Journal of the Geological Society, London, Vol. 152, 1995, pp. 873-882, 13 figs., 2 tables. Printed in Northern Ireland

Tectonic controls on stratigraphic evolution of the Adana Basin, Turkey

G.D. WILLIAMS’, U CANUNLUGENC’, G. KELLING’ & C. DEMIRKOL2 ’Geology Department, Keele University, Keele, Staffordshire, ST.5 5BG, UK 2 Geology Department, Cukurova University, 01330 Adana, Turkey

Abstraet: The Neogene Adana Basin of SE Turkey was initiated after thrust emplacement of the Tauride Belt to the north of the basin. Seismic reflection profiles across the southern part of the Adana Basin provide information on structural and stratigraphic evolution of thebasin. Based on seismiccharacter and theidentification ofunconformities, three megasequences and two mega sequence boundaries are identified. Thefirst megasequence is partly coincident with an early Miocene rifting event and it comprises reefs that have grown on fault footwall crests with fore and back-reef sediments in intervening lows. Subsequent rapid flexurally induced subsidence generated an under- filled basin whichwas then passivelyfilled by turbiditicsediments (megasequence 2) showing aggradational character on seismic profiles. Further extensional faulting and coupled sinistral wrench faulting took place after the deposition of megasequence 2. Erosional truncation of its upper part is followed by the deposition of continental and shallow marine sediments of megasequence 3 which shows localized progradational sequences characteristic of shallow water deposition. Further minor extensional faulting took place after the deposition of megasequence 3.

Keywords: Adana Turkey, structural geology, stratigraphy.

The structuralevolution of SE Turkey has been described in sediments represent seismic ‘basement’ with little resolvable terms of the interaction of several major wrench faults in the stratigraphy beneath this level. The interpretation of seismic Kharaman Mara? triple junction (Sengor 1980; Robertson & reflection profiles linked to field observations of structure Dixon 1984; Sengor et al. 1985). These major faults are the and stratigraphy in theAdana Basin hasproved to bea N-S-trending Dead Sea fault zone separating Africa from powerful tool inunderstanding basin forming mechanisms Arabia,the NE-SW-trending Bitlis suture which divides and in establishing an outline of basin evolution. This paper Arabia from Eurasia and the eastern part of the Hellenic is anattempt to integrate the tectonicevolution of the trenchwhere Africa is subducting beneath Eurasia. The Adana Basin with the filling of the basin in Neogene times. Adana Basin is locatedentirely onthe Anatolian Plate whose southerly boundary is marked by the Bitlis Suture which appearsto continue to the SW intothe Misis Traditional stratigraphic treatment Structural High (Fig. 1) (Sengor & Yllmaz 1981; Dewey et The traditional stratigraphy has involved subdivision of the al. 1986). basin fill into formations on the basis of lithostratigraphic The Adana Basin is bounded by the Ecemis Fault Zone and biostratigraphiccorrelations (Kirk 1935; Blumenthal to the west, the Misi? Structural High to the east and the 1941; Ternek 1957; Abdiisselamogou 1959; Schmidt 1961). overthrust Tauride Orogenic Belt to the north (Fig. 1). The More recent palaeontological and sedimentological research main Adana Basin was initiated afterthe late Eocene to has been carried out by Goriir (1979,1982), YalGin & Goriir Oligocene thrust emplacement of an ophiolitic complex and (1984) and Yeti? & Demirkol (1986). Todate, little associated melange in the Taurides to the north of the area. emphasishas been placed on the possible diachroneity of Awidespread, early Miocene phase of rapidsubsidence formations noron the nature of formation (or sequence) probably in a foreland basin setting (Kelling et al. 1987) and boundaries (but see Goriir 1992). A full stratigraphic accompanied by extensionalfaulting gave rise to marine column for the Adana Basin is given in Table 1. invasion followed by gradual passive infilling and shoaling of The KarsantiFormation was depositedin a separate the basin during mid to late Miocene times. Late Miocene intermontane basin tothe northwest of the main Adana deformation occurred in the Misis Structural High and this Basin. It unconformably overlies Tauride ophiolitic rocks producedan area in thesouth of the basin of extensive which were eroded and derived into the Karsanti Formation erosion marked by shallow angular unconformity followed sediments which comprise alluvial fan, fluvial, lagoonal and by the deposition of Tortonian and Messinian continental lacustrinedeposits (UnliigenG & Demirkol 1991). These deposits. sediments were deformed by a compressional event of late Seismic reflection profiles across the southern part of the Oligocene age in the NE of theAdana Basin andare Adana Basin (Fig. 2) and selected well logs have been made unconformably overlain by succeeding sequences. The available by theTurkish Petroleum Company (TPAO). Gildirli Formation is restricted to the northern part of the Because of thegeneral southerly dip of the Neogene Adana Basin and comprises a thick sequence of sediments, sequences observed at outcrop in the north of the fluvio-lacustrine sediments. In the NW of the Adana Basin a basin are present atdepth in the seismic profiles. The conformable passage of the Gildirli Formation into younger seismic profiles are unmigrated, and early Miocene reefal sequences is seen. 873

Downloaded from http://pubs.geoscienceworld.org/jgs/article-pdf/152/5/873/4890413/gsjgs.152.5.0873.pdf by guest on 02 October 2021 a74 WILLIAMS G. D. ET AL.

37

36

Fig. 1. Location map of the Adana Basin in SE Turkey: major faults are indicated (+, upthrown and -,dow- nthrown side). D.S.F.Z., Dead Sea fault zone; E.A.F.Z., east Anatolian fault zone.

Field investigationshave shown thatthe Karaisali (TWTT). The seismic lines have been tied by well data Formation is predominantlya carbonate reefalsequence where possible. Miocenereefal sediments of the Karaisali (Goriir 1977, 1979, 1985) thatappears to be mainly Formation form a bright positive reflection event and this is developed on isolated highs. Thereare flanking fore-reef effectively seismic basement beneath which the sections are and shallow marine sequences surrounding the reefal bodies. largely seismically transparent (Figs 3 & 4). TheAdana This formation passes laterally intothe Kaplankaya Basin stratigraphy may be subdivided intothree megase- Formation which marks the first input of marine clastics into quencesbased on internal seismic character and megase- the basin. The Cingoz and GiivenG Formations represent a quence boundary relationships. The megasequences broadly sequence of turbiditic sediments that show a shallowing of relate to traditional stratigraphy as shown in Table 2. the basin through time. Turbidites are point-sourced to the Megasequence 1 is a bright reflection event representing north and northwest and exhibit southerly and southeasterly Lower Miocene reefal deposits which appear to have formed palaeocurrents (Giirbiiz 1993). preferentially on the crests of major extensional fault blocks The Pliocene Kuzgun Formation overlies the GiivenG (Fig. 4). Megasequence 2 comprises parallel continuous Formation with slight angular unconformity. Field exposures reflectors indicative of turbiditic sediments. There is no show that at this boundary there is locally a marked facies evidence of expansion or growth of sequences in extensional change from outer marine shelf to continental fluvio-deltaic fault hanging walls (Figs 5 & 6) and therefore this is deposits (Unliigenq 1993). interpreted to represent sediment that has passively infilled a deep basin. There is some evidence for local onlap at the base of megasequence 2 on to megasequence 1 (Fig. 5) a Seismic sequence stratigraphy: Adana Basin relationship also observed in the field within the Adana Morethan 300 km of onshore seismic reflection data Basin (as in the Karaisali region; Goriir 1977). Marked supplied by TPAO (Fig. 2) havebeen interpreted in an erosionaltruncation at thetop of megasequence 2 occurs attempt to understand the stratigraphy and structure of the beneath the 213 megasequence boundary (Fig. 5). Megase- Adana Basin. The seismic is of 1986 to 1988 vintage, is quence 3 shows local evidence for onlap at its base (Fig. 6). unmigrated and was shotto 4s two way traveltime It is shown seismically as largely parallel reflectors that dip

Downloaded from http://pubs.geoscienceworld.org/jgs/article-pdf/152/5/873/4890413/gsjgs.152.5.0873.pdf by guest on 02 October 2021 STRATIGRAPHICEVOLUTION ADANATHE OFBASIN, TURKEY 875

Fig. 2. Map to show the extent of seismic coverage in the Adana Basin (individual lines identified by three-figure numbers).

broadlysouthwards. Some progradational sequences, pos- and displacement of the bright reflector of megasequence 1 sibly representingdeltaic deposits, are present atthe (Figs 3, 5 & 6). The megasequence 2/3boundary is southern part of line 307 (Fig. 3). displaced by the same extensional faults, but only a minor amount of displacement is present (Figs 5 & 6). At the south Structural geology: seismic lines of the seismic line shown Fig.in a 3 suite of southward-downthrowingextensional faults is present in Megasequences 1 and 2 are cut by numerousextensional megasequence 3. Relativelycontinuous reflection events faults asshown by truncated reflectors (megasequence2) deep in the profiles beneath megasequence 3 dip northwards

Table 1. Traditional stratigraphic scheme for the Tertiary and Quaternary of the Adana Basin

NE of Adana Basin NW of Adana Basin

Quaternary Terrace alluvium Terrace alluvium ...... Pliocene Miocene Messinian Handere Formation Handere Formation Miocene Tortonian Kuzgun Formation Kuzgun Formation

Miocene Serravalian GiivenG Formation GiivenG Formation Miocene Langhian Cingoz Formation Cingoz Formation Miocene Langhian Karaisali Formation Karaisali Formation Miocene Burdigalian Kaplankaya Formation Kaplankaya Formation Miocene Aquitainian Gildirli Formation Oligocene Karsanti Formation

Downloaded from http://pubs.geoscienceworld.org/jgs/article-pdf/152/5/873/4890413/gsjgs.152.5.0873.pdf by guest on 02 October 2021 876 G. D. WILLIAMS ET AL.

S N

Fig. 3. (a) Seismic reflection profile 307. (b) Line drawing of interpretation of seismic line 307: base of megasequence 3 in stipple; top of megasequence 1 in vertical hachuring. Megasequence 2 shows aggradational nature of reflectors. North dipping reflectors beneath megasequence 3 are interpreted as Tauride thrusts. In the south of the line, south-directed progradational sequences are present in megasequence 3 and these are cut by normal faults with a southerly component of downthrow.

at ashallow angle (Figs 3, 5 & 6) and are interpreted as for megasequence 2 have beengenerated. The time Tauride thrustfaults associated with northtosouth structure map for base megasequence 2 (Fig. 7) shows two thrusting. These faults may have become reactivated during distinct fault trends: a NW-SE trend for major extensional extensionaldeformation. Bright continuous reflectors of faults to the north of Adana and a N-S trend outlined by megasequence 2 outline folding at a wavelength of tens of the Imamogou fault zone. An anticline/syncline pair to the kilometres that occurred prior to erosion and the deposition north of Adana has a NW-SE axis and is parallel to the of megasequence 3 (Figs 5 & 6). mainextensional fault trend. Contourpatterns show a A large scale, N-S-trending positive flower structure, the general N-S dip for the megasequence boundary but this is Imamoglou fault zone, is present on the seismic line of Fig. modified into a deep N-S trough tothe west of the 4. This has been active after the deposition of megasequence Imamogou fault zone and an erosional high associated with 2 as shown by erosional truncations beneath megasequence this zone. 3 toboth sides of thestructure (Fig. 4). The Imamogou The basemegasequence 3 (Fig. 8) time structuremap fault zone was reactivated as a positive flower structure shows NW-SE faults tothe north of Adanaand an during and after the deposition of megasequence 3 as there erosional high along the Imamoglou fault zone. The contour are internal erosional unconformities within mega-sequence pattern for this boundary indicates abroad plunging syncline 3 to the west of the fault zone. Also there is local evidence whose axis trends NE-SW, passing through the city of of internal angular unconformities in megasequence 2 to the Adana. east of this fault zone (Fig. 4). The isochron for megasequence 2 (Fig. 9) indicates the thickness of this unit in TWTT. Megasequence 2 becomes erosionally truncatedto the Nand NW of the area of Structuring and basin fill: time-structure maps seismic coverage and along the Imamoglou fault zone. It is Using all available seismic and well data, time structure thickest between a major NW-SE-trending extensional fault maps for the two megasequence boundaries and an isochron and the Imamoglou fault zone. Another NW-SE-trending

Downloaded from http://pubs.geoscienceworld.org/jgs/article-pdf/152/5/873/4890413/gsjgs.152.5.0873.pdf by guest on 02 October 2021 STRATIGRAPHIC EVOLUTION OF THE ADANA BASIN, TURKEY a77

W E

Fig. 4. (a) Seismic reflection profile 106. (b) Line drawing of seismic line 106. The Imamoglou Fault Zone is represented by a positive flower structure that has been active syn-megasequence 3. Erosional truncations to the west and east of this structure are present beneath the megasequence 3 unconformity.

Table 2. Simplified seismic stratigraphy used in this The thick sequences were preserved in tectonic lows which paper with approximate correlations with the tradi- were generatedprior to the erosionalevent of the base tional stratigraphy megasequence 3 boundary. The preservation of thick sections of megasequence 2 Megasequence 3 HandereFormation may be illustrated by flattening interpreted sections on the Kuzgun Formation megasequence 213 boundary (Fig. 10a & b). The Megasequence 2 GiivencFormation post-depositionalextensional fault control of thick se- Cingoz Formation quences is seen on a dip line (Fig. 5) where faults have a Kaplankaya Formation northerlycomponent of downthrowand on a strike line Megasequence 1 KaraisaliFormation (seismic basement) (Fig. 6) where faults downthrow to the east.

Tertiary to Quaternary evolution of the Adana ‘thick’ region occurs to the north of Adana. It shouldbe Basin: discussion notedthat the ‘thick’ areasdo not represent syn-tectonic TheAdana Basin was formedentirely on theAnatolian depocentres for megasequence 2. Extensional faulting and plate and its south easterly boundary is the Misis Structural movement on the Imamogou fault zone were synchronous High which is considered to be a continuation on the Bitlis and occurred following the deposition of megasequence 2. Suture Zone. Prior to basin development, ophiolitic thrust

Downloaded from http://pubs.geoscienceworld.org/jgs/article-pdf/152/5/873/4890413/gsjgs.152.5.0873.pdf by guest on 02 October 2021 878 G. D. WILLIAMS ET AL.

S N

I '4

Fig. 5. Line drawing of interpretation of seismic line 211: base of megasequence 3 in stipple; top of megasequence 1 in vertical hachuring. Megasequence 2 shows aggradational nature of reflectors and erosional truncations beneath megasequence 3 in the south of the line. - Extensional faults occurred after megasequence 2 and may link to pre-existing Tauride thrusts.

sheets were obductedon to the South Anatolian plate that containlargea proportion of derived ophiolitic during an Eocene collisional event. The Tauride ophiolitic material. sheets overrode an ophiolitic melange (Fig. lla). Regional Marine sequences of the Adana Basin commenced with erosion and planation then occurred in earlyOligocene Miocene shallow marine, littoral and reefal deposits many of times (Fig. llb). which appear to be localized on tectonic highs, possibly the To the north of the present-day Adana Basin large scale footwallcrests of extensional faults (Fig. 12a). It is likely extensionalfaults controlled the deposition of Oligocene that earlyMiocene extensional faults in theAdana Basin continentalsequences of the Karsanti Formation and also formed in response to load-induced flexure resulting from the earlyMiocene Gildirli Formation(Goriir 1992). renewed thrusting in the Taurides to the north. Continued Deposition of thesesequences is thought to have taken thrusting to the north of the Adana Basin led to a major placein major half graben controlled by deeprooted subsidence event that generated a deep underfilled foreland basementfaults that cut and displaced the thin-skinned basin prior to input of clastic sediments (Fig. 12b). The ophioliticthrust sheet (Fig. llc).The lower part of the turbiditic sediments of megasequence 2 are point sourced to Karsanti Formation is represented by alluvial fan deposits thenorth and north west of the basin and show no

W E -0

-1

r? U (L) v, -2 l= 3 t

-3

I 4 Fig. 6. Line drawing of interpretation of seismic line 310: base of megasequence 3 in stipple; top of megasequence l in vertical hachuring. Megasequence 2 shows aggradational nature of reflectors and erosional truncations beneath megasequence 3 in the west and central part of the line. Extensional faults with an easterly component of downthrow occurred after megasequence 2 and link to the pre-existing Tauride thrusts. Westerly onlap is shown by megasequence 3.

Downloaded from http://pubs.geoscienceworld.org/jgs/article-pdf/152/5/873/4890413/gsjgs.152.5.0873.pdf by guest on 02 October 2021 MEDITERRANEAN

J Fig. 7. Two-way-time-structure map for base megasequence 2. Contours in seconds TWTT. Major NW-SE-trending faults are present north of Adana and the Imamogou Fault Zone is represented by the N-S-trending erosional high.

Fig. 8. Two-way-time-structure map for base megasequence 3. Contours are in seconds TW7T. A broad SW-plunging syncline has an axis running through Adana city. The spatial extent of the progradational sequence is shown as dashed lines with stipple. Eroded areas are controlled by the Imamoaou Fault Zone and the northern uplift of the main Adana Basin.

Downloaded from http://pubs.geoscienceworld.org/jgs/article-pdf/152/5/873/4890413/gsjgs.152.5.0873.pdf by guest on 02 October 2021 880 G. D. AL.WILLIAMS ET

Fig. 9. Isochron (thickness in seconds TW'IT) for megasequence 2. The map shows an area of thick megasequence 2 between Adana city and the Imamoglou Fault Zone (eroded MS2 on map).

21 1 S N 31 0 W

(a) (b) Fig. 10. Line drawing interpretations of seismic lines flattened on base megasequence 3. (a) line 211 (Fig. 3); (b) line 310 (Fig. 4). Flattened sections show the control on thickness of megasequence 2 by NE-downthrowing extensional faults.

Downloaded from http://pubs.geoscienceworld.org/jgs/article-pdf/152/5/873/4890413/gsjgs.152.5.0873.pdf by guest on 02 October 2021 S N Eocene

1 ophiolitic p rnelanqe

S

1 ophiolitic p melanqe

Fig. 11. Eocene-Oligocene evolution of the S Anatolian plate: (a) Southerly S obduction of ophiolitic thrust sheet N which overrides ophiolitic melange. (b) Oligocene Early Oligocene erosion and planation of the thrust sheet. (c) Late Oligocene extensional faulting in the north of the region and deposition of continental sediments (Karsanti and Gildirli El Formations).

S Aquitainian N Burdigalian

shollow marine on fault block crests

\'

aheod of thrustsheets

S Langhian N Imarine tronsgression I

Fig. 12. Early to mid-Miocene evolution of megasequence 2: (a) Minor exten- sional faults with associated growth of reefs on fault block crests. Faults are formed in response to flexural loading by S Langhian- N renewedTaurides thrust activity in the Serravalian to the north of the area. (b) Flexurally induced subsidence generates a deep undertilled basin in Langhian times and carbonate reefs step back towards the north during a transgressive phase. (c) During Langhian and Serravalian times the basin is passively filled with a shoaling upwards sequence of turbidites.

Downloaded from http://pubs.geoscienceworld.org/jgs/article-pdf/152/5/873/4890413/gsjgs.152.5.0873.pdf by guest on 02 October 2021 882 G. D. WILLIAMS ET AL.

S N 1s thought to relate to thelocal uplift of the Misis Structural High (Fig. 13a). Further broad scale folding on a NE-SW Tortonian axis was controlled by uplift to the north of the basin (Fig. Messinian 13b) and uplift in theImamogou fault zone.Extensional faults cutting megasequences 1 and 2 were reactivated at a 1 prog-1 late stage and show small extensional displacements of the megasequence 213 boundary. -4 -4 un conformity1 References ABDUSSELAMO~LOU,M. S. 1959. Yukari Seyhan BolgesindeDo@ Toroslarin Jeolojik Etiidii. Ankara MTA Enstitiisii Derleme Raporu, 2668. BLUMENTHAL,M,-M. 1941. Nigde ue Adana uilayetleri Dahilindeki Toroslarin Jeolojisine Umumi bir bakis. Ankara MTA Eustitiisii Derleme Rapor, 6, Seri B. COVEY,M. 1986. The evolution of foreland basins to steady state: Evidence from the W Taiwan foreland basin. In: ALLEN,P.A. & HOMEWOOD,P. (eds) Foreland Basins. International Association of Sedimentologists Special Publications, 77-90. S N DEWEY,J.F., HEMPTON,M.R., KIDDE.W.S., SARO~LU,F. AND SENGOR, A.M.C. 1986. In: COWARD,M.P. & RIES, A.C. (eds) Collision Tectonics. Geological Society, London, Special Publications, 19, 3-36. GORUR,N. 1977. Sedimentology of the Karaisali Limestone and Associated Clastics (Miocene) of the Northwest Flank of the Adana Basin, Turkey. PhD thesis, Univ. London. - 1979. Karaisali kirectaginin (Miyosen) sedimantolojisi. Turkish Geological Society Bulletin, 22, 227-232. - 1982. Adana Havzasi’nin petrolpotansiyelinin deger lendirilmesinde yeni bir goriis. Tiirkiye 6 Petroleum Kongresi, 73-80. -1985. Depositional history of Miocene Sediments on the NW flank of the Adana Basin. Proceedings of the Sixth Colloquium on Geology of the Aegean region, izmir, 185-208, (In Turkish). - 1992. A tectonically controlled alluvial fan which developedinto a marinefan -delta at a complex triplejunction: Miocene Gildirli Formation of theAdana Basin, Turkey. Sedimentary Geology, 81, ’t t t 241-252. GURBUZ,K. 1993. Sedimentology of the Cingoz and GiiuenG Formations of the Adana Basin, SE Turkey. PhD thesis, University of Keele. Fig. 13. Upper Miocene evolution of the southern part of the KELLING,G., GOKCEN,S.L., FLOYD,P.A. & GOKCEN,N. 1987. Neogene Adana Basin. (a) Uplift in the Misis structural high causes erosion tectonics and plate convergence in the eastern Mediterranean: new data of megasequence 2 prior to the deposition of megasequence 3 in from southern Turkey. Geology, 15, 425-429. Tortonian to Messinian times. (b) Regional uplift to the north of the KIRK,H.M. 1935. Seyhari Bolgesinin ilk jeolojietiidleri. MTARaporu, Ankara (Yayimlamnami?), 219. basin generates a south dip on all basinal sequences to give the ROBERTSON,A.H.F. & DIXON,J.E. 1984. Introduction: aspects of the present day geometry of the basin fill. geological evolution of theEastern Mediterranean. In: DIXON,J.E. & ROBERTSON,A.H.F. (eds) The Geological Evolution of the Eastern Mediterranean. Geological Society London, Special Publications, 17, syntectonicsedimentation effects in seismic profiles. 1-14. Megasequence 2 represents the major component of basin SCHMIDT,G.C. 1961. Stratigraphicnomenclature for the Adana region filling. Field studies show that it exhibits a shoaling-upward petroleum district VII. Petroleum Administration Bulletin, Ankara, 6, 47-63 pattern of fill (Giirbiiz 1993) and its seismic character SENGOR,A.M.C. 1980. Tiirkiye’nin neotektoniginin esaslari. Turk.Jeol. indicates an aggradationalsequence consistent with the Kiiriim. Konferans Series, 2, 40. passive infill of an underfilled foreland basin (Fig. 12c) - & YILMAZ,Y. 1981. Tethyanevolution of Turkey:a plate tectonic (Covey 1986). approach. Tectonophysics, 75, 181-241. -, GORUR,N. & SARO~LU,F. 1985. Strike-slip faulting and related basin Mid- tolate Mioceneextensional faulting on NW-SE formation in zones of tectonic escape: Turkey as acase study. In: BIDDLE, faults was synchronous with movement onthe sinistral K.S. & CHRISTIE-BLICK,N. (eds) Strike-slipDeformation, Basin Imamoglou fault zone and these faults dissected the basin Formation and Deformation. Society Economic Paleontologists and fill. This fault activity was essentially post megasequence 2 in Mineralogists Special Publication, 37, 227-264. TERNEK,Z. 1957. Adana Basen’i Alt Nhyosen (Burdigaliyen) Formasyonlari timing. Broad scale folding of megasequence 2 on NW-SE ve diger formasyonlarla iliskisi ve petrol olanaklari. Mineral Research and and N-S axes took place prior to the erosional effects of the Exploration Institute Bulletin, Ankara. 49, 60-80. base megasequence 3 boundary. UNLUCENC,U.C. 1993. Structural and stratigraphic evolution of the Adana Fieldwork has shown that megasequence 3 is composed Basin, SE Turkey. PhD thesis, University of Keele. - & DEMIRKOL.C. 1991. Karsanti-Akdam-Egner(K-KD Adana) of fluvio-deltaic sediments predominantly supplied from the Dolaylarininstratigrafik incelenmesi. In: YETIS,C. (ed.) AhmetAcar northeast (Unliigenq 1993) and these are possibly rep- Jeolojisi Simpozyumu, Adana, 239-254. resented by progradational sequences on the seismic line of YALQN,N.M. & GORUR,N. 1984. Sedimentological evolution of the Adana Fig. 3. Erosional truncation of megasequence 2 on structural Basin. In: TEKELI,0. AND GONCUOGLU,M.C. (eds) Proceedings of the highs prior to the deposition of megasequence 3 sediments International Symposium on the Geology of Taurus Belt. Ankara, 165-172. accounts forthe geometriesshown onthe isochronmap YETIS, T. & DEMIRKOL, C.1966. Adana Baseni Bati kesiminin detay Jeoloji (Fig. 9). This uplift is localized in the south of the basin and etiidii. MTA Raporu, Ankara, 8037.

Received 6 October 1993; revised typescript accepted 28 December 1994.

Downloaded from http://pubs.geoscienceworld.org/jgs/article-pdf/152/5/873/4890413/gsjgs.152.5.0873.pdf by guest on 02 October 2021