Sedimentary Properties of the Middle−Upper Eocene Formations in Çardak, Burdur and İncesu, SW Turkey

EZHER TOKER1,*, M. SERKAN AKKİRAZ2, FUZULİ YAĞMURLU3, FUNDA AKGÜN4 & SEFER ÖRÇEN5

1 Pamukkale University, Department of Geological Engineering, Kınıklı, TR−20020 Denizli, Turkey (E-mail: [email protected]) 2 Dumlupınar University, Department of Geological Engineering, Merkez Yerleşke, Tavşanlı Yolu, TR−43100 Kütahya, Turkey 3 Süleyman Demirel University, Department of Geololgical Engineering, Çünür, TR−32260 Isparta, Turkey 4 Dokuz Eylül University, Department of Geological Engineering, Tınaztepe, Buca, TR−35160 İzmir, Turkey 5 Yüzüncü Yıl University, Department of Geological Engineering, TR−65080 Van, Turkey

Received 04 September 2009; revised typescripts received 30 April 2010, 02 June 2010, 06 January 2011, 18 April 2011 & 04 May 2011; accepted 31 May 2011

Abstract: Th e integration of sedimentological, palynological and palaeontological data in three diff erent outcrops in SW Turkey provides a clearer understanding of the palaeoenvironments in an area between the Çardak-Dazkırı Basin and the Isparta region during the Middle–Late Eocene. In this study, the Çardak-Dazkırı (Başçeşme Formation), Burdur (Varsakyayla Formation) and Isparta (Kayıköy Formation) areas have been studied for facies and facies associations. Th ese formations contain alluvial fan, fan delta, shelf and related marine deposits. Detailed fi eld observations allowed 34 lithofacies and 10 facies associations to be identifi ed. Th e palynomorph assemblages in the Başçeşme and Varsakyayla formations contain biostratigraphically important taxa such as Aglaoreidia cyclops, Triatriopollenites excelsus, Plicatopollis lunatus, Subtriporopollenites constans and Subtriporopollenites anulatus ssp. nanus. Th e mangrove and back mangrove elements such as Psilatricolporites crassus and Spinizoncolpites sp. also occur in these palynomorph assemblages. Th e upper parts of the Başçeşme and Varsakyayla formations, which oft en exhibit reef developments, contain an assemblage of orthophragmines (Discocyclina sp.), nummulitids (Nummulites sp., Assilina sp., Heterostegina sp., Operculina sp.) and other benthic taxa (Halkyardia sp., Fabiania sp., Asterigerina sp., and Sphaerogypsina sp.). Th ese assemblages indicate shallow benthic zones 18-20 (SBZ 18-20). Th e absence of foraminifera in the Kayıköy Formation does not allow a precise age of the unit to be determined. However, the occurrence of some planktonic foraminifera (Globigerinidae) and the presence of clastic sediments suggest a marine environment with turbidity currents. Th e lateral and vertical relations of the Başçeşme, Varsakyayla and Kayıköy formations suggest a marine transgression from west to east in SW Anatolia during the late Middle Eocene–Late Eocene.

Key Words: facies analysis, palynology, benthic foraminifera, Eocene deposits, western Taurides

Çardak, Burdur ve İncesu Havzalarında Orta−Üst Eosen Birimlerinin Sedimanter Özellikleri, GB Türkiye

Özet: GB Anadolu’da, Orta–Geç Eosen boyunca Çardak-Dazkırı ve Isparta arasında yüzlek veren üç farklı istifi n paleoortamları, sedimantolojik, palinolojik ve paleontolojik verilerinin bütünlüğü ile daha iyi anlaşılabilmektedir. Bu çalışmada, Çardak-Dazkırı (Başçeşme Formasyonu), Burdur (Varsakyayla Formasyonu) ve Isparta (Kayıköy Fomasyonu) alanlarına ait birimlerin fasiyes ve fasiyes ilişkileri çalışılmıştır. Çalışma alanına ait tüm istifl er, alüvyal yelpaze, yelpaze deltası, şelf ve denizel ortamı yansıtmaktadır. Ayrınıtlı yapılan arazi gözlemlerine göre, 34 litofasiyes ve 10 fasiyes birliği tanımlanmıştır. Başçeşme ve Varsakyayla formasyonlarında bulunan palinomorf birliği, biyostatigrafi k önemi olan Aglaoreidia cyclops, Triatriopollenites excelsus, Plicatopollis lunatus, Subtriporopollenites constans and Subtriporopollenites anulatus ssp. nanus, ve mangrov ve mangrove-gerisi ortamı karakterize eden Psilatricolporites crassus ve Spinizoncolpites sp. ile temsil edilir. Genellikle resif gelişiminin yaygın olarak görüldüğü Başçeşme ve Varsakyayla formasyonlarının üst kesimleri, zengin ve çeşitli orthophragmines (Discocyclina sp.), nummulitids (Nummulites sp., Assilina sp., Heterostegina sp., Operculina sp.) and diğer bentik foraminifer grupları (Halkyardia sp., Fabiania sp., Asterigerina sp., and Sphaerogypsina sp.) içermektedir. SBZ 18-20 (SBZ 18-20) sığ bentik zonlarını temsil eden bu topluluklar, denizel ortam değişikliklerini anlamada önemli bir araçtır. Kayıköy Formasyonu foraminifer açısından çok fakir olduğundan dolayı ayrıntılı olarak yaşlandırılamamıştır. Ancak, planktik foraminiferlerden Globigerinidae içermesi, birimin

335 MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

açık şelf ortamında çökeldiğini göstermektedir. Diğer taraft an Kayıköy Formasyonuna ait istifi n başlıca kumtaşı-şeyl ardalanmasından oluşan kırıntılı tortul bileşimi ve içerdiği tortul yapılar, türbidit akıntıların geliştiği denizel ortamı yansıtması bakımından önemlidir. Bartonian–Priabonian yaşlı bu üç formasyona ait tortul istifl erin yanal ve düşey yönde gösterdikleri litofasiyes değişimleri, GB-Anadolu’da Geç Eosen dönemi boyunca batıdan doğuya doğru bir transgresyonun geliştiğini yansıtmaktadır.

Anahtar Sözcükler: fasiyes analizi, palinoloji, bentik foraminifer, Eosen çökelleri, Batı Toroslar

Introduction and foraminifera assemblages of these units that Th e Palaeocene–Eocene outcrops mark an important have been widely used in palaeoenvironmental event in the history of basins developed before the interpretations. neotectonic period, which is a known extensional tectonic regime in west Anatolia. During this time Geological Setting interval also occurred the main deformation and HP/ LT metamorphism of the Menderes Massif as a result Th e Middle–Upper Eocene outcrops are distributed of burial beneath the Lycian Nappes (Şengör & Yılmaz in the Çardak-Dazkırı (north of Acıgöl), Burdur 1981; Satır & Friedrichsen 1986; Bozkurt & Satır (north of Lake Burdur) and Isparta (İncesu and 2000; Bozkurt & Oberhänslı 2001; Sözbilir 2002). Th is Gönen towns) areas (Figures 1, 3, 4 & 6). Th ese basins Palaeocene–Eocene sedimentary succession rests are located in the Western Anatolia extensional unconformably on diff erent tectonostratigraphic province characterized by numerous NW–SE-, NE– suites, such as the Lycian Nappes (Özkaya 1991; SW-, E–W-trending basins (Koçyiğit 1984, 2005) and Şenel 1991; Collins & Robertson 1997, 1998, 1999), rest on the Mesozoic Lycian Nappes and ophiolites the Menderes Massif (Poisson 1976; Özkaya 1990, (Sözbilir 2005). 1991; Özer et al. 2001) and the Beydağları carbonate Th e Palaeocene–Eocene sedimentary assemblages platform (Özkaya 1991; Collins & Robertson 1998). of southwestern Anatolia are made up mainly of Th e initial phase of nappe emplacement occurred conglomerate, sandstone, turbiditic sandstone- during the latest Cretaceous (Collins & Robertson mudstone alternations, carbonaceous mudstone, 1998), aft er which sedimentary basins developed bioclastic limestone interbeds and, locally, limestone on top of the imbricated Lycian basement during blocks. Th e sedimentary features of these sedimentary the Late Palaeocene–Early Eocene (Şenel 1991). Th e constituents mainly indicate a supra-allochthonous basin fi ll comprises basal conglomerates with clasts basin type, which developed above the Lycian Nappe derived from the Lycian Nappes, bioclastic platform package (Sözbilir 2002). Th e supra-allochthonous limestones and clastic turbidites and is interpreted sediments are separated from the basement rocks by as a supra-allochthonous unit (Sözbilir et al. 2001; a regional unconformity (Sözbilir 2002). Sözbilir 2002), thought to represent a temporal Following Poisson et al. (2003) the tectonic restoration of a passive margin during relative evolution of the study area and its surroundings tectonic quiescence (Collins & Robertson 1998). can be divided into four main stages. Th ese are in In this study the Middle–Upper Eocene sequences ascending order; (1) closure of the Pamphylian stratigraphically overlying the Lycian Nappes are basin and emplacement of Antalya Nappes (Late represented by the Başçeşme and Varsakayayla Cretaceous–Early Palaeocene); (2) emplacement of formations, and the Kayıköy Formation on the Lycian Nappes (end of Eocene–Early Oligocene); Beydağları carbonate platform (Figures 1 & 2). (3) formation of the Oligocene molasse basins and Th e purpose of this paper is to provide a facies (4) opening of the Baklan and Acıgöl grabens under description and interpretation of the Middle– NW–SE and N–S extensional regimes. Upper Eocene Başçeşme, Varsakyayla and Kayıköy Deposition in the supra-allochthonous Eocene– formations, to identify the factors that controlled Oligocene marine basins in SW Anatolia, was their deposition and to describe the palynological controlled mainly by the emplacement of the Lycian

336 E. TOKER ET AL.

N Quaternary Menderes Massif Marine Miocene Homa Tertiary basins 3 Sultan Dağ 5 Bey Dağları Autochthon 1 Menderes Massif 4 Eğridir Denizli Antalya Nappes Isparta Alanya Massif Burdur Beyşehir Tavas 2 Hadım Nappes Lycian Nappes Lycian Nappes Muğla Seydişehir ophiolites Bodrum thrust fault

Kos Korkuteli Hadım Nappes Antalya Akseki Serik Hadım Göcek Fethiye Kemer Greater Caucasus Alanya Massif Bey Dağları EURASIAN Black Sea PLATE NCE Alanya ANOHTRATOLIAN PROVI NAFZ NEAFZ West Anatolian East Anatolian Kaş extensional contractional Fenike province ANATOLIAN province PLATE EAFZ .BG . Isparta Bitlis-Zagros Aegean Sea Suture Zone

Strabo Pliny Cyprus ARABIAN ndgaerit rc N MRndea A an Cyprean Arc Aege PLATE Mediterranian Sea 0 200 0 25km AFRICAN DSFZ Africa PLATE Km

Figure 1. Simplifi ed geological map of SW Turkey showing the study areas: (1) Çardak-Dazkırı, (2) Burdur, (3) İncesu, (4) İğdecik and (5) Gönen basins (modifi ed from Gutnic 1977; Akgün & Sözbilir 2001).

Nappes in the region at the time. However, the mainly Stratigraphy ophiolitic detrital constituents of the Başçeşme, In this study, our fi eld observations were focused Varsakyayla and Kayıköy formations indicate a on three diff erent locations, namely the Middle– Late Eocene synsedimentary emplacement of the Upper Eocene deposits cropping out in the Çardak- ophiolite assemblages of the Lycian Nappes. Th e Dazkırı (Başçeşme Formation), Burdur (Varsakyayla emplacement of the Lycian Nappes in SW Anatolia Formation) and İncesu (Kayıköy Formation) basins. continued until the end of the Late Miocene. Field Th e major geological characteristics of these Eocene observations in the Burdur and Isparta regions show that ophiolitic allochthonous units of the basins are briefl y described below. Lycian Nappes are overthrust on to Early Miocene (Aquitanian–Burdigalian) marine sedimentary units. Çardak-Dazkırı Basin Multiple overthrust systems of the Lycian Nappes on to the Beydagları autochthonous carbonate and Th e Çardak-Dazkırı basin is located north of the detrital units (Late Palaeocene to Early Miocene) Acıgöl Graben, mainly fi lled by Tertiary sedimentary suggest an anticlockwise rotation of the western side sequences and characterized by molasse type clastic of the Isparta Angle. Palaeomagnetic studies (Kissel deposits (Figure 1) (Koçyiğit 1984; Göktaş et al. 1989; et al. 1993; van Hinsbergen et al. 2010) indicated that Yağmurlu 1994; Akgün & Sözbilir 2001; Sözbilir the Lycian block on the western limb of the Isparta 2005). Th e Upper Eocene Başçeşme Formation, Angle rotated anticlockwise by about 40° since the exposed near Başçeşme village and fi rst named by Eocene. Furthermore, the palaeomagnetic data Göktaş et al. (1989), unconformably rests on the suggest that the dominant tensional forces in the Lycian Nappes (Figure 2) (Göktaş et al. 1989). Th e study area mainly trend NW–SE. formation is composed mainly of a fi ning-upward

337 MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

clastic sedimentary succession, which starts with pebble to cobble conglomerates at the base (Göktaş et LITHOLOGY al. 1989; Akkiraz 2008; Toker 2009; Toker et al. 2009). Vertically and laterally, these coarse conglomerates

AGE

GROUP display gradual transition to a monotonous alternation

FORMATION THICKNESS(m) of sandstone, mudstone with coal and reef carbonates (Göktaş et al. 1989; Akkiraz et al. 2006; Akkiraz 2008; gravel-sand-clay Toker 2009). Th is internal lithological variation is

alluvium

Quaternary divided into the following members: the reddish- clayey limestone claret Dazlak conglomerate; the Maden sandstone travertine and coaly mudstone and the Asar limestone with

650 corals, algae and benthic fragments (Figure 3b). Çameli mudstone-sandstone

Late Mid.Plio. conglomerate

sandstone-mudstone Burdur Basin

500 limestone Th e Burdur basin is located on the northwestern side Bozdağ of Lake Burdur and fi lled with Tertiary deposits which sandstone-mudstone are divided into supra-allochthonous sediments, the coal Acıgöl group and neo-autochthonous cover units reefal limestone (Yalçınkaya et al. 1986; Şenel 1997) (Figure 4). Th e

2000 Tokça sandstone-mudstone pre-Eocene basement comprises ophiolitic melange conglomerate and olisthostrome of the Lycian Nappes (Poisson conglomerate 1977). Th e Varsakyayla Formation from around Oligocene sandstone-mudstone Varsakyayla village, named by Poisson (1977), is well exposed in this area and is mainly made up of locally

Acıgöl 1500 reefal limestone

Hayrettin channellized conglomerates, planar cross-bedded coal sandstones, massive and locally coaly mudstones and bivalve and gastropod-bearing limestone (Akkiraz

200

Çardak conglomerate-sandstone 2008). Th e Varsakyayla Formation is linked with the ı Başçeşme Formation due to the similarities of their sandstone-mudstone sedimentary constituents. 300 conglomerate

Armutalan reefal limestone İncesu Basin Th e İncesu Basin is located in the apex of the sandstone-mudstone Isparta Angle and its deposits crop out around coal limestone Gönen town to the north of Isparta (Figure 7). Th e

800

Başçeşme Kayıköy Formation, named aft er Kayıköy village, sandstone-mudstone coal where it is well exposed (Karaman et al. 1989), is generally greyish and includes very poorly sorted

?Lutetian-Priabonian conglomerate-sandstone conglomerates, amalgamated sandstones with mudstone interbeds (Figures 13 & 14). Th e Kayıköy Formation is turbiditic and is composed mainly of Lycian clastics and carbonates sandstone and shale alternations and also contains

Mesozoic clayey and cherty interbeds and conglomerate not to scale intercalations dominantly of turbiditic origin. Th e Figure 2. Generalized lithostratigraphic columnar section of Middle–Late Eocene age of the formation is deduced the Çardak-Dazkırı basin (modifi ed from Şenel 1997; Sözbilir 2005). from its stratigraphic position (Figure 6).

338

E. TOKER ET AL.

Nappes

Lycian Formation Başçeşme Armutalanı Formation Kızılören Formation Kayaköy dolomite Karaova Formation Asar member Dazlak member Maden member normal fault strike-slip fault contact location of the measured sections (open circles shows beginning of the section) dip and strike of bed syncline axis sample locations 58

alluvium e Upper Eocen Upper

EXPLANATION Triassic Middle- Miocene Quaternary Lower Oligocene b N 500m Başçeşme village. Locations of measured sections are sections measured are of Başçeşme Locations village. 1014 24 0 Boztümbek tepe 22 18 Figure 9 Figure 28 18 Figure 8 Figure 65 54 52 65 26 40 48 35 55 54 56 58 30 48 62 40 55 Öküz tepe 59 37 20 33 47 56 1181 Dazlak tepe Detailed geological map of the studied area, north of north of area, the studied of map Detailed geological (b) a 100 m Çardak 0 Avdan Hayrettin Bozkurt Armutalanı Baklan Geological map of the Çardak-Dazkırı area. area. the Çardak-Dazkırı of Geological map Boğaziçi indicated. N Figure 3. (a) 3. Figure

339 MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

Facies and Facies Associations In this section, three Eocene formations have been TION LITHOLOGY analyzed in terms of their facies associations. Th ese AGE associations are based on the facies defi ned on

GROUP

FORMA logged stratigraphic sections and used palynological THICKNESS(m) data (Figures 8, 9, 11–14). Detailed descriptions of gravel-sand-clay the sedimentary features and palaeoenvironmental

alluvium interpretations of the facies and facies assemblages Quaternary are given in Tables 1–4, 7 & 8. Facies classifi cation mudstone-sandstone conglomerate of alluvial and fl uvial environments is aft er Miall

1500 (1978), who assigned gravel-bearing successions to Aksu coal G facies, while sandy and clay facies were assigned Aquitanian to S and F facies, respectively. Small letters following conglomerate-sandstone-mudstone reefal limestone the capital letter indicate the textural and structural reefal limestone 150 coal characteristic of each facies. Kavak reefal limestone

conglomerate Başçeşme Formation sandstone-mudstone Th e Başçeşme Formation is well-exposed on the north recristalized limestone western margin of the Acıgöl Graben (Figure 3a). Two outcrop sections have been logged (Figure 3b), one of which is located northeast of Öküz Tepe, while

Acıgöl

Oligocene Ardıçlı recrystalized limestone the other is southwest of Boztümbek Tepe (Figure 1000-1500 3b). Th e Öküztepe section is up to approximately conglomerate 240 metres thick and extends laterally over a few sandstone-mudstone kilometres (Figure 8), while the Boztümbek section is approximately 360 metres thick (Figure 9). In sedimentary logs, fi ft een lithofacies have been defi ned sandstone-mudstone based on type of individual beds, grain size, primary

150 sedimentary structures and fossil contents (Table 1). Saraycık Field photos also illustrate some of the lithofacies reefal limestone features of the Başçeşme Formation (Figure 10). Th is lithofacies diversity was grouped into three sandstone-mudstone-limestone main facies associations: FA1 to FA3 (Table 2). FA1 correlates with the coarse-grained Dazlak Member,

270 FA2 correlates with the fi ner-grained Maden Member

Varsakyayla limestone and FA3 correlates with the carbonate Asar Member (Figures 8 & 9).

?Lutetian-Priabonian sandstone-mudstone Alluvial Fan Deposits (FA1): Description – Th e coal alluvial fan facies association is characterized by the relative abundance of facies Gmm, Gp, Sg, Sp, Lycian clastics and carbonates St, Shs (Table 1; Figures 8 & 9). Th e FA1 is generally

Mesozoic made up of conglomerates intercalated with pebbly not to scale sandstones. Th is polygenetic conglomeratic facies Figure 4. Generalized lithostratigraphic columnar section of the association is commonly reddish and brownish, Burdur basin (modifi ed from Yalçınkaya et al. 1986; pebble to cobble grain size, thick bedded to massive, Şenel 1997). poorly-sorted, matrix-supported, with erosive

340 E. TOKER ET AL. N b 40 43 42 48 İnekboğazlayan hill sample location Dede hill 54 18 47 40 location of the measured section (open circle shows beginning of the section) strike and dip of bed 04YC/01-05 ated. Figure 11 Figure Dolmaşa tepe Ardıçlı 1792 Oligocene Formation Detailed geological map of the northern side of the northern side of of map Detailed geological (b) Kulfa taşı 1643 1591 Formation Varsakyayla Middle-Upper Eocene 500m 1769 Lycian Nappes Lycian Çataltaş Tepe Upper Cretaceous 0

Acıgöl Group N KEÇİBORLU Senir

_ + sediments

studied area Lycian Nappes contact uncharacterised fault alluvium

ed from Şenel 1997b). See Figure 1 for location. location. Şenel 1997b). Seeed from 1 for Figure Saraycık Formation Miocene - Pliocene Ardıçlı Formation Varsakyayla Formation Delikarkası Formation Oligocene Akdağ Kara tepe EXPLANATIONS Aydoğmuş Quaternary Middle- Cretaceous Upper Eocene Kaplanlı Ardıçlı 01 km 01 Yeşilçat Göktepe Saraycık LAKE BURDUR Çamlı İlyas Dikilitaş tepe Beltarla Sarıköy Yelalan Oyuklutekke Ovacık Akkoyunlu Kızıl dere Geological map of the northern part of Lake Burdur (modifi the Lake northern of partBurdur of Geological map Yukarıcimbili village (north of Lake Burdur). Location of measured sections, geological sections and sample locations are indic are locations sample sections and sections, geological measured of Location Lake (north Burdur). of village Yukarıcimbili Afyon Çevlik ANTALYA Figure 5b Figure Başmakcı 50 km Mediterranean 0 Değirmen dere a BAŞMAKÇI Figure 5. (a) 5. Figure

341 MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

TION LITHOLOGY LITHOLOGY

AGE AGE

SERIES SERIES

FORMA FORMATION

THICKNESS(m) THICKNESS(m)

gravel-sand-clay conglomerate

gravel-sand-clay trachy-andesite

Pliocene-Quaternary

conglomerate sandstone-mudstone sandstone-mudstone

Lower-Middle Miocene Lower-Middle

850

İncesu limestone limestone

“Middle” Oligocene conglomerate coal

Barladağ Lycian nap. Lycian sandstone-mudstone

Lower -

850

İncesu coal coal conglomerate

“Middle” Oligocene sandstone-mudstone coal

Lower - neritic limestones

conglomerate 230 sandstone-mudstone Delikaras

conglomerate limestone sandstone-mudstone blocks of neritic and pelagic coal

100-200

Barladağ series

Kayıköy limestones coal conglomerate-sandstone- mudstone alternation

Kayıköy pelagic limestones 1000 coal coal Palaeocene-Eocene neritic and hemipelagic

Kırladağları series

20-70

Palaeocene-Eocene limestones,vsandstone,vmarl neritic and hemipelagic limestones Isparta series pelagic limestones Kırladağları series Isparta series

(Beydağları autochthon) Cretaceous

Mesozoic (Beydağları autochthon) not to scale not to scale

Figure 6. Generalized lithostratigraphic columnar sections of the İncesu Area, (a) Around İncesu Village. (b) Around İğdecik, Gümüşgün villages, and Gönen and Atabey towns. See Figure 7 for location (modified from Gutnic 1977; Görmüş & Özkul 1995;Yağmurlu 1994).

342 E. TOKER ET AL.

fault thrust fault

measured sections study area İncesu Formation Miocene sediments Delikarkası Formation alluvium Lycian Nappes Lycian Antalya Nappes Kırdağları series Isparta series volcanics Barladağ series Kayıköy Formation

Autochthon Oligocene

ğları Bey Da Bey ” “Middle

EXPLANATIONS Lower- Middle Eocene Plio- Quaternary Quaternary N 1km 0 Afyon Atabey ANTALYA İslamköy 50 km Mediterranean Delikarkası hill 0 Yassıviran Gök tepe 1989 Tınaz tepe 2447 Kapıdağ Gönen Kömürlük Figure 12 ed from Gutnic 1977; Yağmurlu 1994 ). 1977; Yağmurlu Gutnic ed from İğdecik Figure 13 İleğidağ Tepelce Güneykent Göktepe ed geological map of north Gönen Town (modifi northTown Gönen of map ed geological Keçiborlu Simplifi Figure 14 Çapalı İncesu Figure 7.

343 MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

Table 1. Description and environmental interpretation for the lithofacies in the Başçeşme Formation.

Facies Description Interpretation

granule to cobble size, massive, matrix-supported, chaotic, pebbles are rounded to Gmm; massive sub-rounded, poorly sorted to unsorted, generally erosive basement, irregular top, debris-fl ow deposits conglomerates reddish-claret coloured, locally contains sandstones; dimensions: bed thickness up to 10 m, lateral extent: tens to hundred metres, commonly intercalated with facies Sb,Sr

granule to pebble size clast supported by coarse sandy matrix, subangular and poorly Gp; panar cross- sorted clasts, sand lenses, generally fi ning upward with erosive base, planar cross channel fi ll bedded conglomerates bedded, channel fi ll occurs, reddish-brown coloured; dimensions: bed thickness up to 4 m, lateral extent: few ten metres; intercalated with facies Sr

granule to pebble size clasts supported by sandy matrix, poorly sorted, poorly bedded, Gms, matrix- few crudely developed normal to inverse grading,yellowish red coloured,angular debris fl ow to hyper-concentrated supported gravelstone to subangular clasts; dimensions: bed thickness up to 6 m, lateral extent: few tens fl ow deposits metres, intercalated with facies Sb, Sl,Fl and C

granule to coarse-grained sandstones, poorly sorted and rounded, cross-laminated, Sg, gravelly deposits from sand-dominated channel-fi lls, reddish coloured, dimensions; bed thickness up to 20 cm, laterally sandstones chanellized fl ows extent: few metres, intercalated with facies Gmm, Gp

medium- to fi ne-grained sandstone, moderately sorted, horizontally stratifi ed Shs, horizontally bioturbated, locally ripple laminations on top, locally hematite concretions bearing, planar bed fl ow, upper fl ow regime stratifi ed sandstones reddish-yellowish red coloured; dimensions: bed thickness up to 30 cm, laterally extent: few tens of metres, intercalated with facies Gms,Sg

medium- to fi ne-grained sandstone, generally parallel laminated at the bottom and subaqeous deposits at lower fl ow Sr, rippled sandstones ripples at the top of bed, lenses with mud, greyish red coloured; dimensions: bed regime thickness up to 20 cm, lateral extent: few metres, intercalated with facies Sp, Gmm

medium- to fi ne-grained sandstone, moderately sorted, massive bedding, planar Sp, planar cross- cross-stratifi ed, yellowish red coloured, dimensions: bed thickness up to 25cm, lower fl ow regime, sand waves stratifi ed sandstones laterally extent few of metres, intercalated with facies Gmm, Gh

medium- to fi ne-grained sandstone, moderately sorted, normal graded, greyish Sm, massive rapid sedimentation, sediment red coloured; dimensions: bed thickness up to 35 cm; lateral extent: a few metres; sandstones gravity fl ow intercalated with facies Gh, Fm

medium- to coarse-grained sandstone, moderately sorted, planar cross-stratifi ed, Sf, fosilliferous corals, gastropods and bivalves-bearing, greyish red coloured; dimensions: bed decreasing current velocity sandstones thickness up to 60 cm; lateral extent: a few tens of metres; intercalated with facies Fm

medium- to coarse-grained sandstone, massive bedding, calcareous sandstone, Sc, calcareous yellow coloured; dimensions: bed thickness up to 5 m; lateral extent: a few metres; edge of bank platform and shelf sandstones intercalated with facies Sf, Lr

Sandy limestone with bioclast, grainstone, fl at bedded, coarse grain size, fossil sporadic storms and currents Ls, sandy limestone fragments such as bivalves, benthic foraminifers, yellowish grey coloured; dimensions: across reef, relatively low wave and bed thickness up to 5 m; lateral extent: a few metres; intercalated with facies Lr current energy

mudstone, laminated, medium- to coarse-grained sandstone, massive bedding, Fm, massive suspension sediments, overbank greyish yellow coloured; dimensions: bed thickness up to 50 cm; lateral extent: a few mudstone deposits, waning currents metres; intercalated with facies Sg, Sf

reefal limestone, fl at bedding, mixing of coarse skeletal fragments such as corals, bivalves, benthic foraminifers and algal mounds, abundant milliolid association, low energy, sporadic currents and Lr, reefal limestones greyish yellow coloured; dimensions: bed thickness up to 10 m; lateral extent: a few quiescent shallow water tens of metres; intercalated with facies Sc

coal, horizontally laminated, dark brown-black coloured, abundant plant fragments; subaerial low energy, channel C, coal-coally dimensions: bed thickness up to 40 cm; lateral extent: a few tens of metres; overbanks, vegetated swamps mudstone intercalated with facies Sm, Fm deposits and marsh, coastal plain

344 E. TOKER ET AL.

Struct. Struct. LITHO.

ed. Struct. Fm. Struct.

Age

Color Loc. Bed.

Mem. Fm. L.B.S.

Age

Color Loc. B

Mem. LITHOL. LITHOLOGY L.B.S. m 9 Sm LIT. ed. 11

Fm. 7 560 Fm.

Age Color Loc. Coord: 25342/94691 B

Age

Color

Mem. Loc. Bed. L.B.S. Sm 19 CFm Mem. L.B.S. m m 11 A22 4 370 7 7 CSm A21 Ls (F f l e h S 180 Gmm 11 C A20 4 Fm 555 7 m 2 A19 9 Sm 600 A18 A17 365 1 175 Gp 11 C A16 2 550 5 2 4 Sf 5 Sm 595 A15 Lr 170 360 A14

A13 A3) 5 Sf 545 ASAR x A12 1 590 A11 1 11 Fm A10 355 5 C A9

165 UPPER EOCENE

11 A8 Lr F a n D e l t a / D e l t a F r o n t (F t n o r F a t l e D / a t l e D n a F 2 Gmm C 540 A7 585 A6 A5 5 9 Gp A4 160 350 Sm A3 535 BAŞÇEŞME A2 580 10 A1 1 5 Sm 155 345 530 1 Sp 12 5 575 6 Fm 5 5 150 340 1 Fm Sf 5 Sp 525 Sm

1 MADEN Sm 570 7

2 Gp (F t n o r F a t l e D / a t l e D n a F 5 145 335 Fm 3 Sg 5 11 11 6 2 520 1 C 6 2 Sm 1 C 565 Fm Gp 5 1 9

Fm MID.-?UPPER EOCENE 140 330 5 1 Sm 9 Sm 5 Sm 515 L M FMC G P C B 5 Sand 3 Gms 135 5 325 4 Sm 510 EXPLANATIONS 5 Gmm 4 130 320 3 5 Sp 7 505 Fm coarse conglomerate Sm 125 5 315 7 3 Sand 505 Sm medium conglomerate

MADEN 7 5 Gp 310 BAŞÇEŞME 3 Sm 120 1 fine conglomerate 495

MIDDLE-?UPPER EOCENE 11 11 C 7 Sg 305 C 4 3 pebbly coarse sandstone 115 Gp Gms 7 Sg 490 6 Fm 7 Gp 300 3 Fm coarse sandstone 110 485 295 1 pebbly sandstone Sg Sm Sf 105 7 (F n a F l a i v u l A 6 480 290 9 Fm sandstone

MADEN

BAŞÇEŞME

100 DAZLAK 7

BAŞÇEŞME 7 Sg 6 Gms 475 7 Gp 285 mudstone 7 Sg MIDDLE-?UPPER EOCENE Sm 95 MIDDLE-?UPPER EOCENE 7 11 9 7 Gp 1 C 470 sandy limestone 7 Fm 280 3 7 9 Gms limestone 90 11 7 Sg 465 1 C 275 coal 7 1 Fm 85 7 460 270 Sr covered 7 1 Sm

80 1 Sm A2) 1 455 11 Gp 265 1 9 Fm coral Sg 9 Sm 75 1 Sr 450 9 Gp benthic foraminifer 260 9 Fm 9 Sm 70 2 7 Gp gastropod 445 3 255 3 1 Sm Fm bioclast 65 7 Sp 11 C 440 bivalve 7 250 4 3 Sm 11 C channel fill 60 4 435 Sm 4 Sf planar bedding 7 Gp 245

55 (F n a F l a i v u l A 430 Fm cross lamination 1 6 Gmm 4 240 4 Gms bioturbation

5 Sg A1) 4 50 Gp 425 4 Fm A2) 4 Sm hematite concretions 5 235 6 11 C 1 Gp Sm 45 420 1 fractured 1 230 6 4 Gp 7 3 Gp erosive 40 415 7 6 2 Sm gradational Sg 225 6 Gp 7 4 Fm sharp 35 7 410 massive bedding 220 7 Sp flat bedding 4 Sm 30 6 Shs 405

DAZLAK 10 215 BAŞÇEŞME 4 Fm coarsening upward 25 1 400 4 Sm fining upward 7 210 MIDDLE-?UPPER EOCENE Gp 11 C 7 2 Sf 20 Gp Gp 395 7 5 1 grey 205 Sm 2 greyish yellow 7 Sg 1 Sm 15 6 Sp 390 greyish green 7 1 3

Gmm A1) 200 7 greyish red 5 6 1 4 10 7 Sg Gp 385 1 yellow 1 5 195 Ls 7 Gp 6 Sm 6 yellowish red 5 7 380 11 C red Sg 6 7 7 190 Fm green Gmm Sm 9 6 cream L M FMC G P C B L M FMC G P C B L M FMC G P C B 10 Sand Sand Sand 11 black

Figure 8. Measured section of the Başçeşme Formation northeast of Öküztepe. See Figure 3b for location.

345 MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

Structures Structures Structures LITHO.

Fm. LITHO. LITHOLOGY Age

Color

Mem.

Loc. m L.B.S. Bed.

Fm.

Age

Fm.

Age

Color

Mem.

Color

Mem.

Loc. Bed.

Loc. L.B.S. Bed. L.B.S. 360 A/52 Lr 4 C 10 m Sp 130 4 5 Sm 10 A/51 m 355 Lr 260 10

125 t (FA-2) n a F a t l e D 5 Fm 350 6 Sp 255

120 7 7 345 7 250 Sm 5 Gp 11 115 2 1 11 340 5 Sf 245 7 110 MADEN MEMBER 5 5 Sf 7 Gp 335 240 TION 4 Sm

105 (FA-2) t n o r F a t l e D / a t l e D 4 Fm 330 235 5 Sm 4 Fm Sm 5 100 Fm 4 325 230 7 5 Sf Coastal /Shel f (FA-3)

TION

95 BAŞÇEŞME FORMA 5 Sm 5 Sm

MIDDLE - ?UPPER EOCENE 320 7 Gp 225 5 Gp 90 7 5 Sm 5 315 220 5

ASAR MEMER 85 UPPER EOCENE

BAŞÇEŞME FORMA Sm 11 5 TION 4 C Gmm 310 215 Sm 7 5 Gp 80 2 Sm 305 210 Sm Gmm 2 Fm 5 75

MADEN MEMBER

MIDDLE - ?UPPER EOCENE 9 Sm 300 7 Sp 205

BAŞÇEŞME FORMA 9 Sf 70 7 Gp 9 Fm 5 295 200

65 (FA-1) n a F l a i v u l A Sc 290 7 195 7 Gmm 60 5 285 190 55 7 Sp Sc 280 185

50 DAZLAK MEMBER 2 A/49-50 5 Sc

275 Fan(FA-2) Delta 180

45 270 5 Gp 175

7 MADEN MEM. 5 Sm Gp M.- ? IPPER EOC. 7 4 7 170 Sm L M F M C G P C B 7 Gp Sand 35 7 4 Sm 1 St EXPLANATIONS 165 5 7 Gp 7 Gp coarse conglomerate 30 coral Sp medium conglomerate 7 160 benthic foraminifer Shs fine conglomerate 25 2 gastropod 7 Gmm coarse sandstone bioclast 155 bivalve calcerous sandstone 20 channel fill 7 sandstone planar bedding Sm 150 trough cross-bedding 15 mudstone fractured limestone erosive 7 145 2 Fm gradational 7 Sp 10 coal sharp 7 Gmm covered massive bedding 140 1 grey flat bedding 5 2 imbrication 7 4 Sm greyish yellow Gmm 4 greyish red fining upward 135 5 yellow 4 Fm coarsening upward 6 yellowish red L M F M C G P C B L M F M C G P C B Sand Sand 7 red 9 green 10 cream 11 black Figure 9. Measured section of the Başçeşme Formation south of Boztümbek Tepe. See Figure 3b for location.

346 E. TOKER ET AL.

Table 2. Facies associations of the Başçeşme Formation.

Facies Associations Constituent Lithofacies

FA1, alluvial fan facies associations Gmm, Gp, Sg, Sp, Sm, Shs

FA2, fan-delta/delta front facies associations Gms, Shs, Sr, Sm, Sf, Ls, Fm, C

FA3, shelf facies associations Gp, Sm, Sf, Sc, Ls, Lr

a b

c d

e Figure 10. Field photographs of (a) bioturbation traces in the Dazlak member (b) bivalves, gastropods and bioclasts in the Maden member, (c) coral colony and gastropods in the Maden member, (d) coal lens in the Maden member, (e) coal seams in the Maden member. White arrows indicate the scale of the photos. Pencil is ~15cm long; Lens cap is ~50mm in diameter.

347 MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

bases and irregular tops, generally structureless and are characteristic syn-sedimentary structures and chaotically organized, with sub-rounded to rounded occur at various stratigraphic levels (facies Shs, clasts (Facies Gmm) (Figures 8 & 9). Th ey can be Sr and Sm) and fragments of fossils such as corals, traced laterally for up to a hundred metres. Th e most gastropods and bivalves were also observed in FA2 common clast components are black dolomites, (facies Sf) (Figure 9). Coarsening-upwards sequences serpentinites, and ophiolitic fragments that are were commonly observed in this facies association. most probably derived from the Lycian Nappes. Th e Th e mudstone and coal are intercalated with massive cross-bedded conglomerates are compositionally sandstones (facies Sm) (Figure 8). Intercalation of the same as the massive conglomerates (Gmm), debris fl ow facies such as Gmm and Sp indicates an but diff er in exhibiting planar cross-bedding (facies interfi ngering relationship with FA1. Gp) (Figure 9). Clasts within the conglomerate are Interpretation – Th e sand-dominated FA2 facies poorly-sorted, within a coarse-grained matrix. Th e association was probably deposited in a delta setting coarse-grained gravelly sandstones (facies Sg) are at the toe of FA1 where the alluvial fan system is commonly observed as interbeds in conglomerates continuous through to a fan delta system. Th is facies and are poorly sorted and cross-laminated (Figures association concordantly overlies the alluvial fan 8 & 9). Planar cross-stratifi ed sandstones and trough sediments (FA1). Coal layers represent quiescent cross-bedded sandstones (facies Sp, St) were also subaerial conditions and the massive, laminated observed in massive conglomerates. Horizontally mudstone with shell fragments indicates an alluvial stratifi ed bioturbated sandstones (facies Shs) consist swamp environment. of medium–fi ne-grained sandstones with hematite Shelf Deposits (FA3): Description – Th e shelf facies concretions and locally ripple laminations on top association is composed of Sf, Sc, Ls, Lr facies varieties (Figure 9). (Tables 1 & 2; Figures 8 & 9). Th e sandstones mostly Interpretation – Th e abundance of matrix- consist of gastropod, bivalve- and bioclast-bearing supported, massive to thick bedded, and scarcity of fossiliferous sandstones and calcareous sandstones internal structures in reddish conglomerates and (facies Sc and Sf). Sandy limestones with benthic sandstone beds of the FA1 indicate mainly debris foraminifera and bivalves and reef limestones were fl ow processes of alluvial fan deposition (Reineck & observed at the top of FA3. Th e lateral extent of these Singh 1975; Miall 1996). Th e clasts are polygenetic facies usually exceeds tens of metres. and derived from basement metamorphic rocks by Interpretation – Th e FA3 facies was probably dominantly cohesive and stream debris fl ow (Nemec deposited in a lagoon and shelf environment and is & Steel 1984; Göktaş et al. 1989; Nemec & Postma characterized dominantly by sandy limestone and 1993; Blair 1999; Sözbilir 2002). All these facies of FA1 reef limestone. Th is facies association overlies fan suggest deposition in an alluvial fan setting in front of delta sediments (FA2). Th e calcareous sandstone high ground fed from a Lycian Nappes source area. In (facies Sc) commonly occurs near the seaward edge the upper parts of the fan (facies Gmm, Gp, Sg, Sp), of the bank platform and shelf. Th e development with a steeper gradient, high energy fl ow dominated of this deposit requires sand-size sediments and a and thus, overbank deposits are rarely preserved. means of removing sediment smaller or larger than Generally, the FA1 facies association demonstrates a sand-size material. Th ese requirements coincide with fi ning upward sequence and laterally passes into fan wave action or strong tidal currents in an area of high deltaic conditions. carbonate production (Tucker & Wright 1990). Th e Fan-delta/Delta Front Deposits (FA2): Description sandy limestone represents open shelf environments – Th e Fan delta/delta front facies association is (facies Ls). Th e limestone contains corals, benthic composed of Gms, Shs, Sp, Sr, Sf, Sm, Ls, Fm, C foraminifera and bivalves typical of a shelf facies (Table 1; Figures 8 & 9). Th e grain size is environment. However, the presence of abundant highly variable, ranging from fi ne grained to gravel milliolid association in packstones indicates back- size. Horizontal lamination, ripples, planar cross- reef or lagoonal environmental conditions (Toker bedding, normal graded bedding, and bioturbations 2009).

348 E. TOKER ET AL.

Fossil Contents – Benthic foraminifera have been facies association is predominantly sandy facies identifi ed, particularly in the FA3 facies association comprising medium- to fi ne-grained, moderately of the Asar Member (Başçeşme Formation) (Figures sorted sandstones, interbedded with conglomerates 8 & 9). Th e Nummulites assemblage, including and thick-bedded mudstones. Planar cross Nummulites fabianii and Nummulites striatus, was bedding, ripple lamination, channel-fi lls, hematite identifi ed and in addition, Fabiania cassis, Eorupertia concretions, plant debris and bioclasts are common magna, Halkyardia minima, Spahaerogypsina globulus sedimentary structures in the sandstones, together Asterigerina rotula, Quinqueloculina sp., Asterigerina with sharp, sometimes erosive bases (facies Sp and sp., Discocyclina sp., Cibicides sp., Heterostegina sp., Sr). Th e conglomerates have interbeds of sandstones Eponides sp., Amphistegina sp., Alveolina sp., Assilina which are horizontally bedded, poorly sorted and are sp., Halkardia sp., Nummulites sp., Operculina sp., supported by a sandy, silty matrix. Clasts are rounded Praebulalveolina sp., Eorupertia sp., Fabiania sp., to well-rounded in the pebble to gravel range (facies Neoalveolina sp., Halkyardia sp., Anomalina sp., Gh). Th e clasts in the conglomerates are polygenetic Mississippina sp., Pararotalia sp., Pyrgo sp., Rotalia and mainly derived from ophiolites of the Lycian sp., Sakesaria sp. and Orbitolites sp., were recorded Nappes. Mudstones in the fl uvial facies are massive from reef limestones (Akkiraz et al. 2006; Akkiraz to thick bedded, have sharp contacts at base and top 2008). Th e nummulitids (Nummulites fabianii) and contain plant debris (facies Fm). Th e gravel and indicate Shallow Benthic Zonation (SBZ) 19 or 20 medium-sand-dominated units in this facies are (Less et al. 2008). Heterostegina sp., which is found mostly grey. in the Başçeşme Formation, occurs in SBZ 18-19 and indicates an upper Bartonian–Priabonian age (Özcan Interpretation – Th e sandy-muddy dominant facies et al. 2007). Furthermore, Fabiania cassis, Halkardia association (FA4) contains trough cross-bedding sp., Rotalia sp., Miliolids, coralline red algae, and fi ning-upward cycles indicating the dominance corals, gastropods and bivalves in these sections of fl uvial distributary system during deposition. of the Başçeşme Formation indicate a Bartonian– Th e sand and mud dominated facies assemblage is Priabonian age. In this part of the section, a shallow characterized by a very high proportion of fl oodplain shelf is indicated by the presence of Nummulites facies, with fewer channel-fi ll deposits (Nichols and towards deeper water, a distal-middle ramp is & Fisher 2007). Planar-cross bedding is produced indicated by orthophragminid assemblages (Bassi by the downstream migration of two dimensional 2005). bedforms (Harms et al. 1982). Overbank deposits are represented by thick-bedded, greyish mudstone. Fan Delta Deposits (FA5): Description – Th e Varsakyayla Formation fan delta facies association (FA5) is composed of Th e Varsakyayla Formation is well exposed southwest Gmm, Gh, Sm, Sp, Sf, Sc, Fm lithofacies (Table 3; of the Burdur Basin (Figure 5). One outcrop section Figure 11). Th e coarse-grained gravels in the FA5 has been logged through this formation (Figure facies association consist of matrix-supported, 11). Th e section is north of Yukarıcimbilli village weakly stratifi ed, massive, poorly sorted, rounded to and up to approximately 270 m thick (Figure 5a). subrounded pebble to cobble gravels, (facies Gmm) Sedimentary logs defi ned ten lithofacies based with horizontally bedded sandy, silty matrix-support, on types of individual beds, grain size, primary erosive bases and locally irregular tops (facies Gh). sedimentary structures and fossil contents (Table 3). Th e FA5 facies association is characterized by mostly Th e observed lithofacies diversity was classifi ed into sandy facies (facies Sm, Sp, Sf, Sc) which are medium three main facies associations: FA4, FA5 and FA6 to coarse grained, and moderately sorted. Planar (Table 4). A further fi ft een samples were analysed cross-bedding and locally channels are common palynologically (Table 7). sedimentary structures in the sandstones (facies Sp, Fluvial Deposits (FA4): Description – Th e Sm). Benthic shell fragments such as shallow water fl uvial facies association (FA4) includes Gh, Sm, gastropods and bivalves are abundant in this facies Sp, Sr, Fm facies varieties (Table 4; Figure 11). Th e association, and individual beds are bioturbated and

349 MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

Table 3. Description and environmental interpretation for the lithofacies in the Varsakyayla Formation.

Facies Description Interpretation

ganule to cobble size clast, silty, sandy and gravelly matrix-supported, massive and unstratifi ed, Gmm, massive poorly sorted rounded to subrounded, generally erosive basement, locally sand lenses, average debris dlow deposits conglomerates clasts size is up to 23 cm, grey-greyish yellow coloured; dimensions: bed thickness up to 4 m; lateral extent: few tens of metres; commonly intercalated with facies Sp, Sc, Lr

ganule to pebble size clasts, supported by sandy, silty matrix, horizontally bedded, rounded to debris fl ow to Gh, horizontally well rounded, erosive basement and some part irregular top, sand lenses are common, grey- hyper-concentrated bedded conglomerates greyish yellow coloured; dimensions: bed thickness up to 2 m; lateral extent: less than 10 metres; fl ow regime commonly intercalated with facies Sp, Lr

medium- to coarse-grained sandstone, moderately sorted, massive bedded, locally sand lenses, deposits from Sm, massive fractured, bioclasts, bioturbated, greyish coloured; dimensions: bed thickness up to 1–2 m; lower-concentrated sandstones lateral extent: few tens of metres intercalated with facies Sp, Sf fl ow regime

medium- to coarse-grained sandstone, pebbly, poorly sorted, sharp base, planar cross-bedded, Sp, planar cross- hematite concretions, some part channelized, greyish yellow coloured; dimensions: bed mid-channel sand stratifi ed sandstones thickness up to 50 cm; lateral extent: few tens metres; commonly intercalated with facies Gmm, bars Sm

medium- to coarse-grained sandstone, moderately sorted, sharp base, cross-stratifed, Sf, fosilliferous decreasing velociy of gastropods, bivalves bearing, fl at bedded, greyish cream coloured; dimensions: bed thickness sandstones water close to shelf up to1 m; lateral extent: tens of metres; intercalated with Fm

medium- to coarse-grained sandstone, moderately sorted, calcareously, fi ning upward, contains sporadic storms, Sc, calcareous shell fragments (benthic foraminifera, gastropods, bivalves etc.), sharp base and top, cream back-reef zone of sandstones coloured; dimensions: bed thickness up to 1 m; lateral extent: few tens of metres; intercalated land with Lr

medium- to fi ne-grained sandstone, moderately to well-sorted, sharp base, fi ning upward, fl at Sr, ripple-laminated subaqeous deposits at bedded, parallel laminated at base and rippled laminated on top, grey coloured; dimensions: bed sandstones lower fl ow regime thickness up to 60 cm; lateral extent: tens of metres; intercalated with Sm, Sp, Fm

lower fl ow regime, Fm, massive mudstone, massive, sharp at base and top, plant debris, greyish yellow coloured; dimensions: channel mudstone bed thickness up to 40 cm; lateral extent: tens of metres; intercalated with facies Sp, Sm overbank deposits

vegetated swamp C, coal-coally coal, carbonaceous mud, dark brown-black coloured, plant remains; dimensions: bed thickness deposits, low energy mudstone up to 20 cm; lateral extent: less than 10 metres; intercalated with facies Fm fl ow

limestone, included gastropods, bivalves, corals and algal mounds, cream coloured; dimensions: Lr, reefal limestone reef framework, shelf bed thickness up to 3 m; laterally extent: less than 10 meters; intercalated with Sc, Sh

Table 4. Facies associations of the Varsakyayla Formation.

Facies Associations Constituent Lithofacies FA4, fl uvial facies associations Gh, Sm, Sp, Sr, Fm FA5, fan delta facies associations Gmm, Gh, Sm, Sp, Sf, Sc, Fm, FA6, shallow shelf facies associations Gmm, Sp, Sc, Lr

350 E. TOKER ET AL.

Structures Structures LITHOLOGY LITHOL.

Age

Fm.

Age

Color

Fm.

Loc. Bed. Color L.B.S.

Loc. L.B.S. Bed. 04YC/13 Structures m m 10 04YC/12 120 245 LITHOL.

Age

Fm.

Loc. Bed. 04YC/11 Color L.B.S. 04YC/10 04YC/37-39 1 04YC/23 10 04YC/9 Lr Sr m 10 04YC/22 265 04YC/21 Coastal/Shelf(F 115 240 Lr 10 1 Sm 1 Sm

235 10 AYLA 110 04YC/8 260 1 Gmm 1 Sm

105 230 Sm

UPPER EOCENE 1 255 VARSAKY 1

Sm A-6) 1 04YC/20 10 04YC/19 100 225 04YC/18 Lr Lr 10 04YC/17 Sc 250 04YC/16 04YC/15 04YC/14 Sm L M F M C G P C B

1 (F a t l e D n a F 220

95 04YC/7 (F f l e h S / l a t s a o C Sand 10 04YC/6 1 Gmm 5 EXPLANATIONS 90 215 10 Gmm 2 Gh 1 coarse conglomerate 1 Gh 1 85 UPPER EOCENE 210 medium conglomerate 4 Gmm 2 1

80 205 1 1 Gh calcerous sandstone 1 1 Gh 04YC/27 Lr 1 04YC/26 75 200 pebbly sandstone 1 Gh 04YC/25 04YC/24 1 Sr 1 Sm sandstone 70 195 1 Sp 10 AYLA mudstone 1 Fm 65 AYLA 190 5 Sm Lr limestone

VARSAKY 04YC/31 Sc UPPER EOCENE 60 10 04YC/30 185 coral

VARSAKY A-5)

10 A-6) benthic foraminifer 10 55 Sf 180 algal mound 04/YC/36 50 175 gastropod 04/YC/35 1 Sm bioclast 10 Sc 45 170 04/YC/34 bivalve 1 04YC/29 04/YC/33 channel fill 1 Fm 40 165 bioturbation 1 Sm 04/YC/32 1 Fm 1 Sm 1 Gmm fractured 35 160 1 1 Sm 1 Fm hematite concretions F l u v i a l (FA-4)

F a n D e l t a (F 1 1 plant debris 30 1 155 Sp 1 Sm 1 Fm ripple lamination 5 Gmm 1 1 25 150 trough cross-bedding 1 Fm Sm 1 Sr erosive 1 Sm

20 MIDDLE - ? UPPER EOCENE 145 1 Sm gradational 04YC/05K 1 sharp Fm Sm 1 04YC/04K massive bedding 15 04YC/03K 140 flat bedding 1 Sm Sp Sm 1 fining upward 2 A-5) 10 135 1 Sc Fm 2 1 04/YC/33 productive sample

130 Sc 5 2 Sm 1 04YC/03K barren sample 04YC/02K 1 04YC/01K Fm 1 grey 1 04YC/28 Sp 1 Sm 0 1 125 1 Gmm 2 greyish yellow Sm 1 Sp 4 greyish red L M F M C G P C B L M F M C G P C B 5 Sand Sand yellow 10 cream Figure 11. Measured section of the Varsakyayla Formation north of Yukarıcimbili village. See Figure 3 for location.

351 MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

have sharp bases. Th e fi ner unit (facies Fm) present Palynological Contents – Five palynological in FA5 consists of massive to thick bedded mudstone, samples were collected from the clastic part of with grey plant fragments and bioturbation. the Varsakyayla Formation (Figure 5a). However, Interpretation – Th e FA5 facies association only two samples were suitable for palynological represents deposition in a deepening-upward fan- counting. Due to the low diversity and relative delta system in the Varsakyayla Formation. FA5 percentages of the species, 175 pollen grains in is probably deposited on a fan-delta front and fan- one sample and 164 pollen grains in the other one delta slope. Th e fan-delta front facies is characterized could be counted (Table 5). In total, 37 spore pollen by pebble to cobble conglomerates, sandstones in species were determined. Only two spore species, both channelized and nonchannelized horizontally Leiotriletes triangulus and Baculatisporites primarius bedded units. Fan-delta slope strata are dominated ssp. Oligocaenicus, were counted. Th e angiosperm by extensively bioturbated, locally cross-bedded, pollen average is always higher than that of spores coarse sandstones, overlain by sandstone/fossil and gymnosperm. Th e pollen species Plicatopollis conglomerate couplets (Figure 11). Th us, the fan- plicatus (~13%), Momipites punctatus (~10%) delta slope sandstones record deposition in shoreface Momipites quietus (8%), Tricolpopollenites retiformis to inner-shelf environments (Rigsby 1994). (15%) and Tricolpopollenites liblarensis (8%) had Shelf Deposits (FA6): Description – Th e shelf high percentages. Th e other angiosperms had facies association (FA6) is composed of Gmm, Sp, comparatively lower percentages (1–3%). Marine Sc, Lr facies (Table 3, Figure 11). Coarser-grained Cleistosphaeridium sp. and Cordosphaeridium sp., conglomerates are rarely preserved and their and undiff erentiated dinofl agellate cysts were also lateral extent is very limited in FA6 (facies Gmm). described from the samples (Table 5). Conglomerates with erosive bases are intercalated Th e characteristic Early Eocene taxa Normapolles, with sandstones. Th is facies association dominantly such as Basopollis, Interpollis and Urkutipollenites, do consists of creamy bioclastic limestone (facies Lr). not occur in the Varsakyayla Formation. According Th e bioclasts include foraminifera, algae, corals to Riegel et al. (1999), the variety of Normapolles is and bivalves and consist of beds of dense skeletal higher in the Early Eocene than in the Middle Eocene. limestone rich in miliolid foraminifera and coralline Normapolles were not recorded from the Middle– algae alternating with calcareous sandstones (facies ?Late Eocene coal occurrences of central Anatolia Lr, Sc). by Akyol (1980), Akgün (2002) and Akgün et al. Interpretation – Th e FA6 facies association was (2002). However, the species Plicatopollis lunatus, presumably deposited in a shelf environment. Th e Triatriopollenites excelsus, Subtriporopollenites calcareous sandstone with shell fragments was anulatus ssp. nanus and Compositoipollenites probably deposited in a back-reef sand facies (Figure rhizophorus ssp. Burghasungensis, generally observed 11) (Toomey 1981). All the features of the back- in Eocene sediments, were also identifi ed from the reef zone of land fringing platforms are strongly Varsakyayla Formation. infl uenced by the both water exchange between the open sea and infl ux of river water (Einsele 2000). Furthermore, the palynomorph content of the two Limestone composed of corals and algal mounds samples is similar to the palynomorph content of the is called bind stone or frame stone. Th e ratio of Maden member (Başçeşme Formation) previously organisms comprising the skeleton components of made by Akkiraz et al. (2006). In particular, the these limestones (facies Lr) exceeds 50%. Th e shelf mangrove species Psilatricolporites crassus (Pelliciera) facies association is characterized by the presence of is present in high percentages in the Maden member abundant shallow-marine fauna, as observed in the (upper part of the Başçeşme Formation) and also bioclastic limestone facies of the upper part of the occurs in the Varsakyayla Formation, as a few grains. Varsakyayla Formation. Th e marine transgression is Th e clastic parts of the Varsakyayla Formation are also well documented by presence of reef limestones well correlated with the Maden member (Başçeşme containing rich marine fossils, such as coral reefs, Formation). However, the diversity of species benthic foraminifera and echinoderms. obtained from the Varsakyayla Formation is less than

352 E. TOKER ET AL. 43 34 2 1 11 1 2 1 1 23 72 2 2 921 1 29 24 12 15 18 25 14 18 10 7 17 7 1 1 1 2 1 2 1 3 1 1 Montane Unknown Shallow - marine Shallow Lowland - Riparian Lowland Lowland - Riparian Lowland Lowland - Riparian Lowland Lowland - Riparian Lowland Swamp - Freshwater Swamp Palaeovegetation Types Sample numbers

04/YC01 04/YC02 )32 )115 )1 )65 Eucomminia ) ) ) ) ) ) ) ) ) ) ) ) haploxylon type) Montane 11 4 Rhus )Unknown 1 Osmunda ) Carya Engelhardia Engelhardia Myrica Myrica Ulmus Salix/Platanus Olea, Fraxinus, Ligustrum Fraxinus, Olea, Quercus Quercus Castanea,Castanopsis,Lithocarpus,Pasania Castanea,Castanopsis,Lithocarpus,Pasania Quercus Pinus Pinus Cissus )Mangrove22 Pelliciera Trigonabalanus (?Fagaceae, ?Eucommiaceae: ? ?Eucommiaceae: (?Fagaceae, (Fagaceae: (Fagaceae: (Fagaceae: (Saliaceae: ( (Sapotaceae) - Riparian Lowland 1 (Ulmaceae: (Nyssaceae) (Icacinaceae) (?Fabaceae, ?Rosaceae, ?Anacardiaceae) (?Fabaceae, (Tiliaceae) (Cupuliferae) (Juglandaceae: ? (Juglandaceae: (Oleaceae) (Juglandaceae: (Juglandaceae: (Juglandaceae: (Juglandaceae: (Oleaceae: (Juglandaceae) (Juglandaceae) (Cyrillaceae) (Myricaceae) (Cyrillaceae) (Myricaceae: (Myricaceae: (Fagaceae: (Fagaceae: (Fagaceae: (Fagaceae: ( ) ?Palmae (?Arecoideae, (Myricaceae: Back - Mangrove 1 (Anacardiaceae: (Anacardiaceae: (Pinaceae: (Fagaceae: (Fagaceae: (Osmundaceae: (Osmundaceae: (?Fagaceae) (?Fagaceae) (Vitaceae: (Vitaceae: brühlensis brühlensis exactus exactus burghasungensis pusillus pusillus oviformis oviformis fusus ssp. ssp. ssp. ssp. ssp. nanus (Mastixiaceae) pseudolaesus . fallax . fallax . liblarensis . liblarensis oligocaeinus ssp. ssp. ssp. ssp. ssp. typicus ssp. ssp ssp ssp. ssp. ssp. ssp. ssp. agellate cysts agellate sp. rimarius rimarius m sp. p Quantitative counting results of palynomorphs in the Varsakyayla Formation of the Burdur Area. the Burdur of Formation in the Varsakyayla palynomorphs of results counting Quantitative erentiated dinofl erentiated Tricolpopollenites henrici henrici Tricolpopollenites Tricolpopollenites parmulariusTricolpopollenites Tricolpopollenites microhenrici microhenrici Tricolpopollenites Undiff Tricolpopollenites retiformis retiformis Tricolpopollenites Psilatricolporites crassus Tetracolporopollenites obscurus Tetracolporopollenites CEDIS INCERTAE Cleistosphaeridium Cordosphaeridiu Polyporopollenites undulosus undulosus Polyporopollenites Tricolporopollenites kruschiTricolporopollenites Compositoipollenites rhizophorus Tricolporopollenites solé de portai solé Tricolporopollenites Intratriporopollenites indubitalibis Tricolporopollenites villensisTricolporopollenites Subtriporopollenites anulatus anulatus Subtriporopollenites Tricolporopollenites oleoides Tricolporopollenites Momipites punctatus punctatus Momipites Momipites quietus quietus Momipites Tricolporopollenites microreticulatus microreticulatus Tricolporopollenites Plicatopollis plicatus Tricolporopollenites edmundi edmundi Tricolporopollenites Plicatopollis lunatus Triatriopollenites excelsus Triatriopollenites Tricolporopollenites megaexactusTricolporopollenites Triatriopollenites bituitus Triatriopollenites Tricolporopollenites cingulumTricolporopollenites Tricolporopollenites marcodurensis marcodurensis Tricolporopollenites Tricolporopollenites megaexactusTricolporopollenites Tricolporopollenites cingulumTricolporopollenites Tricolporopollenites cingulumTricolporopollenites ANGIOSPERMOUS ANGIOSPERMOUS MONOCOTYLEDONEAE brandenburgensis Arecipites DICOTYLEDONEAE rurensis Triatriopollenites Tricolporopollenites pseudocingulum Tricolporopollenites Pityosporites microalatus microalatus Pityosporites GYMNOSPERMOUS GYMNOSPERMOUS Tricolporopollenites asper Tricolporopollenites Tricolpopollenites liblarensisTricolpopollenites Baculatisporites Tricolpopollenites liblarensisTricolpopollenites TAXA SPORE Leiotriletes triangulus Total 175 163 Table 5. Table

353 MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

in the Maden member (see Akkiraz et al. 2006 for the lithofacies were defi ned, based on type of individual whole assemblage). beds, grain size, and sedimentary structures (Table Foraminifera Contents – In this study, thirty-seven 7). Measured sections were logged in three diff erent samples suitable for analysis of benthic foraminifera places: two from southeast of İncesu, while a third in the Varsakyayla Formation contained: Nummulites was logged east of Karakaya Tepe and the last section fabianii Prever, Peneroplis sp., Peneropliidae, was logged from the northeastern part of Kızıldere Halkyardia minima, Mississippina sp., Textularia north of Gönen (Figures 12–14). Th e lithofacies sp., Planorbulina sp., Linderina? sp., Discorbiidae, diversity was grouped into main four main facies Ditrupa sp., Halkyardia minima Liebus, Eorupertia associations, FA7 to FA10 (Table 7). magna Le Calvez, and Sphaerogypsina globolus Major Channel Deposits (FA7): Description – Th e (Table 6; Figure 11). Haurinidae and Rotaliidae major channel facies association (FA7) is characterized occur rarely in samples. Also, Nummulites fabianii by the relative abundance of facies F1, F2, F3, F4, F5 (nummulitids) primarily occur in samples 04YC/32– and F6 (Table 8; Figure 12). It is dominated by pebble 04YC/36, 04YC/24–04YC/25, 04YC/13–04YC/22 to cobble grain size conglomerates intercalated with and 04YC/37–04YC/39 (Figure 11). In this study pebbly sandstones. Conglomerates are generally no orthophraminids have been identifi ed in any of thick-bedded to massive, very poorly sorted, sandy the sections. Small benthic foraminifera (miliolids), silt matrix-supported, well-rounded, erosively based fragments of bivalves and corals were also observed. and amalgamated (Figure 12). Pebbly sandstones are Th e abundance of nummulitids suggests an inner poorly sorted and pebbles and granules are dispersed and middle shelf environment, deposited during late in a matrix of sand (facies F4). Scours and load casts Middle Bartonian–Priabonian (SBZ 18-20). at the bottom of the bed are common sedimentary structures (Table 7). However, disorganized and Samples between 04YC/06 and 04YC/12 have a stratifi ed sandstones were also observed in the FA7 reef character, and do not include Nummulites and facies associations (Figure 12). Discocyclina, because these kinds of shallow marine environments are not their optimal living conditions. Interpretation – Th e FA7 facies assemblages, Samples between 04YC/29 and 04YC/31 indicate composed of conglomerate and sandstone, represent a shelf lacustrine environment. Samples 04YC/32– long distance transport by high concentration 04YC/36 and 04YC/25–04YC/27 indicate a deeper turbidity currents or debris fl ows and fi nal rapid marine carbonate shelf environment. Sample 04YC/24 sedimentation of all grains (Stanley & Kelling 1978; indicates a reef environment. Samples between Nemec et al. 1980). Gravels may slide into place on 04YC/06 and 04YC/11 indicate a shelf environment, liquefi ed mud. Some muddy gravel occurrences while samples between 04YC/12 and 04YC/23 could have formed from thorough mixing of gravel suggest a deeper shelf environment. Sample 04YC/21 and mud aft er sliding down a steep slope (Crowell indicates a shallow marine environment. Samples 1957). Stratifi ed sandstones are represented by between 04YC/37 and 04YC/39 suggest a carbonate deposits from traction bed loads or traction carpets shelf environment (Figure 11). Anomaliniidae, at the base of a high-concentration turbidity current Discorbiidae, Peneropliidae, Textulariidae and (Hendry 1973, 1978; Mutti & Ricci-Lucci 1975; Hein Valvuliniidae were also described from the samples 1982; Hein & Walker 1982; Lowe 1982; Surlyk 1984). (Table 6). Disorganized sandstones were deposited by rapid sedimentation from a high-concentration turbidity current by consolidating a dense cohesionless Kayıköy Formation suspension and/or post-depositional liquefaction Th e Kayıköy Formation is well-exposed around to destroy any previously formed sedimentary Gönen and Atabey towns and İncesu village (Figure structures. Grain fl ow processes on steep slopes could 7). Four outcrop sections were logged through the form disorganized sands (Piper 1978; Lowe 1982). Kayıköy Formation to document its lithological Proximal (Upper) Fan Deposits (FA8): Description characteristics (Figures 12, 13 & 14a, b). Nine – Th e proximal (upper) fan facies association (FA8)

354 E. TOKER ET AL.

sp.

Age

sp.

Epoch

sp.

Period

sp.

Foraminifera

sp.

? sp.

Formation

sp.

Burdur Area

Sample

Anomalina

Mississippina

Asterigerina

Peneroplis

Pyrgo .

Heterostegina Planorbulina

Amphistegina

Nummulites

Eupertia magna

Nummulites fabianii

Pararotalia .

Rotaliidae

Ethelia

Eponides

Operculina .

Halkyardia minima Halkyardia

Sphaerogypsina globulus Sphaerogypsina

Quinqueloculina Linderina

Textulariidae

Peneropliidae Haueriniidae

Gypsina

Valvuliniidae

Discorbiidae

Anomaliniidae

Textularia 04YC/39 04YC/38 04YC/37 04YC/23 04YC/22 04YC/20 04YC/19 04YC/18 04YC/17 04YC/16 04YC/15 04YC/14 04YC/13 04YC/12 04YC/11 04YC/10 04YC/09

Priabonian 04YC/08

EOCENE 04YC/07 PALEOGENE 04YC/06 04YC/27 gure 5 for sample location. sample 5 for gure LATE 04YC/26

Varsakyayla 04YC/25 04YC/24 04YC/36 04YC/35 04YC/34 04YC/33 04YC/32 04YC/31 04YC/30 04YC/29

MIDDLE

Bartonian 04YC/02K 04YC/01K Not to scale

exactus brühlensis

nanus

oviformis fusus pusillus

ssp. ssp.

pseudolaesus

ssp. ssp. ssp.

ssp.

typicus

ssp. ssp.

ssp.

oreticulatus

codurensis

ensisensis liblarensis fallax

ohenrici

hizophorus

Palynomorhps

ensis

sp.

etiformis

oalatus

ghasungensis

opollenites obscurus

opollenites indubitalibis

opollenites anulatus

burghasungensis

opollenites pseudocingulum opollenites cingulum opollenites cingulum opollenites cingulum opollenites mar

opollenites megaexactus opollenites megaexactus opollenites edmundi opollenites micr opollenites villensis opollenites oleoides

opollenites undulosus

ssp.

Tricolporopollenites solé de portai Tricolporopollenites kruschi Tricolporopollenites Psilatricolporites crassus Tetracolpor Cleistosphaeridium Cordosphaeridium dinoflagellate cysts Undifferentiated

Arecipites bur Arecipites Leiotriletes triangulus Pityosporites micr rur Triatriopollenites bituitus Triatripollenites excelsus Triatripollebites Plicatopollis lunatus Plicatopollis plicatus Momipites punctatus Momipites quietus Subtripor Intratripor Compositoipollenites r Polypor r Tricolpopollenites micr Tricolpopollenites parmularius Tricolpopollenites henrici Tricolpopollenites liblar Tricolpopollenites liblar Tricolpopollenites asper Tricolpopollenites Tricolpor Tricolpor Tricolpor Tricolpor Tricolpor Tricolpor Tricolpor Tricolpor Tricolpor Tricolpor Tricolpor

Baculatisporis primarius ssp. oligacaenicus

sp.

dia minima

Epoch Age

Period

Foraminifera

Formation

Sample

Burdur Area

Asterigerina

Eorupertia

Nummulites

Eorupertia magna

Pararotalia .

Operculina .

Nummulites fabianii

Rotaliidae

Halkyar

Textulariidae

Quinqueloculina

Haueriniidae

Textularia 04YC/05 Occurrence of palynomorphs and benthic foraminifera in the Varsakyayla Formation. See fi Formation. in the Varsakyayla foraminifera benthic and palynomorphs Occurrence of 04YC/04 04YC/03 04YC/02

EOCENE

Priabonian

Varsakyayla 04YC/01

PALEOGENE

Table 6. Table not to scale

355 MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

Structures Age Fm. Color Local Lithology Structures L.B.S. bedding Age Fm. Color Local Lithology m L.B.S. bedding 60 1 1 F1 F1 m 1 1 F6 120 1 1 F6 F1 1 1 1 55 1 1 F4 4 F6 1 4 115 1 4 03/06G 1 1 1 t F1 1 F1 1 4 50 1 4 F5 1 1 110 F1 1 1 F1 F1 45 1

M a j o r c h a n n e l f a c i e s (F 1 F6 105 1 1 1 1 1 F1 M a j o r c h a n n e l f a c i e s (F 40 1 1 1 F1 1 100 1 1 F1 11 1 1 F6 1 1 35 F6 1 1 95 1 F1 1 1 1 1 F1 1 30 F1 1 F1 1 90 1

KAYIKÖY

KAYIKÖY 1 1 F1 1 F1

MIDDLE EOCENE MIDDLE EOCENE 1 25 1 1 1 F4 85 1 1 F1

A-7) 1 20 F1 1 F2 80

1 A-7)

15 F6 1 1 75 F2 1

03/10G 10 1 1 1 F6 70 1 1 F3 03/11G F6 F1 4 5 1 1 1 65 1 F6 1 1 1 1 F1 7 1 L M F M C G P C B 1 F1 Sand L M F M C G P C B Sand

Figure 12. Measured section of the Kayıköy Formation in the northeastern part of Kızıl Dere, north of Gönen Town. is characterized by lithofacies F1, F2, F3, F5, F6 and disorganized conglomerates and medium- to coarse- F9 (Table 8 and Figure 13). It consists of massive, grained sandstones. Conglomerates are badly sorted pebble to cobble grain size conglomerates, bedded, but fi ne upwards, with well-rounded clasts, sharp

356 E. TOKER ET AL.

Structures Structures Structures LITHOLOGY LITHOLOGY

Fm.

Age

Color Color LITHOLOGY

Fm.

Age

Local Bed.

Color

L.B.S.

Local Bed. 4 F2 L.B.S. m 4 F2 4 F5 m 1 350 4 F5 m 1 255 1 4 F2 125 4 F6 4 F1 4 F5 6 F6 250 6 345 120 8 5 F6 4 F6 6 4 F2 1 F2 4 F1 245 6 340 8 F6 115 F5 4 F5 6 F6 4 4 Medial fan lobe facies (F 240 6 F6 335 4

4 F2 5 F5 Medial fan depositional lobe facies (F 110 4 F6 8 6 4 F5 4 F2 F5 8 235 330 8 F2 6 F2 105 6 5 8 F6 6 F5 5 F1 F2 1 F2 4 F3 230 6 325 6 1 F6 100 4 F6 6 F5 1 F2 8 F3 1 F6 225 320 4 1 F6 95 4 4 5 F5 4 F6 1 220 6 F5 5 F3 1 F6 315 5 8 6 F5 F6

90 r o x i m a l ( Upper ) F a n (F P 8 F2 A9) 5 F5

8 215 310 5 F6 8 F5 85 8 F6 1 F6 KAYIKÖY 5 F5 1 8 F6

F3 MIDDLE EOCENE 1 210 5 5 F1 305 F5 80 8 F5 8 5 F2 6 F6 6 F6 5 F5 205 6 300 3 F9 8 F6 5 F6 75 6 F2 6 1 F2 5 200 F5 295 1 1 70 8 F6 KAYIKÖY 6 1 F2

KAYIKÖY F5 4 MIDDLE EOCENE F3 195 1 MIDDLE EOCENE 1 290 F5 65 4 F2 4 8 F2 A9) 6 F1 1 190 285 F2 4 60 4 F6 F1

F5 Medial fan channeled facies (F 6 185 280 1 F5 5 F3 55 1 F1 8 A8) 6 F6 F5 F6 3 180 6 275 F2 6 1 50 4 4 F6 4 5 1 8 F1 6 175 4 270 8 F6 45 1 4 F1 1 F6 1 F5 F1 170 1 265 1 F6 40 4 F1 4 8 F6 165 F6 5 F6 260 1 F2 8 5 35 5 F1 F6 F1 8 F6 A9) 1 8 8 8 F5 1 F5 8 160 8 F1 1 4 L M F M C G P C B 30 8 F5 4 F5 Sand 4 F2 4 155 4 EXPLANATIONS 8 F6 4 F2

25 8 Medial fan lobe facies (F 8 erosive 8 F6 1 coarse conglomerate 8 F5 gradational F6 150 8 fine conglomerate sharp 8 F6 20 4 F5 massive bedding 8 coarse sandstone flat bedding 8 4 F6 8 145 8 F1 4 F2 medium sandstone coarsening upward 15 8 4 F6 mudstone fining upward 8 140 F6 covered 10 1 grey benthic foraminifera 3 greyish green 135 4 F1 4 8 F1 bioclast greyish red

A9) 5 4 F2 5 4 channel fill yellow F6 8 F6 fractured 6 yellowish red F2 130 8 9 8 F6 4 hematite concretions 8 brown L M F M C G P C B L M F M C G P C B Sand Sand load cast 9 green amalgamation

Figure 13. Measured section of the Kayıköy Formation east of Karakaya Tepe.

357 MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

Table 7. Description and environmental interpretation for the lithofacies in the Kayıköy Formation.

Facies Description Interpretation

granule to cobble size clasts, very poorly-sorted, well-rounded clasts, sandy, silty subaqueous debris fl ow, long F1, disorganized matrix-supported, locally sandstone lenses, non-stratifi ed bedded, fl at basement distance conglomerates and irregular top surface, hematite concretions, grey coloured; dimensions: bed transport by high thickness up to 6 m; lateral extent: less than fi ve metres; intercalated with Sm concentration

rapid deposition from granule to cobble size clasts, very poorly-sorted, well-rounded clasts, clast- to turbulent F2, poorly sorted gravel matrix-supported with a coarse-grained sandy matrix, locally iregular clusters of hyperconcentrated fl ows and with cobble to boulder size clasts, erosive base, locally normal graded, green-brown coarser gravel clusters coloured; dimensions: bed thickness up to 4 m; laterally extent: few tens of metres; gravel clusters; refl ect intercalated with facies F5 hydraulic lateral grain size segregation granule to pebble size clasts, normally graded clast-supported by medium- to F3, normal graded coarse-grained sand, sandy matrix, moderately to poorly sorted, well-rounded clasts, deposition by waning gravels locally erosive basement, commonly fi ning upward, greyish coloured; dimensions: high-density turbidity fl ows bed thickness up to 1 m; lateral extent: few tens of metres; intercalated with facies

long-distance transport by medium- to coarse-grained sandstone, pebbly, massive bedded, poorly sorted, fl at high concentration turbidity F4, disorganized pebbly based and irregular upper surface common structures are scours and load casts at current; sandstones the bottom of bed, greyish rapid collective grain coloured; dimensions: bed thickness up to 2 m; lateral extent: less than ten metres deposition of a pebble-sand

medium- to coarse-grained sandstone with sharp fl at undulose or loaded base, rapid deposition from high F5, disorganized gravel lenses in some part bioclasts, bioturbated, amalgamated, greyish, yellowish concentration turbidity sandstones red coloured; dimensions: bed thickness up to 70 cm; lateral extent: few metres; current intercalated with facies F2, F6

medium- to coarse-grained sandstone, moderately cemented, matrix-supported, traction bed load of high parallel stratifi ed, locally normal to inverse graded, locally gravel lenses, benthic F6, stratifi ed sandstones concentration turbidity foraminifera fragments, greyish coloured, dimensions; bed thickness up to 2 m, current laterally extent few metres, intercalated with facies F5

medium-grained sandstone-mudstone couplets, medium -thick- bedded, well- F7, thick bedded developed normal graded, sand/mud ratio is high, generally sharp base, contact, deposition by high- sandstone-mudstone locally erosive base, partly sandstone lenses visible in mudstone, pervasive Tabc concentration turbidity couplets Bouma divisions are present, load structures in sandstones and parallel laminations, current amalgamations, yellowish coloured, sand; lateral extent: few metres

medium-grained sandstone-mudstone couplets, medium-thick-bedded, well-sorted, well-developed normal graded, sand/mud ratio is low, generally sharp base, contact, F8, thin bedded locally erosive base, partly sandstone lenses visible in mudstone, pervasive Tabc deposition by low-density sandstone-mudstone Bouma divisions are present, load structures in sandstones and parallel laminations, turbidity currents couplets amalgamations, yellowish coloured; lateral extent: few metres

mudstone, fl at bedded partly massive, sharp base and upper surface, parallel deposited suspension of low- F9, mudstone/shale lamination on top, fractured, burrows, grey coloured; dimensions: bed thickness up density turbidity to 2 m; lateral extent: tens of metres; intercalated with facies currents bases, contain benthic shell fragments and are Interpretation – Th e massive, disorganized intercalated with sandstones (facies F1) (Figure 13). conglomerates of the Kayıköy Formation are Th e sandstones are poorly-sorted, fl at based and considered to be debris fl ow deposits in the proximal bioturbated. Most of them have scoured surfaces, and (upper) fan (FA8), associated thin alternating sand bed amalgamation is present (Figure 13). and mud deposits that can be interpreted as overbank

358 E. TOKER ET AL.

deposits. Similar disorganized conglomerates can be 1982; Surlyk 1984). Th e base-missing sandstone interpreted as relating to deposition within either the beds (Tb, Tbc) are interpreted as the deposits proximal (upper) fan or proximal parts of the medial of low-concentration turbidity currents (Lowe fan distributary channels (Table 7; Figure 13). All 1982). Th e medial fan depositional lobes occur as these coarse clastics represent high-concentration, thickening-upward and thinning-upward sequences turbidity currents (Mutti & Ricci-Lucci 1975). which correspond to lobe progradation and lobe Medial Fan Deposits (FA9): Description – Th e abandonment, respectively. medial fan facies association (FA9) includes the F1, Distal Fan Deposits (FA10): Description – Th e F2, F3, F5 and F6 facies varieties (Table 7, Figure 13). distal fan association (FA10) includes facies F1, Medial fan deposits were observed as two diff erent F6, F7, F8 and F9 (Table 8; Figure 14a, b) and is facies, namely the medial fan channel facies and dominated by moderately thick, massive mudstone medial fan depositional lobe facies. Th e medial fan with thin (0.5–5 cm), fi ne-grained sandstones channel facies is characterized by massive poorly- which are massive, or exhibit Bouma Td/e sequences sorted conglomerates, with well-rounded clasts, sharp characteristic of this facies. Th e sandstone beds show bases and locally irregular tops, hematite concretions typical base-missing Bouma sequences, such as Td/e, and bioclasts (Figure 13). Th e depositional lobe Tb-e, Tb/e. Th e sandstone/mud ratio is less than 1. Th e facies is composed of medium- to coarse-grained, lower contacts of sandstone beds are sharp, whereas thick-bedded, parallel stratifi ed, non-channelized, the upper contact of the same beds is gradational thickening-upward sandstones with load casts, with overlying mud beds (Figure 14b). (facies F5 and F6; Figure 13). Th ese thick-bedded Interpretation – Th e distal fan facies association sandstones are characterized by classical Bouma (FA10) comprises thin and fi ne turbidites (facies sequences but complete Bouma sequences are absent. F8 and facies F9) and mud interbedded with base-

Most of the beds consists of Ta-c Bouma sequences, missing sandstone beds. Th ey were probably whereas the Tb, Tab, Tbc/e divisions are less commonly deposited by low-concentration turbulent fl ows far observed. Th e sand/mud ratio of these deposits is from channel sources (Bouma 1962, 1964; Stow et al. very high and bed amalgamation is typical. 1996; Einsele 2000). Interpretation – Th e middle fan association (FA9) Formanifera Contents – Th e Kayıköy Formation is also a combination of channel-fi ll deposits (facies is characterized by a lack of fossil content and only F1), interchannel deposits (facies F2, F3, F4) and yielded a few fossil samples, such as Nummulites overbank deposits (facies F6 and F9). Th e sandstones, sp., Assilina sp., Discocyclina sp., Rotaliidae and with sharp, scoured to fl at bases, normal grading and Nodosariidae (Plate 3). Some samples also contain parallel laminated tops, suggest deposition from planktonic foraminifera, such as Globigerina sp., traction bed loads or traction carpets at the base and Globigerinidae. Th is formation is repesented by of a high- concentration turbidity current (Hendry fl ysch deposits containing planktonic foraminifera 1973, 1978; Hein 1982; Hein & Walker 1982; Lowe and thin-bedded mudstone-sandstone alternations.

Table 8. Facies associations of the Kayıköy Formation.

Facies Associations Constituent Lithofacies

FA7, major channel facies associations F1, F2, F3, F4, F5, F6

FA8, proximal (upper) fan facies association F1, F2, F3, F5, F6, F9

FA9, medial (middle) fan facies association (channeled and depositional lobes) F1, F2, F3, F5, F6

FA10, distal fan/basin plain facies association F1, F6, F7, F8, F9

359 MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

Structures a b LITHOLOGY Structures

Fm.

Age

Loc. Bed.

Color L.B.S. Local

Fm. m Age LITHOLOGY Color L.B.S. bedding 130 1 m 4

Medial fan (F 1 F9 F7 1 125 1 1 1 1 120 1

A-9) 1 3,5 1 1 1 1 1

F7 Distal Fan /Basin plain 115 1 1 1 F9 1 1 1 F6 1 F8 1 110 1 1 F9 1 1 1 3 F6 1 6 4 F6 F9 105 1 1 5 4 F6 Distal Fan /Basin plain F6 1 100 1 5 4 F8 1 1 2,5 1 95 4 4 4 5 1

F9 (FA-10) “flysch” 90 1

85 2

4 F6 KAYIKÖY 1 1 5 5 MIDDLE EOCENE 7 5 7 80 1 F9 1 F9 7

fyc”(FA-10) “flysch” F 7 75 5 F5 5 6 F9 5 1,5 5 F6

KAYIKÖY 6 70 MIDDLE EOCENE 4 4 1 1 4 1 8 4 5 65 1 5 F8 1 1 1 1 F9 1 1 F8 60 5 1 1 1 1 1 F9 1 F9 8 55 1

0,5 50

1 F9 1 F9

45 4 F7

5 Distal Fan /Basin plain 4 40 1 L M F M C G P C B 1 Sand 5 1 F8 5 EXPLANATIONS 5 35 5 5 F8 medium conglomerate fractured 1 F9 1 F6 5 F9 fine conglomerate hematite concretions 30 5 F6 plant debris 1 coarse sandstone 4 1 laminated 25 4 F9 5 F6 medium sandstone 1 F9 load cast 1 fine sandstone 20 1 F6 bioclast 1 (FA-10) “flysch” 1 mudstone bioturbation 4 F9 1 F8 15 1 trace fossil 4 coal 4 F1 4 burrow F7 covered 10 1 F1 erosive 1 F6 1 1 F8 grey gradational 1 1 sharp 1 F9 4 greyish red 5 massive bedding 1 F1 1 5 yellow flat bedding 1 F6 6 yellowish red 1 fining (thinning)upward L M F M C G P C B red Sand 7 coarsening (thickening) 8 brown upward

Figure 14. (a) Measured section of the İncesu Formation near the Oluk Çeşme southeast of İncesu village, (b) Measured section of the Kayıköy Formation northeast of İncesu. See Figure 7 for location.

360 E. TOKER ET AL.

Depositional Systems facies analysis and palaeontological data is very useful Th e collected data, comprising a preliminary facies in order to understand the palaeoenvironmental analysis of the Middle–Late Eocene terrigenous history of this basin. Th e basal part of the Eocene deposits in this basin is composed of transgressive sequences of the Başçeşme, Varsakyayla and Kayıköy units. Th is transgressive sedimentation started with formations, and tectonic structures which have the Dazlak member (FA1) (Başçeşme Formation) progressively aff ected these transgressive deposits, let while the prograding fan delta and shelf deposits are us establish a palaeoenvironmental model. Figures represented by the Maden (FA2) and Asar members 15–17 schematically illustrate the depositional (FA3) (Başçeşme Formation). Th e Dazlak member, system in the Başçeşme, Varsakyayla and Kayıköy deposited mostly by debris fl ow processes of alluvial formations, based on the data presented so far. Th e fan deposits, consists of a thick unfossiliferous deepening trends of these units and correlation of the polygenetic conglomeratic succession. Fan deltaic sections, based on facies relations and fossil contents, sandstone-mudstones intercalated with coal seams can be shown in block diagrams. (Maden member) grade up into shallower marine Th e Çardak-Dazkırı area was aff ected by post- sandstones and reef limestones (Asar member) in the orogenic tectonic processes (Koçyiğit 1984; Göktaş et Bartonian–Priabonian. In the upper part of the Asar al. 1989; Sözbilir 2005). Th erefore, providing detailed Member the foraminifera Fabiania cassis, Eorupertia

alluvial fan Lycian Nappes (debris flow) fan delta (delta front) FA1 shelf (reef) FA2

FA3

Figure 15. Schematic block diagram of the alluvial fan to shelf setting, showing generalized subenvironments and their respective lithofacies in the Başçeşme Formation during the Eocene.

361 MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

Lycian Nappes fluvial environment FA4 (flood plain, channel fill deposits)

fan delta

Flood plain (fan delta front- fan delta slope)

shelf environment (back reef) bed load deposit FA5 FA6

Figure 16. Schematic block diagram of the fl uvial to shelf setting, showing generalized subenvironments and their respective lithofacies in the Varsakyayla Formation during the Eocene. magna, Halkyardia minima, Sphaerogypsina globulus Bartonian–Early Priabonian. A benthic foraminifer Asterigerina rotula, Quinqueloculina sp., Asterigerina assemblage, Nummulites fabianii Prever, Peneroplis sp., Discocyclina sp., Cibicides sp., Heterostegina sp., sp., Peneropliidae, Halkyardia minima, Mississippina Eponides sp., Amphistegina sp., Alveolina sp., Assilina sp., Textularia sp., Planorbulina sp., Linderina? sp., sp., Halkardia sp., Nummulites sp., Operculina sp., Discorbiidae, Ditrupa sp., Halkyardia minima Liebus, Praebulalveolina sp., Eorupertia sp., Fabiania sp., Eorupertia magna Le Calvez, and Sphaerogypsina Neoalveolina sp., Halkyardia sp., Anomalina sp., globolus from the uppermost part of the sequence Mississippina sp., Pararotalia sp., Pyrgo sp., Rotalia records an inner and middle shelf environment. sp., Sakesaria sp. and Orbitolites sp., indicate an inner In the eastern part of the study area in the to middle shelf environment. Isparta region, marine conglomerate, sandstone and Th e other Eocene outcrop located in the Burdur mudstone (Kayıköy Formation) was deposited in a area is a transgressive deposit starting with the fl ysch-like unstable basin. Major channel facies (FA7) Varsakyayla Formation. Th e basal part of the changes to the lateral and medial fan association Varsakyayla Formation is composed mainly of (channel and depositonal lobe facies) (FA9) and distal sandstones with trough and planar cross-bedding and ripple lamination and mudstones with plant fan (thin-bedded sandstone-mudstone alternations) debris. Th ese unfossiliferous clastic deposits association (FA10). Fossils from the Kayıköy represent a fl uvial environment (FA4) and change up- Formation indicate a depositional environment section to fi ne-grained fan-deltaic (FA5) and shallow in which the benthic foraminifera, Nummulites marine (FA6) sediments containing small benthic sp., Assilina sp., Discocyclina sp., Rotaliidae and foraminifera, coral reefs and echinoderms in the late Nodosariidae are rarely found, although planktons

362 E. TOKER ET AL.

alluvial fan Lycian Nappes (debris flow) fan delta (delta front) FA1 shelf (reef) FA2

FA3

Lycian Nappes fluvial environment FA4 (flood plain, channel fill deposits)

fan delta flood plain (fan delta front- fan delta slope)

shelf environment (back reef) bed load deposit FA5 FA6

Figure 17. Schematic block diagram of the marine setting, showing generalized subenvironments and their respective lithofacies in the Kayıköy Formation during the Eocene.

363 MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

like Globigerina sp., and Globigerinidae are frequently • Coaly seams of the Başçeşme and Varsakyayla present in these transgressive deposits. formations were deposited during the Middle– In the study areas, Bartonian–Priabonian ?Late Eocene, as indicated by the presence of deepening trends may result from global sea level stratigraphically important species such as changes, as well as post-orogenic tectonic movements. Aglaoreidia cyclops, Triatriopollenites excelsus, During the Middle–Late Eocene, the transgressive Subtriporopollenites anulatus ssp. nanus, sedimentation in these basins caused by rising Subtriporopollenites constans, Plicatopollis sea level can be linked to global warming eff ects. lunatus, Compositoipollenites rhizophorus Th is climatic change is detected by palynofl oral ssp. burghasungensis and Nowemprojectus features. Th e mangrove species Psilatricolporites tumanganicus. crassus (Pelliciera) occurs in the palynofl ora of the • Palaeoclimatically, the mixture of temperate Varsakyayla Formation and this indicates warm climatic conditions, as the mangroves need a tropical and tropical taxa indicates that from the coastal and humid climate to develop (Frederiksen 1985; to montane environments prevailed during the Westgate & Gee 1990). In addition only planktonic Middle–Late Eocene. Th e presence of warm foraminiferal fauna was found in the Kayıköy Tethys waters permitted growth of mangroves in Formation. western Anatolia at this time. • Benthic foraminiferal fauna such as Nummulites Conclusions fabianii (nummulitids), deposited in an inner- middle shelf environment, indicates a Late Th is paper presents a new aspect of the interpretation Bartonian–Priabonian age in the Varsakyayla of the Middle–Late Eocene sedimentary evolution Formation. However, the orthophragmines (with of the Başçeşme, Varsakyayla and Kayıköy formations. Th ree Eocene formations in SW Turkey: genera Discocyclina) indicate a Priabonian age the Başçeşme Formation (north of Acıgöl), the and deposition on a distal shelf. Th e Kayıköy Varsakyayla Formation (north of Lake Burdur) and Formation is characterized by Globigerina the Kayıköy Formation (north of Isparta) were all sp. and Globigerinidae planktic foraminifera, investigated sedimentologically, palynologically and indicative of a marine environment. Th e variation palaeontologically. of the depositional environment is interpreted as a result of the sea level changes in the western Taurides. • Detailed observations showed that within the Başçeşme, Varsakyayla and Kayıköy formations are thirty-three lithofacies, which can be grouped Acknowledgements into ten facies associations. Th e fi rst depositional setting is represented by the alluvial fan, fan-delta We thank Dr. André Poisson for his helpful and shallow marine settings in the Başçeşme constructive remarks for the revision of the Formation, which can be well correlated with manuscript and improvement of the English. Th e the middle and upper part of the Varsakyayla authors thank Ercan Özcan, Ali Aydın, Ömer Elitok Formation. Th e Kayıköy Formation is dominantly and two anonymous reviewers for their invaluable characterized by fl ysch-type sandstone-mudstone criticisms and comments that improved an early alternations. version of the paper.

References

Akgün, F. & Sözbİlİr, H. 2001. A palynostratigraphic approach Akgün, F. 2002. Stratigraphic and palaeoenvironmental signifi cance to the SW Anatolian molasse basin: Kale-Tavas molasse and of Eocene palynomorphs of the Çorum-Amasya area in the Denizli molasse. Geodinamica Acta 14, 71– 93. central Anatolia, Turkey. Acta Palaeontologica Sinica 41, 576– 591.

364 E. TOKER ET AL.

Akgün, F., Akay, E. & Erdoğan, B. 2002. Tertiary terrestrial to Göktaş, F., Çakmakoğlu, A., Tarı, E., Sütçü, Y.F. & Sarıkaya, H. shallow marine deposition in central Anatolia: a palynological 1989. Çivril-Çardak Arasının Jeolojisi [Geology of Çivril-Çardak approach. Turkish Journal of Earth Sciences 11, 127–160. Area]. Mineral Research and Exploration Institute of Turkey

Akkİraz, M.S. 2008. Palynological Investigations and Foraminifer (MTA) Report no. 8701[in Turkish, unpublished]. Contents of the Eocene–Miocene Deposits in the Çardak–Tokça, Görmüş, M. & Özkul, M. 1995. Stratigraphy of Gönen-Atabey Burdur and İncesu Areas, Western Anatolia. PhD Th esis, Dokuz (Isparta) and Ağlasun (Burdur). Science Institute of Süleyman Eylül Üniversitesi [unpublished]. Demirel University 1, 43–64. Akkİraz, M.S., Akgün, F., Örçen, S., Bruc, A.A. & Mosbrugger, Gutnic, M. 1977. Géologie du Taurus Pisidien au nord d’Isparta V. 2006. Stratigraphic and palaeoenvironmental signifi cance Turquie: Principaux resultats estraits des notes de M.Gutnic of Bartonian–Priabonian (Middle–Late Eocene) microfossils emre 1965 et 1971 par O. Monod, Universite de Paris-sud, from the Başçeşme Formation, Denizli Province, Western Orsay, p.130. Anatolia. Turkish Journal of Earth Science 15, 155–180. Harms, J.C., Southard, J.B. & Walker, R.G. 1982. Structures and Akyol, E. 1980. Etude palynologique de l’Eocene de Bayat (Çorum– Sequences in clastic rocks. Society of Economic Paleontologists Turquie) et essai de correlation entre Karakaya et Emirşah. and Mineralogists Short Course 9, 8–51. Mineral Research and Exploration Institute of Turkey (MTA) Bulletin 91, 39–53. Hein, F. J. 1982. Depositional mechanisms of deep-sea coarse clastic sediments, Cap Enrage Formation, Quebec. Canadian Journal Bassi, D. 2005. Larger foraminiferal and coralline algal facies in of Earth Science 19, 267–287. an Upper Eocene storm-infl uenced, shallow-water carbonate platform (Colli Berici, north-eastern Italy). Palaeogeography, Hein, F.J. & Walker, R.G. 1982. Th e Cambro–Ordovician Cap Palaeoclimatology, Palaeoecology 226, 1–35. Enrage Formation, Quebec, Canada: conglomeratic deposits of a braided submarine channel with terraces. Sedimentology Blair, T.C. 1999. Sedimentology of the debris fl ow dominated 29, 309–329. Warm Spring Canyon alluvial fan, Death Valley, California. Sedimentology 46, 941–965. Hendry, H.E. 1973. Sedimentation of deep marine conglomerates in Lower Ordovician rocks of Quebec – composite bedding Bouma, A. H. 1962. Sedimentology of Some Flysch Deposits. A produced by progressive liquefaction of sediment? Journal of Graphic Approach to Facies Interpretation. Elsevier. Sedimentary Petrology 43, 125–136. Bouma, A.H. 1964. Ancient and Recent Turbidites. Geologie en Hendry, H.E. 1978. Cap des Rosiers Formation at Grosses Roches. Mijnbouw 43, 375–379. Quebec – deposits in the mid-fan region of an Ordovician Bozkurt, E. & Satir, M. 2000. New Rb-Sr geochronology from submarine fan. Canadian Journal of Earth Science 15, 1472– the southern Menderes Massif (southwestern Turkey) and its 1488. tectonic signifi cance. Geological Journal 35, 285–296. Karaman, M.E., Merİç, E. & Tanse, I. 1989. Gönen-Atabey Bozkurt, E. & Oberhänsli, R. 2001. Menderes Massif (western arasındaki bölgenin jeolojisi [Geology of the Gönen-Atabey Turkey): structural, metamorphic and magmatic evolution – a area]. Cumhuriyet Üniversitesi Mühendislik Fakültesi Dergisi synthesis. International Journal of Earth Science 89, 679 –708. Yerbilimleri 6-7, 129–143. Collins, A.S. & Robertson, A.H.F. 1997. Th e Lycian Melange, Kissel, C., Averbuch, O., Lamottle, D., Monod, O. & Allerton, southwest Turkey: an emplaced accretionary complex. Geology S. 1993. First paleomagnetic evidence for a post-Eocene 25, 255–258. clockwise rotation of the western thrust belt east of the Isparta Collins, A.S. & Robertson, A.H.F. 1998. Processes of Late reentrant (SW Turkey). Earth Planetary Science Letters 117, Cretaceous to Late Miocene episodic thrust sheet translation 1–14. in the Lycian Taurides, SW Turkey. Journal of the Geological Koçyİğİt, A. 1984. Güneybatı Türkiye ve yakın dolayında levha içi Society, London 155, 759–772. yeni tektonik gelişim [Intra-plate neotectonic development Collins, A.S. & Robertson, A.H.F. 1999. Evolution of the Lycian in Southwestern Turkey and adjacent areas]. Bulletin of the allochthon, western Turkey, as a north-facing Late Palaeozoic Geological Society of Turkey 27, 1–15. to Mesozoic rift and passive continental margin. Geological Koçyİğİt, A. 2005. Th e Denizli graben-horst system and the eastern Journal 34, 107–138. limit of western Anatolian continental extension: basin fi ll, Crowell, J.C. 1957. Origin of pebbly mudstones. Bulletin of the structure, deformational mode, throw amount and episodic Geological Society of America 68, 993–1010. evolutionary history, SW Turkey. Geodinamica Acta 18, 167– Einsele, G. 2000. Sedimentary Basins: Evolution, Facies and Sediment 208. Budget. Berlin, Springer. Less, Gy., Özcan, E., Papazzoni, C.A. & Stockar, R. 2008. Th e Frederıksen, N.O. 1985. Review of early Tertiary sporomorph middle to Late Eocene evolution of nummulitid foraminifer paleoecology. American Association of Stratigraphic Heterostegina in the Western Tethys. Acta Palaeontologica Palynologists Contributions Series 15, 1–92. Polonica 53, 317–350.

365 MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

Lowe, D.R. 1982. Sediment gravity fl ows, II. Depositional models Poisson, A. 1977. Recherches géologiques dans les Taurides with special reference to the deposits of high density turbidity Occidentales (Turquie). Th ese Doctorate d’Etat, Université currents. Journal of Sedimentary Petrology 52, 279–297. Paris- Sud (Orsay). Miall, A.D. 1978. Tectonic setting and syndepositional deformation Poisson, A., Yağmurlu, F., Bozcu, M. & Şentürk, M. 2003. New of molasse and other nonmarine-paralic sedimentary basins. insights on the tectonic setting and evolution around the apex Canadian Journal of Earth Science 15, 1613–1632. of the Isparta Angle (SW Turkey). Geological Journal 38, 257– Miall, A.D. 1996. Th e Geology of Fluvial Deposits: Sedimentary 282. Facies, Basin Analysis and Petroleum Geology. Springer, New Reineck, H.E. & Singh, I.B. 1975. Depositional Sedimentary York. Environments. Springer Verlag Berlin Heidelberg. Mutti, E. & Ricci-Lucci, F. 1975. Turbidite facies and facies Riegel, W., Bode, T., Hammer, J., Hammer-Schiemann, G., Lenz, associations. Examples of Turbidite facies and associations O. & Wilde, V. 1999. Th e palaeoecology of the Lower and from selected formations of the Northern Appennines. Middle Eocene at Helmstedt, northern Germany – a study in Field trip Guidebook A-11. 9th International Association of contrasts. Acta Palaeobotanica Supplement 2, 349–358. Sedimentologists Congress, 21 –36. Rigsby, C.A. 1994. Deepening-upward sequences in Oligocene Nemec, W. & Steel, R.J. 1984. Alluvial and coastal conglomerates: and Lower Miocene Fan-delta deposits, Western Santa Ynez their signifi cant features and some comments on gravelly Mountains, California. Journal of Sedimentary Research 64, mass-fl ow deposits. In: Koster, E.H. & Steel, R.J. (eds), 380–391. Sedimentology of Gravels and Conglomerates. Canadian Society Satir, M. & Friedrichsen, M.H. 1986. Th e origin and evolution of of Petroleum Geologists Memoir 10, 1–31. the Menderes Massif, W-Turkey. A rubidium/strontium and Nemec, W., Porebski, S.J. & Steel, R.J. 1980. Texture and structure oxygen isotope study. Geologische Rundschau 75, 703–714. of resedimented conglomerates: examples from Ksiaz Formation (Famennian–Tournaisian), southwestern Poland. Şenel, M. 1991. Palaeocene–Eocene sediments interbedded with Sedimentology 7, 519–538. volcanics within the Lycian Nappes: Faralya formation. Mineral Research and Exploration Institute (MTA) of Turkey Nemec, W. & Postma, G. 1993. Quaternary alluvial fans in Bulletin 113, 1–14. southwestern Crete: sedimentation processes and geomorphic evolution. In: Marzo, M. & Puigdefabregas, C. (eds), Şenel, M. 1997. 1/100 000 Ölçekli Türkiye Jeoloji Haritaları Denizli Alluvial Sedimentation. Special Publication of International J10 Paft ası [1/100 000 Scale Geological Map of Turkey, Denizli Association of Sedimentology, 235–276. J10 Sheet]. Mineral Research and Exploration Institute (MTA) of Turkey Bulletin 13, 1–16. Nichols, G.J. & Fisher, J.A. 2007. Processes, facies and architecture of fl uvial distributary system deposits. Sedimentary Geology Şengör, A.M.C. & Yilmaz, Y. 1981. Tethyan evolution of Turkey: a 195, 75–90. plate tectonic approach Tectonophysics 75, 181–241. Özcan, E., Less, Gy., Baldi-Beke, M., Kollányi, K. & Kertész, Sözbİlİr H. 2002. Revised stratigraphy and facies analysis of the B. 2007. Biometric aalysis of Middle and Upper Eocene Palaeocene–Eocene supra-allochthonous sediments and their Discocyclinidae and Orbitoclypeidae (Foraminifera) from tectonic signifi cance (Denizli, SW Turkey). Turkish Journal of Turkey and udated Orthophragmine znation in the Western Earth Sciences 11, 1–27. Tethys. Micropaleontology 52, 485–520. Sözbİlİr, H. 2005. Oligocene–Miocene extension in the Lycian Özer, S., Sözbİlİr, H., Özkar, İ., Toker, V. & Sarı, B. 2001. orogen: evidence from the Lycian molasse basin, SW Turkey. Stratigraphy of Upper Cretaceous–Palaeogene sequences in Geodinamica Acta 18, 255–282. the southern and eastern Menderes Massif (western Turkey). Sözbİlİr, H., Özer, S., Sari, B. & Avşar, N. 2001. Supra-allochthon International Journal of Earth Sciences 89, 852–866. sedimentary succession in western Anatolia: new stratigraphic Özkaya, İ. 1990. Origin of the allochthons in the Lycian belt, data and tectonic results. Abstracts, Fourth International southwest Turkey. Tectonophysics 177, 367–379. Turkish Geology Symposium, p.36. Özkaya, İ. 1991. Evolution of a Tertiary volcanogenic trough in Stanley, D.J. & Kelling, G. 1978. Sedimentation in submarine SW Turkey – the Alakaya basin of the Lycian belt. Geologische canyons, fans and trenches. Dowden, Hutchinson & Ross, Rundschau 80, 657–668. Stroudsburg, Pennsylvania, p. 395. Piper, D.J.W. 1978. Turbidite muds and silts on deep-sea fans Stow, D.A.V., Reading, H.G. & Collison, J.D. 1996. Deep seas. and abyssal plains. In: Stanley, D.J. & Kelling, G. (eds), In: Reading, H.G. (ed), Sedimentary Environments: Processes, Sedimentation Submarine Canyons, Fans and Trenches. Facies and Stratigraphy, 395–453. Dowden, Hutchinson & Ross Inc. Stroundsburg, Pennsylvania, Surlyk, F. 1984. Fan-delta to submarine fan conglomerates of 163–176. the Volgian-Valanginian Wollaston Foreland Group, East Poisson, A. 1976. Essai d’interprétation d’une transversale Greenland. In: Koster, E.H. & Steel, R.J. (eds), Sedimentology Korkuteli-Denizli (Taurus ouest-anatolien-Turkuie). Bulletin gravels and conglomerates. Canadian Society Petroleum of the Geological Society of France 2, 499–509. Geological Memoir 10, 359–382.

366 E. TOKER ET AL.

Toker, E. 2009. Acıgöl-Çardak (Denizli) Grabeninin Kuzeyindeki Westgate, J.W. & Gee, C.T. 1990. Palaeoecology of a Middle Tersiyer Çökellerinin Tektono-sedimanter Gelişiminin Eocene mangrove biota (vertebrates, plants and invertebrates) İncelenmesi [Th e Investigation of Tectono-sedimentary Evolution from southwest Texas. Palaeogeography, Palaeoclimatology, of the Tertiary Deposits in the North of Acıgöl-Çardak (Denizli) Palaeoecology 78, 163–177. Graben Basin]. PhD Th esis. Süleyman Demirel Üniversitesi [in Yağmurlu, F. 1994. Isparta kuzeyinde yeralan Oligosen yaşlı Turkish with English abstract, unpublished]. molas tipi kırıntılı tortulların tektono-sedimenter özellikleri Toker, E., Akkİraz, M.S., Yağmurlu, F., Akgün, F. & Örçe, S. [Tectono-sedimetary characteristics of Oligocene molassic 2009. Facies, Architecture and Palaeoecology of the Middle– clastics sediments in the north of Isparta]. Abstratcs, Çukurova Late Eocene formations outcropping in western Taurides, SW Üniversitesi, 15. Yıl Sempozyumu, 241–252. th Turkey. 27 IAS 2009 Meeting of Sedimentologists, 380–381. Yalçınkaya, S., Engin, A., Taner, K., Afşar, P., Dalkılıç, H. & Toomey, D.F. 1981. European Fossil Reef Models. Society of Economic Özgönül, E. 1986. Batı Torosların Jeolojisi [Geology of Western Paleontologists and Minerologists, Special Publication 30. Taurides]. Mineral Research and Exploration Institute of Turkey (MTA) Report no. 7898 [unpublished]. Tucker, M.E. & Wright, V.P. 1990. Carbonate Sedimentology. Blackwell Scientifi c Publications. Van Hinsbergen, D.J.J., Dekkers, M.J. & Koç, A. 2010. Testing Miocene Remagnetization of Bey Dağları: timing and Amount of Neogene Rotations in SW Turkey. Turkish Journal of Earth Sciences 19, 123–156.

367 MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

PLATE 1

Figure 1. Nummulites fabianii Prever, sample A4 (Başçeşme Formation) Figure 2. Assilina sp., sample A3 (Başçeşme Formation) Figures 3, 4. Discocyclina sp., sample A14 (Başçeşme Formation) Figures 5, 6. Praebullalveolina sp., Figure 5. Sample A6; Figure 6. Sample A15 (Başçeşme Formation) Figures 7–9. Cibicides sp., Figure 7. Sample A1; Figure 8. Sample A18; Figure 9. Sample A15 (Başçeşme Formation)

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369 MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

PLATE 2

Figures 1–3. Nummulites fabianii Prever, Figure 1. Sample 04YC/01; Figures 2, 3. Sample 04YC/14 (Varsakyayla Formation). Figure 4. Eorupertia magna Le Calvez, sample 04YC/01 (Varsakyayla Formation). Figures 5–7. Peneroplis sp., sample 04YC/16 (Varsakyayla Formation). Figures 8, 9. Peneropliidae, sample 04YC/11 (Varsakyayla Formation).

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371 MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

PLATE 3

Figure 1. Nummulites sp., sample 03/10G (Kayıköy Formation). Figure 2. Assilina sp., sample 03/13G (Kayıköy Formation). Figure 3. Discocyclina sp., sample 03/14G (Kayıköy Formation). Figures 4–6. Rotaliidae, Figure 4. Sample 03/13G; Figure 5. Sample 03/11G; Figure 6. Sample 03/06G (Kayıköy Formation). Figure 7. Nodosariidae, sample 03/11G (Kayıköy Formation).

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