the sea. Thus, two different environments were mentological characteristics of the different available for the people who lived in this area: a sedirnentary environments. lagoon on the inner side and a shallow marine environment along the outer coast of the barrier. Coastal processes, especially shoal-bar-barrier VIII. Acknowledgements formation and beach accretion, have been domi nant in the formation of the present Beş ik plain. First ofall , 1 would like to express my gratefulness Regardless of Troian War implications, it is ob to Prof. Dr. M. Korfmann. This study has been vious that the Beş ik bay could have been used as possible thanks to him. He encouraged me to work a harbour. Therefore, Holocene paleogeographical on this subject, kindly invited to join his team and changes on the Karamenderes plain, especially supported my studies in many ways since 1983. coastline positions related to the archaeological Prof. Dr. O. Erol, my former professor, helped periods, must be studied in detail. The results of over the years in developing my background. We the study of the Beşik area, especially the sea level started this study together and he left me his rights changes, will be very useful for the new study at to the investigation. 1 anı deeply indebted fo r his the Karamenderes plain. The geomorphic evolu help and stimulating discussions and suggestions tion is much more complicated in the Karamen on this study. Prof. Dr. J. C. Kraft, also my former deres area because of the extensive alluvial deposi professor, helped me to begin the study of the tion. Instead of barrier system and beach accre paleogeography of the Troia area. 1 anı grateful to tion of the Beşik coast, delta progradation and him for productive discussions, helpful advice and flood plain development are dominant in the suggestions. 1 thank Dr. Kromer (Institut für Karamenderes plain. Small sea !eve! fluctuations Umweltphysik der Universitat Heidelberg) for after sea !eve! reached to the present position about radiocarbon dating and Dr. Falkner for his study 6.000 years ago will not have affected the con on some fossil molluscs taken from pre-Holocene tinuous delta progradation and the receding lagoonal sediments. 1 anı grateful also to Prof. Dr. coastline. H. P. Uerpmann and Prof. Dr. C. Hannss for their A new paleogeographic research project has begun helpful discussions and suggestions on evaluation on the Karamenderes-Dümrek plains, parallel to of the radiocarbon dates of sedimentary environ the new archaeological studies. Thirty-eight drill ments, particularly on the sea level positions of cores were taken in 1988 and 1989 using the pre-Holöcene lagoonal sedirnents. Also 1 thank my "Archaeomog" to penetrate to 21 meters. In this workers (especially Ali Güler from Yeniköy) for area this depth is not enough to reach the base of their effort to obtain more information under dif Holocene sediments in the main body of the plain. ficult working conditions. However, it is enough to provide information This paper was edited by Prof. Dr. G. Rapp Jr. 1 about the sediments deposited in the last 6.000 thank him for his great effort. Prof. Dr. M. Korf years. In many places drill holes encountered mann read the final text and made some corrections Jayers which included human artifacts such as pot concerning the archaeological aspect. For ali of his sherds, stones, charcoal and shells (as food re helps 1 anı greatly indebted. mains). Correlation of archaeological data with evidence of the changing environment may give us a complete cultural-natural history of the evolution of this area. BIB LIOG RAPHY Our drill core studies will continue through the alluvial plain in the environs of Troia to determine BİLGİ N, TURGUT. 1969. Biga Yarımadası Güneyba tı coastline positions and general paleogeography Kısmınınleomorfolojisi. İstanbul Üniversitesi Coğ rafya during human occupation. Prof. Dr. J. C. Kraft Enstitüsü Yayın No. 1433. 274 pp. İstanbul. and Prof. Dr. G. Rapp Jr. have joined this in- DARKOT, BESİM. 1938. Boğazların menşei , in: Coğrafi 92 İLH AN KAYAN Araşurma lar 1: 1- 14 . İstanbul Üniversitesi Coğ rafy a Held at Bryn Mawr College, October 1984. Ed. M. J. Enstitüsü Yayın No. 4. İs tanbul. Mell ink, 17-28. New York. DARKOT, B ESİM. 1938a. Ege haliçlerinin me n şe ve KoRFMA NN, MANFRED. 1986b. Beşik-Tepe. Vorbericht tekamülü, in: Coğrafi Araşurmalar 1: 29- 52. İs tanbul über die Ergebnisse der Grabungen von 1984. Grabun Üniversitesi Coğrafya Enstitüsü Yay ın No. 4. İstanbul. gen anı Beşi k-Yass ı tepe , Beşik-Sivritepe und Beş ik E Rİ NÇ , SIRRI. 1955. Gediz ve Küçük Menderes Graberfeld, Archöologischer Anzeiger: 303-63. d eltalarının morfolojisi, in: Dokuzuncu Coğrafya Beri in. Meslek Haftası, Tebliğler ve Konferanslar, 33- 66. KORFMANN, MANFRED. 1989. B eşi k-Tepe . Vorbericht Türk Coğ rafya Kurumu Y ayın No. 2. İ stanbul. über die Ergebnisse der Arbe iten von 1987 und 1988. EROL, Ocuz. 1969. Çanakkale Boğaz ı çevresinin Auswertungsarbeiten Beş ik-S i vritepe, Beş ik-Yass ıtepe , jeomorfolojisi hakk ında ön not (A preliminary report B eş i k-Grabe rfeld , Grabungen anı Beş ik-Sivritepe, Ar on the geomorphology of the Çanakkale area - The chtiologischer Anzeiger: 473-81. Berlin. Dardanelles, Turkey). Ankara Üniversitesi Coğrafya KRAFT, JOHN C ., İLHA N KAYA N and Ocuz EROL. Araştırmaları Dergisi 2. Ankara. 1980. Geomorphic reconstructions in the environs of EROL, Ocuz. 1972. Truva çevresinin foto-jeomorfo lojik ancient Troy, Science 209: 776-82. Washington. h aritas ı , Jeomorfoloji Dergisi 4. Ankara. 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Kazı Sonuçları Toplantı s ı, 229-38. Ankara. ment of Geology. Newark. KORFMANN, M ANFRED. 1986. Troy: Topography and avigation, in : Troy and the Trojan Wa r. A Symposium Held at Bryn Mawr College, October 1984. Ed. M. J. Prof Dr. İlhan Kayan Mellink, 1-16. New York. Ege Üniversitesi KoRFMANN , MANFRED. l986a. Beş i k-Tepe: New Edebiyat Fakültesi Evidence for the Period ofthe Trojan Sixth and Seventh Coğrafya Bölümü Settlements, in: Troy and the Trojan War. A Symposium TR-35100 Bornova/İzmir TAF EL 5 PRESENT I I I I I / I I ,,,..,I \ ,,,,.,. / ,'' / / 6 \ / \ I I / / -""I ~ 4'.-' ( ~ / {!zL O Mil\ / \ \ ) \ ) _,,/'' 6 ) /// "" ( 4 ~ \ I 1 6 10\ ·--- o__ c:::_c::=: .... 500 m LOW PLATEAU SLOPES ON THE NEOGENE BEDROCK (MAINLY SANDY - LIMY SEDI M ENT S) ----+ STEEPER. GE NTLER GEN TLE SLOPE - FOOT ON COLLUYIAL DEPOSIT 40 LAGOON LOW COASTAL L A ND F ORM S 30 SC ARPS AND CL I FFS - - - -" SMALL STREAMS, 20 ELE VA T ION S (m) 1.0 Gcornorphological rnap of the Beş i k plain. TAFEL 6 6000 B.P. SEA LEVEL : 0 m . . . . 8 E $ K 8 AY o SOOm ı==:J LOW PLATEAU SLOPES ON THE NEOGENE BEOROCK (MAINLY SANDY-LIMY SEDIMENTS) ~ STEEPER, ___.. GENTLER D GENTLE SLOPE-FOOT ON COLLUVIAL DEPOSIT c:::J SHOAL ..ılı. COASTAL SWAMP :rn:m: SCARPS AND CLIFFS OC OLO CLI FF Palaeogeographic reconstruction of the Beş ik plain about 6000 years ago when sea level was almost the same as present. TAFEL 7 5000 B.P. SEA LEVEL: 0 m I I I o 500 m LOW PLATEAU SLOPES ON THE NEOGENE BEDROCK (MAINLY SANDY- LIMY SE DIMENTS ) - STEE PER, ----'- GENTLER GENTLE SLOPE-FOOT ON CO LLU VIAL DEPOSIT C:::J LAGOON LJ COASTAL BARRIER - BEACH .1lı.. COASTAL SWAMP rn:m: SCARP S AND CLI F FS OC OLD CLIFF ---~" SMALL STREAMS Palaeogeographic reconstruction of the Beş ik plain about 5000 years ago when sea level was almost the same as present. TAFEL 8 3500 - 3000 B.P. SE A LEVEL : -2 m I I ,I I ... ___ _ o / / LOW P L ATEAU SLOPES ON T HE NEOGENE B EDROCK / (MAINLY SANDY- LIMY SEDI MENTS) --+ STE EPER, GENTL ER GENTLE SLOP E - F OOT ------:::-/\ ON CO LLUVI AL DE POSIT C:=J LAGOON <_\~ c=J COASTAL BA RR I E R ' ' ..ili. COASTAL SWAMP 1 SCAR P S AND CL IFFS '\1 "' mrm 1' oc OL D CLI FF 1 ' CE OLD CEMETE RY F OU ND iN 198 4 S L SEA L E VEL Palaeogeographic reconstruction of ehe Beş i k plain about 3500-3000 years ago whe n sea level was about 2 rn lower than the prcsent. Coastl ine 2000 years B. P. is included when sea level was about -0.5 rn lower than thc present.