A Miocene Palaeovalley Network in the Western Taurus (Turkey)

Home , Alanya, Aras (river), Manavgat, Manavgat River

OLIVIER MONOD1, CATHERINE KUZUCUO⁄LU2 & ARAL ‹. OKAY3

1 ISTO, UMR 6113, Université d’Orléans, 45067–Orléans, France (E-mail: [email protected]) 2 Laboratoire de Géographie Physique, UMR 8591, 1 pl A. Briand, 92195–Meudon, France 3 ‹stanbul Technical University, Eurasian Institute of Earth Sciences, Ayaza¤a, TR–80626 ‹stanbul, Turkey

Abstract: Lower Miocene conglomerates in the Köprü and Manavgat basins contain pebbles that can be confidently traced back to their source areas, owing to their distinctive lithologies. Among others, are the green Hu¤lu volcanics (Late Trias), known only in allochthonous units from the Beyﬂehir region, or the Alanya blueschists, restricted to the Sugözü unit in the Alanya Massif. The problem is to find out how this detrital material could have travelled about eighty kilometres through the Taurus calcareous units during the Miocene. Fortunately, the present drainage system is not yet fully reorganised in the Taurus, and large areas of the chain still retain fossil morphologies. These may be seen in the upper karstic areas of the chain, where a large part of a high surface (1500–2200 m) is preserved. On this surface several dry valleys, some of them 400 m deep, with meanders and tributaries, have been recognised. They are disconnected from the present drainage, and represent fragments of a former network directed NE–SW, at right angles to the structures of the Taurus chain. The age of this network may be attributed indirectly to the Early Miocene. On the other hand, the presence of blueschist fragments in conglomerates of the Aksu Basin cannot be explained through a NE–SW-directed drainage system, and implies instead that the Alanya Massif extends to the west below the Miocene cover of the Antalya Gulf. Later, Late Miocene faulting fragmented the high surface and disrupted the drainage system. Uplift of the Taurus chain followed in the Pliocene and Quaternary, and is responsible for the extensive karstic circulation seen today, which left aside remnants of the ancient morphology of the chain.

Key Words: fluviatile network, tracer pebbles, Miocene morphology, karst, Taurus, Turkey

Bat› Toroslar'da Miosen Yaﬂta Bir Akaçlama Sistemi

Özet: Köprü ve Manavgat havzalar›nda bulunan Alt Miyosen konglomeralar›n›n kaynak alan›n›n saptanmas›, çak›llar›n karakteristik litolojik özellikleri nedeni ile kolayd›r. Örne¤in, baz› çak›llar sadece Beyflehir bölgesindeki allokton birimlerden bilinen, Erken Triyas yaflta yeflil Hu¤lu volkanitlerinden, veya Alanya Masifi'nin Sugözü Nap›'nda tan›mlanan maviflistlerden oluflmufltur. Bu klastik malzemenin Miyosen'de Toroslar›n karbonat birimleri üzerinden akarsular ile nas›l 80 km tafl›nd›¤› önemli bir sorundur. Bu konuya ›fl›k tutabilecek bir gözlem, Toroslarda günümüz akaçlama sisteminin tam geliflmedi¤i ve genifl alanlarda akaçlaman›n fosil özellikler tafl›d›¤›d›r. Fosil akaçlama bilhassa Toroslar›n yüksek k›s›mlar›nda (1500–2200 m) korunmufltur. Bu yüzeylerde, yer yer derinlikleri 400 metreye ulaflan, yan kollar› bulunan menderesli kuru vadiler yer al›r. Bu eski vadiler modern akaçlama sisteminden izole olmufl, Toros da¤ silsilesi yönüne dik, KD–GB gidiflli eski bir akaçlama sisteminin art›klar›n› oluflturur. Dolayl› veriler eski akaçlama sisteminin yafl›n›n Erken Miyosen oldu¤unu gösterir. Köprü ve Manavgat havzalar›ndan farkl› olarak Aksu Havzas› konglomeralar›ndaki maviflist çak›llar›n› KD–GB gidiflli bir akaçlama sistemi ile aç›klamak mümkün de¤ildir. Aksu Havzas›ndaki maviflist çak›llar›n›n varl›¤›, Alanya Masifi'nin Antalya Körfezi Miyosen örtüsünün alt›ndan bat›ya do¤ru uzand›¤›na iflaret eder. Geç Miyosen'deki faylanma ile yüksek düzlükler parçalanm›fl, ve KD–GB gidiflli akaçlama sistemi bozulmufltur. Toros da¤ silsilesinin Pliyosen ve Kuvaterner'de tekrar yükselmesi sonucunda bugünkü kapsaml› karstik akaçlanma geliflmeye bafllam›fl, ve eski akaçlama sistemi ancak izole olarak baz› yüksek bölgelerde korunmufltur.

Anahtar Sözcükler: akaçlama sistemi, k›lavuz çak›llar, Miyosen morfolojisi, karst, Toroslar, Türkiye

1 MIOCENE PALAEOVALLEY NETWORK, WESTERN TAURUS

Introduction from three major fluviatile basins (Köprüçay River, In southern Turkey, Miocene deposits generally Manavgat River and Alaraçay River), whereas to the unconformably overlie pre-existing structures of Late north – the other base level – at about 1000 m altitude, Cretaceous to Late Eocene age (Blumenthal 1951; Gutnic corresponds to an endoreic depression in central Anatolia, et al. 1979; Koçyi¤it et al. 2000; fienel 2002). Within the where the Beyflehir and Su¤la lakes are situated. In western Taurus range, this disposition implies that a addition to these catchment areas, the drainage of a large period of exhumation and erosion occurred before the surface of the Taurus chain (HS in Figure 2) is not yet Miocene marine transgression, as shown by polymict connected to any organised surficial system. Due to this conglomerates which are usually present at the base of disposition, this high, isolated area is itself subdivided into the Miocene basins (Blumenthal 1951; Monod 1977, a number of closed depressions, and includes the two 1979). These conglomerates are irregularly distributed largest poljes (Kembos Ova and Eynif Ova, cf. Louis from Adana to Antalya and reflect a rugged topography 1956) of the chain. The high surface is almost entirely (Akay et al. 1985; Flecker et al. 1995; Ocako¤lu 2002). comprised of Mesozoic carbonates (Jurassic–Cretaceous) Clast composition suggests that the pebbles were and exhibits an intense karstic morphology. Surprisingly, generally derived from the surrounding mountains, although no organised drainage exists in this part of the typically made up of Mesozoic carbonates, or from Taurus, many large, dry valleys are present on the high overlying nappes, which often include ophiolitic rocks. In surface (Figure 3). As shown below, we suggest that most cases, however, the exact origin of the Miocene these fossil valleys are remnants of a former fluviatile pebbles cannot be assigned more precisely, owing to the network situated upon a Miocene erosion surface. ubiquity of neritic carbonates and the widespread distribution of ophiolitic units in the Taurus range. Only a The High Palaeosurface few particular lithologies can be recognised unambiguously among the pebbles, and these crop out in The general topography of the high surface (HS) of the such restricted areas of the western Taurus that it is Taurus, at present between 1500 m and 2000 m altitude, is rather smooth, albeit intensively karstic (cf. possible to identify their origin with a good precision. Nazik 1992; Ekmekçi 2003), but is not a structural Among them, the Precambrian diabases of Bozburun surface, as shown by the various underlying carbonate Da¤, red Carboniferous sandstones of Dipoyraz Da¤, formations ranging in age from Late Trias to Late metamorphic limestones and blueschists of the Alanya Cretaceous. Limiting the high surface, very steep slopes Massif and the green Hu¤lu volcanics (Trias) are excellent generally result from regressive and differential erosion source indicators (Figure 1). The problem is to find out or younger faulting (Figure 3). To the south, the Karpuz how these materials travelled across the Taurus chain River, the Alara River and the Manavgat River have early in the Miocene. The aim of this paper is to point out carved extremely steep gorges (over 1000 m deep) ancient morphological features still preserved in the through Mesozoic carbonates, demonstrating the young western Taurus and, with the help of these markers, to uplift of the Taurus chain. The Manavgat River, in reconstruct and date the river network which brought particular, flows down through three deep gorges, and detrital material from the Miocene catchment areas down near Üzümdere village a sharp bend at a right angle to the to the Antalya Basin. NW probably reflects a former capture (Figure 2). To the northeast, the high karstic surface is limited by high Evidence for Fossil Morphological Features calcareous cliffs above Seydiflehir (Figure 3), which Preserved in the High Western Taurus probably reflect an important fault line, as suggested by Birot & Dresch (1956). Last but not least, Miocene to The Present Drainage System Recent normal faulting has uplifted or lowered parts of Superficial drainage in the western Taurus exhibits many the Taurus chain and has thus fragmented this surface, irregularities, showing that its evolution is far from which rises to 2250 m in Burmahan Da¤, but disappears complete. A simplified topographical sketch (Figure 2) at 1100 m under Pliocene sediments along Beyflehir Lake. shows five major drainage basins, with two different base Thus, owing to the importance of Pliocene–Quaternary levels: to the south, the Mediterranean receives water erosion and tectonics (cf. Koçyigit & Özacar 2003) only

2 O. MONOD ET AL.

31° 00' 30° 30' 31° 30' Ýstanbul

Anamas Dað TurkeAnkaray Beyþehir ISPARTA Lake BD Western v v Taurus Beyþehir Lycian Eastern v Taurus Taurus Central AN Taurus LN Dipoyraz AN Dað 0 km 200 BHN AA Bozburun T. v BD AKSU THRUST a Kasýmlar AKSU BASIN 37° 30' HUÐLU 37° 30' UNIT Seydiþehir Sarýalan o v

Suðla

Lake

KÖPRÜÇ KÖPRÜÇ KÖPRÜÇ AN AA

BD AN

AY AYBAS AYBAS BHN Section +

(Figure 13) + BASIN BHN

IN IN Ýbradi Yarpuz * KIRKKAVAK FAULT HUÐLU ? Eynifova PEBBLES P PATHWAYS 37° 00' P Akseki 37° 00' ? AA * Sevinç Serik AN MANAVGAT BASIN ANTALYA Kepez t AN I M a PO ?! SS AN IB Manavgat ALANYA LE MASSIF Mediterranean Sea PA ?! TH SG WAY ! 025 50 km 32° 00'

Huðlu volcanics Alanya Massif (Trias) metamorphics Huðlu pebbles pathways other detritus pathways SG: Sugözü unit v v ophiolitic rocks Huðlu pebbles Alanya metamorphic pebbles v v SG with blueschists probable extent of + blueschist pebbles Precambrian pebbles Precambrian the Alanya Massif, Aksu thrust Kýrkkavak other Pre-Miocene diabases * and two isolated inliers (Late Miocene) fault faults thrusts

Karpuzçay turbidites Lycian Nappes a Recent Oymapýnar limestone LN (Serravallian-Tortonian) (Burdigalian-Langhian) (Middle Miocene) travertine Köprüçay Formation Tepekli conglomerate Beyþehir-Hadim t BHN (Langhian-Serravallian) (Burdigalian) Nappes (M. Eocene) Aksuçay Formation Beydað/Anamas-Akseki Antalya Nappes P Pliocene BD AN (Tortonian) AA autochthonous platform (U. Cretaceous)

Figure 1. Sketch map of the Antalya Miocene basins showing distribution of the main conglomeratic bodies, with their source rocks and locations of derived pebbles.

3 MIOCENE PALAEOVALLEY NETWORK, WESTERN TAURUS

Beyþehir Lake Dipoyraz Dað (1121) N 2998 BEYÞEHÝR

Ýncebel Pass 1713 1690 Çarsamba River Bozburun Dað 2000

2181

1982 1807 B 2304 S 2135 2354 SEYDÝÞEHÝR 2405 2585 Dökük Dað 2022 2220 Ke m 1977 bos 2056

Ov Suðla Lake

Köprü River 2300 2251 (1090) a (1230) 2288 2354

2409 2300 Burmahan HS Dað 2268 2251 Cevizli 1980 Eynif K Üzümdere 1550 2560 Ova Ýbradi 1877 HS 1984 Ponor (960) Akseki Polje 2600 1439 (1050) HS 1356 Sevinç HIGH SURFACE (no drainage system) 1012 1503 ENDOREIC BASINS:

Köprü River B Beyþehir basin M Suðla basin 1600 S

Manavgat Manavgat River MARINE DRAINAGE BASINS: K Köprü River basin

Karpuz River r e Manavgat River Mediterranean Sea A v M basin drainage Alara Ri A Karpuzçay and divide 0 km 20 Alara River basins

Figure 2. Map of the catchment areas in the western Taurus; the white area (HS) in the centre has no surficial drainage towards the present rivers, but only through underground circulation in this highly karstic area. It contains remnants of a palaeosurface where most of the fossil morphological features are present.

4 O. MONOD ET AL.

31° 30' Beyþehir Beyþehir Lake (1121) a Recent deposits Section I Pliocene marls and in Figure 7 P conglomerates ? 2997 a P Tortonian deposits Dipoyraz Lower-Middle ? Ç M Miocene deposits Dað a r 2690 1690 1520 sa

0 . m 5 high surface 1219 1713 b HS . 14 a 1400 1258 R

i Ýn.V Þamlar So.V v areas eroded after ? er 1547 Miocene Ýncebel 1250 1464 Pass P ? 1490 P palaeovalleys and 1093 2273 1501 1457 possible confluences Saraycýk Y. a Yaka normal fault (Late 1350 1557 1300 Miocene or younger) 37°30' (1450) a 1701 ? 1982 and fault scarp (grey) M HUÐLU Huðlu unit outcrop Çetmi 1828 and probable extent P Sarýalan Y. P 1300 1300 ? during Miocene 1450 2304 2181 Huðlu pebbles (1450) Kelsu T. 1290 ? P present valley of HS 1500 the Manavgat River 1250 2135 2585 2354 ? 1106 Seydisehir 2405 1270 ? a 2222 D.V. 1250 D.V. 1350 Derebucak 2100 ? 2321 2022 K 1756 1650 e 1409 m 1350 b 1977

? o Suðla s 2249 ? Lake HS ? ? 2056 Kýrkkavak (1230) 2251 (1090) O 2300 1700 v 1550 a 2100 HS 2450 1650 1850 ? 1951 ? a 1750 ? 1850 S.V. 2409 M 1956 2100 2332 F 2230 1600 ? igure 1950 1950 2217 M 2354 an 5 1650 Section II 1700 1250 1750 Z.V. av 2099 ga

T in Figure 7 t Ri Cevizli 1950

L 2123 ver Burmahan 1000 HS 1400 2371 U Dað 2251 1250 2200 1700 1980 1850 a V. 1850 A H. ? V. E F 1600 580 1350 Y. y 1650 n 1050

i 1532 .

f 1210 1550

K K K 1870 P 1666 C.V 1250 Ya rpuz

2200

A A A 950 S. Eynifova Üzümdere 1350 1200 1700

1300 O 1877 V V V ? v a

1757 Ýbradi 1900

A A A 1984 960 2560

420 V.

K K

K . M ? 1250 P. .V

? 1561 2550 K K K 1527 A Ürünlü 1040 919 900 1500 HS

? 920 1502 HS 1150 R R R . 900 1047 Akseki

1439 I I I .V ? 1050 850

Ü a Section I 2535

K K

K 1261 1221 37° 00' in Figure 7 37° 00' 1668 1629 630 1356 1023 1407 2401 250 ? 1380 700 Sevinç ? 2332 1586 1700 2254 1212 1313 1567 ? 2400 1086 1587 1405 2064 Oymapýnar 750 1503 Dam Kepez 1183 1700 2427 M Ma Ri Section II ? 0510 km v n er avgat 1012 in Figure 7 ?

31° 30' 32° 00'

Figure 3. Reconstructed Early Miocene drainage network in the western Taurus. The main palaeovalleys are in blue: A.V.– Akseki Valley; D.V.– Derebucak Valley; H.V.– Hallaç Valley; In.V.– ‹ncebel Valley; P.V.– Piser Valley; S.V.– Sultançukuru Valley; So.V.– Sobova Valley; Ü.V.– Ürünlü Valley; Y.V.– Yarpuz Valley; Z.V.– Zimmet Valley. Arrows indicate the present slope. Remaining parts of the high surface HS are in yellow. Normal faults figured here are Late Miocene or younger, with fault scarps in light grey. Manavgat River gorge (purple) is younger (Plio–Quaternary).

5 MIOCENE PALAEOVALLEY NETWORK, WESTERN TAURUS

disconnected fragments of the high surface may now be connection with the main fossil valleys occurs not on the recognised (HS in Figure 3). valley floor, but always on a valley shoulder about 200 to The fragments outlined in Figure 3 were delineated 250 m higher (cf. Zimmet valley). This general on 1/25000 topographical maps, partly directly and disposition (Figures 6 & 7-Section I) implies that the partly with a digital elevation model (DEM); they are meandering river network was initially created with a defined as remnants of an upland morphology where no weak slope on the high surface, and was succeeded by significant slopes are steeper than 25°. In most cases, two or more cycles of erosion with rapid karstic these areas are sharply delimited by a conspicuous break developments following each fall of base level in the main of slope due to Quaternary regressive erosion, as in the valleys (cf. Ford & Williams 1989). Manavgat valley, or to the denudation of a former, The dry valleys are typically V-shaped with rather steeply inclined structural slope, as south of Derebucak steep flanks (from 30° to 40°) in the deepest valleys, village. In most cases, however, the break of slope indicating a very rapid rate of incision within the reflects younger faulting, as exemplified west of ‹bradi or carbonates, but a limited time for lateral erosion to south of Seydiﬂehir. Areas displaying imprecise enlarge the width of the valley floors (cf. de Broekert & boundaries when mapping the high surface are few. As a Sandiford 2005). The steeper slopes are found result of this cartography (Figure 3), the high surface preferentially to the SW (Ürünlü Valley), whereas much appears now as a disconnected puzzle of remnant smoother shapes are recorded in the NE (Sobova Valley, morphologic pieces of limited size and variable altitudes near Beyﬂehir). As a rule, the directions of the which were parts of a larger, evolved surface, including palaeovalleys trend NE–SW and the tributaries, when not not only high points but also deep valleys, as shown at right angles to the main valleys, suggest a below. southwesterly direction of flow. Although complete profiles cannot be drawn precisely, owing to their discontinuous preservation, some of the palaeovalley Streamless Hanging Valleys fragments are long enough to suggest that the original Across several remnants of the high surface, a striking slope was weak: for instance, the Hallaç Valley (8 km) feature is the presence of large, streamless valleys, which and the Piser Valley (10 km) exhibit roughly the same are well preserved in spite of the karst in the calcareous altitude at both ends. However imprecise, where several areas (cf. Nazik 1992). These valleys are conspicuous in segments can be connected to one another, a realistic the field (Figure 4) as well as on satellite pictures, and picture of a 70-km-long palaeovalley emerges (Figure 7- some are followed for a few kilometres by roads crossing Section II), with a source about 2000 m high to the NE, the Taurus range. A common characteristic of these and a base level at 750 m altitude to the SW, as valleys is their abrupt interruption at both ends, hanging demonstrated by the deltaic deposits near Kepez from one to four hundred metres above the present-day (Karab›y›ko¤lu et al. 2000). However, in most of the drainage. Another typical feature is the karstic reconstructed profiles of the palaeovalleys, such a picture morphology of the hanging valleys, which are paved with is not obtained, and the river profiles show sharp adjacent dolines and sinkholes. discontinuities, or even slope reversals, that we interpret On 1/25000 topographic maps (Figure 5), the as reflecting later tectonic events (mainly faulting) which hanging valleys can be delineated with precision. The disrupted the original profile of the valleys. main palaeovalleys may reach 1 to 1.5 km in width (Zimmet Valley), 250 to 400 m in depth (Hallaç Valley), Reconstruction of a Palaeodrainage System and 10 km in length (the longest being Piser Valley). Most are oriented NE–SW (Figure 6), and some exhibit Once recognised, the palaeovalleys appear as isolated clear meander morphologies (Hallaç Valley) with well- fragments scattered all over the high surface of the preserved meander necks. A few tributaries may be noted Taurus. In order to restore the shape of the on both sides (Figure 5), in spite of the very rough karstic palaeodrainage network, we assume that all the fossil landscape. Interestingly, the tributaries are not deeply valleys belong to a single drainage system, although this incised into the high surface (150–200 m); thus, their certainly is questionable. First, due to complete

6 O. MONOD ET AL.

Road to Beyşehir Eo

1455 Eo J-K

K Eo Cinli D. 1340 HS 1409 1250

J-K P Eo P

CİNLİ PALAEOVYALLEY

HS J 1786 K

L J-K

LLEY EOVA PALA 1250 ER L İS P J J

J BelenDağı Road to km 1 1877 Akseki 1050 0 J-K HS

Figure 4. Aerial view north of Akseki showing the high surface (HS) incised by the Cinli palaeovalley inclined southwestward, and the much deeper Piser palaeovalley. The sun is to the south. P– Permian isolated klippe from the Beyﬂehir-Hadim Nappes; Eo– Eocene limestone and flysch; J–K– Upper Jurassic to Upper Cretaceous carbonates, displaying a highly karstic morphology; J– Middle Jurassic dolomite; L– Liassic shales and sandstones. Location given in Figure 5. denudation of the slopes and, in most cases, the absence allochthonous units) which had overlain the Mesozoic of valley fill, the age of each valley cannot be directly carbonates, so that the locations of the original known. Second, the present shape of the valleys results confluences are now lost. from a succession of erosion cycles, which cannot be However, the size of the main fossil valleys suggests identified individually. Third, the relative altitude of the a much larger catchment area than the present one, and different fragments may have been changed by later therefore implies that the fossil fragments were tectonic events, as shown by slope reversals along the somehow connected to one another, forming an extensive profile of several valleys. Last but not least, drainage system throughout the Taurus chain. A tentative Plio–Quaternary erosion has removed parts of the softer sketch is presented (Figure 3), in which the nearest formations (Eocene flyschs, Palaeozoic and other connections have been drawn, based on the orientations

7 MIOCENE PALAEOVALLEY NETWORK, WESTERN TAURUS 7 7 navgat River) flows in the main roads karstic area of the Taurus

and tributaries

to Konya Konya to to Manavgat River gorges (Plio-Quaternary) Konya to A Zimmet palaeovalley Hallaç palaeovalley Cinli palaeovalley Piser palaeovalley

to Akseki Ýmrasan Pass D 1510

1250 o o Figure 4 1877 1786 Belen Dag HS : Section II (part) on Figure Section I (part) on Figure to Beyþehir

1050 Cinlidað 1409 1500 B D

- -

to Antalya Antalya Antalya to to to

C A Cevizli

" " " 0 0 0 0 0 0 ' ' ' 5 5 5 4 4 4 ° ° ° 1 1 1 3 3 3

1050 1050 Emerya 1050 streamless valleys: High Surface 1512 1512 HS 1532

1050 CÝNLÝ PALAEOVALLEY PALAEOVALLEY CÝNLÝ CÝNLÝ Sivri T. Sivri PALAEOVALLEY CÝNLÝ

PÝSER PALAEOVALLEY PALAEOVALLEY PÝSER PÝSER 1582 PALAEOVALLEY PÝSER part of sections I & II in Figure 7. Location given in Figure 3.

Çýnardibi 0 1372 .

110 1405 Akþahap T

15 Ulu A-B, C-D Üzümdere Zilan

1354

500 500

0 500

0 B

M a n a v g a t R i v e r r r e e e v v v i i i R R R t t t a a a g g g v v v a a a n n n a a a M M M

1664 HS

1200 1200

1200 420 420 420 1050 500 Akkuyu Y. Akkuyu Hörtebek T. Hörtebek 1398

Kuyucak

31°37'30" 31°37'30" 31°37'30"

3 3 3 1 1 1 ° ° ° 3 3 3 7 7 7 '3 '3 '3 0 0 0 " " "

1200 1200 r 1200 1662

o 1800 2023 1980 Saksaðan T. Saksaðan

Kýraç Daðý 1100 1832 1250

n a v g a t R i v e 1973 HALLAÇ PALAEOVALLEY PALAEOVALLEY HALLAÇ HALLAÇ a PALAEOVALLEY HALLAÇ Ýbradi 1550 M

1800 1502 Km

HS Sodu T. Sodu

1550 1550

1550 1150 1774 2000 2 Yoncalý T. T. Yoncalý 2223 2332 Masata Seyran T. Seyran

2099

1450 1450 1450 . Entrenched meanders in the Hallaç palaeovalley and a few hanging tributaries are still recognisable. The present drainage (Ma 0 2409 14 deepest gorge (dark grey) incised during the Plio–Quaternary. (HS) Detailed map of the topography of the Taurus NW of Akseki showing several hanging dry valleys (light grey) incised into a high

2165

(Equidistance: 50 m)

ZÝMMET PALAEOVALLEY PALAEOVALLEY ZÝMMET ZÝMMET C PALAEOVALLEY ZÝMMET

2217

" "

" Pýnarcýk Daðý

31°30'00 31°30'00 31°30'00

37°15'00" 37°15'00" 37°15'00"

" "

37°07'30" 37°07'30" 37°07'30" " 31°30'00 31°30'00 31°30'00 Figure 5.

8 O. MONOD ET AL. SE 1877 HS Belen Dağı PİSER palaeovalley 1786 3km HS tion given in Figure 5. ote the meandering Hallaç palaeovalley) with CİNLİ palaeovalley (420 m) Sivri Tepe 1532 Manavgat River (600) (1050) 1520 1664 Cevizli Üzümdere HS (1080) İbradi tributary HALLAÇ palaeovalley 1956 6km 1980 (1150) Masata 8km tributary HS ZİMMET 2099 palaeovalley : high surface tributaries, and the much deeper gorge (at Üzümdere) through which the Manavgat River is now flowing. Sun is to the west. Loca Digital Elevation Model (DEM) picture of the Taurus seen from the south, showing the hanging position of several dry valleys (n tributary HS HS 2409 NW Figure 6.

9 MIOCENE PALAEOVALLEY NETWORK, WESTERN TAURUS 500 3000 3000 2500 2000 0 1000 1500 500 2000 2500 0 1500 1000 S NE ivers (in AKSEKÝ 10 km PALAEOVALLEY D 1877 m Belen D. High Surface conglomerates at the base lometres of its course, but lower than the fossil valley, ) and Alanya Massif (AM). In ines indicate where the softer the where indicate ines

PÝSER YARPUZ CÝNLÝ PALAEOVALLEY

follows the course of the palaeoriver

PALAEOVALLEY C PALAEOVALLEY YARPUZ MANAGAT Section II High Surface A PALAEOVALLEY tributary HALLAÇ PALAEOVALLEY

in Figure 5). Geological structures are not detailed within the Mezosoic PÝSER High Surface 2023 m Saksaðan T. Saksaðan

A-B C-D, PALAEOVALLEY ZÝMMET 2332 m

Manavgat River Seyran T. Seyran PALAEOVALLEY B C High Surface 2450 m Manasýr T. Manasýr PALAEOVALLEY SULTAN ÇUKURU SULTAN tributary Manavgat River ÜRÜNLÜ High Surface Kembos Ova polje (1230) PALAEOVALLEY extends N–S from Beyﬂehir Lake to Akseki and shows the incisions of the main palaeovalleys (in blue) and those of the present r DEREBUCAK PALAEOVALLEY High Surface

Section I C KEPEZ

(AN) I black) into the high karstic surface. The high surface is deformed and culminates at 2450 m (Manas›r Tepe). (dark blue line) which ran from the top of the Yarpuz palaeovalley (1850 m) down to Kepez (750 m) where lie the deltaic Tepekli grey with black dots: Eocene flysch. Two morphological profiles (heights x 2) across the Taurus chain (location and carbonates. of the Manavgat Basin. The depth of incision of the palaeovalley is relatively uniform (300 to 400 m) throughout the seventy ki l Dashed Taurus. the of carbonates the through deep, 1000-m nearly today, circulation underground karstic huge a draining hence formations of the Taurus (flysch and allochthonous units) were eroded after the Early Miocene. Hatched area: Antalya Nappes (AN younger faulting has disrupted the former profile in several places. The projected profile of the Manavgat River is about 500 m 10 km Lower Miocene deltaic conglomerates Beyþehir m) Lake (1120 Figure 7.

(AM) Section II Section 0 0 SW N 500 500 3000 1500 1000 2000 2500 3000 1500 1000 2000 2500

10 O. MONOD ET AL.

of the palaeovalleys, independently of their present that the ‹ncebel palaeovalley was incised before, or at altitude. The branching of the valleys remains most during, the early–Middle Miocene. As suggested by hypothetical upstream, and several river courses are the apparently coherent palaeodrainage pattern, the equally conceivable in places where their former trace has uniform morphologic shapes of the valleys and the been eroded. Whatever the case, the resulting network broadly similar altitudes of the valley floors in this part of shows a general drainage trend from NE to SW, with the western Taurus, we infer that most of the rivers cutting the calcareous ridges at right angles, with palaeovalleys should be of about the same age. junctions in the softer formations running parallel to the structures, thus forming a bayonet-like pattern, resembling that of the Jura Mountains today. Latest Miocene and Younger Morphotectonic Events The Messinian Crisis: No Evidence in the Taurus Heights Dating the Palaeotopography on the Taurus Heights Could the incision of the palaeovalleys be related to the The age of the high palaeosurface into which the valleys Messinian crisis? Messinian morphology usually were incised is: (i) more recent than the youngest, corresponds to a regressive erosion process that is best underlying strata, of Late Eocene age; and (ii) older than expressed by deep canyons in the lower parts of the the earliest Neogene deposits covering this surface. In the valleys. This is probably the case in the lower Aksu Basin regions of Ermenek and Mut (Figure 15), although (Figure 13), where the incision of a narrow canyon filled Oligocene lacustrine carbonates have been dated locally, by Lower to Middle Pliocene marine deposits has been an Early Miocene age is attributed to the first extensive attributed to the Messinian by Poisson et al. (2003). By brackish to marine deposits lying above the Mesozoic contrast, the palaeovalleys are situated in the highest basement (Ilgar & Nemec 2005; Erifl et al. 2005). This parts of the western Taurus, far upstream from the leaves a large span of time (from Early Oligocene to the marine basins, and their incision could not have been earliest Miocene) for erosion to build the surface. triggered by the Messinian crisis, the effects of which are Concerning the palaeodrainage system, a minimum not noticeable at such altitudes. age could be estimated by dating the valley infills (cf. de Broekert & Sandiford 2005; Zilberman 1992). Sediments occupying palaeovalleys have allowed Erifl et Hanging Valleys al. (2005) in the Mut region, and Ocako¤lu (2002) north The hanging of the large Miocene fossil valleys over of Adana, to date a lower Miocene palaeotopography. today’s river network can be attributed to Mio–Pliocene However, the method is not applicable in this part of the and Quaternary uplift of the Taurus, followed in turn by: Taurus chain, insofar as most of the palaeovalleys do not (i) karstification with the development of a large contain any infill. Fortunately, a notable exception underground network (Ekmekçi 2003), and (ii) concerns the conspicuous Miocene deposits situated differential erosion and incision by superficial waters of below the ‹ncebel Pass (2000 m) south of the Dipoyraz today’s surficial river network. Surprisingly, however, Da¤ (In.V. on Figure 3). In this locality (Figure 8), thanks many of the fossil tributaries are also in a hanging to a younger offset of the K›rkkavak Fault cutting position above the main palaeovalleys (Figure 5), and through the ‹ncebel palaeovalley, a 750-m-thick infill of could result either from glacial erosion during the horizontal, fluviatile conglomerates is clearly exposed Quaternary, or from an older step succession induced by (Deynoux et al. 2005). Interestingly, on the western side the drop of the water base-level in the karst. of the ‹ncebel Pass, near Yaka village, these fluviatile conglomerates interfinger with shallow marine sediments of the Köprüçay Basin (Figure 3) which contain pelagic Impacts of the Quaternary Glaciations? With the micro- and nannofaunas of Langhian age (NN5) (Deynoux conspicuous exception of Dipoyraz Da¤ (2998 m), where et al. 2005). Albeit indirectly, owing to the distance (9 several recent glacial valleys and lateral moraines have km) separating the fossiliferous locality from the fluviatile been recorded (Monod 1977; fienel 2002), no significant deposits of the ‹ncebel Pass, this age strongly suggests remains of glacial imprint are present on the high surface. The obvious reasons are its insufficient mean altitude and,

11 MIOCENE PALAEOVALLEY NETWORK, WESTERN TAURUS N KKF 2998 m (1350 m) carbonates Dipoyraz Dað Triassic

normal stratigraphic contact side western the On carbonates. Triassic on ing 2005). Location on Figure 3.

et al. wireless relay

(track) E O V A L L E Y E L L A V E O Ýncebel Pass (2000 m) P A LA A P

(width: 1 km) (Late Miocene thrust) Ý N C E B L Miocene fluviatile conglomerates x shales x Triassic KKF fault plane ‹ncebel Pass, viewed from the east, and showing the 750-m-thick fluviatile conglomerate infill of the ‹ncebel palaeovalley rest palaeovalley ‹ncebel the of infill conglomerate fluviatile 750-m-thick the showing and east, the from viewed Pass, ‹ncebel of the pass, near Yaka village, these conglomerates interfinger with marine deposits of Langhian age (Deynoux (Tr-J) Figure 8. S

12 O. MONOD ET AL.

in the higher areas, the lack of large, high summits from Ova, 950 m; Sarayc›k and Sar›alan Yayla, 1450 m), and which ice could accumulate and flow. By contrast, inverted the profile of several palaeovalleys towards the immediately east of the present study area and in a very NE (DV, ZV, and those west of Eynif Ova). The age of similar carbonate landscape, Arpat & Özgül (1972) and these faults is clearly post-early Tortonian (at Sar›alan), Çiner et al. (1999) have described widespread moraines and pre-Pliocene (at Eynif Ova) (Deynoux et al. 2005). On at about 2000 m and several U-shaped valleys around the the eastern side of the area, block faulting also occurred Geyik Da¤ (2875 m). Except for a very limited cirque and is conspicuous south of Seydiflehir (Figures 3 & 14) west of the Kembos Ova (Çeflgar Tepe 2288 m), no with a normal offset exceeding 1000 m. The result was glacial morphology could be detected in the surveyed the raising of the dry valley floors to 1900 m, with area. It can thus be confidently ruled out that the small steeper westward slopes. The lacustrine Plio–Quaternary tributaries winding on the high surface and hanging over deposits near Beyflehir seem unaffected, thus the main dry valleys resulted from Quaternary glacial constraining the age of these faults to the Late erosion. Miocene–Early Pliocene (cf. Koçyigit & Özacar 2003).

Abandoned Tributaries: Successive Karstic Stages? The Miocene Palaeomorphology in the Western Taurus: hanging tributaries most probably result from the drop of New Evidence from Tracer Pebbles the underground network, as described in accounts of A first study by Flecker (1995) showed that significant heavily karstic areas (Ford & Williams 1989). Each variations in composition of the pebbles reflected the successive uplift of the Taurus resulted in a sudden parent lithologies surrounding the Miocene lowering of base level, which was rapidly reached through conglomerates. This is especially clear around the karstic dissolution, hence abandoning the former metamorphic Alanya Massif, which is surrounded by tributaries as soon as the main valleys were deep enough. Burdigalian conglomerates containing abundant The fossilised valleys and their hanging tributaries now metamorphic pebbles derived from the Massif. Another remain remarkably well preserved in the Mesozoic case of close relationship is found in the northern part of limestones, in spite of the rugged karstic landscape of the the Köprüçay Basin, where abundant pebbles of pre- high surface (Figure 4). Cambrian diabase and red Carboniferous sandstone may be easily traced to their source rocks in the neighbouring Tectonic Deformation of the High Surface Dipoyraz Da¤ (Figure 1). Other lithologies, however, pose more problems, as no convenient source rocks are If the Early Miocene age of the river network described available in the neighbourhood. Such are the green above is accepted, the reconstructed fossil morphology tuffites of Hu¤lu, which are good tracers to reconstruct may be used as a guide to infer the age of several tectonic and date the Miocene fluvial network above, and the features which later disrupted the high surface and its Alanya blueschists which suggest a much larger extent for drainage system. As a whole, the central part of the study the Alanya Massif during the Miocene than now. area seems little affected, as shown by the coherent altitudes of both ends of the hanging valleys (AV, PV, CV, HV on Figure 3), with a weak slope oriented to the SW. Hu¤lu Pebbles in the Antalya Basin: Dating the However, a continuous rise of the high surface (Figure 7- Palaeoriver Network of the Western Taurus Section I), from Beyﬂehir Lake (1121 m) to Manas›r Tepe Dark green tuffites of Late Triassic age, associated with (2450 m) and a decrease east of Akseki (1500 m) may dacitic lava flows form the bulk of the Hu¤lu unit in the reflect a blind, deep-seated thrust of Late Miocene age. western Taurus (Monod 1977; Gökdeniz 1981; Andrew In contrast, the western and eastern borders of the & Robertson 2002). Among the various lithologies surveyed area are strongly affected by late Miocene and present in the green tuffites (Figure 9), some exhibit younger faulting. To the west, the K›rkkavak Fault distinctive facies which are readily recognizable. Especially (Dumont & Kerey 1975) and several associated N–S noticeable are the facies that include small green chlorite trending faults have elevated several horsts above 2000 speckles, 1 to 3 mm across, scattered in a finer chloritic m (Figure 3), foundered grabens or half grabens (Eynif matrix containing small quartz and feldspar grains, and

13 MIOCENE PALAEOVALLEY NETWORK, WESTERN TAURUS other pebbles (not circled) include th “Y”-branching in a green chloritic matrix chloritic green a in “Y”-branching th peridotite (P), radiolarite (R) and carbonates (L). Two thin sections from Hu¤lu pebbles show: 1– Tuffite with glassy shards wi shards glassy with Tuffite 1– show: pebbles Hu¤lu from sections thin Two (L). carbonates and (R) radiolarite (P), peridotite (AMA50E); 2– Typical tuffitic facies with chloritic specks dispersed in a finely quartzose matrix (AMA50F). Scale bar: 0.25 mm. Hu¤lu tuffitic pebbles (circled) in the Tepekli Dere conglomerate (Burdigalian) near Sevinç (Manavgat Basin, see Figure 3). The Figure 9.

14 O. MONOD ET AL.

typical glassy shards with curved shapes and Y-shaped branches. Other facies in the Hu¤lu unit include green volcaniclastic rocks and dacitic breccias. These siliceous facies are hard enough to produce resistant, conspicuous pebbles which are found in great numbers in the conglomerates that lie either at the base of the Manavgat Basin (Tepekli Dere near Sevinç, Burdigalian) (Figure 9), or at the top of the Köprüçay Basin (Sar›alan Yayla, lower Tortonian) (Figure 3). The distance separating the source from their depositional area is over 80 km for the former and about 50 km for the latter. Thus the pre-Langhian age of the network suggested by the ‹ncebel palaeovalley infill is compatible with that of the Hu¤lu tracer pebbles found in Burdigalian Figure 10. Blueschist pebble in the Aksu basin from Tafldibi unit conglomerates of the Manavgat Basin (Karab›y›ko¤lu et (Serravallian–Tortonian), location on Figure 12. A typical al. 2000). However, at Sar›alan Yayla, east of the Köprü HP-LT Alanya facies containing large, rotated garnet (Gt) Basin, the age of the conglomerate containing the Hu¤lu surrounded by phengite (Ph, clear), embedded in a schistose matrix of sodic blue amphibole needles pebbles is clearly younger (early Tortonian; Babinot (Glaucophane-barroisite) (Gln), and clinozoisite smaller 2002) and reflects the latest and highest Miocene crystals (Czo). (HES54.1). Scale bar: 0.25 mm. transgression which extended landwards as far as the Kelsu locality near Beyflehir Lake, probably through the pre-existing ria of the ‹ncebel palaeovalley (Figure 11). In unit is composed of polymictic conglomerates of Middle any case, once eroded from their source area, alluvial to Late Miocene age, containing pebbles of metamorphic pebbles can easily be reworked during another or several rocks, sandstone, limestone and spilite. About 20% of the other phases of erosion and transportation affecting the pebbles consist of metamorphic rocks, which include earlier deposits. This possibility leads us to select a white and dark marble, calc-schist, garnet-quartz mica Burdigalian age for the establishment of the Neogene schist and more importantly blueschist metabasite. The palaeo-network preserved on the western Taurus primary mineral assemblage in the blueschist metabasite heights, in agreement with the presence of Hu¤lu pebbles is garnet + crossite + clinozoisite + phengite + rutile. in the ‹ncebel Pass infill and in the Tepekli Dere Garnet porphyroblasts, up to 2 mm across, are set in a conglomerate. fine-grained matrix of sodic amphibole, clinozoisite and phengite. Crossite is rimmed by barroisite and garnet is partly replaced by chlorite. Some of the calc-schist Alanya Blueschists in the Aksu Basin: Nearby or pebbles also contain sodic amphibole along with calcite, Distant Sources? quartz and phengite. Lithologically and petrographically the blueschist metabasite, calc-schist and garnet-quartz In the lower part of the Miocene Aksu Basin, the mica schist pebbles are very similar to those from the occurrence of metamorphic pebbles, including typical Sugözü nappe of the Alanya Massif (Okay & Özgül 1984). blueschist with high pressure-low temperature As there is no other unit of such blueschists in the amphiboles, poses an intriguing problem as it cannot be western Taurides, the metamorphic pebbles in the interpreted (“IMPOSSIBLE PATHWAY” on Figure 1) as a Miocene conglomerates must have been derived from the result of transport by a palaeodrainage system as Alanya Massif, 100 km to the southeast. The problem is described above. The presence of metamorphic pebbles in that, during the Miocene, it is impossible that any the Aksu Basin was already noted along the Sinne Dere by drainage system could have existed between the Sugözü Akay et al. (1985). In the course of a survey of the nappe and the Aksu Basin, as they were separated at that Antalya Neogene basins (Deynoux et al. 2005), rapid time by large marine expanses (namely, the Manavgat and mapping of the area disclosed the presence of an Köprüçay basins). Moreover, the size of the rock imbricated tectonic unit, 7-km long and 500-m thick at fragments (up to half a metre) and their poor rounding most, near Tafldibi village (cgt in Figures 12 & 13). This

15 MIOCENE PALAEOVALLEY NETWORK, WESTERN TAURUS

N 31° 30' Beyþehir Lake Beyþehir ? Dipoyraz Dað

2998 Köprüçay River L E G E N D ÝNCEBEL PAS S Sarýalan marls and conglomerates (2000 m) ? (Lower Tortonian, marine), and 2273 KASIMLAR probable extent Yaka SARAYCIK Y. Kelsu Tepe lagoonal (1450 m) ? marls, (?Lower

37° 30' Tortonian) and 1828 Kesme 2181 Çetmi probable extent SARIALAN Y. HUÐLU KELSU TEPE (1450 m) ? (1300 m) Gencek

2405 probable inland seawaysof ? 2185 the Tortonian shallow- marine transgression ÝKÝZPINAR Derebucak

KÖPRÜÇAY BASIN

B fluviatile

O S conglomerates O

A (Langhian in part) 2450

shallow-marine conglomerates (Langhian in part) KÖPRÜÇAY BASIN ? limestone breccias KIRKKAVAK FAULT (KKF) (Langhian in part)

2251 Beskonak Karpuzçay turbidite E Y (Langhian and N

Ý Köprüçay River F youngers)

V A Oymapýnar Limestone (Burdigalian-Langhian) ? 1757 Ýbradi 1984

LOWER Miocene and younger ? ? EYNÝF OVA normal faults (950 m) 1527 Late Tortonian thrust (northern part of KKF) 37° 31° 30

Figure 11. Sketch map of probable Tortonian seaways into the western Taurus. One is in the north, through the ancient ria of the ‹ncebel palaeovalley and accounts for the Lower Tortonian marls in the Sarayc›k, Sar›alan and Kelsu localities. Another seaway may have been situated south of the Eynif Ova polje, but is not documented.

16 O. MONOD ET AL.

Isparta in grey : marine Miocene N a Kargý 482 Ispart 975 to lake Taþdibi unit Seydiþehir 252 37° 1023 ver Antalya Alanya U Ri Massif ° AKS 31 663 Tu 850

a Recent / scree K

976 x x x x x Quaternary terrace x x s K cgd A marine Pliocene conglomerates R R cg Kargý A m (cg) and marls (m) tunnel D cgd Karadað conglomerates (cgd) R s A (Middle-Upper Miocene) m R 1077 Ð

1036 Tu Aksu Fm. turbidites (Tu) x x cg and conglomerates (cg) 409 x x x x s x Taþdibi unit: conglomerates x x x cgt (cgt) with metamorphic x x pebbles (o) x Taþdibi x x x x Kargý red conglomerates (cgk) 246 x x x x B cgk cg x (? Tortonian) cgt 37°15' s R Upper Miocene reefs (R) m 37°15' and carbonate breccias re Eskiköy Sinne De s Upper Eocene (e) e limestone imbrication

A 381 cg s serpentine (s) e cgk R Mesozoic carbonates of the K Antalya Nappes (undivided) Nalbantlar thrust 75 R A B section Figure 13 (part) Ortaköy cg s 101 Araplar Mah. a 0 1000 m x R 191 x m x x 256 Tu x

AKSU s 25 R 2 R iver

244 m to R A nt al y a Karaahmetler

Figure 12. Map of the southern part of the Aksu valley showing the tectonic position of the Taﬂdibi inlier containing metamorphic pebbles (white circles) derived from the Alanya Massif. A-B: part of the section in Figure 13.

17 MIOCENE PALAEOVALLEY NETWORK, WESTERN TAURUS 2000 1000 0 1 2 E aﬂdibi conglomerates (cgt, ANTALYA NAPPES ANTALYA Cgd Soyataþ T. Soyataþ AN AKSU THRUST AKSU Tu Cgd Tu B R Karadað s Cgk Ta þdibi Ta R Kargý tunnel s P Pliocene thrusts AN Eskiköy Aksu Valley Messinian canyon A 2 Section of the Taﬂdibi unit. Explanation as Middle–Late Miocene). Location given in Figure 1. for Figure 12. White circles – metamorphic pebbles (including blueschists) in the T BD km 0 Figure 13. W 0 1 2 2000 1000

18 O. MONOD ET AL.

preclude lengthy transport. A westerly origin, from the - During the Late Langhian, a rapid rise of sea level HP-LT rocks of the Lycian nappes can be excluded, owing (Karab›y›koglu et al. 2000) induced a short-lived to the distance and the distinct facies with abundant transgression which allowed deltaic sedimentation at carpholite of the high-pressure units surrounding the the mouths of the rivers, as vividly exemplified by the Menderes Massif (Rimmelé et al. in press). thick accumulation of Langhian fluviatile to marine We must therefore conclude that, during the Miocene, conglomerates in the Incebel Valley (Deynoux et al. the metamorphic Alanya Massif extended much farther 2005). westward, probably as far as Antalya, as shown in Figure - During the Middle and early Late Miocene, although 1. This conclusion is further supported by two small no direct evidence is available, the drainage system of inliers (less than one kilometre long) of typical the Taurus was still continuously active, as suggested metamorphic rocks of the Alanya Massif situated in an by the abundance of polymict coarse detrital materials intermediate position (two stars on Figure 1), that were shed into the Manavgat and Köprü basins during that already noted on Akay’s map (1985). Erosion of the interval (Karpuzçay formation, Karab›y›koglu et al. Sugözü nappe took place first, as indicated by the greater 2000). abundance of HP-LT pebbles in the lowest part of the - Early in the Tortonian, a final transgression brought Taﬂdibi conglomerates, in agreement with the higher tectonic position of the Alanya Massif atop the Antalya shallow-marine influences far into the chain (Figure units. Subsequent erosion affected the underlying Antalya 11) through a few narrow rias corresponding to the nappes and progressively produced the usual polymictic main palaeovalleys, as shown by the deltaic facies of the Miocene conglomerates in which conglomerates and shallow-marine marls in the metamorphic pebbles become quite scarce. Sar›alan, Sarayc›k, Kelsu and (possibly) Eynif Ova localities (Figure 3). - Late in the Tortonian, the fluvial network of the Conclusions Taurus was suddenly disrupted by major tectonic Morphotectonic Evolution of the Western Taurus events, which resulted in a series of normal and during the Neogene reverse faults in the western part of the chain (Figure Although highly speculative in places, several steps may 3). Some of the faulted blocks were elevated, and be proposed in deciphering the morphotectonic evolution rapid development of karstic circulation through the of the western Taurus: carbonate rocks prevented further erosion of the former fluviatile morphology, thus preserving the - During the Oligocene and earliest Miocene (Figure fossil valleys in the higher parts of the Taurus. 14A), erosion prevailed and partly levelled the recently (Late Eocene) structured Taurus chain, - In the nearby Aksu Basin, strong uplift during the Late resulting in a somewhat irregular, but low Miocene is indicated by the complete erosion of the topography, which was cut into either calcareous or neighbouring metamorphic Alanya Massif, which was softer formations. Most of the tracer pebbles (Hu¤lu situated atop the Antalya nappe pile, and the coeval tuffites) were transported and deposited at that time. deposition of metamorphic pebbles in a shallow- As suggested by the meanders of several palaeovalleys marine environment. This uplift was probably induced flowing from NE to SW, the regional topography by a compressional event such as the Aksu Phase displayed a weak slope. This pattern also suggests the (Poisson et al. 2003), which is responsible for most probable absence of significant karstic circulation, of the westward imbricated structures in the Aksu which would have disrupted the river flows. Basin (Figure 13). - Subsequent rise of the Taurus belt resulted in deep - During the Pliocene and Quaternary (Figure 14C), incision of the valleys (Figure 14B) which could, major uplift of the western Taurus as a whole however, maintain their former shapes, hence subjected the chain to intense erosion, renewing producing entrenched meanders through the karstic circulation in the carbonate rocks, removing calcareous ridges, with hanging tributaries due to the part of the softer terrains, and so destroying the rapid onset of underground circulation in the karstic ancient fluviatile morphologies there. Plio–Quaternary areas. coarse detrital materials accumulated in the endoreic

19 MIOCENE PALAEOVALLEY NETWORK, WESTERN TAURUS

HUÐLU UNIT

BHN allochthonous units

HV A Sevinç PV Late Oligocene ÜV to Early Miocene

meandering rivers KepeKepez J-K HV: Hallaç Valley PV: Piser Valley ÜV: Ürünlü Valley YV: Yarpuz Valley AM AN

HUÐLU UNIT repeated uplifts

BHN allochthonous units

B Sevinç PV HS Lower- Middle Miocene ÜV dry tributary

A Kepez J-K incision of N deep valleys AM AN F F F Seydiþehir Huðlu major uplift YV Suðla Yarpuz HS Lake F HV

Üzümdere BHN allochthonous units HS C River PV Sevinç Present Manavgat ÜV Manavgat Kepez J-K hanging valleys

M Mid-Upper Miocene Fms. M of the Manavgat Basin Tepekli conglomerate (Burdigalian) AN HS: High Surface AM AM Alanya Massif J-K Mesozoic carbonates AN Antalya Nappes F: Mio-Pliocene normal faults BHN Beysehir-Hadimç Nappes

Figure 14. Three cartoons illustrating the morphologic evolution of the western Taurus from Oligocene to Present. (A) A flat morphology in the western Taurus during the Oligocene and Early Miocene; (B) Uplifting and incision of deep valleys (in red) into the high surface (HS) during Lower–Middle Miocene; and (C) Present aspect of the Taurus chain with isolated remains of the High Surface and several fragments of the former drainage system (“hanging valleys”).

20 O. MONOD ET AL.

basins (Beyﬂehir depression) but mostly seawards Mediterranean. Because it escaped the main Miocene (Belkis conglomerates, Blumenthal 1951). deformations, this area has preserved its original - On a larger scale, the fossil drainage identified here palaeogeographic framework. In addition to the area (Figure 15) embraces only part of a much wider area discussed above, between Beyﬂehir and Manavgat, a of southern Turkey which was exposed during the rough DEM map (Figure 15) illustrates the probable Neogene, shedding materials mostly towards the extent of the Miocene aerial surface in the Taurus,

31û 32° 33° 34°

38° 38° Konya Isparta K N Figure 3

SeydiþehirÁ

37° A 37° Mut Antalya Ermenek

Alanya Massif M Mediterranean Sea

0 100 km

A M K DEM High Surface Antalya Basin Mut Basin Konya Basin (pre-Miocene) (L-U. Miocene) (L-M. Miocene) (non-marine Neogene)

Miocene Pre-Miocene thrusts Aksu thrust fluviatile (late Eocene) (Late Miocene) network

Figure 15. Extent of the High Surface (in black) as shown by a Digital Elevation Model (DEM) of the western and central Taurus, and the three surrounding Neogene basins (Antalya, Mut, Konya). In blue, situation of the fossil drainage network described above.

21 MIOCENE PALAEOVALLEY NETWORK, WESTERN TAURUS

thus showing where other ancient morphologic Miocene detrital materials, to M. Bakalowicz for fruitful features could be preserved. Delimitation of this vast information on the karstic processes, to B. Vigier for area is only approximate, and additional fossil producing a DEM map of part of the Taurus, and N. features have still to be identified and dated where Rouchon for the figures. W.T. Dean very kindly corrected possible, to refine the shape of the oldest morphology the English text. The authors acknowledge the Turkish of the Taurus chain. Academy of Sciences, the French Ministry of Foreign Affairs (MAE), ISTO-CNRS (Orléans) and MTA (Ankara) for financial support, exchanges and fieldwork facilities. Acknowledgements The authors thank A. Koçyigit and K. Dirik for their useful suggestions. This work formed part of the O.M. is grateful to M. Karab›y›ko¤lu, M. Deynoux and A. TÜB‹TAK-CNRS joint project N° 5785. Çiner for numerous hot discussions in the field on the

References

AKAY, E., UYSAL, S., POISSON, A., CRAVATTE, J. & MÜLLER, C. 1985. EKMEKÇ‹, M. 2003. Review of Turkish karst with emphasis on tectonic Stratigraphy of the Antalya Neogene Basin. Bulletin of the and palaeogeographic controls. Acta Carsologica 32, 205–218. Geological Society of Turkey 28, 105–119. ER‹ﬂ, K., BASSANT, P. & ÜLGEN, U. 2005. Tectono-stratigraphic evolution ANDREW, T. & ROBERTSON, A.H.F. 2002. The Beyﬂehir-Hoyran-Hadim of an Early Miocene incised valley-fill in the Mut Basin, southern nappes: genesis and emplacement of Mesozoic marginal and Turkey. Sedimentary Geology 173, 151–185. oceanic units of the Northern Neotethys in southern Turkey. FLECKER, R., ROBERTSON, A.H.F., POISSON, A. & MÜLLER, C. 1995. Facies Journal of the Geological Society, London 159, 529–543. and tectonic significance of two contrasting Miocene basins in ARPAT, E. & ÖZGÜL, N. 1972. Rock glaciers around Geyik Da¤, Central south coastal Turkey. Terra Nova 7, 221–232. Taurides. Mineral Research and Exploration Institute of Turkey FORD, D.C. & WILLIAMS, P.W. 1989. Karst Geomorphology and (MTA) Bulletin 78, 28–32. Hydrology. Unwin Hyman, London, 583 p. BABINOT, J.-F. 2002. Ostracodes miocènes de séries annexes aux bassins GÖKDENIZ, S. 1981. Recherches géologiques dans le Taurus occidental de Köprüçay et de Manavgat, région d’Antalya (sud Turquie). entre Karaman et Ermenek. Les séries à Tuffites vertes triasiques. Revue Paléobiologie, Genève 21, 735–757. PhD Thesis, Université Paris-Sud, Orsay, 202 p [unpublished].

BIROT, P. & DRESCH, J. 1956. La Méditerrannée et le Moyen Orient, t. 2, GUTNIC, M., MONOD, O., POISSON, A. & DUMONT. J.-F. 1979, Géologie des 526 p. Taurides occidentales. Mémoire Société géologique de France BLUMENTHAL, M. 1951. Recherches géologiques dans le Taurus 137, 1–112.

Occidental dans l’arrière-pays d’Alanya. Mineral Research and ILGAR, A. & NEMEC, W. 2005. Early Miocene lacustrine deposits and Exploration Institute of Turkey (MTA) Publications D5, 134 p. sequence stratigraphy of the Ermenek Basin, central Taurides,

ÇINER, A., DEYNOUX, M. & ÇÖREKÇ‹O⁄LU, E. 1999. Hummocky moraines in Turkey. Sedimentary Geology 173, 233–275.

the Namaras and Susam Valleys, Central Taurides, SW Turkey. KARABIYIKO⁄LU, M., ÇINER, A, MONOD, O., DEYNOUX, M., TUZCU, S. & ÖRÇEN, Quaternary Science Reviews 18, 659–669. S., 2000. Tectonosedimentary evolution of the Miocene Manavgat

DE BROEKERT, P. & SANDIFORD, M. 2005. Buried inset-valleys in the Basin, Western Taurids, Turkey. In: BOZKURT, E., WINCHESTER, J.A. eastern Yilgarn Craton, western Australia: geomorphology, age, & PIPER, J.A.D. (eds.), Tectonics and Magmatism in Turkey and and allogenic control. The Journal of Geology 113, 471–493. the Surrounding Area. Geological Society, London, Special Publications 173, 475–498. DEYNOUX, M., ÇINER, A., MONOD, O., KARAB›Y›KO⁄LU, M., MANATSCHAL, G. & TUZCU, S. 2005. Facies architecture and depositional evolution of KOÇY‹⁄‹T, A. & ÖZACAR, A. 2003. Extensional neotectonic regime through alluvial fan to fan-delta complexes in the tectonically active the NE edge of the outer Isparta Angle, SW Turkey: new field and Miocene Köprüçay Basin, Isparta Angle, Turkey. Sedimentary seismic data. Turkish Journal of Earth Sciences 12, 67–90. Geology 173, 315–343. KOÇY‹⁄‹T, A., ÜNAY, E. & SARAÇ, G. 2000. Episodic graben formation and

DUMONT, J.-F. & KEREY, E. 1975. K›rkkavak fay›: bat› Toroslar ile extensional neotectonic regime in west Central Anatolia and the Köprüçay Baseni s›n›r›nda kuzey–güney du¤rultu at›ml› fay Isparta Angle: a case study in the Aksehir-Afyon Graben, Turkey. [K›rkkavak fault: A N–S-trending strike-slip fault at the contact In: BOZKURT, E., WINCHESTER, J.A. & PIPER, J.A.D. (eds.), Tectonics between the western Taurides and Köprüçay Basin]. Bulletin of and Magmatism in Turkey and the Surrounding Area. Geological the Geological Society of Turkey 18, 59–62 [in Turkish with Society, London, Special Publications 173, 405–421. English abstract].

22 O. MONOD ET AL.

LOUIS, H. 1956. Die Enstehung der Poljen und ihre Stellung in der POISSON, A., WERNLI, R., SAGULAR, E.K. & TEM‹Z, H. 2003. New data Karstabstragung, auf Grund von Beobachtungen im Taurus. concerning the age of the Aksu Thrust in the south of the Aksu Erdkunde Archiv für wissenschaftliche Geographie X, 33–53. Valley, Isparta Angle (SW Turkey): consequences for the Antalya Basin and the Eastern Mediterranean. Geological Journal 38, MONOD, O. 1977. Recherches géologiques dans le Taurus Occidental au 311–327. sud de Beyflehir (Turquie). PhD thesis, Université Paris-Sud Orsay, 442 p [unpublished]. RIMMELÉ, G., OBERHÄNSLI, R., CANDAN, O., GOFFÉ, B. & JOLIVET, L. (in press) The wide distribution of the HP-LT rocks in the Lycian belt (W MONOD, O. 1979. Carte géologique du Taurus Occidental au sud de Turkey): implications for the accretionary wedge geometry. Beysehir et Notice explicative. Editions du CNRS, Paris, 60 p. fiENEL, M. 2002. Geological Map of Turkey (1/500000), Konya Sheet. NAZIK, L. 1992. Beyflehir Gölü Güneybat›s› ile Kembos Polyesi Aras›n›n Mineral Research and Exploration Institute of Turkey (MTA) Karst Jeomorfolojisi [Karst Geomorphology of the Area between Publications, Ankara. Kembos Polye and SW Beyflehir Lake]. PhD thesis, ‹stanbul Üniversitesi, 298 p [in Turkish with English abastract, ZILBERMAN, E. 1992. Remnants of Miocene landscape in the central and northern Negev and their paleogeographical implications. Israel unpublished]. Geological Survey Bulletin 83, 1–54. OCAKO⁄LU, F. 2002. Palaeoenvironmental analysis of a Miocene basin in the high Taurus (southern Turkey) and its palaeogeographical and structural significance. Geological Magazine 139, 473–487.

OKAY, A.‹. & ÖZGÜL, N. 1984. HP/LT metamorphism and the structure of the Alanya Massif, southern Turkey: an allochthonous composite tectonic sheet. In: ROBERTSON, A.H.F. & DIXON, J.E. (eds.), The Geological Evolution of the Eastern Mediterranean. Geological Society, London, Special Publications 14, 429–439

Received 23 April 2005; revised typescript accepted 12 June 2005